The Pleistocene of North America and its vertebrated animals from the states east of the Mississippi River and from the Canadian provinces east of longitude 95° (part 3 of 4)

The Pleistocene of North America and its vertebrated animals from the states east of the Mississippi River and from the Canadian provinces east of longitude 95° (part 3 of 4)

(Map 16.)

1. Wheeling, Ohio County.—The geologist J. W. Foster (Proc. Amer. Assoc. Adv. Sci., 10th meeting, p. 160) reported that Alfred Sears had deposited in the Smithsonian Institution some elephant remains obtained 4.5 miles below Wheeling Creek. They were found on the second bottom or terrace and at a depth of 17 feet from the surface. Within a few feet of this place was an Indian mound. When the mound was built, 17 feet of sediment had accumulated over the elephant remains. One can, however, hardly refer the bones to a time farther back than the Wisconsin. A record in the U. S. National Museum shows that Mr. Sears, in 1852, sent a tusk and a tooth of an elephant to Washington. These were doubtless placed in the collection of the Old National Institute. If they were transferred to the Smithsonian Institution the record has apparently been lost.

NORTH CAROLINA.

(Maps 16, 39.)

1. 16 miles below Newbern, on Neuse River, in Pamlico County.—Harlan, in 1842 (Amer. Jour. Sci., vol. XLIII, p. 143), stated that he had seen, in the collection made by Nuttall on Neuse River, remains of an elephant. Elisha Mitchell, in the same year (Elements of Geol., p. 128), stated that there was in the cabinet of the University of North Carolina a tooth of an elephant from the locality mentioned. Possibly the tooth referred by Croom (Amer. Jour. Sci., vol. XXVII, 1835, p. 170) to the mastodon and which was 7 inches wide and 9.5 inches deep, was really that of an elephant. Were it not for the fact that Elephas primigenius has been found in this region of North Carolina, one might, with confidence, refer the tooth found below Newbern to E. columbi. For other species found at this place the reader may consult pages 358 to 359.

2. Harlowe, Carteret County.—Elisha Mitchell (Amer. Jour. Sci., vol. XIII, 1827, p. 347) stated that in digging the Clubfoot and Harlowe Canal remains of both the mastodon and the elephant had been found. Nothing more definite was communicated. The probability is that the animal was Elephas columbi.

3. Duplin County.—At the meeting of the American Association for the Advancement of Science in Charleston, South Carolina, in 1850, Dr. R. W. Gibbes reported that he had obtained a part of a molar of an elephant found somewhere in Duplin County. He spoke of its resemblance in narrowness and in thinness of plates to a tooth found in Vermont and exhibited by Agassiz. Possibly it belonged to Elephas primigenius.

FLORIDA.

(Map 16.)

1. Wakulla Springs, Wakulla County.—In the collection of the Florida Geological Survey is a right tibia of an elephant reported found at the place named. The measurements shown in the accompanying table were secured. For comparison the dimensions of the tibia of the great Elephas primigenius in the American Museum of Natural History at New York are presented.

Measurement of tibias, in millimeters.

┌─────────────────────────────────────┬───────────────┬───────────────┐ │ │Wakulla Springs│ │ │ │ elephant. │E. primigenius.│ ├─────────────────────────────────────┼───────────────┼───────────────┤ │Total length │ 813│ 735│ │Greatest width across upper end │ 266│ 245│ │Fore-and-aft diameter at middle of │ │ │ │ length │ 106│ 100│ │Side-to-side diameter at middle of │ │ │ │ length │ 132│ 106│ │Greatest width across lower end │ 215│ 205│ └─────────────────────────────────────┴───────────────┴───────────────┘

With the tibia from Wakulla Springs is the distal half of an immense femur of the left side. The distance across the articular surface of the distal end was at least 241 mm., but the bone has suffered some abrasion. The outer articular surface measures 115 mm.; the inner 1,202 mm. When the bone is placed on a table with the hinder face downward the inner ridge which bounds the patellar groove rises 280 mm. above the table. Whether these bones belong to Elephas imperator or to E. columbi is uncertain.

2. Stokes Ferry, St. Mary’s River, Nassau County.—In 1909, Sellards (2d Ann. Rep. Florida Geol. Surv., p. 147) stated that Dr. L. W. Stephenson, of the U. S. Geological Survey, had found at this place, in a phosphate deposit, a fragment of an elephant tooth together with 3 teeth of a fossil horse and some ear-bones of a whale. The elephant belonged probably to E. columbi, but possibly to E. imperator.

3. Bartow, Polk County.—Dr. W. H. Dall (Proc. Acad. Nat. Sci. Phila., 1891, p. 120) has recorded the discovery at this place of tusks supposed to be those of Elephas columbi. Possibly the tusks were those of E. imperator or even those of Mammut americanum.

MISSISSIPPI.

(Map 16.)

1. Natchez, Adams County.—In his report on the Geology and Agriculture of Mississippi, 1854, page 284, Wailles wrote that fossil remains of the elephant were not then known to have been found in the State. However, on page 286, Elephas primigenius is included in the list of fossil Mammalia furnished by Leidy. The latter does not say where in Mississippi elephant remains had been discovered, but it was probably at Natchez.

In his work on the Lafayette formation (12th Ann. Rep. U. S. Geol. Surv., part 1, p. 400), McGee stated that at least one skull of the American elephant had been found at Natchez in gravel, well down toward the Port Hudson clays, and that to this adhered some of the coarse gravel of the matrix. Probably the species was Elephas columbi. It is likely that the skulls referred to by McGee were not as complete as he supposed.

TENNESSEE.

(Map 16. Figure 23.)

1. Gallatin, Sumner County.—In 1835, Professor G. Troost (Trans. Geol. Soc. Penn., vol. I, 1835, p. 144) reported that a Mrs. Ephraim Foster possessed a tooth of Elephas primigenius found in a well at a depth of 40 feet. The identification followed the opinion of that time that only one species of elephant had existed in the country. It more probably belonged to E. columbi.

2. Columbia, Maury County.—In the publication just referred to the geologist G. Troost stated that he owned a tooth of Elephas primigenius, found a few miles below Columbia, probably near Duck River, but no details as to the exact locality and kinds of deposits were furnished. Hayes and Ulrich (Folio 95, U. S. Geol. Surv.) appear not to have recognized any Pleistocene in this quadrangle. On page 6 they stated that narrow strips of bottom lands occur along the larger streams, particularly along Duck River. The tooth was probably that of E. columbi.

KENTUCKY.

(Map 16.)

1. Bigbone Lick, Boone County.—Remains belonging certainly to both Elephas primigenius and E. columbi have been found here, and there is no reason for supposing that any other species has ever been collected. Many specimens have, however, been mentioned in the literature of the subject which one may have difficulty in referring to either of these species. The difficulty arises from the insufficiency of the descriptions and of the illustrations when there are any.

Two elephant molars from America were figured by Cuvier (Oss. Foss., ed. 4, plate XV, figs. 9, 11), without any exact locality being given, so far as the present writer can discover. Adams (Palæontograph. Soc., vol. XXXIII, p. 122) says of these that one was from Mississippi, the other from Bigbone Lick, but which is from the latter place is not indicated. Caspar Wistar (Trans. Amer. Philos. Soc., n. s., vol. I, 1818, p. 376) reported that in the Jefferson collection there were teeth which he referred to the Siberian elephant. Among these were some which belonged to a young animal.

William Cooper (Monthly Amer. Jour. Geol., vol. I, 1831, pp. 168–171) recalled the quantity of elephant remains found at Bigbone Lick before his visit. In the Finnell collection was a tusk with part of the base missing, which was still 11 feet 10.5 inches long and 22 inches in circumference. It was much curved, a fact which induced him to refer it to an elephant. In the same collection were numerous other parts of elephants, including 20 or more teeth. A Mr. Bullock secured a skull nearly entire. It is pretty certain that the greater part of all this fine material has been lost. Many of the bones and teeth collected in early times went to the museums of Europe; some are mentioned by Leith Adams (Palæontograph. Soc., vol. XXXIII, pp. 75, 122) and Lydekker (Cat. Foss. Mamm. Brit. Mus., pt. IV, p. 191).

2. Newport, Campbell County.—In 1871 Professor Shaler (Amer. Naturalist, vol. IV, p. 160) stated that he had a tooth of Elephas primigenius, which had been found in the uppermost terrace of the alluvial plane opposite Cincinnati, at a depth of over 60 feet from the surface.

In 1877 (Geol. Surv. Kentucky, vol. III, p. 79), the same writer stated that a molar tooth of Elephas primigenius had been found in the city of Newport, about 25 feet above high-water mark and at a depth of 40 feet. It is not improbable that the two accounts refer to the same specimen.

3. Bluelick Springs, Nicholas County.—In the collection of Mr. Thomas W. Hunter, made at this place, were several much water-worn teeth of elephants, the species not determined.

4. Eminence, Henry County.—The geologist David D. Owen, in 1857 (3d Geol. Surv. Kentucky, p. 103), reported that bones and teeth of the mammoth had, at times, been found here. They do not appear to have been preserved.

FINDS OF PLEISTOCENE EQUIDÆ IN EASTERN NORTH AMERICA.

MASSACHUSETTS.

(Map 17.)

Gay Head, Martha’s Vineyard.—In 1900 (Bull. Geol. Soc. Amer., vol. XI, p. 459, plate XLII, fig. 2), J. B. Woodworth reported finding an astragalus of a horse in an osseous conglomerate, regarded as belonging to the Miocene. It was identified by Professor H. F. Osborn, who remarked that it resembled closely the same bone of some Pleistocene horses. From this conglomerate have been obtained bones of whales, supposedly also a skull of a walrus. While the size of the astragalus suggests more that of a Pleistocene horse, it is possible that there was some large Miocene equid that lived there. The present writer is inclined to believe it will be found that the astragalus came from one of the older Pleistocene deposits recognized as present at Gay Head.

NEW YORK.

(Map 17.)

1. Throg’s Neck, New York County.—In 1866 (Smithson. Contrib. Knowl., vol. XV, art. 3, p. 16), Charles Whittlesey stated he had a tooth of a horse, taken from the compact marine drift at Throg’s Neck. It was obtained by J. A. Bailey from excavations at Fort Schuyler, 18 feet below the surface.

According to Folio No. 83 of the U. S. Geological Survey, Harlem Quadrangle, Throg’s Neck is occupied by till which usually thinly covers, or leaves exposed, the underlying Hudson schist; Salisbury gives an account of the drift on page 14 of the folio cited. At the depth indicated the tooth was probably lying in pre-Wisconsin deposits; and taking into consideration the geological age of other horse remains, one may reasonably conclude that the tooth at Throg’s Neck was of a horse that lived during the middle or early Pleistocene. That there may be materials of a pre-Wisconsin stage underlying the surface drift at Throg’s Neck is indicated by Woodworth’s discovery (Bull. 48, N. Y. State Mus., p. 626, plate I) of deposits older than the Wisconsin along Hempstead Bay, Long Island.

NOTE.—In 1858 (Proc. Boston Soc. Nat. Hist., vol. VI, p. 303), Dr. Skilton, of Troy, wrote that a farmer had dug up, in what had been marshy ground, 17 teeth of a horse. These, Skilton stated, belonged to Equus major. The teeth were greatly decayed. The writer of the report said that the enamel of the first upper molar, meaning the anterior of the six grinding teeth, measured 1.9 inches (47.5 mm.); that of the corresponding lower teeth 2.33 inches (58 mm.). If these measurements were taken correctly, they indicate a horse much larger than any yet known, unless it be Equus giganteus of Texas. There is no evidence that Dr. Skilton had made any serious study of the dentition of horses and the teeth were probably those of a domestic horse, or even of some other animal.

In 1884 (Trans. Linn. Soc. N. Y., vol. II, p. 47), Dr. C. Hart Merriam, in his paper “The Vertebrates of the Adirondack Region,” stated he had examined several fossil molar teeth of Equus major exhumed at Keenes Station, near the Oswegatchie Ox Bow, in Jefferson County, New York. He compared them with the corresponding teeth of an immense dray horse and found them much larger.

Professor G. C. Manse, of St. Lawrence University, Canton, New York, sent me for examination 4 upper teeth of a horse which must be those examined by Dr. C. H. Merriam. They are labeled as having been collected at Gouverneur, a town not far from Keenes Station. After a careful study of these teeth and comparison with those of the domestic horse, the writer concludes that they belonged to the latter. Domestic horses are known to have larger teeth. Professor Manse has unfortunately been unable to trace the history of the teeth back to Dr. C. C. Benton, of Ogdensburg, who showed them to Dr. Merriam.

NEW JERSEY.

(Map 17.)

1. Swedesboro, Gloucester County.—In 1868 (Cook’s Geol. New Jersey, p. 741), Cope stated that Equus complicatus was represented in New Jersey by a series of teeth obtained while a mill-dam at Swedesboro was being cleared. No further information has been secured. At the Academy of Natural Sciences of Philadelphia, the writer has seen a horse-tooth labeled as coming from the town named; but whether or not it is one of those referred to by Cope it is impossible to say.

2. Fish House, Camden, Camden County.—In 1869 (Trans. Amer. Philos. Soc., vol. XIV, p. 250, fig. 55), Cope wrote that a partial skull of Equus fraternus had been found at Fish House in a blackish clay at a depth of 20 feet from the top of the clay. Over the clay was imposed a bed of sand from 8 to 15 feet thick. This important skull appears to have been lost (fig. 7).

In 1897 (Ann. Rep. Geol. Surv. New Jersey for 1896, p. 208, plate X), Lewis Woolman described other remains of horses supposed to belong to Equus complicatus, secured in the same Fish House clays. The writer has seen these and regards them as belonging to the species just named. These remains of horses will be mentioned on pages 302–303.

3. Navesink Hills, Monmouth County.—Somewhere in the northeastern part of Monmouth County, in the region of the Navesink (or Neversink) Hills, have been found remains of a fossil horse. They were first mentioned by S. L. Mitchill (Cat. Organ. Remains, 1826, pp. 7, 8). He mentioned a cervical vertebra and teeth in sound condition. Leidy (Jour. Acad. Nat. Sci., Phila., vol. VII, p. 261) wrote that a vertebra and teeth were associated with remains of a mastodon. Mitchill mentions only a part of a tibia of a mastodon. These objects were all presented by Mitchill to the Lyceum of Natural History in New York. The writer believes these teeth had been buried in an early Pleistocene deposit.

PENNSYLVANIA.

(Map 17.)

1. Pittston, Luzerne County.—In the collection of the Academy of Natural Sciences at Philadelphia are 2 horse-teeth found at or near Pittston. They were described and figured by Leidy in 1873 (Monograph U. S. Geol. Surv., I, pp. 245–246, plate XXXIII, figs. 16, 17) as E. major (=E. complicatus). He stated they were found on the banks of the Susquehanna River, associated with remains of mastodons and Bison latifrons. The last was, however, a species of Symbos. In 1869 (Jour. Acad. Nat. Sci., Phila., vol. VII, p. 262), Leidy stated that it was reported these remains had come from a stratum “full of bones.” This stratum belonged probably to an early or middle Pleistocene interglacial stage.

2. Stroudsburg, Monroe County.—In 1889 (Ann. Rep. Geol. Surv. Pennsylvania for 1887, p. 6), Leidy reported the finding of “a pair of teeth of a horse, which were yet incompletely developed,” in Hartman’s Cave, near the town mentioned. He thought they belonged to an indigenous species. The position of the cave, its fossils, and their age will be considered in discussing the Pleistocene geology of the State on pages 308 to 311.

3. Port Kennedy, Montgomery County.—As long ago as 1871 (Amer. Jour. Sci., ser. 3, vol. I, pp. 235, 384), Wheatley announced the discovery of 2 unidentified species of horses in the great bone cave at the place named. They were associated with the remains of 40 other species of vertebrates, besides many insects. In 1899 (Jour. Acad. Nat. Sci., Phila., ser. 2, vol. II, pp. 193–267, plates XVIII-XXI), Cope described the materials collected up to that time from the same cave. Of horses he recorded 2 forms, which he named Equus fraternus fraternus and E. fraternus pectinatus. He was inclined to believe the latter would prove to be a distinct species. It is not certain whether this conclusion was correct; but if not a species, it is probably a subspecies of Equus complicatus. The teeth referred to E. fraternus fraternus are pretty certainly those of E. complicatus. Of this species Cope had a decayed skull of a young animal with teeth, besides a considerable number of other teeth and some bones of the skeleton. The geological relations of these remains and those of the other species will be discussed on pages 311 to 320.

4. Rutherford, Dauphin County.—In 1868 (Proc. Acad. Nat. Sci., 1868, p. 195), Leidy described a horse-tooth, loaned him by Mr. W. Lorenz and found somewhere between Rutherford and Highspire. It was met in a depression 6 feet deep and 20 feet across, filled with diluvium. Leidy thought the tooth might have belonged to a contemporary of the mastodon, but this was equally improbable. All the cement was dissolved from the tooth, and the latter was stained by iron, but not petrified. It was an upper second true molar. It has probably suffered the fate of such specimens as are retained in private hands.

5. Frankstown, Blair County.—From Mr. O. A. Peterson, of the Carnegie Museum, Pittsburgh, the writer learns that some part of an unidentified species of horse has been found in the collection made some years ago at Frankstown. For a list of the species page 321 may be consulted.

OHIO.

(Maps 17, 36.)

1. Cincinnati, Hamilton County.—In 1895 (Jour. Cin. Soc. Nat. Hist., vol. XVII, p. 217), Mr. Seth Hayes recorded the discovery of a molar tooth and a vertebra of a horse, identified as Equus fraternus. It was met with in exhuming the remains of the “Shaw mastodon” in Hyde Park, in the northeastern part of Cincinnati. The details of the exhumation are given in the description of the mastodon. The geological age of these animals dates probably from about the Sangamon stage. The writer has not been able to examine the horse remains referred to. It is probable that the tooth belonged to Equus complicatus.

2. Columbus, Franklin County.—In 1848 (Amer. Jour. Sci., ser. 1, vol. V, p. 215), Charles Whittlesey stated that bones and teeth of a horse had been found in fissures or “clay seams” of the Cliff limestone at Columbus. In 1866 (Smithson. Contrib. Knowl., vol. XV, art. 3, p. 16), the same geologist reported that Joseph Sullivant, of Columbus, had, many years before, obtained from the crevices of the Cliff lime rock, on the west side of Scioto River, a number of bones embedded in red clay. Among these was the tooth of a horse. The crevice had not been open since the date of the white settlement of the country and it was wholly filled by the red clay which results from the decomposition of the limestone. Probably all the remains mentioned by Whittlesey have been lost.

In 1875 (Cin. Quart. Jour. Nat. Hist., vol. II, p. 154), Klippart wrote that, in excavating the exterior wall at the Ohio penitentiary, the warden, Mr. Burr, found the fossil jaw of a horse with the molars in good condition. He stated the horse must have been one-third larger than the ordinary horse of to-day.

From Professor Clinton R. Stauffer, of Adelbert College, Cleveland, the writer received for examination a horse-tooth, labeled: “Catalogue No. 356. Horse-tooth. Given by Robert Cartwright. Found at Columbus, Ohio, in excavating in a peat-bed for a gas holder in the penitentiary grounds, October 30, 1873.” It is possible that this is the same tooth mentioned by Klippart, but probably it is another. The present writer identifies the tooth as that of Equus complicatus. The geological age is probably approximately that of the Sangamon stage.

3. Salt Creek, Columbiana County.—In 1866 (Smithson. Contrib. Knowl., art. 3, vol. V, p. 16), Charles Whittlesey reported a tooth of a horse found, about 20 years before, in making the Sandy and Beaver Canal, along Sandy Creek, in Columbiana County, at a depth not exceeding 12 or 15 feet. Probably the locality was in the southwestern corner of the county. The sources of Salt Creek are in Hanover Township, not far from the sources of Little Beaver Creek. From this vicinity Salt Creek flows westward. This county lies within the Illinoian drift region and the horse probably lived during the Sangamon stage or earlier.

INDIANA.

(Map 17.)

1. Evansville, Vanderburg County.—So far as the writer knows, remains of extinct horses have been found in Indiana only at the mouth of Pigeon Creek, a short distance below Evansville. Only a single vertebra, a last cervical, was secured. This formed part of a collection made at the place named by Mr. Francis A. Lincke. The collection was described by Dr. Leidy (Proc. Acad. Nat. Sci. Phila., 1854, p. 199). The bone was referred to Equus americanus, a name employed at that time for the horse now known as Equus complicatus. Although it would usually be impossible to identify a species of horse on such materials, it is probable that Leidy was correct. The geological age of the bone-bed is discussed on page 32. It is concluded that the age is most probably the Sangamon, but possibly Aftonian. The same species has been found at Bigbone Lick, above Louisville, on the Kentucky side. The deposits there overlie the Illinoian drift and are, in part at least, Sangamon.

Associated with the horse bone at Pigeon Creek were megalonyx, a probably extinct bison, the Virginia deer, a tapir, and the extinct wolf Ænocyon dirus.

ILLINOIS.

(Map 17.)

1. On the line between Bond and Fayette Counties.—In 1899, Leidy (Trans. Wagner Inst., vol. II, p. 39, figure) described under the name of Equus major an equine maxilla, containing 4 premolars, sent him by A. H. Worthen, State geologist of Illinois. This maxilla had been found in a bog between Bond and Fayette counties. It was referred by Gidley (Bull. Amer. Mus. Nat. Hist., vol. XIV, p. 135, fig. 24) to Equus pectinatus Cope. The specimen is in the collection of the State museum at Springfield and has been studied by the writer, who regards it as belonging to Equus complicatus. A fossil horse-tooth found at Bigbone Lick, Kentucky, greatly resembles one of the premolars of this jaw.

The region where this jaw was found lies within the area of the Illinoian drift; and, inasmuch as the specimen was found on a bog lying on this drift, the animal must have lived after the withdrawal of the Illinoian ice-sheet. The bog deposit belonged probably to the Sangamon stage.

The writer has endeavored earnestly, but in vain, to obtain more exact details regarding the locality where the jaw was found and the depth of interment.

2. Alton, Madison County.—At a meeting of the St. Louis Academy of Science, December 4, 1882 (Trans. St. Louis Acad. Sci., vol. IV, p. LXXX), William McAdams reported he had seen the fossil tooth of a horse from near Alton. No details were added, except that all the horses he had seen from the drift were large animals, while those from the bad lands of Dakota were mostly quite small.

In the McAdams collection, an account of which will be given on page 339, is a fragment of an incisor of a horse. It has on it McAdams’s No. 25. It is doubtful that this tooth was found in the loess. All the fossils of that collection purporting to have been found in the loess are very white, while this is of a brownish color, and there is a coat of iron oxide adhering to some parts of it. This may or may not be the tooth mentioned by McAdams as above reported.

3. Greene County.—At the meeting of the St. Louis Academy of Science just referred to, Mr. McAdams stated that teeth of an extinct horse had been brought up from the bottom of a well being dug in Greene County. More exact situation and the depth of the well were not mentioned.

Both Greene and Madison counties are occupied by the Illinoian drift-sheet. The horse-teeth found in these counties might have come from Sangamon deposits; or possibly the Illinoian drift had been passed through and Yarmouth interglacial had been entered.

The geologists J. A. Udden and E. W. Shaw (Belleville-Breese Folio, No. 195, U. S. Geol. Surv., p. 7) have noted in those quadrangles deposits which may consist of pre-Illinoian till; also old black soils which may belong to the Yarmouth. The quadrangles mentioned lie along the southern border of Madison County. The old soils were found at depths varying from 30 to 75 feet. In this region, too, the Illinoian drift is overlain by a blanket of loess. To arrive at any valuable conclusion, one ought to know just where specimens are found and at what depths and in what kind of deposits. On the other hand, the information is of the most meager kind. The specimens mentioned are not in a collection made by McAdams and now in the National Museum.

MARYLAND AND DISTRICT OF COLUMBIA.

(Map 17.)

1. Marshall Hall, Charles County.—In the U. S. National Museum is an upper right molar, first or second, of a horse labeled as found at this place. It is credited to Mr. O. N. Bryan, who, some years ago, contributed many articles to the museum. The conditions of discovery are not known. The length of the grinding-surface is 28 mm., the width 27 mm. It probably belongs to Equus leidyi. According to Shattuck’s map of the Pliocene and Pleistocene of Maryland (Maryland Geol. Surv., 1906, plate I) this locality is occupied by Talbot deposits. Shattuck regards the Talbot as belonging to late Pleistocene times. The present writer does not accept this view.

2. Georgetown, District of Columbia.—In 1835 (Med. and Phys. Researches, p. 267), Dr. Richard Harlan acknowledged the receipt, at the Academy of Natural Sciences of Philadelphia, of remains of a fossil horse found at Georgetown in constructing the canal along the Potomac. These were probably teeth and had been sent by Colonel I. J. Abert, of Washington. They ought now to be in the Academy mentioned. In 1850, R. W. Gibbes (Proc. Amer. Assoc. Adv. Sci., vol. III, p. 67) presented before the American Association of Sciences a specimen (a tooth?) which he said came from the bank of the Potomac and was associated with a tooth of Bos (Bison). How he came to have this was not related, nor is it certain that it was found near Washington.

3. Mitchellville, Prince George’s County.—In the U. S. National Museum are 2 upper teeth, molars or premolars (No. 8813), of a horse found on his estate northwest from the town named, by Mr. Edward S. Walker. They were presented to the National Museum by Dr. Edward W. Berry, of John Hopkins University. These teeth, apparently first and second molars, seem to belong to an undescribed species. The table gives the height of the teeth and dimensions of the grinding-surface in millimeters.

┌────────────┬────────────┬────────────┬────────────┬────────────┐ │ Tooth. │ Height. │ Length. │ Width. │ Protocone. │ ├────────────┼────────────┼────────────┼────────────┼────────────┤ │M^1 │70 │29.5 │25 │12 │ │M^2 │73 │30 │23 │14.5 │ └────────────┴────────────┴────────────┴────────────┴────────────┘

The teeth present the appearance of having been little worn. Measurements of the crown taken about one-third the distance to the base are as follows:

┌────────────────┬────────────────┬────────────────┬────────────────┐ │ Tooth. │ Length. │ Width. │ Protocone. │ ├────────────────┼────────────────┼────────────────┼────────────────┤ │M^1 │25 │25 │11 │ │M^2 │26 │25.2 │13 │ └────────────────┴────────────────┴────────────────┴────────────────┘

The teeth are moderately curved, so that the outer face is convex, the inner concave. Some of the cement is retained and is colored blue with vivianite. The enamel presents less complication than is usually found in either Equus complicatus or E. leidyi. The dimensions of the teeth and the narrowness, especially of the second molar, seem to exclude reference to either of the species mentioned.

4. Chesapeake Beach, Calvert County.—Mr. William Palmer, of the U. S. National Museum, had for many years been making collections, mostly of Miocene vertebrates, along the cliffs at Chesapeake Beach. Among other fossils found there are some remains of horses, among them one much worn upper tooth, probably a premolar. The height is only 21 mm., the length of the grinding-surface 22.4 mm., the width 24 mm. It may be referred provisionally to E. leidyi. Mr. Palmer had also an ungual phalanx and a cervical vertebra and various other bones and teeth of horses. The geological situation at the place and the other Pleistocene species found there will be discussed on pages 347–348.

5. Cavetown, Washington County.—In his work on the exploration of Bushy Cavern, near Cavetown, Mr. Charles Peabody (Bull. IV, Dept. Archæol., Phillips Acad., p. 12) stated that in a limestone quarry, south of the cave, in the red earth, was found a tooth which J. W. Gidley identified as probably Equus complicatus. In 1920 (Proc. U. S. Nat. Mus., vol. LVIII, pp. 96–109), the writer described a collection made at Cavetown. In this were other remains referred to Equus complicatus. Some fragments of a large tooth were referred with doubt to Equus giganteus.

6. Corriganville, Allegany County.—In a crevice in a limestone rock, at a point about 3 miles west of north of Cumberland, taken in a straight line, J. W. Gidley, in the fall of 1912, made a large collection of fossil vertebrates. In this collection is a first phalanx of an extinct horse. The species has not been determined. A list of the accompanying species, so far as determined, will be presented on pages 349–350.

VIRGINIA.

(Map 17.)

1. Abingdon, Washington County.—In the U. S. National Museum is the outer half of an upper hindermost molar of a horse sent, in 1869, by Mr. Wyndham Robinson. With it were remains of Mammut americanum. The length of the grinding-surface is 30 mm. It belongs pretty certainly to Equus complicatus.

2. Saltville, Smyth County.—Mr. O. A. Peterson (Ann. Carnegie Mus., vol. XI, p. 474) reported the occurrence of an upper left molar of a horse at Saltville. The species has not been determined. The matter will be referred to again on pages 352–353.

3. Ivanhoe, Wythe County.—In 1869 (Proc. Amer. Philos. Soc., vol. XI, pp. 171–182), Cope gave an account of the discovery of remains of numerous fossil vertebrates somewhere along New River, in the county named. Among these animals were upper and lower milk and permanent molars of a horse. Cope identified these as belonging doubtfully to Equus complicatus. On page 353, the Pleistocene geology of the region and a list of the accompanying vertebrates will be presented.

4. Staunton, Augusta County.—From Dr. W. F. Deekens, surgeon dentist of Staunton, a tooth of a horse found somewhere in that vicinity, was sent to the U. S. National Museum. It had been found in a limestone quarry, 70 feet below the surface, in a narrow stratum of clay. Probably the tooth had been carried down into a crevice in the limestone by a current of water. The length of the grinding-surface is 31 mm. The arrangement of the enamel folds is simple, but the tooth had only just begun to be worn. The narrowness of the tooth is remarkable and it may belong to an unrecognized species.

5. Denniston, Halifax County.—From Mr. G. W. Joyner, living near this place, the U. S. National Museum in 1920 received a left lower grinding-tooth of a horse, found by the donor in a little stream on his farm.

WEST VIRGINIA.

(Map 17.)

1. Point Pleasant, Mason County.—From Dr. L. V. Guthrie, superintendent of the West Virginia Asylum, at Huntington, the U. S. National Museum received for examination a horse-tooth dredged up with gravel from Ohio River at Point Pleasant. The writer has not been able to distinguish this tooth (either the last or the next to the last premolar) from that of Equus niobrarensis. If further discoveries confirm this provisional determination, the known range of the species will be greatly extended. The tooth has been deposited in the U. S. National Museum by the owner, Captain H. S. Wert, of Point Pleasant. The presence of this tooth proves that there are, somewhere not far away, some early Pleistocene deposits, probably in some high terrace along the Ohio, such as are found in abundance along the upper part of the river and its affluents.

NORTH CAROLINA.

(Maps 17, 39.)

1 Elizabethtown, Bladen County.—The geologist E. Emmons (North Carolina Geol. Surv., 1858, p. 197, fig. 18) described and figured an upper left second or third molar tooth of a horse which he called Equus caballus, the domestic animal. It, with a tooth from the lower jaw, had been found in a bed of Miocene age at Elizabethtown. Whatever may have been the age of the marl-bed, the horse lived during the Pleistocene. Conrad, however (Amer. Jour. Sci., vol. XLVII, 1869, p. 359), insisted on the Miocene age of the animal. The same tooth was, in 1860 (Holmes’s Post-Pl. Foss. South Carolina, plate XV, fig. 16), figured by Leidy and referred to E. fraternus. It is now known as E. leidyi. Miller (North Carolina Geol. and Econom. Surv., vol. III, p. 248) points out that patches of Miocene marl do occur in the vicinity of Elizabethtown.

2. Sixteen miles Southeast of Newbern, on the Neuse River, in Pamlico County.—In a locality on the left bank of Neuse River, about 16 miles below Newbern, bones of Equus and various other animals were first found long ago, apparently by Nuttall. T. A. Conrad, in 1838 (Fossils Medial Tert. U. S., p. X), spoke of great numbers of bones of horse, mastodon, etc. Harlan (Med. Phys. Res., p. 267) says that Conrad possessed specimens from the locality. Lydekker (Cat. Foss. Mamm. Brit. Mus. part 3, p. 89) states that there is in that museum an upper cheek-tooth from Newbern. So far as the writer knows, none of the teeth found here has been figured or accurately described.

On pages 358–359 will be found a list of the vertebrate fossils collected at Newbern and a consideration of the geology.

3. Greenville, Pitt County.—In 1852, E. Emmons (Geol. Surv. North Carolina, p. 106) said he had procured a grinder of a horse at Greenville, in the sandy stratum just above the Miocene marl. In 1858 (Geol. Surv. North Carolina Agric., Eastern Counties, p. 197, fig. 21), the same writer figured an incisor tooth found in the Miocene of Pitt County. Conrad (Amer. Jour. Sci. 1871, vol. I, p. 468) spoke of the finding of black and mineralized teeth of a horse, which he regarded as E. fraternus, in Miocene marl. Leidy (Proc. Acad. Nat. Sci. Phila., 1871, p. 113) reported on the upper molar tooth which Conrad had found. He regarded it as occurring accidentally in the Miocene and as belonging to E. complicatus; but as the tooth was injured, Leidy thought it might belong to Hipparion. In the collection of the Academy of Natural Sciences at Philadelphia the writer has seen quite certainly the same tooth. It appears to be an upper premolar, the third or the fourth. It has a height of about 50 mm. and a length of 30 mm. The inner half has been split off. It is that of E. complicatus.

4. Plymouth, Washington County.—E. Emmons, in 1858 (North Carolina Geol. Surv. Agric., Eastern Counties, p. 197, figs. 19, 20), figured 2 teeth, an upper left molar or premolar and a hindermost left molar, which had been washed up on the beach at Plymouth. This place is on the south bank of Roanoke River. Judging from Emmons’s figures, one must conclude that these teeth belong to Equus leidyi.

SOUTH CAROLINA.

(Map 17.)

1. Beaufort, Beaufort County.—In the museum of Rutgers College, at New Brunswick, New Jersey, the writer has seen 6 teeth of Equus, presented by Mr. G. U. Shepard jr., and obtained on Coosaw River; but no more detailed information has been furnished. In the Charleston Museum is a tooth of Equus complicatus which was found by Mr. Earle Sloan, in Coosaw River.

2. Charleston, Charleston County.—The remains of horses, especially teeth, are among the most abundant Pleistocene fossils in the region around Charleston. Most of the specimens have been discovered in dredging for phosphate rock, and usually nothing is recorded about the exact locality where found or about the conditions of burial. A considerable number of well-preserved teeth have, however, been discovered in known localities and under defined conditions.

The earliest collection of fossils described from about Charleston was made by Professor F. S. Holmes, of Charleston, and Captain A. H. Bowman, U. S. Army. These fossils were sent to Dr. Joseph Leidy and described by him as early as 1858, but more fully in 1860, in Holmes’s “Post-Pleiocene Fossils of South Carolina.” Most of these fossils were obtained on the shores of Ashley River, about 10 miles above Charleston. From this locality were described 5 upper teeth of Equus complicatus (Leidy, op. cit., p. 102, plate XV, figs. 2–5, 7) and 2 lower ones (plate XVI, figs. 19, 21).

Of Equus leidyi (=E. fraternus Leidy) the author quoted described from Ashley River 2 lower teeth (op. cit., plate XVI, figs. 20, 22). Leidy (Proc. Acad. Nat. Sci. Phila., 1870, p. 98) reported that there were in the collection of C. N. Shepard, at Amherst College, teeth of Equus major (=E. complicatus) and E. fraternus (=E. leidyi) secured in the Ashley River deposit. Leidy, in 1873 (Contrib. Ext. Vert. Fauna West. Terrs., p. 245, plate XXXIII, figs. 14, 15) reported an upper molar and a lower one of E. complicatus, found in the “phosphate beds” of Ashley River.

From Doctor Swamp, Johns Island, southwest of Charleston, Leidy (op. cit., p. 103, plate XV, fig. 6) described an upper tooth as that of his Equus fraternus. This was afterwards made by Cope the type of this species; but Gidley (Proc. U. S. Nat. Mus., vol. XIV, p. 111) determined that this type belongs itself to E. complicatus. It was this determination which made it necessary to give a new name, E. leidyi, to the teeth of medium size which had gone under the name of E. fraternus.

In the National Museum is a finely preserved upper right third or fourth premolar of what appears to be Equus complicatus which is recorded having been found in Wando River, northwest from Charleston. The tooth is 75 mm. high, 31 mm. long on the grinding-face, and 27 mm. wide. The enamel is much complicated. In Holmes’s “Post-Pleiocene Fossils of South Carolina,” on pages 102 and 104, Leidy mentions an upper second premolar of Equus fraternus found on Goose Creek, about 12 miles from Charleston. He added a paragraph on the geology. Further reference to this will be found on page 363. In the Charleston Museum and in the private collections about Charleston the writer has seen many teeth of horses found in that region, most of them without statements about exact localities, though some were found in Stono River. The teeth of E. leidyi appear to be more numerous in the collections than those of E. complicatus. Many teeth of both species are contained in the Scanlan collection, made in the region about Charleston and now owned by Yale University. In this collection are found also two lower molars which the writer refers to Equus littoralis. The reader is referred to pages 362 to 366.

3. Richland County.—On the occasion referred to in the next paragraph, Robert W. Gibbes presented a tooth of a horse found in Richland district at a depth of 17 feet, in a slough, supposed to have been a former bed of Congaree River.

4. Darlington, Darlington County.—In 1850 (Proc. Amer. Assoc. Adv. Sci., vol. III, p. 67), Gibbes showed before the Association several specimens of horse-teeth, referred to Equus americanus (E. complicatus), found in supposed Pliocene at Darlington. They were reported as having been discovered associated with bones of a mastodon, presumably of Mammut americanum. No additional information was furnished. Darlington is situated on a branch of Black Creek, an affluent of Great Pedee River. The teeth were probably found in a Pleistocene terrace deposit.

GEORGIA.

(Map 17.)

Apparently remains of extinct horses have been found in Georgia in only two places, as follows:

1. Brunswick, Glynn County.—During the construction (in 1838–39) of a canal which connected Altamaha and Turtle Rivers, remains of various fossil vertebrates were discovered. A list of these will be given on page 370. Among the remains was a lower left last premolar or first molar of an extinct horse, described by Leidy in 1847 (Proc. Acad. Nat. Sci. Phila., 1847, p. 266) and again in 1860 (Holmes’s Post-Pleiocene Foss. South Carolina, p. 104, plate XVI, fig. 23). In the first publication he referred the tooth to his species Equus americanus (=E. complicatus); but in 1860 he referred it to his Equus fraternus (=E. leidyi). The size of the tooth appears to justify his later conclusion.

Lyell, in his “Second Visit to the United States,” made in 1845 (ed. 2, vol. 1, p. 348), stated that remains of Equus had been found in the Brunswick Canal. He referred it to Equus curvidens, and stated that this species had the upper teeth more curved than any living horse.

On page 436 of Bulletin No. 26 of the Geological Survey of Georgia, J. W. Gidley furnished a list of vertebrates dredged up somewhere near Brunswick. Among the species are 3 horses, Equus fraternus (=E. leidyi), E. complicatus, and E. tau (probably E. littoralis). Through the liberality of Professor S. W. McCallie, State Geologist of Georgia, the writer has been permitted to study these teeth. There is one damaged upper molar which belongs to E. complicatus; 4 upper and 1 lower grinders belong to E. leidyi; 2 upper left molars are certainly those of E. littoralis; one having a height of 72 mm., a crown-length of 23 mm., and a width of 22 mm. The length is slightly greater than that of the type of the species.

In the collection of the Academy of Natural Sciences of Philadelphia the writer has examined an equine tibia presented by J. H. Couper, probably found in the Brunswick Canal with the other remains presented by Mr. Couper. It is compared in size with a tibia of the horse Edwin Forrest, with that of a draft horse in the U. S. National Museum, and with that of E. scotti, No. 10628, in the American Museum of Natural History.

Measurements of tibiæ of horses, in millimeters.

┌─────────────────────────────┬─────────┬─────────┬─────────┬─────────┐ │ │Brunswick│ Edwin │ Draft │ E. │ │ │ horse. │Forrest. │ horse. │ scotti. │ ├─────────────────────────────┼─────────┼─────────┼─────────┼─────────┤ │Total length of tibia │ 455│ 365│ 420│ 370│ │Side-to-side diameter at │ 65│ 42│ 50│ 49│ │ middle of length │ │ │ │ │ └─────────────────────────────┴─────────┴─────────┴─────────┴─────────┘

The Brunswick horse was evidently a very large one, but it may have been an unusually large specimen of Equus complicatus.

2. Skidaway Island, near Savannah, Chatham County.—On page 27 of William B. Hodgson’s “Memoir on the Megatherium,” in Joseph Habersham’s memorandum, is noted the fact that among the fossils found here was a well-preserved tooth of a horse. The height of the tooth is given as being 2.75 inches, greatest diameter 1.2 inches, the least 1 inch. The tooth was evidently an upper premolar or molar. It belonged probably either to Equus complicatus or E. leidyi, but to which is uncertain.

In 1850 (Proc. Amer. Assoc. Adv. Sci., vol. III, p. 67), Robert W. Gibbes reported the discovery of horse remains, probably a tooth, in the alluvium of Skidaway Island, a few miles southeast of Savannah. No further information was furnished. The geological conditions at this island and the fossils found there will be considered on pages 370 to 372.

FLORIDA.

(Maps 17, 18.)

1. Stokes Ferry, St. Mary’s River, Nassau County.—In 1909 (2d Ann. Rep. Florida Geol. Surv., p. 147), Sellards stated, on authority of notes received from Dr. L. W. Stephenson, that 3 teeth of a fossil horse had been found at the place named. At the same place was discovered a fragment of a tooth of an elephant, most probably Elephas columbi, and some ear-bones of a whale. The writer has not seen these and does not know to what species they belonged.

Measurements of tibiæ of horses.

┌───────────────────────────────────────┬─────────┬─────────┬─────────┐ │ Dimensions taken. │Equus sp.│ E. │ E. │ │ │Florida. │ scotti. │caballus.│ ├───────────────────────────────────────┼─────────┼─────────┼─────────┤ │Total length of bone │ 396│ 370│ 392│ │Length on outer border │ 360│ │ │ │Length on inner border │ 378│ │ │ │Width across upper end │ 125±│ 107│ 108│ │Fore-and-aft diameter at middle of │ │ │ │ │ length │ 45│ 40│ 37│ │Side-to-side diameter at middle of │ │ │ │ │ length │ 56│ 49│ 43│ │Greatest width at lower end │ 94│ 93│ 86│ └───────────────────────────────────────┴─────────┴─────────┴─────────┘

2. Almero Farm, St. John County.—In the collection of Mr. Fred R. Allen, of St. Augustine, Florida, the writer has examined a left tibia of an extinct horse, found in the Inland Waterway Canal, about 28 miles south of St. Augustine. The species has not been determined, but it may be well to put on record the measurements. It apparently belonged to a rather large horse. For comparison, other corresponding measurements are given, taken from Equus scotti, No. 10628 of the American Museum of Natural History, and from Equus caballus, No. 74 of Mr. Chubb’s collection at the museum mentioned, a trotting stallion.

It will be seen that the tibia found below St. Augustine is a relatively stouter bone than those it is compared with. The large horse, known to have existed in Florida, is Equus complicatus.

3. Neals, Alachua County.—This place is near Newberry. Here have been collected Gomphotherium floridanum, Tapirus terrestris?, and Hipparion sp. indet.

4. Wade, Alachua County.—The writer has seen at Tallahassee, 4 fossil Equus teeth, found at this place. One is No. 1470 of the Florida Geological Survey and labeled as found in the Buttgenbach “cummer” mine. It is a lower left second premolar, 40 mm. high, 31 mm. long, and 14.5 mm. wide, not including the cement present. Another tooth, No. 1462, from Buttgenbach’s river mine, near Wade, is the hindermost left molar of the lower jaw, 32 mm. long, and 13 mm. wide in front. It is thought these teeth belonged to Equus leidyi.

5. Newberry, Alachua County.—This is the locality mentioned by Dall (Bull. 84, U. S. Geol. Survey, p. 128) under the name of Hallowells; but he mentioned no fossils from this place. In the Report of the Florida Geological Survey, volume v, page 58, Sellards stated that a species of Hipparion had been discovered in the hard phosphate. In the eighth report of the same survey, on page 42, the present writer described a specifically undetermined species of Parahippus, also from the phosphate deposits. On page 94 Dr. Sellards reported Equus littoralis and Odocoileus from Newberry. The writer has identified as Equus littoralis, a horse represented by a lower left hindermost molar, found at Newberry.

6. Archer, Alachua County.—Dr. Joseph Leidy, in 1885 (Proc. Acad. Nat. Sci. Phila., pp. 32, 33), described from this place a rhinoceros, Rhinoceros proterus, and Hippotherium ingenuum. In 1886 (ibid., pp. 11, 12) he again mentioned these species and described in addition to them Mastodon floridanus and 3 species of camels which he referred to the genus Auchenia. In a list furnished by Leidy to Dr. W. H. Dall (Bull. U. S. Geol. Surv., No. 84, p. 129), there are listed, besides the species mentioned, Megatherium and Cervus virginianus?, all found in the Alachua clays and usually referred to the Lower Miocene or Upper Pliocene. In the list presented on page 375, under the geology of Florida, a species of tapir is added. At present the writer assigns the deposits known as the Alachua clays to lowermost Pleistocene.

7. Williston, Levy County.—In the American Museum of Natural History, New York, is an upper last molar of Equus, found at the place named and presented by E. Mixon. The enamel is not much plicated. The size of the tooth indicated that it belonged to E. leidyi. In the list of vertebrates unearthed at Mixon’s (near Williston), furnished by Leidy to Dall, were included two species of Hippotherium, H. ingenuum and H. plicatile. These species are now referred to the genus Hipparion. H. plicatile was described by Leidy in 1887 (Proc. Acad. Nat. Sci. Phila., p. 309). A list of the species at present known to have been obtained here is to be found on page 375 under the geology of Florida. They have all been found in the Alachua clays and are usually regarded as belonging to the late Tertiary.

8. Ocala, Marion County.—In 1889 (Trans. Wagner Inst., vol. II, p. 13), Leidy reported the discovery of some fossil vertebrates in a fissure in a limestone rock near Ocala. Some equine teeth he referred to Equus fraternus (=E. leidyi). The other species were identified as Smilodon floridanus, Elephas columbi, and (with some doubt) Procamelus minimus. For conclusions regarding the geology of the locality see page 378.

9. Dunnellon, Marion County.—The writer has examined 2 fossil horse-teeth found near Dunnellon, now the property of the Florida Geological Survey. No. 1366 is from the Camp Phosphate Company’s Blue Run mine. It is a first or second upper molar, worn down to a height of only an inch and having a grinding-surface 26 mm. long and 25 mm. wide and with a protocone 12 mm. long fore-and-aft. No. 1444, also a first or second upper molar, has a height of 47 mm., a length of 24 mm., a width of 23 mm., and a protocone of 11.5 mm. The enamel of the lakes is much plicated. The teeth are identified as those of Equus leidyi. No. 1444 has been figured by Sellards (7th Ann. Rep. Florida Geol. Surv., p. 111, fig. 40) and described as dredged from the Schilmann and Bene river mine, on Withlacoochee River.

On page 376, under the geology of Florida, will be found a list of the species obtained at Dunnellon and the surrounding region. In this list is included Parahippus sp. indet. and Hipparion plicatile. Dr. Sellards believes that many species of that list belong to the Pleistocene. The horse-like species, the rhinoceros, and the camel are held by him as being older than the Pleistocene.

10. Hernando, Citrus County.—At this place have been secured Gomphotherium floridanum, Hipparion sp. indet., and Procamelus sp. indet., all from the phosphate deposits and referred by Sellards to the Upper Miocene or the Lower Pliocene.

11. Holder, Citrus County.—In the collection of Dr. H. G. Bystra, of Holden, is a fossil horse-tooth dredged from Withlacoochee River, in section 29, township 17 south, range 19 east. The species to which the tooth belonged has not been determined.

12. Orange County.—The writer has seen, in the collection of the Academy of Natural Sciences of Philadelphia, an upper right last molar of Equus, labeled as found in the county named. Nothing more is known by the writer about the tooth.

13. Eau Gallie, Brevard County.—In 1916 (8th Ann. Rep. Florida Geol. Surv., p. 105), Sellards stated that at this place, in the Hopkins drainage canal, had been collected teeth of Elephas columbi and Equus complicatus.

14. Kingsford, Polk County.—In the U. S. National Museum are 3 horse-teeth collected in 1903 by Mr. Juan C. Edmundoz, from some of the phosphate mines in the region about Kingsford. Although most of the fossils from these mines have been supposed to belong to the late Miocene or early Pliocene, these horse-teeth are certainly of Pleistocene age. One tooth, No. 8620, is an upper right true molar, either the first or the second. It is worn down to about half its original length. The length of the grinding-surface is 25 mm.; its width is 26 mm. The enamel surrounding the lakes is extremely complicated. Another tooth, No. 8619, is a right hindermost molar with the protocone missing. A third tooth, No. 8618, is a little-worn lower molar, probably the second. The height is 83 mm., the length 25 mm., width 14 mm. The teeth are to be referred to Equus leidyi.

15. Brewster, Polk County.—In volume VIII of the Florida Geological Survey, pages 95, 96, Dr. Sellards states that from the phosphate mines at Brewster have been obtained teeth of Hipparion minor. A list of the associated species is to be found in the discussion of the Pleistocene geology of Florida on page 380.

16. Alafia River, Hillsboro County.—In the American Museum of Natural History, New York, is a collection of 10 teeth of Equus, said to have been dredged in Alafia River. Some belong to E. leidyi. One, a right third or fourth upper premolar worn down to a height of 40 mm., has still a length of 30 mm. and a width of 27 mm.; apparently it belongs to E. complicatus. The writer has described an extinct species of box-tortoise, Terrapene putnami (Fossil Turtles, N. A., p. 360) dredged by Professor F. W. Putnam in Alafia River about a mile above its entrance into Tampa Bay. With the bone, which forms the type of the species, were dredged a peripheral bone of a Testudo, possibly T. crassiscutata, and remains of horses and tapirs. It is pretty certain that the 10 teeth above mentioned were secured by Professor Putnam.

In Heidelberg University, Tiffin, Ohio, is a part of a lower right premolar of Equus, apparently E. leidyi, said to have been found near Tampa Bay.

17. Palmetto, Manatee County.—At several places about the mouth of Manatee River have been found relics of fossil horses. Mr. Ernest Leitzel, of Palmetto, sent to the U. S. National Museum for identification some teeth found in Manatee River, others in Terra Ceia Bay. The teeth are all well fossilized; some are upper teeth, others belong below. The writer regards them as belonging to Equus leidyi.

In the same museum are 2 lower right true molars, a second and a third, sent from Manatee by Mr. N. B. Moore. The teeth are moderately worn. The length of the grinding-surface of the hindermost molar is only 23 mm., the width 12 mm. They must have belonged to a small horse and are referred to Equus littoralis.

From Mr. Charles T. Earle the U. S. National Museum received in February 1921, several teeth of Equus leidyi, 2 of E. complicatus, and 1 of E. littoralis, which had been washed up on the beach at Palma Sola, about 10 miles below Palmetto. With these teeth came parts of antlers of a deer, a part of a metacarpal and an astragalus of Bison latifrons?, a part of a beak of a platanistid porpoise, a part of a tooth of Elephas columbi, a fragment or two of a terrapin (Trachemys sp. indet.), a fragment of the carapace of a soft-shelled turtle, and teeth of sharks. The porpoise and the sharks, also a part of a metapodial of a camel, may belong to Miocene or Pliocene deposits near the locality.

18. Sarasota Bay, Sarasota County.—The region a little further south than Manatee River has furnished remains of extinct horses. Sellards (7th Ann. Rep. Florida Geol. Surv., p. 112, fig. 47) has figured a lower tooth of a large horse, found by Mr. Joseph Willcox, at White Beach, on Sarasota Bay. Inasmuch as the fore-and-aft dimension of the tooth is 30 mm., it very probably belonged to Equus complicatus. Mr. Willcox has submitted to the writer 2 large lower teeth, regarded as belonging to the species just mentioned. Another lower tooth, apparently a third or fourth lower premolar, found on the same beach, has the fore-and-aft dimension only 26 mm., the width 15 mm. This is referred to Equus leidyi. At Blackburn’s place, 12 miles south of White Beach, Mr. Willcox secured a tooth of Equus apparently little worn. The height is 83 mm., the length at the summit 28 mm., but a little further down only 26 mm.; the width 12 mm. This tooth is to be referred to Equus leidyi.

In the American Museum of Natural History, New York, are 7 teeth of Equus, collected in 1911 by Mr. Barnum Brown at a place 8 miles southeast of Sarasota. They appear to belong to the Florida horse of medium size, Equus leidyi.

19. Calvenia, Hardee County.—In the U. S. National Museum (No. 4838) is an upper right last molar of a horse labeled as found near the mouth of Charlie Apopka Creek and as having been presented by Captain Le Baron through L. C. Johnson. The tooth belongs to Equus leidyi. Another tooth found at the same place, at the same time (December 16, 1883), and presented in the same way, is a lower grinder. The height is 75 mm., the length, 27 mm., the thickness 12.3 mm. It is to be referred to E. leidyi.

20. Arcadia, De Soto County.—Many remains of horses, especially teeth, have been collected at and near this place, by Mr. Joseph Willcox, on a sand-bar at Arcadia being explored for phosphate. The first published description of these remains appears to be that of Leidy in 1889 (Trans. Wagner Inst., II, p. 19). Leidy had at hand 17 upper molars, 2 lower molars, and 2 incisors. He was, at that time, uncertain whether these teeth pertained to an indigenous species of Equus or to the domestic horse. The manager of the Arcadia Phosphate Company, Mr. T. S. Moorhead, informed Mr. Willcox that the main source of the materials of the bar extended for miles along the shores of Peace Creek and was about 8 feet thick.

Among the materials examined by Leidy (Proc. Acad. Nat. Sci. Phila., 1890, p. 182) was a tooth which he regarded as belonging to Equus major (=E. complicatus), but, on the suggestion of Professor Cope, he described and figured as Hippotherium princeps. Later, Lucas (Trans. cit., vol. IV, p. 49, plate XIX, figs. 12, 13) concluded that Leidy’s first opinion was correct. The tooth is abnormal in having the column of the protocone free from the other cusps of the tooth for a short distance from the grinding-surface. In Bulletin No. 84 (p. 129) of the U. S. Geological Survey, Leidy referred the Peace Creek horses to his Equus fraternus (=E. leidyi), and it is found that in size and other respects the type of Hippotherium princeps agrees with this species. It is retained, however, as Equus princeps.

In the U. S. National Museum are 6 teeth collected on Peace Creek, probably not far from Arcadia, which all apparently belong to E. leidyi. J. W. Gidley (Bull. Amer. Mus. Nat. Hist., vol. XIV, 1901, p. 121) stated that there is in the American Museum a tooth from Peace Creek, much too small to be referred to any species at that time reported from the United States, but resembling closely Equus tau, from Mexico. This tooth probably belongs to Equus littoralis.

Besides the horses of the genus Equus, there have been found at or near Arcadia the 3–toed horse Hipparion ingenuum. Whether this is to be referred with the great majority of the fossils found in this region to the Aftonian fauna of the first interglacial or to the Nebraskan stage it is impossible to say.

21. Vero, St. Lucie County.—Numerous remains of extinct horses have been found here, but they always consist of single bones or teeth, sometimes in fine condition, sometimes somewhat water-worn. The remains occur in both deposits, designated as No. 2 and No. 3, but in the latter the materials are more fragmentary and not specifically identifiable. Sellards has figured some of the teeth in his seventh Annual Report (1915, pp. 110, 111, figs. 40–43). In his eighth report, on page 149, he has recognized the occurrence here of 3 species, Equus complicatus, E. leidyi, and E. littoralis.

The writer has examined a large canine tooth found in the stratum of sand, No. 2. From its size it is referred to Equus complicatus. Its fore-and-aft diameter is 14 mm. Another tooth from the stratum, an upper right third true molar, finely preserved and retaining some of the cement, is regarded as belonging to E. leidyi. Two lower teeth from No. 2 are water-worn, but retain their structure. The fore-and-aft diameter of each is 21 mm. They must have belonged to the little horse called E. littoralis. A fragment of an upper tooth is referred to this species. It is not water-worn, but has been split from the crown to the root. A hinder first phalangeal bone found in the canal (No. 1802 of the Florida Geological Survey) is 96 mm. long. This indicates a horse as large as our ordinary domestic horses and it probably belonged to Equus complicatus.

22. Labelle, Lee County.—In 1889 (Trans. Wagner Inst., vol. II, p. 17), Leidy stated that Mr. Joseph Willcox had obtained, from a Pliocene shell-bed on Caloosahatchee River, some remains of a fossil horse, consisting of two cervical vertebræ and a part of a lower jaw, which contained the first and second molar teeth. These teeth are probably what would be called premolars 2 and 3. Leidy referred the remains to his Equus fraternus (=E. leidyi).

Dall (Bull. No. 84, U. S. Geol. Surv., p. 129) stated that Equus fraternus, Bison latifrons, and Elephas columbi were found in Pliocene beds on the Caloosahatchee, but Sellards (8th Rep. Florida Geol. Surv., p. 102) corrects this error as to the age.

The writer has received a letter from Mr. Willcox in which he states that the fragment of lower jaw was found about 2 or 3 miles below Labelle.

23. Palm Beach, Palm Beach County.—In 1916 (8th Ann. Rep. Florida Geol. Surv., p. 105), Sellards wrote that Mr. J. L. Hayes had secured for the Florida State Geological Survey, from the Palm Beach Canal, teeth of Elephas columbi and Equus complicatus and a femur of a species of Bison.

ALABAMA.

(Map 17.)

1. Newbern, Hale County.—In August 1914, there was received at the U. S. National Museum, from Mr. J. W. White, of Newbern, a lower left first incisor of a horse. This, with a lower molar of a species of Bison, had been found in a creek. The incisor is somewhat worn, but still retained a part of the cup. The grinding-face is 14 mm. from side to side. The species can not be determined.

2. Bogue Chitto, Dallas County.—In the U. S. National Museum is an upper right true molar, first or second, of a horse, found at this place in 1883, by L. C. Johnson, of the U. S. Geological Survey. The tooth is identified as that of Equus leidyi. The enamel is much crenated. At the same place was found a tooth (a lower molar) of Elephas imperator, and teeth of Mammut americanum. It seems to the writer that the presence of these species indicates that the deposits along Bogue Chitto belong to the early part of the Pleistocene, about equivalent to the Aftonian.

MISSISSIPPI.

(Map 17.)

1. Orizaba, Tippah County.—In the U. S. National Museum (No. 1907) is a fossil tooth of a horse, a third or fourth right premolar, found apparently not far from this little town. It is labeled as having been picked up at Lander’s mill, 9 miles south of Ripley, on Cane Creek, out of débris of Cretaceous marl, and given to Dr. T. E. Stanton. How it came to be mingled with the marl is not known. The tooth is only moderately worn, the height being 75 mm. The length of the grinding-surface is 28 mm., the width 27 mm. It has the enamel unusually strongly folded. The tooth is referred provisionally to Equus leidyi.

2. Natchez, Adams County.—Elsewhere will be found an account of the discovery of fossil vertebrates near Natchez by Dr. M. W. Dickerson (p. 390), among which were found horse-teeth, referred to two species. One of these horses, represented, as supposed, by 12 teeth, was at first called by Leidy Equus americanus (Proc. Acad. Nat. Sci. Phila., 1847, vol. III, p. 265, plate II); but later Equus complicatus (Proc. cit., 1858, p. 11). In 1901 (Bull. Amer. Mus. Nat. Hist., vol. XIV, p. 109, fig. 7), Gidley selected one of the teeth, that of Leidy’s plate II, figs. 1, 6, referred to above, as the special type of the species Equus complicatus. These Natchez teeth are now in the collection of the Philadelphia Academy of Natural Sciences.

Some of the teeth from Natchez were described by Leidy in 1860 (Holmes’s Post-Pliocene Fossils of South Carolina, pp. 100–105, plate XV, figs. 11–15, plate XVI, figs. 24–26, 30, 31) as Equus complicatus. Others (pp. 100105, plate XV, figs. 17, 18, plate XVI, fig. 27) were referred to a hitherto unrecognized species Equus fraternus.

TENNESSEE.

(Map 17. Figure 23.)

1. Rogersville, Hawkins County.—In the U. S. National Museum (No. 520) is a single horse-tooth found many years ago in a crevice in a marble quarry at this place. It is referred by the writer to Equus leidyi (Proc. U. S. Nat. Mus., vol. LVIII, p. 84). With it were sent a canine tooth and a few bones of a peccary, described as Mylohyus setiger (p. 394).

2. Whitesburg, Hamblen County.—In 1885 Mr. Ira Sayles collected at this place a lot of bones and teeth of vertebrates, described by the present writer (Proc. U. S. Nat. Mus., vol. LVIII, p. 87). Among them is an upper right second premolar of a horse, identified as Equus leidyi. A list of the species will be found on page 395. E. littoralis also is present.

3. Lookout Mountain, Hamilton County.—In the American Museum of Natural History, New York, is an upper second molar tooth brought from Lookout Mountain (Gidley, Bull. Amer. Mus. Nat. Hist., vol. XIV, p. 121). Under what conditions this tooth was found have not been recorded. It belongs probably to the species Equus littoralis.

4. Nashville, Davidson County.—From William Edward Myer, of Nashville, Tennessee, the writer received, June 26, 1920, some fossils collected near Nashville, about 300 yards upstream from Lock A, in Cumberland River, at a depth of nearly 30 feet beneath a bank of gravel. Below this gravel is a bed of sand apparently 2 or 3 feet thick and this is underlain by another bed of gravel apparently about 2 feet thick. This itself lies on bed-rock at about the level of low water in the river. In the lower gravel were found a lower molar of Equus leidyi, a part of a left femur of a large horse, and an antler of a small undetermined and probably undescribed deer. In the layer of sand were discovered a heel bone of a camel, a part of a tooth of a young mastodon, and some fragments of turtle bones. The equine tooth belongs to the right side. It has a height of about 80 mm., a length of 28 mm. on the grinding-surface, and a width of 16 mm. It is black, and like the others thoroughly fossilized.

The fragment of femur appears to have belonged to a horse perhaps larger than Equus leidyi. It begins at the lower border of the third trochanter and descends to the lower part of the deep fossa for the plantaris muscle. Immediately above the fossa the side-to-side diameter of the bone is 50 mm., the fore-and-aft 60 mm. In a horse of medium size these diameters are respectively 45 mm. and 53 mm.

Later there was discovered at the same locality the upper two-thirds of the right metatarsal. The fragment is 230 mm. long. The upper articular end is somewhat injured; 75 mm. below the upper end the fore-and-aft diameter is 45 mm., the side-to-side diameter 38 mm. The latter diameter was somewhat greater, as the bone appears to be slightly crushed. The specimen is referred to Equus complicatus. Probably the femur mentioned above belonged to this species.

KENTUCKY.

(Map 17.)

1. Bigbone Lick, Boone County.—In their report published in 1831 (Amer. Jour. Sci., vol. XX, p. 371), Cooper, Smith, and Dekay reported they found in the collection from this place large teeth and bones of a horse. They regarded these as being of equal antiquity with the extinct animals associated with them. In 1847 (Proc. Acad. Nat. Sci. Phila., vol. III, p. 263, 264) Leidy stated that there were in the Academy 10 permanent molars of a horse from Bigbone Lick. These he referred to Equus curvidens. In 1853 (Jour. Acad. Nat. Sci. Phila., vol. VII, p. 263) he wrote that several teeth supposed to have come from this locality had possibly been obtained elsewhere.

In 1851 (Proc. Acad. Nat. Sci., Phila., p. 140), he spoke of foot-bones of the horse, a calcaneum and first phalanx, from the same place. In 1860 (Holmes’s “Post-Pliocene Fossils of South Carolina,” p. 104), Leidy mentioned several horse-bones from Bigbone Lick presented to the American Philosophical Society by President Jefferson. In Rochester University are 2 hoof phalanges labeled from Bigbone Lick. Osborn (“Age of Mammals,” p. 478) puts down Equus from Bigbone Lick as being doubtful. There appears to be no good reason for this.

The remains of horses from this locality appear all to belong to Equus complicatus.

2. Monday’s Landing, Mercer County.—From Professor Arthur M. Miller, of the University of Kentucky, the writer has received for examination a much-worn upper left molar or premolar of a horse found at the place named. It was met with in a fissure filled with crystallized calcite, near the bank of Kentucky River. The vein of calcite was about 6 feet wide. Similar veins at this locality have been worked down to a depth of 200 or 300 feet. A part of a lower jaw of a deer-like animal was found in one of these veins. The horse-tooth is badly worn, but it appears to have belonged to a small species, the fore-and-aft length of the crown being only 19 mm. The enamel of the anterior lake is considerably complicated. It is impossible, from the lack of other fossil remains, to determine the geological age of this horse.

FINDS OF PLEISTOCENE TAPIRIDÆ IN EASTERN NORTH AMERICA.

PENNSYLVANIA.

(Map 19.)

1. Port Kennedy, Montgomery County.—In 1871, Wheatley announced (Amer. Jour. Sci., ser. 3, vol. I, p. 384) that he had discovered in the Port Kennedy bone cave 2 species of tapirs (Tapirus americanus and T. haysii). In 1899 (Jour. Acad. Nat. Sci., Phila., vol. II, p. 253), Cope stated that remains of 35 or more tapirs had been discovered in this cave. He referred all to T. haysii. These tapirs will be mentioned again on page 312, where the geological relations of the cave and its contents are considered.

2. Frankstown, Blair County.—In 1908, Dr. W. J. Holland reported (Ann. Carnegie Mus., vol. IV, p. 231) found in a bone cave at Frankstown the third and fourth lower premolars of a tapir about the size of Tapir americanus, which name is a synonym of T. terrestris. This will be mentioned in the discussion of the geology of the region on page 321.

OHIO.

(Maps 19, 36.)

1. New Salisbury?, Columbiana County.—Somewhere in the region probably of the town named was found, about 1850, a jaw of a tapir, apparently mentioned first by Louis Agassiz (Proc. Amer. Assoc. Adv. Sci., vol. V, 1851, p. 179), who referred to it as a jaw of a pachyderm. Leidy, in 1860 (Holmes’s “Post-Pliocene Fossils of South Carolina,” p. 107), reported that he had studied a much-mutilated fragment of the lower jaw of the smaller variety of the extinct tapir, which had belonged to Professor J. Brainerd, of Cleveland. It had been found in the valley of Yellow Creek, in Columbiana County, in an erosion of the coal series. It was covered with 30 feet of clay, at a height of 186 feet above low-water in Ohio River. Charles Whittlesey, in 1866 (Smithson. Contrib. Knowl., vol. XV, art. 3, p. 16), stated that this specimen was taken from “valley drift,” of Yellow Creek, in Columbiana County, by Mr. E. White, C. E., in a cut of the Pennsylvania Railroad. Inasmuch as Yellow Creek itself does not enter the county named, reference must be to what is called, on the topographical sheet of the U. S. Geological Survey, North Fork of Yellow Creek. The railroad follows this creek for many miles in the county. The town of New Salisbury is taken as being probably not far from the locality. It is not known what became of this specimen, nor is it possible to say to which species it belonged. It is to be referred probably to the Sangamon stage.

INDIANA.

(Map 19.)

1. Evansville, Vanderburg County.—Tapir remains have been found at only one place in Indiana, viz, in the banks of the Ohio River at the mouth of Pigeon Creek, a short distance below Evansville. A single lower hinder molar formed part of a collection made by Mr. Francis A. Lincke and described by Leidy (Proc. Acad. Nat. Sci. Phila., 1854, p. 199). This tooth was figured by Leidy in 1860 (Holmes’s “Post-Pliocene Fossils of South Carolina,” p. 107, plate XVII, figs. 9, 10) under the name Tapirus haysii. Associated with the tooth were remains of Megalonyx jeffersonii, a bison of probably an extinct species, the Virginia deer, the horse known as Equus complicatus, and the large extinct wolf Ænocyon dirus.

On page 32 is discussed the probable age of the bone-bed which contained the animals named above. It is concluded that the age is possibly the Aftonian, but more probably the Sangamon. This species of tapir has been found at Bigbone Lick, Kentucky, between Louisville and Cincinnati, in deposits containing Equus complicatus, 2 extinct species of Bison, deer, etc. The deposits lie on Illinoian drift and are in part, at least, of Sangamon age.

MARYLAND.

(Map 19.)

1. Corriganville, Allegany County.—In a crevice in limestone rock, at a point about 3 miles west of north of Cumberland, Mr. J. W. Gidley found a tooth of a tapir. The tooth has never been specifically identified. A list of the associated species, as far as determined, will be given on page 350.

VIRGINIA.

(Map 19.)

1. Ivanhoe, Wythe County.—In 1869 (Proc. Amer. Philos. Soc., vol. XI, p. 176), Cope announced the discovery of several lower molars of a tapir in what he regarded as cave breccia, along New River. These teeth he found to be somewhat larger than those of T. terrestris, the Central and South American species, and he referred them to Tapirus haysii. A list of the species found here is given on page 353.

SOUTH CAROLINA.

(Map 19.)

1. Charleston, Charleston County.—In 1860 (Holmes’s “Post-Pliocene Fossils of South Carolina,” p. 106, plate XVII, figs. 2, 3), Leidy described briefly and figured 2 injured upper cheek-teeth of a tapir found in the Pleistocene of Ashley River, and referred by him to Tapirus americanus fossilis, on the supposition that they were not different from those of the existing South American tapir, but larger. The larger of the two teeth (fig. 2) appears to have had a fore-and-aft diameter of about 29 mm. It seems, therefore, to belong to Leidy’s species Tapirus haysii. Under the same name, T. americanus fossilis, Leidy illustrated (figs. 11, 12) a lower molar found on Ashley River. This appears to be too small to have belonged to T. haysii. Instead, however, of referring it to T. americanus (=T. terrestris) it may possibly be found to belong to T. veroensis Sellards, the lower molars of which are not certainly known. The length of the tooth figured by Leidy is that of a second molar of T. terrestris, but the width is greater than in the latter.

In the Charleston Museum is a part of a left ramus of the lower jaw of a tapir likewise referred to T. veroensis Sellards. This fragment contains all 3 of the true molars. The following measurements were secured:

Measurements, in millimeters, of lower molars of tapirs in the Charleston Museum.

┌───────────────────────────────┬───────────────┬───────────────┐ │ │ Tapirus │ │ │ │ veroensis? │Tapirus haysii.│ ├───────────────────────────────┼───────┬───────┼───────┬───────┤ │ │Length.│Width. │Length.│Width. │ ├───────────────────────────────┼───────┼───────┼───────┼───────┤ │Length of all 3 molars combined│66 │ │79 │ │ │First molar │20 │17 │25 │28 │ │Second molar │23 │18.5 │26 │31.5 │ │Third molar │24 │18 │28 │32 │ └───────────────────────────────┴───────┴───────┴───────┴───────┘

In the collection of Charles C. Pinckney, at Lambs, South Carolina, are 2 tapir teeth, one of which is an upper molar, not yet come into use, apparently the last tooth of the right side. The length of the crown is 25.5 mm., the width in front 27.5 mm., behind about 23 mm. In front is a pretty strong cingulum, but there is none behind. This tooth is referred to Tapirus haysii.

In the Scanlan collection from Charleston, now the property of Yale University, are various specimens of tapirs. An upper left second molar is slightly worn. The length is 24 mm., the width 30 mm. The outer border of the crown makes a right angle with the anterior border; in T. terrestris the outer anterior corner is considerably less than a right angle. In the latter the hinder faces of the protocone and of the hypocone are concave; in the tooth here described both hinder faces are swollen, and the crests appear more depressed than in T. terrestris. It is regarded as belonging to T. haysii.

In the Scanlan collection are 3 lower molars which the writer refers to T. haysii. The following are the measurements:

Measurements, in millimeters, of lower molars of tapirs in the Scanlan collection.

┌────────────────────────────────────────────────────┬───────┬───────┐ │ │Length.│Width. │ ├────────────────────────────────────────────────────┼───────┼───────┤ │Left third? molar, with the rear cingulum broken off│28± │22.5 │ │Left second molar │25.5 │21 │ │Right second molar │27 │21 │ └────────────────────────────────────────────────────┴───────┴───────┘

In the Scanlan collection is a fragment of the left maxilla with 4 teeth, the last premolar and the 3 molars. The specimen resembles figure 1 of Leidy’s plate XVII of Holmes’s “Post-Pliocene Fossils of South Carolina.” The teeth of the Scanlan specimens are, however, less worn. The hinder molar had not yet come through the gum. The specimen is referred to T. terrestris. The following are the measurements:

Measurements, in millimeters, of upper teeth of Tapirus terrestris.

┌─────────────┬───────────────────────────┬───────────────────────────┐ │ Tooth. │ Tapir from Charleston. │ T. terrestris, U. S. Nat. │ │ │ │ Mus. No. 238110 │ ├─────────────┼─────────────┬─────────────┼─────────────┬─────────────┤ │ │ Length. │ Width. │ Length. │ Width. │ ├─────────────┼─────────────┼─────────────┼─────────────┼─────────────┤ │ Pm^1 │19 │24.5 │19 │25 │ │ M^1 │20 │25.5 │21 │23 │ │ M^2 │22.5 │28 │23.5 │27 │ │ M^3 │24.5 │27.5 │25.5 │26 │ └─────────────┴─────────────┴─────────────┴─────────────┴─────────────┘

The molar teeth have an acute angle between the anterior and the outer borders, and the front and the hinder faces of the protocone and the hypocone are not so swollen as in the tooth referred to T. haysii. In apparently every respect the teeth of the fossil agree with the teeth of Tapirus terrestris from Brazil. It is to be hoped that before long a good skull of the Pleistocene tapir whose teeth so closely resemble those of T. terrestris will be discovered. If the two prove to be the same species it will seem that only the descendants of those which migrated to North America perished during the Glacial period.

There is another tooth, an upper left second molar, of T. terrestris in the Scanlan collection; also the rear half of an upper molar labeled as coming from Bull River. Other fragments of teeth are recorded as coming from Ashley River.

In the Charleston Museum (No. 13495) is a part of the left ramus of the lower jaw with the 3 molars. On measurement it is found that the teeth and jaw agree closely with those of T. terrestris.

GEORGIA.

(Map 19.)

1. Brunswick, Glynn County.—In Bulletin No. 26 of the Geological Survey of Georgia, Mr. J. W. Gidley published a list of species of vertebrate fossils which belong to the State collection at Atlanta, secured during some dredging operations at Brunswick. This list, with modifications, is incorporated in that presented on page 370. Among the fossils examined by Gidley, a tooth was recognized as that of Tapirus haysii.

FLORIDA.

(Map 19.)

1. Neals, Alachua County.—Through the kindness of Dr. E. H. Sellards, State geologist of Florida, the writer has been permitted to examine various teeth (No. 1186, Florida Geological Survey) taken from the T. A. Thompson phosphate mines at Neals. Among these is a lower left milk molar of a tapir. The length of the crown is 21 mm., the width at the front lobe 14 mm., at the hinder lobe 12.5 mm. The buttresses are well developed. The tooth may be provisionally referred to Tapirus terrestris, yet living in Brazil. Although this tooth was found in phosphate materials, it seemed to Dr. Sellards more probable that it was an intrusion from Pleistocene deposits. The present writer refers the Alachua clays to the Nebraskan stage of the Pleistocene. Sellards has referred to this tooth in his Eighth Annual Report, 1916, p. 94.

2. Archer, Alachua County.—In 1884 (Proc. Acad. Nat. Sci. Phila., 1884, p. 119), Leidy briefly described a tooth of a tapir found by Dr. J. C. Neal, of Archer, Florida. This is now in the U. S. National Museum, No. 3329. The tooth is the third premolar of the left side, implanted in a fragment of maxilla. The crown is 23 mm. long and 27 mm. wide. Leidy stated that it differed neither in form nor size from the corresponding tooth of the living Tapirus americanus (T. terrestris); but in a specimen of this the corresponding tooth is only 18.5 mm. long and 25 mm. wide. The fossil agrees in size with the same tooth of T. haysii from the Port Kennedy Cave in Pennsylvania (Hay, Geol. Surv. Indiana, vol. XXIII, p. 593). With this tooth had been found teeth of a young mastodon, remains of several individuals of a species of rhinoceros, some foot-bones of a llama, a calcaneum which Leidy thought possibly belonged to the extinct Cervus americanus (Cervalces scotti), and vertebral centra of a small crocodile. The cervalces was afterwards dropped from the lists. These remains had been found in a bed of clay, occupying a ridge in a pine forest. The deposits are now known as the Alachua clays, and they, as well as the contained fossils, will be discussed on page 375. The tapir remains are not included in Leidy’s list given in Bulletin 84 of the U. S. Geological Survey.

3. Dunnellon, Marion County.—The writer has examined a number of tapir teeth found in phosphate beds in Withlacoochee River, at Dunnellon. From the Florida geological survey an upper left second premolar (No. 1440) has been received which is considerably larger than the corresponding tooth of Tapirus terrestris and presents other peculiarities. It may have belonged to T. haysii. An upper second true molar (No. 1440) has the crown 23 mm. long, 27 mm. wide across the front lobe, and 23 mm. across the hinder lobe. The corresponding dimensions of a specimen of T. terrestris from Surinam are 24 mm., 25.5 mm., and 21.5 mm. A tooth (No. 1378) which appears to be the lower left second molar is 22.5 mm. long, 19 mm. wide in front, and 20 mm. wide behind. The corresponding measurements of T. terrestris are 22.5 mm., 18.5 mm., and 17.5 mm. The buttresses which descend from the outer ends of the crests of the fossil tooth are not so strongly developed as in T. terrestris. Probably these teeth belong to an undescribed species. An upper molar having a length of 23 mm. has been shown the writer by Dr. L. W. Stephenson; it was found in phosphate deposits at Dunnellon and sent to him by Sister M. Catherine, of St. Joseph’s Academy, at St. Augustine.

4. Near Ocala, Marion County.—Mr. J. D. Robertson, of Ocala, presented to the National Museum a tooth of a tapir, found in phosphate deposits a few miles from Ocala, section 5, township 15 south, range 23 east.

5. Tampa, Hillsboro County.—In the collection of fossils, at Vanderbilt University, made from the phosphate-producing beds in Hillsboro County, is part of the left ramus of a lower jaw of a tapir containing the first and second true molars. The first molar has a length of 24 mm. and a width of 20 mm. in front. This is smaller than the corresponding tooth of T. terrestris and near that supposed to belong to T. veroensis. The second molar has lost its hinder crest. Under the first molar the jaw is 54 mm. deep and 37 mm. thick.

The writer (Fossil Turtles of North America, p. 361) reported the finding of tapir teeth in Alafia River, in this county.

6. Vero, St. Lucie County.—At this important locality remains of tapirs have been found in the bed of sands known as No. 2, and likewise in the bed of muck mentioned in discussions of the locality as No. 3. From the latter have been secured parts of 2 lower jaws and a number of detached teeth (Sellards, 8th Ann. Rep., p. 149). One at least of these (No. 6943) appears to belong to Tapirus haysii. From No. 2 Dr. Sellards has obtained a nearly complete skull of a tapir, described (10th and 11th Ann. Rep. Fla. Geol. Surv., p. 57, plates I-IV) as Tapirus veroensis. From the same stratum he (8th Ann. Rep., p. 139) secured a part of a tooth which he referred with some doubt to T. haysii.

7. Arcadia, De Soto County.—Dr. Joseph Leidy (Trans. Wagner Free Inst., vol. II, p. 19) stated he had examined 3 crowns of upper molars and fragments of others. In no way did he find them differing from those of the South American tapir, T. americanus (T. terrestris). On page 380 will be found a list of the vertebrate fossils found in this vicinity.

MISSISSIPPI.

(Map 19.)

1. Natchez, Adams County.—In 1849 (Proc. Acad. Nat. Sci. Phila., vol. IV, p. 182), Dr. Leidy wrote that there was in the collection of the Academy a tooth of a tapir discovered by Dr. M. W. Dickeson near Natchez. It had been found in association with remains of the mastodon and the horse Equus americanus (=E. complicatus). The tooth was pronounced a lower molar of the left side, apparently the third milk molar, and was referred to Tapirus americanus fossilis; that is, it was looked upon as a fossil tooth of the existing South American tapir. The molar was mentioned by Leidy in 1860 (Holmes’s “Post-Pliocene Fossils of South Carolina,” p. 106). The writer has seen this tooth in the Academy of Natural Sciences at Philadelphia.

In 1852 (Proc. Acad. Nat. Sci. Phila., vol. VI, p. 148), Leidy called the attention of the Academy to a fragment of a left lower jaw with 2 teeth of a tapir found in the Pleistocene near Natchez and sent to Leidy by the geologist B. L. C. Wailles. It was referred to Tapirus haysii. This specimen was figured and described by Leidy in 1860 (Holmes’s “Post-Pliocene Fossils of South Carolina,” p. 107, plate XVII, figs. 4, 5). Wailles mentioned this jaw in his work (Agric. Geol. Mississippi, 1854, p. 285), and stated that it was found in a ravine on Pine Ridge, which runs through townships 7 and 8, range 3 west, about 6 miles north of Natchez.

In a list (furnished by Dr. Joseph Leidy) of fossil mammals found in the Pleistocene of Mississippi, 2 species of tapirs are included, viz, Tapirus americanus (=T. terrestris) and T. haysii (Wailles, op. cit., p. 286; Hilgard, Agric. Geol. Mississippi, 1860, p. 196). The associated species will be listed on page 391.

TENNESSEE.

(Map 19. Figure 23.)

1. Whitesburg, Hamblen County.—In the U. S. National Museum is a collection of bones and teeth of several species of vertebrates, made in what may once have been the floor of a cave, near the village mentioned. On page 395 will be found a list of the species. Among the remains are 10 teeth, in fine preservation, of a young tapir, described by the writer (Proc. U. S. Nat. Mus., vol. LVIII, p. 88, plate III, figs. 4 to 11), and made the type of a new species, Tapirus tennesseæ.

2. Dandridge, Jefferson County.—On the left bank of Dumplin (or Dumpling) Creek, about 5 miles above its entrance into French Broad River, and apparently about as many miles northwest from Dandridge, is a cavern known as Zirkel’s Cave. Dr. H. C. Mercer briefly described (Dept. Amer. and Prehist. Archæology, Univ. Penn., 1896) his investigation of the cave. He reported the finding of remains of tapir, peccary, bear, and small rodents; but these were not specifically determined.

3. Lookout Mountain, Hamilton County.—In 1894 (Amer. Naturalist, vol. XXVIII, p. 356), Mercer reported that he had found teeth of a tapir in a cave on Lookout Mountain. Cope, on page 597 of the same volume, identified these teeth as those of T. haysii. With them was found a bone, thought to belong to a mylodon.

According to a letter received by the writer from Dr. Mercer, the tapir specimen consisted of a lower right ramus, 1 left incisor, and 5 molars. The teeth appear all to have been loose and the jawbone was broken into about 8 fragments. The cave and its contents will be discussed on page 398.

4. Bristol, Sullivan County.—In the U. S. National Museum are 2 tapir teeth in a fragment of the left maxilla. These are the fourth premolar and the first molar, both considerably worn. The size of these teeth indicates that they belong to Tapirus haysii.

KENTUCKY.

(Map 19.)

1. Bigbone Lick, Boone County.—The evidences for the occurrence of a species of tapir at this place are not as convincing as might be desired. In 1852, Dr. I. Hays (Proc. Acad. Nat. Sci. Phila., vol. VI, p. 53) presented to the Academy a tooth of a tapir which he had had in his possession two years and which was said by him to have come from the bed of a canal in North Carolina. This tooth was named by Leidy Tapirus haysii on page 106 of the volume cited and again on page 148, but without description. It was again mentioned by him in 1853 (Jour. Acad. Nat. Sci. Phila., vol. VII, p. 201) and again without description. In 1860, Leidy (Holmes’s “Post-Pliocene Fossils of South Carolina,” p. 106, plate XVI, figs. 7, 8) described and figured the tooth and stated that it was supposed to have come from Bigbone Lick. Which of the statements was correct the writer does not know.

2. Stamping Ground, Scott County.—In 1910 the writer received for examination from Professor Arthur M. Miller, professor of geology in the State University at Lexington, Kentucky, a part of a lower jaw of Tapirus haysii, found between the town named and Georgetown, in the bottom of a filled-up sink-hole encountered in lead-mining operations, on McConnell’s Run. In this specimen all the molars are complete and the roots of the 3 hinder premolars are present.

3. Yarnallton, Fayette County.—From Professor Miller there was received with the specimen above described pieces of the jaws of Tapirus haysii, discovered in an old stream-deposit at the place named. A fragment of a lower jaw was sent; also a piece of a right maxilla, with the anterior true molar complete and parts of the second molar and of the hindermost premolar. Some other parts of the skeleton were found, but they seem not to have been cared for.

FINDS OF RHINOCEROSES IN EASTERN NORTH AMERICA.

FLORIDA.

1. Archer, Alachua County.—Two species of rhinoceros have been described from this locality. In 1884 (Proc. Acad. Nat. Sci. Phila., p. 118), Dr. Joseph Leidy reported the discovery, with other fossils, of remains of a species of the genus Rhinoceros in Alachua clays, but he gave it no name. This was, however, done in 1885 (same Proceedings, 1885, p. 32). In 1896, after the death of Leidy, his unfinished paper, completed and edited by Professor F. A. Lucas, was published (Trans. Wagner Free Inst. Sci., vol. IV, p. 41 seq., with numerous figures). This species is now referred to Teleoceras, as Teleoceras proterus.

In 1890 (Proc. Acad. Nat. Sci. Phila., 1890, p. 94), Leidy described another species which he called Rhinoceros longipes, from the same place and deposit. This species is now called Aphelops longipes.

These species are usually credited to the Upper Miocene or Lower Pliocene. The reader is referred to page 376, where the geological position of these beds is discussed.

2. Williston, Levy County.—In his list of 1892 (Bull. U. S. Geol. Surv., No. 84, p. 129), furnished by Leidy, W. H. Dall included Rhinoceros proterus among the fossils found at Mixon’s, near the village of Williston.

3. Dunnellon, Marion County.—In 1913 (5th Ann. Rep. Florida Geol. Surv., p. 58), Dr. E. H. Sellards stated that some remains of a rhinoceros had been found in the mines worked along Withlacoochee River, in the region about Dunnellon. In volume VIII of the Florida Survey, page 94, Aphelops malacorhinus (=A. longipes) is included among the fossils found in the Dunnellon formation. It is not included in his list of Pleistocene species found in the Withlacoochee River (Florida Geol. Surv., vol. VIII, p. 104). This was doubtless because he regarded it as belonging to an earlier formation.

4. Mulberry, Polk County.—In 1915 (7th Ann. Rep. Florida Geol. Surv., p. 72), Sellards stated that a tooth of Teleoceras fossiger (in the present work recognized as T. proterus) had been discovered in the Bone Valley phosphate formation, at the place named. As in other cases, the Bone Valley formation was referred to the Late Tertiary.

5. Brewster, Polk County.—In the volume last referred to, on page 72, Sellards mentions parts of jaws and teeth found in a phosphate mine at Brewster which are different from those of Teleoceras proterus. Some of these are figured by Sellards on his pages 107 and 108. They have not been specifically or generically determined.

FINDS OF PLEISTOCENE PECCARIES IN EASTERN NORTH AMERICA.

NEW YORK.

(Map 20.)

1. Rochester, Monroe County.—In 1889 (Trans. Wagner Inst. Sci., vol. II, pp. 33–40), Leidy described and figured a skull of Platygonus compressus, purchased of Ward’s Natural Science Establishment, at Rochester, and said to have been found in a gravel bank in a railroad excavation, a few miles from Rochester. This skull was a part of 2 incomplete skeletons found lying together.

The writer received word from Professor Henry L. Ward, director of the Milwaukee Public Museum, that he recollects that, when a small boy, about 1873 or 1874, he went with his father, Henry A. Ward, to some point on the New York Central Railroad, where peccary remains had been found. He thinks the place was at or near Pittsford. Dr. F. A. Lucas, director of the American Museum of Natural History, New York, then in the employ of the elder Ward, writes that the place was at Pittsford, and in a gravel bank being worked by the railroad company to obtain materials for a fill. The exact depth at which the bones were found is not recalled, but it was not great.

The locality, according to Fairchild’s plate 42 (Bull. 127, State Mus., New York), is on the predecessor of Irondequoit Bay, extending out from Lake Iroquois. The peccaries possibly lived rather early in the late Wisconsin stage; but more probably their time of existence was considerably later, when the climate had become milder.

2. Gainesville, Wyoming County.—From Mr. C. A. Hartnagel, assistant State geologist of New York, the writer received notice of the discovery, in 1914, of the remains of 2 peccaries at a point about one-third of a mile northwest of Gainesville. The remains consist of 2 nearly complete skulls, parts of 5 ribs, 2 scapulæ, 2 metacarpals, 1 innominate bone, 1 ilium, 1 radius, 1 ulna, and 2 tibiæ. These have been identified by Dr. John M. Clarke as belonging to Platygonus compressus.

The manner of burial of these peccaries is puzzling and interesting. They were found in a hill, or drumlin, which stands out on a plain of considerable extent and whose long axis runs north and south. The elevation is 1,625 feet above sea-level. The drumlin is about 600 feet long, about 300 feet wide, and 40 feet high. It is composed of sand, gravel, and stones up to a foot in diameter. The bones are said to have been discovered by a contractor who was removing sand and gravel. The bones were at the south end of the drumlin and buried in a considerable pocket of sand. Those reporting the position of the bones place them at least 10 feet from the surface, and perhaps as much as 30 feet. Mr. Hartnagel thinks it is almost necessary to suppose that the skeletons were there when the drumlin was built. To the writer it would appear still more difficult to explain how they happened to be there at that time.

NEW JERSEY.

(Map 20.)

1. Shark River, Monmouth County.—In 1869 (Jour. Acad. Nat. Sci. Phila., vol. VII, p. 387), Leidy described a tooth of a peccary shown to him by Timothy Conrad, but found by Dr. P. Knieskern, supposedly in a Miocene formation of Shark River. Leidy expressed the conclusion that the tooth resembled very closely a premolar of Dicotyles nasutus, now called Mylohyus nasutus. It is very probable that the tooth had gotten into Miocene materials by accident or that there was some error in the history, and that it really belonged to a Pleistocene peccary.

PENNSYLVANIA.

(Map 20.)

1. Stroudsburg, Monroe County.—Leidy (Proc. Acad. Nat. Sci. Phila., 1880, p. 347) reported Dicotyles nasutus from the Crystal Hill (Hartman’s) cave near Stroudsburg; but later (Ann. Rep. for 1887, Pennsylvania Geol. Surv., p. 8, plate II, figs. 3–6) he described the teeth and parts of the jaws as Dicotyles pennsylvanicus. This species will be found on page 310 under the name Mylohyus pennsylvanicus, in the list of fossils found in this cave. There too will be found a discussion of the location of the cave and the probable age of the remains.

2. Port Kennedy, Montgomery County.—In the bone cave at this place have been found 3 species of peccaries. Cope, in 1899 (Jour. Acad. Nat. Sci. Phila., ser. 2, vol. II, pp. 259–263) described these under the names Mylohyus tetragonus, M. pennsylvanicus, and M. nasutus. The first was a new species, based on a damaged lower jaw with some of the teeth (op. cit., plate XXI, figs. 3–3b). For the present the writer refers it to the genus Tagassu, inasmuch as the interval between the canine and the first premolar (pm^2) is only half the length of the whole tooth row, and the molars have the structure found in Tagassu. Some teeth belonging to an upper jaw were referred with doubt to this species. They may have belonged to Mylohyus pennsylvanicus. Of the species last named, Cope had fragments of 2 lower jaw’s with some teeth in them and some teeth free from the jaws. Of Mylohyus nasutus, Cope had from the cave only an upper canine and its reference to this species is uncertain.

On page 312 will be found a list of the species of vertebrates found in the Port Kennedy Cave; also remarks on their geological age.

3. Milroy, Mifflin County.—In 1882, Leidy described (Proc. Acad. Nat. Sci. Phila., 1882, p. 302) a species of peccary found in a limestone cave in the county named, but he gave no more exact information; nor did he do so in his two subsequent references to it in 1889 (Trans. Wagner Inst., vol. II, p. 49; Ann. Rep. Geol. Surv. Pennsylvania for 1887, p. 12, plate II, figs. 1, 2). The specimen is in the Academy of Natural Sciences at Philadelphia. In the Pennsylvania survey, as quoted, the giver is called John Schwarzer. The name of the species is Platygonus vetus. The writer has been informed by J. C. Swigart, county surveyor of Mifflin County, that the proper name of the donor of the specimen was John Swartzell, a former surveyor who lived near Milroy and who was much interested in geology.

From Professor Mosheim Swartzell, of Washington, D. C., son of John Swartzell, the writer has received a letter in which are given this son’s recollections regarding the finding of the specimen in question. He states that it was discovered in Naginey’s limestone quarry, 1.5 miles south of Milroy. It came from a considerable, but now unknown, distance from the surface and was first noticed in the débris of the quarry. While Mr. John Swartzell was observing it, an ignorant workman struck it with a tool and damaged it, exclaiming that it was only the jaw of a hog. It was later sent to Philadelphia. Professor Swartzell writes that there was a cave not far away, but that the jaw was not found in it; it probably had fallen down into a crevice of the limestone.

4. Frankstown, Blair County.—In 1908 (Ann. Carnegie Mus., vol. IV, p. 231), Dr. W. J. Holland reported remains of a number of peccaries found in a bone cave at the place named. He mentioned especially Dicotyles pennsylvanicus, but thought it belonged properly in Platygonus. It is probably to be referred to Mylohyus as M. pennsylvanicus.

OHIO.

(Maps 20, 36.)

1. Wilmington, Clinton County.—In the collection of the Archæological and Historical Museum of the University of Ohio, at Columbus, are considerable parts of the jaws, teeth, and other parts of the skeleton of a specimen of Platygonus compressus exhumed at a point about 4.5 miles north of west of Wilmington. The locality is given as being in the northeast corner of Adams Township, south of the road running northeast and southwest between Todd and Dutch Creeks; also about 0.6 mile south of the north line of Adams Township and about 0.75 mile from the east line. It would therefore be near the second northwesterly directed loop of Todd Creek in that neighborhood.

2. Columbus, Franklin County.—In 1875 (Proc. Amer. Assoc. Adv. Sci., vol. XXIII, Hartford, pp. 1–6; also in Cin. Quart. Jour. Sci., vol. II, pp. 1–6), J. H. Klippart gave an account of the finding of about a dozen skeletons of Platygonus compressus. These were buried in 2 “nests” not far from each other. The bones were rather brittle and were damaged somewhat in exhuming them. The place of burial was in the bank (apparently the right) of Olentangy River, at the crossing of Olentangy and Montgomery streets. The remains were here buried in a sand-bank. One lot of 6 of the smallest animals was found in penetrating the sand bank about 20 feet from the entrance and at a depth of 8 feet from the surface. They were embedded in calcareous clay and sand. The other 6 and largest animals were found about 6 feet farther in and about 4 feet deeper. It appears that all the animals were lying with their snouts directed toward the southeast. Klippart thought that they had been destroyed suddenly and violently. It is, however, probable that they had been frozen in their beds during a winter storm. Of these skeletons it appears that half went to Professor O. C. Marsh, of Yale University, and the present writer has had the privilege of studying them. The geological age of the animals will be considered on page 330.

3. Chalfants, Perry County.—In the collection of the Archæological and Historical Museum at the University of Ohio are considerable parts of a specimen of Platygonus compressus found not far from Jonathan Creek, about a mile northeast of Chalfants. The locality, as given the writer by Professor W. C. Mills, is as follows: center of southwest quarter of section 14, township 17 north, range 16 west. The name of the political township is Hopewell. The locality appears to be on the area covered by Illinoian drift. This fact makes it possible that the animals lived during the Sangamon stage.

4. Lisbon, Columbiana County.—In the collection just mentioned is the left ramus of a lower jaw of a peccary which the writer referred with doubt to Mylohyus nasutus Leidy. It lacks so much of the front end that only 18 mm. of the symphysis is present; also, the ascending ramus is broken off. There are present the 3 milk molars and the first molar, but this is yet in its cavity in the bone. A comparison with Leidy’s M. pennsylvanicus seems to show that the jaw did not belong to that species. Of M. nasutus no lower jaw is known.

Table of measurements, in millimeters.

┌─────────────┬───────────────────────────┬───────────────────────────┐ │ Specimen. │ Lisbon jaw. │ M. penn. │ ├─────────────┼─────────────┬─────────────┼─────────────┬─────────────┤ │ │ Length. │ Width. │ Length. │ Width. │ ├─────────────┼─────────────┼─────────────┼─────────────┼─────────────┤ │ Dm_{2} │ 9│ 5│ 7│ 4.5│ │ Dm_{3} │ 12│ 8│ 11│ 7│ │ Dm_{4} │ 19.5│ 11│ 18│ 10.5│ │ M_{1} │ 16.5│ 12│ 16│ 13│ └─────────────┴─────────────┴─────────────┴─────────────┴─────────────┘

This specimen was found near the southern edge of Lisbon, on Middle Fork of Little Beaver Creek, in the northwest quarter of the northeast quarter of section 24, township 18 north, range 3 west. The locality is apparently outside of the glaciated area; and it is at present impossible to determine the geological age of the animal beyond that it undoubtedly belongs to the Pleistocene. The writer believes that Mylohyus nasutus did not survive the Wisconsin ice-stage. The specimen was described and figured by the writer in 1914 (Iowa Geol. Surv., vol. XXIII, p. 226, plate XXV, figs. 4–6).

MICHIGAN.

(Map 36.)

1. Belding, Ionia County.—So far as the writer knows, no species of peccary has been found in the State of Michigan, except at Belding. The remains are in the palæontological collection of the University of Michigan, at Ann Arbor, and belong to the species Platygonus compressus Le Conte. The remains are said to consist of bones of 5 individuals; and Mr. N. A. Wood, preparator at the university, informed the writer there are 294 bones. The skull of one of the 5 individuals was missing when the collection was made. The skeletons were found in a peat-swamp, in 1877, and were sent to Professor Alexander Winchell by Mr. A. Tuttle. A skull belonging to this collection was described in 1903 (Jour. Geology, vol. XI, p. 777, figs. 1–4) by Mr. George Wagner.

It seems probable that there, as in two or three other known cases, a herd of these animals, asleep together, had succumbed to rigorous weather, probably to a winter blizzard.

Belding is situated on Flat River, a tributary of Grand River. It lies close to a part of the Charlotte moraine system, thought to be correlated with the Valparaiso system. These peccaries could not have lived in that region until after the Wisconsin ice had retired into Lake Michigan, or nearly so. It is more probable that they lived there long after this retirement, at a time when the climate had become much warmer.

INDIANA.

(Map 36.)

1. Gibson County.—The type specimen of Mylohyus nasutus was found somewhere in this county. The specimen was first mentioned by Leidy in 1860 (Proc. Acad. Nat. Sci. Phila., p. 416), but without other designation than peccary. Leidy wrote that it had been sent to him by Dr. David D. Owen, who informed him that it had been discovered in Gibson County, in digging a well, at a depth of between 30 and 40 feet. No more exact locality has ever been determined. The specimen consisted of the front of the skull only. It was later described by Leidy (Proc. same Academy, 1868, p. 230), under the name Dicotyles nasutus; and in 1869 (Jour. Acad. Nat. Sci. Phila., vol. VII, p. 385, plate XXVIII, figs. 1, 2) was further described and illustrated. The figures referred to have been reproduced by the present writer in 1912 (Geol. Surv. Indiana, vol. XXXIII, p. 607, text-figs. 42, 43), and again in 1914 (Iowa Geol. Surv., vol. XXIII, plate XXVI, figs. 1, 2).

It is unfortunate that Owen and Leidy did not more accurately establish the locality where this jaw was found. In Gibson County there is a considerable variety of geological deposits, even considering only those belonging to the Pleistocene and Recent. The eastern and the southeastern portion lies outside the drift-covered region. A strip along the Wabash is occupied by alluvial deposits belonging to the Recent epoch. Outside of this is another strip covered mostly by Illinoian drift.

The Patoka Quadrangle, described in Folio No. 105 of the U. S. Geological Survey, published in 1904, covers nearly the whole of Gibson County. An examination of this folio shows how complicated are the later geological features of the region. It is fair to suppose that a well from 30 to 40 feet in depth was dug, especially at that time, in the higher parts of the county, where the elevation is somewhere near 500 feet above sea-level. Here such a well would probably go through the rather scattering Wisconsin deposits of various kinds or through the loess referred to the Iowan stage, reaching perhaps the Sangamon; or through later Illinoian or early Sangamon lake deposits and Illinoian glacial accumulations into pre-Illinoian deposits. The folio cited notes (p. 3) the presence of deposits supposed to belong to the beginning of the Illinoian stage. These contained zones of black muck and other organic materials; and in places were found logs and what were thought by the well-diggers to be “black-oak” leaves. All these might have been of Aftonian age; and in deposits of that time might have been found the jaw of Mylohyus nasutus.

This species has been reported from a number of other localities; but the remains have been of so imperfect character that the identifications may have been erroneous. Professor Cope reported in 1869 (Proc. Amer. Philos. Soc., vol. XI, p. 176) that he had found several molars and canine teeth of this animal in cave breccia in Wythe County, Virginia. The breccia appeared to be very old, and in them were found a species of Megalonyx, Equus complicatus?, Tapirus haysii, Ursus amplidens, and many other extinct species.

Cope in 1899 (Jour. Acad. Nat. Sci. Phila., vol. XI, p. 263) announced this species from the Port Kennedy cave in southeastern Pennsylvania. In this case there were found only a canine and 4 molars; hence not too much reliance must be placed on the identification. A large majority of the numerous species found in the Port Kennedy cave are extinct. Among these are species of Megalonyx, a mylodon, a bear, 2 species of saber-tooth tigers, a tapir, 1 or 2 species of horse, and 3 species of peccaries. One can hardly doubt that the animals belonged to the early part of the Pleistocene. The indications are that the known examples of Mylohyus nasutus belonged to the first half of the Pleistocene; that is, to the Sangamon stage or to the Aftonian.

2. Near Williams, Lawrence County.—In the collection of the University of Indiana are some peccary remains found in Rock Cliff quarry, not far northwest from Williams. These were described by the writer in 1912 (Geol. Surv. Indiana, vol. XXXIII, pp. 596, 605). The remains were secured by Professor J. W. Beede. A part of a lower jaw which contained a first true molar and impressions of the second and third molars was referred to Leidy’s species Tagassu lenis. A large last upper molar (op. cit., p. 605, plate IV, fig. 2) was referred with some doubt to Platygonus vetus.

These remains, together with some bones of one or the other of these species and a carapace of the box-tortoise still living in that region, were inclosed in masses of stalagmite which appear to have pretty completely filled an old cave in the limestone, encountered in quarrying operations. According to Professor Beede, the cave had, when he saw it, been all quarried away except one corner. This was from 20 to 30 feet below the general surface at that place. It was about 100 feet above the present level of White River, about on a level with the highest terrace along that stream. The probabilities are that the peccaries and the box-tortoise belong to one of the earlier Pleistocene interglacial stages. Professor Beede is inclined to believe that the cave was filled during the Illinoian glacial stage by streams carrying in mud and sand and gravel. If this view is correct the inclosed remains would be at least as old as the Yarmouth.

The species Tagassu lenis is closely related to the peccary which now lives in southwestern Texas and Mexico, and it has been regarded as identical with it; but there appear to be reasons why it should be retained under its own name. It was first described from teeth found among materials coming from the phosphate deposits about Charleston, South Carolina. Certainly many of the species found there lived during the early part of the Pleistocene.

It is possible that certain teeth referred by Cope (Proc. Acad. Nat. Sci., Phila., 1867, p. 155) to the existing peccary belonged to T. lenis; but there is nothing known regarding their exact geological age. Other teeth found in the lead region of Illinois were identified by Wyman as those of the existing peccary. They too may have been those of T. lenis. The writer regards the animals found in the lead crevices as belonging to rather late Pleistocene, possibly to Peorian or Sangamon times. As to the remains found in the cave in Lawrence County it is probable that they date back to the Sangamon stage.

3. Laketon, Wabash County.—In the Fourteenth Annual Report of the Geological Survey of Indiana, page 20, Cope and Wortman stated there was in the Survey’s collection the symphyseal portion of the lower jaw and a large part of the left ramus with all the premolar teeth, except the last. This had been found at Laketon, in Wabash County. There were given no further details, and the writer failed to find the specimen in the collection. In the collection of Earlham College, Richmond, are photographs of probably this specimen and of a part of the upper jaw. The latter bone shows 3 premolars and the first molar; the lower jaw presents the symphysis, the right canine, and the 2 anterior premolars. The photographs are labeled as those of Platygonus compressus, determined by Cope, and as made from the Wabash County specimen.

All the region about Laketon is covered with Wisconsin drift or materials derived from it. The peccary found must have lived after the retirement of the border of the glacier beyond the Wabash River. It was probably long after this and when the climate was perhaps warmer than it is now.

ILLINOIS.

(Maps 20, 38.)

1. Galena, Jo Daviess County.—In 1848, Dr. John L. Le Conte (Amer. Jour. Sci., vol. V, pp. 102–106) described what he regarded as 5 new species of fossil mammals from the lead region of Illinois. These had been secured by Mr. Wm. Snyder, of Galena, in a lead crevice 50 feet below the surface, filled with a mixture of clay and sand cemented by oxide of iron into a hard mass from which the specimens could not be removed without great injury. The species described were called Platygonus compressus, Hyops depressifrons, Protochœrus prismaticus, Procyon priscus, and Anomodon snyderi. The last was regarded as related to the moles. Procyon priscus resembled closely the existing P. lotor. The 3 species first mentioned are now regarded as belonging to a single species, which takes the name Platygonus compressus. It may be remarked that the original spelling of the generic name was due perhaps to a lapsus calami or to a printer’s error. In the complete paper published shortly afterward the name was spelled Platygonus. It is to be added that the teeth which served as the type of the so-called species Protochœrus prismaticus were found at a locality 15 miles from the place where the other remains were obtained; but as to where this place was nothing is said.

In 1848 (Mem. Amer. Acad. Arts, Sci., vol. III, pp. 257–274, plates I to IV) Platygonus compressus was more completely described. Various teeth and parts of the skull and some limb-bones were figured. In this article it is stated that the remains described had been found in a lead crevice a few miles from Galena. A portion of the bones had been preserved by the miners and had at length found their way into the hands of Mr. Snyder, a merchant in Galena.

In 1852 (Proc. Acad. Nat. Sci. Phila., vol. VI, pp. 3–5) Hyops depressifrons and Protochœrus prismaticus were further described, the first being placed in the genus Dicotyles. Both of these are now regarded as belonging to Platygonus compressus.

The writer has considered it as probable that the peccary remains, as well as Procyon priscus and Anomodon snyderi, are of Late Wisconsin age; but it is possible that they are somewhat older. The reader is referred to page 343, where the Pleistocene of the lead region is discussed.

2. Alton, Madison County.—In the McAdams collection, of which a general account has been given on page 339, is a part of a lower canine tooth which apparently differs in no way from the corresponding canine of Platygonus cumberlandensis, found by Mr. J. W. Gidley in a limestone fissure near Cumberland, Maryland. On page 350 will be found a list of the species found in this fissure and their geological age.

WISCONSIN.

(Map 20.)

1. Bluemounds, Dane County.—In 1862, Professor J. D. Whitney reported (Geol. Surv. Wisconsin, vol. I, pp. 135, 136) that he had discovered in a crevice at Bluemounds, accompanied by bones and some teeth of the mastodon, a buffalo, and a wolf, several fragments of jaws and some teeth and other bones of a peccary, in an excellent state of preservation. At the top of his page 134 Whitney indicates that these remains belonged to the species now called Platygonus compressus. On page 422 of the same volume Jeffries Wyman, in reporting on the vertebrate remains collected in the lead region, mentions only 3 teeth; and these, he said, differed much from either of the fossil species and agreed with the existing peccary. From Whitney’s note at the bottom of his page 135 we may suppose that these 3 teeth were found in Iowa, near Dubuque. It is probable that the teeth found at Bluemounds belonged to Tagassu lenis.

In 1866 (Geol. Surv. Illinois, vol. I, p. 162), Whitney stated that from a crevice near Bluemounds he got peccary bones and teeth which were supposed to be identical with the animals now living. Leidy (Jour. Acad. Nat. Sci. Phila., vol. VII, p. 384) stated that he believed that teeth found in Wisconsin belonged to Dicotyles lenis. One can not be certain regarding the age of these animals found in this lead region. They are probably pre-Wisconsin. The age will be discussed on page 343.

MARYLAND.

(Map 20.)

1. Benedict, Charles County.—More than 50 years ago Cope (Proc. Nat. Sci. Phila., 1867, p. 155) reported the finding of peccary jaws mingled with remains of Miocene vertebrates collected by James T. Thomas, near his residence in Charles County, not far from Patuxent River, near Benedict. Cope recognized that the peccary and a part of a jaw of Grison macrodon (referred by Cope to Galera) belonged to the Pleistocene. The peccary was referred to the existing species Dicotyles (Tagassu) torquatus; likewise their similarity to the remains described by Leidy from Charleston, South Carolina, was noted. They are assigned here to Tagassu lenis. The jaws from the Patuxent locality are now in the Academy of Natural Sciences at Philadelphia.

2. Chesapeake Beach, Calvert County.—Mr. William Palmer, of the U. S. National Museum, has shown the writer 3 teeth of a peccary secured at the place named. These will be mentioned in the discussion of the geology of the locality. A left third premolar is 10.3 mm. long and 6.2 mm. wide. A left second molar is 12 mm. long and 10 mm. wide. These apparently belonged to Tagassu lenis.

In March 1921, Dr. Adolph H. Schultz, of the Johns Hopkins Medical School, presented to the U. S. National Museum a part of the left ramus of the lower jaw of a peccary found at Chesapeake Beach. This fragment contains the first and second molars and the sockets of the fourth premolar and the third molar. This jaw and the teeth have been compared with the corresponding parts of a specimen of Tagassu angulatus (No. 35815, U. S. Nat. Mus.), secured along the boundary between the United States and Mexico. In size the fossil teeth differ little from those of T. angulatus; the first molar is, however, somewhat wider; the conule between the two hindermost cones, the hypoconulid, is much smaller than in the existing peccary used for comparison. The inner face of each tooth is not so flat in the fossil as in the other species. In the fossil the height of the jaw at the second molar is 28 mm.; in T. angulatus 35 mm. The specimen is referred to Tagassu lenis.

3. Corriganville, Allegany County.—In a rock crevice 3 miles west of north of Cumberland, J. W. Gidley found abundant remains of peccaries. These were described by him in 1920 (Proc. U. S. Nat. Mus., vol. LVII, pp. 651–678, plates LIV, LV, 13 text-figs.). He recognized 4 species, 2 belonging to Platygonus and 2 to Mylohyus. The new species, Platygonus cumberlandensis and P. intermedius and Mylohyus exortivus, are based on materials found in the fissure. With the other materials he recognized a part of a lower jaw, which he referred to M. pennsylvanicus.

4. Cavetown, Washington County.—In 1920 (Proc. U. S. Nat. Mus., vol. LVII, pp. 96–109), the writer described a collection of fossil vertebrates made at Cavetown by the officers of Phillips Academy, Andover, Massachusetts. Among the species are 6 which belong to the group of peccaries, as follows: Mylohyus nasutus (Leidy), M. exortivus Gidley, M. obtusidens Hay, Tagassu? tetragonus? (Cope), Platygonus vetus Leidy, P. cumberlandensis Gidley.

These and the associated species apparently lived here during approximately the Middle Pleistocene, probably the Sangamon stage. A list of the species found in the fissure and their geological relations are presented on page 348. The specimen above referred provisionally to Tagassu tetragonus was called, in the paper cited above, Platygonus tetragonus. It appears, however, to be nearer Tagassu. It may even belong to an unnamed genus.

VIRGINIA.

(Map 20.)

1. Ivanhoe, Wythe County.—In 1869 (Proc. Amer. Philos. Soc., vol. XI, p. 176), Cope reported he had found several molar and canine teeth of Dicotyles nasutus, in cave breccia on New River, with remains of many other species of vertebrates. This now bears the name Mylohyus nasutus. A list of the species is given on page 353, where the Pleistocene geology of Virginia is discussed.

2. Augusta County.—In 1857 (Trans. Amer. Philos. Soc., vol. XI, p. 104), Leidy stated he had examined a fragment of a lower jaw of a young individual of Platygonus compressus, found in the county named. The jaw contained the last milk molar, unworn. The first true molar had not yet begun to protrude. The writer has seen this specimen in the collection of the Academy of Natural Sciences at Philadelphia. No other information regarding its place of origin has been secured.

WEST VIRGINIA.

(Map 20.)

1. Renicks, Greenbrier County.—In 1920 (Rep. Smithson. Inst, for 1918, p. 288, plates I-VI), J. W. Gidley reported on a visit he had made to a cave situated on Greenbrier River, near Renicks. The cave was discovered during quarrying operations in limestone. The greater part of the bones had been destroyed before the workers appreciated their value. Only a part of a skull of a peccary was secured, probably of the species Platygonus intermedius (Gidley, Proc. U. S. Nat. Mus., vol. LVII, p. 669). It has the catalogue No. 8003 of the U. S. National Museum. This animal is to be referred to the Middle Pleistocene.

SOUTH CAROLINA.

(Map 20.)

1. Charleston, Charleston County.—In 1860 (“Holmes’s Post-Pliocene Fossils of South Carolina,” p. 108, plate XVII, figs. 13, 14), Leidy reported the finding of teeth of a peccary in the Ashley River deposits. These teeth, a lower third molar and probably a lower second molar, were described under the name Dicotyles fossilis and were said to have the size and form of the corresponding teeth of the collared peccary, Dicotyles torquatus (=Tagassu tajacu). Fragments of some upper teeth were said to have the size of those of D. labiatus. In 1869 (Jour. Acad. Nat. Sci. Phila., ser. 2, vol. VII, p. 384), the fossil teeth just mentioned were referred, with some others, to the new species Dicotyles lenis. The principal character distinguishing the teeth of this species from those of the existing peccaries mentioned is the absence of accessory tubercles. This is shown also in an upper hindermost molar of the same species, described by the writer (9th Ann. Rep. Florida Geol. Sur., 1917, p. 48, plate III, fig. 2) under the name Tayassu lenis. The name should have been Tagassu lenis.

In the Pinckney collection, at the Pinckney residence, Lambs, South Carolina, near Charleston, the writer examined a tooth of a peccary, which apparently belongs to another species. It is taken to be a lower hindermost molar. A part of the anterior crest and a part of one side are broken off. The heel is relatively large, consisting of a hinder and 2 anterior tubercles; between the anterior tubercles is another minute one. In the middle of each cross-valley is a tubercle. The length of the fragment is 20.2 mm., the width 9.5 mm. This was evidently a larger animal than Tagassu lenis.

FLORIDA.

(Map 20.)

1. Vero, St. Lucie County.—Apparently 2 species of peccaries have been found in the deposits along the drainage canal, near Vero, in the uppermost stratum (No. 3). One, represented by a canine tooth, has not been determined (Hay, Rep. Florida Geol. Surv., vol. IX, p. 50). It appeared to be too large to belong to Tagassu lenis.

The other remains belonged to a small peccary and have been referred to Tagassu lenis. In 1916 (Rep. Florida Geol. Surv., vol. VIII, p. 149), Sellards reported the finding of 2 cheek-teeth and a tibia. One of the teeth was taken from the stratum called No. 2; the other teeth and the tibia had washed out of the bank and it was uncertain from which stratum they had come. In 1917 (Rep. Florida Geol. Surv., vol. IX, pp. 45, 48, plate III, fig. 2), the writer reported the finding of a hindermost molar of a small peccary, believed to be T. lenis, in stratum No. 2; also the discovery by Isaac M. Weills of a small canine of T. lenis in stratum No. 3 (op. cit., plate III, fig. 3). On page 50 of the same paper the writer referred provisionally to T. lenis the tibia above mentioned.

2. Palma Sola, Manatee County.—From this place have been sent to the U. S. National Museum many specimens of fossil vertebrates, a list of which will be found in the discussion of the Pleistocene geology of Florida (p. 379). Some of these belong to the Pleistocene, others apparently to the Miocene. Among the specimens is a right astragalus of a peccary. While it is possible that the original possessor of this astragalus lived during the Miocene, it does not seem probable. It may have belonged to Tagassu lenis. The length of the bone is 32 mm., the width across the lower end 19 mm.

TENNESSEE.

(Map 20. Figure 23.)

1. Rogersville, Hawkins County.—In the U. S. National Museum is a part of a lower left canine tooth of a peccary found near the place mentioned. With it came an upper molar of Equus leidyi. The tooth lacks most of the crown. It has been described by the writer under the name Mylohyus setiger (Proc. U. S. Nat. Mus., vol. LVIII, p. 84, plate III, figs. 21–23). The root of the tooth is 93 mm. long, measured along the convexity of the curve. A little of the tip of the root is missing. The size of the tooth indicates a very large animal.

2. Whitesburg, Hamblen County.—In the U. S. National Museum is a considerable collection of bones and teeth made in 1885 near Whitesburg. This locality and the accompanying species will be discussed on another page. Among the remains are 3 upper canine teeth, referred by the writer (Proc. U. S. Nat. Mus., vol. LVIII, p. 90, plate III, figs. 12–13) to Mylohyus nasutus Leidy. A list of the associated species will be found on page 395.

3. Dandridge, Jefferson County.—In 1896 (Dept. Amer. and Prehist. Archæol. Univ. Penn.), Dr. H. C. Mercer reported he had found remains of the tapir, peccary, bear, and small rodents in Zirkel’s Cave. The cave is situated on the left bank of Dumplin Creek, about 5 miles above its entrance into French Broad River. The species to which the peccary remains belonged was not determined.

KENTUCKY.

(Map 20.)

1. Rockcastle County.—In 1853, Dr. Leidy (Trans. Amer. Philos. Soc., vol. X, p. 331, plates XXXV, XXXVI, XXXVII, figs. 5–8, 17, 19) described under the name Euchœrus macrops, a fine skull of a peccary which had been lying for 47 years in the collection of the society. It had been sent there by Dr. Samuel Brown, of Lexington, Kentucky, and was said to have been found in one of the nitrous caves of that State. The writer is informed by Dr. Arthur M. Miller, Professor of Geology in the University of Kentucky, that it is unlikely that the skull came from any of the caves in the region about Lexington, as he had never heard any of them had been worked for saltpeter. In the Transactions of the American Philosophical Society for 1804 (vol. VI, pp. 235–247) is a paper by Samuel Brown, in which he describes a cave in what is now Rockcastle County. In this and some other neighboring caves were found immense quantities of saltpeter. Probably the skull which Leidy afterward described from this region was brought to light. It appears to have been mentioned by Dr. B. S. Barton as early as 1806 (Phila. Med. and Phys. Jour., vol. II, plate I, p. 158). It is now in the collection of the Academy of Natural Sciences at Philadelphia. It was recognized by Leidy as belonging to Platygonus compressus.

FINDS OF PLEISTOCENE CAMELIDÆ IN EASTERN NORTH AMERICA.

PENNSYLVANIA.

(Map 21.)

1. It is not certain that any fossil camel remains have ever been found in Pennsylvania. In 1899 (Jour. Acad. Nat. Sci. Phila., ser. 2, vol. XI, p. 264, plate XXI, figs. 4, 4_a_) Cope described Teleopternus orientalis and referred it to the Camelidæ. This was found in the Port Kennedy cave, and whatever its relationships it belongs to the early Pleistocene. Matthew (Osborn, Age of Mamm., p. 469) suggested that its affinities might be with the musk-oxen.

FLORIDA.

(Map 21.)

1. Archer, Alachua County.—In 1886 (Proc. Acad. Nat. Sci. Phila., 1886, p. 12), Dr. Joseph Leidy briefly described three species of the genus Procamelus from materials collected near Archer by Dr. W. H. Dall. The teeth and bones had been found in what has been called the Alachua clays, and were associated with a considerable number of species of vertebrates. The list will be found on page 375, where the Pleistocene geology is considered. The three species of camels were called Auchenia major, A. minor, and A. minimus. They are now referred to the genus Procamelus. In 1896 they were (Trans. Wagner Free Inst. Sci., vol. IV, pp. VII-XIV, 15–61, with plates) described in more detail and illustrated by Leidy and Lucas. The error of calling P. minor by the name P. medius, first introduced by Cope, was followed in the paper just mentioned; and some authors have continued this practice. Dr. W. H. Dall included these camels in his list (Bull. U. S. Geol. Surv. No. 84, p. 129). Authors have in general referred to the Tertiary the deposit which furnished these camels; the present writer believes that the Alachua beds belong to the first glacial stage. The matter is further discussed on pages 376 to 378.

2. Williston, Levy County.—In 1892 (Bull. U. S. Geol. Surv., No. 84, p. 129), Dr. W. H. Dall published a list, furnished by Joseph Leidy, of the vertebrate fossils found at what was then known as Mixon’s bone-bed. The species, with some additions, are listed on page 375. Among others is Procamelus major. The species were found in the Alachua clays, and these clays are referred by Sellards to the Upper Miocene or Lower Pliocene.

3. Ocala, Marion County.—In 1889 (Proc. Acad. Nat. Sci. Phila., 1889, p. 31; Trans. Wagner Free Inst. Sci., vol. II, pp. 13–17), Leidy mentioned the discovery of a tooth of a camel, regarded by him as belonging to Procamelus, in a limestone quarry at Ocala. With it were described the saber-tooth tiger Machairodus floridanus. Teeth were found also of a horse which is referred to Equus leidyi. A list of the species found at this locality is on page 378. In the Philadelphia Academy paper Leidy called the camel Auchenia minor. In the next paper cited he regarded it as A. minimus.

4. Dunnellon, Marion County.—In 1916 (8th Ann. Rep. Florida Geol. Surv., pp. 94, 104), Dr. Sellards presented a list of the species of vertebrates discovered in the Dunnellon formation at Dunnellon and vicinity. Among the species is the camel Procamelus minor. This, however, he did not include among the Pleistocene animals.

Undetermined teeth of a camel are mentioned by Sellards as found in the phosphate mines at Dunnellon (5th Ann. Rep. Fla. Geol. Surv., p. 58).

5. Hernando, Citrus County.—Sellards (5th Ann. Rep. Florida Geol. Surv., p. 58) reported a discovery of teeth of an undetermined species of camel in a phosphate mine at Hernando. These probably are of the genus Procamelus.

6. Vero, St. Lucie County.—Some remains of a camel have been found in the stratum at Vero known as No. 2, the one immediately overlying the bed of marine marl. Sellards (8th Rep., p. 149) states there had been secured up to that time two upper cheek-teeth, a distal end of a cannon-bone, and a phalanx. The latter, a hinder first phalanx, is figured (plate XXX, fig. 5). It resembles considerably the bone figured by Leidy and Lucas (Trans. Wagner Free Inst., vol. IV, plate XVIII, fig. 8), but it presents important differences.

The anterior phalange figured by Leidy and Lucas is 85 mm. long; a hinder phalange of the same animal would have been shorter. The hinder phalange found at Vero is 104 mm. long. The probability is that its owner was an animal considerably larger than Leidy’s Procamelus minimus. The phalanx referred by Leidy and Lucas to Procamelus medius (=P. minor) has exactly the length of that of P. minimus, but is a much stouter bone, the side-to-side diameter at the middle of the length being one-half greater. The Vero camel appears, therefore, to be distinct from any of the Pliocene camels of Florida. It probably belongs to the genus Camelops.

TENNESSEE.

(Map 21. Figure 23.)

1. Nashville, Davidson County.—From Mr. W. E. Myer, of Nashville, the writer has received for examination a right calcaneum of an undetermined species of camel, belonging probably to the genus Camelops. This was found near Nashville, in the bank of Cumberland River. At the same locality were found part of a tooth of a young mastodon, a tooth of Equus leidyi, a fragment of a femur of a probably larger horse, an antler of a young deer, a tooth of Mylodon, and some fragments of turtle bones. However, the horse remains and the antler are said to have been lying in a layer of gravel, while the camel and mastodon were in a bed of sand just above the gravel. Over these beds are nearly 30 feet of gravel.

The total length of the calcaneum is 138 mm., the greatest height 67 mm., and the thickness at the rear of the articular surface for the astragalus, 45 mm. From the rear end to the surface for the astragalus is 85 mm. The surface for union with the cuboid is 19 mm. wide, considerably narrower than in the dromedary and in an astragalus from Denver, Colorado, which apparently belongs to Camelops huerfanensis. The outer face of the bone is considerably less concave than in either of the two species referred to. The tuberosity is relatively thicker at the middle of its length than is either of the species mentioned; its height at its middle is relatively less than in the Denver specimen. It is believed that the age of the beds containing these fossils is about that of the Aftonian interglacial.

FINDS OF PLEISTOCENE DEER OF THE GENUS ODOCOILEUS IN EASTERN NORTH AMERICA.

ONTARIO.

(Map 22.)

1. Toronto.—In the Guide Book No. 6, issued by the Ontario Bureau of Mines in 1913, and prepared by Professor A. P. Coleman, it is recorded on page 18 that in the Don beds at Toronto, supposed to belong to the Sangamon stage, had been found bones of a deer resembling those of the Virginia deer. On page 29 deer bones are reported as found in other beds situated in the western part of Toronto. The age of these is uncertain; they may be older than the Don beds or younger than the Scarboro beds. In these same beds have been found also a lower jaw of a bear, possibly Ursus americanus; an atlas of a bison, a part of an antler of Cervalces borealis, and some parts of either a mastodon or a mammoth.

The geology of the Pleistocene in the region about Toronto is treated on pages 281 to 283, figure 3.

NEW YORK.

(Map 22.)

1. Orange County.—Emmons, in 1858 (Geol. Surv. North Carolina, East. Counties, p. 201), stated he had found, in a fresh-water marl-bed in Orange County, a horn of an extinct deer, associated with remains of mastodon. The exact locality is unknown.

2. Greenville, Greene County.—In 1846 (Boston Jour. Nat. Hist., vol. V, p. 390), James Hall mentioned the finding of a jawbone, with teeth, of a deer in Greene County. It was associated with remains of a mastodon.

3. Cuba, Allegany County.—In 1843 (Geol. 4th Dist., p. 367), Hall reported that an engineer of the Genesee Valley Canal informed him that near New Hudson, 4 miles from Cuba, several antlers of deer and one of an elk had been found 12 feet below the surface, in a muck deposit. New Hudson appears to be about 10 miles north of Cuba, and not on the canal. The locality is said to be at the summit of the canal.

4. Hinsdale, Cattaraugus County.—James Hall (op. cit., pp. 364, 366) stated that a tusk, supposed to belong to a mastodon, with some horns of deer, had been found at Hinsdale in sand and gravel, 16 feet below the surface. Clarke (Bull. 69, N. Y. State Mus., p. 933) suggested that these may have been antlers of the elk.

There appear to be no good reasons for suspecting that any of the deer remains found in New York are older than Late Wisconsin.

NEW JERSEY.

(Map 22.)

1. Woodstown, Salem County.—In the palæontological collection at Yale University is a fragment of an antler of a deer, most probably of Odocoileus virginianus, discovered in Salem County. It is not accompanied by any information as to the exact locality where found or as to the conditions of burial. The fragment of the shaft is 135 mm. long, and from it springs a tine, the partial length of which is about 45 mm.

2. Vincentown, Burlington County.—In the collection of the Academy of Natural Science at Philadelphia are some fragments of antlers labeled as having been found at Vincentown.

In 1869 (Jour. Acad. Nat. Sci., Phila., vol. VII, p. 376), Dr. Joseph Leidy stated that remains of the deer had been found in Burlington and Monmouth Counties, but no exact localities were mentioned. Many of the specimens seem to have been found, as accidental occupants, in marl-beds of Cretaceous age. In the Academy of Natural Sciences at Philadelphia there are specimens from Pemberton.

3. Deal, Monmouth County.—In the Academy’s collection, at Philadelphia, there is a specimen labeled as having been found at this place. No details are recorded.

PENNSYLVANIA.

(Map 22.)

1. Stroudsburg, Monroe County.—In 1889 (Ann. Rep. Geol. Surv. Pennsylvania for 1887, p. 6), Dr. Joseph Leidy reported on a collection which many years before had been found in Hartman’s Cave, near Stroudsburg. Nearly all the species still exist, but in the collection was included Castoroides and Rangifer. Among the fossils were jawbones, with teeth, and broken bones of the Virginia deer. It seems possible that the remains had collected there at the close of the Pleistocene; but some may belong to the Recent.

2. Frankstown, Blair County.—In 1908 (Ann. Carnegie Mus., vol. IV, p. 231), Dr. W. J. Holland reported the discovery of remains of a deer, possibly Odocoileus virginianus, in a cave at Frankstown. With this deer were many other species of mammals. A list is presented on page 321.

OHIO.

(Map 22.)

1. New Knoxville, Auglaize County.—In his “History of Ohio and of Auglaize County,” 1905, on page 338, C. W. Williamson, in describing the finding of a skull of Castoroides near New Knoxville, stated that some bones of the deer had been found in what was believed to have been the house of the giant beaver. They were supposed to have been brought there by carnivorous animals; but the deer may have died there before the house was covered up.

MICHIGAN.

(Map 22.)

1. Adrian, Lenawee County.—In 1880 the U. S. National Museum received from Professor Kost, then of Adrian College, a skull of Castoroides ohioensis discovered at the place named above. In his communication he wrote that at the same place there had been found previously a mastodon and bones of an elk and of a deer. The place was in a marsh, in Adrian, and the fossils were at a depth of 4 feet.

2. Ann Arbor, Washtenaw County.—In 1908, Russell and Leverett (Folio 155, U. S. Geol. Surv., p. 9) reported the discovery of bones of deer and elk in a peat-swamp, 3 miles south of Ann Arbor. In the same swamp had been found, at a depth of 5 feet, a skull of Castoroides ohioensis. The bones of the deer and elk were at a somewhat higher level, so that it is not wholly certain they belong to the Pleistocene.

The specimens found both at Adrian and Ann Arbor lived there after the retreat of the Wisconsin ice.

INDIANA.

(Map 22.)

1. Evansville, Vanderburg County.—In a collection of bones and teeth made at the mouth of Pigeon Creek, a short distance below Evansville, and described by Leidy (Proc. Acad. Nat. Sci., Phila., 1854, pp. 199–200) were included remains of the Virginia deer. With these bones were parts of the skeleton of Megalonyx jeffersonii, a bison of probably an extinct species, a cervical vertebra of the horse known as Equus complicatus, a tooth of a tapir, and the type upper jaw of the extinct wolf Ænocyon dirus.

On page 32 is discussed the age of the bone-bed. It is concluded that it belonged possibly to the Aftonian stage, but more probably to the Sangamon. Although this species of deer yet exists, abundant remains of a species not yet distinguishable from it are found in early Pleistocene deposits in Florida and elsewhere. According to D. D. Owen (Smithson. Contrib. Knowl., vol. VII, art. V, p. 7), this deer was found associated with megalonyx bones a few miles below Henderson, Kentucky. Also, these two species, together with Equus complicatus and an extinct species of Bison and other extinct species of mammals, have been exhumed at Bigbone Lick, halfway between Louisville and Cincinnati, on the Kentucky side.

Under this number may be considered the deer Odocoileus dolichopsis, which Cope described in 1878 (Amer. Naturalist, vol. XII, p. 189). This was represented by a left ramus of the mandible, found, as reported by the State geologist, John Collett, in a late lacustrine deposit in Vanderburg County. In the same deposits was found an ulno-radius of a species of Bison. The deer jaw was further described and figured by Cope and Wortman in 1884 (Geol. Surv. Indiana, vol. XIV, p. 22, plate ii). Here, in quoting Cope’s description found in volume IV of Bulletins U. S. Geological Survey, page 379, the authors substituted Harrison County for Vanderburg County. In 1912 (Geol. Surv. Indiana, vol. XXXVI, p. 615), the present writer accepted Cope and Wortman’s statement as to the county; but it appears that the locality was really in Vanderburg County. Cope and Wortman’s plate was reproduced by the writer in 1912 (Geol. Surv. Indiana, vol. XXXVI, p. 615, plate VI, figs. 2, 2_b_). Figure 1 of the plate represents a part of an upper jaw which may or may not belong to the same species. It was supposed to have been found in the same deposits.

2. Harrisville, Randolph County.—In the collection at Earlham College, Richmond, Indiana, the writer has examined some bones which apparently belonged to the Virginia deer, Odocoileus virginianus. The distal end of the radius, a right calcaneum, and a sacrum have been identified. These were found in a swamp known as “The Dismal,” situated about 6 miles nearly east of Winchester. This would not be far from the village of Harrisville. In this swamp were collected the fine specimen of the giant beaver, preserved at Earlham College, and the bones of an elk. The swamp is located near the Union City moraine, and the animals buried there must have lived at some time after the retirement of the Wisconsin ice-sheet; probably the time was long enough after that retirement for the climate to become relatively mild.

3. Roann, Wabash County.—In 1892 (Geol. Surv. Indiana, vol. XVII, p. 241), Elrod and Benedict reported that in 1882 a Mr. Rantz, while digging a ditch on the farm of William Runkle, 3 miles north of Roann, unearthed, at a depth of 9 feet, the antlers and part of the skeleton of the deer Odocoileus virginianus. The locality is evidently north of Eel River and near the southern border of the great moraine which runs parallel with this stream and north of it. Undoubtedly this deer lived after the Wisconsin ice had withdrawn from the vicinity. In similar situations in that region have been found several mastodons. It is probable, therefore, that the deer belonged to the late Pleistocene.

From Mr. B. E. Galtry, of Roann, the writer learns that Mr. Runkle informed him that none of the bones found has been preserved. There were many found, shin-bones, ribs, and antlers, from 3 to 4 feet below the surface. Large numbers of poles were found, and the ditch diggers got the notion that these poles had formed a bridge.

ILLINOIS.

(Maps 22, 38.)

1. Niantic, Macon County.—In 1873, Worthen, State geologist of Illinois, reported (Geol. Surv. Illinois, vol. V, p. 308) that he had found some deer bones in a bog near Niantic; with them were remains of the mastodon, buffalo, and elk. What is known regarding the locality and the geology is here recorded on page 102. All these remains were probably buried near the close of the Wisconsin glacial stage.

2. Whitewillow, Kendall County.—In Netta C. Anderson’s list, page 11. E. S. Riggs, assistant curator of palæontology in Field Museum of Natural History, reported that in 1902 Mr. John Bamford, in enlarging a spring in a bog, encountered a layer of about 2 feet of bison, deer, and elk bones at a depth of about 5 feet. With these were found skulls of at least 6 mastodons. From Mr. George Langford, of Joliet, the writer has received a base of a large antler and a nearly complete small antler of the right side. These are not to be distinguished from those of O. virginianus. Mr. Langford wrote that the mastodon bones were mingled with the other bones to the bottom of the pit dug. In the same excavation were found remains of mastodon, Cervalces, the existing moose, the elk, the buffalo, and the cannon-bone of a large sheep-like animal. The exact levels in which these bones occurred is not known. The reader may consult page 109.

3. Ottawa, La Salle County.—J. D. Caton (“Antelopes and Deer of North America,” p. 227) tells of having found a nearly complete skeleton and three antlers of the Virginia deer in the valley of Fox River, near Ottawa. These remains were in a stratum of gravel at a depth of more than 16 feet. Over this was the surface loam, then sand, sand and clay, then more sand. It seems probable that these deposits belonged to the Late Wisconsin.

4. Evanston, Cook County.—Dr. Frank C. Baker (Univ. Ills. Bull, XVII, pp. 4, 86) presented a geological section taken in the Toleston beach at Evanston. This beach was laid down after the withdrawal of the Wisconsin ice. At the depth of about 9 feet was found a bone of a deer. In 1891, W. K. Higley (Bull. Chicago Acad. Sci., vol. II, No. 1, p. XIV) reported that a pelvis, referred to a deer, had been found in Late Wisconsin deposits at Evanston. He had in mind the bone found in Toleston beach. At the same place was found a femur of a deer at a depth of 9 feet (Leverett, Bull. Chicago Acad. Sci. Geol. Nat. Hist. Surv., II, 1897, pp. 76, 77). Apparently the femur and the pelvis had been discovered by Dr. Oliver Marcy in 1864, from whom both Leverett and Baker quote the geological section.

5. Lemont, Cook County.—Dr. F. C. Baker (op. cit., pp. 56, 89) reported the finding of a portion of a skull of Odocoileus virginianus and a skull of the muskrat in the Des Plaines Valley, at Lemont, in a bed of peat.

WISCONSIN.

(Map 22.)

1. Lead region.—In 1862 (Geol. Surv. Wisconsin, p. 421), Jeffries Wyman, in his report on the vertebrate animals found by J. D. Whitney, stated that there was a series of several molar teeth which, in form and size, corresponds exactly with those of the red deer (Cervus virginianus). He mentioned also various bones which seemed to belong to the same species, but some were larger than those of the Virginia deer.

In 1876 (Amer. Jour. Sci., vol. XI, p. 49), Allen described as a new species Cervus whitneyi, basing the name on a left humerus, a left radius, and a right metatarsal found in the Whitney collection. It appears probable that these bones are those mentioned by Wyman as being larger than the existing Virginia deer and the mule deer. Allen does not, however, mention what Wyman wrote. Allen’s species is now referred to the genus Odocoileus. It is not stated by either Wyman or Allen even from what State the remains were secured. It is most probable that it was Wisconsin.

From the Pleistocene of that region two species of Odocoileus are therefore known, O. virginianus and O. whitneyi.

2. Menomonie, Dunn County.—In a letter to the author dated January 21, 1917, Dr. S. Weidman, State geologist of Wisconsin, noted that a vertebra of a deer had been found in brick clay at Menomonie. It was sent to the American Museum of New York and identified by Dr. W. D. Matthew. This clay is at present regarded by Dr. Weidman as probably belonging to the Sangamon interglacial.

MARYLAND.

(Map 22.)

1. Oxford Neck, Talbot County.—In 1869 (Proc. Amer. Philos. Soc., vol. XI, p. 178), Cope reported that fragments of antlers not distinguishable from those of the Virginia deer, Odocoileus virginianus, had been found on the farm of Lambert Kirby, in Oxford Neck. These, with remains of other vertebrates, were placed in the Baltimore Academy of Sciences.

2. Cavetown, Washington County.—In 1920 (Proc. U. S. Nat. Mus., vol. LVIII, p. 104), the writer described the distal end of two radii found at Cavetown in a fissure in a limestone quarry. These were associated with remains of 24 other species of vertebrates, mostly mammals. The radii appeared to be those of Odocoileus virginianus. Another deer, Sangamona fugitiva, was found in the same fissure.

A list of the accompanying species is given on page 348.

VIRGINIA.

(Map 22.)

1. Saltville, Smyth County.—Mr. O. A. Peterson (Ann. Carnegie Mus., vol. XI, p. 474, fig. 7) reported the finding of an astragalus of some deer-like animal at Saltville. He states that the bone agrees with that of Odocoileus virginianus, but is larger. To the present writer the bone is not only too large to be that of the Virginia deer, but is relatively too narrow, it being assumed that Peterson’s figure is correct. In both the Virginia deer and the elk the width of the bone is about 70 per cent of the greatest length, while the figure given is only 60 per cent as wide as long. It is not improbable that the animal belonged to another genus.

2. Ivanhoe, Wythe County.—In 1869 (Proc. Amer. Philos. Soc., vol. XI, p. 176) Cope stated that molars and other fragments of Cariacus (Odocoileus) virginianus were abundant in the cave breccia which he examined. A list of the accompanying species will be found on page 353.

WEST VIRGINIA.

(Map 22.)

1. Wood County.—In 1835 (Amer. Jour. Sci., vol. XXIX, p. 147), Hildreth stated that bones of a deer had been found in this county, then a part of Virginia, involved in the travertine on the floor of the cave. No facts are known that give any clue to the geological age of these bones. They probably belong to some early or middle stage of the Pleistocene.

NORTH CAROLINA.

(Maps 22, 39.)

1. On Neuse River, Pamlico County, 16 Miles below Newbern.—According to both Croom (Amer. Jour. Sci., vol. XXVII, 1835, p. 168) and Harlan (op. cit., vol. XLIII, 1842, p. 143), remains of deer had been found at this locality. For want of more exact information we may refer them to Odocoileus virginianus. On page 359 will be found a list of the species collected here.

SOUTH CAROLINA.

(Map 22.)

1. Charleston, Charleston County.—Numerous fragmentary remains of Odocoileus have been found in the region about Charleston. F. S. Holmes, as early as 1859 (Proc. Acad. Nat. Sci., Phila., 1859, p. 177), announced the discovery of remains of deer in the vicinity of Charleston. Leidy (Holmes’s Post-Pliocene Foss. South Carolina, p. 109, plate XX, figs. 1–4) stated that the collections of Professor Holmes and Captain Bowman contained fragments of antlers, portions of jaws, and teeth which had been found in the Post-Pliocene beds of Ashley River. Leidy concluded these remains did not differ from the corresponding parts of the existing white-tailed deer (O. virginianus). Many fragments of antlers belong in the Scanlan collection at Yale University. They are thoroughly fossilized and are hard and heavy.

In the Charleston Museum (No. 1047) is an anterior cannon-bone of a deer, but no definite locality is recorded. It is black and apparently phosphatized, as are the numerous fragments of antlers found in the private collections at Charleston. The cannon-bone mentioned is 188 mm. long.

While the materials so far discovered do not enable us to distinguish the deer remains found about Charleston from Odocoileus virginianus, it is not improbable that they belonged in reality to another species, some perhaps to the Floridan Pleistocene species O. sellardsiæ.

Antlers of the white-tailed or Virginia deer are common in the collections about Charleston. In the Scanlan collection are bases of antlers of adult bucks and two simple spikes of young deer. One base is different from the others in being much flattened in one border, probably the one on which the first tine arose. It is possible that it represents a distinct species.

2. Darlington, Darlington County.—In 1848, Tuomey (Rep. Geol. South Carolina, pp. 177–180) stated that on the land of a Rev. Mr. Campbell, somewhere in the vicinity of Darlington, he had found fragments of the horns of a deer. He regarded the beds as belonging to the Pliocene. In the neighborhood, in a similar deposit, had been found molars of Mastodon maximus (=Mammut americanum). Both species may belong to the early Pleistocene.

FLORIDA.

(Map 22.)

1. Pablo Beach, Duval County.—Dr. Sellards (8th Ann. Rep. Florida Geol. Surv., p. 106) reported remains of Odocoileus found at station 120 of the Inland Waterway Canal, about 5 miles south of Pablo Beach. Further mention is made of this on page 374.

2. Neals, Alachua County.—In his eighth report (page 94) Sellards stated that at Neals, near Newberry, teeth had been collected which probably belonged to a species of Odocoileus. These were found while phosphate rock was being mined; but they, with a tooth of a tapir and one of Equus littoralis, doubtless belong to the early Pleistocene.

3. Archer, Alachua County.—In 1896 Leidy (Trans. Wagner Free Instit., vol. IV, p. X), in a note on the species of vertebrates found in the Alachua clays, included among these a tapir, a mastodon, and a megatherium. In his list furnished for Dr. W. H. Dall’s report (Bull. U. S. Geol. Surv. No. 84, p. 129), is included Cervus virginianus?. The tapir, the deer, and the megatherium have been regarded as Pleistocene fossils which became mixed with those of the Pliocene. For that reason Odocoileus is here credited to Archer. See also Sellards’s conclusion (6th Ann. Rep. Florida Geol. Surv., p. 162). It is not certain exactly where the species above named were found. One locality mentioned by Leidy is 10 miles south of Archer, now Williston; another is 10 miles north of the same town, now Newberry. For the geological age of the species found at Archer, consult page 375.

4. Ocala, Marion County.—From a fissure in a limestone rock at Ocala, Sellards (8th Ann. Rep., p. 103) secured some remains of Odocoileus, but it was not determined to what species they belonged.

5. Dunnellon, Marion County.—The writer (8th Ann. Rep. Florida Geol. Surv., p. 43, plate VIII, figs. 3–5) described some teeth of a deer found near Dunnellon, in the “Cullens river mine.” These were referred provisionally to the species or subspecies now living in that region, Odocoileus osceola.

6. Palmetto, Manatee County.—In a small collection of fossil vertebrates sent from this place by Mr. Ernest Leitzel to the U. S. National Museum for identification were some fragments of antlers of Odocoileus.

7. Palma Sola, Manatee County.—From Mr. Charles T. Earle the U. S. National Museum received, in 1921, many fragments of antlers found on the beach at Palma Sola, about 10 miles below Palmetto and on the south side of Manatee River. With these came teeth of Equus leidyi, E. complicatus, E. littoralis, teeth and bone of Bison latifrons?, a tooth of Elephas columbi, and a fragment of the beak of a ziphoid porpoise. The last and various sharks’ teeth probably originated in Miocene deposits not far away. A list of the species found at this place and believed to belong to the Pleistocene is presented on page 379.

8. Arcadia, De Soto County.—In 1889 (Proc. Acad. Nat. Sci., Phila., 1889, p. 96; U. S. Geol. Surv. Bull. No. 84, p. 129), Leidy reported the discovery of antlers of deer, Odocoileus (Cervus) virginianus, at Arcadia. These may have belonged to O. osceola or O. sellardsiæ. In 1884 (Proc. U. S. Nat. Mus., vol. VI, p. 428), Mr. S. T. Walker reported the finding of fossils, among them fragments of deer antlers, on sand-bars in Peace River, from a point about where the town of Hull now is to a point 8 miles by land above Fort Ogden, apparently not far from the present town of Owens. On this matter see Sellards (8th Ann. Rep. Florida Geol. Surv., p. 109). This locality and its fossils are further described on page 381.

9. Vero, St. Lucie County.—Numerous remains belonging to one or two species of Odocoileus have been found at Vero. Fragments of various parts of the skeleton and some teeth have been found in the two upper strata, No. 2 and No. 3, which lie above the marine marl. The writer (9th Ann. Rep. Florida Geol. Surv., 1917, pp. 50–57, plate III, fig. 3) referred some of these bones to the new species, O. sellardsiæ. Possibly only this species is represented at that locality, but probably some of the bones belong to O. osceola. Lists of the species found in the two deposits bearing fossil vertebrates will be found on pages 381 to 383.

MISSISSIPPI.

(Map 22.)

1. Natchez, Adams County.—Dr. Leidy wrote (Proc. Acad. Nat. Sci., Phila., 1854, p. 199) as follows:

“Fossil bones of a deer not larger than the Cervus virginianus have been found in association with bones of the Megalonyx, Mastodon, etc., in the vicinity of Natchez, Mississippi. In the cabinet of the Academy mentioned there are several specimens from the locality, consisting of a portion of a lower jaw, a fragment of an antler, and the posterior and inferior portions of two crania.”

The geology of this important locality is discussed on pages 389 to 393.

2. Aberdeen, Monroe County.—In 1869 (Jour. Acad. Nat. Sci., ser. 2, vol. VII, p. 376), Leidy stated that remains of a deer had been found at this place in a railroad cutting. No details were given.

TENNESSEE.

(Map 22. Figure 23.)

Whitesburg, Hamblen County.—In 1920 (Proc. U. S. Nat. Museum, vol. LVIII, pp. 85–95), the writer described bones and teeth of Pleistocene animals which had been found at Whitesburg. A list of the species is given on page 395. In the collection are 21 teeth which were referred to Odocoileus virginianus, but their small size suggests that they may belong to another species of deer.

Nashville, Davidson County.—On page 201 is presented an account of a collection made at Nashville. Among the fossils was an antler of a deer which is referred by the writer to an undetermined species of Odocoileus (p. 399).

KENTUCKY.

(Map 22.)

1. Bigbone Lick, Boone County.—The bones and teeth of the Virginian deer have been reported with some doubt from Bigbone Lick; even if found it is not certain that they belonged to Pleistocene deposits.

2. Bluelick Springs, Nicholas County.—In the collection made in cleaning out Bluelick Springs, in Nicholas County, remains of a deer were secured. The geological age of these can not be determined with certainty, but they were probably of Late Wisconsin time. For a list of the associated species see page 405.

3. Henderson, Henderson County.—In a letter to Dr. Joseph Leidy, published by the latter (Smithson. Contrib. Knowl., vol. VII, art. 5, p. 7), Dr. D. D. Owen stated that many antlers and bones of deer had been found about 6 miles below Henderson, associated with bones of Megalonyx jeffersonii.

FINDS OF CERVUS CANADENSIS IN THE PLEISTOCENE OF EASTERN NORTH AMERICA.

ONTARIO.

(Map 23.)

1. Hamilton, Wentworth County.—On Burlington Heights, near Hamilton, many years ago antlers of the elk were found associated with a jaw of a beaver. They were discovered 30 feet from the surface and at a level 7 feet higher than the jaw of Elephas columbi described on page 147. The age of all these bones is late Pleistocene. The elk had, therefore, spread over the northern part of our country before the close of the Wisconsin stage.

The geology of this locality and the species found there are considered on pages 284–285.

2. Near Strathroy, Middlesex County.—In 1901 (Ottawa Naturalist, vol. XV, pp. 95–97, fig.) L. H. Smith wrote on the occurrence of the elk in Ontario. None had been known to exist there since the settlement by white men. The writer of the article had a number of specimens of antlers collected in the neighborhood of Strathroy and the neighboring county, Lambton. A fine pair of antlers and a part of a skeleton of an elk had been discovered in a boggy spring in lot 15, 12th concession, township of Lobo. It was evidently not deeply buried. This and the others, notwithstanding shallowness of burial, may have been buried in Late Pleistocene times; but there is no assurance that they did not live during the early Recent.

3. Kingston, Frontenac County.—In 1898 (Bull. Geol. Soc. Amer., vol. IX, p. 377), Robert Bell stated that remains of the elk had been found in shell marl in at least two places near Kingston.

VERMONT.

(Map 23.)

1. Grand Isle, Champlain Lake.—In 1840 (Rep. on Quadrupeds, Massachusetts, p. 82), Emmons reported the finding of an antler on this island, which he concluded belonged possibly to a young elk. It had been thrown out by the plow from an elevated piece of ground, near a spring of water. He concluded that it was the antler of the second year, and stated that it had no branches. It was somewhat curved and had a total length of 849 mm. The diameter just above the burr was given as 183 mm.; but this is much greater than that in any specimens of young elks at hand. Possibly some other species is represented and it may not have belonged to Pleistocene.

NEW YORK.

(Map 23.)

1. Racket River, St. Lawrence County.—J. E. De Kay, in 1842 (Zool. N. Y., Mamm., p. 120, plate XXIX, fig. 1), described a part of a skull, to which were attached the damaged antlers of an elk, which had been dug up near the mouth of Raquette River. This must have been not far from the town of Racket River. Nothing appears to be known regarding the conditions under which the skull was found. Leidy (Jour. Acad. Nat. Sci., Phila., vol. VII, 1869, p. 377) refers to the specimen. It was at one time in the Lyceum of Natural History, New York, but is probably no longer in existence.

2. Seneca Castle, Ontario County.—Mr. E. Hitchcock (Science, vol. VI, 1885, p. 450) reported the finding of an antler of an elk at this place. It was associated with supposed remains of a mastodon, in a peat morass, near Flint Creek. It is to be credited to the Late Wisconsin.

3. Farmington, Ontario County.—James Hall, in 1887 (6th Ann. Rep. State Geologist, New York, p. 391), reported the discovery of about two-thirds of the skeleton of an elk at the place named, in a cedar swamp, buried in peat at depths of from 6 to 18 inches. The antlers had projected above the surface and had been gnawed by rodents. Hall remarked that the elk had not been known to live in that region since the coming of the white race. The skeleton may or may not have been deposited there during the late Pleistocene.

4. Livingston County.—In the collection at Princeton University is a calvarium of an elk labeled as found in Livingston County. The finder had, with a tool, chopped off the antlers and otherwise hacked the skull. One can not be certain as to the geological age of the specimen.

5. Cuba, Allegany County.—In 1843, James Hall (Geol. 4th Dist., p. 367) reported that several horns of deer and one of an elk had been found at the summit of the Genesee Valley Canal. The place given was New Hudson, 4 miles from Cuba; but this town is about 10 miles from Cuba and apparently not on the canal. The antlers were found at a depth of 12 feet, in muck.

6. Jamestown, Chautauqua County.—Hall (op. cit., p. 365) stated that Dr. Emmons had in his possession a tooth which he regarded as belonging to this species. De Kay (Zool. N. Y., Mamm., p. 120, plate XXIX, fig. 4) describes and figures this tooth. Emmons, in 1840 (Rep. Quadrupeds of Massachusetts, p. 82), first mentioned the tooth and said it had been found in a clay bed with several others. The tooth may belong to the Pleistocene, but this can not be proved. It is of value, as are the other cases, as showing the former distribution of the species.

7. Boonville, Oneida County.—In 1884 (Trans. Linn. Soc. N. Y., vol. II, p. 46), Dr. C. Hart Merriam reported that Mr. Calvin V. Graves, of Boonville, had parts of elk horns, plowed up in an old beaver meadow. These may have belonged to very late Pleistocene time or to any part of the Recent.

8. Third Lake of Fulton Chain, Herkimer County.—In the publication just referred to and on page 45, Merriam stated he had seen a number of elk antlers, found in a bog near the place mentioned. Their geological age can not be determined any more closely than in the preceding case.

9. Steele’s Corners, St. Lawrence County.—On page 46 of the paper just cited, Merriam reported that Dr. C. C. Benton, of Ogdensburg, had parts of antlers discovered at the place named. No details as to mode of occurrence were given. The antlers were discarded by their owners some time after the clearing away of the Wisconsin drift.

NEW JERSEY.

(Map 23.)

1. Deal, Monmouth County.—In 1869 (Jour. Acad. Nat. Sci. Phila., vol. VII, p. 377), Leidy stated that there were in the museum of the Philadelphia Academy portions of two antlers of the elk obtained in the earth just above the Cretaceous greensand near Deal. No further information was furnished. Deal is about 5 miles south of Long Branch. The antlers may have belonged to the Pleistocene or to the Recent.

2. Trenton, Mercer County.—In 1911 (Papers Peabody Mus., vol. V, p. 123), Mr. Ernest Volk detailed the finding of a fragment of an antler of an elk in the glacial gravels at Trenton, at a depth of 5.5 feet. For the geology of this locality see page 304.

Cope (Cook’s Geol. N. J., 1868, p. 742) wrote that this species has left antlers and bones in various parts of the State in the gravel drift, but he mentions no localities.

PENNSYLVANIA.

(Map 23.)

1. Stroudsburg, Monroe County.—In 1899 (Ann. Rep. Geol. Surv., Pennsylvania, for 1887, p. 6), Leidy reported the discovery of various fragmentary remains of this species in the Crystal Hill (Hartman’s) Cave, near Stroudsburg. This cave and its contents will be considered on page 310.

2. Riegelsville, Bucks County.—From Durham Cave, situated near Riegelsville, there was sent to the Academy of Natural Sciences of Philadelphia, about 70 years ago, a collection of bones. They were examined by Leidy, who reported on them (Proc. Acad. Nat. Sci. Phila., 1880, p. 349). In this list the elk was not mentioned. In 1889 (Ann. Rep. Geol. Surv. Pennsylvania, 1887, pp. 18, 19), further attention was given to the collection, and the elk was included. The bison, which was mentioned in the first list, was omitted in the second.

MICHIGAN.

(Map 23.)

1. Adrian, Lenawee County.—In 1880, Professor J. Kost, of Adrian College, sent to the U. S. National Museum a skull of Castoroides ohioensis and a jaw of a mastodon found in a marsh in the town of Adrian, at a depth of 4 feet. At the same place another mastodon, together with bones of a deer and of an elk, had previously been secured. These belong to a late period in the Wisconsin.

2. Ann Arbor, Washtenaw County.—In 1908 (Folio 155, U. S. Geol. Surv., p. 9), Russell and Leverett told of the finding of bones of elk and deer in a peat-swamp, 3 miles south of Ann Arbor. In the same swamp, at a depth of 5 feet, a skull of Castoroides ohioensis had been discovered. The bones of the elk and deer were at a somewhat higher level. While they are probably of late Pleistocene age, one can not be wholly sure of it.

INDIANA.

(Map 23.)

1. Cambridge City, Wayne County.—In the collection of Earlham College, at Richmond, Indiana, is a part of the skull of an elk (No. 5070) labeled as found a mile northwest of Cambridge City, and as presented by Lee Ault, superintendent [of schools?]. It is recorded on the specimen that it was found in Little Simond’s Creek and lay partly exposed in a bed of gravel 4 rods below the mill-dam, and 0.25 mile from where the creek empties into the West Fork of Whitewater River. The specimen is pretty thoroughly mineralized and stained with iron oxide. The geological age of the skull is uncertain, but it has the appearance of being old. Found in that region, it must, however, be younger than the Shelbyville and Bloomington moraines, which are nearby.

2. Fountain City, Wayne County.—In Earlham College is the rear of the skull of an elk recorded as found on Nolan’s Fork, near the border of the Bloomington moraine. It has the No. 5069 and is credited to Mr. Isaac Thomas. The remark made in the preceding paragraph about the age of the specimen from Cambridge City may be repeated here.

3. Harrisville, Randolph County.—In the collection at Earlham College, Richmond, are some bones which belong to Cervus canadensis and reported found in May 1893, by Messrs. Shoemaker, Graves, and Moore, in a ditch or canal being put through the swamp known then by the name of “The Dismal,” apparently about 6 miles east of Winchester, near the town of Harrisville. It was here that was found the fine specimen of Castoroides ohioensis which is at Earlham. Just at what depth the elk bones were found is not known. With them came some bones of the white-tailed deer, Odocoileus virginianus. Of the elk there are a dorsal and two lumbar vertebræ, most of the sacrum, some pieces of ribs, the articular end of the scapula, a complete humerus, most of the right side of the pelvis, most of the left pubis, the left cubo-navicular bone, the distal end of the left cannon-bone, and three phalanges.

We can not be certain that the animal lived at that place during Pleistocene times. At most, it lived after the Wisconsin ice had withdrawn from that vicinity. Dr. A. J. Phinney (Geol. Surv. Indiana, vol. XXI, p. 181) stated that in draining swamps in this county elks’ antlers had been found, but no details were given. At any rate, in that region all such remains would belong to a time following the middle of the Wisconsin stage.

4. Pennville, Jay County.—McCaslin, in his report on the geology of Jay County (Geol. Surv. Indiana, vol. XII, p. 169), stated that the bones of the mastodon and post-glacial deer, or elk, had been frequently met with. “The gigantic antlers of the latter have been found in size indicating an animal 8 or 9 feet high and 10 or 11 in length. These have been picked up in a bog north of Camden.” Making proper allowances for miscalculations, we must conclude that these antlers belonged to the elk (Cervus canadensis). The antlers had probably been laid out so as to give their maximum extent. This township (24 north, range 12 east) is in the northwest corner of the county. The name Camden no longer appears on the maps, being apparently a former name for Pennville. The bog referred to was evidently north of the Salamonie River and close to or on the moraine bearing the same name. The elk must have lived there after, probably a long time after, this moraine was laid down.

5. Wabash County.—Elrod and Benedict reported in 1892 (Geol. Surv. Indiana, vol. XVII, p. 240) that a Mr. Longnecer had unearthed the head and antlers of an elk in a swamp on his farm “near the west county line.” The antlers measured 8 feet from tip to tip. In this case they probably were given their greatest possible span. It is to be regretted that no more definite locality was given. For those in that region who might be interested, it would be possible to learn the location more accurately by searching the office of the county surveyor or of the county clerk. At any rate, the animal lived there in Late Wisconsin time.

6. Foresman, Newton County.—In the State Museum at Indianapolis is the left antler of an elk said to have been found in 1884, at Foresman. It is credited to D. E. Howe, and the writer has not been able to get any additional information. Foresman is on Iroquois River; and, according to Leverett’s map (Monogr. LIII, plate VI), the region about there is occupied by clay of a glacial lake bottom. The antler may be of the Recent period, but more probably of Late Wisconsin times.

7. Rensselaer, Jasper County.—In the State collection at Indianapolis just mentioned is a part, about 16 inches long, of the antler of an elk, presented by Dr. Loughridge, of Rensselaer, but no additional information is furnished. The animal may have lived at any time during or since the Late Wisconsin stage.

8. Lake County.—In the Twenty-second Annual Report of the State Geologist of Indiana, page 90, Blatchley stated that antlers of the elk had been found in this county, but no details were given.

9. Kouts, Porter County.—In the report just cited, on page 90, Blatchley, State geologist, reported antlers of a large elk found close to teeth of a mastodon. This was somewhere near Kouts.

The reports of fossil remains of Cervus canadensis in Indiana are not very satisfactory. In few cases has any effort been made to record anything like exact information as to the locality and the depth of burial and the nature of the deposit and to preserve the specimens. Nevertheless, in most instances at least, it is quite certain that the remains referred to this species were really such. While, again, some of the remains have possibly belonged to the Recent period, probably most of them date back to late Pleistocene; that is, Late Wisconsin times. In many cases the remains have been found at a depth of several feet in swamps that were being drained. It is certain that these swamp deposits accumulated with exceeding slowness. Not infrequently fossil mastodon bones and teeth have been found within a few inches of the surface. In the case of none of the finds of elk materials is there any indication of an age beyond that of the Late Wisconsin.

ILLINOIS.

(Maps 23, 38.)

1. Niantic, Macon County.—in 1873 (Geol. Surv. Illinois, vol. V, p. 308), A. H. Worthen reported the discovery of remains of mastodon, elk, buffalo, and deer in a bog near Niantic. The exact locality and the conditions are described on page 102. In that account it is concluded that the mastodon remains went to the museum of C. F. Günther, of Chicago, and from there to the collection of the Chicago Academy of Sciences. What became of the bones of the elk, the buffalo, and the deer is not known. As no record appears to have been kept of the depths at which each of the species was found, we do not know whether or not the others were as old as the mastodon. However, it is certain that these old ponds and marshes left on the surface of the Wisconsin drift filled up very slowly.

2. Near Whitewillow, Kendall County, 5 miles west by north of Minooka.—Dr. E. S. Riggs, of the Field Museum of Natural History, informed the writer that he had found here bones of the elk. These were also reported by him in Netta C. Anderson’s list (Augustana Coll. Publ., No. 5, page 11). Mr. George Langford, of Joliet, has likewise found elk antlers here and remains of Cervalces and Alces americanus.

For the location of this place and its geological situation page 337 may be consulted. All the species found are without doubt of Late Wisconsin age. Riggs’s statement referred to appears to indicate that the elk, buffalo, and deer bones found are of more recent age than those of the mastodons, but Mr. Langford writes that the antlers were mixed up with the mastodon bones.

3. Palos Park, Cook County.—This place is on the Wabash Railway, about 20 miles southwest of Chicago. Dr. E. S. Riggs wrote the author that in October 1915, the Field Museum of Natural History had received a fine head and antlers of the elk from the Sag Drainage Canal near Palos Park. It was found in peat at a depth of 13 feet. One can hardly doubt that the animal lived there during the latter part of the Wisconsin stage.

4. Batavia, Kane County.—Dr. E. S. Riggs, writing April 3, 1916, informed the author that he had picked up the jaw of an elk along a ditch, somewhere about Batavia, in which mastodon bones had been found. At what depth the bones had been buried could not be determined. In this case all that can be said is that the animal lived there after the Wisconsin ice had retired from that place.

5. Union Grove, Whiteside County.—In the U. S. National Museum, No. 7335, is a right astragalus of an elk found near Union Grove, 3 feet below the surface of a bed of peat, in an old channel of the Mississippi River. This astragalus was presented by Mr. Leo B. Lincoln, of Chicago, through the peat expert of the U. S. Geological Survey, Professor Charles A. Davis.

The locality is said to be in the southeast quarter of the southeast quarter of section 7, Union Grove Township, apparently township 21 north, range 4 west. This section appears to be about 5 miles away from the present bed of the river. Although the area is outside of the Wisconsin drift-sheet, it is not probable that the elk antedates the Wisconsin stage. Its age is more probably Late Wisconsin.

6. Lead Region of Illinois.—In 1876, J. A. Allen (Amer. Jour. Sci., vol. XI, p. 48) stated he found in a collection made in this region by J. D. Whitney an imperfect radius that seemed not to differ at all from that of a young male Cervus canadensis. This collection is that reported on by Jeffries Wyman in 1862 (Geol. Surv. Wisconsin, vol. I, pp. 421–423). It is impossible to say whether the specimen was found in Wisconsin, Iowa, or Illinois.

As elsewhere stated, the writer formerly regarded the vertebrate fossils found in that region as belonging mostly to the Late Wisconsin; but it now appears possible they lived during a pre-Wisconsin time.

7. Beecher, Will County.—Mr. George Langford, of Joliet, Illinois, an intelligent collector of the fossils of that region, informed the author that he obtained an antler of the Cervus canadensis at a place along Trim Creek, about 3 miles north of east of Beecher. The fragment included the base and two tines. The exact locality and the geological conditions are discussed on page 107. Mr. Langford reported that the antlers were above the mastodon bones. At the same place was found a fragment of an antler of Cervalces. All these species belonged probably to very late Pleistocene time.

WISCONSIN.

(Map 23.)

1. Wauwatosa, Milwaukee County.—In the Public Museum of Milwaukee are parts of both antlers of an elk found at Miller’s brewery, in Wauwatosa, at a depth of 4 feet.

Wauwatosa is a suburb west of Milwaukee, on the Menomonie River, situated principally on one of the moraines laid down just before the Wisconsin ice-sheet retired into Lake Michigan. The elk must have lived there since that withdrawal of the ice. It is possible that the antlers were found in marsh deposits of Recent age along the Menomonie River.

2. Pewaukee, Waukesha County.—This town is situated about 20 miles north of west of Milwaukee. In the Public Museum at Milwaukee is an antler which was plowed up somewhere about Pewaukee by Stanley G. Haskins and presented by him to the museum. Probably the antler belongs to the Recent epoch.

3. Whitehall, Trempealeau County.—From Dr. S. Weidman, State geologist of Wisconsin, the writer received a tibia found near Whitehall and which he identifies as belonging to Cervus canadensis. The following account of the discovery has been furnished by Dr. Weidman:

“The gully (fig. 2) in which the tibia was found is eroded out of stratified sand, containing fragments of local sandstone and cherts. The stratified sand, with local small fragments of sandstone, is, of course, pre-loessial in origin, but the erosion of the lower terrace is post-loessial, and the gully is very recent. The tibia was taken 2 feet below the lower terrace, along the side of the gully about 5 or 6 feet deep at the lower end and 3 or 4 feet deep at the upper end; length of gully 300 or 400 feet. The bone may possibly have been inserted after the development of the lower terrace, but I could see no indication of disturbance or change in the upper 2 feet of the lower terrace further exposed by the gully at this point, the upper 2 feet being essentially the same at this point as elsewhere along the side of the gully. If the bone was deposited along with the small fragments of sandstone in the stratified formation, the fragments being usually flat, about 0.5 inch thick by 1 to 2 inches wide, then the bone is evidently pre-loessial in age. I am inclined to think the bone was deposited with the sandstone fragments during the process of the filling up of the valley with the stratified surface, long before the loess was deposited in the region, rather than after the loess and the lower terrace was formed.”

According to this account the specimen belonged to the Peorian stage or an earlier one.

MARYLAND.

(Map 23.)

1. Oxford Neck, Talbot County.—In 1869 (Proc. Amer. Philos. Soc., vol. XI, p. 178), Cope stated that a collection of vertebrate fossils had been found on the farm of Lambert Kirby, in Oxford Neck, including parts of antlers. These were not distinguishable from those of the elk and the Virginia deer. They were placed in the Baltimore Academy of Natural Sciences.

NORTH CAROLINA.

(Maps 23, 39.)

1. On Neuse River, Pamlico County, 16 miles below Newbern.—On page 117, in discussing the occurrence of mastodons at this place, it is stated that H. B. Croom had reported also the presence of elk remains. A more competent witness was Richard Harlan, who included the elk in his list of species (Amer. Jour. Sci., vol. XLIII, 1842, p. 143). The reader is referred to page 358, where the locality and the species are further considered.

SOUTH CAROLINA.

(Map 23.)

1. Charleston, Charleston County.—Dr. Joseph Leidy does not seem to mention the occurrence of the wapiti at Charleston. F. S. Holmes, in the introduction to his work on Post-Pliocene fossils of South Carolina, page 7, mentions the elk among the animals found in the Pleistocene beds which still have living representatives.

In the collection of the Academy of Natural Sciences, at Philadelphia, are two teeth, labeled as from Ashley River and credited to Captain A. H. Bowman. It is possible that Leidy did not mention them because he regarded them as teeth of elk that lived within Recent times.

GEORGIA.

(Map 23.)

1. Brunswick, Glynn County.—In a list of fossil vertebrates dredged, probably, from the harbor at Brunswick, Gidley (Bull. No. 26, Geol. Surv. Georgia, p. 436) announced the finding of some part, supposedly a tooth, of a cervuline, “probably belonging to the genus Cervus.” That C. canadensis might have lived in that region during some part of the Pleistocene is not at all improbable; that it lived there during the time that Megatherium existed we have not at present sufficient evidence.

FLORIDA.

(Map 23.)

1. Alafia River, Hillsboro County.—From the late Professor F. W. Putnam the writer learned that he had obtained from Alafia River some part of the elk. The present writer has not seen the specimen.

TENNESSEE.

(Figure 23.)

Whitesburg, Hamblen County.—In a collection of fossil vertebrates secured at Whitesburg and described by the writer in 1920 are some fragments of teeth which were referred to Cervus canadensis (Proc. U. S. Nat. Mus., vol. LVIII, p. 92). A list of the species is presented on page 395.

KENTUCKY.

(Map 23.)

1. Bigbone Lick, Boone County.—In his report of 1831 on Bigbone Lick, William Cooper (Monthly Amer. Jour. Geol., vol. I, p. 207) stated that he had found remains of Cervus canadensis; but he did not appear to be wholly certain of this. Shaler was likewise in doubt regarding the presence of the elk (Geol. Surv. Kentucky, vol. III, n. s., p. 197). Other authors have mentioned the elk as occurring here, but not in a convincing way. Nevertheless, it is not at all improbable that this species was represented here. The geology of this locality is considered on pages 401 to 404 and a list of the species is presented.

2. Bluelick Springs, Nicholas County.—In the collection of fossil vertebrates secured by Mr. Thomas W. Hunter, living near Bluelick Springs, were teeth, some bones, and fragments of antlers. This collection had been secured in an attempt to clean out and restore the failing springs. Whether or not these remains date back to the Pleistocene is uncertain. They are reported to have been found above the bones of the mastodon.

FINDS OF RANGIFER IN THE PLEISTOCENE OF EASTERN NORTH AMERICA.

GRINNELL LAND.

Dumbbell Harbor.—In 1877 (Ann. Mag. Nat. Hist., ser. 4, vol. XX, p. 488), Fielden published a paper on the post-Tertiary beds of Grinnell Land and north Greenland. In 1878 (Quart. Jour. Geol. Soc. Lond., vol. XXXIV, p. 566), Fielden and De Rance presented a report on the same subject.

At a station in latitude 82° 30′ N., in beds at an elevation of 400 feet, there were secured meager remains of Ovibos moschatus and Phoca hispida. At another station, in latitude 82° 25′, there were obtained remains of Rangifer tarandus, Ovibos moschatus, and Phoca barbata. The invertebrate fauna was found to be identical with that now existing there. In case the beds are Pleistocene they are probably those of a late stage.

ONTARIO.

(Map 24.)

1. Toronto, York County.—In 1899 (Ottawa Naturalist, vol. XII, p. 195), Coleman stated that horns of the caribou were common in the Carleton Bar, just west of Toronto. This bar belonged to the Iroquois beach. In the same bar near York, east of Toronto, mammoth teeth had been found. In 1904 (Jour. Geol., vol. XV, p. 366), the same writer states that antlers are very common at Toronto Junction. This is probably the same locality as that spoken of as Carleton Bar.

In 1901 (Jour. Geol., vol. IX, pp. 290, 298), Coleman wrote that a shed horn of a caribou had been found at Taylor’s brickyard. This is nearly a mile north of the Gerard street bridge in Toronto (Amer. Geologist, vol. XIII, p. 87). It was in a blue peaty clay, in which were found also unios and wood. This clay is about 4 feet 6 inches thick and near the top of the warm-climate beds. Notwithstanding the presence of the antler of a caribou, the stratum is assigned by Coleman to the warm-climate beds, because of the character of the vegetation. At present the caribou is not known to come nearer than 150 or 200 miles to Toronto.

VERMONT.

(Map 24.)

1. Woodbury, Washington County.—In 1910 (Rep. Geol. Surv. Vermont, p. 7), Professor G. H. Perkins stated that there are in the State Cabinet at Burlington a fully developed antler and a part of the upper jaw, with five molars, of Rangifer caribou found at Woodbury in a peat-bog at a depth of 7 feet. Probably the animal lived at about the close of the Pleistocene epoch. The species has not been known in the State since historical times.

CONNECTICUT.

(Map 24.)

1. New Haven, New Haven County.—In 1875 (Amer. Jour. Sci., ser. 3, vol. X), Professor J. D. Dana gave an account of the finding of a humerus and a tibia of a reindeer in the Quinnipiac Valley, near New Haven. The humerus was discovered in a bed of clay at a depth of 11 feet; the tibia at a depth of 7 feet. The two bones belonged to different individuals. Marsh, as quoted by Dana, thought that the tibia resembled more closely that of Rangifer tarandus of Europe than it did that of R. caribou, but that the humerus was more similar to that of the caribou. Dana concluded that the clays had been laid down after the glacier had retreated from the valley, but while it was yet near enough to send down ice-floes. Woodworth (17th Ann. Rep. U. S. Geol. Surv., pt. 1, p. 978) was inclined to refer the clays to some pre-Wisconsin time.

NEW YORK.

(Map 24.)

1. Ossining, Westchester County.—In 1859, Dr. Joseph Leidy (Proc. Acad. Nat. Sci. Phila., vol. XI, p. 194) read a letter from Dr. G. J. Fisher, of Ossining (then Sing Sing), in which was reported the finding of an antler of a reindeer in that vicinity, in excavating a peat-bed, 6 feet from the surface. The peat-bed had an area of about an acre, was surrounded by high ground, and looked as if it had been the site of an ancient lake. It is to be regretted that the situation of the place was not more accurately given.

Woodworth (Bull. 84, New York State Mus., 1905, p. 187) remarked that he did not know the circumstances under which the reindeer remains had been found; but its occurrence there was consonant with his views of the non-submergence of the lower Hudson valley. On the other hand, there appears to be no good reason why the caribou might not have occupied that region step by step as the glacier retired, and have remained there long enough for its bones to become buried in mucks overlying the deposits laid down in the Hudson while it was at sea-level.

2. Racket River, St. Lawrence County.—In 1869 (Jour. Acad. Nat. Sci. Phila., vol. VII, p. 377), Leidy mentioned the occurrence of caribou (“Cervus tarandus”) remains at Racket River, basing his statement on a remark of S. L. Mitchill (Cat. Organ. Remains, 1826, p. 26). On the same page Leidy referred to Mitchill’s skull of the elk found at Racket River, and to De Kay’s figure of it. In De Kay’s description (Zool. N. Y. Mamm., p. 120) of the skull he stated that it bore a label in Mitchill’s handwriting purporting that the skull belonged to the reindeer. It looks, therefore, very much as if the crediting of the caribou to this locality is due to an error of identification on the part of Mitchill; on the other hand, it is barely possible that Mitchill had remains of both animals from the locality.

NEW JERSEY.

(Map 24.)

1. Vincentown, Burlington County.—In 1869 (Jour. Acad. Nat. Sci. Phila., vol. VII, p. 377, plate XXVIII, fig. 9), Leidy described and figured a part of an antler of a reindeer found at Vincentown. It was discovered 4 feet from the surface in soil overlying greensand. According to Lewis and Kümmel’s geological map, the region about Vincentown is occupied by Cape May deposits resting on Manasquan marl, of Cretaceous age. It may be supposed, therefore, that this reindeer was in that region during the prevalence of the Wisconsin glacial stage (Geol. Surv. New Jersey, vol. VIII, p. 183). This antler is peculiar in having no brow-tine, in having the bez-tine placed at an unusual height, 6 inches above the base, and in having no tine arise from the rear of the shaft up to a height of about 2 feet from the base. Where the last-mentioned tine might be expected is simply a sharp ridge. Leidy thought that the antler resembled more closely that of the barren-ground reindeer than that of the woodland reindeer. It may, however, belong to a distinct but as yet unnamed species.

2. Trenton, Mercer County.—In 1884 (17th Ann. Rep. Peabody Mus., Harvard Univ., for 1883, p. 372), Professor F. W. Putnam reported as follows on a fragment of antler of Rangifer found at Trenton by Dr. C. C. Abbott: “A piece of worked antler, probably a handle to a stone knife, from the gravel in the railroad cut where the human tooth (No. 27798) was found. Collected and presented by Dr. C. C. Abbott.”

This specimen is mentioned by Mr. S. N. Rhoads (Mamm. of Pennsylvania and New Jersey, 1903, p. 241) as belonging to Rangifer grœnlandicus. From Dr. C. C. Willoughby, director of Peabody Museum, the writer learns that this part of an antler is yet in that museum. He writes that it has been a handle for apparently a steel knife and that he sees nothing whatever about the specimen to indicate a prehistoric origin. It may, he thinks, have been washed out of some recent Indian grave. In a personal letter to Mr. S. N. Rhoads, Professor Putnam wrote that the fragment had been identified by Dr. J. A. Allen as belonging to Rangifer. In 1883 (Jour. Franklin Inst., vol. CXV, pp. 366, 374), H. C. Lewis stated on the authority of Dr. C. C. Abbott that remains of Rangifer had been discovered in the Trenton gravels.

PENNSYLVANIA.

(Map 24.)

1. Stroudsburg, Monroe County.—In Crystal Hill (Hartman’s) Cave, near Stroudsburg, there was found, many years ago, bones and teeth of what Leidy (Proc. Acad. Nat. Sci. Phila., 1880, p. 347) called Rangifer caribou. In 1889 (Ann. Rep. Geol. Surv. Pennsylvania for 1887, p. 5) the remains are spoken of as fragments of jaws and teeth.

2. Riegelsville, Bucks County.—In his earliest mention of remains found in Durham Cave, near Riegelsville, Leidy included the woodland caribou (Rangifer caribou). In his list published in 1889 (Ann. Rep. Geol. Surv. Pennsylvania for 1887, p. 18) this species is not included, but the writer does not know why it was not.

ILLINOIS.

(Map 24.)

1. Alton, Madison County.—In the collection of fossils made in the region about Alton by William McAdams, a list of which will be given on page 339, is a single upper right molar, the first or second, which belongs to this genus. The tooth has McAdams’s No. 11. To the base of the tooth a mass of very hard matrix adheres and a part of the grinding-surface is covered by the same material. The tooth is likewise somewhat shattered. The length of the tooth is 19 mm., the width across the anterior lobe 13.5 mm.

From the materials at hand it is not possible to determine to what species the tooth belonged. It is referred provisionally to Rangifer muscatinensis. This tooth differs from other Rangifer teeth observed in having the front of the protocone, at its base, less fully rounded out, and in that the mesostyle, on the inner face of the tooth, widens more extensively as it approaches the base than in any other species observed. Nevertheless, the width of the mesostyle varies in species and individuals.

WISCONSIN.

(Map 24.)

1. Menomonie, Dunn County.—From Professor S. Weidman, of the Wisconsin Geological and Natural History Survey, the writer received a part of an antler of a female or a young individual of some species of Rangifer. Professor Weidman sends the information that this was obtained in a sand formation just below the clays worked at Menomonie for brick. He regards the brick-clays as being of Sangamon interglacial age. He states, too, that a part of a leg-bone believed to belong to a mastodon had been found in the clays; also bones of a fish, which have been identified by Dr. Hussakof as the Mackinaw trout, Cristivomer namaycush (Jour. Geology, vol XXIV, pp. 685–689, figs. 1, 2).

Probably the caribou represented by this specimen lived in that region at the beginning or at the close of some one of the glacial stages, when the climate was yet severe. The supposed mastodon bone may have belonged to Elephas primigenius. It is described on page 111.

At a later time Dr. Weidman sent the writer a large part of the beam of an antler of a caribou which likewise had been found in the lacustrine clay at Menomonie. It was met with in the red clay, near the top of the lacustrine clay bed.

KENTUCKY.

(Map 24.)

1. Bigbone Lick, Boone County.—The presence of reindeer bones at this place appears first to have been mentioned by William Cooper (Monthly Amer. Jour. Geol., vol. I, p. 207). He wrote that “antlers, jaws, and other remains of Cervus canadensis, C. virginianus, C. alces, and perhaps C. tarandus are not very rare.” Shaler (Proc. Bost. Soc. Nat. Hist., vol. XIII, 1871, p. 167; Geol. Surv. Kentucky, n. s., vol. III, p. 197) reported that antlers of the caribou had been found by him here. A list of the species found at Bigbone Lick will be given on page 403.

FINDS OF MUSK-OXEN IN THE PLEISTOCENE OF EASTERN NORTH AMERICA.

GRINNELL LAND.

Dumbbell Harbor.—In 1877 (Ann. Mag. Nat. Hist., ser. 4, vol. XX, p. 488), H. W. Fielden presented a paper on the post-Tertiary beds of Grinnell Land and north Greenland. He reported the discovery of a bone and a tooth of Ovibos moschatus and a bone of Phoca hispida in deposits at an elevation of 400 feet. This was in latitude 82° 30′ N. At another station, in latitude 82° 25′, Fielden procured fossil remains of Rangifer tarandus, Ovibos moschatus, and Phoca barbata. A report to the same effect was presented by Fielden and De Rance in 1878 (Quart. Jour. Geol. Soc. Lond., vol. XXXIV, p. 566).

NEW JERSEY.

(Map 25.)

1. Trenton, Mercer County.—In 1900 (Ann. Rep. Amer. Mus. Nat. Hist. for 1899, p. 16), Professor F. W. Putnam stated that Mr. Ernest Volk, of Trenton, had found in the Trenton gravels a part of the scapula of a musk-ox, now at the American Museum of Natural History, New York. The part present is that bearing the glenoid cavity. This report is reprinted on pages 248 to 249 of Volk’s “Archæology of the Delaware Valley” (Papers Peabody Mus., vol. V). On page 111 of this work, Mr. Volk gives an account of the discovery of the bone, and illustrates it by plates LXXXVI and LXXXVII. The bone was identified by Putnam, Matthew, Allen, Boas, Lambe, True, and Lucas. Inasmuch as the comparison must have been made with the scapulas of Ovibos moschatus, the fossil probably belonged to this species.

PENNSYLVANIA.

(Map 25.)

1. Pittston, Luzerne County.—In 1872 (Contrib. Ext. Fauna West. Terrs., p. 255, plate XXVIII, fig. 8), Leidy briefly described and figured a molar tooth which he referred to Bison latifrons. It had been found along the bank of Susquehanna River at Pittston, associated with the mastodon and a horse. Dr. J. A. Allen (Amer. Bisons, 1876, p. 12) expressed the opinion that the tooth belonged to some species of Ovibos. The present writer agrees that the tooth is not that of Bison. It seems to agree more nearly with teeth of Symbos cavifrons; but it differs from the teeth of that species in some respects. The writer has examined this tooth at the Academy of Natural Sciences at Philadelphia. It is worn almost to the roots and is 34 mm. long and 32 mm. thick at the base of the hinder lobe. It agrees in form more closely with the first molar of both Ovibos and Symbos; but it is much larger than the same tooth in Ovibos moschatus and somewhat larger than that of Symbos cavifrons. The inner face of the anterior lobe is much more rounded than in Symbos, and the inner face of the hinder lobe forms an angle with the hinder face, instead of rounding into it, as it does in Symbos cavifrons. The teeth appear to have been packed together more closely, on the lingual side, than in Bison, Symbos, and Ovibos. The tooth is probably worthy of being given a new name.

Mr. S. W. Rhoads has examined this tooth and concluded that it belonged to Bison bison. To this view it seems sufficient to say that in Bison teeth the outer face of each of the lobes is very convex and column-like, while the parastyle and especially the mesostyle are relatively small. In the Pittston tooth the mesostyle stands out beyond the outer face of the hinder lobe, and the latter is nearly flat; this is also the condition in Symbos. The writer will say further that the accessory column is not always present in teeth of Symbos.

2. Riegelsville, Bucks County.—Mr. Rhoads, as cited above, on pages 246 to 248, described a part of a horn-core of a bovine animal to which he applied the name Bison appalachicolus. Later (Proc. Acad. Nat. Sci., Phila., 1897, p. 492) he concluded that the horn-core had belonged to an animal of the genus Ovibos; and accordingly it bears the name O. appalachicolus. Leidy had in 1889 called attention to a collection of bones made in Durham Cave, near Riegelsville (Ann. Rep. Geol. Surv., Pennsylvania, for 1887, pp. 18–19). He recorded 20 species, all of which lived there or at most, not far away, when the country was discovered. These may have all entered the cave at a later period, but the musk-ox may have antedated the others. A list of these fossils is presented on page 311.

OHIO.

(Map 25.)

1. Urbana, Champaign County.—At Urbana, Ohio, in the possession of Mr. Charles McDarg, the writer has seen a skull of Symbos cavifrons which had been found on the farm of Ed. Jennings, while a ditch was being dug. It was buried in mud at a depth of 10 feet. This region is covered by the Wisconsin drift, and the animal must have lived not long after the ice had withdrawn from the neighborhood.

2. Youngstown, Mahoning County.—In the geological collection of the Ohio State University is a part of a skull of Ovibos moschatus secured at Youngstown. The specimen shows the base of the skull and the forehead. Between the bases of the horns is a narrow channel, characteristic of Ovibos. The specimen shows the effects of abrasion, the horn-cores being worn down to their bases. The specimen is said to have been found in gravel at a depth of 60 feet. It appears to have been presented in 1890 by H. McGinnis. It is probable that this skull was found along Mahoning River, but the elevation was, unfortunately, not given. The probability is that the deposits inclosing the fossil were laid down during the Wisconsin stage.

According to Leverett (Monogr. U. S. Geol. Surv., XLI, p. 149), the old trough of Beaver River was filled with gravel during the Wisconsin glacial stage, and this filling is now in process of excavation. The same is probably true of its tributary, the Mahoning. If the skull was buried in this gravel its age is thereby determined.

3. Trumbull County.—In 1853 (Smith. Contrib. Knowl., vol. V, art. 3, p. 16), Leidy stated that he had received, for inspection, from Professor Samuel St. John, of Hudson, Ohio, a fragment of a skull, with one horn-core attached, which had been found in Trumbull County. No further details were given as to the locality or of the geological conditions. The skull appeared to be much water-worn. It belongs to Symbos cavifrons. Trumbull County is wholly occupied by Wisconsin drift. The animal is, then, probably to be credited to the Late Wisconsin. It is possible, however, that this skull was found in an older deposit exposed in the valley of some stream.

MICHIGAN.

(Map 25.)

Up to the present time it appears that remains of musk-oxen have been found in Michigan in only two localities, Manchester, Washtenaw County, and near Moorland, in Muskegon County. These remains belonged to two different genera, Symbos and Boötherium.

1. Manchester, Washtenaw County.—In No. 13 of the Occasional Papers of the Museum of Zoology, pages 1–3, plates I, II, issued by the University of Michigan, November 12, 1915, Dr. E. C. Case reported the finding of a fine skull of Symbos cavifrons at a place near Manchester. This was given by Case as being about 3 miles northeast of Manchester, but Mr. Schlicht, owner of the farm, has sent the writer a description and plat of the section which show that the spot is situated about 0.5 mile northwest of the town. It is near the center of the northwest quarter of the northwest quarter of section 1, township 4 south, range 3 east. A drain was being made in a swampy tract and the skull was found at a depth of 4 feet, lying on a bed of clay. This was covered by a black muck filled with plant remains and interrupted by a few thin layers of fine gravel.

The skull was in fine condition, but lacked the lower jaw. The spade of a workman struck the nose and injured the bones so that some parts were lost. The teeth were almost perfectly preserved.

The locality which furnished this skull is in the valley of the Raisin River. According to Leverett’s glacial map of Michigan (Monogr. U. S. Geol. Surv., LIII, plate VII), this valley crosses, at this point, the northern end of the Fort Wayne moraine. It is not improbable that this musk-ox lived when the foot of the ice-sheet was not far removed. Even in case the skull had gotten into a drainage channel it could not, because of its fine state of preservation, have been moved far from where the animal died. The circumstances appear to indicate that the skull had been left on the clayey bottom of a shallow pond of a tundra and become covered by the muck of a milder epoch.

2. Moorland, Muskegon County.—In 1908 (Proc. U. S. Nat. Mus., vol. XXXIV, p. 683, plate LXXIX), J. W. Gidley described, as belonging to a new species, Boötherium sargenti, a skull of a musk-ox found on the farm of Mr. Charles McKay, reported to be near Grand Rapids. Further inquiry showed that the farm is located near Moorland, in the northeast quarter of section 16, township 10 north, range 14 west. The skull was found in a marsh at a depth of 2 or 3 feet and lying beneath the pelvis of a mastodon. It and the mastodon are now preserved in the Kent Scientific Museum, at Grand Rapids, Michigan.

In 1915 (Proc. U. S. Nat. Mus., vol. XLVIII, p. 525, plate XXXI), the writer redescribed the specimen. Dr. J. A. Allen, in 1913 (Mem. Amer. Mus. Nat. Hist., vol. I, pp. 214, 215), referred to this skull and concluded that it had belonged to the female of Symbos cavifrons. The writer does not accept this opinion. He has examined more than 25 skulls of S. cavifrons, some of which must have been females. In none did the rough surfaces for the horns fail to meet at the midline as it does fail in the Moorland specimen.

The Moorland marsh is surrounded by what Leverett has called the Lake Border moraines. It is probable that this musk-ox existed there after, but not long after, the ice had withdrawn into Lake Michigan. From what is known about the habits of musk-oxen in general, we must conclude that the climate was yet cold.

The fact that the mastodon remains were so closely associated with the musk-ox skull does not prove that the animals lived there together. Near Alma, in Gratiot County, the late Charles A. Davis found mastodon bones in a peat-bog within a few inches of the surface. If by chance the pelvis of a modern horse or cow had fallen on that spot, it might easily have been pressed down into contact with those bones.

INDIANA.

(Map 25.)

1. Wailesboro, Bartholomew County.—In the American Museum of Natural History, New York, is a portion of a skull of a musk-ox which the writer identifies as Symbos cavifrons. It is labeled as found along the East Fork of White River, in 1904, near Wailesboro, Bartholomew County, Indiana. This locality is about 45 miles east of south of Indianapolis. The skull is reported to have been washed out of a bank composed of alluvium which overlies from 10 to 20 feet of glacial gravel. It is also said that out of the same gravel a tooth of Elephas primigenius had been secured. It seems to be implied that the musk-ox skull came from the gravel; but the record is not clear. It was presented to the museum in New York by Dr. J. J. Edwards, of Columbus, Indiana. He is said to have been interested to some extent in collecting palæontological materials. It is likely that he depended on others for his knowledge of the origin of the skull.

The specimen presents the brain-case to the rear of the orbits, including the basioccipital bone and the bases of the horn-cores. It has been rolled somewhat and many ridges and processes have been eroded off. Measurements were given by the writer in his paper on the “Pleistocene Period in Indiana and its Vertebrata” (Geol. Surv. Indiana, vol. XXXVI, pp. 638–639). Dr. J. A. Allen (Mem. Amer. Mus. Nat. Hist., vol. I, p. 201) has examined this skull and concluded that it is not specifically determinable, but the writer, after re-examining the specimen, sees no reason for changing his original conclusion.

This skull was found within the area of Illinoian drift; but the border of the Wisconsin forms the high ground just east of the river. According to Leverett’s glacial map of Indiana (Monogr. LII, U. S. Geol. Surv., plate VI), the valley of the river is filled with sands and gravels resulting from glacial drainage, and this came mostly, if not all, from the Wisconsin ice. Most probably the animal which possessed this skull lived there at some time when the Wisconsin glacial ice was not far away.

2. Richmond, Wayne County.—In the collection at Earlham College, Richmond, Indiana, is the brain-case of a skull identified as that of Ovibos moschatus. This fragment was described and figured by the writer in 1912 (Geol. Surv. Indiana, vol. XXXVI, p. 641, plate IX, fig. 2). The skull was unearthed by some workmen in the vicinity of Richmond and put into the hands of Professor D. W. Dennis, who loaned it to the writer. It is referred to Ovibos moschatus, the species now existing in the Arctic region of North America. Possibly if we had more complete remains specific differences might be found.

This animal probably lived in the region about Richmond at a time when the Wisconsin moraine was yet lingering in Indiana and when the climate was yet severe.

3. Randolph County.—In the collection belonging to Earlham College is the rear portion of the skull of a musk-ox, identified as belonging to Symbos cavifrons. At what place in Randolph County it was found is not known. It had been somewhat eroded and injured. Measurements approximately correct were given by the writer in 1912 (Geol. Surv. Indiana, vol. XXXVI, p. 638). We may suppose that the animal lived in that region at some time during the last half of the Wisconsin stage.

4. Beaver Lake, Newton County.—In 1870, F. H. Bradley (Geol. Surv. Illinois, vol. IV, p. 229), reported that upon the bottom of Beaver Lake, just east of the State line, since the lake had been partially drained, skeletons of Mastodon and Boötherium had been found by Dr. H. M. Keyzer, of Momence, Illinois, and others. Unfortunately, we do not know what became of these valuable materials. Probably the “Boötherium” was the animal now known as Symbos cavifrons, inasmuch as it is far more abundant than any other species of musk-ox. If any parts of the skeleton of this musk-ox were really found the loss is great, inasmuch as very few bones have ever been discovered.

The time when the mastodon and the musk-ox lived about Beaver Lake must have been after the withdrawal of the Wisconsin glacial sheet beyond that region. For remarks on this locality see page 96. The name Beaver Lake has disappeared from the maps, but it was in township 30 north, range 9 west.

5. Hebron, Porter County.—In the American Museum of Natural History is a nearly complete skull of the musk-ox known as Symbos cavifrons, collected about 6 miles east of Hebron. It was found by workmen while making excavations for a railroad bridge. The exact location is given as section 16, township 33 north, range 6 west, in the marshy lands just north of Kankakee River. The depth was about 7 feet and the deposit was described as a mixture of sand and clay. Doubtless the animal died near the spot where its skull was found, inasmuch as this had undergone little injury.

This skull was described and figured by the writer in 1912 (Geol. Surv. Indiana, vol. XXXVI, pp. 635–638, figs. 49, 50) and in 1914 (Iowa Geol. Surv., vol. XXIII, pp. 299–302, figs. 98, 99); also by Dr. J. A. Allen (Mem. Amer. Mus. Nat. Hist., vol. I, p. 214, plates XVII, XVIII).

On Leverett’s glacial map of Indiana this region is represented as being occupied by sand and gravel deposits resulting from glacial drainage. The musk-ox must have lived after the foot of the glacier had withdrawn nearly to the end of Lake Michigan.

ILLINOIS.

(Map 25.)

1. Bondville, Champaign County.—In the collection of the University of Illinois, at Champaign, is the rear portion of the skull with the horn-cores of a specimen of Symbos cavifrons. It is reported as found on the farm of John Busey, southwest of Champaign and 4 miles from Bondville. Professor S. A. Forbes informed the writer that the locality is in section 31, township 19 north, range 8 east. No details are known regarding the conditions under which the skull was found. The region is occupied by the Champaign moraine and it was after the retirement of the ice from this moraine that the animal lived. It may, however, have been not long after that time.

2. Manito, Mason County.—Mr. John Wiedmer, of St. Louis, presented to the U. S. National Museum (No. 7800) the rear half of the skull of a specimen of Symbos cavifrons found near Manito, at a depth of 5 feet, by workmen who were cutting out peat. A tooth of a mastodon, Mammut americanum, sent with the skull, is said to have been embedded in the upper part of the sand which underlies the peat. The skull was reported as found at about the same depth, but it was quite certainly not in the sand.

The exact location of the skull was in section 22, township 23 north, range 6 east, within the area of the Illinoian drift-sheet, but the Wisconsin drift is not far away. The valley of the Illinois River in this county is mapped by Leverett as occupied by sands and gravels of Wisconsin age. Probably the animal lived when the Wisconsin ice-sheet was not far distant.

The skull described apparently belonged to a rather small, perhaps not fully grown individual. For purposes of comparison with other skulls, as the one found at St. Louis, Missouri, and the one found at Hebron, Indiana (p. 252), the following measurements have been taken of this skull:

mm. From tip to tip of horn-cores 437 Height of rear of skull from bottom of condyles 168 Width across the mastoid region 183 Width between hinder ends of temporal fossæ 117 Width at space between bases of horn-cores and orbits 127 Width at the rear border of orbits 231 Length of rough surface of forehead, at midline 200 Fore-and-aft width of base of horn-core 98 Vertical thickness of base of horn-core 78 From front of foramen magnum to rear of nasal bones 260

The exostosis between the bases of the horn-cores is longitudinally deeply excavated, the excavation being 50 mm. wide and 27 mm. deep. The tips of the horn-cores come forward only even with the rear border of the orbits. In some other cases the horn-cores come forward to the front, or even in advance of the front border of the orbits. It is possible that this Manito skull was that of a cow.

3. Alton, Madison County.—In a collection of fossil mammals made at Alton by William McAdams and now in the U. S. National Museum is a single tooth, a lower left second molar, referred with some doubt to Symbos promptus. The crown is 34 mm. long and 25 mm. wide at the base. The tooth has been described briefly by the writer (Proc. U. S. Nat. Mus., vol. LVIII, p. 115). A list of the species accompanying it will be found on page 339.

WEST VIRGINIA.

(Map 25.)

1. Mahan, Brooke County.—In 1902 (Science, n. s., vol. XVI, pp. 707–709, fig.), J. B. Hatcher reported the finding of a part of a skull of Symbos cavifrons at a point in Brooke County, somewhat over a mile below Steubenville, Ohio. The locality is further defined as being the sand-pit of the Steubenville Sand Company, on the Thomas Mahan farm, on the east side of the Wheeling branch of the “Panhandle” Railroad. The details regarding the locality were furnished by Mr. Sam Huston. The sand-pit was located in the glacial terrace which rises about 70 feet above low-water mark and from about 35 to 40 feet above high-water. The river has never been known to rise as high as to the spot where the skull was found. It had doubtless been brought down by the waters which built up the terrace. These waters probably came from the Wisconsin ice-sheet. The skull is now in the Carnegie Museum at Pittsburgh.

The interesting geology of this region is described on page 355.

MISSISSIPPI.

(Map 25.)

1. Natchez.—The first notice of the occurrence of any species of the Ovibovinæ at Natchez seems to be the inclusion of Symbos (Boötherium) cavifrons in Leidy’s list of fossil Mammalia found in the State of Mississippi (Wailles’s Rep. Agric. Geol. Mississippi, 1854, p. 269), but the locality is not mentioned. The occurrence of the species in the State was not mentioned by Leidy in 1853 in his “Memoir on Extinct Species of Fossil Ox” (Smithson. Contrib. Knowl., vol. V, art. 3). Leidy’s list mentioned above was quoted by Hilgard in 1860 (Agric. Geol. Mississippi, p. 196). In neither place was any statement made regarding the part preserved. In his “Memoir on the Extinct Sloth Tribe of North America,” published in 1855 (Smithson. Contrib. Knowl., vol. VII, art. 5, p. 6), Leidy stated that Boötherium had been found at Natchez. Five years later (Proc. Acad. Nat. Sci. Phila., 1870, p. 73) Leidy reported that an isolated tooth, a last lower molar not yet protruded from the jaw, had been received from Natchez and was preserved in the museum of the Philadelphia Academy. On comparison with a last molar in a jaw of a supposed Ovibos cavifrons received at the Smithsonian Institution and found near Woodbine, Iowa, Leidy concluded that the Natchez tooth belonged to the same species. Probably he had already based on this tooth the announcement of the presence of this species at Natchez. At least, the writer knows of no other parts of Symbos cavifrons found at Natchez, and he has seen neither the tooth from Natchez nor the jaw from Woodbine, Iowa.

Leidy stated that the tooth in question had a height of 2.25 inches, a length antero-posteriorly of 2 inches.

KENTUCKY.

(Map 25.)

1. Bigbone Lick, Boone County.—In his account of Bigbone Lick and the collections made there (Monthly Amer. Jour. Geol., vol. I, pp. 158–174, 205–217), William Cooper included in his list of species both Bos bombifrons (Boötherium bombifrons) and Bos pallasii (Symbos cavifrons). Already in 1818 Wistar (Trans. Amer. Philos. Soc., ser. 2, vol. I, p. 379, plate XI, figs. 10, 11) had described, without systematic name, the skull which later was made the type of Bos bombifrons by Harlan (Fauna Amer., p. 271). This skull was a part of the collection made at Bigbone Lick by Governor William Clark for President Thomas Jefferson. In the account presented by Cooper (p. 173) he stated that in the Finnell (sometimes spelled Phinnell) collection, made in 1830, he had found a second head of the species, but what became of it is not known. Harlan, as cited (p. 272), stated that in the collection of fossils made at Bigbone Lick by Major Long were teeth which probably belonged to the musk-ox. They differed little from those of the bison, but were thicker at the crown, more deeply grooved at the sides, and altogether more robust. In 1870 (Proc. Acad. Nat. Sci. Phila., p. 97), Dr. Leidy mentioned that in the Museum of Comparative Zoology, in Cambridge, he had seen a skull of Symbos cavifrons which Professor Shaler had collected at Bigbone Lick. The present writer has seen this skull. A list of the species found at this locality is recorded on page 403.

2. Bluelick Springs?, Nicholas County.—In the collection at Yale University is the hinder part of a skull of Symbos cavifrons, bought in 1876 from Henry Ward, Rochester, and labeled as found in the Bluelick region. The locality is not more definitely known.

3. Winchester, Clark County.—In the U. S. National Museum is a part of the rear of the skull of Symbos cavifrons labeled as found at Winchester. It is credited to J. W. Fitch. It shows well the condyles, some of the base of the skull, and the base of the right horn-core.

Besides the remains above described a part of a cranium of Symbos cavifrons from Kentucky is preserved in the Boston Society of Natural History. Leidy (Smithson. Contrib. Knowl., vol. V, art. 3, p. 16) stated that it had been found in the alluvium of Kentucky River.

FINDS OF EXTINCT BISONS IN THE PLEISTOCENE OF EASTERN NORTH AMERICA.

ONTARIO.

(Map 26.)

1. Toronto, York County.—Through the kindness of Professor B. A. Bensley, of the University of Toronto, the writer has had the opportunity to examine a malar bone of a bison found in the Don interglacial beds at Toronto. It is slightly water-worn and the edges are somewhat injured. The bone has been compared with the corresponding one of a large specimen of Bison bison, No. 22374 of the U. S. National Museum, and with a complete skull of Bison alleni from Alaska. The Toronto bone is about one-third larger than that of the Bison bison and about one-tenth larger than that of B. alleni. The projecting outer plate, immediately below the orbit, narrows little if any from behind forward, while in both the other species referred to it becomes much narrower toward the front. The bone quite certainly belonged to an extinct species, but without the horn-cores it is impossible to determine to which one.

In 1901 (Jour. Geol., vol. IX, p. 301), Coleman stated that a large atlas vertebra of a bison which he thought might belong to B. americanus had been found in interglacial beds in Toronto. It is more probable, however, that it belonged to one of the extinct species. It is uncertain whether the deposits belonged to the Don series or the Scarboro.

The geology of this region is treated on pages 281 to 283.

PENNSYLVANIA.

(Map 26.)

1. Pittston, Luzerne County.—In 1873 (Contrib. Ext. Fauna West. Terrs., p. 255, plate XXVIII, fig. 8), Leidy described and figured a tooth as that of Bison latifrons. This has been referred here to an undetermined species of Symbos. In a paper on the distribution of the American bison in Pennsylvania, Mr. S. N. Rhoads (Proc. Acad. Nat. Sci. Phila., 1895, p. 245) concluded that this tooth belonged to the existing bison. He stated also that the Academy had two other teeth, lower molars, from the same place, which Leidy had labeled as “Bison americanus” and regarded as more recent than the figured tooth. Rhoads thought the identification correct, but that they belonged to the same individual as did the tooth figured by Leidy. The writer has not seen these lower teeth and admits them here only provisionally. They were found along Susquehanna River, in association with remains of Mammut americanum and Equus complicatus? (“E. major”). If any of the bovine teeth belong to Bison the species belonged to early or middle Pleistocene and is now extinct.

2. Port Kennedy, Montgomery County.—The presence of Bison in the famous cave at this place was announced by Wheatley in 1871 (Amer. Jour. Sci., ser. 3, vol. I, p. 384). Cope, in his account of 1899 (Jour. Acad. Nat. Sci. Phila., vol. XI), does not mention the genus; but Mercer, on page 280 of the same volume, credits Wheatley with having found remains of three individuals of one undetermined species. He used the generic name Bos.

A description of the Port Kennedy Cave and its contents and remarks on the geological age of the fossils will be given on pages 311 to 320.

OHIO.

(Map 26.)

1. Fincastle, Brown County.—In 1887 (Jour. Cin. Soc. Nat. Hist., vol. X, p. 20), Horace P. Smith, curator of the society, described a fine pair of horn-cores of Bison latifrons found in Brown County and which had come into the possession of the society. They were discovered at a depth of 18 feet, in making excavations for the piers of a bridge across Brush Creek. Inasmuch as nearly the whole of the course of this stream is in Adams County, the locality must have been in the northeastern corner of Brown County, near Fincastle, where the creek has its source, and within the area of the Illinoian drift. Smith thought that the horn-cores were in the drift; but, if so, the overlying materials must have been washed down over them after their burial. It is improbable that they were ever beneath or in the glacier. The animal probably lived during the Sangamon interglacial stage; quite certainly before the Wisconsin.

2. North Fairfield, Huron County.—In the Norwalk Museum, at Norwalk, are some skull-bones of a bison found at some point not known to the writer, about 7 miles from North Fairfield, while search was being made for bones of the megalonyx which belongs partly to the museum at Norwalk, partly to the Niver family at North Fairfield. These bison bones served as the type of Bison sylvestris, described by the writer in 1915 (Proc. U. S. Nat. Museum, vol. XLVIII, p. 515, plate XXX). This is the only species of extinct bison known that lived after the close of the Wisconsin stage.

INDIANA.

(Map 26.)

1. Evansville, Vanderburg County.—Many years ago Dr. Leidy (Proc. Acad. Nat. Sci. Phila., 1854, pp. 199–200) described a collection of mammalian remains made on the banks of Ohio River at the mouth of Pigeon Creek, a short distance below Evansville. Among these materials was a fragment of a cervical vertebra of a species of Bison, which Leidy identified with doubt as Bison americanus, the existing bison, now known as Bison bison. It would be impossible to determine to which of our several species of the genus Bison this bone belonged; but it probably did not belong to B. bison. This species is not known from times preceding the Wisconsin drift and the bone-bed at Pigeon Creek is undoubtedly older. On page 32 is a discussion of the probable age of the bone-bed. It may be as old as the Aftonian stage, but more probably it belonged to the Sangamon.

The other species found at the locality named are Megalonyx jeffersonii, the Virginia deer, the extinct horse known as Equus complicatus, Tapirus haysii, and the extinct wolf Ænocyon dirus. At Bigbone Lick, midway between Louisville and Cincinnati, on the Kentucky side, have been found two extinct species of Bison, B. antiquus and B. latifrons. At the same place has been found Equus complicatus. The beds there overlie the Illinoian drift and belong, in part at least, to the Sangamon.

Under this number may be included mention of a bone of a species of Bison which Cope reported in 1878 (Amer. Naturalist, vol. XII, p. 189) from Vanderburg County. Cope stated that John Collett, then State geologist of Indiana, had discovered in a late Pleistocene deposit a number of fossils. One of these was the ulno-radius of a Bos (now to be referred to Bison); another was a part of the mandible of the deer Odocoileus dolichopsis. In 1884 (Geol. Surv. Indiana, vol XIV, p. 22), Cope and Workman, inaccurately quoting Cope’s original description of the deer Odocoileus dolichopsis, state that this deer and the bison bones were found in Harrison County.

By consulting the Patoka Folio, No. 105, of the U. S. Geological Survey, it will be seen that the northern part of Vanderburg County, four townships, Nos. 4 and 5 south, ranges 10 and 11 west, are included. The two northern townships are largely occupied by lacustrine deposits which the geologists Fuller and Clapp regarded as having been laid down in lakes produced by the damming of the drainage by the Illinoian ice-sheet. Farther south, along the streams emptying into Pigeon Creek, are wide areas which are covered by “fine silts, mainly of pre-Wisconsin age, but including some of more recent age.” Whether or not the bison bone and the jaw of Odocoileus dolichopsis were found in any of these deposits we are unfortunately left in the dark. It is most probable that the bison and the deer lived there after the Illinoian stage and before the Wisconsin.

2. Vincennes, Knox County.—In the geological collection of Earlham College, Richmond, Indiana, is preserved the greater part of the skull of a bison which belonged to the species known as Bison antiquus. This skull was first described and figured by Mr. W. G. Middleton and Professor Joseph Moore (Proc. Ind. Acad. Sci. for 1899, pp. 178–181, with a plate); afterwards by the writer (Geol. Surv. Indiana, vol. XXXVI, p. 651, figs. 50, 51).

This fine skull is said to have been found in 1896 by a Mr. Brower, a few miles from Vincennes, in a ditch, at a depth of 6 feet. Beyond this the writer has not been able to learn. It would be of value to know exactly where this place was, for then some conclusion might be reached as to the geological age of the animal. The greater part of the county is occupied by drift of Illinoian age, which appears in some places to have on it some loess, and doubtless its surface has been much modified since the materials were laid down. Even in this area there may be some deposits of later times, interglacial and glacial.

According to Leverett’s glacial map of the region, there are along Wabash River sand and gravel terraces of Wisconsin age; while along White River there are said to be alluvial terraces older than Wisconsin.

At present one can arrive at a conclusion only from general knowledge. The writer knows of no extinct bison (except one rather peculiar species) which lived after the Wisconsin glacial stage. It appears most probable that the skull at Earlham College came from some interglacial deposits laid down about the middle of the Pleistocene, most likely during the Sangamon stage.

The writer has been informed that another skull of a buffalo was for years on exhibition in a business house conducted by Mr. T. L. Cheney, but it seems to have disappeared. Mr. J. Gimble, of Vincennes, informs the writer that it was found in the bed of Wabash River, near St. Francisville, Illinois, about 10 miles below Vincennes.

ILLINOIS.

(Map 26.)

1. Alton, Madison County.—In the U. S. National Museum are four teeth of an undetermined species of Bison found somewhere in the vicinity of Alton. They are part of a collection made many years ago by Mr. William McAdams, and afterwards passed into the hands of Professor O. C. Marsh, then vertebrate palæontologist of the U. S. Geological Survey. It now belongs to the U. S. National Museum. Nearly all of these fossils were originally inclosed, wholly or partially, in nodules of fine sand, cemented together with carbonate of calcium. Where the teeth are exposed to view they are shown in a beautifully white condition; but the remaining matrix is so hard and adheres so strongly that it is practically impossible to remove it without greatly damaging the teeth. A list of the species found at Alton will be given on page 339; also a discussion of their geologic age.

The bison teeth consist of four upper molars and the hinder half or more of the left hindermost molar. They were described by the writer (Proc. U. S. Nat. Mus., vol. LVIII, p. 115). They are somewhat larger than any belonging to the existing buffalo measured. They are larger, too, than those of the commonest extinct species, B. occidentalis. It is impossible to say at present to which extinct species they belonged. One naturally thinks of Bison latifrons, the bearer of the immense horns, but teeth have not yet been found associated with the horn-cores of that species.

WISCONSIN.

(Map 26.)

1. Coon Valley, Vernon County.—In the U. S. National Museum is a well-fossilized tooth of a species of bison which was sent, in 1899, by Rev. P. Moe, of Coon Valley. This tooth has been regarded as belonging to Bison bison, but its fossilization seems to indicate that it antedates the time of this species. It was found in section 26, township 14 north, range 6 west. This would be between the towns of Coon Valley and Chaseburg. This locality lies within the “driftless area,” and it would probably be difficult for the geologist, even on the ground, to determine the age of the deposit, especially as no details were furnished regarding the depth at which the tooth was found or the nature of the inclosing materials.

MARYLAND.

(Map 26.)

1. Chesapeake Beach, Calvert County.—Mr. William Palmer, of the U. S. National Museum, collected at this place, in 1912, a fragment of a lower last molar which apparently belonged to some species of Bison. A few other remains have later been secured.

VIRGINIA.

(Map 26.)

1. Saltville, Smyth County.—In the U. S. National Museum is an upper second molar of a species of Bison, found at Saltville. It was sent in 1904 by Mr. H. D. Mount, of Saltville, with remains of Elephas primigenius and Mammut americanum. It is understood that all were found in excavating for the water reservoir of the town. The bison tooth is little worn, the height being still 46 mm. At the summit the crown is 34 mm. long, at the base 23 mm. long and 29 mm. wide. It resembles closely that of Bison bison, but is slightly larger than the same tooth in a large specimen of the existing species. The base of the skull is present, with the occipital condyles. The latter are slightly larger than in the specimen of B. bison just mentioned. The species can not be determined, but it probably was not B. bison. A list of the associated species found at this locality is presented on page 352.

2. Ivanhoe, Wythe County.—In 1869 (Proc. Amer. Philos. Soc., vol. XI, p. 176), Professor Cope stated that he had found molar teeth of a bison which he identified with doubt as Bison antiquus. The animal may quite as well have belonged to any one of four or five other extinct species.

SOUTH CAROLINA.

(Map 26.)

1. Charleston, Charleston County.—In 1860, Leidy (Holmes’s Post-Pl. Foss. South Carolina, p. 110, plate XVII, figs. 15, 16) described briefly and figured a tooth of a bovine animal found in the Pleistocene of Ashley River. This he suspected belonged to Bison latifrons, but he added that it presented nothing to distinguish it from that of the existing bison. Numerous teeth resembling those of the domestic ox and the bison have been found on Ashley River and have been regarded as those of the domestic animal. (See letter of Agassiz to Professor F. S. Holmes in the Introduction to Holmes’s work cited above.) While the teeth of our cattle may have been picked up along the shores of Ashley River, it is highly probable that the great majority of similar teeth belonged to some extinct species of Bison. Probably only the discovery of horn-cores will lead to the determination of the species. Leidy probably used the name Bison latifrons in a very wide sense. In the collection at Amherst College the writer has seen an upper molar of a bison, apparently the second molar, which is 38 mm. long on the outer face. This length is too great for B. bison and the tooth probably belongs to B. latifrons. It was probably found in the region about Charleston.

In the Charleston Museum the writer has seen an anterior cannon-bone of Bison which had quite certainly been found somewhere about Charleston. The following measurements were secured, and corresponding measurements of B. bison are added for comparison:

Measurements of anterior cannon-bones of bisons, in millimeters.

┌─────────────────────────────────────────┬─────────────┬─────────────┐ │ │Fossil bison.│ B. bison. │ ├─────────────────────────────────────────┼─────────────┼─────────────┤ │Length along the outer border │ 242│ 206│ │Width of upper articular surface │ 90│ │ │Side-to-side diameter at middle of length│ 64│ 52│ │Fore-and-aft diameter at middle of length│ 39│ 33│ │Width of lower articular surface │ 96│ 91│ └─────────────────────────────────────────┴─────────────┴─────────────┘

Other measurements may be found in J. A. Allen’s work, “The American Bisons,” page 45. Apparently the bison which possessed the bone described above had a height about one-eighth greater than the large individual of the existing bison compared with it. Fossil remains found elsewhere show that at least one large species of Bison formerly inhabited this country. B. latifrons was a species with very large horns, and its body may also have been larger than that of the existing bison. To this species may have belonged the large cannon-bone described above.

GEORGIA.

(Map 26.)

1. Brunswick, Glynn County.—Remains of an undetermined species of Bison were found at the time of excavating the Brunswick Canal, south of Darien, in 1838–39. In a communication to the Academy of Natural Sciences (Proc. Acad. Nat. Sci. Phila., vol. I, pp. 216–217), Mr. J. Hamilton Couper gave an account of the geology of the locality and mentioned the fact that remains of Megatherium, Elephas primigenius, Mastodon giganteus, Hippopotamus, horse, Bos, and Sus americana had been secured. As was later determined by Owen (Proc. Acad. Nat. Sci. Phila., 1848, p. 93), the supposed hippopotamus incisor was a lower tusk of a mastodon. Sus americana was referred by Owen to his genus Harlanus; but was afterwards found to belong to Bison. Owen (Jour. Acad. Nat. Sci. Phila., ser. 2, vol. I, p. 20, plate VI) described and furnished an excellent figure of the jaw. The jaw is now in the collection of the Academy of Sciences at Philadelphia. Measurements show that it is larger than the jaw of Bison bison, corresponding well with the other bones of Bison found at the same place. Leidy regarded it as belonging to B. latifrons; but he used this name in a very wide sense. In the Academy of Natural Sciences at Philadelphia is a part of the right ramus of the lower jaw labeled “Bison latifrons, Darien canal, Ga.” The teeth are badly worn. The jaw itself is larger than that of Bison bison. The following measurements were taken:

Measurements of bison jaws, in millimeters.

┌────────────────────────────────────────┬─────────────┬─────────────┐ │ │B. latifrons.│ B. bison. │ ├────────────────────────────────────────┼─────────────┼─────────────┤ │Height of jaw just behind third molar │91 │83 │ │Thickness of jaw just behind third molar│36 │32.5 │ │Height of jaw in front of third molar │63 │52 │ │Thickness of jaw in front of third molar│31 │29 │ └────────────────────────────────────────┴─────────────┴─────────────┘

The jaw has the appearance of being much more massive than that of B. bison.

In his work on the “Extinct Species of American Ox” (Smiths. Contrib. Knowl., vol. V, p. 11), Leidy stated that Couper had presented to the Academy in Philadelphia a tibia and a part of a humerus of Bison, which bones he reported were larger than those of the existing American bison, and he referred them to the species Bison latifrons. The tibia was 456 mm. long and 87 mm. wide at the lower end; in a large Bison bison in the U. S. National Museum the tibia is 412 mm. long and 78 mm. wide below.

Couper presented to the Boston Society of Natural History an atlas and a metatarsus from the same locality. The atlas had a width of 247 mm.; that of the existing bison just referred to is 220 mm. wide. The metatarsal is said to have been 272 mm. long; that of the living bison mentioned is 255 mm. A front cannon-bone at Harvard is 256 mm. long. In a collection determined by J. W. Gidley (Bull. No. 26, Geol. Surv. Georgia, p. 436) some bison remains, probably a tooth or teeth, were referred with doubt to Bison bison. It is far more probable that they belonged to an extinct species, and that B. latifrons.

2. Skidaway Island, near Savannah, Chatham County.—On page 29 of Joseph Habersham’s Memorandum, forming a part of William B. Hodgson’s “Memoir on the Megatherium,” published in 1846, a portion of the humerus of a Bos is listed among the fossils found at Skidaway Island. This bone is to be assigned to an undetermined species of Bison. The width across the condyles is given as 4.5 inches, which is not greater than in B. bison; but it is not probable that it was this species. Lyell (Second Visit, etc., ed. 3, vol. I, p. 348) includes “a species of the ox-tribe” among the fossils found at this locality.

For further remarks on the species of vertebrates found at Brunswick, the reader may consult page 371, where also the geology of the locality is discussed.

FLORIDA.

(Map 26.)

1. Wade, Alachua County.—In the collection of the Florida Geological Survey is an upper left last molar of Bison, found in the Buttgenbach river mine, in Santa Fe River, 6 miles north from Wade. Although this tooth was found in a phosphate mine, it certainly belongs to Pleistocene time. The tooth is but little worn and is well fossilized. Its height is 45 mm., the length on the outer face 30 mm., the length at the middle of the width 27 mm., the width at the base of the first lobe 24 mm.

There is another tooth in the collection, apparently the second upper molar of the left side, from the same place and fossilized in the same way. For a list of the species found at this locality and the writer’s view regarding their geological age, the reader is referred to page 376.

2. Pablo Beach, Duval County.—In the collection just mentioned there are, from near Pablo Beach, three bones which apparently belonged to some extinct species of Bison. No. 4444 is the left fibular bone; No. 4443 the left third cuneiform of the hinder foot; and No. 4442, a first phalange of a hinder foot. These were found along the Inland Waterway Canal, about 20 miles north of St. Augustine. The locality appears to be about 5 miles south of Pablo Beach. At the same place have been found Mammut americanum, Elephas columbi, and remains of a species of Odocoileus.

3. Ocala, Marion County.—Sellards (op. cit., p. 103) reported remains of an undetermined species of Bison found in a fissure in limestone rock near Ocala.

4. Dunnellon?, Marion County.—Sellards (op. cit., p. 104) presented a list of Pleistocene vertebrates, found in or along Withlacoochee River, but the exact localities are not given. Among these is an undetermined species of Bison. Lucas (Proc. U. S. Nat. Mus., vol. XXI, 1898, p. 767) stated that there is in the U. S. National Museum an imperfect skull of Bison latifrons, obtained from Withlacoochee River. The writer has not seen this skull. On page 376 the other species found here are listed and their geological age discussed.

5. Tampa, Manatee County.—In the Jarman collection, now in Vanderbilt University, and made in the region about Tampa, is a right lower third molar of Bison. It is well fossilized, but structurally does not appear to differ from a tooth of the existing American bison. It belonged, however, quite certainly to an extinct species. In the American Museum of Natural History, New York, is a well-worn lower left last molar of a bison, dredged up in Alafia River. With it were a mastodon tooth, teeth of two or three extinct horses, and various extinct tortoises. The reader is referred to page 379.

6. Palmetto, Manatee County.—Mr. Ernest Leitzel, of Palmetto, sent from that place to the U. S. National Museum some teeth for determination. Teeth of the horses are described on page 379. With these was a part of a lower right molar, possibly the last molar, of Bison.

From Palma Sola, on the south side of Manatee River and about 10 miles below Palmetto, there has been sent to the U. S. National Museum, by Mr. Charles T. Earle, the distal end of a metacarpal bone. This has a width of 93 mm. It may have belonged to Bison latifrons. With it came teeth of Equus complicatus, E. littoralis, and E. leidyi, a part of an antler of a deer (Odocoileus), a part of a beak of a platanistid porpoise, and a tooth of Elephas columbi. Probably the porpoise and teeth of sharks came from Miocene deposits somewhere in the neighborhood.

7. Grove City, Charlotte County.—Leidy, in 1889 (Trans. Wagner Free Inst., vol. II, p. 12), stated that Mr. Joseph Willcox had found, on Rocky Creek, 30 miles north of Sarasota Bay, some remains of the great extinct Bison latifrons. Sellards (8th Rep., pp. 103, 112) learned that the locality was really Stump Pass, near Grove City. The horn-core was lost by accident, but Leidy speaks of it as being huge. With it was the proximal part of a radius whose upper end measured transversely 1.4 times that of an existing bison.

In a letter to the author, Mr. Willcox writes that, as nearly as he can recollect, the diameter of the horn-core was about 5 or 6 inches.

8. Vero, St. Lucie County.—Sellards (8th Rep., Florida Geol. Surv., p. 150) stated that an extinct bison is represented in the collection of the Florida Geological Survey by a number of teeth, the distal end of a humerus, and some foot-bones. They were supposed to have been derived from stratum No. 2.

When in Vero in 1916, the writer secured a much-worn upper left premolar 3 of Bison from the base of the muck layer No. 3. It is in some respects different from the corresponding tooth of the existing bison. For lists of the species found at Vero and for a discussion of the geological age the reader may consult pages 381 to 383.

9. Arcadia, De Soto County.—In the U. S. National Museum are some teeth of Bison, obtained at or near Arcadia, on Peace Creek. In general, these resemble closely the corresponding teeth of B. bison. Leidy (Trans. Wagner Free Inst., vol. II, p. 22) mentioned a tooth and a first phalanx of Bison from Peace Creek. These are probably in the collection of the Wagner Free Institute.

In the U. S. National Museum (No. 1989) is a hinder cannon-bone from Arcadia. It resembles the corresponding bone in B. bison, but doubtless belonged to a species now extinct. Lucas (Proc. U. S. Nat. Mus., vol. XXI, p. 767) referred the teeth and the metacarpal to B. latifrons.

In the same museum is a calcaneum labeled as collected on Peace Creek by J. F. Le Barron. The reader may consult page 381 for further information.

10. Labelle, Lee County.—Remains of Bison apparently have been found at Labelle, or near there. Leidy, in Dall’s report (Bull. No. 84, U. S. Geol. Surv., p. 129) referred this to B. latifrons. The bison, Elephas columbi, Equus fraternus, and a mylodon were supposed to have been buried in Pliocene deposits, but this opinion appears to be erroneous. Sellards (8th Rep., p. 102) has shown that the elephant and probably the horse were in Pleistocene marls. As shown on page 384, the elephant is Elephas imperator.

11. Palm Beach, Palm Beach County.—In his eighth report, Sellards (p. 105) stated that a femur of an undetermined species of Bison was found near this place, in the Palm Beach Drainage Canal. In the collection of the Museum of Comparative Zoology, at Harvard University, are a front cannon-bone, lacking the epiphyses, and the proximal end of a humerus. The size of these indicates that they belong to B. latifrons. The glenoid cavity measures 80 mm. by 60 mm. The neck of the humerus is 100 mm. wide.

ALABAMA.

(Map 26.)

1. Newbern, Hale County.—In August 1914, there was received at the U. S. National Museum, from Mr. J. W. White, of Newbern, a lower right last molar of a species of bison reported found in a creek, and an incisor tooth of a horse, which appear to be fossilized. The bison tooth had just begun to wear. The fore-and-aft length of the crown is 37 mm. The locality is somewhat outside of the range of Bison bison as given by Allen on his map (“American Bisons, Living and Extinct”). The fossil may well belong to some extinct species and have lived in that region in middle Pleistocene times.

MISSISSIPPI.

(Map 26.)

1. Natchez, Adams County.—In Dr. M. W. Dickeson’s account of a collection of bones and teeth made near Natchez (Proc. Acad. Nat. Sci. Phila., 1846, p. 106) he included remains of the genus Bos. To-day these would be referred to the genus Bison.

In 1854 (Smithson. Contrib. Knowl., vol. V, art. III, p. 9, plate II, figs. 2–7), Leidy described and figured bovine teeth from Natchez, which he referred to Bison latifrons. Two of these teeth had been found, as Leidy stated, by M. W. Dickeson, in association with remains of Mastodon (Mammut), Equus, Ursus, Cervus (Odocoileus), Megalonyx, and Mylodon. Three others had been presented by W. H. Huntington, who discovered them in association with remains of Mammut americanum, Equus complicatus, and Felix atrox. Three of the teeth were upper molars, the others, lower molars. Leidy gave the measurements of most of these. The following measurements are those of an upper second and an upper third molar:

_Measurements of bovine teeth, in millimeters._

┌────────────┬───────┬───────┬───────┐ │ Tooth. │Height.│Length.│Width. │ ├────────────┼───────┼───────┼───────┤ │Second molar│ 67│ 37.5│ 27│ │Third molar │ 75│ 42.5│ 29│ └────────────┴───────┴───────┴───────┘

These teeth are considerably larger than those of Bison bison and B. occidentalis (Geol. Surv. Iowa, vol. XXIII, p. 320).

KENTUCKY.

(Map 26.)

1. Woolper Creek?, Boone County.—The type of Bison latifrons is usually regarded as having been found at Bigbone Lick, but Leidy (Jour. Acad. Nat. Sci. Phila., vol. VII, p. 372) stated it had been found a dozen miles or more north of Bigbone Lick, in the bed of a creek that enters into the Ohio River. It seems probable that this creek is the one named above.

2. Bigbone Lick, Boone County.—It was at this place that was found the horn-core and attached part of skull which forms the type of Bison antiquus. It was a part of the Jefferson collection and was described by Leidy (Proc. Acad. Nat. Sci., Phila., vol. VI, 1852, p. 117). Richard Lydekker (Cat. Foss. Mamm. Brit. Mus., pt. 2, p. 27) wrote that there is in that museum a fragment of a right mandible, probably belonging to Bison latifrons. However, the identification is hardly to be relied on. Shaler (Geol. Surv. Kentucky, n. s., vol. III, p. 197) reported the finding of bones of Bison latifrons, but it is doubtful in what sense he used this name; and he did not indicate how these bones differed from those of other bisons. He probably had in mind B. antiquus. Hence the presence of the species with the widely spread horns at Bigbone Lick is doubtful.

A list of the species of mammals collected at this place will be found on page 403.

FINDS OF BISON BISON IN THE PLEISTOCENE OF EASTERN NORTH AMERICA.

ONTARIO.

(Map 27.)

1. North Bay, Nipissing County.—In the U. S. National Museum is a horn-sheath, found at this place. It was sent by Dr. Charles E. Cook, of Lockport, New York, who himself saw it thrown out of a ditch, about 5 feet deep, which was being made from the shore of the lake. The horn was found at a distance of 600 feet from the lake and in front of the Hotel Queen’s. It certainly belongs to the existing species, Bison bison. Whether the presence of the horn at that spot is due to the former existence of the American buffalo there or to its introduction by man it is impossible to say at present.

MASSACHUSETTS.

(Map 27.)

1. Orleans, Cape Cod.—In 1920 (Jour. Mamm., vol. I, pp. 161–164, figs. 1–3), Dr. G. M. Allen presented an account of the discovery of a maxilla containing the penultimate and the hindermost milk teeth of a calf of Bison bison, at Orleans, Cape Cod. This specimen had been collected about 20 years previously by Dr. A. W. Grabau and presented by him to the Boston Society of Natural History. The bone and teeth were found “wholly embedded in till about halfway up on a section of a glacial moraine, situated on Town Cove and about 70 or 80 feet high.” With the specimen were associated many fragments of the shells of the mollusk Venus. Dr. Allen suggested that this bison calf had either come to its end while wandering on the moraine or had more likely lived and died during the preceding Peoria interglacial stage. It might be questioned whether bones which had been buried and thereby become softened would have endured the rough treatment of a glacial mill.

NEW YORK.

(Map 27.)

1. Albany, Albany County.—Dr. John M. Clarke, State geologist of New York, sent the writer some teeth of a species of Bison, probably B. bison, for which he gives the assurance that they were found somewhere in the vicinity of Albany, and in the “Albany clays.” These clays are supposed to belong to the Champlain stage. While this is somewhat further east than the bison has extended within historical times, it is entirely reasonable to suppose that at some time in the not distant past its range went to the Hudson. Indeed, Dr. G. M. Allen has recently shown (Jour. Mamm., vol. I, pp. 161–164) that at some time during the late Pleistocene a bison lived in the region of Cape Cod. The specimens sent by Dr. Clarke must have occupied eastern New York late in the Wisconsin stage.

2. Syracuse, Onondaga County.—In 1890 (Amer. Naturalist, vol. XXIV, p. 953), Professor Lucien Underwood reported the discovery of a skull of a bison in Syracuse, while a sewer was being excavated. Underwood stated that it was found at a depth of 10 feet, in a black muck. Professor E. D. Cope identified the skull as that of Bison bison. The present writer, in 1914, examined the skull at Syracuse University. He also talked with Mr. John Cunningham, who bought the skull from the finder, a laborer, paying him one dollar. Mr. Cunningham stated that he went to the spot and measured the depth from the surface, and found it to be 17 feet. Above the muck that inclosed the skull was what he regarded as clay. Dr. Burnett Smith has examined the deposits in a cellar dug within a few rods of the spot where the skull was found. The upper 7 or 8 feet was a mixture of shells and clay, and had been used to make a kind of cement. This discovery appears to make it certain that the bison lived in New York shortly after the Wisconsin ice had retired from the Finger Lake region.

3. Jamestown, Chautauqua County.—In the American Journal of Science, volume XXVII, 1835, page 166, is an account, by Knight, of the discovery, at Jamestown, of what were probably two teeth of a bison in a fragment of the jaw. These were encountered by John Hazeltine, in digging for a foundation of a building at the outlet of Chautauqua Lake, and at a depth of 10 feet. The soil was mostly gravel, but the jaw was said to have been lying in black muck. It was sent to Yale College, but was not recognized as belonging to Bison. Reasons were suggested why it did not belong to a young mastodon. The measurements given of the teeth agree well with the upper molars of an American buffalo. Joseph Leidy (Jour. Acad. Nat. Sci., Phila., vol. VII, 1869, p. 371) quoted Knight’s account as indicating a buffalo. The discovery is interesting, taken in connection with the finding of the specimen at Syracuse.

NEW JERSEY.

(Map 27.)

1. Trenton, Mercer County.—Mr. Ernest Volk (Papers Peabody Mus., vol. V, 1911, p. 209, plate CXX) reported the discovery of a part of a femur of Bison (probably B. bison) in the “yellow drift,” at Trenton, 2.5 feet from the surface. A first right upper molar, identified as that of Bison, was found in another sand-pit at a depth of 9 feet (op. cit., p. 136). This appears to have belonged in the Trenton gravel, but at that point the materials were apparently a mixture of sand and loam. The reader is referred to page 304, where the geology of this locality is described and a list of the species is given.

PENNSYLVANIA.

(Map 27.)

1. Stroudsburg, Monroe County.—In Crystal Hill (Hartman’s) Cave, near Stroudsburg, was found a lower jaw containing the last molar, as noted by Leidy (Proc. Acad. Nat. Sci., Phila., 1880, p. 347; Ann. Rep. Geol. Surv. Pennsylvania for 1887, p. 5). Mercer (Proc. Acad. Nat. Sci. Phila., 1894, p. 98), mentions a tooth of the existing bison found in Hartman’s Cave.

2. Riegelsville, Bucks County.—From a cave near Riegelsville, was sent to the Academy of Natural Sciences of Philadelphia, more than 70 years ago, a collection of bones, reported on by Leidy in 1880 (Proc. Acad. Nat. Sci., Phila., 1880, p. 349) and in 1889 (Ann. Rep. Geol. Surv., Pennsylvania, 1887, pp. 18–19). In the contribution of 1880, Leidy included Bison among the animals represented, but this is not included in the list of 1887. Why this was omitted is not known. If Bison occurred there, the probability is that it was represented by the existing buffalo.

INDIANA.

(Map 27.)

1. Jasper County.—The only record known to the writer of the finding of buffalo bones worthy to be regarded as fossil is that of the former State geologist, John Collett (Geol. Surv. Indiana, vol. XII, p. 73), who makes the statement that in Jasper County bones of the buffalo, the beaver, and the bear are common.

ILLINOIS.

(Map 27.)

1. Sullivan, Moultrie County.—In 1875 (Geol. Surv. Illinois, vol. VI, p. 186), the geologist George C. Broadhead reported that he had found the skull of a bison on the west bank of Kaskaskia River, about 3 miles southeast of Sullivan, on the land of John Purvis. The locality appears, therefore, to have been somewhere near the south half of the eastern line of township 13 north, range 5 east. The summit of the bluff here is described as rising about 25 feet above the stream. At the height of about 8 feet was a bench approximately 10 feet wide, and the skull was found on this bench, “a few feet from the top.” The surrounding clay was described as being a rich black loam.

Broadhead stated that the skull measured 12 inches across the forehead above the eyes and the same between the roots of the horns. The latter were short, thick, and slightly curved. In the Transactions of the St. Louis Academy of Science, volume III, page XXIII, practically the same account is given of the discovery. Here Broadhead expressed the idea that the skull belonged to Bison latifrons, and said that the horns were short, thick, and curved upwards and forwards. It is not known where the skull now is. To the writer it appears most probable that the skull was that of Bison bison. There is nothing in the description to indicate any of the other known species. As to the age of the deposits, the presumption is reasonable that they belong to the Late Wisconsin or Recent, for the locality is north of the Shelbyville moraine. It is possible that the bench belongs to the Illinoian; but the nature of the material, “a rich black loam,” seems to show that the bench is an alluvial deposit laid down since Wisconsin times.

2. Homer, Champaign County.—In the collection at the State University of Illinois, at Champaign, are the horn-cores and the rear of the skull of Bison bison, reported to have been thrown out of a ditch near Homer. The writer is informed by Professor R. M. Bagg, of Appleton, Wisconsin, that the specimen was found in excavating a ditch, at a depth of 4 feet, according to the report made to him. Homer is situated on a part of the Champaign moraine and the bison in question must be not older than Late Wisconsin. If it was really found at a depth of 4 feet it would seem to date well back in the Recent, if not into the Pleistocene.

3. Niantic, Macon County.—Professor A. H. Worthen reported (Geol. Surv. Illinois, vol. V, p. 308) the presence of bones of the buffalo in an old filled-up marsh near Niantic. The situation is more particularly described on page 102. With the bison bones were found those of the mastodon, the elk, and the Virginia deer. The bones of these animals are said to have been found under 4 feet of black muck, partly embedded in a light-gray quicksand filled with shells of Planorbis, Cyclas, and Physa.

Inasmuch as Niantic is situated near the border of the Shelbyville moraine, all these remains probably belong to Late Wisconsin times. It would be useful to know whether the bones of the buffalo, the elk, and the deer were found above those of the mastodons or mingled with them.

4. East of Whitewillow, Kendall County.—In township 35 north, range 8 east, probably in section 27, on land owned by John Bamford, in clearing out a well in a bog, have been found the bones of mastodons and other species of vertebrates. For a description of the locality and the species found there see page 337. Mr. George Langford, of Joliet, has reported the occurrence of bones of the existing bison there and has sent to the writer a maxilla which contained finely preserved teeth.

Unfortunately, no thorough and systematic examination of the place has yet been made. All of the species and the deposit belong to the Late Wisconsin, that part of it following the withdrawal of the ice. Mr. George Langford informed the author that he found the bison and deer bones mixed up more or less with the mastodon bones. At a depth of about 4 to 5 feet the owner of the place began to strike bones of the bison, which appeared very fresh, retaining considerable animal matter. From about 6 feet down to gravel, about 13 feet, mastodon and other bones were literally packed together.

5. Batavia, Kane County.—Dr. E. S. Riggs, of the Department of Palæontology, Field Museum of Natural History, wrote to the author that he had picked up some bison bones along a ditch in which mastodon bones had been found; but the depth at which they had been met with could not be determined. At the same time bones of the elk were found. Undoubtedly the mastodon remains belong to Late Wisconsin times; and it is probable that the bison and elk remains are to be referred to the same.

6. Galena, Jo Daviess County.—In the collection of the Academy of Natural Science of Philadelphia is a lower hindermost molar collected in a lead crevice somewhere near Galena. It was presented to the Academy by Mr. Henry Green, of Elizabeth, a town near Galena. This, with a metacarpal bone of Megalonyx jeffersonii, had been found at a depth of 130 feet from the surface. It was described and figured by Leidy (Contributions to Extinct Vert. Fauna, etc., 1873, p. 255, plate XXXVII, fig. 4). Leidy thought that it might have belonged to Bison bison, but not improbably to B. latifrons. J. A. Allen (The American Bisons, etc., p. 13) concluded that it belonged undoubtedly to the existing American species. The structure of the tooth will apparently not decide this matter. It is probable that most of the animals found in those lead crevices belong to pre-Wisconsin times; and the tooth in question may belong to an extinct species. A list of the species found in the lead region of Illinois, Iowa, and Wisconsin is to be found on page 343.

7. Mitchell, Madison County.—In “Records of Ancient Races in the Mississippi Valley” (1887), William McAdams, of Alton, Illinois, stated that in a large mound, square in shape, 300 feet on each side and 30 feet high, through which the railroads pass in the American bottom, at Mitchell, had been found, in contact with a number of copper implements and ornaments, a number of teeth of the buffalo. These McAdams had in his possession. While these teeth can not be regarded at all as belonging to Pleistocene times, the fact is of interest in connection with McAdams’s statement that in all his explorations during a period of more than 30 years, in no other case had he been able to find any evidences of the buffalo associated with the remains of the ancient people of this country. In this connection may be considered Shaler’s views on the modern coming of the buffalo east of the Mississippi River. On the other hand, account must be taken of the finding of a skull of a buffalo deep in lake deposits at Syracuse, New York.

WISCONSIN.

(Map 27.)

1. Bluemounds, Dane County.—In his report, made in 1862, on the geology of the lead region of Wisconsin (Geol. Surv. Wisconsin, vol. I, p. 136), J. D. Whitney recorded the finding of bison bones in a crevice at Bluemounds. From the same crevice were obtained bones and teeth of the mastodon and of a peccary, and bones of a wolf. It was supposed that these remains were found at a depth of about 40 feet and embedded in the red clay commonly found in such crevices. These bones were put into the hands of Jeffries Wyman for identification, who, on page 421, stated that the bison bones were all of the size of the same parts of the existing buffalo and closely resembled them. J. A. Allen (Amer. Jour. Sci., vol. XI, 1876, p. 47), in referring probably to the same bones, speaks of “an extinct bison,” without, however, giving any reasons for his conclusion. It is nevertheless possible that he was correct.

The writer formerly believed that the fossil vertebrates, collected in the fissures in the lead region, had lived after the close of the Wisconsin glacial stage. It seems now more probable that they belong to a pre-Wisconsin time.

2. Oshkosh, Winnebago County.—The writer has received from Dr. S. Weidman, State geologist of Wisconsin, a humerus, found in a marsh near Oshkosh, quite evidently that of Bison bison. Although stained by iron on the outside, the remainder of the bone is white and full of animal matter. The animal may have lived during the Recent period.

KENTUCKY.

(Map 27.)

1. Bigbone Lick, Boone County.—Great numbers of individuals of Bison bison have been found at Bigbone Lick. Cooper (Monthly Amer. Jour. Geol., vol. I, pp. 207, 211) reported numerous bones of buffaloes and even an entire skeleton, but they appear to have been near the surface or even on it. Lyell (“Travels in North America,” Murray’s ed., vol. II, p. 65) stated that he had seen great quantities of remains of the bison in a superficial stratum in the river bank; but he was left in doubt whether or not the animals had been contemporaneous with the mastodon. Shaler (Geol. Surv. Kentucky, n. s., vol. III, p. 197) found abundant remains of the buffalo at this place; but the bones were not found at any great depth, except in the bog about the spring. He regarded it as proven that the musk-ox and the caribou did not come into contact with the recent buffalo, but were extinct before it came. Some of the bison materials collected by Shaler were described by Dr. J. A. Allen, in 1876 (Mem. Mus. Comp. Zool., vol. IV; Mem. Geol. Surv. Kentucky, vol. I, pt. 2). It may be difficult to prove that any of the bison bones and teeth found here are of Pleistocene age; but there appears to be no good reason why this species might not have reached that region at the close of the Wisconsin ice-stage. A list of the species of mammals found here is given on page 403.

2. Bluelick Springs, Nicholas County.—In the mass of materials collected in the spring at Bluelick Springs by Mr. Thomas W. Hunter, were skulls and parts thereof, teeth, limb-bones, and vertebræ. The actual geological age of these remains can not be established; but they were of probably late Wisconsin age.

FINDS OF CASTOROIDES IN PLEISTOCENE OF EASTERN NORTH AMERICA.

NEW YORK.

(Map 28.)

1. Clyde, Wayne County.—A skull of the giant beaver was found, about the year 1846, near Clyde, on the farm of Gen. W. H. Adams. The locality and the geological conditions were described by James Hall (Proc. Boston Soc. Nat. Hist., vol. II, 1846, p. 167; Boston Jour. Nat. Hist., vol. V, p. 385). The region is on the divide between the streams flowing north into Lake Erie and those flowing southward into Clyde River. The actual spot was at the head of a shallow stream which flows into Lake Ontario. At this point the Sodus Canal was cut and ran in a north-and-south direction. The farm was only partly swampy. Hall’s section is as follows from above downward:

1. Vegetable soil, 2 feet or more.

2. Fine sand, with some alternating layers of clay, containing twigs, leaves, etc., 2 to 3 feet.

3. Muck, or peaty soil, with decayed wood, bark, leaves, and even trunks of large trees, about 4 feet.

4. Fine sand, with fresh-water shells, 2 to 3 feet.

5. Drift, with boulders; depth unknown.

The skull was found at the bottom of No. 3, at a depth of 8 feet. It is evident that this animal lived here near, or after, the close of the Wisconsin stage, and after the old Lake Iroquois had withdrawn from the region.

2. Canastota, Madison County.—In 1914, Dr. Burnett Smith, of Syracuse University, reported (Amer. Jour. Sci., vol. XXXVIII, p. 463) the discovery, at this place, of an incisor tooth of the giant beaver. The exact locality is given as about 225 paces northwest from the southeast line of lot 10, town of Lenox, on Cowaselon Creek, otherwise known as the “State ditch.” The tooth was found at a depth of 9 feet, in a sticky blue clay, containing a few fresh-water shells. Just above this, at a depth of 7 feet, is a layer made up principally of shells, with some vegetable matter. This animal could not have lived here until after the withdrawal of Lake Iroquois, and therefore not till near the close of the Wisconsin stage.

PENNSYLVANIA.

(Map 28.)

1. Stroudsburg, Monroe County.—In 1889, Dr. Joseph Leidy reported (Ann. Rep. Geol. Surv. Pennsylvania, 1887, p. 14, plate II, figs. 7–20) the discovery of teeth of Castoroides ohioensis in Hartman’s (or Crystal Hill) Cave, about 3 miles southwest of Stroudsburg and 5 miles from Delaware Water Gap. Its elevation is about 800 feet above the level of Delaware River. The species associated with this giant beaver will be listed on page 309. The parts figured by Leidy are a portion of a palate, with the molars and some of the premolars, and both rami of the lower jaw, showing the three temporary molars and the first true molars, with some incisors and the permanent canines.

OHIO.

(Maps 28, 29, 36.)

1. Nashport, Muskingum County.—In 1836 (Amer. Jour. Sci., ser. 3, vol. XXXI, pp. 79–83), S. P. Hildreth, in an unsigned article, gave an account of the finding of remains of the type specimen of the giant beaver, in association with remains of mastodon and of a supposed fossil sheep, at a point 2 miles north of Nashport. A canal, now abandoned, was being constructed, which followed two small streams, one of which flowed into Licking River, the other into Wakitomika Creek. The land traversed was flat and swampy. The distance from Nashport to Wakitomika Creek is nearly 4 miles, so that in saying that the spot was on this creek Hildreth spoke in general terms. The bones of the mastodon and the right halves of the lower jaws of two giant beavers were found resting on a bed of gravel at a depth of 14 feet. Foster (2d Ann. Rep. Geol. Surv. Ohio, 1838, p. 80) stated that a molar and a tusk of an elephant had also been found here. Hildreth concluded that the jaws and teeth were perhaps those of an animal of the beaver family; “or, from the grooved outer surfaces of the incisors, a marine animal of the walrus or seal race, and a borderer of the ancient ocean.” It was afterwards described by J. W. Foster (2d Ann. Rep. Geol. Surv. Ohio, 1837, p. 80, figs.) under the name of Castoroides ohioensis. The remains described consisted of the front end of one side of a lower jaw with its incisor, an upper incisor, and a radius. They showed signs of some attrition; but in a region like that they could not have been transported any considerable distance.

In the mud in which the canal at this point was cut, there were found three skulls of a species of sheep, which Hildreth thought were different from those of the domestic sheep and to which he gave the name of Ovis mamillaris. They are said to have been discovered at a depth of 8 feet. It seems quite possible that they had been lying on or near the surface and had made their way to the side of the canal by the flow of the mud, which gave much trouble by filling up the canal during the night. Most, if not all, of the differences thought to separate these skulls from the domestic sheep disappear on comparison. The specimens of both Castoroides and of the sheep have probably been lost. They appear not to be at Zanesville. On page 82 of the article above cited, Hildreth stated that he had received, from some point on Wills Creek, a portion of a tooth similar to the one found at Nashport; the place was said to be about 40 miles east, apparently, of Zanesville. This would seem to be in Noble County. The tooth was described as being embedded in dark-colored carbonate of lime and as having fallen from a calcareous rock which lies near the tops of the hills, 150 feet above the bed of the creek. It is very probable that this was not a tooth of Castoroides. It may have been the spine of a palæozoic shark.

2. Wilmington, Clinton County.—From Professor W. C. Mills, of the Ohio State University, the writer in 1913 obtained information that a fine skull of Castoroides, without the lower jaw, had been found on the farm of Mr. J. M. Richardson, on the western border of Wilmington. Nothing more has been learned about the discovery. The locality is north of the Hartwell moraine, and the animal must have lived there after the withdrawal of the ice-sheet from that region.

3. Germantown, Montgomery County.—One mile east of Germantown, Edward Orton, State geologist of Ohio, found along Twin Creek a large tooth which (Amer. Jour. Sci., ser. 2, vol. L, 1870, p. 54) he compared with the tusk of a hog. It was later identified by J. S. Newberry (Proc. Lyc. Nat. Hist. New York, vol. I, 1870, p. 83) as belonging to Castoroides. It was found in a bed of peat which is overlain by from 50 to 100 feet of glacial drift. One might conclude that the animal had lived there at some time between the Illinoian and Wisconsin stages. However, opinions have differed.

The geology along Twin Creek has been studied by Orton, Wright, and Leverett. The last named published his views in 1902 (Monogr. U. S. Geol. Surv., XLI, pp. 363–365, plate XIV, fig. 1). He states (p. 365) that there seem to be good reasons for believing that the peat-bed indicates the lapse of a considerable interval of deglaciation. Whether the interval preceded or followed the formation of the early Wisconsin moraine is yet to be determined. That seems to mean that the interval may be mid-Wisconsin or pre-Wisconsin. Wright thought that but a few hundred years had elapsed between the deposit of the till below the peat and that above. Orton’s description of the locality was published in 1870 (Amer. Jour. Sci., ser. 2, vol. L, p. 54).

4. West Sonora, Preble County.—In 1893 (Amer. Geologist, vol. XII, p. 73), Professor Joseph Moore reported that a fragment of an upper incisor of Castoroides had been found at West Sonora. It was associated with remains of a mastodon. West Sonora is on the Englewood moraine.

5. Greenville, Darke County.—In 1883 (Jour. Cin. Soc. Nat. Hist., vol. VI, p. 238), F. W. Langdon described a tooth of Castoroides, found at a depth of 4 feet, in a swampy locality near Greenville. In 1893 (Amer. Geol., vol. XII, p. 73), Joseph Moore stated that this tooth belonged to Dr. J. W. Jay, of Richmond. It may now possibly be in the collection of Earlham College. Moore said that it had been found associated with mastodon.

In the public library at Greenville is a fragment of an upper incisor of Castoroides, found in making a ditch along Bridge Creek, in 1889, by Mr. Leo Katzenberger, who writes that the place is in the northwest corner of section 1, township 11, range 2 west, 1.5 miles southwest of Greenville. These animals likewise lived on or near the Sidney moraine.

6 New Knoxville, Auglaize County.—In C. W. Williamson’s “History of Ohio and Auglaize County,” 1905, on page 338, with a figure, is an account of the finding of a skull of Castoroides ohioensis in section 29 of Washington Township, which is in township 6 south, range 5 east, and near New Knoxville. The discovery had been made that beneath a bed of humus there was a stratum of gravel of a quality for road making. In removing the upper peaty layer, the head of the giant beaver was discovered, near the south margin of the pond. Williamson stated that the house of the animal was uncovered. It was between 3 and 4 feet high and about 8 feet square; the poles of which it was constructed were about 3 indies in diameter and were laid after the manner of the houses of modern beavers. Apparently the beaver died in the house, and it was thought that after the death of the beaver wolves or other carnivorous animals had inhabited the house, since bones of deer and other animals were strewn over the floor. It is to be regretted that the house, if such it was, was not taken up in a way that it might have been accurately reconstructed. Williamson’s account is reproduced in Bulletin 16, Geological Survey of Ohio, 4th series, 1912, page 39.

In Heidelberg University, Tiffin, Ohio, the writer has seen a very large skull of Castoroides, labeled as found at Wapakoneta, but it is quite certainly the one found at New Knoxville. Both incisors are broken off close to their insertion in the skull. Williamson’s figure represents at least the left one present.

MICHIGAN.

(Map 28.)

1. Berrien County.—In the American Museum of Natural History, New York, is a nearly complete skull with the left ramus of the lower jaw, purchased from Mr. George A. Baker. The exact place in the county where it was found is unknown, and the writer has been unable to get into communication with Mr. Baker.

As to the time in the Pleistocene when this individual lived, we may be sure that it was after the Wisconsin glacial ice-sheet had abandoned this county. How long after this retirement it is impossible to say. It is to be noted that both mastodons and mammoths have been found in this county, in what appear to be deposits of the same age.

2. Adrian, Lenawee County.—In the U. S. National Museum is a skull of Castoroides (Cat. No. 197), of which the lower jaw is missing. This was received June 10, 1880, from Professor J. Kost, then of Adrian College, Michigan. In his letter Professor Kost wrote as follows:

“Found in fresh-water marsh, 4 feet under, in Adrian, Lenawee Co., Michigan. In same place as the Decker mastodon, now in Adrian College; also of lower jaw of smaller mastodon (sent in this consignment), with various bones of elk, deer, etc.”

The mastodon jaw referred to is in the U. S. National Museum (No. 188). The present writer has not been able to learn exactly where all these bones were obtained. It would be interesting to know whether all–mastodons, giant beaver, elk, and deer–were found in the same excavation. It is probable that they were at least in nearly the same spot. For remark on the age of the deposits at Adrian see page 81.

3. Ann Arbor, Washtenaw County.—In the collection of the Department of Geology in the University of Michigan is a skull which lacks the lower jaw and is otherwise slightly injured. A report of this specimen was made in 1914 by Mr. N. A. Wood (Science, n. s., vol. XXXIX, p. 759). This was found several years ago in a peat-bog on the farm of Professor J. B. Steere, 3 miles south of Ann Arbor, at a depth said to have been about 3 feet. Beneath the peat and muck is a gravelly marl. According to the Ann Arbor Folio (No. 155, U. S. Geol. Surv.), there is, running south from the city, a strip of low ground designated as occupied by peat and muck. This borders on the east a part of the Fort Wayne moraine, and must have provided an ideal spot for colonies of these great beavers. Naturally these specimens must be credited to the Late Wisconsin stage.

4. Attica, Lapeer County.—In the collection of Alma College, Alma, Michigan, is a fragment of an upper incisor, found at a depth of 7 feet, in digging the tail-race of a mill in Attica. The statement was made that at the same place there were often found what appeared to have been beaver dams made of wood. This wood crumbled on coming to the air. In cases like this there is a fine opportunity to determine whether or not the wood had been gnawed by the broad incisors of Castoroides or by the narrower ones of the existing beaver. The wood might easily be prevented from crumbling by replacing the water with a solution of gum arabic or even of glue.

Attica is situated some distance outside of the beaches of old Lake Maumee, and on low ground between morainic tracts left by the Saginaw lobe in its retreat. These gigantic beavers must, therefore, have lived near the close of the Pleistocene.

5. Owosso, Shiawassee County.—In the collection of the University of Michigan (No. 3109) is the greater part of a lower jaw of a giant beaver, found somewhere near Owosso, in a swamp deposit. An account of this specimen was given in 1914 by Mr. N. A. Wood (Science, n. s., vol. XXXIX, p. 758). It was received from Mr. A. G. Williams in 1892. According to Leverett and Taylor’s glacial map of Michigan, Owosso lies a few miles outside of the beach of old Lake Saginaw. This is supposed to have come into existence about the close of the period of Lake Maumee. The earliest time when this beaver might have existed, leaving out the question of the climate, would coincide closely with the time when the one found at Attica might have lived. It is most probable that both lived at a time when the glacier front was farther away.

INDIANA.

(Maps 28, 30.)

1. Vanderburg County.—In 1884 (14th Ann. Rep. Geol. Surv. Indiana, pt. 2, p. 37), in a footnote written probably by John Collett, State geologist, it is stated that remains of Castoroides ohioensis had been found in this county. Inasmuch as this county lies outside of the drift region, and as no details as to place and depth were given, we can arrive at no conclusion as to the stage of the Pleistocene in which the possessor of this tooth lived. The reader may consult page 258.

2. Richmond, Wayne County.—About 2 miles east of Richmond, where a farmer was scooping out wet earth for a fish-pond, there was found by Joseph Moore (Amer. Geologist, vol. XII, p. 73) a fragment of an upper incisor of this species. With it were sound and decayed teeth of the mastodon. Most probably this fish-pond was being excavated in low ground where a marsh had existed. Richmond is situated just south of the Bloomington moraine, on an area which is undulating and more or less morainic. The animal must have lived at some time after the culmination of the Wisconsin stage.

3. Greenfield, Hancock County.—In 1893 (Amer. Geologist, vol. XII, p. 73), Joseph Moore mentioned the fact that some remains of Castoroides had been found near Greenfield and that these were in the possession of Dr. M. M. Adams. In 1900 (Proc. Ind. Acad. Sci. for 1899, p. 171, plates I, II), Moore presented figures of the skull and made some brief statements regarding it. At that time the skull had come into the possession of Earlham College. If restored this skull would have had a length of 13 inches. Nothing is known as to the exact place where it was found, but it can not be doubted that the animal lived after the Wisconsin ice had retreated further north.

4. Jamestown, Boone County.—In the State Museum at Indianapolis is a lower jaw of a giant beaver which has all of the molars, but whose incisors are broken off at the border of the bone. This specimen was presented by Mr. A. E. Deatley, of Lizton, Hendricks County, who found it in earth thrown out by a dredging machine, but the exact locality was not stated. Jamestown is situated on Eel River where it crosses the Champaign moraine. The geological age of the animal is therefore Late Wisconsin.

5. Summitville, Madison County.—In the State Museum at Indianapolis is an upper right incisor of the giant beaver in its premaxilla, labeled as presented by Mr. J. F. Cartwright. Nothing more is known of the history of the specimen.

Summitville is surrounded by plains of Wisconsin drift. It is about 12 miles from the place where was found the fine mounted specimen of Elephas primigenius now in the American Museum of Natural History, New York.

6. Union City, Randolph County.—Here was found the nearly complete skeleton of Castoroides ohioensis at Earlham College, Richmond, Indiana. This was secured by Professor Joseph Moore, who described and figured it. It was discovered on the farm of John M. Turner, about 8 miles nearly east of Winchester. Mr. Turner has informed the writer that the farm is a part of section 15, township 17, range 1.

The bones occurred in a layer of fine-grained marly silt from 2 to 3 feet thick, overlain by from 3 to 4 feet of dark loose mold abounding in fragments of shrubby stems and vines in various stages of decay. Under the silt containing the bones were coarser and finer drift gravels which formed the bottom of the ditch. In the silts were found fresh-water gasteropods and bivalve shells. Along the same ditch, within a distance of 30 rods, other fragments were found which were supposed to indicate 9 individuals of Castoroides. As this region is covered by Wisconsin drift, the animal evidently lived after the Wisconsin ice-sheet had retired from the Union City moraine, possibly a long time thereafter.

7. Fairmount, Grant County.—Near Fairmount were found some limb-bones and other parts (but no skull) of the giant beaver. These were obtained not far from where the large specimen of Elephas primigenius was discovered which is mounted in the American Museum of Natural History in New York. The remains of this Castoroides are in the Field Museum of Natural History. No details regarding the find have been published. It was stated that near the bones were parts of trees, as though a dam had been built there; but this interesting matter appears not to have been investigated.

The elephant mentioned above was found on the farm of Dora C. Hitt, in the southeast quarter of section 23, township 23 north, range 8 east.

8. Carroll County.—In 1884 (14th Ann. Rep. Geol. Surv. Indiana, pt. 2, p. 37) the State geologist, John Collett, wrote that Castoroides had been found in this county; but nothing was added to this statement. On the map the number is placed arbitrarily.

9. Logansport, Cass County.—In the U. S. National Museum is a fine skull of Castoroides, without lower jaw, which, according to the newspaper report accompanying it (dated January 30, 1894), was found 2 or 3 miles north of Logansport, by Mr. S. L. McFadin, who sold it to the National Museum. It lay at a depth of 7 feet on a fine sand, above which was a foot of solid gravel, then 3 feet of solid clay, and at the top 3 feet of alluvium. According to Leverett and Taylor’s map of the region (Monogr. U. S. Geol. Surv., vol. LIII, plate VI), this place would be on the moraine which lies north of the Wabash River, the meeting-place of the ice-lobes coming from Lake Michigan, Lake Erie, and Saginaw Bay.

10. Macy, Miami County.—From Mr. C. F. Fite, Denver, Indiana, the writer received a photograph of a tooth of Castoroides, apparently the lower right incisor. This was found in Allen Township. Mr. Fite gives as the exact locality section 23, township 29, range 3 east. This would be not far from Macy. It lies, therefore, on or near the northern border of the great moraine which extends from Delphi, Indiana, to the northeastern corner of the State.

11. Kosciusko County.—As in the case of Cass County, we depend for our knowledge of the discovery of Castoroides in Kosciusko County on the statement made by John Collett, in the place there cited.

12. Grovertown, Starke County.—From Dr. E. S. Riggs, of Field Museum of Natural History, the information has been received that there is at that museum a fine skull, with the right half pf the mandible, of a giant beaver which was found 1.5 miles west of Grovertown, in making an excavation for the abutment of a bridge, 6 feet below the surface in township 34 north, range 1 west. This is within the region of the Pleistocene Lake Kankakee.

ILLINOIS.

(Maps 28, 38.)

1. Shawneetown, Gallatin County.—In the collection of the Academy of Natural Science of Philadelphia are a part of one incisor, two molars, and two petrous bones which were many years ago obtained by a Dr. Feuchtwanger, from a well at a depth of 40 feet. These were mentioned by Le Conte in 1852 (Proc. Acad. Phila., vol. VI, p. 53). Leidy has figured the incisor (Holmes’s “Post-Pliocene Fossils of South Carolina,” 1860, plate XXII, fig. 5; Ann. Rep. Geol. Surv. Pennsylvania, 1887, plate II, fig. 10). Leverett (Monogr. U. S. Geol. Surv., vol. XXXVIII, p. 65) states that at Shawneetown a boring for gas and oil penetrated 112 feet of alluvial and other deposits before reaching rock. His map (plate VI) indicates that here the valley of the Ohio is composed of sand and gravel plains of Wisconsin age. Under the conditions it seems impossible to form any certain conclusions regarding the geological age of this specimen. It belongs possibly to the later half of the Pleistocene.

2. Alton, Madison County.—In the McAdams collection, described on page 338, is a part of a large upper incisor, in two pieces, of a specimen of Castoroides, with McAdams’s Nos. 209, 210, and a small fragment of another incisor. All three specimens are more or less enveloped in nodules of hard materials. In 1883 (Trans. St. Louis Acad. Sci., vol. IV, p. LXXX) McAdams stated that he had seen, both in true and modified drift, remains of rodents large and small, but one, an extinct beaver, was of monstrous size.

For conclusions as to the age of the fauna secured by McAdams see page 339.

3. Charleston, Coles County.—In 1867 (Proc. Acad. Nat. Sci. Phila., p. 97), Leidy briefly described a skull of Castoroides, sent to him for examination by Professor A. H. Worthen. It lacked both zygomatic arches and the incisor teeth. The length of the skull was 10.5 inches. This skull had been found by someone while he was plowing in a field near Charleston. The region about Charleston is covered by the Shelbyville lobe of the early Wisconsin drift. The animal must have lived at some time after the deposition of that drift.

4. Naperville, DuPage County.—H. M. Bannister (Geol. Surv. Illinois, vol. IV, p. 113) reported a skull and other parts of the skeleton of Castoroides, found by a farmer in a slough not far from Naperville. The skull went to Colonel Wood’s Museum in Chicago, and it was probably destroyed in the great fire of 1871. This animal quite certainly lived after the retirement of the Wisconsin ice-sheet.

SOUTH CAROLINA.

(Map 28.)

1. Charleston, Charleston County.—In 1860, Dr. Joseph Leidy (Holmes’s Post-Pl. Foss. South Carolina, p. 114, plate XX, figs. 6–8) recorded the fact that fragments of the teeth of the giant beaver had been found in the Pleistocene deposit of Ashley River.

In the Pinckney collection is an upper cheek-tooth, the fourth premolar. The height of the tooth is 37 mm., the length is 16 mm., the width 11.5 mm. It was found in the vicinity of Charleston.

In the Scanlan collection, the property of Yale University, and made in the vicinity of Charleston, are five more or less injured teeth. One is a left upper molar, either the second or the third. The length of the grinding-surface is 12 mm., the width 13 mm. Two fragments of upper right incisors are interesting. One of these, 140 mm. long, bears the oblique excavated surface worn by the lower incisors. Each diameter of the tooth is 25 mm. The other fragment is 123 mm. long and comes from the middle of the tooth. The two diameters of this tooth are, as in the other one, 25 mm. Both of these teeth appear to be more strongly curved than the teeth of more northern specimens. Also, the striation on the outer face of the tooth is finer, finally becoming hair-like lines as the rear face is approached. More of the larger ridges in the front of the tooth are directed obliquely and terminate along a front groove than in specimens hitherto observed. It is possible that an undescribed species is indicated. The two teeth present some differences between themselves. Another fragment, 103 mm. long, has a diameter of 20 mm. At the base is seen a part of the pulp-cavity.

GEORGIA.

(Map 28.)

1. Brunswick, Glynn County.—In a small collection of vertebrate fossils made during dredging operations at Brunswick not many years ago, and which now belongs to the Geological Survey of Georgia, Gidley found a fragment of an incisor tooth of Castoroides ohioensis. The accompanying species will be recorded on page 370. Gidley’s list is found on page 436 of Bulletin No. 26 of the Geological Survey of Georgia.

MISSISSIPPI.

(Map 28.)

1. Natchez, Adams County.—James Hall, in 1846 (Proc. Bost. Soc. Nat. Hist., vol. II, p. 168; Jour. Bost. Soc. Nat. Hist., vol. V, p. 380), announced that remains of this animal had been found in the neighborhood of Natchez. The exact locality is unknown and likewise the conditions under which the specimens were discovered. This species is not included by Leidy in his list of fossil mammals found in Pleistocene deposits in Mississippi up to 1854 (Wailles, Agri. Geol. Mississippi, p. 196).

A list of the species found in the vicinity of Natchez is presented on page 392.

TENNESSEE.

(Map 28. Figure 23.)

1. Memphis, Shelby County.—In 1850, Dr. Jeffries Wyman reported (Proc. Bost. Soc. Nat. Hist., vol. III, p. 281) that a part of a lower jaw of Castoroides had been found at Memphis. With it were a toe-bone of Megalonyx, a tooth of a young mastodon, and a part of the lower jaw of a beaver. It was thought that these remains had been buried in the deposits laid down by Mississippi River. It is to be regretted that the locality and the height above the river were not more exactly specified. The specimen of Castoroides, a right ramus of the lower jaw, is now in the Academy of Natural Sciences of Philadelphia.

ON THE PLEISTOCENE GEOLOGY OF NORTH AMERICA AND ITS RELATION TO ITS FOSSIL VERTEBRATES.

ONTARIO.

For a knowledge of the Pleistocene of Canada, the student ought first to read Dr. J. W. Dawson’s “Canadian Ice Age,” published in 1894. In this will be found references to the earlier literature of the subject. For the results of more recent studies the reports of the Canadian Geological Survey are to be consulted, as well as papers published in the scientific journals. For the more important of these papers the reader may consult the list published by Dr. H. L. Fairchild in 1918 (Bull. Geol. Soc. Amer., vol. XXIX, pp. 229).

To state the matter briefly, one may say that almost everywhere in Ontario are deposits of glacial drift of Wisconsin age. In a few localities have been discovered beds which belong to earlier glacial and interglacial epochs. On the other hand, around Hudson Bay, around the Gulf of St. Lawrence, along St. Lawrence and Ottawa Rivers, and the Bay of Fundy are marine deposits, laid down after the Wisconsin ice had retired from those localities and while the region which had been occupied by this ice-sheet was depressed so much that the sea could enter the basins named.

The most interesting locality in Canada for the student of vertebrate palæontology is doubtless Toronto, because of the presence there of Pleistocene deposits belonging to more than one stage, and because of the discovery of several species of extinct vertebrates and of many mollusks, insects, and plants. For an understanding of the geology of the region Coleman’s papers must be studied, as well as those of authors cited by him. On the interglacial deposits three of Coleman’s papers may be especially cited (Jour. Geol., vol. IX, 1901, pp. 285–310; 10th Internat. Cong. Geol., 1906, Mexico, pp. 1237–1258; Bull. Geol. Soc. Amer., vol. XXVI, 1915, pp. 243–254).

According to Coleman’s figure 1 of the first paper cited, the known interglacial deposits in that region extend from the mouth of Humber River eastward beyond the mouth of Rouge River, a distance of about 22 miles, and away from the lake a distance of about 8 miles. Deposits have been found even 14 miles north of Toronto (Coleman, 1915, p. 246). Coleman’s sketch map of the region, taken from his paper of 1901, is here reproduced (fig. 3).

According to Coleman (paper of 1915, p. 243) there are known at Toronto five well-defined sheets of boulder clay, with four sheets of interglacial sand and clay separating them. So far as the writer knows, only the lowest of these beds have been described with any particularity. These lowest beds constitute the Toronto formation, and it is these which have furnished nearly all the fossil animals and plants discovered in that region. This Toronto formation is divisible into two portions, and these have been designated as the Don beds and the Scarboro beds. They are regarded as having been deposited in the valley of an ancient river running from Georgian Bay to Scarboro. Of these the Don beds are the older. Sections of these are found in Toronto and outside, especially along Don River. They have been laid down usually on a boulder clay, 1 to 9 feet thick, which itself reposes on Hudson River shales. At one point along the Don an interglacial river had cut through both the boulder clay and the shale to a depth of 16 feet. The Don deposits consist of varying layers of sands, gravels, and clays. At one point the section obtained amounted to about 27 feet; but this, combined with another, made up about 44 feet. At one place trunks, 12 or 15 feet long, of trees have been found, which were flattened into the surface of the boulder till; also shells of unios, which are embedded in clay close to the boulder till.

In 1913 (Ontario Bur. Mines. Guide Book No. 6, pp. 15–18), Professor Coleman presented a list of the species found in the Don beds. Of the plants 32 species of trees had been secured, among them the pawpaw, the red cedar, and the osage orange; 41 species of fresh-water mollusks were listed, of which 12 were Unionidæ.

As bearing on the climate, it may be said that there are 12 species of the genus Unio listed, of which 4 species are now known only from localities south of the St. Lawrence drainage; while 3 other species live in Lake Erie, but not in Lake Ontario. The plants are mostly trees; and several species, as the osage orange and the pawpaw, are now found only considerably farther south. One species of maple no longer exists. Penhallow gave it as his opinion that the flora points conclusively to the existence of climatic conditions of a character more nearly like that of the middle United States to-day. The unios now missing from that region give evidence to the same fact. For these reasons the Don deposits are spoken of as the warm-climate beds.

The Scarboro beds are finely displayed at Scarboro heights, a few miles east of Toronto. The thickness of the clay here amounts to about 94 feet. In these deposits have been found possibly mammoth or mastodon and caribou, but there is some uncertainty about these. Only 14 species of plants have been secured and these are trees; but apparently no mollusks have been reported. As an offset there are great numbers of beetles. Of these there have been described 72 species, and all are extinct except 2.

The trees, according to Penhallow, indicate a climate somewhat cooler than that now prevailing in that region. The same conclusion was reached by Scudder from his study of the insects. In his paper of 1901, Coleman took the view that the Toronto formation had been laid down in the interval between the Iowan and the Wisconsin glacial stages, that is, during what is now known as the Peorian. In the address of 1906, page 44, he appears to have been inclined to accept Leverett’s view that at least the Don beds belonged to the Sangamon stage. By 1915 (paper cited, p. 252) he had about concluded that the Toronto beds were as old as the Aftonian stage.

Dr. G. F. Wright, in 1912 (Bull. Geol. Soc. Amer., vol. XXV, pp. 205–218), accounted for the deposits and fossil animals and plants found at Toronto in a different way. At a certain time in the Pleistocene the region about Toronto was occupied by some species of animals and plants now found only considerably further south. An ice-sheet from the Keewatin center extended thither and laid down the Don beds. Later the Labrador glacier pushed into that region and deposited the Scarboro beds. According to this view the whole succession of events would be much shortened.

The writer is disposed to accept Leverett’s estimate of the geological position of the interglacial beds at Toronto. The presence there of Elephas primigenius, Mammut americanum, and the probable Ursus americanus hardly counts in the determination of the geological age, for all these animals appear to have continued on from at least the Aftonian interglacial to the close of the Wisconsin. There are no specimens that show that either Rangifer or Cervalces existed during the Aftonian, although one can hardly doubt that they did then exist. In order to show that the Toronto formation belongs to the Aftonian, it would be necessary to produce satisfactory stratigraphical evidence or to find there genera and species of mammals which characterize the Aftonian, such as camels, Elephas imperator, and those horses which belong to the early Pleistocene. If the deposits belong to the Sangamon stage, such horses as Equus complicatus and E. leidyi ought in time to be discovered there.

Coleman has discussed the interglacial beds that occur elsewhere in Canada (10th Internat. Geol. Congr. 1906, Mexico, pp. 1237–1258; Bull. Geol. Soc. Amer., vol. XXVI, 1915, pp. 243–254). He refers to Chalmers’s account of interglacial deposits along Lake Erie; but so far as the writer has been able to determine, most of the deposits referred to are of Late Wisconsin age. However, as he says, Spencer found interglacial materials near Niagara Falls. Other beds have been discovered along Moose River, south of James Bay; but their geological position has not been definitely determined, and the fossils discovered there, mostly proboscideans, are not referred with certainty to the interglacial deposits.

Most of the vertebrate fossils found in Ontario, excepting many of those found at Toronto, belong to the Late Wisconsin stage; and in studying their geological relations one must, as in the States of New York, Ohio, Indiana, and Michigan, take into consideration the history of the Great Lakes after the Wisconsin ice-sheet began to retire. According to Leverett and Taylor’s maps (Monogr. LIII, U. S. Geol. Surv., plate XIV), as early as the time when the glacial ice had just begun to withdraw from Lakes Michigan and Erie, a considerable area of land had become cleared of ice in the peninsula bounded by Georgian Bay, Lakes Huron, Erie, and Ontario. We can hardly suppose, however, that any mastodons or any elephants, except possibly Elephas primigenius, could have made their way to that area. Even the last-mentioned species would have had to travel over many miles of glacial ice. Conditions were hardly more favorable when Lake Whittlesey had come into existence (op. cit., plate XVI). At a later stage (op. cit., plate XVII) the ice-free parts of the peninsula could have been reached only by crossing the lakes or over wide stretches of glacier. It is possible that some of the mastodons and elephants that have been found had crossed over into Ontario at about the stage represented by plate XIX of the work cited, but it is more probable that they lived there at a later time.

Brief mention is here made of the fossil vertebrates found in Ontario and their localities. More detailed statements will be found on the pages cited.

Beginning in the west, a mastodon has been found at Blythewood, Essex County (p. 45). In Elgin County a mastodon has been met with at St. Thomas (p. 45), and a mastodon (p. 45) and an undetermined species of elephant at Highgate (p. 45). A little farther back from the lake, at London, Middlesex County, has been found a mastodon (p. 45). At Marburg, not far from the shore of Lake Erie, Dr. H. M. Ami exhumed a mastodon (p. 45). The writer has not learned how this locality is related to the ancient beaches. At Dunnville, Haldimand County, a mastodon has been secured (p. 46). It could hardly have lived there before the lake had assumed nearly its present level. The same remark will apply to the time when the mastodon (p. 46), Elephas columbi (p. 147), and possibly E. primigenius (p. 166) lived at St. Catharines. From Hamilton, at the extreme western end of Lake Ontario, have been described remains of Elephas columbi (p. 147), E. sp. indet. (p. 166), elk, Cervus canadensis (p. 235), and the beaver. Elephas primigenius has been found at Toronto, (p. 130); also Cervalces, a bison (p. 256), and a reindeer (p. 244). The same elephant has been discovered at Amaranth, in Dufferin County (p. 130). The elk, Cervus canadensis, has been reported from Strathroy, Middlesex County, and Kingston, Frontenac County (p. 235). At Smith’s Falls, Lanark County, the humpback whale, Megaptera boöps, has been discovered (p. 17). White whales, Delphinapterus leucas and D. vermontanus, have been found at Pakenham, Lanark County (p. 17), at Cornwall, Stormont County (p. 18), Nepean Township (p. 17), Ottawa East, Carleton County, and Williamston, Glengarry County (p. 18). At Ottawa has been discovered an assemblage of species, as listed on page 287.

The geology of the Hamilton locality has been described by Logan (Geol. Canada, 1863, p. 914), by Spencer (Canad. Naturalist, vol. X, 1883, pp. 222–230, 306–308), and by Coleman (Bull. Geol. Soc. Amer., vol. XV, 1904, p. 351). The remains mentioned were found in deposits forming what is called Burlington Heights. Here Dundas Valley opens into the extreme western end of Lake Ontario. The valley is about a half mile wide. Across this had been formed a bar, interrupted only at its northern end, with a height of 108 feet above the level of the lake and a width varying from a few hundred yards to less than a half mile. Its height is almost that of the Iroquois beach found on the south shore of the lake and continuing on the northern shore. Many years ago a canal was cut through the narrowest part of the bar, and it was in the construction of this that the elephant (p. 166), elk (p. 235), and beaver bones were found. It is evident that the bones were deposited there while the bar was being built and at a time when it lacked 38 feet of being as high as it now is. The elephant jaw is in good condition, and this indicates that the animal died near the spot.

Coleman (op. cit., p. 352) stated that afterwards a railroad cut had been made across the southern end of the bar, exposing 30 feet of coarse stratified gravel, followed below by 2 feet of brown clay (evidently an old soil) and 8 feet of blue till. In the old soil were found quantities of decayed wood, as well as bones of mammoth and other animals. About a mile farther west, pits were opened for clay, sand, and gravel. Coleman gives the following geological section at this place. The column at the right gives the heights above the lake level.

feet. feet. Clay making red brick 6 78 Gravel 30 72 White sand 5 42 Hard pan 4 37 White sand with mammoth tusks and bones 33 Covered to level of the bay 0

The mammoth tusks and bones were not water-worn. It will be observed that they were found 83 feet below the top of the Iroquois beach (116 feet above the present lake), while the jaw was only about 45 feet below the beach. Both Coleman, as cited, and Fairchild (Bull. Geol. Soc. Amer., vol. XXVII, p. 247) regard the formation of the bar at Hamilton as showing that during Iroquois times the lake became flooded to a height of about 82 feet.

Besides the interglacial species found at Toronto, which have already been mentioned, there may be noted a tooth of Elephas primigenius (p. 130), a cast of which was reported by Winchell. Whether this was derived from interglacial or late Wisconsin beds is not known. Coleman, as elsewhere cited, reported the finding of remains of one of the elephants on the Iroquois beach. On the same beach have been collected antlers of reindeer (p. 244). These animals must have lived there not earlier than the time when that beach was forming, perhaps later.

In a buried gorge extending in a northwestern direction from the whirlpool at Niagara to the Niagara escarpment, Dr. J. W. Spencer (Bull. Geol. Amer., vol. XXI, p. 433) has discovered what he regards as deposits equivalent to the Toronto formation, while older glacial and interglacial beds are found below and more recent ones above. No fossils were met with except wood. At Amaranth have been secured considerable parts of a skeleton of Elephas primigenius (p. 130). This elephant must have existed rather late in the Wisconsin stage. About Kingston in Frontenac County, at two places, have been secured remains of the elk (p. 235), but lack of details as to places and conditions precludes certainty as to their geological age. The fact that they were found in shell marl is favorable to the idea that they belonged to the Pleistocene. Here may be mentioned again the bison horn of uncertain geological age which was found on the north shore of Nipissing Lake (p. 266). In Algoma County, on the banks of Moose River, was found a part of a skull of a mastodon, but there is uncertainty whether it had been buried in interglacial deposits or in marine Champlain beds. The region in the extreme eastern end of Ontario is interesting because it furnishes a considerable fauna belonging to the Champlain stage. During the last glacial stage the region on which the Wisconsin ice-sheet was resting became depressed to such an extent that when this ice retreated beyond the St. Lawrence River, marine waters occupied the basin nearly to the eastern end of Lake Ontario and Ottawa River as far as Lake Coulonge. Coleman’s figure of the region (Bull. Geol. Soc. Amer., vol. XII, pp. 129–146, fig. 1) is here reproduced (fig. 4) to show the western limits of the marine waters, so far as known, and the corresponding fresh-water beach along the north shore of Lake Ontario. Figure 5 from Coleman shows how the Champlain Sea was limited on the south. Marine fossils, especially mollusks, have been found along the upper St. Lawrence as far as Brockville, Quebec, and on the opposite side of the river, in New York. On Coleman’s map the present elevations of the old beaches at important localities are marked, that at Ottawa having an elevation of 450 feet and at Coulonge 370 feet. According to Johnston, who has described the Pleistocene geology in the vicinity of Ottawa (Mem. 101, Canad. Dept. Mines, 1917), there is a point about 8 miles northwest of the city where a marine terrace is found at a height of 690 feet above sea-level. The marine beds at Ottawa are divided into the Leda clays at the base and Saxicava sands above. The former have a maximum thickness of about 200 feet, the Saxicava sands, a thickness of about 40 feet. The fossils occur mostly in the Leda clays. In 1897, Dr. H. M. Ami (Ottawa Naturalist, vol. XI, pp. 20–26), and again in 1901 (Geol. Surv. Ann. Rep., XII, G, pp. 51–56), published lists of the fossils found in the Ottawa Valley, nearly all of them in the vicinity of Ottawa. There were listed 26 species of plants, about 13 species of marine mollusks, and the following vertebrates:

Mallotus villosus, capelin. Cyclopterus lumpus, lump-sucker. Osmerus mordax, smelt. Artediellus atlanticus (Cottus uncinatus), sculpin. Gasterosteus aculeatus, stickleback. Phoca vitulina, common seal (p. 22). Phoca grœnlandica, Greenland seal (p. 23). Tamias striatus, chipmunk.

The aquatic forms are all species existing in the Gulf of St. Lawrence and along the northern Atlantic coast. The chipmunk lives at Ottawa. Specimens of feathers of birds also have been found in nodules, but the species have not been determined. The remains of the chipmunk were probably washed in by some fresh-water stream.

According to Johnston’s paper just cited, there are deposits of glacial drift underlying the marine Champlain beds, but they have furnished no fossils. The marine deposits extend up the Ottawa Valley at least as far as Coulonge Lake, and here has been found Mallotus villosus. At Welshe’s, 3 miles north of Smith’s Falls, Lanark County, have been found some remains of the humpback whale, Megaptera boöps (Dawson, Amer. Jour. Sci., vol. XXV, 1883, p. 200). It was met with (p. 17) at an elevation of 440 feet above present sea-level. It appears to have been left there during the time when the Saxacava sands and gravels were being laid down (Coleman, Bull. Geol. Soc. Amer., vol. XII, p. 133).

QUEBEC.

The Pleistocene of Quebec was described by Logan in 1863 (Geol. Canada, pp. 917–926) and by J. W. Dawson, 1894, in his “Canadian Ice Age.” Dawson divided the epoch, as represented in Canada, into the early Pleistocene, the mid-Pleistocene, and the later Pleistocene. He did not accept the glacial theory as it is now understood, admitting only great local glaciers. His early Pleistocene deposits embraced the great bulk of the boulder clays. His mid-Pleistocene represents an interglacial period, during which were deposited the marine Leda clays, Saxicava sands, and their fresh-water equivalents. The climate was supposed to be milder than at present. During the later Pleistocene there was to some extent a recurrence of local glaciation and of deposition of boulder clay. This stage was followed, according to Dawson, by the Early Modern, which he regarded as the age of the mammoth and mastodon.

Mr. J. Stansfield has described with some detail the Pleistocene and Recent deposits of the island of Montreal (Mem. 73, Geol. Surv. Canada, 1915). The boulder clay is of variable thickness and does not appear to be divisible into beds of different epochs. The Leda and Saxicava deposits are present. When the latter were laid down the region about Montreal was depressed about 600 feet below its present elevation. This has been confirmed by Goldthwait (Summary Rep. for 1913, p. 211). Later it began to rise; and Stansfield thinks that when the elevation had reached about 100 feet less than that of the present the water of the St. Lawrence at that point had become fresh. He found some apparent evidences of a recurrence of glaciation after the Champlain stage, but, on the whole, left the question undecided. He published a list of about 85 species of marine invertebrate fossils, collected from the Leda clay about Montreal, and 22 species obtained from the Saxicava sands. Besides the invertebrates secured from the Leda clays at that place, there are two vertebrates, Phoca grœnlandica (p. 22) and Delphinapterus leucas, or D. vermontana (p. 18). At Rivière du Loup, in Temiscouata County, whale remains were reported in 1894 (p. 18), which were thought to belong to Delphinapterus leucas. At Metis, Rimouski County, a jawbone of a whale has been discovered in the shelly marl of the lower terrace (p. 19); whether or not it belonged to Megaptera boöps is not certain. The specimen of the former species was described by Leidy in 1856.

According to Logan’s report of 1863 (Geol. Canada, p. 920), the single bone was found in a brickyard. At the same place was found some vertebræ of the whale. At Bic, Rimouski County, has been found a nearly complete skeleton of a walrus, at an elevation of more than 100 feet (p. 21). Dawson (Canadian Record Sci., 1895, vol. VI, p. 352) described a nearly complete skeleton of the whale which had been found at Montreal in the Leda clay, 22 feet below the surface. This Leda clay was supposed by Dawson to have been deposited at a depth of from 50 to 80 fathoms, which depth, he said, corresponded approximately to the marine shore-lines at Montreal at an elevation of about 470 feet above sea-level, and to the sea-beach at Smith’s Falls, above referred to. Hence at the time that the whale was buried the mountain at Montreal was only a rocky islet in the sea which prevailed then over the region from the Laurentian hills on the north to the highlands of Quebec, south of the St. Lawrence.

At Tétreauville, in Ottawa County, on Ottawa River, have been found some bones, supposed to belong to the harbor seal, Phoca vitulina.

NEW BRUNSWICK, NOVA SCOTIA, AND CAPE BRETON ISLAND.

All three of these regions were involved in the glaciation of the Wisconsin stage. According to Goldthwait (Summary Rep. for 1913, pp. 244–250), New Brunswick was the center from which the ice flowed out over the other two lands. From this center it moved southward over the western end of Nova Scotia, more and more southeastward over the rest of the peninsula, while over Cape Breton Island the direction was eastward and northeastward. Some indications were observed of an earlier glaciation. As regards post-glacial submergence, Goldthwait found that at St. John, New Brunswick, this had amounted to about 190 feet, while on Cape Breton Island no signs of any submergence were found. Robert Chalmers had arrived at similar conclusions; and these agree well with the theoretical isobases drawn by Taylor for that region (Monogr. U. S. Geol. Surv. LIII, 1915, p. 503). G. F. Matthew in 1879 (Geol. Surv. Canada, Rep. for 1877–78, EE, pp. 1–36) described the geology of southern New Brunswick. Few fossil vertebrates of Pleistocene age have been discovered in these countries. On Cape Breton Island mastodon remains have been found in two places, Middle River and Baddeck (p. 46). As long ago as 1874 remains supposed to belong to Delphinapterus were found near the mouth of the Jaquet River, in the northernmost part of New Brunswick; but Professor G. H. Perkins has shown that the animal was probably the narwhal, Monodon monoceros. The discovery is discussed here on page 19. At the southern extremity of New Brunswick, along Mace’s Bay, Charlotte County, a jaw supposed to belong to a species of Delphinapterus was found, which had been buried in the Leda clay (p. 19). Near Fairville, at the mouth of St. John River, there has been discovered some bones of the seal Phoca grœnlandica (p. 21). In the Academy of Sciences at Philadelphia is a skull of a walrus (p. 21) found apparently in the water near Sable Island about 50 years ago. It is not certain that it is a Pleistocene fossil.

NEW ENGLAND.

Inasmuch as relatively few vertebrates belonging to the Pleistocene have been discovered in the New England States, it will not be necessary to enter into details regarding the geology of the glacial period in this region. Nevertheless, the subject is one of great interest and one which has engaged the attention of many geologists. For those who wish to enter on the study, the writer recommends first a paper written in 1906 (Bull. Geol. Soc. Amer., vol. XVIII, pp. 505–556) by Frederick G. Clapp, entitled “Complexity of the Glacial Period in Northeastern New England,” which gives a brief history of the development of the idea that in the region mentioned there are evidences of more than one glacial and of more than one interglacial stage. There are also citations of the principal papers written on the subject. Among the writers cited are Shaler, Woodworth, Fuller, Upham, Stone, and Tarr. Clapp concluded that New England had been invaded by at least three ice-sheets and that these invasions had been separated by two interglacial intervals of long duration. On account of the greater thickness of the drift and because of fewer favorable exposures, due to the rocky nature of the coast and other causes, many difficulties are encountered in studying the deposits. He regarded absolute correlations as not yet possible. The last glaciation he accepted as corresponding closely with the Wisconsin, as displayed in States further west. What is known as Montauk drift, forming a part of the Gay Head interval of Woodworth, appeared to Clapp to correspond possibly to the Illinoian. Still older drifts would seem to have their place nearer the pre-Kansan (Nebraskan) than to the Kansan. What have been called “Leda clays” are found from Boston north into the St. Lawrence Valley. Clapp divides them into the “high-level” and the “low-level” clays. The former are the older and regarded as being about the equivalent to the Iowan stage. The “low-level clays” are referred to the Wisconsin stage. Another body of clays named by Fuller (Bull. Geol. Soc. Amer., vol. XVI, p. 375) the Gardiner clays, from their type locality, Gardiner Island, near the east end of Long Island, lies beneath the Montauk till and has been referred by Fuller to the Yarmouth interglacial.

In his paper cited Clapp presents (pp. 520–523) a list of the fossils, mostly mollusks, which have been collected in the Pleistocene deposits from New Brunswick to New York.

Along the New England coast are evidences of uplift which followed the retirement of the Wisconsin ice. Katz (Jour. Washington Acad. Sci., vol. VIII, 1918, p. 410) reported elevations of 155 feet at Stratham, New Hampshire, and 300 feet at Pawnal, Maine. Fairchild (Bull. Geol. Soc. Amer., vol. XXIX, p. 214) records the elevations at various localities in Maine.

A brief interesting account of the Pleistocene epoch as recorded in Massachusetts and Rhode Island may be found in an article by B. K. Emerson (Bull. U. S. Geol. Surv., No. 597, pp. 134–149). It deals in part with the geology of the valley of the Connecticut River.

Goldthwait (Appalachia, vol. XIII, pp. 1–23) and Foshay (Amer. Jour. Sci., ser. 4, vol. XXXVIII, pp. 345–348) have found evidences of an early Pleistocene glaciation in the White Mountains of New Hampshire.

Vermont is interesting especially on account of the Pleistocene history of Lake Champlain. This history has been recently discussed by Professor H. L. Fairchild (Rep. State Geologist Vermont, vol. X, 1916, pp. 1–41, with maps and views), who presents (pp. 40–411) a list, 37 in number, of the more important papers relating to the subject.

While the Wisconsin ice-sheet was resting upon Canada and the northern part of the United States, the land thus occupied, and probably a considerable area beyond the ice, became depressed. The valleys of the St. Lawrence, the Ottawa, the Hudson, and the Connecticut had been pressed down to such an extent that, as the ice-sheet retired these valleys became filled with water standing at sea-level. When at length the glacial front had retreated beyond the St. Lawrence, sea-water entered Lake Ontario and passed up Ottawa River far above the city of Ottawa (Leverett, Monogr. U. S. Geol. Surv., LIII, plate XXI). South of the St. Lawrence, marine waters occupied what is now Lake Champlain and as much of the surrounding land as was then at or below sea-level. In his account Fairchild makes use of the plate which is here reproduced (map 31) from his article of 1917 (Bull. Geol. Soc. Amer., vol. XXVIII, p. 279, plate XI). This geologist believes that the Hudson formed for a while a connection with Lake Champlain, although the Hudson waters may not have been actually saline. But in Lake Champlain the presence of fossil marine mollusks and at least one whale skeleton shows that its waters were salt. The lines crossing the plate obliquely are the isobases which show the amount of elevation which has taken place along those lines since the end of the Pleistocene. South of New York City this is zero. At the northern end of Lake Champlain the elevation is 800 feet. This means that the north end of the lake for a while stood 800 feet lower than now. Marine fossils have, however, been found at an elevation of only about 300 feet. The waters which first occupied the lake and stood at the highest level were of glacial origin and fresh. When the ice-front had receded so as to open the St. Lawrence and admit sea-water, the northern end of the lake had been uplifted about 500 feet. It was then that the marine animals entered.

Other important papers to be consulted in this connection are as follows: One by J. B. Woodworth (Bull. 84 New York State Mus.); one by Charles E. Peet (Jour. Geol., vol. XII, 1904, pp. 415–469; 617–660), and two by Professor Fairchild (Bulls. 105, 127, New York State Mus.).

It is proper to say that certain glacial geologists maintain that the depression in the New England States has been less than supposed by Fairchild, and that the isobases curved around toward the north as the New England coast was approached, somewhat as represented by Taylor (Monogr. LIII, U. S. Geol. Surv., p. 503). Fairchild, in a later paper (Bull. Geol. Soc. Amer., vol. XXIX, 1918, pp. 187–244), has reached the same conclusion and presented a map on which are drawn the isobases, or lines passing through points affected by the same amount of post-glacial uplift; from this map 32 has been prepared. On his map the location of the heavy or solid lines is regarded by Fairchild as being based on clear evidence. Where the lines become thin the evidence is less trustworthy; where the lines are broken their positions are hypothetical. The numerals on the lines show the amount of uplift along those lines. Two points of importance are brought out on the map. The first is that Newfoundland formed an independent center of glaciation and of subsequent uplift, a conclusion based on good geological evidence. The second point is that the center of the Wisconsin glaciation was located southeast of James Bay, considerably farther south and west than is usually supposed. The confirmation of this is left to the future.

It does not seem to have been demonstrated that there are in Connecticut any Pleistocene deposits older than those laid down by the Wisconsin ice-sheet. In case Fuller (U. S. Geol. Surv. Prof. Paper 82) is correct in his determination of beds of the early, middle, and late Pleistocene on Long Island, it is to be expected that beds of corresponding ages will yet be recognized in Connecticut. Woodworth (17th Ann. Rep. U. S. Geol. Surv., pt. 1, p. 978) mentions deposits of clay at Berlin and at New Haven that may be older than the Wisconsin.

While the correlations recorded above of the Pleistocene of the New England States with the glacial and interglacial stages of the Mississippi Valley may be subject to modifications, it is interesting to learn that the presence of Middle and Early Pleistocene deposits in the Eastern States has received the recognition of so many students of glacial geology. The hope is awakened that in New England there may yet be found interglacial deposits which will furnish remains of Pleistocene vertebrates, as these have come to light from Throg’s Neck, New York, to southern Florida. It is possible that the astragalus of an equine animal (p. 183), found at Gay Head, Martha’s Vineyard, belongs to a species of Equus of early Pleistocene age.

In order to illustrate still further the events connected with the history of the Pleistocene in the region of the Great Lakes, three additional figures are introduced. One of these (map 33) shows J. W. Spencer’s conception of the drainage of the region in preglacial times. The areas now occupied by the lakes were then traversed by rivers. It will be observed that the rivers above Pittsburgh now discharging into the Ohio then emptied northward into the Erigan. This is shown also by a map (fig. 6) taken from Leverett (U. S. Geol. Surv. Monogr. XLI, p. 89). Figure 5, on page 287, shows the position of the shore of this Champlain Sea.

The number of Pleistocene vertebrates found in the New England States is limited, and most of them have been mentioned.

Somewhere on the coast of Maine have been found specimens of the fish Mallotus villosus (Gould, Proc. Bost. Soc. Nat. Hist., vol. III, 1848, p. 67). At Charlotte, Vermont, a white whale, Delphinapterus vermontanus, was found many years ago (p. 19). Some bovid teeth were found many years ago at Gardiner, Maine, and referred to Bison bison, but it is now believed that they are teeth of the domestic ox. However, Dr. G. M. Allen has reported from Cape Cod, Massachusetts, teeth of a young bison (p. 266). At Woodbury, Washington County, Vermont, at a depth of 7 feet, an antler and a piece of the upper jaw with five molars of Rangifer caribou (p. 244) have been discovered (Rep. Geol. Surv. Vermont, vol VI, p. 7). Mastodons have been discovered in Massachusetts at Coleraine and Shrewsbury (p. 47). Many years ago a tooth and a tusk and some bones of an elephant were found at Mount Holly, Vermont (p. 148); the writer refers the animal to Elephas columbi. An undetermined elephant has been found in Vermont at Richmond (p. 167). Walrus remains have been recovered at Addison Point (p. 23), Andrews Island (p. 23), Gardiner (p. 23), and Portland (p. 24), all in Maine; off Portsmouth, New Hampshire (p. 25); and on Martha’s Vineyard, Massachusetts (p. 25). At the latter place a tooth supposed to belong to the hooded seal (p. 26) was found long ago. With respect to the specimens found at this place there is some doubt as to their geological age. With the exception that the reindeer bones (p. 244) found near New Haven may be of pre-Wisconsin age, no Pleistocene vertebrate fossils older than Late Wisconsin appear to have been discovered anywhere in Connecticut. As shown elsewhere (p. 48), there were found long ago at Sharon, Litchfield County, remains which were identified as those of mammoth, but these have since been regarded as those of the common mastodon. Only a single vertebra was preserved.

Mastodons have been found in four other places, Cheshire, New Britain, Bristol, and Farmington (pp. 47, 48). The animals which left their bones at those places certainly lived after the last glacial sheet had withdrawn from the State. As mentioned on page 291, Fairchild has found reasons for believing that, while the Wisconsin ice-sheet was withdrawing from the Hudson and Connecticut Valleys, the whole region was so depressed that these valleys became occupied by water at sea-level. In these waters there were laid down thick deposits which now stand at levels much above tide, varying, in Connecticut, from nearly 200 to about 300 feet. Map 31, reproduced from Professor Fairchild (Bull. Geol. Soc. Amer., vol XXVIII, 1917, plate XI) is intended to show how wide an extent of territory along the Connecticut Valley was then submerged. It is probable that the emergence of these deposits was not accomplished until after the glacier had retired beyond the State.

It will be observed (map 6) that the localities just mentioned, where the mastodons have been found, lie very close to or on the areas covered by the deposits mentioned. The pond in which the Farmington mastodon (fig. 6, No. 3) was buried is in a range of hills which must have stood as an island in the Connecticut inlet. While it is possible that mastodons lived on this island while the land was depressed, it is more likely that they lived there after it had been more or less elevated. Judging from the topographical maps, one may conclude that the mastodons that have been found at Cheshire (fig. 6, No. 1) and New Britain (fig. 6, No. 2) were buried in deposits that overlie those laid down at sea-level. Their time of existence must have been near the end of the Pleistocene. Too little is known about the mastodons reported from Bristol and Sharon to form any definite opinion about the stage of the Pleistocene when they lived; but it was probably after the withdrawal of the last ice-sheet.

NEW YORK.

From the geologist’s point of view there is hardly, if at all, another State which presents for solution more numerous or more interesting problems connected with the Pleistocene than does New York. Among these are the geography and topography of the State at the beginning of the Pleistocene; the number and identity of the glacial stages which affected its surface; the origin and development of the bordering Great Lakes, of the numerous interior lakes, and of the river courses, actual and abandoned. For a knowledge of these one must consult the various reports issued by the Geological Survey of the State; above all, the numerous and instructive papers that have been published by Professor H. L. Fairchild, of the University of Rochester.

For the student of Pleistocene vertebrate palæontology, the State of New York is not so attractive as some others; but it is far from being devoid of interest. Few species of vertebrates of Pleistocene age have been found in its deposits, and these, with one exception, belong to the latest episodes of the last glacial stage. So far as the writer is aware, the following list comprises all of the Pleistocene vertebrates known to have been found within the borders of the State; those marked with an asterisk (*) are now extinct:

*Equus sp. indet (p. 183). *Platygonus compressus (p. 212) Bison bison (pp. 266, 267). Odocoileus virginianus (p. 226). Cervus canadensis (pp. 235, 236). Rangifer caribou? (p. 245). *Mammut americanum (pp. 48–63). *Elephas columbi (p. 149). *Elephas primigenius (pp. 131, 132). Castor canadensis. *Castoroides ohioensis (p. 272).

Deposits of materials belonging to Pleistocene stages older than the Wisconsin are apparently of rare occurrence in the State. If existing they are usually concealed beneath the widely spread Wisconsin drift. On Long Island, Fuller (U. S. Geol. Surv. Prof. Paper 82) has described beds of gravels, sands, and clays, which he regards as belonging to the Nebraskan, Aftonian, Yarmouth, and Illinoian. None of these has furnished any vertebrate fossils. However, in 1866 (Smithson. Contrib. Knowl., vol. XV, art. 3, p. 16), Whittlesey reported that he had a tooth of a horse (p. 183) found at Fort Schuyler, Throg’s Neck, 18 feet below the surface. This must have been lying beneath the Wisconsin drift. Inasmuch as Fuller has found the Manhassett formation, regarded as equivalent to the Illinoian, around Manhassett Bay, within 4 or 5 miles of Throg’s Neck, it seems entirely reasonable to suppose that deposits of similar or earlier age exist at Throg’s Neck.

With the exception of small areas, the whole of the State was at one time covered by the ice-sheet of the Wisconsin stage. The glacial ice filled the basins of the Great Lakes, and overrode even the peaks of the Adirondack and Catskill Mountains. Only along the southern side of Long Island and in the loop formed in Cattaraugus County by Allegheny River does the ice-sheet appear to have been absent.

Nearly everywhere, even on the southern coast of Long Island as outwash, it left its burden of clay, sand, gravel and boulders, usually many feet in thickness; in the mountainous regions this drift material is present, at least in the valleys. At the extreme southern edge of the glacial sheet there was laid down the terminal moraine, which, more or less distinctly determinable, has been traced from the eastern end of Long Island to the southwestern corner of Cattaraugus County, and onward into Pennsylvania. This moraine is shown here on maps 3 and 6–A.

As the ice-sheet withdrew toward the north, the surface which it had occupied was, for many reasons, very uneven, and in the depressions there were formed numerous lakelets and lakes. Into the smaller lakes and ponds especially, were swept, by running water and blown by winds, coarse materials and dust, so that they began at once to fill. Water-loving plants in due time took possession of their borders, and in time marshes were formed. In some of these bodies of waters are now found deposits of shell marl, which show that for a long period the lakes and ponds were inhabited by fresh-water mollusks. Sometimes below this marl, but usually above it, is found a layer of peat, the product of the partial decay of the vegetation. It is in such peat-bogs, sometimes buried in the peat, sometimes in the marl, that have been found most of the bones and teeth of the fossil animals recovered. Inasmuch as such deposits lie upon the Wisconsin drift, it is certain that these animals lived, at the localities where found, after the retirement of the glacier from that locality; how long afterward one usually can not be certain.

It is in such Late Wisconsin deposits that have been found the numerous remains of mastodons on Long Island, on Staten Island, around New York City, and especially in Orange County (pp. 48–54). This county has furnished some of the most complete skeletons of mastodons ever discovered. Whether or not the conditions for their existence were more favorable in this region than in that between this county and the Finger Lake region may be regarded as doubtful; but it is certain that the conditions for the preservation of skeletons were extremely favorable.

A remarkable case is presented at Cohoes, where a part of a skeleton of a mastodon was found in one of the great pot-holes existing there, and another part of the same skeleton in a neighboring pot-hole. The case is discussed below.

In the western half of the State, after the foot of the glacier had retired beyond the divide between the present northward and southward flowing streams, bodies of water began to collect between the divide and the foot of the glacier. To these bodies, regarded as lakes, changing from time to time their dimensions and their outlets, have been given various names. At first, the waters that collected in the Finger Lake region found their outlet southward through the Susquehanna River; later through the Mohawk and Hudson; then westward into the Mississippi drainage; afterward through a channel leading around west and north of the Adirondacks and into Lake Champlain and down the Hudson; and finally, as now, into the St. Lawrence River (map 34).

The waters of the Erie basin, for most of the time, found their outlet toward the west into the Mississippi; but at a later time they escaped for a while eastward through central New York into the Mohawk. For information regarding these lakes one must consult Leverett and Taylor (Monogr. LIII, U. S. Geol. Surv.) and Fairchild (Bulls. 127, 160, N. Y. State Mus.).

From a study of the geological history we may arrive at some approximately correct ideas as to the time when the mastodons, elephants, horses, giant beavers, etc., lived within the limits of the State. Of these animals, apparently none of the specimens discovered up to this time belongs to any pre-Wisconsin stage, except the horse whose tooth was found at Throg’s Neck (p. 183). The history of our extinct horses and the depth at which the specimen was found indicate that the animal had lived either during the first or the second third of the Pleistocene.

We may be certain that none of the mastodons (p. 49) which have been reported from Long Island lived there while the northern border was occupied by the glacier, and the remainder by the ocean. Not until the land had risen to about its present level could mastodons have become buried in the muck-filled ponds where they have been met with. Where the glacier front was when mastodons got foothold on the island we can not tell certainly; but it required perhaps hundreds or probably thousands of years for the elevation of the island to the extent of about 100 feet. We can hardly doubt that the mastodon lived on up to near, possibly into, the Recent period (see map 34).

It is interesting to speculate on the time and manner of entombment of the skeleton, described on page 56, which was found at Cohoes, part in one pot-hole, part in another not far away. Hall adopted the theory that the carcass of the mastodon had been frozen in the glacial ice and, on the thawing of this ice, had been dropped into the pot-holes. In fact, he thus explained the frequent presence of mastodon skeletons in swamps. We have, however, no evidence that mastodons were ever thus frozen up in the ice of the glacier; but there is a possibility that this happened sometimes. If a skeleton should thus have been engaged in the moving stream of ice it is not probable that it would ever have emerged in a recognizable condition. In the production of cracks and crevices in the glacial ice, of which Hall spoke, the bones would have been broken up and scattered, if not ground to powder. If a cadaver had been frozen in the ice for any considerable time it would certainly have come out in such a waterlogged condition that it would hardly have floated. Weighted down by its heavy tusks, it would have drifted against rocks and at least the tusks would probably have been broken off. If we exclude the idea that the mastodon had first been frozen in the glacier, the writer sees no reason for denying that it might thus have been transported for some distance; but little is gained by granting it. The animal could as well have lived near Cohoes as farther up the Mohawk.

As stated on another page, James Hall concluded that the pot-holes belonged to some preglacial time. Professor H. L. Fairchild has expressed in a letter to the present writer the following opinion:

“When the ice-sheet melted from Cohoes the locality was 355 feet lower than it is to-day. Deep estuary deposits partially filled the Hudson Valley and buried the Cohoes district. The Mohawk channel at Cohoes is excavated through marine sediments. There is no suggestion of any river channel there previous to the present river work. The pot-holes are post-glacial, but they probably represent a more copious and vigorous flow than that of the present river. That was supplied by the diminishing Iromohawk, the latest outflow through the Mohawk Valley of the Iroquois water. In this view the pot-holes were drilled by the latest glacial waters.”

It appears that, when the mastodon skeleton fell into the pot-holes, these had been drilled long before; for the principal one had become filled with gravel to a depth of at least 10 feet. They were, therefore, probably well above the stream-level, except in times of high-water. However the carcass reached the locality, it must have arrived in a complete state. Had it already attained an advanced stage of decay, some limbs or the feet or the lower jaw, probably the whole head, weighted down as it was by the heavy tusks, would have dropped off. It may be assumed that the skeleton was lying on land or in some pond not far above the pot-holes. The flesh was not wholly decayed, and the bones were held together by the ligaments. While the skeleton was in this condition the river rose and swept it over the first pot-hole, where the right leg dropped off; and then onward over the second, where more of it was deposited. Some unimportant parts may have been carried farther, and some of the missing bones may have decayed in the pot-holes. After the bones were deposited there the pot-holes became slowly filled up, probably mostly during times of high-water, with muck and branches and trunks of trees of several species (Hay, Science, n. s., vol. XLIX, 1919, p. 378).

The retreat of the Wisconsin ice-sheet far beyond the St. Lawrence and the rise of the land to its present elevation, 350 feet above the sea at Cohoes, belong to the closing chapter of Pleistocene history. When the Cohoes mastodon was buried the ice-sheet was probably already north of the St. Lawrence and, as Professor Fairchild writes, 150 feet of the rise of the land had already occurred. The time could, therefore, not have been long before the beginning of the Recent epoch. If these animals lived at such a late time at Cohoes they doubtless existed at the same time in all parts of the eastern region where their remains have been discovered. They may have been able to occupy Long Island a little earlier than places further north, but the interval would be geologically inconsiderable.

The writer has learned of no discoveries of mastodon bones in materials laid down by the marine waters that occupied Lake Champlain, the St. Lawrence Valley, and that of Ottawa River, or in deposits overlying these marine beds.

On the basis of one of Professor H. L. Fairchild’s plates (Bull. 127, N. Y. State Mus., plate XXXV) the writer has prepared map 34, which is intended to show the position of the Wisconsin ice-sheet in New York after it had retired somewhat north of the divide. This divide is marked by a line of dots. The area then occupied by the ice is stippled. Lake Erie was already nearly free from ice and was discharging its water by way of the Mississippi. Impounded waters from the melting glacial ice were collecting in the region of the Finger Lakes, forming Newberry Lake, and escaping down the Susquehanna. The Mohawk afforded outlet for the water from the southeastern lobe of ice. Fairchild’s plates 36 to 42 show the successive positions occupied by the ice-front as it retired northward and the various lakes that were formed.

Although not many species of vertebrate animals have been found in the Pleistocene deposits of New York, a large number of localities have furnished remains of the mastodon, Mammut americanum. These localities are recorded and brief descriptions of the remains and their geological environment have been presented on pages 48–63. The localities are indicated on map 34. It will be seen that several specimens have been found on Long Island and many in Orange County, in the southeastern corner of the State. In the western half of the State most of the finds occur within the area once occupied by the successive lakes. The animals could have lived there only after the ice-sheet and the lake waters had disappeared. It will be seen that a few finds have been made close to the shores of the present lakes. The animals must have lived there at the very end of the Pleistocene, if not within the Recent epoch.

The finds of other vertebrates are recorded on the following pages: Equus sp. indet. on page 183; Platygonus compressus on page 212; Bison bison on page 266; Odocoileus virginianus on page 226; Cervus canadensis on page 235; Rangifer caribou on page 245; Elephas columbi on page 149; Elephas primigenius on page 131; Castor canadensis on page 272; Castoroides ohioensis on page 272.

In 1850 (Proc. Amer. Assoc. Adv. Sci., vol. II, pp. 255–256), W. C. Redfield reported that he had received remains of a fox of the genus Vulpes from Gulf Summit, Broome County. The lower jaw and other bones had been discovered in a cutting of the New York and Erie Railroad, 40 feet below the natural surface. The deposit above these bones was evidently the Wisconsin drift. The fine clay inclosing the bones may have belonged to the Sangamon, or even some older interglacial deposit. It is impossible to say whether this fox was Vulpes fulvus or Urocyon cinereoargenteus.

NEW JERSEY.

(Map 6–A.)

In the consideration of the problems of Pleistocene geology and palæontology, New Jersey is one of the most important States. Its northern part is occupied by glacial drift deposits, while the southern two-thirds is covered more or less completely by materials laid down beyond the limits of the glaciers. The glacial materials appear to belong to two widely separate epochs. The geologists who have been connected with the geological survey of New Jersey recognize in the materials composing the Pleistocene deposits south of the glacial region three formations, the Bridgeton, oldest; succeeded by the Pensauken; and the Cape May, the youngest. The geologists of Maryland recognize in New Jersey three formations which correspond to the three of Maryland, the Sunderland, the Wicomico, and the Talbot. However, the author of the Maryland Pliocene and Pleistocene volume, Professor Shattuck, insists that parts of Salisbury’s Bridgeton, Pensauken, and Cape May all enter into the Sunderland; parts of the Cape May, Pensauken, and possibly of the Bridgeton, into the Wicomico; and parts of the Pensauken and Cape May into the Talbot.

There are wide divergences in the views of the two groups of geologists regarding the manner in which the materials have been laid down. The Maryland geologists hold that their three terraces represent three epochs of submergence, and that the gravels, sands, and clays were deposited in the salt waters of the ocean or of estuaries. Salisbury and Knapp (Geol. Surv. New Jersey, vol. VIII, 1917, p. 3) adopt the view that the formations are partly of subaerial and partly of marine and estuarine origin, with emphasis on the subaerial mode. Of the Bridgeton, the authors referred to say (their p. 18 ) that the accessible parts are primarily of terrestrial origin. A part of what remains may be marine or estuarine, and part of what has been removed may have been so. No palæontological evidences of marine deposits of this epoch are found in the State. The writer records his dissent from the theory that the terraces and the deposits called the Sunderland, Wicomico, and Talbot have been the product of marine submergence. A part only of the Talbot can be referred to deposition in the sea.

Of the Pensauken, Salisbury and Knapp say (p. 87): “There is nothing in its constitution to negative the hypothesis of the whole formation being river work; nor is there anything, as now understood, to prove it.” As to the deposits which they refer to the Cape May, the authors quoted say (p. 162) that the southern part of the State seems to have stood a few feet (30 to 50) lower than at present; but that it could not have stood long at this height, for sea-cliffs are essentially wanting. At one point, near Millville, Cumberland County, marine fossils are met with at an elevation of about 10 feet above tide.

The Cape May was, according to Salisbury and Knapp, laid down during the last glacial epoch, the Wisconsin (p. 162). This determination of age would doubtless gain the acceptance of the Maryland geologists and their adherents, although the latter would include under this name many local deposits which Salisbury puts in the Pensauken.

It is remarkable that, so far as the writer knows, no remains of Pleistocene vertebrates have ever been discovered in that portion of New Jersey which is mapped as occupied by the Cohansey sands, an area including nearly half the State. It lies southeast of a straight line which would run from Navesink River to Salem. The reason for this lack of fossil vertebrates does not occur to the writer. A large portion of this region is mapped as being covered with deposits of all three of the Pleistocene formations, Bridgeton, Pensauken, and Cape May. On or near to the line of outcrop of the Cretaceous deposits from Salem to Raritan Bay, not fewer than ten localities are known where mastodon remains have been discovered, besides two localities which have furnished horses and two which have furnished elephants. Since the southeastern part of the State has yielded no vertebrate fossils and little else to throw light on the age of its deposits, we shall dismiss it from consideration.

The glacial geology of the State has been studied by Professor Rollin D. Salisbury, of the University of Chicago, and his assistants, Henry B. Kümmel, Charles E. Peet, and George N. Knapp. The results of their studies on the glacial-drift deposits have been published in volume v of the final report of the State geologist, 1902.

The Quaternary formations of the southern part of the State are described in volume VIII of the final report. A more succinct description of the events of the Quaternary period is found in Bulletin 14 (1915) of the New Jersey Survey. The authors are J. Volney Lewis and Henry B. Kümmel.

In the vicinity of Perth Amboy is a heavy glacial moraine which may be traced eastward through Staten and Long Islands. West of Perth Amboy it turns northward, and swinging around it reaches Springfield. Thence it runs northwestward to Rockaway, and continues west by south to Delaware River, at Belvidere. This moraine marks, in New Jersey, the southward limit of the last ice-sheet, the Wisconsin. All the drift deposits of the State north of this moraine are regarded as belonging to the Wisconsin stage. It is to be supposed that this is, at least to some extent, underlain by older drift deposits.

South of the moraine just described are scattered deposits of glacial drift and other evidence of glacial action which are referred to a much older ice-sheet, one supposed to correspond to the Kansan drift of the Mississippi Valley (Salisbury, Geol. Surv. New Jersey, vol. V, p. 781). On the other hand, it is sometimes referred (Chamberlin and Salisbury, Geology, vol. III, pp. 383, 384) to the first glacial (sub-Aftonian).

As has been said, three formations are recognized which were laid down otherwise than by glacial ice-sheets, the Bridgeton, the Pensauken, and the Cape May. The deposition of the Cape May is regarded as being contemporaneous with the Wisconsin ice-sheet (Salisbury and Knapp, New Jersey Geol. Surv., vol. VIII, p. 162; Lewis and Kümmel, Bull. 14, p. 120). The Pensauken formation is believed to be much older than the Cape May; it may (Salisbury and Knapp, op. cit., p. 78) be older than the extra-morainic drift, mentioned above as being of about Kansan times; but it may have coincided in part only with the Kansan. According to Lewis and Kümmel (op. cit., p. 111) the old, extra-morainic, Jerseyan drift was coincident with at least the later stages of the Pensauken. Hence, we may believe that the Pensauken corresponds somewhat to the Aftonian stage of Iowa. The Bridgeton formation is still older than the Pensauken and, being Quaternary, must be referred either to the early part of the first interglacial or to the first glacial; but the New Jersey geologists are not specific on this point.

It is unfortunate that nowhere in New Jersey has any considerable number of species of Pleistocene vertebrates been found buried together. We are thus deprived of one means of estimating the age of the species and of the beds. Most of the specimens found, as the mastodon and the two elephants, belong to species which lived during the whole or a large part of the Pleistocene and hence do not testify definitely to the age of the deposits in which they occur. Too often the information we have regarding the place and conditions of burial is extremely meager.

In Salem County a mastodon has been found in Mannington Township, at Chestnut Hill (p. 63); and a deer, probably Odocoileus virginianus, at Woodstown (p. 226). Although the geological map shows that in Mannington Township Cape May Pleistocene prevails, while about Woodstown there is Pensauken, one can not well conclude that the animals are of corresponding age.

In Gloucester County Mammut americanum has been found at Harrisonville (p. 63), Mullica Hill (p. 64), and Woodbury (p. 64); Equus at Swedesboro (p. 184). As to the former species, we can not be certain of the age, either from our knowledge of the age of the deposits inclosing the remains or from the history of the species. As to the horse found at Swedesboro, one may, from the history of the genus in this country, arrive at some conclusion; but this will be deferred to page 303.

In Camden County, so far as the writer has knowledge, no vertebrate remains have been found except in the Fish House beds, along Delaware River, just above Camden; but the horse remains (p. 184) are of great importance. These beds were originally supposed to be of Cretaceous age, but in 1869 (Trans. Amer. Philos. Soc., vol. XIV, p. 250), Cope expressed the conviction that they belonged to the Pliocene period. He presented a geological section (fig. 7) of the beds which shows a thin stratum of soil above, then from 8 to 15 feet of light-brown sand, followed below by a blackish clay about 25 feet in thickness. Near the bottom of the latter was found a layer containing shells of several species of Unio and Anodonta. Just above this bed of unios there was discovered a large part of a skull of an extinct horse which Cope referred to Equus fraternus. This was deposited in the collection of the Academy at Philadelphia, but later disappeared.

In 1897 (Rep. State Geologist, New Jersey, for 1896, pp. 201–247, plates X-XIV) Woolman published a paper on the stratigraphy of the Fish House beds and described and illustrated other horse-teeth which he referred to Equus complicatus. These teeth were found at a depth of 12 feet below the top of the black clay; 6 feet of surface gravels had been removed from the clay. The teeth are now in the collection of the Academy, at Philadelphia. Woolman stated that in the same collection are a patella and a fragment of a long bone of a horse found in the black clay, in 1892.

Woolman regarded the clay in question as belonging to Pensauken times. Salisbury and Knapp (op. cit., p. 104, fig. 49) state that there is here 20 feet of black clay overlying Pensauken sand and that the clay is overlain by Pensauken gravel. If this judgment of the geological age of the clay is correct, the horses probably lived during the first interglacial (Aftonian) or the beginning of the second glacial stage (Kansan). There are, however, those who insist that these Fish House clays belong really to the Cape May formation. This would make the geological age of the horse about that of the Wisconsin drift.

Besides the horse remains, only some bones of a wolf have been found in the clays mentioned, and these too have disappeared. They probably would have thrown little light on the age of the beds. We must reach conclusions from other data.

This fact seems to be pretty certain: Had horses lived at Fish House during the deposition of the Cape May they would (as did the mastodon, Elephas primigenius, and E. columbi) quite certainly have spread out over northern New Jersey and over the grassy plains of New York and Ohio; and their remains would somewhere have been found, as are those of the other species just mentioned, in old swamp and lake deposits overlying the Wisconsin drift; but no horse remains have ever been reported from such deposits. Furthermore, in all the digging that has been done at Trenton, in deposits acknowledged by all to belong to Wisconsin times, no trace has been found of horse remains.

Near the bottom of the Fish House clay bed, just below the level of the horse remains, there is found a layer which contains river clams represented by the genera Unio and Anodonta. Ten species of Unio have been recognized and two of Anodonta. When these were first studied the beds were believed to belong to the Cretaceous. Nevertheless, the close resemblance of the shells to still living species was recognized; and to them were given names differing from those of the related existing forms by the ending oides. The species were described by Lea and Whitfield and have been restudied by Dr. H. A. Pilsbry, of the Academy of Natural Sciences, Philadelphia. The species are probably identical with forms yet living; but half of them no longer exist in the region of Delaware River. Pilsbry (Proc. Acad. Nat. Sci. Phila., 1896, pp. 567–570) stated that five of them have no longer any representatives in the Atlantic drainage south of the St. Lawrence River system. It is probable that these species had, when they lived at Fish House, spread into other rivers south of the Delaware and thus were not trapped in this river by the Wisconsin ice. It seems certain, therefore, that a longer period of time and a longer series of vicissitudes must have intervened to produce such changes in geographical distribution. According to C. T. Simpson’s work, “Descriptive Catalogue of the Naiades,” 1914, Unio (Quadrula) subrotundus now inhabits the Ohio, Cumberland, and Tennessee Rivers; U. (Lampsilis) anodontoides occupies the Mississippi River and Gulf drainage regions; while Anodonta corpulenta is found in the Upper Missouri region. The Wisconsin ice-sheet and the short period of time since its disappearance are hardly sufficient to explain this wide dispersion of species, while others have been able to retain their place in the Delaware.

Opposed to this view regarding the identity of the unios of the Fish House beds, see Ortmann (Proc. Amer. Philos. Soc., vol LII, p. 280, 1913) and Baker (Univ. Ills. Bull., XVII, p. 205, 1920). These writers contend that the species have no especial relationship to western forms. According to Baker the deposits are older than the earliest glacial stage. On the other hand, according to Dr. E. W. Berry (quoted by Baker), who has studied the plants, the beds belong to the late Pleistocene.

We have, then, these reasons for holding that the Fish House clays are of early Pleistocene age: (1) Competent geologists have determined them as belonging to the Pensauken formation, laid down at or before the time of the Kansan stage; (2) the presence of remains of horses, evidences of whose existence during or after the Wisconsin have not been produced; (3) the presence of many species of naiades, some of which yet live in that region, but the majority of which now live only in far-distant regions.

We may confidently conclude that the horse remains which were found at Swedesboro belonged likewise to the Pensauken.

In Burlington County mastodons have been found at Pemberton ( p. 64), but one can not be certain of their geological age. A reindeer has been unearthed at Vincentown (p. 64). It seems highly probable that it lived there while the Wisconsin ice-sheet occupied the northern part of the State; but there is a possibility that it is older. In the Academy of Natural Sciences at Philadelphia are some remains of Odocoileus found at Vincentown (p. 227).

In the vicinity of Trenton, Mercer County, scant remains of six species of Pleistocene mammals have been reported. These are Mammut americanum (p. 64), Elephas primigenius (p. 132), Bison bison (p. 287), Ovibos moschatus (p. 248), Cervus canadensis (p. 237), and Rangifer caribou? (p. 248). All are known to have existed elsewhere during late Pleistocene times, and three indicate a cold climate. The presence of fossil vertebrates here is of special interest because many evidences have been found of man’s occupation of the region in apparently late Pleistocene times.

At and in the vicinity of Trenton are found both Pensauken and Cape May deposits, the latter overlying the former (Salisbury and Knapp, op. cit., pp. 120, 165). The Cape May rises about 60 feet above sea-level. At various places the Pensauken protrudes through the mantle of Cape May and rises to a height of as much as 130 feet above sea-level. Its base is about 20 feet above sea-level. The materials consist of sand, gravel, and cobblestones. So far as the writer knows, no fossils have been found in the Pensauken about Trenton.

The Cape May at Trenton is held to have been laid down principally during the presence of the Wisconsin ice-sheet in the northern part of the State; and naturally it consists mostly of sands, gravels, coarse and fine, and some boulders. In the localities where excavations have been made for sand and gravel for building purposes, for sewers, and for railroads, and in search for relics of man, two principal divisions are recognized. Below are strata of clays, sands, gravels, and boulders which are believed to have been deposited by the floods of varying intensity which issued from the glacial moraine then about 60 miles above Trenton (figs. 8, 9). Over this lies a bed of what is called yellow drift, which reaches a thickness of about 3 feet. It consists mostly of fine sand, but there are many pebbles and occasionally some large boulders. It is everywhere characterized by wavy red bands. While some geologists have held the opinion that this deposit had been produced by winds, it appears to be definitely determined that it was waterlain (Wissler, Scient. Monthly, vol. II, p. 237). This “yellow drift” is overlain by about a foot of black soil which belongs to the Recent epoch and is the result of cultivation by whites. For details regarding the Trenton gravels and the yellow sands above it the reader should consult Ernest Volk’s work, “Archæology of the Delaware Valley” (Papers Peabody Mus., vol. V, 1911).

All the species mentioned above have been reported from the beds known as the Trenton gravels. A femur of a bison was found also in the yellow drift (see p. 287).

Monmouth County has furnished more fossil vertebrates of the Pleistocene than any other county. Mastodons have been discovered at Englishtown, Freehold, Marlboro, Long Branch, Manasquan, and in the Navesink Hills (pp. 65, 66). Many specimens, as those about Freehold and Long Branch and Manasquan, are in such superficial positions in peat that they do not seem to be very old, probably of Cape May age; and yet of this one can not be wholly certain. The discovery of a heel-bone of a megatherium (p. 31) at Long Branch appears to indicate the presence there of early Pleistocene deposits. At Englishtown the remains had apparently become mixed with marl, and they may belong to an older stage of the Pleistocene. In the Navesink Hills, according to Leidy, the mastodon remains were associated with those of an extinct horse (p. 184). If so, both species probably were buried in Pensauken deposits. In this same region there was found long ago a tooth of Elephas columbi (p. 149); but it is useless to speculate on its geological age. At Long Branch (p. 26), damaged skulls of walruses, probably of the existing species, have been met with. It seems natural to associate this southward migration, which extends to South Carolina, with the Wisconsin epoch; but it is possible that it was earlier. At Deal (p. 227) have been found remains of a deer, probably Odocoileus virginianus.

Somewhere about Shark River, a tooth of a peccary (p. 213) was found, as was supposed, in Miocene marl. Leidy could not distinguish this tooth from that of Mylohyus nasutus. So far as our evidence goes, this species belongs to the early and middle Pleistocene.

Near North Plainfield a tooth was found which is referred to Elephas primigenius (p. 133). The locality is very close to the moraine of the Wisconsin ice-sheet, and the animal probably lived there when the Plainfield outwash plain (Salisbury, Geol. Surv. New Jersey, vol. V, 1902, p. 738) was being laid down.

Near Schooley’s Mountain, but west of Musconetcong River and in Warren County, remains of a mastodon (p. 67) were encountered in excavating the Morris Canal. It is probable that these were buried in a swamp left over from the Wisconsin times; but Lewis and Kümmel’s map of 1910–1912 indicate in this region only drift older than the Wisconsin.

The mastodons found at Hackettstown and Hope, in Warren County, are probably of Late Wisconsin origin (pp. 67, 68).

Near Mount Hermon, about 5 miles northeast from Delaware, in Warren County, and about 2 miles northwest of Hope, was found the splendid skeleton of the moose Cervalces scotti, which forms one of the treasures of Princeton University (Scott, Proc. Acad. Nat. Sci. Phila., 1885, p. 174). It was discovered in a bog. All this region is (Salisbury, Geol. Surv. New Jersey, vol. VIII, plate XXVIII) occupied by Wisconsin drift and the bog doubtless rested on this drift. It seems certain, therefore, that this stately relative of our existing moose lived after the disappearance of the Wisconsin ice-sheet.

A mastodon (p. 68) which was found at Greendell in Sussex County quite certainly lived there after the last glacial stage.

Berry (Torreya, vol. X, p. 261) has studied a collection of nine species of plants which had been obtained in peat from near Long Branch. Only three of these now range north of Long Branch. He concluded that the last glacial stage had been followed by a period of climate warmer than the present climate. This is in accord with views which the present writer has held. It ought not, however, to be assumed with too much confidence that the peat-bed is of Late Wisconsin origin.

PENNSYLVANIA.

About half of the area of Pennsylvania lies outside of the region which was glaciated. Figure 10 is a map taken from Folio 172 of the U. S. Geological Survey, published in 1910 and compiled by Dr. W. C. Alden in 1901. A broad strip along the southern part of the State, being non-glaciated, is not represented. The areas shaded by parallel ruling and stippling are those which present evidences of glacial action.

The glaciated area consists of two principal portions. One of these, that subjected to the action of the Wisconsin ice-sheet, is represented on the map by means of oblique parallel lines coming down to an interrupted heavy line. This line, representing the Wisconsin terminal moraine, starts on Delaware River north of Easton, runs northwestward to Potter County, thence into New York, thence back into Pennsylvania, in Warren County, and then enters Ohio north of the Ohio River. The course of this moraine was worked out especially by H. C. Lewis and G. F. Wright and was described in report L of the Pennsylvania Geological Survey, in 1881. The moraine crosses the Delaware at Belvidere, New Jersey, and passes through the following counties: Northampton, Monroe, Carbon, Luzerne, Columbia, Sullivan, Lycoming, Tioga, Potter, Warren, Crawford, Venango, Butler, Lawrence, and Beaver.

South of this moraine are two areas which, on this map, are represented by stippling. These are occupied by drift materials, usually forming a considerably thinner covering, which are believed by most glaciologists to belong to an older Pleistocene stage, probably about as old as the Kansan. Especially in the valleys these older drift deposits may reach thicknesses of 200 or 300 feet. These old glacial deposits are represented also by terraces along the margins of the valleys. Some of these in the vicinity of Warren stand at a height of about 1,400 feet above the sea. Figure 17 is taken from Shaw and Munn (Folio 178, U. S. Geol. Surv., p. 12). The uppermost gravels are supposed to represent the Kansan stage. A few small patches lying in the angle of the unglaciated area are of doubtful age, as indicated on the map. It must be stated, however, that there is some dissent from this conclusion as to the age of this outer drift. Professor E. H. Williams has published a number of papers in which he takes the position that this drift is a deposit laid down by the same ice-sheet that later on built up the Wisconsin moraine (Amer. Jour. Sci., vol. XLVII, 1894, pp. 32–36; Science (n. s.), vol. XXXVII, pp. 447–450; Pennsylvanian Glaciation, first phase, 1917, pp. 1–101). Professor G. F. Wright appears to take the same view. The writer sees no sufficient reason for distrusting the opinions of Dr. Alden and his colleagues.

It must not be assumed that an animal whose remains have been found within the area occupied by the Wisconsin drift lived during or after that stage. Even within this area there may occur fossil-bearing deposits of an older Pleistocene time. These older deposits may underlie the Wisconsin drift or they may occur as old terraces high up on the sides of the valleys of rivers. Cases of the latter kind are found along Allegheny River (Leverett. Monogr. XLI, U. S. Geol. Surv., pp. 229–252; Shaw Jour. Geol., vol. XIX, 1911, pp. 140–156; folio 178, U. S. Geol. Surv., p. 8). On the other hand, an animal of very late Pleistocene age, or even of the Recent, may be buried in deposits which overlie an old Pleistocene deposit. It is necessary, if it can be done, to determine the actual age of the deposit containing the remains; otherwise one must depend on the geological age of the species involved, or be content to wait for further information. Unfortunately, but few of the quadrangles in the glaciated area have had their geological structure studied and reported on. At present the U. S. Geological Survey has published only Folios 92 (Gaines) and 93 (Elkland and Tioga), lying mostly in Tioga County, partly in Potter; also Folio 172 (Warren), occupying a part of Warren County. Information may sometimes be secured from the numerous volumes which have been published by the Geological Survey of Pennsylvania and from articles in the scientific journals.

The Pleistocene deposits which lie outside of the glaciated areas have been mostly laid down along rivers. Some of the materials were transported by the streams which carried away the drainage from the glaciers; in other cases the materials were brought down from the higher lands and laid down along the lower and less sloping parts of the streams. In the unglaciated area many of the quadrangles have been surveyed by the U. S. Geological Survey and the folios aid in determining the age of deposits which contain fossil vertebrates.

Important collections have been made in a few localities, and these will now be considered:

At Pittston, in Luzerne County, on Susquehanna River, have been found teeth of the horse Equus complicatus (p. 184), remains of mastodon (p. 68), and of a musk-ox (p. 248). The presence of the horse makes it evident that the deposit containing the fossils belongs to a stage older than the Wisconsin, although the locality is within the area of the Wisconsin.

We consider now the contents of a cave found near Stroudsburg, Monroe County. The Hartman (or Crystal Hill) Cave was discovered in 1880 and explored first by Mr. T. Dunkin Paret, of Stroudsburg. It was soon afterward examined by Dr. Joseph Leidy, of Philadelphia, and Dr. Thomas C. Porter, of Easton. Leidy published the first description of it in 1880 (Proc. Acad. Nat. Sci. Phila., pp. 346–348) and presented a list of the species of animals which had been secured by Mr. Paret. In 1889 (Ann. Rep. Geol. Surv. Pennsylvania, for 1887, pp. 1–18, plates I, II), a more detailed report was made by Leidy, including descriptions and illustrations of some of the vertebrates and of certain artifacts which had been discovered.

In 1894, Dr. H. C. Mercer made a re-exploration of the cave and gave a more extended description of it (Proc. Acad. Nat. Sci. Phila., pp. 96–104).

Combining the statements of Leidy and Mercer with data obtained from the Delaware Water Gap topographical sheet issued by the U. S. Geological Survey, one finds that the cave is situated on Crystal Hill, about 3.5 miles in a straight line southwest of Stroudsburg and close to the village of Stormville. Crystal Hill is a part of an anticlinal fold, Godfrey Ridge, of the Helderberg limestone. South of the fold runs Cherry Creek; north of it, Mt. Michaels Creek. On the northeast the hill is cut off from the rest of the ridge by a valley about 300 feet deep. Mercer’s account states that the cave is on the top of the hill, about 0.25 mile from Cherry Creek, but the topographical map locates the top of the hill about 0.75 mile away from this stream. Mercer also wrote that the cave was 800 feet above Delaware River, 5 miles away. However, the hill has an elevation of somewhat less than 840 feet above sea-level, while the river at the nearest point is somewhat more than 280 feet above sea-level. Inasmuch as the cave is probably somewhere on the southern slope of the hill, it is about 500 feet above the Delaware and about 300 feet above the bed of Cherry Creek.

The opening of the cave in the rock was wide (Mercer, p. 96, fig. 1), but had become almost wholly choked by débris. Nevertheless, a hole large enough for adventurous boys to enter remained (Leidy, op. cit., 1880, p. 346). After a few feet descent the cave extended nearly horizontally more than 100 feet. It had become filled nearly to the roof by various deposits. Excavations showed that on top was a layer, about a foot, of “black friable earth mingled with animal and vegetal remains” (Leidy). Mercer describes it as a “top layer of limestone roof-splinters and down-slidden outer talus thinning inward into less stony cave earth.” Beneath this layer was a thin stratum of stalagmite. Further digging showed that below this stalagmite flooring the cave was filled to a thickness of as much as 14 feet in one place. This deposit is described by Mercer as being a continuous homogeneous bed of exquisitely fine clay deposited in thin laminæ rarely sprinkled with sand pockets and underlain with a thin film of sand. Neither in this deposit nor in the stalagmite was there found a trace of any formerly living thing. All the remains of animals and all the artifacts were discovered in the uppermost layer.

It should be noted at this point that this cave is situated about 5 or 6 miles north of the Wisconsin moraine.

The following is a list of the species of vertebrates identified by Leidy. When his names differ from those now in use they are inclosed in parenthesis.

List of species of vertebrates.

Chelydra serpentina. Terrapene carolina (Cistudo clausa). Meleagris gallopavo sylvestris (M. gallopavo). Equus sp. indet. (p. 185). Mylohyus pennsylvanicus (Dicotyles) (p. 213). Rangifer caribou (p. 246). Odocoileus virginianus (Cervus) (p. 237). Cervus canadensis (p. 237). Bison bison? (B. americanus) (p. 267). Marmota monax (Arctomys). Tamias striatus. Sciurus carolinensis. Castor canadensis (C. fiber). Peromyscus leucopus (Hesperomys). Neotoma magister (N. floridana). Microtus pennsylvanicus (Arvicola riparius). Erethizon dorsatum. Castoroides ohioensis (p. 272). Sylvilagus floridanus (Lepus sylvaticus) Myotis subulatus (Vespertilio). Eptesicus fuscus (Vespertilio). Scalopus aquaticus (Scalops). Procyon lotor. Mustela noveboracensis (Putorius ermineus). Mephitis putida (M. mephitica). Urocyon cinereoargenteus (Canis virginianus). Canis lycaon? (C. lupus). Lynx canadensis (Felis).

Besides these vertebrates, there were reported by Leidy the land snails Helix albolabris, H. alternata, and H. tridentata; also a pair of valves of the river mussel Margaratina margaritifera and a fragment of another valve. Leidy regarded these as showing that this mussel formerly lived in Delaware River; whereas in his view it no longer existed there; but specimens of it from Philadelphia are in the U. S. National Museum.

An examination of the list shows that nearly all of the species of vertebrates are yet in existence and most of these still living in that general region. Rangifer caribou lives now far to the north and Lynx canadensis has its range somewhat further north. The two indicate a colder climate, especially the reindeer. Both got into the cave probably after the glacial front had withdrawn from that vicinity. The remains of Castoroides may have been carried in there at about the same time. The type specimen of Mylohyus pennsylvanicus was found in this cave. Cope referred specimens of a peccary found in Port Kennedy Cave to the same species with doubt. Undetermined species of the genus were recognized by Barnum Brown in his collection made in the Conard fissure in northwestern Arkansas. Dr. W. J. Holland reported Mylohyus pennsylvanicus from the cave at Frankstown, Pennsylvania. The type of the genus, M. nasutus, was found in Indiana. Beyond the testimony furnished by the Crystal Hill Cave, we have no evidence that the genus Mylohyus existed after the Wisconsin stage; the possibility exists that this species got into the cave before this stage.

The specimen of Equus is still more doubtful. It consisted of two isolated first and second milk molars of a very young colt. Leidy was in doubt whether the colt belonged to the domestic horse or to an indigenous species. The specimen had been collected with no record as to the part of the cave or of the depth in the upper layer of soil where it was buried. A fragment of a jaw of a colt might easily have been carried into the cave by some carnivorous animal since the coming of the whites. A fragment of the lower jaw of a bison also was found which had in it the last molar; and this was referred by Leidy to the existing buffalo.

It can hardly be doubted that this cave was hollowed out before the Wisconsin ice period. It may have been formed during the early Pleistocene. The fact that it was filled to a depth of 14 feet, in some places, with a fine laminated clay devoid of all traces of organic beings seems to indicate that for ages it had been shut off from the outer world, and that streams charged with fine sediment were permitted to pass through it. During possibly some glacial stage preceding the Wisconsin, erosion may have opened the cave so that the horse remains, those of a bison, and of Castoroides were dragged into it. The evidence for these suppositions is slender, but so too is that for a late Wisconsin indigenous species of horse in Pennsylvania. It is probable that most of the species found in the cave belong to the late Pleistocene or even to the Recent.

Fossil vertebrates found in a cave in Bucks County require our attention.

In 1880 (Proc. Acad. Nat. Sci. Phila., 1880, p. 349), Leidy presented a list of vertebrate remains which had been lying unstudied for 40 years in the collection of the Academy. These had been found in Durham Cave, somewhere near Riegelsville, in Bucks County. It is not improbable that the cave took its name from the village of Durham, about 2 miles southwest of Riegelsville. Leidy stated that the cave appeared to have been obliterated in the quarrying of limestone. In 1889 (Ann. Rep. Geol. Surv. Pennsylvania, for 1887, pp. 18–19) Leidy published a list of the species which he had identified.

List of fossil vertebrates from Durham Cave.

Acipenser sturio. Ameiurus nebulosus (Amiurus atrarius). Thamnophis sirtalis (Eutænia). Chelydra serpentina. Terrapene carolina (Cistudo clausa). Meleagris gallopavo sylvestris (M. gallopavo). Rangifer caribou (p. 246). Cervus canadensis (p. 237). Alces americanus (Alce). Odocoileus virginianus (Cervus) (p. 227). Erethizon dorsatum. Marmota monax (Arctomys). Sciurus carolinensis. Castor canadensis (C. fiber). Neotoma pennsylvanica (N. floridana). Ondatra zibethica (Fiber). Sylvilagus floridanus (Lepus sylvaticus). Ursus americanus. Procyon lotor. Mephitis putida (M. mephitica). Urocyon cinereoargenteus (Vulpes virginianus).

This list differs in its species from Leidy’s list of 1880 only in the exclusion of the bison and the inclusion of the elk, Cervus canadensis. All the species are still in existence, most of them in that region. The presence of the reindeer, the moose, and the porcupine suggests a cooler climate than now prevails there. These animals may all have become buried in that cave during the latest times of the Wisconsin stage or even during the Recent.

We are now to study a case which furnishes us with a store of knowledge regarding the life of the Pleistocene. In 1871 there was found at Port Kennedy, Montgomery County, a cave which was worked for its fossils by Charles Wheatley and later by Dixon, Mercer, and Cope, the latter having devoted himself to the description of the vertebrates. First of all will be given a list of the species of vertebrates, mostly mammals which have been recognized in the materials found in the cave. When Cope’s names differ from those employed here they are put in parenthesis.

List of species of vertebrates found in Port Kennedy Cave.

Ranidæ: Rana sp. indet. Emydidæ: Clemmys insculpta. C. percrassa. Terrapene eurypygia (Toxaspis anguillulatus). Colubridæ: Coluber acuminatus (Zamenis). Meleagridæ: Meleagris superbus (M. altus). Megatheriidæ: Megalonyx (p. 31). M. scalper (p. 31). M. tortulus (p. 31). M. wheatleyi (p. 31). Mylodon harlani? (p. 31). Equidæ: Equus complicatus (E. fraternus) (p. 185). E. pectinatus (E. f. pectinatus) (p. 185). Tapiridæ: Tapirus haysii (p. 203). Tagassuidæ: Mylohyus nasutus (p. 213). M. pennsylvanicus? (p. 213). Tagassu tetragonus (Mylohyus) (p. 213). Camelidæ?: Teleopternus orientalis (p. 224). Cervidæ: Odocoileus lævicornis. O. virginianus? Bovidæ: Bison sp. indet. (Bos) (p. 256). Elephantidæ: Mammut americanum (Mastodon) (p. 69). Sciuridæ: Sciurus calycinus. Castoridæ: Castor canadensis (C. fiber). Cricetidæ: Peromyscus leucopus? (Hesperomys). Anaptogonia hiatidens. Sycium cloacinum. Microtus dideltus. M. diluvianus. M. involutus. M. speothen. Zapodidæ: Zapus hudsonius? Erethizontidæ: Erethizon dorsatum? Ochotonidæ: Ochotona palatina (Lagomys). Leporidæ: Sylvilagus floridanus (Lepus sylvaticus). Talpidæ: Scalopus sp. indet. (Scalops). Soricidæ: Blarina simplicidens. Vespertilionidæ: Myotis? sp. indet. (Vespertilio). Ursidæ: Ursus americanus. Arctotherium haplodon. Mustelidæ: Taxidea taxus (T. americana). Mephitis fossidens. M. leptops. M. obtusata. M. orthostica. M. putida. Osmotherium spelæum. Pelycictis lobulatus. Mustela diluviana. Gulo luscus. Lutra rhoadsii. Canidæ: Canis priscolatrans. C. dirus? (C. indianensis). Urocyon cinereoargenteus. U. latidentatus. Felidæ: Machairodus gracilis. Smilodontopsis mercerii (Smilodon). Felis eyra. F. inexpectata (Uncia). Lynx calcaratus.

Into this list there are admitted 60 species, of which 54 are mammals. Of these, 41 are extinct, not counting the doubtful species unless there is good reason for it. There are, therefore, 68 per cent of the species extinct.

No remains of Rana were mentioned by Cope in his list of 1899. One species unnamed was recorded by Wheatley in his lists of 1871 and by Mercer in his paper of 1899. The turkey (Meleagris superbus) was not included by Cope in 1899, but it was included by Wheatley and Mercer and Cope in their papers of 1871 and in that of Cope in 1896 (p. 378). Mercer (1899, p. 280) mentions a leg-bone of a turkey, with spur, found by Wheatley. Remains of Megalonyx were abundant, but of M. loxodon only a single tooth was met with. Mylodon, believed to be M. harlani, was found only by Wheatley and was represented, as stated by Cope, by only a claw phalanx. The horse remains were originally (Cope, 1895, p. 447) referred to Equus major (=E. complicatus). Mercer, in 1899, in his figure 9, following Cope’s nomenclature, uses the name E. complicatus. In 1899, Cope concluded that the equine remains represented two races of Equus fraternus, E. f. fraternus and E. f. pectinatus. The present writer believes that the teeth referred to the subspecies fraternus are too large to belong to the species which was called E. fraternus, but which is now called E. leidyi. Only a single species of tapir, Tapirus haysii, was recognized. Cope (1895, p. 447) stated that it was the most abundant of the larger mammals. Cope (1899, p. 257) reported that 18 individual peccaries were represented by teeth, while bones were numerous. He recognized the presence of three species. The identifications of Mylohyus nasutus and M. pennsylvanicus were uncertain. A new species, M. tetragonus, was based on a ramus of a lower jaw. Milk molars were yet present and the third molar had not appeared. Cope spoke of the long diastema; but, to judge from his figure, the diastema equals only about the length of the milk molars and the first molar.

Cope, in 1899, described Teleopternus orientalis, basing it on a few teeth which belonged to three individuals. He was doubtful about the family position of the animal, but put it provisionally in the Camelidæ. In many respects the teeth resembled those of the Cervidæ. Matthew (Osborn, Age of Mammals, p. 469) has suggested its affinity to Ovibos.

Two species of deer were found in the cave, of which one was not distinguishable from Odocoileus virginianus. In Wheatley’s second list of 1871 and that of Cope of the same year there was recorded an undetermined species of Bos (Bison). Mercer (1899, p. 280) recorded from the Wheatley collection remains of three individuals of one species of the same genus. In Cope’s paper on the remains of this cave nothing is said about the genus; but in 1872 (Proc. Amer. Philos. Soc., XII, p. 96) he stated that Bos was represented by a part of a femur and some other bones. Hence in the list given above an undetermined species of Bison is included.

Abundant remains of the mastodon occurred in the cave, but none of any of the elephants. One need not, however, on that account conclude that elephants were not living in that region at that time.

It will be observed that a considerable number of rodents is included in the list. One species of porcupine is recognized. This was at first regarded by Cope as an extinct form and called Erethizon cloacinum; but in 1899 he referred all the remains, with some doubt, to the existing species, E. dorsatum. Cope found remains of about 50 individuals of a species of rabbit which he determined as Lepus sylvaticus, but this is now called Sylvilagus floridanus. In the Wheatley collection a species of bat was recognized and put in Vespertilio. Probably it belonged to Myotis.

Bears were abundantly present in the cave. One species, Arctotherium haplodon, was larger than the grizzly bear and represented by parts of about 25 individuals. A smaller bear, indicated by 8 individuals, appeared to be in no way different from the existing black bear, Ursus americanus. Of skunks there are listed 7 species, belonging to 3 genera, all the species being extinct except a supposed Mephitis putida. Besides these mustelids, there have been identified remains of the existing badger, the existing glutton, an extinct weasel, Mustela diluviana, and an extinct otter, Lutra rhoadsii. Remains of true dogs were not abundant in the collection. Cope recognized, however, 2 species of the genus Canis, one of about the size of the more common form of the existing wolf; the other exceeding in size the largest wolf known to him. This he thought might belong to Leidy’s Canis indianensis (=C. dirus Leidy). There were present 2 foxes, the existing gray fox (Urocyon cinereoargenteus) and an extinct species, U. latidentatus. Of the cat family a species, thought at first to be a hyæna (Crocuta), received the name Felis inexpectata. It had the size of the jaguar, and was represented by teeth and various bones. An extinct lynx, much like Lynx ruffus, was present. Another cat was identified as Felis eyra. Of this species G. S. Miller (Bull. 79, U. S. Nat. Mus., p. 116) remarks that its type locality is Paraguay and that it is supposed to range north to Central America. It appears somewhat doubtful, therefore, that the fossil remains belong to this species. Nevertheless, the progenitors of the species, in their wandering from Asia or Alaska to Central America and Paraguay, might have sent a colony into Pennsylvania, later to become extinct. Cope stated (1899, p. 250) that there was an isolated calcaneum in the collection which was of the proper size for Felis eyra, but which differed from that of this species. Two species of saber-tooth cats were found, Smilodontopsis gracilis and S. mercerii. The former is represented by various bones and teeth, especially by a damaged skull which presents the dentition. The crown of the great canine is 113 mm. long.

Besides the species included in the list given above, there are a few whose presence for one reason or another is doubtful. In both of his lists of 1871 Wheatley reported the presence of Crotalus, Coluber, and Tropidonotus (Natrix). Cope (1871, p. 98) said that the reptiles included three or four serpents, but in 1895 (p. 447) he wrote that two species of Ophidia were recognized. In his final paper he mentioned only his Zamenis acuminatus, here referred to Coluber. Wheatley (1871, p. 255) recorded an unidentified snipe as belonging to Scolopax. Cope (1871, p. 98) wrote that a snipe was one of two species of birds present. Mercer (1889, p. 280) recognized the same remains as belonging to a species of Gallinago. Wheatley in his last list (1871, p. 384) and Cope (1871, p. 98) reported Scalopus (Scalopus) as being represented by an undetermined species. It is catalogued by Mercer in the same way. Cope (1895, p. 447) stated that the raccoon was very rare; but it was not mentioned in any of his later papers. On the same page he wrote that there were fragments of teeth closely similar to those of Bassariscus astutus; but the species was not mentioned afterward.

As already said, there are admitted into the list given above, as identified in a reasonably good manner, 60 species, of which 54 belong to the Mammalia. It is a matter of interest to compare these with the species of mammals which were living in that general region before the fauna was disturbed by the arrival of the whites. The number of species of the existing mammals, as shown in the second column, is obtained from Rhoads’s “Mammals of Pennsylvania and New Jersey.” The subspecies are not included.

Families of land mammals represented in Port Kennedy Cave and those that have lived in that region within Recent times, together with the number of known species in each family at each of the two epochs.

┌──────────────────────┬──────────────────────┬──────────────────────┐ │ Families. │ No. of species, Port │ │ │ │ Kennedy. │No. of recent species.│ ├──────────────────────┼──────────────────────┼──────────────────────┤ │Megatheriidæ │ 5│ │ │Didelphidæ │ │ 1│ │Equidæ │ 2│ │ │Tapiridæ │ 1│ │ │Tagassuidæ │ 3│ │ │Camelidæ? │ 1│ │ │Cervidæ │ 2│ 2│ │Bovidæ │ 1│ 1│ │Elephantidæ │ 1│ │ │Sciuridæ │ 1│ 6│ │Castoridæ │ 1│ 1│ │Cricetidæ │ 7│ 9│ │Zapodidæ │ 1│ 2│ │Erethizontidæ │ 1│ 1│ │Ochotonidæ │ 1│ │ │Leporidæ │ 1│ 2│ │Soricidæ │ 1│ 5│ │Talpidæ │ 1│ 3│ │Vespertilionidæ │ 1│ 8│ │Procyonidæ │ ?│ 1│ │Ursidæ │ 2│ 1│ │Mustelidæ │ 11│ 9│ │Canidæ │ 4│ 3│ │Felidæ │ 5│ 3│ └──────────────────────┴──────────────────────┴──────────────────────┘

In the column of fossils there are 54 species; in that of the Recent there are 58 species. Of two families represented at present in the region, but not included in the Pleistocene column, Didelphidæ and Procyonidæ, the latter named has had remains referred to it with doubt. Without doubt members of both families existed there at that time.

Of the families of the Pleistocene column two no longer live anywhere near the region; four nowhere on the continent; one nowhere on the earth. Even of such families as the Ursidæ and the Felidæ important elements, as Arctotherium and the saber-tooths, are extinct. Of the 54 species admitted in the Pleistocene column 40 are extinct; that is, 74 per cent.

If we consider the sizes of the animals in question we gain this result: Only 15 of the existing species are of any considerable size, ranging from that of a raccoon to that of a bison, about 26 per cent. Of the 54 fossil species of mammals, about 30 vary in size as indicated, about 57 per cent. It is hardly to be doubted that this preponderance is due to the poorer chances which the smaller skeletons had of preservation and of rescue from the matrix. Had the smaller fossil species been preserved and collected in the same proportion that the smaller existing ones have to the larger, the cave ought to have furnished twice as many species of mammals as it did. It is, of course, possible that the larger species are more liable than the smaller ones to become extinct as time passes on. We can hardly doubt, in any case, that when the Port Kennedy animals were being buried in that cave there lived in that region a considerably larger number of species than within Recent times. There must have existed in that region more moles, more rabbits, more cricetids, more squirrels, and many more bats. Certainly there is no adequate record of the number of birds, snakes, turtles, and amphibians that must have existed about Port Kennedy and have perished in that cave.

From the collection that has been made in the cave at Port Kennedy some definite conclusions ought to be reached regarding their time of existence. In his account of the cave and of the exhumation of the animal and vegetable remains, Mercer (1899, pp. 269–286) has shown what extreme care was taken in recording the position which each specimen occupied in the deposits. In his figure 9 he has noted the levels which the various species occupied. While the existence of four beds of materials makes it evident that the deposition went on for some time, it is noted that few or no differences exist in the character of the species included. Possibly Mercer’s subdivision 1 is to be excepted in this statement. Certainly no great changes went on in the fauna while the cave was being filled; no such changes as occurred in the glaciated region from the Aftonian interglacial stage up to the Late Wisconsin. It appears more probable that the deposits in the cave and the animals entombed there appertain to about a single Pleistocene stage. Is, then, the stage the Late Wisconsin?

This cave is situated only about 55 miles south of the Wisconsin moraine. At the time the species found in the cave existed they must each have occupied a wide extent of territory. It is not to be doubted that the range of nearly every species extended northward far beyond the moraine mentioned. Why, then, in deposits overlying the Wisconsin drift have there never been found any remains of the four Port Kennedy species of Megalonyx, of Mylodon, of the two species of horses, of the tapir, of the three species of peccaries, of the deer Odocoileus lævicornis, of the five extinct species of cricetids, of Ochotona, of the extinct species of Blarina, of the great bear Arctotherium, of the six extinct species of skunks, of the extinct otter, of the extinct dog, of the extinct fox, of any species of saber-tooth tiger, or of the extinct cats Felis inexpectata and Lynx calcaratus? The absence of so many species of animals, most of them of large size, from deposits so well adapted to preserve bones and teeth, render it very certain that the animals no longer existed there.

Did the extinct species which are referred to above exist in eastern Pennsylvania at some time during the Wisconsin glacial stage and perish before the close?

A few of the species found in the cave and still existing are at present inhabitants of regions somewhat more northerly than Port Kennedy. Such are Erethizon dorsatum and Gulo luscus; but the great majority, living and extinct, indicate a climate at least as warm as that of the present; many of them suggesting a still milder condition. Within historical times both of the species just named have inhabited the Alleghany Mountains at least as far south as Port Kennedy. Cope, in 1871 (Proc. Amer. Philos. Soc., vol. XII, p. 99), concluded that he had then identified in the cave remains of 11 neotropical species. It appears, therefore, wholly improbable that this assemblage of animals lived in that region, so close to the foot of the glacier, during the Wisconsin stage. These animals must have had their time of existence previous to this inhospitable epoch. It seems to the writer that the proportion of extinct species, three-fourths, and the history of many of the genera and species, indicate a time about equivalent to the Aftonian.

Professor A. Heilprin (Proc. Phila. Acad. Nat. Sci., 1895, p. 451) expressed himself as being inclined to refer this cave fauna to the Pliocene. An examination of this opinion would show that it is no more tenable than the opinion that the fauna is of the Wisconsin stage. It will not be discussed here beyond saying that deposits containing a similar fauna are found along the Atlantic coast from New Jersey to the Gulf, and that at one place at least, Vero, Florida, these are underlain by abundant Pleistocene sea-shells.

Besides the vertebrates which have been listed, a number of beetles were found and about 10 specifically determined plants. Wheatley (1871, p. 385) presents a list of the beetles as determined by Dr. G. H. Horn, but the names were not accompanied by descriptions. When later (Trans. Amer. Entom. Soc., vol. V, 1876, pp. 241–245) Horn came to describe them he reduced the number of species and, in some cases, gave them other names. The following is a list as given in Horn’s paper just cited: Cychrus wheatleyi, C. (minor), Pterostichus (spp. indet.) Cymindis aurora, Chlænius punctulatus, Dicælus alutaceus, Choeridium? ebeninum, Phanæus antiquus, Aphodeus precursor. All of these, as the writer is informed by Dr. E. A. Schwarz, of the U. S. Department of Agriculture, are regarded as extinct, but as closely allied to species now living in that general region. The plants, as reported by Mercer, are Quercus palustris, Q. alba, Q. macrocarpa, Fagus ferruginea, Corylus americana, Pinus rigida, Carya porcina, C. alba, Ampelopsis quinquefolia, Cratægus crus-galli?, and all still flourish in eastern Pennsylvania.

Mercer (1899, p. 269) has given a description of the cave found in quarrying operations. It was located on the right bank of the Schuylkill River, at the village of Port Kennedy and about 2 miles below Valley Forge. Wheatley (1871, p. 236) gave a map which showed the position of the quarries. A comparison of this with the topographical map of Folio 162 of the U. S. Geological Survey shows that they were situated about 800 feet away from the river and facing the valley of an unnamed streamlet. None of the descriptions give the elevation of the cave above the river or above the sea. The river at that place is apparently about 70 feet above sea-level. The 100–foot contour-line runs along near the location of the quarries, but these may have extended back to a higher level. Putting all of the statements together, it appears probable that the mouth of the cave was, in Wheatley’s time, about 50 feet above the level of the river. Originally the surface elevation may have been still greater, but may have been reduced by erosion of the hill. The surface rock here is red shale of the Stockton formation, belonging to the Triassic, and is underlain by the Shenandoah limestone, a member of the Cambro-Ordovician series. This limestone was being quarried in 1871, when a cave was broken into, filled with incoherent materials and exposing fossil bones in abundance. It was visited by Charles Wheatley, who proceeded to make excavations and collect the fossils. In studying the fossils he worked with Professor E. D. Cope and Dr. G. H. Horn. The results were published in Wheatley’s two papers of 1871 and in two papers by Cope in the same year (Proc. Amer. Philos. Soc., vol. XII, pp. 15, 73–102). According to Wheatley’s description and his figures, the part of the cave seen was about 20 feet wide at the top, expanded below to about 30 feet, and then narrowed at the bottom, as then recognized, to about 10 feet. The depth was given as 40 feet, but Mercer thinks that this was improbable and that Wheatley’s measurements were to some extent guesses. Mercer (1899, p. 271) stated that this cave might be compared to a bottle of unknown size. It had opened to the surface; and on his page 283 Mercer spoke of it as forming a well-like hole that might have been as much as 70 feet deep. Evidently Mercer here included that part of it which he himself excavated. The materials filling it were, according to Cope (1871, p. 73), the débris of the neighboring Triassic strata. Figure 11 is taken from Mercer’s paper and is a reproduction of a sketch made by Wheatley in 1871. After Wheatley had made his collection the cave was covered over by débris from the quarry and forgotten.

In the course of further quarrying operations the same cave was broken into again in 1893. Excavations in the materials that filled the cave were made in 1894 by Dr. Samuel Dixon, H. C. Mercer, and others, resulting in the securing of the collection which formed the subject of Cope’s paper of 1894 and his final report of 1899. At this time, according to Mercer, the quarrying operations carried on from 1855 had transformed a gently sloping hillside into an amphitheater several acres in extent, walled with perpendicular escarpments of rock, sometimes a hundred feet high. At this time the floor of the quarry had been lowered and the cave was broken into at a level below that reached by Wheatley. Figure 12, reproduced from Mercer’s figure 5, shows the relation of the later excavations to those of 1871. As already stated, Mercer concluded that Wheatley’s dimensions were probably results of guesses, inasmuch as the top of Mercer’s exposure was not more than 30 or 33 feet below the original level of the hilltop. According to Mercer’s figure 5, his own excavation probably extended down about 16 feet below the level reached by Wheatley; but other statements appear to make this somewhat greater.

Mercer wrote that the materials filling the cave had been stratified by the action of water. He recognized four subdivisions, most of which stood higher around the walls than at the center of the cave. Of these subdivisions, the first and uppermost was supposed to mark the lowest level attained by Wheatley. It consisted of fine clay and loam of black color, intermingled with fine and coarse muck, in which were found some remains of small mammals, just what species was not stated. On his chart, his figure 9, a tapir is indicated as occurring in it. Subdivision 2 was composed of from 4 to 11 feet of sandy clay, with fragments of sandstone and limestone, from small ones up to about 2 feet in diameter. In this matrix there were numerous bones and teeth of large animals, but it lacked small ones and vegetal matter. Subdivision 3 was a sandy clay, blackened by vegetable matter and containing numerous bones of vertebrates, large and small. The lowest subdivision, 4, was a zone which was followed down about 10 feet and which consisted of sand, clay, and stones, all of a yellow color. In this were found remains of the larger mammals, better preserved than in the upper subdivisions. At the lowest depth reached the excavation appears to have extended below the level of the Schuylkill River and the water came in so rapidly that further descent was not practicable.

Mercer’s theory of the filling of the cave is expressed in these words, on his page 277:

“Enough had been seen to convince us that a fresh-water flood, rising to a level of from 15 to 20 feet above the present level of the hilltop, hence a general inundation of the whole surrounding country, bearing in its current the clay, stones, and earth of neighboring levels, had tumbled into the fissure, carrying with it the bones of creatures previously denuded of flesh and softened by decomposition.”

And further, on page 284:

“Not unreasonably, therefore, we may suppose, not only that the creatures had perished together, but also that they had perished on the spot or at the chasm—not meeting this fate during a long interval of time, and through a long series of chance tumbles, but suddenly and by force of a common event.”

Are we to suppose that during some summer freshet animals in such numbers were swept away that those that were found in the cave, and doubtless many more which decayed utterly, were only the relatively few that happened to pass over that 20–foot hole? Where, then, were picked up all the other animals that must have burdened the swollen Schuylkill? Or did it possibly happen that all the animals that were swept away were in some unaccountable manner directed into that hole? If the current was strong enough to sweep along stones up to 2 feet in diameter, how did it happen to deposit there fine sand and clay, leaves, cones, seeds, and sticks? It is difficult to accept the theory that the filling of the cave was due to a cataclysm such as has been invoked. It seems far more probable that the mouth of the cave was open for many hundreds of years, possibly thousands of them, so that animals, plants, stones, and fine and coarse earth could in various ways get into it. Animals wandering about might inadvertently fall in or be pushed in by the herd. Doubtless at some former time the Schuylkill flowed at a higher level than now, and during times of unusually high-water might have risen to the level of the mouth of the cave and carried into it at each rise some mud, some vegetation, and some animals. The filling was quite certainly a slow process.

To the writer the part of the cavern which was worked and pictured by Wheatley has all the marks of an enormous pot-hole, such as those which have been discovered at Cohoes, New York. While the latter appear to have been drilled out in late Pleistocene times, the Port Kennedy hole must have been fashioned during the early Pleistocene or even in the Pliocene. One may suppose that, after the pot-hole had reached the depth where the constriction was found, the water began to find its way out at the bottom through fissures or passages in the limestone. When this happened, the passages may have been enlarged mechanically or by means of solution, resulting in the formation of the various lower caverns. When the river had been lowered enough to reach only occasionally the mouth of the pot-hole, the latter became choked first by the coarse materials now found in subdivision 4, and afterwards by finer sand and mud.

Some vertebrates of the late Pleistocene or early Recent observed at Carlisle deserve consideration.

In 1850 (Proc. Amer. Assoc. Adv. Sci., vol. II, 1849, pp. 352–355) Professor S. F. Baird gave an account of his explorations in the caves in the region about Carlisle, Cumberland County. One of these caves was near Carlisle, and in it Baird found a large number of animal remains. A second cave, the situation of which was not given, was on the top of a hill and was a vertical shaft 30 feet deep, which opened into a large gallery. It furnished a skeleton of a bear, but this appeared to have only recently fallen into the cave. Another cave was on the bank of the Susquehanna, 0.5 mile below a railroad bridge. It was, therefore, probably near Harrisburg. The entrance was in limestone rock, nearly vertical, and 20 feet deep. Here Baird found many bones, embedded in mud, but of these he obtained only a few. Another cave, apparently nearby, which Baird spoke of as “the main cave,” furnished some of his specimens. Still another cave, probably in the same neighborhood, was the source of his most perfect specimens. This presented a series of galleries near the roof and these were reached by ladders. These galleries were filled with mud, and in this mud the bones were buried. The number of species which he obtained, he reported, was nearly twice the number living there at the present time. Of these fossil species he estimated that about 5 per cent were extinct. Baird appears never to have completed his study of his collection. His list designates the animals only by their vernacular names. The mammals consisted of panthers, lynxes, wolves, foxes, otters, bears, muskrats, deer, beavers, and rabbits. There were bird remains in great quantities, and these included wild turkeys, some of great size, swans, wild ducks, and pelicans. There appeared to be 8 or 10 species of tortoises. Bones of snakes were quite common; also scales and vertebræ of fishes, and a lower jaw of a salamander. In the uppermost 2 or 3 inches of mud were many relics of Indians.

Baird supposed that these bones had in most cases been washed in from above through sink holes. This collection, or some of it, was brought by Baird to the Smithsonian Institution; and they, or some of them, are in the collection of mammals; but the bulk of the collection has apparently been lost. All of these animals belong evidently to either the very late Pleistocene or to the Recent period.

A cave at Frankstown has furnished fossils of about Middle Pleistocene time. In 1908 (Ann. Carnegie Mus., vol. iv, pp. 228–233) and again in 1912 (Proc. Internat. Zool. Congr., Boston, 1907, pp. 748–752), Dr. W. J. Holland gave an account of the discovery of vertebrate fossils in a fissure in limestone rock at Frankstown, Blair County. This village is situated on the Frankstown Branch of Juniata River, a little more than 2 miles north of east of Hollidaysburg. The fissure was excavated in a Devonian rock known as the Lewistown limestone. The quarries are reported to be in the village and on the top of a hill that rises about 400 feet above the banks of the Juniata. According to the Hollidaysburg topographical sheet, the 920–foot line crosses the river just above the village. The highest hill, 1,260 feet above sea-level, is 0.3 mile away toward the northwest. In this hill, as Dr. Holland stated, there are several small caves. The one which furnished the fossils appeared to be about 40 feet in length, averaging from 6 to 8 feet in width, and at the most was not more than 10 or 12 feet high. The floor was about 30 feet below the top of the hill. The fissure appeared to have once continued up to the surface, but the opening had been filled with fallen blocks of limestone. The floor of the cave is described as being occupied by about 2 feet of red soil, everywhere traversed by bands and layers of dark materials charged with organic matter. With the finer deposits were mingled fragments of rock, some being large blocks. The fossil remains appear to have been carefully collected, but were mostly fragmentary. They were only cursorily studied at the time of Holland’s writing and nothing has since been published on them. The number of species obtained was estimated to be from 30 to 40. The following genera and species are mentioned:

Meleagris sp. indet. Megalonyx sp. indet. (p. 31). Tapirus sp. indet. (p. 203). Mylohyus pennsylvanicus (p. 214). Odocoileus virginianus (p. 227). Cervalces? sp. indet. Bison sp. indet. Mammut americanum (p. 69). Sciurus sp. indet. Ondatra sp. indet. Erethizon sp. indet. Lepus sp. indet. Ursus americanus. Arctotherium haplodon. Mephitis sp. indet. Canis sp. indet. Felis? sp. indet.

After the foregoing had been put in type Mr. O. A. Peterson, of the Carnegie Museum, sent the writer a revised list in which additions are made. The following are the most important:

Cryptobranchus sp. indet. Rana catesbiana? Clemmys insculpta. Blarina sp. indet. Ænocyon dirus. Canis priscolatrans? Spilogale putorius. Brachyprotoma putorius. Boötherium bombifrons. Equus sp. indet.

Besides these forms, remains belonging to bats, various birds, snakes, and batrachians have been recognized. Of the fossils identified generically or specifically those belonging to Megalonyx, Tapirus, Mylohyus, Cervalces, Mammut, and Arctotherium are certainly extinct. Probably, too, the bison and the species of Felis are extinct. There are, therefore, pretty certainly close to 50 per cent of the species which are no longer living. This percentage and the history of some of the genera make it improbable that the assemblage belongs to the Late Wisconsin stage. Some of them could hardly have been living during the Wisconsin, when the foot of the glacier was within 100 miles toward the northeast and northwest. On the other hand, there are no species or genera present which make it necessary to refer the collection to the first interglacial. The assemblage probably belongs to the middle Pleistocene.

Coming now to the very southwestern corner of the State, we find that. Elephas columbi has been met with in the bed of Hargus Creek, 3 miles above Rogersville, in Greene County (p. 150), and E. primigenius on Gray’s Fork of Ten Mile Creek, near Graysville (p. 133). In the Rogersville Folio (No. 146, U. S. Geol. Surv.), Dr. F. G. Clapp described the geology of this quadrangle. On his page 10 he briefly discussed the meager Quaternary deposits of the area. These he referred to the Carmichaels formation, and indicated his opinion that it belonged to very early Pleistocene. On the geological map it is represented as occurring along Ten Mile Creek at and just below Rogersville. The occurrence of a tooth of Elephas columbi just above this town and of E. primigenius just above Harveys (p. 133) renders it probable that other patches of the formation exist further up the stream and along some of its branches, and that the fossils were derived from that formation. It is, of course, possible that small patches of a later deposit exist there.

Reference has been made to the Carmichaels formation. The type locality is found at Carmichaels, on Muddy Creek in Washington County. The geological description of the locality has been presented by Marius R. Campbell in the Masontown-Uniontown Folio (No. 82, U. S. Geological Survey). The formation occurs extensively along Monongahela River and other streams of western Pennsylvania. For information the reader should consult the Geological Survey Folios Nos. 144, 146, 121, 82, and 177. The deposits occur at levels considerably above the present streams and are regarded as having been laid down in old and now abandoned river channels and in tributaries of these. The time when this occurred is believed by many, if not most geologists to belong to the early Pleistocene, the Kansas stage, or possibly the Nebraskan. In the opinion of some geologists the glacial ice dammed the streams and caused their valleys to be filled with detritus. More recent Pleistocene deposits, possibly of Wisconsin age, occur at lower levels in some places south of the Wisconsin moraine; and perhaps the age of some of them has not yet been recognized. When remains of vertebrate animals are discovered, it is of great importance to determine, if possible, the exact levels of their origin.

On another page mention is made of the finding of a tooth of Elephas primigenius at Lone Pine (p. 133), 7.25 miles south of southeast of Washington. This village is on Little Ten Mile Creek. No details of the discovery have been received. From Folio 144 of the U. S. Geological Survey it is learned that patches of the Carmichaels formation are found for several miles along Ten Mile Creek, near the southern boundary of the quadrangle. It seems probable that there may be patches of the same deposit along Little Ten Mile Creek, in the neighborhood of Lone Pine.

As detailed on page 70, a mastodon tooth was found many years ago about 1.5 miles south of the village of Hickory, Washington County, about twenty miles southwest of Pittsburgh. Westland Run empties into Chartiers Creek, and this into the Ohio at Pittsburgh. The geology of Burgettstown and Carnegie Quadrangles has been described by E. W. Shaw and M. J. Munn (Folio 177, U. S. Geol. Surv. 1911). No Pleistocene deposits are mapped on the stream mentioned; but just a little lower down, on Chartiers Creek, is a patch of the Carmichaels formation. Below Hickory somewhere there must be a Pleistocene deposit of some kind, and it is more probably early than late Pleistocene.

From the vicinity of Pittsburgh there have been reported remains of the mastodon (p. 69), of Elephas columbi (p. 150), and of an undetermined species of elephant (p. 168). Neither of the elephants is certainly determinable. The mastodon, represented by fragments of bones and teeth, is said to have been found in the river bank, at the junction of Monongahela and Allegheny Rivers. It is impossible to determine the Pleistocene stage to which any of these proboscidean remains belong. As shown on the geological map of the Carnegie Quadrangle (Folio 177, U. S. Geol. Surv.) there are indicated here Pleistocene deposits of early, intermediate, and late stages.

Little information is furnished by a mastodon reported found on Dicks Creek in Butler County. The statements regarding the finding of elephant remains on French Creek near Meadville are vague and valueless (p. 168). Some remains of Elephas columbi have been found at Tryonville, at a depth of 7 feet (p. 150). The town is on the Wisconsin moraine and the elephant probably belongs to the Late Wisconsin.

Nearly a hundred years ago a tooth of Elephas primigenius was reported from a place in Erie County, called Beaverdam (p. 133). From Mr. Clyde C. Hill, civil engineer, Northeast, Erie County, the information is received that Beaverdam is a cross-roads hamlet about 23 miles south of the lake, near the prolongation of the western New York boundary line. This is within the area covered by Wisconsin drift, and it is pretty certain that the animal lived there after or near the close of the Wisconsin stage.

Just west of Erie a mastodon tooth has been found along Chase Creek (p. 70). Unless there are some unrecognized pre-Wisconsin deposits along this creek, the animal must have lived there at a time after the lake had retired to about its present limits. This would be near the very close of the Pleistocene epoch. The same conclusion must be arrived at from a study of the proboscidean remains (supposed to be those of an elephant) found at Girard.

Brief mention is made here of finds of fossil vertebrates in Pennsylvania which have not yet been mentioned; also, the localities are given where they are found, and citations of the pages where fuller descriptions are furnished:

A horse has been reported from Rutherford, Dauphin County (p. 185), and a peccary, Platygonus vetus (p. 213), from Milroy, Mifflin County. Mastodons have been reported from Tunkhannock, Wyoming County; Berwick, Columbia County; Reading, Berks County; Jackson Township, York County; near Reedsville, Mifflin County; Chambersburg, Franklin County, and Bedford, Bedford County (see pp. 68, 69). Elephas primigenius has been met with at Brookfield, Tioga County (p. 133); and somewhere about Chadd’s Ford, in Chester or Delaware County (p. 133).

OHIO.

(Maps 35, 36.)

The State of Ohio is partly glaciated, partly not. The unglaciated portion forms the southeastern border and constitutes close to 28 per cent of the whole surface. The glaciated area is mostly covered by the Wisconsin drift, which makes up 60 per cent of the whole surface. The remainder is covered by that part of the Illinoian drift-sheet which projects beyond the edge of the Wisconsin. This occupies about 12 per cent of the surface of the State. The unglaciated area contains Pleistocene deposits along the streams, especially along Ohio, Muskingum, Hocking, and Scioto Rivers. Probably the greater part of the materials forming these deposits were brought down the rivers which headed at the foot of the Illinoian and Wisconsin glacial ice-sheets. However, all that part of the country which was not covered by glacial ice was acted on by atmospheric agencies and suffered erosion. Hence abundant materials of non-glacial origin were swept down those tributaries of the Ohio which had their sources in the Alleghany region and down those which flowed through the unglaciated part of the State. Much of these materials was deposited along the banks of these streams and mingled with the débris from the glacial ice-sheet. Doubtless such deposits were being made during the whole Pleistocene epoch and were mostly swept away; or they may have been covered up by subsequent deposits; or the deposits of one stage may in many cases not be distinguishable from those of other stages. A perusal of chapter V of Leverett’s monograph of 1902 (Monogr. U. S. Geol. Surv., vol. XLI, 1902, pp. 228–252) and of the papers there cited, also of others published since that time, will impress the reader with the fact that an old drift, probably of Kansan or pre-Kansan age, has left traces of itself in Ohio just outside of the terminal moraine of the Wisconsin drift. This is found especially in Columbiana County; but, according to Wright (2d Geol. Surv. Pennsylvania, Z, p. 207) it extends as far westward as Canton, Stark County.

It is shown in Leverett’s paper that the streams, especially the larger ones, of southwestern New York, western Pennsylvania, and eastern Ohio had, at some time preceding that of this old drift, been deeply excavated into the underlying rocks, and that these ancient channels had become filled by the outwash from the older drift. Furthermore, terraces composed of this drift are now found along rivers of the region mentioned, at heights varying from 150 to as much as 500 feet above the present streams. Those old, deeply excavated valleys may therefore have once been filled to the highest terraces and since that time have been re-excavated to the level of the present streams. The ancient rocky floors in many cases lie now from a few to some hundreds of feet below the beds of the existing rivers. It is easily possible that the bones and teeth of early Pleistocene animals may have been buried in such valley fillings and such terrace deposits. Again, remains of such vertebrates may have been buried beneath the glacial “fringe” that has been mentioned. In such cases it may be impossible for one who is not a glaciologist, perhaps not even for him, to determine the real age of the fossils. It is, therefore, of the utmost importance that a record be kept of the exact spot where the fossil was found, so that at some future time the geology of the locality may be studied by a competent person. Naturally, other information, as that relating to the kind of deposit, depth of burial, elevation of place of burial, and the like, is valuable.

A discussion of the Illinoian drift-sheet, including that part found in Ohio, forms chapter VI of Leverett’s work of 1902 (Monogr. cit., pp. 253–291). As shown by his plate II, Illinoian drift covers a small area in the southwestern corner of the State, along Ohio River; then leaving the river and running first in a northeasterly direction, then directly north, it forms a narrow strip outside the border of the Wisconsin as far north as Richland and Holmes Counties. If it extends further east than this, it is concealed beneath the Wisconsin. It is to be expected that Illinoian drift will be discovered here and there in the greater part of the State beneath the Wisconsin where the latter shall have been penetrated in digging wells, in borings, and where streams have cut down through the later drift-sheet. In such places it will be possible to find remains of animals and plants buried in interglacial deposits laid down before the Wisconsin stage; that is, in either Sangamon or Peorian or even more remote times. On page 269 of the work just quoted, Leverett mentions a case near Lancaster, Fairfield County, where a black mucky soil was found between the Wisconsin and the Illinoian drifts. On page 273 of the same work is mentioned the occurrence of logs and pieces of wood at Bethel, Clermont County, in a gravel-bed beneath the Illinoian drift. This might be interpreted as indicating a deposit belonging to the earliest part of the Illinoian or to the Yarmouth.

The general aspects of the Illinoian drift are described by Leverett on his pages 270 to 285.

Deposits of Illinoian age may occur beyond the border of the ice-laid Illinoian drift and even beyond the Wisconsin as the result of outwash. Leverett (op. cit., p. 285) mentions the occurrence of what appears to be an Illinoian terrace along Sandy Creek, near Waynesburg, Stark County, at 70 feet above the stream, while the Wisconsin terrace is hardly 40 feet above the creek. High-level terraces are found along Licking and Muskingum Rivers from Hanover, Licking County, to McConnellsville in Morgan County, and are thought to be possibly of Illinoian age, while lower ones belong to the Wisconsin. Illinoian gravels and cobble are likewise met with along Hocking River (Leverett, op. cit., p. 288); also along the Scioto from Chillicothe nearly to its mouth. On lower-level terraces other deposits of Wisconsin age are to be looked for. Again it is seen how important it is that accurate information should be sought regarding the exact spot of interment of any vertebrate remains, as well as the elevation, the depth, and kind of materials passed through.

Map 35 has been prepared to show the distribution of the Wisconsin and Illinoian drift-sheets in Ohio. The driftless area, shown without shading of any kind, occupies the southeastern side of the State and forms a broad tract somewhat parallel with Ohio River. The Illinoian belt lies between this driftless area and the Wisconsin. Naturally it passes beneath the Wisconsin drift and probably underlies most of it. A part of the map is shaded by horizontal lines in order to show the position and extent of former Lake Maumee. This lake was an early predecessor of Lake Erie and emptied into Wabash River. The moraines laid down by the Wisconsin ice on its gradual withdrawal from the State are indicated by the stippled areas and by the letters at the sides of the map. Most of the names applied to these moraines in Ohio differ from the parts of the same moraines in Indiana. The Germantown, Eaton, and Englewood correspond to the Bloomington of Indiana; the Sidney to the Union City; the Loramie to the Salamanie; the Celina to the Wabash; and the Lima to the Fort Wayne.

Map 36 shows the localities where Pleistocene mammals have been discovered in the State and the relation of these localities to the drift-sheets and the moraines.

It is to be supposed that any animal whose remains are found in deposits overlying the Wisconsin drift lived there after the retreat of the ice-sheet from that locality. Any mastodon (maps 5, 7) that has been discovered within the area covered by the old Lake Maumee probably lived there after that lake had subsided. However, it might be possible to find along rivers, or deep cuts along railroads, animals that had lived there during Sangamon times; but this may be supposed to occur rarely. Mastodons, Nos. 34, 37, and 39 of map 7, probably lived and died after later Lake Warren had shrunken into Lake Erie.

Most of the fossil vertebrates that have been found in Ohio belong to the Late Wisconsin; that is, they lived in their respective localities after the glacial ice had retired from those localities. A few fossils may be credited to an interglacial stage, Sangamon or Peorian, which intervened between the Illinoian and the Wisconsin. Inasmuch as in the area occupied by the Illinoian drift this deposit may be cut through by rivers or railroads, it is possible that pre-Illinoian fossils might be discovered.

A tooth of Elephas primigenius has been found at Waverly, Pike County, on Scioto River, as recorded on page 134. Along that river there are deposits of gravel and sand which were derived apparently from Illinoian drift, while below these Illinoian deposits is a Wisconsin terrace. The tooth above mentioned appears to have been found in a gravel-pit of the Norfolk and Western Railroad about the year 1900. The writer has not been able to secure any information as to the elevation of the pit. The elephant remains observed by Whittlesey along Scioto River, as mentioned on page 169, were probably buried in the Wisconsin terrace. A mastodon has been found in Pike County (p. 70), but the more exact locality is not recorded.

An important but apparently now lost and therefore indeterminable specimen of elephant is that to which was given the name Elephas jacksoni, described on page 168. It was found in the northwestern corner of Jackson County, on Little Salt Creek, probably a short time before 1838. The probability is that it was found in Wisconsin deposits, but its age is possibly greater. According to Leverett (op. cit., pp. 120, 121, 289), there are in this valley deposits which were probably laid down during the Illinoian stage. An elephant skeleton is reported to have been dug up many years ago in the village of Beverly, Washington County (p. 169), on Muskingum River. Leverett (Monogr. XLI, p. 157) states that glacial deposits belonging probably to the Wisconsin stage are found here at a height of 119 feet above the river. Inasmuch as the greater part of the village is below this level, the elephant probably belongs to Wisconsin time.

Further up the Muskingum, at or near Duncan Falls, there was found about 1857 a tooth of Elephas primigenius (p. 135). The animal probably lived and died there at a time when the Wisconsin glacier was not far away. Other remains of the same species have been described from Zanesville. The bed which contained these is said to be at a height of 37 feet above the river and 20 feet from the natural surface of the ground. Inasmuch as drift outwash, believed to be of Wisconsin age, is built up here to a height of 100 feet above the river (Leverett, op. cit., p. 157), it is wholly probable that the elephant, like the one just described, lived in the vicinity of the Wisconsin ice-front. At Nashport have been discovered in swampy ground remains of Castoroides (p. 273) and of Mammut (p. 70). Although there is at Hanover, Licking County, across Licking River, a great dam of supposed Illinoian age and probably more or less hidden deposits of the same age along the river, the giant beaver and the mastodon just mentioned may not be older than the Wisconsin. Nevertheless, as they were found lying on gravel at a depth of 14 feet, they may have been buried there during the Sangamon stage. Along the eastern border of the State, in Columbiana County, on Salt Creek, in the southwestern part of the county, there was found, about 1845, a tooth of a horse (p. 186). It was discovered while a canal was being excavated and at a depth not to exceed 12 or 15 feet. The locality is apparently some miles south of the Wisconsin moraine. The animal lived there evidently at some time preceding the Wisconsin drift stage, possibly after the Illinoian, but quite as likely before the Illinoian. Not far away from where the horse was discovered, apparently on Little Yellow Creek, and probably not far from New Salisbury, there was found, about 1850, a fragment of the lower jaw of a tapir (p. 203). It probably lived at about the same time that the horse did. Near Millport a tooth, referred to Elephas primigenius, has been found (p. 135). The locality is beyond the Wisconsin moraine, but it is impossible to determine whether the beast lived there early or late in the Pleistocene.

At this point may be mentioned the discovery of remains of a peccary, supposed to be Mylohyus nasutus (p. 215), and of Mammut americanum (p. 70) in the southern edge of Lisbon, Columbiana County, apparently along Middle Fork of Little Beaver River. This locality is on the border of the Wisconsin drift-sheet, and the peccary and the mastodon might well have lived there with the horse and the tapir mentioned above.

Not many localities within the area of the Illinoian drift in Ohio have furnished vertebrate fossils.

Lyell in 1843, as stated on page 71, reported that teeth of mastodons and of elephants had been found on the Cincinnati side of the river, on the high terraces.

From Professor N. M. Fenneman the writer learns that Lyell’s reference could hardly apply to any other locality than Terrace Park or Milford. Here are found some fragments of an Illinoian terrace that would hardly be spoken of casually as such, while the Wisconsin deposit is present as an upper and a lower terrace.

In Hyde Park, as detailed on page 71, considerable parts of a mastodon and some remains of a horse (p. 185), probably Equus complicatus, have been discovered. The age of these remains certainly antedates that of the Wisconsin; and it is not improbable that the excavation was carried through the Illinoian drift into an older and probably interglacial deposit. Professor Fenneman writes that this area is only thinly covered by Illinoian drift and is also far beyond the limits of the Wisconsin outwash.

The occurrence of Bison latifrons near Fincastle, in Brown County (p. 257), must be noted. The fine pair of horn-cores now in the Cincinnati Society of Natural History may have been buried in deposits of Sangamon age. It is not, however, impossible that they were in an interglacial bed below the Illinoian drift.

On page 135 there has been given an account of the finding of a skull of Elephas primigenius, somewhat more than a mile east of New Burlington. The locality is treated in proper detail in N. M. Fenneman’s paper entitled “Geology of Cincinnati and Vicinity” (Bull. 19, Geol. Surv. Ohio, p. 158). According to this account the skull was buried in a lacustrine silt laid down probably when the Wisconsin glacier was not far away from that region. The surrounding country is covered with Illinoian drift. This skull is now the property of the U. S. National Museum.

In the collection of the Ohio State Archæological and Historical Society at Columbus there are remains of Platygonus compressus, jaws and good teeth, which were found about a mile north of Chalfants, in Perry County, and along Jonathan Creek. This place is within the area covered by Illinoian drift. It is possible that the remains are as old as the Sangamon, but it is also possible that they belong to the close of the Wisconsin stage (p. 215).

The writer knows of no other fossil vertebrates that have certainly been found within the area occupied by the Illinoian till as a surface deposit.

As shown by map 36, by far the larger number of Pleistocene vertebrates which have been discovered in Ohio have been met with within the region occupied by the Wisconsin drift-sheet. One reason for this preponderance is the greater area included. Another reason may be found in the fact that the conditions were more favorable for the preservation of teeth and bones. Much of the country was flat and swampy and the bones buried in clay and muck have always been soaked with water. Also there has been less erosion going on. Erosion leads to exposure and therefore to destruction of skeletons.

On the map referred to are shown the various moraines that were left by the Wisconsin ice-sheet in its retreat toward the north. Inasmuch as most of the burials were in swamps resting on the drift, the animals must have lived and died there after the ice had left that vicinity; how long after one may not be able to determine. The mastodons and elephants which have been found close to the shore of Lake Erie, especially if buried near the surface, must have lived there at or after the time when the waters had shrunken into Lake Warren. Such cases are furnished by the mastodons and elephants found at Amboy (east of Ashtabula) (pp. 137, 150), at Cleveland (p. 79), and in Brownhelm Township, in Lorain County (p. 79). The town of Amboy is about 130 feet above lake level and the gravel-pit which there furnished Elephas primigenius and E. columbi was probably at about the same level. The writer has not been able to confirm any case in which remains of proboscideans have been met with on the south shore of the lake at a level lower than the Warren beach. Mastodons may be traced to a lower level at the western end of the lake. The one found in Springfield Township, Lucas County (p. 77), was buried in deposits only about 45 feet above Lake Erie. As shown by the topographical maps, the descent from this place and from Bowling Green, Wood County, to the lake is a gradual one. It may become possible to follow the presence of the mastodons, the elephants, and the giant beaver in Ohio up to the time when the lake assumed its present level.

For information regarding the several interesting discoveries of the giant beaver (Castoroides ohioensis) pages 273 to 275 may be consulted.

It is hardly necessary to take up one by one all the cases of vertebrates that have been met with within the area covered by Wisconsin drift. With the few exceptions noted below, their geological age is usually to be regarded as Late Wisconsin. Along the southern border of this drift, where the remains are deeply buried, it is not unlikely that they lie in a pre-Wisconsin interglacial deposit. Along Great Miami and Muskingum Rivers there is always a possibility that the fossils may occur in a terrace or in a deep valley deposit of Illinoian age.

About a mile east of Overpeck, Butler County, there has been found the skull of an extinct bear, Ursus procerus Miller (Hay, Geol. Surv. Indiana, vol. XXXVI, 1912, pp. 772–776, figs. 71–73). It was found at a depth of 28 feet and about 3 or 4 feet above the limestone rock of that region. To the writer it seems quite certain that the Wisconsin drift had been penetrated and that the skull was in either a Sangamon interglacial deposit or something still older.

Columbus furnishes one of the rare cases in which horse remains have been found within the Wisconsin glaciated area (p. 186). We are then required to determine whether or not the horse, Equus complicatus, did not live there after the close of the Wisconsin stage. As said on the page cited, the first remains of horses discovered at Columbus were reported as having been found in crevices of the limestone and in the red clay filling such fissures. An examination of the Columbus Folio (197, U. S. Geol. Surv., p. 8) will show that in such crevices, south of Scioto River, a red clay is found which antedates the Illinoian drift, so that one might fairly refer the horse remains reported by Whittlesey to a pre-Illinoian interglacial stage, possibly the Aftonian. The horse-teeth found in the excavations at the penitentiary close to Scioto River may be as old as those found in the rock fissures, or they may have been buried in a post-Illinoian interglacial deposit. Such deposits have been found at various places in the quadrangle (fol. cit., p. 9).

As to the peccaries discovered at Columbus (p. 214), the writer sees no reason why they should not be regarded as belonging to the Late Wisconsin.

MICHIGAN.

To understand the Pleistocene geology of the southern peninsula of Michigan, it is indispensable to study Monograph LIII of the U. S. Geological Survey, by Frank Leverett and F. B. Taylor. The whole peninsula is overlain by glacial deposits laid down by the Wisconsin ice-sheet. A glance at their glacial map (plate VII) will indicate to the student the complexity of glacial problems in this region. The ice invaded the State from three sides: on the west from Lake Michigan, on the east from Lake Huron, and on the southeast from Lake Erie.

On the west, close to Lake Michigan, is a system of Lake-border moraines. This system has been traced more or less satisfactorily around to Saginaw Bay, Lake Huron. A little farther out, in the southwestern corner of the State, is Valparaiso moraine. This extends nearly to the northern end of the peninsula, where it connects with Charlotte moraine system. Farther in than the Valparaiso system is the Kalamazoo. This extends northeastwardly from the Indiana line to Barry County, where it turns east and at Jackson joins the Mississinawa system reaching northeast from the northeastern corner of Indiana. The Valparaiso and Kalamazoo moraines are in places closely associated. The attack on the eastern side of the State came principally from a lobe which flowed through Saginaw Bay. Nearest Lake Huron, following it around from Port Huron to the northern end of the peninsula and then turning west, the Port Huron moraine connected with the moraine along Lake Michigan.

Farther inland is the Charlotte system. On the north, just above latitude 44°, this joins the Valparaiso moraine, runs southward west of Lansing, then turns eastward, then northeastward, and connects with the Defiance moraine, which passes around the western end of Lake Erie. Reaching far out from the head of Saginaw Bay, and concentric with it, to Hastings, 100 miles away, are many minor moraines.

Besides the Wisconsin drift which forms the surface deposit in Michigan, there are, according to present indications, one or more pre-Wisconsin drifts. Leverett (Monogr. LIII, p. 72) mentions several localities where what appears to be more indurated till is encountered, sometimes at a depth of 100 feet. Taylor (op. cit., pp. 289–290) states that “a till older than that deposited by the Wisconsin ice-sheet seems to underlie more or less continuously all of the later, or Wisconsin, drift in Indiana and the southern peninsula of Michigan.” Along the western shore of Lake Huron, north of Port Huron and along the streams, as reported by Taylor (p. 290), there are several exposures of Illinoian till, in some cases as much as 30 to 50 feet thick. In one case there is an old soil at the top of this till. In such old soils it may be possible to find fossil vertebrates of Sangamon or Peorian times, horses for example.

The fossil vertebrates found up to the present time in Michigan are not numerous in species or individuals; all appear to belong to the middle or late Wisconsin times. A peccary, Platygonus compressus, has been found at Belding, Ionia County (p. 215). Two musk-oxen have been discovered in the State. At Manchester, Washtenaw County, has been found a fine skull of Symbos cavifrons (p. 250). At Moorland, Muskegon County, was obtained a skull which has been called Boötherium sargenti.

Details regarding the mastodons which have been found in Michigan are given on pages 80 to 88. Only two localities in the State have furnished remains of Elephas primigenius. These are Three Oaks, Berrien County (p. 137), and Eaton Rapids, Eaton County (p. 137). Elephas columbi has been encountered only once in the State, as far as is known; this was in the northern part of Jackson County (p. 151).

Elephants belonging quite certainly to either E. primigenius or E. columbi, but for one reason or another not determined, have been found in four localities. These are East Saginaw, Saginaw County; Macomb County; Grand Ledge, Eaton County; and Buchanan, Berrien County. (See page 171.)

The giant beaver, Castoroides ohioensis, found a congenial home in the swamps of southern Michigan in the late Pleistocene. It has been met with somewhere in Berrien County; at Adrian, Lenawee County; at Ann Arbor, Washtenaw County; at Attica, Lapeer County; and at Owosso, Lapeer County (pp. 275–276).

INDIANA.

(Map 37.)

Whoever wishes to gain a knowledge of the Pleistocene geology of Indiana, as it is understood to-day, must study Leverett’s two great treatises, forming Monographs XXXVII and LIII of the U. S. Geological Survey. The first is entitled “The Illinois Glacial Lobe,” and was published in 1899; the second has the title “The Pleistocene of Indiana and Michigan and the History of the Great Lakes.” The portion of the latter monograph which deals with Michigan was written by F. B. Taylor. On pages 33 to 54 is a very full bibliography of the subject, consisting of about 400 titles.

From the glacial map of Monograph XXXVIII, plates V and VI, the writer has prepared map 37. This shows which part of the State has escaped glaciation, which has been subjected to the action of the Illinoian ice-sheet, and which has been covered by the last, or Wisconsin, glacial ice. It will be seen that about one-sixth of the State, that forming an irregular triangle whose apex is in Brown County and whose base is formed by the Ohio River, has never been covered by glacial ice. North of this is a bilobed area which is covered by till of Illinoian age. The rest of the State (somewhat less than two-thirds of it) is overlain by the débris left by the Wisconsin ice-sheet and subsequent deposits.

This northern area is to a great extent occupied by belts called moraines, along which the materials are usually coarse, often full of boulders, and frequently standing at a higher level than the surface on each side of them. These moraines show where for long periods during its retreat, or perhaps sometimes its advances, the ice-sheet paused and piled up a part of its load of rocks, gravel, and sand. It will be noticed that these moraines are somewhat concentric. On the right of the map are seen those moraines which were left by the ice-lobe which came down Lake Erie and later retired in that direction. Around the southern end of Lake Michigan are the moraines laid down by the ice of the Michigan lobe. The latter will be better seen on a glacial map of Illinois (Monogr. U. S. Geol. Surv. XXXVIII, plate VI). In their advance the two lobes met and coalesced and produced more or less irregular and anastomosing moraines.

On the right hand the moraines of the Erie lobe pass on into Ohio, where, however, they have often been given other names. On the left the moraines of the Lake Michigan lobe continue into Illinois and retain the same names. Both groups of moraines are prolonged into the southern peninsula of Michigan.

On account of the comparatively recent recession of the Wisconsin ice-sheet, the surface has not become eroded sufficiently to drain away the water which was left in depressions of the surface. A large part of Indiana is, or has been until recently, covered by swamps, lakes, and ponds, and in such localities the bones and teeth of vertebrate animals are best preserved during the early stages of fossilization. For this reason great numbers of teeth and bones, sometimes nearly whole skeletons, are met with in draining these swamps.

The southern border of the Illinoian drift, beginning at Cincinnati, follows Ohio River on the Kentucky side to Jeffersonville, then passes west of north into Brown County, whence, turning southwest, it strikes the East Fork of White River in Du Bois County; thence, following White River a short distance, it crosses the Wabash in Posey County. Northward, along this terminal moraine (map 37, figs. 1, 2) of the Wisconsin drift, the Illinoian, passing beneath this, disappears from the surface.

The surface of the Illinoian area is better drained than the Wisconsin area. Fewer fossils are found, and on various accounts they are of less value. Usually the exact locality and kind of deposit is not recorded. They may be found washed out of river and creek banks and may have in reality been buried in sediments that were laid down in Wisconsin times by the streams that carried away the mud, sand, and gravel from the glacier. The driftless area has been exposed for many geological ages to the influence of physical and chemical agencies. Its surface is, therefore, more diversified by hills and valleys and streams. In the limestones of this region caves are likely to be found, and these now and then furnish fossil bones and teeth.

During more than one of the glacial stages, perhaps during the earliest, the Ohio has served as the drainage-way for the waters that escaped from the glacial front. This subject is discussed by Leverett in Monograph XLI of the U. S. Geological Survey. As a result of this conveyance of glacial waters, the great trough of this stream may contain here and there deposits of the Illinoian stage or even of older deposits. Remains of Megalonyx (p. 32) and of a horse (p. 186) have been found in the right bank of the Ohio, at Evansville, Indiana. At Bigbone Lick, Kentucky, close to the Ohio, horses have been discovered, Mylodon and Megalonyx. These seem to occur in Sangamon interglacial beds overlying the Illinoian.

The Illinoian drift, probably everywhere in central and northern Indiana, underlies the Wisconsin. For some miles back from its terminal moraine the Wisconsin drift is thin; and possibly the Illinoian may. be found exposed in creek or river banks, or in railroad cuts. Furthermore, Leverett (Monogr. LIII, p. 72) writes:

“Probably a considerable number of the heavy deposits of drift in central and northern Indiana are of pre-Wisconsin age, but as they are largely sand and gravel, or loose-textured material, they can not easily be discriminated from the Wisconsin.”

Such deposits are likely to be covered by only a thin layer of Wisconsin till. In many places in Indiana there have been found, deep down in the drift, old soils, muck beds, and vegetation in various forms. These beds appear to indicate interglacial deposits, most probably the Sangamon. Now, various genera of vertebrates, among them horses, tapirs, and mylodons, are not known to have existed after the Wisconsin glacial stage. If, however, remains of such animals should be collected in central or northern Indiana, or Ohio, or in southern Michigan, they might be reported as having been found in late Wisconsin beds, when really they had been derived from pre-Wisconsin interglacial soils.

It is interesting to observe that when the Wisconsin ice-sheet began to withdraw lakes began to form along its borders. One of these, Lake Chicago, appeared at the south end of the present Lake Michigan and for a long time discharged its waters down Illinois River. Another, Lake Maumee, occupied the basin of Maumee River as far west as Fort Wayne, and emptied down the Wabash. For details connected with the close of the Pleistocene in the region of Lake Michigan the reader should consult Frank C. Baker’s “The Life of the Pleistocene, or Glacial Period” (Univ. Ill. Bull. XVII, 1920).

A brief mention will be made here of the principal Pleistocene vertebrates that have been found in Indiana; also the localities where found, together with citations of the pages where fuller information is furnished.

The ground-sloth Megalonyx has been collected near Evansville (p. 32). With it were secured remains of an undetermined bison (p. 257), a Virginia deer (p. 228), a horse (p. 186), a tapir (p. 203), and the dog Ænocyon dirus (p. 32). Peccaries have been found in Gibson County (p. 216), in Wabash County (p. 218), and two species at Williams, Lawrence County (p. 217). At the same place was discovered the shell of a box-tortoise. Remains of deer have been discovered somewhere in Vanderburg County, including the existing deer and an extinct species, Odocoileus dolichopsis; at Harrisville, Randolph County; and at Roann, Wabash County. Bisons of an extinct species have been secured at Vincennes (p. 258).

The existing bison appears to have been found in Jasper County (p. 268). Of musk-oxen, Symbos cavifrons has been collected at Hebron, Porter County (p. 252); at Wailesboro, Bartholomew County (p. 251); somewhere in Randolph County (p. 252); and probably in Beaver Lake, Newton County (p. 252). The existing musk-ox, Ovibos moschatus, has been discovered near Richmond (p. 252).

Mastodon remains are not uncommon, especially in the northern half of the State. It is hardly to be supposed that these animals were more abundant there during the late Pleistocene than in many other places in the region east of the Mississippi. The conditions for their preservation were evidently more favorable there than anywhere else, unless in Orange County, New York. Burial in swamp mud kept the bones from decay; and the imperfect drainage protected them from destruction by erosion. The various finds are described on pages 88 to 100.

Elephants are less well represented in Indiana than are the mastodons, but are not rare (pp. 138, 151, 171). Two species were present in the State, Elephas primigenius and E. columbi. Beavers were doubtless abundant, but there appears to be no definite record of any find. However, the giant beaver has been recorded from several localities (pp. 276 to 278).

The great extinct dog Ænocyon dirus was first found near Evansville (p. 32), and the coyote, Canis latrans, has been reported from Boone County. The latter is said to have been found in association with the mammoth (Cope and Wortman, 14th Ann. Rep. Geol. Surv. Indiana, p. 7).

ILLINOIS.

(Map 38.)

As a foundation for a knowledge of the Pleistocene geology of Illinois, the student must take Leverett’s work entitled “The Illinois Glacial Lobe.” This is Monograph XLVIII of the U. S. Geological Survey, a volume of 817 pages, with maps and figures. For a knowledge of the changes which occurred around the south end of Lake Michigan on the retirement of the Wisconsin glacier, see Dr. Frank C. Baker’s work, “The Life of the Pleistocene, or Glacial, Period” (Univ. Ills. Bull. XVII, 1920).

Illinois is eminently a glaciated State, as is to be recognized on Leverett’s plate VI. A little triangle in the northwestern corner, comprising about 600 square miles, and an irregular tract of perhaps 3,000 square miles at the southern end of the State constitute the whole of the unglaciated area out of 56,650 square miles. Two glacial stages are prominent, the Wisconsin and the Illinoian. The first was laid down by the Lake Michigan lobe, which sent its icy mass southwestward as far as Shelbyville. Westward the border moraine extends to Peoria, then north to west of Princeton, then northeast to enter Wisconsin 55 miles west of Lake Michigan. Eastward, of course, the deposits of till and the moraines extend into Indiana. North of the Shelbyville moraine is the Champaign. A more powerful moraine is the Bloomington, which forms a loop through the State, extending from Danville, Illinois, through Bloomington to Peoria, where it appears to have overridden the Shelbyville and thence northward, forming the outer border of the Wisconsin drift area. North of this moraine is located that called the Marseilles, while sweeping around the south end of Lake Michigan into Indiana and Michigan is the Valparaiso system.

South and west of the area of the Wisconsin drift is the Illinoian. At Mount Vernon the border crosses the Wabash and traverses Illinois, striking the Mississippi River at Carbondale. It then follows the Mississippi north to a point above Keokuk, where it enters Iowa. It reenters Illinois between Rock Island and Clinton and extends into Wisconsin.

On Leverett’s map (Monogr. XXXVIII, plate VI) there is indicated in northern Illinois, between the Illinoian and the Wisconsin, a tract supposed to belong to the Iowan; but Alden (U. S. Geol. Surv., Prof. Pap. 106, 1918, p. 173) holds that there is no good evidence that the Iowan extends into southern Wisconsin and Illinois. The supposed Iowan (op. cit., plate III) is mapped as Illinoian.

The glacial stage which preceded the Illinoian is the Kansan. This in Iowa extends eastward to the Mississippi, and one might naturally expect that it would be found underlying the Illinoian east of the river. Leverett (Monogr. XXXVIII, p. 105) presents evidences of its presence in western Illinois. Among these evidences is the presence in Hancock and Adams Counties of another till sheet below the Illinoian and separated from it by a black soil. This Kansan or some other pre-Illinoian till sheet has been found in many places in Illinois (op. cit., pp. 107–118).

Animal remains are not likely to be inclosed in the materials of the moraines or of the intermorainal till; but this is possible. A musk-ox or a hairy mammoth might have died not far away from the foot of a stationary or advancing glacier and its bones might have become incorporated in the moraine. Furthermore, inasmuch as any glacial stage began while the glacier was yet in the far north and ended only when it got back there, many non-glacial deposits belonging to that glacial stage were probably laid down south of it; and it would be difficult or impossible to distinguish these from interglacial deposits. However, it was these deposits which were laid down after the glacial ice had withdrawn, whether glacial or interglacial, which are of more interest to the palæontologist, because in them are to be found the fossil remains of animals and plants.

The last of the interglacial stages, that which immediately preceded the Wisconsin and followed the Iowan, is known as the Peorian. This takes its name from a locality a few miles east of Peoria (Leverett, Monogr. XXXVIII, p. 187). Here the Shelbyville till sheet is underlain by a bed of fossiliferous loess from 8 to 12 feet in thickness. Beneath the loess is fully 100 feet of Illinoian drift. This loess seemed to the geologists who examined it to be a deposit of more recent date than the Sangamon.

The Peorian interglacial stage and the preceding Iowan glacial stage have received much attention within recent years. In 1917 (Geol. Surv. Iowa, vol. XXVI, pp. 49–212), Alden and Leighton presented the results of their studies on the Iowan drift and the loess associated with it. In 1918 (U. S. Geol. Surv., Prof. Pap. 106, pp. 1–356), Alden dealt with the Quaternary geology of southeastern Wisconsin. The results of these investigations have been to establish the fact that a sheet of till intermediate between the Illinoian and the Wisconsin had been laid down, that which had already been designated as the Iowan; furthermore, that immediately following this there was deposited a covering of loess. It was further concluded that this is the main loess deposit, much of what has been regarded as Sangamon loess being really loess of a later stage, the Peorian.

As no Iowan drift is known to be present in Illinois to separate the loess of the Sangamon from the Peorian, it must be difficult, often impossible in our present state of knowledge, to distinguish the one from the other. The Sangamon loess was laid down probably long after the Illinoian ice disappeared, so that there was time for the Illinoian drift to become leached and otherwise modified and for the accumulation of old soils and peat-beds.

On the other hand, the old soils of the Peorian stage are likely to overlie the loess. Unfortunately, the desired indications of geological age are not always present where bones and teeth are found; or, if present, are not always observed. We must, therefore, make our assignments of fossils to one stage or the other with great circumspection or leave the decision in abeyance.

Reference has already been made to the presence of Kansan drift in western Illinois and of black soils intervening between it and the Illinoian. Such soils must be referred to the Yarmouth interglacial stage. Whether or not still older glacial or interglacial deposits occur in Illinois is problematic.

In Illinois any considerable number of species of fossil vertebrates are rarely found together. The localities are widely scattered and a single species or two in each is the rule (map 38). In later glacial deposits around the south end of Lake Michigan have been discovered the dogfish Amiatus calvus and a sun-fish belonging to the genus Lepomis. Baker (Univ. Ill. Bull. XVIII, p. 85) reported the humerus of the merganser, Mergus serrator, from the same region. The ground-sloth Megalonyx jeffersonii (pp. 33–34) has been found at Urbana, Galena, and Alton.

The few horses are described on page 187. Peccaries have been found at three localities (p. 218). For the specimens of deer that have come to light, see page 229. A species of Cervalces and the moose Alces americanus have been met with in Will County (p. 107). The reindeer has been recognized from poor materials found at Alton. The prong-horn Antilocapra appears to have lived in the region of Galena, as shown by Wisconsin specimens. The remarkable antelope Taurotragus americanus has been found at Alton (p. 339). As to the musk-oxen and the bisons, the reader may refer to pages 251, 259, 268; for the mastodons and elephants, to pages 100, 140, 152, and 176.

Of the rodents, the muskrat has been found about Chicago; the pocket gopher at Alton and Galena; the ground hog at the same places (p. 343). The beaver (p. 339) likewise occurs at Alton. The giant beaver, Castoroides ohioensis, has been collected at four widely removed places (p. 279). The rabbit, Sylvilagus floridanus, was included among the animals found in the lead crevices of the region about Galena, where also have been found an extinct species of raccoon, Procyon priscus, what appears to be a large dog Canis (or Ænocyon) mississippiensis, the coyote, Canis latrans, and the fox Urocyon cinereoargenteus. The bear, Ursus americanus, and the common gray wolf, Canis nubilus, appear to have existed in the middle Pleistocene at Alton.

A skull of Felis couguar, the yet existing panther or mountain lion, has been found in Randolph County, in the bed of Kaskaskia River. It probably belongs to the late Pleistocene.

A considerable fauna has been secured in the lead region about Galena, in Illinois, Iowa, and Wisconsin. The collectors and describers of this were not careful to designate the localities, and in some cases these can not at present be determined. These collections are discussed on page 343, in the account of the geology of Wisconsin.

An interesting list of Late Wisconsin mammals has been secured near Whitewillow, Kendall County. From Dr. E. S. Riggs, of Field Museum of Natural History, and from Netta C. Anderson’s list, the writer learns that at least six skulls of the common mastodon, together with many other parts of the skeleton, has been taken from a well 10 feet in diameter (p. 109). Above, there were bones of bison (p. 269), deer (p. 229), and elk (p. 240). It is stated that a layer of these about 2 feet thick was encountered at a depth of about 5 feet.

Mr. George Langford, of Joliet, states that he made a collection of bones 15 miles west of Joliet and 5 miles west by north of Minooka. The more exact locality he gave as township 35 north, range 8 east, and probably section 27, on the farm of John Bamford. Apparently both Riggs and Langford obtained their materials at the same spot. The latter has sent the writer some bones from this place, including those of Cervalces, Alces americanus, and a leg-bone of some undescribed species of sheep or goat. He also reported the finding of the elk. For other remarks see page 269. This locality is in the region mapped by Leverett as having been occupied, after the retirement of the Wisconsin glacial ice, by temporary lakes. The presence of the moose here seems to indicate a climate somewhat severer than that now prevailing in that region. Since the occupancy of the country by the European race the moose has not been known to come further south than northern Wisconsin. The list of species obtained is as follows: Mammut americanum, Ovis sp. indet., Odocoileus virginianus, Cervus canadensis, Alces americanus, Cervalces roosevelti?.

A brief description of the bone referred to Ovis is presented. The lower epiphysis is missing, but an allowance is made for this (fig. 13).

Comparisons of the metatarsals of a sheep, of a goat, of Næmorhedus, and of Orvis sp. from Whitewillow, in millimeters, together with indices in one-hundredths of the length.

┌──────────────┬───────┬─────╥───────┬─────╥──────┬─────╥───────┬─────┐ │ Measurements │ │ ║ Capra │ ║ │ ║White- │ │ │ taken. │ Næmo- │Indi-║hircus │Indi-║ │Indi-║willow │Indi-│ │ │rhedus.│ces. ║155623.│ces. ║Sheep.│ces. ║animal.│ces. │ ├──────────────┼───────┼─────╫───────┼─────╫──────┼─────╫───────┼─────┤ │Length on │ │ ║ │ ║ │ ║ │ │ │ outer border│ │ ║ │ ║ │ ║ │ │ │ of bone │ 170│ 100║ 120│ 100║ 152│ 100║ 185±│ 100│ │Side-to-side │ │ ║ │ ║ │ ║ │ │ │ width of │ │ ║ │ ║ │ ║ │ │ │ upper │ │ ║ │ ║ │ ║ │ │ │ articular │ │ ║ │ ║ │ ║ │ │ │ surface │ 36│ 21.2║ 23│ 19.2║ 23│ 15.1║ 37.5│ 20.3│ │Fore-and-aft │ │ ║ │ ║ │ ║ │ │ │ width of │ │ ║ │ ║ │ ║ │ │ │ upper │ │ ║ │ ║ │ ║ │ │ │ articular │ │ ║ │ ║ │ ║ │ │ │ surface │ 30.5│ 17.4║ 20│ 16.7║ 21│ 13.8║ 37.5│ 20.3│ │Side-to-side │ │ ║ │ ║ │ ║ │ │ │ width, at │ │ ║ │ ║ │ ║ │ │ │ middle of │ │ ║ │ ║ │ ║ │ │ │ length │ 23│ 13.5║ 15│ 12.5║ 14│ 9.2║ 19.0│ 10.3│ │Fore-and-aft │ │ ║ │ ║ │ ║ │ │ │ width at │ │ ║ │ ║ │ ║ │ │ │ middle of │ │ ║ │ ║ │ ║ │ │ │ length │ 17.5│ 10.3║ 11.5│ 9.1║ 13│ 8.6║ 20.0│ 10.8│ │Side-to-side │ │ ║ │ ║ │ ║ │ │ │ width at │ │ ║ │ ║ │ ║ │ │ │ lower end │ │ ║ │ ║ │ ║ │ │ │ just above │ │ ║ │ ║ │ ║ │ │ │ epiphysis │ 38│ 22.4║ 27│ 22.5║ 27│ 17.8║ 35.0│ 19.5│ │Side-to-side │ │ ║ │ ║ │ ║ │ │ │ width across│ │ ║ │ ║ │ ║ │ │ │ lower │ │ ║ │ ║ │ ║ │ │ │ articular │ │ ║ │ ║ │ ║ │ │ │ surface │ 41│ 24.1║ 27.2│ 22.5║ 25│ 16.4║ │ │ └──────────────┴───────┴─────╨───────┴─────╨──────┴─────╨───────┴─────┘

From Alton, the U. S. National Museum has come into possession of a collection which furnishes 15 species of fossil mammals. This was made some time before 1883 by Hon. William McAdams, of Alton. It was briefly mentioned by him at the Minneapolis meeting of the American Association for the Advancement of Science in 1883 (Proceedings, vol. XXII, p. 268). Apparently the collection was secured for the U. S. Geological Survey by Professor O. C. Marsh and remained at Yale University until after his death. The species were described by the writer in 1920 (Proc. U. S. Nat. Mus., vol. LVIII, pp. 109–117). This collection seemed especially valuable because the species were found inclosed in supposed nodules of loess. In our country the loess has furnished few such remains. The following is the list of the species as determined. Those marked by a dagger are extinct.

†Megalonyx jeffersonii (p. 33). †Equus sp. indet. (p. 187). †Platygonus cumberlandensis? (p. 219). †Sangamona fugitiva. †Cervalces roosevelti?. †Rangifer muscatinensis? (p. 246). †Taurotragus americanus. †Symbos cavifrons (p. 254). †Bison sp. indet. (p. 259). †Mammut americanum (p. 102). Castor canadensis. Marmota monax. †Castoroides ohioensis (p. 279). Geomys bursarius. Ursus americanus.

Of these 15 species at least two-thirds are now extinct. This large number might appear to indicate that the time of their existence was rather early in the Pleistocene. However, it is quite certain that the loess belongs somewhere about the middle of the Pleistocene; and there are no species that require an earlier date.

After the writer’s descriptions of the fossils had been published, an important paper on the geology of the locality was issued (Jour. Geol., vol. XXIX, 1921, pp. 505–514) by Professor Morris M. Leighton, who had been commissioned by the Illinois Geological Survey to visit and study the deposits involved. With the aid of Mr. John D. Adams, son of the collector of the mammalian fossils, Professor Leighton succeeded in finding the quarry in which most of the fossils had been collected.

At one quarry in Alton Professor Leighton obtained the following geological section, the description of which is here somewhat abridged:

Feet. Soil loessial, dark brown, leached 1 Loess, brown above, grading below into buff, leached 4 to 5 feet, maximum thickness 20 Loess distinctly more reddish than that above; many fossil snails, thickness about 30 Glacial till, reddish, with pebbles of Canadian rocks; more oxidized than overlying loess; thickness 1–3 Mississippian limestone, about 100

The concretions which hold the mammalian fossils were found to lie between the upper surface of the till and the overlying loess; occasionally a concretion bears a drift pebble. The concretions have resulted from the lime which in solution was brought down from the loess and again precipitated so as to cement the loess materials around the fossils.

Professor Leighton was not able to determine definitely the ages of the till and of the two deposits of loess. As to the till, its geographic location suggested that it belonged to the Illinoian, but it had many of the characteristics of the Kansan. The latter is believed to be present at St. Louis and other localities not far away. Before the overlying reddish loess had been deposited the till had suffered weathering and erosion, indicating a considerable lapse of time had intervened. The lower reddish loess presented many evidences that it is a deposit distinct from the upper buff loess; and there seemed to be some indications of at least a short interval between them. Leighton’s conclusion was as follows:

If the drift is Kansan in age, the reddish loess may be Sangamon; if, on the other hand, the drift be Illinoian, the reddish loess probably is Peorian. It is unlike any Peorian loess of which the writer knows, but the color does not necessarily preclude that possibility.

As to the upper loess, Leighton thought it might be of early Peorian age, but possibly of early Wisconsin. However, his final conclusion was thus expressed:

“If the till proves to be Kansan in age, the weathering of the drift may be credited to the Yarmouth interglacial epoch, the mammalian fauna to late Illinoian or early Sangamon times, the reddish loess probably to the Sangamon, and the buff loess to the Iowan.... However this may be, the Illinoian and Sangamon epochs are post-mid-Pleistocene from the standpoint of duration of the Pleistocene and the fauna represented by the McAdams collection may be regarded as post-mid-Pleistocene.”

WISCONSIN.

The greater part of this State is covered by the drift-sheet which has derived its name from the State, but in the southwestern corner is a considerable tract which has never been subjected to glacial action. A small part of this area extends southward into Illinois and another part into northeastern Iowa. In Wisconsin it reaches eastward to Baraboo. East of this driftless area is a tract lying along the southern border of the State and reaching eastward about to 88° 40′ longitude, which is covered by the Illinoian drift.

The most detailed geological survey of any part of Wisconsin, so far as regards the Pleistocene, is that made by Dr. W. C. Alden, of the U. S. Geological Survey, of the area comprised between the boundary of the State on the south and 44 degrees of latitude on the north and between Lake Michigan on the east and 90 degrees of longitude on the west. On the western side it joins the Mineral Point Quadrangle, to be mentioned further along. There is, therefore, a wide strip surveyed across the whole State. The area treated by Alden is, of course, nearly entirely covered by Wisconsin drift. In the southwestern corner a considerable part of the driftless region is included. East of this, as already stated, is a tract which the Wisconsin ice-sheet did not reach and which shows Illinoian ground moraine and some terminal moraines of Illinoian drift. This narrows as it approaches its eastward limit.

Alden (p. 166) informs us that at no place in the area subjected to vigorous glaciation by the Wisconsin ice-sheet had soils or vegetal deposits been found between the Wisconsin drift and the earlier drifts. At several places, however, deposits have been discovered which probably belong to earlier glacial stages. Just outside the area mapped by Alden, in Calumet and Outagamie Counties, Lawson (Bull. Wis. Nat. Hist. Soc., vol. II, pp. 170–173) has recorded the discovery of much wood and other vegetable matter. Baker (“Life of the Pleistocene,” p. 317) has referred the deposits to the Sangamon. These interglacial deposits of uncertain age need not be here noted further. In this Wisconsin area some remains of mastodons and elephants have been met with, but all are relics of a time after the partial or complete recession of the Wisconsin glacier. Remains of two individuals of Elephas primigenius have been found in Milwaukee (p. 143). It is evident that they lived there after the withdrawal of the Wisconsin ice-sheet. One of these was buried beneath peat and clay at a depth of 10 feet or more and at a level of about 100 feet above the present level of Lake Michigan.

At Dover, in Racine County, in 1878, a proboscidean tusk and some bones were found in a peat-bog. They have been identified as those of a mastodon, but of this one can not be certain. The age of the deposits is that of the Late Wisconsin stage, after the withdrawal from that vicinity of the ice, but how long after one can not say. The Milwaukee Public Museum has a tooth of a mastodon (p. 111), labeled as found at Waukesha. Its geological age is that of the other remains here referred to. In the collection of the University of Wisconsin is a large vertebra of a proboscidean which was found in Lake Monona. Its time of burial must have been late Wisconsin. Inasmuch as no remains of vertebrate animals have yet been found in Wisconsin, in the area covered by the Illinoian drift, it is not necessary to dwell on this region. It is not certain that there is beneath it a still older drift; but there are, according to Alden, some indications of such deposits.

For a knowledge of the driftless area, first of all, may be consulted the report made by Chamberlin and Salisbury in 1885 (6th Ann. Rep. U. S. Geol. Surv., pp. 199–322, with plates). Alden’s work above referred to maps a part of the region. Grant and Burchard have studied the geology of the Lancaster and Mineral Point Quadrangles (Folio U. S. Geol. Surv. 145). Their text-figure 1 is here reproduced, inasmuch as it shows the relation of the region to the surrounding glaciated areas (fig. 14). The topographical map of Folio 145 and that of Chamberlin and Salisbury will show the uneven character of the surface. This has resulted from the erosion undergone during the whole of the Pleistocene. Much of the area is covered with a coating of loess. Along Mississippi River this may be as much as 10 feet thick, but at a distance of from 30 to 40 miles it becomes reduced to a few inches. Considering this erosion, one might conclude that few vertebrate remains would be preserved; nevertheless they are not wholly missing.

In 1862 (Geol. Surv. Wisconsin, vol. I, p. 136), J. D. Whitney stated that he had found in a crevice at Blue Mounds, Wisconsin, remains of the mastodon (p. 111), a peccary (p. 219), bones and teeth of a buffalo (p. 270), and a wolf which he referred with doubt to Canis latrans. The depth was uncertain, but it may have been as much as 40 feet. The fossils were embedded in reddish clayey loam, the usual crevice earth. On page 422 of the same volume, Jeffries Wyman referred the wolf remains to two distinct species, Canis occidentalis and C. latrans. In 1876, Dr. J. A. Allen (Amer. Jour. Sci., ser. 3, vol. XI, pp. 47–49) described from the same lot of bones the species C. mississippiensis. This apparently did not include jaws and teeth that Wyman had referred to C. occidentalis. In Wyman’s paper, on page 422, he assigned three teeth to Dicotyles torquatus, an existing peccary, without stating that it had been found at Blue Mounds. In 1869 (Jour. Acad. Nat. Sci. Phila., ser. 2, vol. VII, p. 384), Leidy referred this peccary to his Dicotyles lenis, an extinct species. Inasmuch as the peccaries found at Galena were identified by Leidy (Whitney, vol. cit., p. 424) as Platygonus compressus (p. 218), it appears pretty certain the Dicotyles lenis (Tagassu lenis) was among the fossils collected at Blue Mounds (p. 219). It must, however, be kept in mind that Whitney, on page 35, stated that he had collected bones and teeth of the same animal near Dubuque, Iowa. Allen regarded the buffalo as belonging to an extinct species; but it is really undeterminable. Accordingly there may be credited to this locality the following species: Tagassu lenis, Bison sp. indet., Mammut americanum, Canis nubilus (C. occidentalis), C. mississippiensis, C. latrans.

In Whitney’s report, on page 133, he announced the finding of a large quantity of bones of mastodons at Sinsinawa Mound (p. 111), but he did not know at what depth they occurred. It seems probable that they had been met with in one or more crevices.

It seems probable that the animals found in crevices in the lead region of Wisconsin, Illinois, and Iowa belong approximately to one geological stage of the Pleistocene. The following appears to include all known to have occurred in such situations:

Megalonyx jeffersonii?. Platygonus compressus. Tagassu lenis. Odocoileus virginianus?. Cervus canadensis. C. whitneyi. Antilocapra americana. Bison sp. indet. Mammut americanum. Marmota monax. Microtus sp. indet. Geomys bursarius. Sylvilagus floridanus? (Lepus sylvaticus). Anomodon snyderi. Procyon priscus. Canis nubilus (C. occidentalis). C. mississippiensis. C. latrans.

The writer was at one time inclined to believe that these animals belonged to the time succeeding the withdrawal of the Wisconsin ice-sheet. Baker (“Life of the Pleistocene,” p. 353) thinks that they belong probably to the Peorian, inasmuch as the region is covered by Iowan loess, beneath which many of the bones have been found. It is quite probable that those crevices were open during at least some part of the Pleistocene and that animal remains collected in them. The fossils are reported as being sometimes inclosed in a matrix of cave or fissure materials which are cemented together by iron. The considerable number of extinct species, certainly 7 out of about 18, makes it probable that the fauna is not so recent as the Late Wisconsin.

It appears to be determined that the Iowan loess was formed immediately after the retirement of the Iowan ice-sheet. It might, therefore, be a question whether all of these animals might have got into those crevices in time to be covered in by the loess. On the other hand, the Illinoian drift was, for a long time, exposed to weathering and erosion before the Iowan drift and loess were laid down. Also, the Sangamon interval was probably much longer than the Peorian, so that the chances for the accumulation of the fossils were greater. It seems, however, that we can only say that the fossils are post-Illinoian and probably pre-Wisconsin.

Besides the vertebrate fossils referred to above, a few others, especially mastodons (pp. 110, 111), have been found at other places, but so little is known of the conditions of their interment that they furnish little geological information.

A very interesting region is found in the western part of the State, in Dunn and Pepin Counties. This has been examined with great care by Dr. Samuel Weidman, State geologist of Wisconsin. About Menomonie there are several brickyards, whose excavations furnish opportunities for studying the formations at that point. Sections of one of these brickyards are described and illustrated by Dr. E. R. Buckley, in Bulletin VII, part 1 (1901), page 194, plate XXXVII. A section and brief description is found also in a paper by Dr. Hussakof (Jour. Geol., vol. XXIV, p. 688). In that region are found outwash gravels which have been definitely correlated by Weidman with Iowan drift. In some places this is overlain by loess. These gravels vary from 10 to 20 feet in thickness at Menomonie. Beneath the gravels are found lacustrine clays varying in thickness from 20 to 40 and even 60 feet. These are stratified and consist of layers from 1 to 12 inches in thickness, with intervening thin layers of sand. Toward the bottom the sand increases in amount. Beneath the clay-bearing formation is a bed of sand attaining a maximum thickness of about 150 feet. This is underlain by coarse sand and gravel. The lacustrine clays and the underlying sands and gravels are included by Weidman in his Menomonie formation, and this is believed by him to be of Sangamon interglacial age. In northwestern Wisconsin are found other glacial deposits believed to belong to the Illinoian drift epoch.

In the lacustrine clay at Menomonie have been found remains of the great lake trout, Cristivomer namaycush (Hussakof, as cited above), of a deer (p. 230), a caribou (p. 247), and probably a mastodon. The deer is represented by a single vertebra, identified by Dr. W. D. Matthew. The supposed mastodon is indicated by the distal end of the right femur, the caribou by an antler of a young and probably female individual and by the shaft of a large individual.

At Woodville, in St. Croix County, about 20 miles west of Menomonie, has been found a forest bed regarded as belonging to the Aftonian. This was described by Arthur Koehler (Amer. Forestry, vol. XXVI, Feb. 1916, p. 92, 3 figs.). Wood was found that was identified as that of spruce.

In 1913 (Science, n. s., vol. XXXVII, p. 457), in a brief abstract, Weidman reported that in Wisconsin he recognized drift deposits of Wisconsin, Iowan, and Kansan ages and another still older. No localities were mentioned, but his statements were doubtless based mostly on his work in the western part of the State. The loess was found to be laid down after the Iowan and before the Wisconsin. Interglacial deposits were found between the Kansan and the Iowan.

In 1905 (Jour. Geol., vol. VIII, pp. 238–256) and in 1910 (Jour. Geol. vol. XVIII, pp. 542–548), Dr. R. L. Chamberlain presented the results of his investigations on the “Pleistocene Geology of the St. Croix Region in Western Wisconsin.” His conclusion (p. 548) was that in that part of the State there were present (1) a surface mantle of gray Wisconsin drift deposited by a glacier from the Keewatin center; (2) red Wisconsin drift deposited by a glacier coming from the Labrador center; (3) a red drift left by an ice invasion from the Labrador center, its age consistent with Illinoian; (4) a grayish-black till that had come from the Keewatin center and whose age was probably Kansan.

MARYLAND AND DISTRICT OF COLUMBIA.

For obvious reasons the Pleistocene geology of the District of Columbia is considered in connection with that of Maryland. This region is of especial interest, because of the long time and the care which has been bestowed on it by geologists and because the conclusions reached have been applied to the geological study of States both toward the north and toward the south.

The most complete exposition of the Pleistocene geology of the region is to be found in the volume of the Maryland Geological Survey entitled “Pliocene and Pleistocene,” published in 1906. The geological treatise itself was written by George Burbank Shattuck and is illustrated by many maps and text-figures. Included in this is a bibliography of the subject which occupies 17 pages. There is a chapter by W. B. Clark, Arthur Hollick, and F. A. Lucas, on the interpretation of the palæontological criteria; another by F. A. Lucas on the mastodons and the elephants. The Pleistocene mollusks found in the State, 40 species, were described and figured by W. B. Clark; while the plants, also nearly 40 in number, were described and figured by Arthur Hollick.

The history of the development of our present knowledge of the geology of Maryland and the classification of its formations up to 1906 is given by Shattuck in the volume just cited (pp. 25–40). This geologist recognized in the superficial deposits of the State five formations (fig. 15). These are, beginning with the oldest, Lafayette, Sunderland, Wicomico, Talbot, and Recent.

The Lafayette is regarded as having been laid down during the Pliocene. The Sunderland, Wicomico, and Talbot form three terraces, of which the Sunderland is the oldest, most elevated, and farthest away from the larger bodies of water. It is composed of clay, peat, gravel, and boulders supposed to have been brought in by the ice. The coarser materials appear to occupy usually the lower parts of the formation. The elevation near Washington is about 200 feet, but southward it descends gently, until in St. Mary’s County it is only about 60 feet. The thickness varies from about 80 feet to nothing. According to Shattuck, at the time of deposition of the Sunderland the coast was depressed to an extent of about 200 feet, so that its materials were laid down either in salt water or in that of wide estuaries. No deposits belonging to it have been found in the eastern peninsula. In the western peninsula considerable areas are recognized along the Potomac up to Washington and along the Patuxent and Chesapeake Bay to Baltimore and Elkton. Except in the southern part of this peninsula, the Sunderland is found only in widely separated patches. No marine organisms are known to have left their remains in the Sunderland, but forest trees of a number of existing genera and several extinct species have been described by Hollick in the volume cited.

The Wicomico formation is described as occupying a large portion of the central and higher parts of the eastern peninsula; in the western it forms a narrow and often interrupted fringe around the Sunderland. North of Washington and Annapolis it occurs only in patches. Its materials are very similar to those of the Sunderland. Its greatest elevation is about 100 feet above sea-level, and this, according to Shattuck’s view, marks the amount of depression of the land at that time. The thickness may be as much as 70 feet, but is usually much less. No marine fossils proper to the period have been discovered in the deposits, but at a point in Prince George’s County plant remains have been found in a deposit about 20 feet thick.

The Talbot formation forms a fringe, sometimes of great width, sometimes narrow or interrupted, along all the large bodies of water in this State and in Delaware. It is the lowest of the terraces. The greatest elevation is about 45 feet; the thickness does not exceed 40 feet. The materials noted are those of the other two formations—clay, peat, sand, gravel, and ice-borne boulders. At several points along Chesapeake Bay and on the lower part of Patuxent and Potomac rivers, deposits containing plant remains have been discovered, including pines, cypress, hickory, beech, elm, and black locust. In contrast with the other formations, the Talbot has furnished many marine fossils, mostly mollusks; but in all cases the localities are close to the present coast.

The writer does not accept the theory that the materials forming what have been called the Sunderland, Wicomico, and Talbot terraces have been to any great extent laid down in the sea. Some part of the Talbot, that lying near the present coast, has undoubtedly had such an origin. Nor has the Coastal Plain suffered, so far as is determinable, any such amount of depression as the theory mentioned requires. The materials of the Sunderland and Wicomico have, in the writer’s opinion, been brought down by rivers whose beds lay at levels nearly as high as those of the real or supposed terraces. When the Talbot materials were laid down, the rivers and estuaries of the coast had been cut down nearly to their present levels, and this was not long after the beginning of the Pleistocene.

The authors of the submergence theory admit that no satisfactory evidence of the presence of marine organisms, vertebrate or invertebrate, are to be found in the body of the assumed terraces, except again in parts of the Talbot which immediately border the ocean or the great estuaries. It is almost inconceivable that the ocean could occupy the Coastal Plain from New Jersey to Mexico for thousands of years and lay down great thicknesses of clay, sand, and gravel without having left somewhere beds of molluscan shells in such situations that they would have been discovered. While these marine fossils are lacking, there are found on all these terraces from Maryland to Florida and to the Rio Grande an abundance of land vertebrates such as elephants, mastodons, horses, camels, peccaries, and many other forms. Nor do our palæobotanists have difficulty in finding oaks, walnuts, hickories, poplars, etc. On the theory of submergence there are missing all the things that ought to be found and there are met with just the things that would not be expected.

A figure is here reproduced (fig. 15) from the Maryland Pliocene and Pleistocene volume, page 66, with the explanation there accompanying it. The reader may judge for himself whether the sea could occupy the Atlantic coast since Pliocene times without leaving any traces of marine fossils, while at the same time there were preserved in those terraces remains of land animals and land vegetation.

Another section (fig. 16) is reproduced from Folio 179 of the U. S. Geological Survey, the authors of which are G. W. Stose and C. K. Swartz. The uppermost terraces are by these authors supposed to belong to the late Pliocene, the formation formerly known as the Lafayette. These figures suggest that the one set of terraces have some connections with the other set.

Beginning at the southern extremity of Maryland, we notice the occurrence of remains of Mammut americanum at or near St. Mary’s City. Other remains of the same animal have been secured near St. Clements in St. Mary’s County (p. 112). Both of the localities are situated on territory mapped by Shattuck as Wicomico; but as remarked on page 112, our knowledge of the conditions under which the fossils were found is not sufficient to allow us to say more than that they belong to the Pleistocene. The species existed from early to late Pleistocene and can not be used to determine the age of the deposits.

Along Patuxent River, in Charles County, not far from Benedict, Cope (Proc. Acad. Nat. Sci. Phila., 1867, p. 155) recognized jaws and teeth of Grison macrodon and of Tagassu lenis (p. 220). Both are extinct species.

According to Shattuck’s map of 1906, this region is covered by the Talbot formation; but inasmuch as the species named were obtained from pits furnishing Miocene marl, one can not be sure that they are not older than the supposed Talbot. It would probably require a search in the land records in order to determine exactly where the objects were found. The presence of Elephas primigenius suggests that this animal had been pushed down here during one of the glacial stages.

Nearly a hundred years ago an elephant tooth (p. 154) was found somewhere in Queen Anne County, but it would probably be now impossible to determine the locality. In case the elephant tooth was found near Chesapeake Bay, as is very probable, there is no record of any Pleistocene vertebrate having been found in the central and eastern parts of the eastern peninsula.

In the eastern peninsula remains of Pleistocene vertebrates have been recorded from only two localities, Oxford Neck, Talbot County, and an undetermined locality in Queen Anne County. From Oxford Neck, Cope (Proc. Amer. Philos. Soc., vol. XI, 1869, p. 178) reported Elephas primigenius, E. columbi, Cervus canadensis, Odocoileus virginianus, Chelydra serpentina, and Terrapene eurypygia.

At Chesapeake Beach, William Palmer, of the U. S. National Museum, discovered a few remains of Pleistocene vertebrates. One of these is a tooth of an undetermined species of Bison, probably not the existing one. Another species is probably Equus leidyi (p. 189). Three teeth appear to represent the peccary Tagassu lenis (p. 220). In 1921, Dr. Adolph H. Schultz, of the Johns Hopkins Medical School, presented to the U. S. National Museum another specimen of T. lenis which he had found at Chesapeake Beach. Inasmuch as the fossils were picked up after having fallen from their resting-place, it is impossible to say to which formation they belonged. In the opinion of the writer, none of the three species indicates a late Pleistocene time.

On the opposite side of the western peninsula, at Marshall Hall, Charles County, there was found long ago a tooth which the writer refers to Equus leidyi.

Coming north into the District of Columbia, we find recorded the discovery of remains of horses and possibly at two different times. According to Darton’s work (Folio 70, U. S. Geol. Surv.), there is some later Columbia laid down along the route of the Chesapeake and Potomac Canal above Georgetown. This would now doubtless be regarded as belonging to the Talbot. It seems to follow that either the Talbot is much older than has been supposed or that some of the extinct horses continued on until a comparatively late time in the Pleistocene.

Within the limits of the city of Washington there has been found a tooth of probably Elephas primigenius at a depth of 35 feet, in the Wicomico formation (see p. 178). On any theory of the origin of the terraces, the presence of the tooth at that depth in the ground and at that elevation appears to indicate a considerable geological age for the animal. To what extent materials may have been washed down from the surrounding higher land may be difficult to determine.

In Prince George County, near Mitchellville, have been found two teeth of an extinct horse (p. 188). These are as yet unidentified. They are in the U. S. National Museum, No. 8813.

Near Towson, in Baltimore County, a mastodon tooth has been found (p. 112); but beyond proving that there is at that locality some Pleistocene deposit, it gives us little information.

In 1920 (Proc. U. S. Nat. Mus., vol. LVIII, pp. 96–109), the writer described a collection of vertebrate fossils, collected in a cave or fissure in limestone at Cavetown, Washington County, by anthropologists from Phillips Academy, Andover, Massachusetts. The following is the list of species that were found in the collection:

Crotalus horridus. *Equus complicatus (p. 189). *Equus giganteus? (p. 189). *Mylohyus nasutus (p. 220). *M. exortivus (p. 220). *M. obtusidens, n. sp. (p. 220). *Platygonus tetragonus? (p. 220). *P. vetus? (p. 220). *P. cumberlandensis (p. 220). *Sangamona fugitiva. Odocoileus virginianus (p. 231). *Elephas columbi? *Sciurus tenuidens, n. sp. S. hudsonicus. S. carolinensis. Marmota monax. Castor canadensis. Ondatra zibethica. Neotoma magister. Microtus pennsylvanicus. Erethizon dorsatum. Sylvilagus floridanus. Ursus americanus. *Smilodontopsis mooreheadi. Felis couguar.

Of the 22 species here recognized 12 are extinct. This large number of itself indicates that their time of existence was not recent. Similarly, the presence of 2 species of horses, several species of peccaries, and of a saber-tooth tiger points to a rather ancient period. The writer believes that the assemblage belongs to the Sangamon stage of the Pleistocene.

In Washington County, probably along Lane’s Creek, was found, in digging a mill-race, the skull of a mastodon (p. 112). Further east, near Clear Spring, and about a mile above the entrance of Conococheague Creek into the Potomac, was discovered a tooth of a mastodon (p. 113). This had been washed out of some deposit along this creek, probably not far away from where it was found. As Stose has shown (Hancock Folio, No. 179, U. S. Geol. Surv.), along the Potomac and its tributary streams there are extensive Pleistocene deposits of sand and gravel, laid down when the river was as much as 200 feet above its present level. It is probable that such deposits date from the early Pleistocene (fig. 17). A more important locality for Pleistocene vertebrates is that near Corriganville, about 3 miles west of north of Cumberland, Maryland. The cave is in Allegany County, west of Wills Creek and south of Jennings Run, about 0.5 mile south of the village of Corriganville. An account of this locality, with a list of the species determined up to that time, has been published by Gidley (Proc. U. S. Nat. Mus., vol. XLVI, 1913, pp. 93–102). In cutting through a spur of limestone in making a railroad, at a depth of about 100 feet there was exposed a cave or fissure which contained many bones and teeth. Gidley secured some hundreds of specimens belonging to about 35 species. Unfortunately nothing has been published which shows the relation of this cave to the terraces which are found along Potomac River and its tributaries. Through the kind offices of Mr. F. S. Rowe, welfare agent of the Western Maryland Railway, the writer has received from the division engineer, Mr. P. Cain, of Cumberland, a topographic map of Allegany County and a profile of the road extending through the rock cut. From these it appears that the level of the track, at the fissure, is 837 feet above sea-level. This seems, therefore, to be considerably above the highest terrace along the Potomac in that region. It is to be supposed that the fissure was formed long before the animal remains accumulated in it.

In a paper published in 1920 (Proc. U. S. Nat. Mus., vol. LVII, pp. 651–678, plates LIV, LV, text-figs. 1–10) Gidley added to his former list four species of peccaries, as follows: Platygonus cumberlandensis, P. intermedius, Mylohyus exortivus (all new), and M. pennsylvanicus. In another communication he reported also a deer, a wolverine, a beaver, a lynx, a badger, a marten, an eland, and a crocodile or an alligator (Rep. Smithson. Inst. for 1918, pp. 281–287). Many of the identifications are merely provisional.

Provisional list of fossils found near Corriganville.

1. Alligator or Crocodylus sp. indet.

2. Blarina brevicauda?.

3. Vespertilio grandis.

4. Vespertilio sp. indet.

5. Myotis sp. indet.

6. Ursus vitabilis.

7. Ursus americanus?.

8. Canis armbrusteri.

9. Canis sp. indet.

10. Vulpes? sp. indet.

11. Mustela vison?.

12. Gulo luscus?.

13. Taxidea sp. indet.

14. Lynx sp. indet.

15. Mammut americanum.

16. Equus sp. indet. (p. 189).

17. Tapirus haysii? (p. 204).

18. Platygonus cumberlandensis (p. 220)

19. P. intermedius (p. 220).

20. P. vetus? (p. 220).

21. Mylohyus exortivus (p. 220).

22. M. pennsylvanicus (p. 220).

23. Odocoileus sp. indet.

24. Taurotragus americanus.

25. Ochotona princeps?.

26. Lepus americanus?.

27. Lepus sp. indet.

28. Sciurus hudsonicus.

29. Sciuropterus alpinus?.

30. Marmota monax?.

31. Castor sp. indet.

32. Neotoma sp. indet.

33. Microtus chrotorrhinus?.

34. Synaptomys borealis?.

35. Synaptomys sp. indet.

36. Peromyscus leucopus?.

37. Napæozapus sp. indet.

38. Erethizon sp. nov.

On account of the present unstudied condition of the collection, it is difficult to reach conclusions that are satisfactory. It appears, however, that there are at least 6 hitherto undescribed species, one-fifth of the whole number. Another 6, if at all correctly determined, indicate a wide removal from their ranges of the present day. Lepus americanus now lives well toward the north, coming down to Saginaw, Michigan. Ochotona princeps lives in the Rocky Mountains of British America. Synaptomys borealis is known only from the region about Great Bear Lake, Mackenzie, Canada. Microtus chrotorrhinus has its habitat in Quebec and the northeastern United States. The species of Napæozapus are Canadian in their range, but descend to southeastern Maryland and to North Carolina in the mountains. Sciuropterus alpinus is found from Alaska to Hudson Bay, but descends on the Pacific coast to southern California. This northern habitat of so many supposed species suggests that the fissure received its contents during one of the glacial stages, and this may be the case. However, it is not unlikely that these species and some others are really undescribed ones. One may reasonably expect to find in a fauna containing Equus and Tapirus a much higher percentage of extinct species than Gidley has recorded.

The most remarkable member of the fauna is Taurotragus americanus, a species closely related to the eland of southern Africa (Gidley, Smiths. Misc. Coll., vol. LX, No. 27). Its presence in western Maryland gives a vivid impression of the widely extended journey that some animals have made from one continent to others. The same species has since been found in collections made at Alton, Illinois (p. 339), and at Kimmswick, Missouri (Proc. U. S. Nat. Mus., vol. LVIII, p. 113).

According to the author’s views, the fauna found at Cumberland, like that of localities in western Virginia, belongs to a time somewhere about the middle of the Pleistocene. Most of the species may be supposed to have lived there during the warm Sangamon stage; others, as the wolverine, at a somewhat earlier or later time when the climate was cooler.

VIRGINIA.

For the student of Pleistocene vertebrate palæontology, as for the geologist, Virginia may be divided into three physiographic regions, the Coastal Plain, the Piedmont Plateau, and the Appalachian Mountains. The line which divides the Coastal Plain from the Piedmont Plateau begins at the southern boundary of the State, at about 77° 31′ longitude. The towns on or not far from this nearly north-and-south line are Emporia, Petersburg, Richmond, Hanover, and Fredericksburg. Near the latter the line inclines slightly eastward and passes a few miles west of Alexandria and Washington, D. C. The Coastal Plain is much less elevated than the region west of it and consists of deposits of Mesozoic or Cenozoic age, and much of it is covered by Pleistocene materials. The Plateau region is elevated and consists mostly of Palæozoic rocks, mostly metamorphosed into a crystalline condition. The Appalachian region presents nearly parallel ranges of mountains and intervening valleys.

For a knowledge of the Pleistocene geology of the Coastal Plain the reader should consult Bulletin iv, 1912, of the Virginia Geological Survey. The authors who discuss the physiography and geology of this region are William B. Clark and Benjamin L. Miller. On pages 19 to 45 they present a very full bibliography of the geological literature pertaining to this region. Additional valuable assistance may be obtained from the various folios issued by the United States Geological Survey, but unfortunately not many species of vertebrate animals have been found on this Coastal Plain of Virginia.

In Bulletin IV, already mentioned, Clark and Miller recognize the presence of three terraces belonging to the Pleistocene. To these are given the names applied in Maryland and North Carolina to what are regarded as equivalent terraces. The oldest of these, most elevated and farthest from the coast, is the Sunderland; eastward of this lies the Wicomico; the Talbot is the youngest and lowest and borders the coast. Unfortunately, the geologists referred to did not map the areas occupied individually or collectively by these terraces. They accept the theory that these terraces were laid down in the sea. It is admitted, nevertheless, that no marine fossils are found in deposits of the Sunderland and Wicomico. In the Talbot, 26 species of marine mollusks have been reported from Talbot deposits of the Dismal Swamp Canal, all regarded as belonging to living species. It will be recollected that Woolman (Proc. Acad. Nat. Sci. Phila., 1898, p. 414), in a study of mollusks collected in the Dismal Swamp Canal, found 7 extinct species in a collection of 49 species, equal to about 16 per cent. It is, however, not unlikely that the collections had been dredged up from deeper deposits.

In Bulletin V of the Virginia Geological Survey, on page 25, Sanford stated that the Talbot had a width of 30 miles at the south. On consulting Stephenson’s map of the superficial formations of the Coastal Plain in North Carolina (North Carolina Geol. Surv., vol. III, plate XIII) it will be seen that this corresponds quite exactly with the width of the Pamlico formation at that line. For the writer’s views on the terraces named the reader may consult page 346 on the geology of Maryland.

On page 113 is recorded the discovery of a tooth of a mastodon in a marsh near Disputanta, in Prince George’s County. Not enough is known about the geology of the region to say more than that the deposit belongs to the Pleistocene.

About 6 miles east of Williamsburg, a little more than 100 years ago, remains which pretty certainly belonged to the genus Mammut and probably to the species M. americanum (p. 113) were discovered, said to have been found on the banks of York River; but by this was probably meant the banks of the flood-plain. The bones were found in marsh mud and were surrounded by roots of cypress trees. The adjacent bank was 20 feet higher than this level. The topographical map of the Williamsburg Quadrangle shows that an abrupt rise of this amount is to be found only about 10 miles away from the river. Whether the cypress roots were those of trees that had grown within recent years or whether they were remains of a Pleistocene forest, such as was exposed at Tappahannock, Essex County (Bull. IV, p. 186), the writer does not know. The information at hand about this case does not make it possible to pronounce on the geological age of the mastodon.

On page 28 an account is given of the discovery of a skull of a walrus on the Atlantic coast of Virginia, at Accomac. It had doubtless been washed up by the sea from a Pleistocene deposit. It is easiest to suppose that the walrus had been driven southward along the coast during the Wisconsin glacial stage; but possibly this happened during an earlier glacial time.

No vertebrate fossils of Pleistocene age appear to have come to light anywhere on the Piedmont Plateau, and little or nothing is known about its Pleistocene geology.

From the geological surveys we get little information about the Pleistocene formations of the Appalachian region. At most, mention is made of soils of undetermined age along the streams; and yet from this region have been obtained a very considerable number of Pleistocene vertebrates.

From Mr. Wyndham Robinson, of Abingdon, Washington County, the U. S. National Museum received in 1869 a tooth of Mammut americanum (p. 113) and one of Equus complicatus (p. 189). Nothing has been learned regarding the conditions under which they were unearthed. The horse-tooth points to an age preceding the Wisconsin drift.

From Saltville, in Smyth County, the following forms have been obtained:

Crocodylus sp. indet. Megalonyx dissimilis (p. 34). Equus sp. indet. (p. 190). Odocoileus? sp. indet. (p. 231). Cervalces sp. indet. Bison sp. indet. (p. 259). Mammut americanum (p. 113). Elephas primigenius (p. 145).

That a crocodile should have lived in this region during the Pleistocene is remarkable. Megalonyx dissimilis is otherwise known only from Natchez, Mississippi, from deposits which appear to be of about Illinoian or Sangamon age. The horse-tooth points to about this time or earlier, while the other species do not contradict this conclusion. The astragalus referred to Odocoileus probably belongs to some other genus.

Mr. M. D. Mount sent to the U. S. National Museum remains of Bison (p. 259), Mammut americanum (p. 113), and Elephas primigenius (p. 145). These, he reported, had been found at a depth not greater than 8 feet in excavating for the city reservoir. He has written that the valley of Holston River at Saltville, within about 80 years, had been a lake, at least at certain times of the year, and that the reservoir was excavated at the margin of this low area.

Mr. O. A. Peterson (Ann. Carnegie Mus., vol. XI, 1917, pp. 469–474) reported from this place the crocodile, the megalonyx, cervalces, the supposed deer, the horse-tooth, and remains of mastodons. The bones were found in a sink-hole, in a layer of coarse gravel, pebbles and cobblestones, a fact indicating that a stream of some size had occupied the place. Overlying this layer was one in which there were fragments of large river shells. The bone layer appears to have been only about 4 feet from the surface. Peterson concluded that at the close of the Pleistocene or later the remains had been moved and redeposited from some place not far away, but this would not affect the geological age of the fossils and it is evident that remains of vertebrates are widely dispersed in that valley. All the species reported are extinct, but only large forms were secured.

Professor Cope, probably in 1868, found the following 24 species. He did not state the localities exactly, except that they were along New River, in Wythe County. Two were on the land of Abraham Painter. The writer applied to the surveyor of the county named and has been informed that the farm which belonged to Abraham Painter is on New River, near the town of Ivanhoe. The nomenclature of the species has been revised. The species preceded by a dagger are extinct.

†Megalonyx jeffersonii (p. 34). Castor fiber. Neotoma floridana? Marmota monax. Peromyscus leucopus. †Tamias lævidens. †Sciurus panolius. Sylvilagus floridanus. Blarina sp. indet. Vespertilio sp. indet. †Tapirus haysii (p. 204). †Equus complicatus? (p. 190). †Mylohyus nasutus (p. 221). Odocoileus virginianus (p. 231). †Bison sp. indet. (p. 260). †Ursus amplidens. Procyon lotor. Spilogale putorius. †Myxophagus spelæus. Crotalus sp. indet. Amyda sp. indet. Terrapene sp. indet. Cryptobranchus sp. indet.

At least 9 of the 24 species are extinct. None of the recorded species requires us to refer the deposit to early Pleistocene times. Ursus amplidens was described from the deposits at Natchez. This and Tapirus haysii, Equus complicatus, and Mylohyus nasutus point to middle Pleistocene, apparently about to Illinoian or Sangamon times.

Cope reported that the teeth and bones were found in a cave breccia. This consisted of a number of irregular masses which occupied “depressions and short galleries” in the southeast side of a line of hills. When those masses were excavated from their beds the floor and roof of a portion of a cave were exposed, with the stalactites, stalagmites, and usual incrustations. It would appear, therefore, that at some time in the early Pleistocene or in the late Pliocene the caves had been formed through the effect of streams of carbonated waters on the limestone; that in some way the bones and teeth of the animals listed above had got into the cave; that by a change in the amount or character of the water the caves had gradually filled up; and that afterwards the limestone which contained these caves had undergone great erosion.

Further north, in the valley of Jackson River at Covington, there is evidently a deposit of Pleistocene clay, for in it at a depth of 12 feet was found a tooth of a mastodon (p. 114). Another mastodon tooth was found near Hot Springs, at the head of Wilson Creek, in Bath County, possibly in similar deposits (p. 114). In Augusta County an unidentified species of horse (p. 190) and the peccary Platygonus (p. 221) have been discovered.

WEST VIRGINIA.

So far as the writer has learned, vertebrate remains belonging to the Pleistocene have been found in West Virginia in only eight places and only seven species are represented: Mammut americanum (p. 115), Elephas sp. indet. (p. 179), Equus niobrarensis? (p. 190), Symbos cavifrons (p. 254), Megalonyx jeffersonii (p. 34), Odocoileus virginianus? (p. 231), and a peccary (p. 221). The horse appears to indicate an early Pleistocene time, possibly pre-Kansan, but all the other species continued from at least the Aftonian stage through to the Late Wisconsin. The specimens, therefore, do not help us to determine the age of the deposits in which they are found.

No part of the State lies within the glaciated area; hence, during the whole of the Pleistocene epoch its surface was subjected to weathering and to the erosion of running water. At times the streams built up deposits on their beds. Later they deepened their channels and left a part of their former deposits as terraces. At a still later time the deposition and deepening may have been repeated, and as a result there is sometimes a series of terraces one above another. The age of these terraces and their origin have been the subjects of a good deal of controversy.

In the Masontown-Uniontown Folio (U. S. Geol. Surv. No. 82), M. R. Campbell has discussed the terraces along the Monongahela River, which occur at an altitude of about 1,000 feet above sea-level and perhaps 150 feet above the present river. Also more than 100 feet above the present river are old abandoned river channels which are now partially filled up.

In 1911 (U. S. Geol. Surv. Folio 178, pp. 11–13), E. W. Shaw and M. J. Munn described the Quaternary of the Foxburg and Clarion quadrangles in Pennsylvania, where the same Pleistocene problems are involved. They present an account of the different views regarding the high-level terraces and the abandoned channels. They concluded, as did Campbell, that these terraces and channels dated back to the early Pleistocene and probably to the Kansan stage. Figure 17 is a reproduction of Shaw and Munn’s figure 10, on their page 12. It represents a section across Allegheny River at Parker’s Landing, Armstrong County, Pennsylvania. The uppermost gravels in the figure would be those of supposed Kansan age; while the lowermost are those laid down during the last glacial stage, the Wisconsin. In the materials of the high terraces one may expect to find fossil vertebrates of the early Pleistocene, as in the case of the mastodon reported from Stewartstown, West Virginia (p. 116). The conditions of burial should, however, be carefully studied and recorded; for it would be possible for remains to be left at a later time on such a terrace and to be covered up by earth washed down from above.

On page 254 an account is given of finding a musk-ox skull near Steubenville, Ohio, on a terrace about 75 feet above the low-water mark. The region of the western part of West Virginia, western Pennsylvania, and northeastern Ohio is interesting because of its history during the late Pleistocene. The reader is referred to Leverett’s monograph, “The Glacial Formations and Drainage Features of the Erie and Ohio Basins” (Monogr. U. S. Geol. Surv., vol. XLI, 1902, pp. 88–158, with figs.). Leverett essays to show that the upper part of the Ohio River, the Allegheny, and the Monongahela with its branches at one time emptied into Lake Erie. The connection was made through Beaver River, which now flows into the Ohio, and Grand River, in eastern Ohio, now emptying into Lake Erie. When the Wisconsin ice filled Lake Erie and occupied its southern shore the mouth of Grand River was dammed and the water could escape only to the south. The flow was reversed, and after it had reached the top of the divide it entered the stream that then represented the head of the Ohio. When at length the mouth of Grand River was reopened, the new channel had been cut so deep that most of the streams of western Pennsylvania and West Virginia continued to flow down the Ohio. Leverett’s figure representing the preglacial drainage of the upper Ohio region is here reproduced (fig. 10).

NORTH CAROLINA.

(Map 39.)

Our knowledge of the Pleistocene geology of North Carolina is at present confined almost wholly to the Coastal Plain of the State. The most recent general discussions of the geology of this region are found in volume III of the North Carolina Geological and Economic Survey, 1912. The authors who contributed to this volume are William Bullock Clark, Benjamin L. Miller, L. W. Stephenson, B. L. Johnson, and Horatio N. Parker. L. W. Stephenson has furnished an article on the Cretaceous deposits, and in his numerous geological sections he has referred to the Pleistocene materials there found. Benjamin L. Miller wrote on the Tertiary formations and likewise noted the Pleistocene materials found in his sections. The most important part of the volume for the student of the Pleistocene is Stephenson’s article on “The Quaternary Formations,” which occupies pages 266 to 290. Clark, Miller, and Stephenson united in a chapter on the “Geological History of the Coastal Plain of North Carolina.” Clark, besides, deals with the “Correlation of the Coastal Plain Formations.” In addition to numerous plates and text-figures, a colored map shows the area covered by the surficial formations of the Coastal Plain and another the distribution of the formations exclusive of the surficial. Finally, Miller and Stephenson presented a bibliography which includes 150 titles, occupying pages 44 to 73.

According to Clark and Stephenson, the Pleistocene of North Carolina comprises five formations; the oldest is the Coharie, farthest removed from the coast and lying back against the so-called Lafayette, itself supposed, with some doubt, to belong to the Pliocene. Toward the coast there come in, in succession of position and time, the Sunderland, the Wicomico, the Chowan, and the Pamlico. These formations are described as forming more or less well-defined terraces having higher and higher elevations as they are followed back from the coast. The Pamlico nowhere exceeds 25 feet above sea-level. The Chowan varies in elevation from about 25 feet to about 50 feet. The Wicomico formation slopes from about 50 feet up to about 90 or 100 feet. The Wicomico may attain elevations of from 140 to 150 feet at the western border. The Coharie varies from about 160 feet along its eastern border to as much as 235 feet along its western border. From its western border each formation sends up the rivers prolongations into or across the next formation toward the west.

Each terrace may present along its coastward border an escarpment of varying elevation and obviousness. The Coharie and Sunderland formations are regarded by the authors named as being correlated with the Sunderland of Virginia and Maryland, although the Coharie may be really Pliocene. The Wicomico is equivalent to that called by the same name in the States farther north, while the Chowan and the Pamlico together are correlated with the Talbot of Virginia and Maryland.

The area occupied by the Pamlico is extremely narrow or absent along the southernmost third of the coast of the State. At longitude 77° the boundary between it and the Chowan turns and runs north, very slightly to the east, striking the northern boundary of the State at about 76° 15′. Just south of Albemarle Sound its width east and west is nearly equal to that of all the other Pleistocene formations at that latitude, taken together.

Clark, Miller, and Stephenson (op. cit., p. 300) accept the theory of McGee that during Lafayette times, probably in the late Pliocene, the Coastal Plain was depressed some 500 feet below its present level and covered by the sea. Into this sea were poured, by the rivers coming down from the higher lands to the west, the clay, sand, and gravel, sometimes boulders, which make up the so-called Lafayette. Somewhat later the region was uplifted enough to expose the Lafayette deposits and they suffered erosion. When the Coharie formation began to be laid down the sea-level must have been about 160 feet higher than at present; it continued to rise until it reached an elevation of about 200 feet. A subsidence and a succeeding elevation occurred, during which the Sunderland terrace was produced. In like manner the succeeding deposits and terraces are supposed, by the geologists named, to have been formed—the Wicomico, the Chowan, and the Pamlico.

One objection already offered (p. 346) to this theory to account for the deposits belonging to the Lafayette and the formations of the Pleistocene is that, instead of beds of sea-shells, remains of marine fishes, porpoises, and whales, there are found scattered here and there over this region the bones and teeth of elephants, mastodons, horses, and other land animals. In maintaining this objection it is not necessary to assume that the lower parts of the Pleistocene area have never been submerged.

The writer has caused to be prepared a map showing the geographical distribution of the five formations referred (in the work cited) to the Pleistocene. It is based on the maps found in that volume. It shows also the localities where fossil vertebrates have been discovered, and where marine fossils and land plants have been secured (map 39).

One difficulty met with in our study of the distribution of the finds of extinct vertebrates in North Carolina, as elsewhere, arises from carelessness in recording and preserving proper data. In several cases here to be considered, no more is known than that a fossil has been found in a certain county. Happily, more is known in many other cases.

Examination shows that no fossil vertebrates are known to have been found in North Carolina within the area of the Coharie formation, but that mastodons have been met with in the areas of all four of the other formations as laid down in Stephenson’s map, plate XIII of the work cited above. Horse remains, too, seem to have occurred within all the areas last noted. This does not mean necessarily that these remains were buried in the corresponding formations. A mastodon may have lived long after the Sunderland was laid down and his remains have become buried in some isolated deposit, say of Pamlico times; or, the remains may be found within the area of Pamlico, but really buried in underlying Chowan. Each case must be decided on the evidence bearing on it.

Mention is made on page 155 of the finding of a tooth of Elephas columbi about 9 miles below Wilmington. Whether this was buried in Pamlico deposits close along Cape Fear River, in Chowan deposits which prevail there, or beneath these, in Wicomico, it is impossible to say. A short distance below this place was found a tooth of Mammut americanum.

On page 190 is given an account of the discovery of a tooth of Equus leidyi in what was supposed to be Miocene marl in the vicinity of Elizabethtown, on Cape Fear River, in Bladen County. Miller (op. cit., p. 248) states that the Pleistocene about Elizabethtown rests usually directly on the Cretaceous, but that south of the town are found some patches of Miocene marls. The region about this town is mostly occupied by the Sunderland formation, but the Wicomico extends up the river far above the place. It is, however, mapped as lying mostly on the north side of the river. It seems pretty certain that the horse-tooth occurred in the Sunderland, probably at its base.

Mastodon remains, as stated on page 115, have been found in Pender County, but where is not known. Along the coast is a narrow strip of Pamlico. The southeastern half of the county is occupied by the Chowan, the northwestern by the Wicomico.

Mastodon teeth have been found in Duplin County, but there is no record as to exact locality, depth, or matrix. The southeastern two-thirds of the county is covered by deposits of the Wicomico, the northwestern third by Sunderland. The mastodon probably belongs to one or the other of these. The Pleistocene deposits are, however, underlain by Tertiary rocks, and possibly the mastodon came from these and belongs to a different genus.

On page 116 will be found an account of remains of a mastodon, probably Mammut americanum, which was found near Jacksonville, in Onslow County. Three of the supposed Pleistocene formations are found near Jacksonville. The Pamlico comes up the New River quite to the town. Immediately at the town is (following Stephenson’s map) the Chowan. The southeastern border of the Wicomico comes down nearly to the town. In which of the three areas the teeth were discovered we do not know. A case is here furnished which illustrates the need of most accurate observation and record of locality, depth, and character of materials.

As stated on page 116, teeth and tusks of Mammut americanum have been obtained at Maysville, Jones County. The writer does not know exactly the place where the remains were discovered. The region about Maysville is occupied by the Chowan formation, but the Pamlico sends an extension up White Oak River as far as Maysville.

Remains of both Mammut and Elephas have been reported from Carteret County. In 1828 (see p. 117) Elisha Mitchell stated that remains of the elephant and mastodon had been met with in digging the Clubfoot and Harlow Canal. This canal passed from Neuse River to Newport River. In 1876 (Senate Ex. Doc. No. 35, 44th Congr., p. 17) S. T. Abert transcribed, from an earlier report made by Professor Olmstead, a geological section taken in this canal. The excavation went to a depth of 16 feet. The uppermost of the four layers consisted of the peaty mold usually found in the swamp. The next layer was made up of a yellowish-brown potter’s clay. The third layer consisted of sand and was full of sea-shells and fossil remains of “mammoths” (mastodons) and elephants. The shells belonged to species now found near Cape Lookout, principally conch, scallop, and clam. The layer below this was blue clay. In the case here presented there can hardly be a doubt that the stratum containing the shells and the bones belonged to a Pleistocene formation older than that assigned to the Pamlico.

On page 145 is described a tooth of Elephas primigenius, dredged up in Core Creek, forming part of the Inland Waterway in Carteret County. The conclusion seems unavoidable that this boreal animal had been driven to this southern latitude during one of the glacial stages, and one naturally thinks of the latest one, the Wisconsin; but it may have been at a much earlier time. A mastodon jaw has been secured in the same canal.

Doubtless the locality in North Carolina, the most important to the student of Pleistocene vertebrate palæontology, is that reported long ago on the northern shore of Neuse River, 16 miles below Newbern. As stated on page 117, in a mention of the mastodon bones discovered, H. B. Croom seems first to publish a statement concerning the animal remains found there. Some of his identifications were certainly wrong. According to Harlan (Amer. Jour. Sci., vol. XLIII, 1842, p. 143), there were secured remains of elephant, mastodon, hog, elk, deer, horse, seal, cetaceans, a tortoise, snake, fish, shark, and skate. As in another case, Harlan may have mistaken worn teeth of Bison for teeth of the hog (Sus). For our purpose the most important animals of the list are the elephant, the mastodon, and the horse. According to Croom, the animal remains were found in a marl pit. He was informed by the owner that in an upper layer there were found teeth of sharks and fragments of bones of marine fishes, mingled with sea-shells. In a deeper layer, 20 to 25 feet below the surface, there occurred the remains of land animals, together with sea-shells of great variety. Croom thought that some teeth belong to the hyena, and Foster reported the hippopotamus; but in both cases the identifications were wrong.

Conrad (Amer. Jour. Sci., vol. XXVIII, 1835, pp. 107–110; Proc. Nat. Inst. Prom. Sci., vol I, pp. 191–192) reported that the bones of animals found here were water-worn, black, and silicified. He concluded that they had been brought down the Neuse River and mingled with sea-shells. The fossiliferous stratum did not rise anywhere more than 10 feet above the river. In the first publication quoted, Conrad published a list of 66 mollusks in this stratum, of which 7 were not yet known as living species and 2 others are noted as new. According to this list, less than 90 per cent are recent. He referred the deposits to his newer Pliocene. In the second publication cited he concluded that the stratum belonged to the post-Pliocene. Stephenson (op. cit., p. 289) refers to the investigations made at this locality. It is not improbable that the deposit which furnished these fossils belongs to the earliest Pleistocene stage, the Nebraskan. The same may be said about the coquina rock mentioned by Stephenson which occurs at Old Fort Fisher, in New Hanover County (op. cit., p. 289, plate XXVIII).

On page 115 the writer refers to a lower jaw of a mastodon found by the geologist W. C. Kerr, near Goldsboro, and described by Joseph Leidy. The jaw was reported to have been found in gravel overlying Miocene marl. The writer believes that the mastodon belonged to the species Mammut progenium. Goldsboro, on Neuse River, is near the western border of the Sunderland formation, but the Wicomico is prolonged up the river far above Goldsboro. According to Stephenson and Johnson (op. cit., p. 475), Miocene sands and clays are found over a portion of the northern part of the county (Wayne). The geological age of this mastodon depends more on the age of the gravels in which it was found than on the age of the terrace, although the writer is willing to concede an early Pleistocene stage for the terrace.

A mastodon tooth has been found (see p. 117) somewhere in Wilson County. The county is covered mostly by Pleistocene of Sunderland age, but a small part of the western end is occupied by the Coharie; while, according to Stephenson’s map, both the Chowan and the Wicomico follow up Contentnea Creek into Wilson County. The geological age of the mastodon is doubtful.

At Greenville, Pitt County, have been found remains of Equus complicatus, perhaps also of another species of horse (see p. 191). While supposed to have been found in Miocene marls, the tooth belonged without doubt to the Pleistocene. Pitt County is occupied by four Pleistocene formations, Pamlico, Chowan, Wicomico, and Sunderland. The probability is that the horse-teeth were found in an early Pleistocene deposit.

As indicated on page 117, remains of Mammut americanum have been found in Pitt County, possibly at Greenville.

As noted on page 117, a tooth of Mammut americanum has been found at or near Tarboro. Nothing more is known about its origin. At this place are found deposits belonging to the Chowan, Wicomico, and Sunderland formations; it is impossible to say from which the tooth was derived.

Emmons (Geol. Surv. North Carolina, 1852, p. 56) reported finding mastodon bones in marl-pits on the farm of Mr. Knight, on the banks of Tar River, in Nash County, 3 miles west of Rocky Mount. The same Pleistocene deposits occur here as at Tarboro. The bones were supposed to have been buried in Miocene marl, and this may have been true. If so, they belonged to some other species of mastodon than Mammut americanum.

On page 191 is given an account of the discovery of teeth of Equus leidyi which were washed up on the beach at Plymouth. This town is on Roanoke River, several miles from Albemarle Sound, and on the border between the Pamlico and the Chowan formations. Our determination of the geological age of the teeth must be based on other evidence than that furnished by the discoverers.

Elsewhere in this work is given an account of finding a part of a skull of a walrus at Kitty Hawk. It was probably during the Wisconsin glacial stage that this animal lived along the coast as far south as Charleston.

As to the geological age of the Pamlico formation, the geologists who have contributed to the report of 1912, the volume cited, hold that it belongs to late Pleistocene. The writer believes that the formation was laid down at a much earlier time. The mastodon jaw and the tooth of Elephas primigenius found in the Inland Waterway Canal may have been buried there during the prevalence of the Wisconsin ice epoch; but, on the other hand, this may have happened during an older Pleistocene stage.

It will be observed that the Pamlico becomes very narrow along the southern third of the coast of North Carolina. In South Carolina it may be represented by one of the older Pleistocene deposits recorded by Sloan; in part possibly by the Wando clays or the Sea island sands. In the author’s view, it is pretty certain that the Pleistocene molluscan fauna which had been found in the Clubfoot and Harlow Canal and at the locality below Newbern corresponds to the Wadmalaw in the vicinity of Charleston. It seems to appear at the southeastern corner of the State, at Southport, and again in the northeastern corner in Dismal Swamp. According to Shaler (10th Ann. Rep. U. S. Geol. Surv., pt. I, 1890, p. 315), a collection of mollusks made near the northern border of the swamp was submitted to Dr. W. H. Dall. There were 29 forms, of which 24 are yet existing, 5 extinct. There were, therefore, 17 per cent of extinct forms. Dall regarded the deposits as belonging to the Pliocene; the writer believes that they may be referred to the Nebraskan stage of the Pleistocene.

From a study of mollusks collected later in the Dismal Swamp Canal, Woolman (Proc. Acad. Nat. Sci. Phila., 1898, pp. 414–428) concluded that they belonged to a time not earlier than late Pliocene and possibly as late as the Pleistocene. Darton (U. S. Geol. Surv., Folio 80) referred the deposits to the Pliocene. Stephenson (op. cit., p. 290) states that recent investigations have led to the conclusion that the beds should be referred to the Pleistocene. The parties in such a dispute may compromise by referring the beds to the Nebraskan stage. It seems probable that the Chowan formation belongs to a stage a little later than these mollusk-bearing beds and represents a strip of old coast marsh, inhabited by elephants, mastodons, horses, and various other animals.

In discussing the causes which led to the production of Cape Hatteras, Professor Shaler (Proc. Bost. Soc. Nat. Hist., vol XIV, 1872, p. 117) remarked that the hard shelly limestone which comes to the surface just above high-tide level along the shore of the mainland from Newbern to the mouth of the Roanoke River looks much like the shell-bed found near Charleston, South Carolina.

SOUTH CAROLINA.

To the reader who wishes to know what work has been done on the Pleistocene geology of South Carolina, two papers may be recommended. The first of these, historical in nature, was published in 1890 by Professor Joseph A. Holmes (Jour. Elisha Mitchell Sci. Soc., vol. VII, pp. 89–117), the second in 1905 by Dr. Griffith T. Pugh (Thesis, Vanderbilt Univ., pp. 1–74). Those who have contributed most to a knowledge of the palæontology of this formation are Tuomey, F. S. Holmes, Leidy, Dall, Dall and Harris, Earle Sloan, and G. T. Pugh. J. A. Holmes, Tuomey, F. S. Holmes, and Dall have made important contributions to the knowledge of the invertebrate animals. For our knowledge of the vertebrates we are indebted principally to F. S. Holmes and Joseph Leidy. The author who has dealt most recently and in considerable detail with the stratigraphy of the Pleistocene deposits is Earle Sloan, State geologist (Bull. No. 2, ser. IV, South Carolina Geol. Surv., 1908, 479 pages). From these authorities we learn that, while the larger part of the Coastal Plain may be to a greater or less extent overlain by deposits referable to McGee’s Columbian, the deposits which bear fossils are confined almost wholly to a narrow strip along the coast. In this strip have been found the numerous mollusks listed and described by Tuomey, F. S. Holmes, and W. H. Dall, as well as most of the species of vertebrate fossils. The fossiliferous deposits do not usually extend back from the coast more than about 10 miles.

Undoubtedly fossil-bearing Pleistocene deposits are to be found here and there along all the rivers, perhaps to the western border of the Coastal Plain. This is indicated by the discovery of remains of horses and mastodons in Darlington and Richland counties. The thickness of the Pleistocene deposits along the coast is said to amount to as much as 60 feet, but it is usually much less. Only a part of this is fossiliferous, a bed that appears to vary in thickness from about 3 to 8 feet. This is found as much as 8 feet above mean-tide level, sometimes below it. The materials of this fossiliferous bed vary greatly. Sometimes they consist almost entirely of shells of mollusks, in other cases of a blue mud or sand, and with these may be mingled peaty materials, gravel, and again rolled masses derived from the underlying deposits. The fossils contained in the bed mentioned consist of mollusks, and in some places bones and teeth of vertebrates occur in more or less abundance. The bed is underlain often by deposits of Tertiary age. Bones and teeth of the vertebrates, as fishes and cetaceans, that lived when those Tertiary rocks were being deposited may occasionally have been washed into the Pleistocene bed. Again, where the older and the newer beds are exposed along the shores, fossils may be washed out of both and commingled on the beach; then again, a great part of the fossils collected along this coast of South Carolina have been rescued from the phosphate rock gathered for commercial purposes. This has been to a great extent dredged from the rivers; and thus remains of Pleistocene and of Tertiary animals have been mixed indiscriminately together. It is often impossible to determine to what formation a fossil may belong. To add to the difficulty of the palæontologist, the vertebrate remains are sometimes found washed out and mingled with bones or teeth of what appear to have been domestic animals.

Beginning at the northern end of the South Carolina coast-line, the first locality furnishing Pleistocene fossils is, or rather was (Pugh, op. cit. p. 33), White (or Price’s) Creek, in Horry County. Here at a height of about 5 feet above tide was found a bed approximately 6 feet thick apparently thrown up on the shore by storms (Tuomey, Geol. Rep., 1848, p. 187). No vertebrates have been reported from the locality. At Laurel Hill, in the extreme northeastern corner of Georgetown County, Tuomey (op. cit., pp. 187, 188) found a perpendicular bluff 30 feet high, at the base of which was a bed 8 feet thick made up of sand and broken shells. The top of the bed was 8 feet above tide, the highest elevation reached by the bed along the South Carolina coast. Tuomey mentions other localities around Georgetown where the fossiliferous bed was discovered. One was on Santee River. No vertebrates appear to have been met with in this region. In Christ Church parish, in Charleston County, Tuomey discovered several exposures of the bed in question, and this was sometimes so superficial as to be within reach of the plow.

Pugh (Pleistocene Deposits, etc., p. 34) quotes from F. S. Holmes a section which was found at Goose Creek, north of Charleston, as follows:

Yellow sand 12 feet Blue mud 29 feet Ferruginous sand, containing bones, etc. 3 inches Yellow sand 3 feet Pliocene marl resting on Eocene white marl 12 feet

The bones occurred likewise in the blue mud, and such were especially well preserved. Leidy (Holmes’s Post-Pl. Foss. S. C., p. 102) recounts his observations at this locality; nevertheless, the only vertebrate fossil that the writer finds credited by Leidy to this locality is a tooth of Equus fraternus (=E. leidyi), which he figured (plate XV, fig. 8).

Dredging for phosphate rock has been carried on extensively in Cooper River; but of Pleistocene vertebrate fossils secured here the writer has record of only Megatherium, mirabile. This is represented in the Charleston Museum by a portion of a lower jaw.

Wando River is situated northeast of Charleston, runs parallel with the coast, and empties into Cooper River. From this have (according to the writer’s knowledge) been secured only Equus complicatus and a part of a tusk of Odobenus. The latter is in the Charleston Museum. In most cases no record has been kept of the origin of the specimens in collections.

The Pleistocene bed along Ashley River is famous for the number of fossil vertebrates which it has furnished. It has been described by F. S. Holmes in various publications, especially in the Introduction to his Post-Pleiocene Fossils of South Carolina, 1860, pages I-XII. In the same work, on pages 99–100, Dr. Leidy briefly described the geological character of the beds; and on subsequent pages he described the vertebrate species found there. The principal beds were located on Ashley River, about 10 miles above Charleston. According to Pugh (“Pleistocene Deposits of South Carolina,” p. 34), the fossiliferous deposits rest on Miocene marls. At the top are 4 feet of yellow sands with bands of clay; below, is a foot or more of blue mud lying on the Miocene. The bones are more numerous and best preserved in the blue mud. The Pleistocene bed is elevated only a few feet above tide-level. Inasmuch as nearly all the species of Pleistocene vertebrates which have been found along the South Carolina coast have been secured along the Ashley River, the few found elsewhere will be included in the following list. Some of those marked found somewhere about Charleston may have been collected in or along Ashley River. In this list the contractions following the names signify as follows: A, Ashley River; B, the region about Beaufort; C, somewhere around Charleston; C. r., Cooper River; E, Edisto River; G. c., Goose Creek; J. i., John’s Island; S. r., Stone River; W. r., Wando River; Y., Yonge’s or Young Island. The species preceded by the dagger are extinct.

Odobenus rosmarus A., W. r. (p. 29). Lynx ruff us C. †Canis sp. indet. C. Procyon lotor A. †Arctodus pristinus A. Ursus americanus C. Sylvilagus floridanus? A. †Hydrochœrus æsopi A. †Hydrochœrus pinckneyi C. (p. 365). †Castoroides ohioensis A. (p. 279). Castor canadensis A. Ondatra zibethica A. †Elephas imperator C. (p. 162). †Elephas columbi A., B. (p. 155). †Mammut americanum A., B. (p. 118). Mammut progenium (p. 118). †Bison latifrons? A. (p. 260). †Bison sp. indet. A. (p. 260). †Alces runnymedensis C. (p. 364). Cervus canadensis A. (p. 242). Odocoileus virginianus? A. (p. 231). Camelops sp. indet. †Tagassu lenis A. (p. 222). †Tagassu sp. indet.? A. (p. 222). †Tapirus haysii A. (p. 204). †Tapirus sp. indet. A. (p. 205). †Equus complicatus A., W. r., B. (p. 192). †Equus leidyi A., J. i., G. c., S. r., B. (p. 192). †Equus littoralis C. (p. 193). †Hipparion venustum A. †Physeter vetus A. †Trichechus antiquus A. †Megatherium mirabile A., C. r., S. r. (p. 35). †Mylodon harlani A. (p. 35). †Megalonyx jeffersonii B. (p. 35). †Didelphis virginiana J. i. †Alligator mississippiensis A. †Pseudemys sp. indet. A. †Testudo crassiscutata? A. Trichiurus lepturus Y. †Istiophorus robustus Y. †Ischyrhiza mira? A. Lepisosteus osseus A. Dasyatis hastata? Y.

Besides the species enumerated, the early collectors found remains which were identified as belonging to such domestic animals as the dog, ox, sheep, and hog. Leidy rejected these as Pleistocene species, while Holmes and Agassiz accepted them as such. Possibly the supposed dog was in reality a wolf and the supposed ox a bison. Small teeth like those of cows are fossilized as are the teeth of extinct animals. At Bee’s Ferry on Ashley River the fossiliferous bed has a thickness of 3.5 feet and is at about high-water mark. It is overlain by from 15 to 20 feet of loose sands.

By far the most of the species have been entered in the list on the authority of Joseph Leidy. Only F. S. Holmes reported the elk (Cervus canadensis), and the writer has seen two teeth of the species at the Academy of Natural Sciences in Philadelphia credited to Charleston. Holmes also reported Glyptodon, but that is not included in the list. Lynx ruffus, Ursus americanus, Hydrochœrus pinckneyi, Elephas imperator, Bison latifrons, Alces runnymedensis, Camelops sp., and Equus littoralis are included on the evidence of specimens seen by the writer in the Charleston Museum or in some of the other collections made on the coast of South Carolina. Loomis has recently (Amer. Jour. Sci., vol. XLV, 1918, p. 438) described a specimen of Mammut progenium (as Mastodon americanus) from near Charleston and another from near Beaufort.

Alces runnymedensis was first briefly referred to in Year Book No. 14 of the Carnegie Institution of Washington, 1915 (1916), page 387. The name is based on an upper right hindermost milk molar in the Charleston Museum (No. 13534). It is the property of Mr. Charles C. Pinckney. Where the tooth was found is not known, but it was somewhere near Charleston, in the phosphate-bearing area. The specific name is that of the estate of the owner. The tooth closely resembles the corresponding one of Alces americanus, but is larger and has a flatter crown. Only the crown of the tooth is preserved, and of this a part of the enamel of the inner anterior cone is broken off; otherwise it is in fine condition. The color is very black. The following measurements are given of this tooth and of the corresponding one of Alces americanus, No. 117055 of the U. S. Biological Survey. The two teeth are only slightly worn.

Measurements of milk molars of Alces, in millimeters.

┌────────────────────────────────────┬──────────────┬─────────────────┐ │ Dimensions taken. │A. americanum.│A. runnymedensis.│ ├────────────────────────────────────┼──────────────┼─────────────────┤ │Length of tooth near outer border │ 24.0│ 25.5│ │Length of tooth at middle width │ 21.5│ 23.0│ │Width of tooth along front border │ 23.0│ 23.0│ │Width of tooth from median style to │ │ │ │ base of inner hinder cone │ 21.0│ 24.0│ └────────────────────────────────────┴──────────────┴─────────────────┘

The angle between the outer and inner faces of the hinder half of the tooth is 54° in the tooth of the existing species, 64° in the fossil tooth. On the grinding-surface the fossettes are wider than in the tooth of the existing moose.

It is interesting to find this moose in the region about Charleston. We must suppose that it lived there during one of the glacial stages, probably when the walrus occupied that part of the coast.

In the Pinckney collection is a tooth of a capybara that deserves attention. A figure of it is here presented (fig. 18), a side view. Exactly where the tooth was found is not known, but it was somewhere in the vicinity of Charleston. The tooth is the upper left hindermost molar. In the figure the front end is directed toward the left hand. There are present 17 plates. None of the plates either in front or behind are missing. The free edges of the plates are not turned backward. The length of the tooth is 62 mm., the width is 17.5, the height of the plates on the inner face 37 mm., but probably the less calcified bases of the plates have been destroyed.

On the grinding-surface the plates run obliquely from the inside outward and backward. As seen on the inner face, the plates, as they pass to the grinding-surface, lean backward. The corresponding tooth of a capybara from Surinam has a length of 37 mm. The length of its skull from foramen magnum to the front of the snout is 215 mm. In case the skull of the fossil was long in proportion to the length of the tooth, the length as given above would be 360 mm., about 15 inches.

To this fine large species I give the name Hydrochœrus pinckneyi, in honor of Mr. Charles C. Pinckney, the owner of a collection of fossils from the region about Charleston and the proprietor of the estate of Runnymede, near Lambs, South Carolina.

In the same collection is a part of the lower jaw, right side, of a rather large wolf. In this jaw there remain the complete fourth premolar, the roots of the third premolar, and one root of the second (fig. 19).

The following measurements are taken from the fragment mentioned; from the corresponding part of a jaw of Ænocyon dirus, No. 8307, from La Brea, California; from the gray wolf, Canis occidentalis, from Fort Simpson, British America, No. 9001, U. S. National Museum; and from the type of C. floridanus, in the U. S. National Museum.

Measurements of jaws and teeth of wolves, in millimeters.

┌───────────────────────┬──────────┬──────────┬────────────┬──────────┐ │ Parts measured. │ │ │ C. │ C. │ │ │Charleston│ La Brea │occidentalis│floridanus│ │ │ jaw. │ jaw. │ jaw. │ type. │ ├───────────────────────┼──────────┼──────────┼────────────┼──────────┤ │Height of jaw in front │ │ │ │ │ │ of pm_{4} │ 28│ 32│ 33│ 21.5│ │Thickness at front of │ │ │ │ │ │ pm_{4} │ 14│ 16│ 14.2│ 10.2│ │Length of pm_{4} │ 18.5│ 20.2│ 18.5│ 14.5│ │Thickness of hinder │ │ │ │ │ │ lobe of pm_{4} │ 9.5│ 11│ 9.5│ 7│ │Thickness of front lobe│ 8.5│ 9.8│ 8.5│ 6.4│ └───────────────────────┴──────────┴──────────┴────────────┴──────────┘

The measurements show that the fossil is much too large to belong to the wolf now inhabiting Florida. It appears also to be too small to belong to the wolf Ænocyon dirus, and A. ayersi was but little if any smaller. The lower teeth of the latter species are not known. The accordance in measurements with those of C. occidentalis makes it probable that the fossil jaw found at Charleston belonged to a wolf not greatly different. With the materials at hand it is impossible to refer the jaw specifically.

Within the city of Charleston the bed bearing vertebrate fossils is said to be several feet below tide-level. At Young Island, Wadmalaw Sound, nearly 20 miles southwest of Charleston, the top of the fossil-bearing stratum is at tide-level. This locality is otherwise known in the literature as Simmons’s. The only Pleistocene vertebrate fossils that the writer finds reported from the place are the fishes Lepisosteus osseus and Trichiurus lepturus.

In the region about Beaufort, the same fossil-bearing stratum, having about the same composition and the same elevation, is met with in many places. A few species of fossil vertebrates and many invertebrates have been secured. Here have been found Mammut americanum (p. 118), Elephas columbi (p. 155), Equus complicatus (p. 191), and Megalonyx jeffersonii (p. 35).

A brief notice will be taken of the few known localities where, away from the immediate coast, vertebrate fossils have come to light.

Tuomey, in 1848 (Rep. Geol. South Carolina, p. 177), in describing marls found near Darlington, on the farm of G. W. Dargan, and which he regarded as belonging to the Pliocene, reported the discovery of two perfect molars of a mastodon (p. 118). The locality was in a swamp, and the bed of marl was covered with 3 or 4 feet of black mud. The teeth were immediately below the mud and enveloped in the marl. These teeth belonged to Mammut americanum and had been deposited at some time during the Pleistocene. At another place fragments of the antlers of a deer were found in the marl. In such cases the marls formed at one time the surface of the ground, or more probably the bottom of a swamp; and the Pleistocene bones and teeth might have been trampled down into the marl by living animals. On page 119 is given an account of another mastodon tooth discovered in the same county; and the teeth of a horse have been reported as having been found, associated with those of the mastodon (see p. 193).

In Lee County, adjoining Darlington County on the southwest, at a locality “near Concord church,” between Lynch’s Creek and Black River, Tuomey (op. cit., p. 178) found a bed of Pliocene marl about 4 feet thick. From an excavation in this marl had been taken a tusk which Tuomey regarded as that of a mastodon, but this may have belonged to an elephant. In Berkeley County, at the head of Cooper River, there is, or was, a morass known as Biggin Swamp. This was passed through in constructing the Santee Canal. On page 156 is an account of the discovery of remains of Elephas columbi and of Mammut americanum; on page 162, the finding of a tooth of Elephas imperator. The discovery of the latter marks the age of the deposits as being about that of the Aftonian interglacial.

It has been seen that at many points along the coast there is a fossiliferous stratum varying from 2 to 8 feet. At most localities the fossils consist principally of marine animals, especially mollusks, and the deposits have evidently been laid down in salt water. Along Ashley River and at some localities in the region about Beaufort it seems evident that the surface was above, but not far above, sea-level, and that it formed a swamp on which a great variety of land animals could move about and feed. After death their bones would suffer the fate which befalls them in such cases. Most of them would undergo decay. Parts would be trampled into the muck, broken into fragments, and undergo still further decay. Only the most durable parts, as the teeth, antlers, and the more solid bones would usually stand a chance for preservation. Apparently, on this coast, no considerable parts of one skeleton have ever been found, or at least reported. In Charleston Museum are many bones of a skeleton of Megatherium, but it is uncertain where it was found.

The list of vertebrates referred to the Pleistocene of the South Carolina coast contains 33 species of mammals, of which 24 appear to be extinct. This high proportion of extinct species seems to confirm our reference of the fauna to the early Pleistocene. Besides the extinct forms, it is to be noted that within historical times the muskrat, beaver, and elk have not lived in the region about Charleston.

Pugh (Pleist. Deposits S. C., p. 66), from a study of the Pleistocene marine mollusca of South Carolina, has concluded that, if the Pleistocene sea-temperature differed at all from that of the present, it was slightly higher rather than slightly lower. It must be remembered, however, that the Pleistocene represented a very long period of time and that, farther north, the climate underwent great fluctuations. That these fluctuations would not have affected the temperature of the sea along the coast of the Carolinas is not probable. It is hardly supposable that capybaras and manatees lived about Charleston at the same time that the moose and the walrus were there. The latter had been forced down there during some glacial stage, possibly the Wisconsin; while the horses, tapirs, elephants, manatees, the mylodon, and the megatherium had their existence, we may suppose, about the time of the Aftonian. During this stage, too, lived the species of mollusks which Pugh has elaborated. It would seem that after that time some change took place in conditions, probably a slight elevation, so that little more than beds of unfossiliferous sand and marls were deposited.

Professor Earle Sloan, in his “Mineral Localities of South Carolina” (Bull. No. 2, ser. IV., South Carolina Geol. Surv.), has recognized the following divisions in the marine Pleistocene of the State:

6. Sea Island loams.

5. Wando clays and sands.

4. Accabee gravels.

3. Bohicket marl-sands.

2. Wadmalaw marl.

1. Ten-Mile sands.

Of these, the fossiliferous deposits referred to above appear to belong to the Wadmalaw marl. It may be confidently expected that somewhere along the South Carolina coast, beneath the beds bearing the vertebrate fossils, there will yet be discovered other Pleistocene deposits, probably shell marls, which belong to the Nebraska stage.

GEORGIA.

The only part of Georgia at present of interest to the student of vertebrate palæontology is that which lies immediately along the Atlantic coast and along a few of the larger rivers. The northwestern corner of the State is mountainous and probably contains little or no Pleistocene. The Coastal Plain extends landward to a line which starts at Augusta, on Savannah River, passes through Milledgeville and Macon, and ends at Columbus, on the Chattahoochee. A large part of this region is mantled by a deposit resulting from the decay of the underlying rocks. These deposits are of uncertain age, a part belonging probably to the Pleistocene, but the large part to the Pliocene or to still older Tertiary. The Pleistocene has not yet been differentiated from the remainder, and, in any case, has furnished no vertebrate fossils. For information on the subject the reader may consult McGee (12th Ann. Rep. U. S. Geol., Surv., pt. I, pp. 478–484), Spencer (Geol. Surv. Georgia, 1890–91, pp. 61–81), and Veatch and Stephenson (Bull. 26, Geol. Surv., Georgia, pp. 400–456).

The deposits in Georgia which can with certainty be referred to the Pleistocene form a broad belt lying along the coast and extending landward a distance of about 30 miles along Savannah River and about 60 miles at the Florida boundary line. For a description of these deposits the reader is referred to Veatch and Stephenson’s article in Bulletin 26 just mentioned, pages 424–456. These deposits are disposed in two terraces, a higher and older and a lower and younger. The older is named the Okefenokee formation, the younger the Satilla formation. The positions of these may be observed in the figure here presented, taken from Bulletin 26 above referred to (fig. 20).

The Okefenokee terrace has a breadth of 20 to 40 miles and an elevation of 60 to about 125 feet above sea-level. It forms a plain which Veatch and Stephenson describe as in general flat and almost featureless. It is dotted with cypress ponds and swamps, with here and there low ridges and hills of sand. Along the larger streams which cross the plain are found terraces supposed to have been laid down while the Okefenokee terrace was forming; they extend far back into the State. In neither the main terrace nor the fluviatile terraces have any fossils been found, except a little silicified wood.

The Satilla Plain extends backward from the coast 20 to 30 miles and varies in elevation from 15 to 40 feet. On the landward side it ends in an escarpment which is taken, by the authors quoted, to be an old sea-beach. Along the large rivers it is continued as a series of terraces occupying a lower position than those of Okefenokee time. According to Veatch and Stephenson, this formation consists of unconsolidated clays, sands, and thin layers of gravel. The thickness averages about 15 feet, but may become as much as 45 or 50 feet.

The Satilla deposits are fossiliferous. At various places, at some distance from the coast, sea-shells occur, especially shells of oysters. This shows that at times the plain, or at least some parts of it, has been under sea-water. Bones and teeth of vertebrate animals have been discovered at several localities, but at only two places have identifiable materials been secured. The region about Brunswick and that just south of Savannah have furnished important collections of vertebrate animals.

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