Bulletin No. 257 B, Descriptive Geology, 64

C, Systematic Geology and Paleontology, 72

DEPARTMENT OF THE INTERIOR

UNITED STATES GEOLOGICAL SURVEY

CHARLES D. WALCOTT, DlRECTOB

GEOLOGY AND PALEONTOLOGY OF THE

JUDITH RIYER BEDS

BY

T. W. STANTON

AND

J. B. HATCHER

WITH A CHAPTER ON THE FOSSIL PLANTS

F. H. KISTOWLTON

WASHINGTON

GOVERNMENT PRINTING OFFICE

1905

CONTENTS.

Page.

Letter of transmittal...................................................... 7

introduction............................................................. 9

Descriptive geology....................................................... 11

The stratigraphic column ......'........................................ 11

Benton shales............................................ 11

Eagle formation.......................................... 12

Claggett formation ........................................ 13

Judith Eiver beds......................................... 13

Bearpavv shales .......................................... 13

Higher horizons.......................................... 14

Historical review......I........................:..............-....... 14

Description of Judith Eiver beds, by areas ............................. 31

Original area..................................................... 31

General features.............-..-..--..--..--.-.....-......... 31

Exposures on Dog Creek...................................... 34

Exposures on Birch Creek .................................... 38

Exposures on Missouri between Birch and Cow creeks.......... 40

Exposures on Cow Creek ...................................... 41

Area near Havre, Mont .............. .............'................ 45

Exposures on Milk River from Havre to the international

boundary................................................... 48

Exposures on Milk Kiver north of the international boundary... 51

Sage Creek area, Assiniboia ....................................... 53

Willow Creek area, in central Montana ............................ 56

Fish Creek area......'............................................ 59

Other probable areas ............................................. 61

Resume and conclusions .................................'............. 62

Vertebrate fauna, by J. B. Hatcher........................................ 67

Pisces ..-....:...................--........-.-.---.,,............. ... 67.

Amphibia ........................................................... 69

Reptilia ........................................................:.... 71

Aves ........................................... '. ..................... 99

Mammalia.... r ...................................................... .100

Summary............................................................ 101

Invertebrate fauna, by T. W. Stanton...................................... 104

Pelecypoda ........:................'................................. 104

Gasteropoda ..................... ................................... 113

Cephalopoda......................................................... 119

Insecta ............................................................... 119

General comments ................................................... 119

Fossil plants, by F. H. Knowlton.......................................... 129

Descriptions of species ................................................ 129

Discussion of the flora ................................................ 150

Index ................................................................... 169

3

ILLUSTRATIONS.

Page.

PLATE I. A, General view of the Eagle formation; B, Sandstones and overlying 

lignite-bearing beds of the Eagle formation at the mouth of Eagle 

Creek ........................................................ 12

II. Cliff of upper Eagle sandstone near mouth of Dog Creek ........... 36

III. A, General view of Birch Creek Canyon from top of bluffs near its 

mouth, looking toward the Bearpaw Mountains; B, Broken anticline of Eagle sandstone on north side of Missouri River 1 mile 

below mouth of Birch Creek ................................... 38

IV. A, View down Missouri River below mouth of Birch Creek; B, Claggett formation and overlying Judith River beds on Birch Creek ... 40

V. Fault contact of highly inclined Eagle sandstone with horizontal

Judith River beds near mouth of Cow Creek .................... 42

VI. A, Undisturbed Judith River beds with overlying Bearpaw shales 

on Cow Creek; B, Fault contact of Judith River beds with Bearpaw shales on Cow Creek 10 miles above its mouth.............. 44

VII. A, Indurated or concretionary mass in upper part of Judith River 

beds, Cow Creek 13 miles above its mouth; B, Upper part of 

Judith River beds with heavy bed of lignite, Cow Creek......... 44

VIII. A, Badlands exposures of Judith River beds, north side of Milk 

River near Havre, Mont.; B, Upper part of Judith River beds 

and overlying Bearpaw shales, south side of Milk River 3 miles 

west of Havre, Mont .......................................... 46

I.. A, Upturned Judith.River beds and base of Bearpaw shales, Meili 

Coulee near Havre, Mont.; B, Claggett shales and base of Judith 

River beds, Milk River one-half mile below Pendant d'Oreille, 

Assiniboia.................................................... 48

X. A, Exposure showing remains of Trachodon skeleton on Sage Creek, 

Assiniboia; B, Contact between Judith River beds and overlying 

Bearpaw shales on Sage Creek, Assiniboia....................... 54

XI. A, Judith River beds on Willow Creek 10 miles north of .Musselshell post-office, Mont.; B, Judith River beds on Fish Creek, 

Montana ..................................................... 58

XII. Fig. 1, Unio priscus Meek and Hay den; figs. 2-4, Unio priscus var.

abbreviatus n. var............................................. 126

XIII. Fig. 1, Unio subspatulatus Meek and Hayden; figs. 2, 3, Unio supenawensisn. sp.; fig. 4, Goniobasis judithensis n. sp.; fig. 5, Melania 

whiteavesi n. sp................................................ 128

XIV. Fig. 1, Fern, indeterminable, enlarged 3 times; fig. 2, Sequoia sp.?; 

figs. 3-5, Sequoia reichenbachi (Gein.) Heer; fig. 6, Osmunda 

montanensis n. sp.; enlarged 2times............................ 158

5
b ILLUSTRATIONS.

Page. 

PLATE XV. Fig. 1, Cunninghamites elegans (Corda) Endlicher; figs. 2-5, Dammara acicularis n. sp.; fig. 6, Carpites pruni n. sp.; fig. 6a, Carpites 

pruni n. sp., enlarged 3£ times; fig. 7, Fern, indeterminable, 

enlarged 3 times ............................................ 160

XVI. Fig. 1, Cunninghamites pulchellus n. sp.; fig. 2, Carpites alatusn. 

sp.; fig. 3, Thuja cretacea? (Heer) Newberry; fig. 3a, Thuja 

cretacea? (Heer) Newberry, enlarged 3 times; fig. 4, Carpites 

judithse n. sp.; fig. 5, Sequoia heterophylla? Vel.; fig. 6, Cunninghamites recurvatus ? Hosius and von der Marck........... 162

XVII. Figs. 1-5, Populus cretacea n. sp.; fig. 6, Quercus montana n. sp.;

fig. 7, Sapindus inexpectans n. sp........ ..................... 164

XVIII. Fig. 1, Populites amplus n. sp.; fig. 2, Quercus n. sp.; fig. 3, Betulites? hatcheri n. sp.; figs. 4, 5, Diospyros judithae n. sp.; fig. 6, 

Phyllites dubius n. sp........................................ 166

XIX. Fig. 1, Populus sp.; fig. 2, Phyllites denticulatus n. sp.; fig. 3,

Diospyros judithse n. sp.; fig. 4, Castalia stantoni n. sp.......... 168

FIG. L Boreodon matutinus Lambe........................................ 100
LETTER OF TRANSMTTTAL.

DEPARTMENT OF THE INTERIOR,

UNITED STATES GEOLOGICAL SURVEY,

Washington, D. C. , May 11, 1904.

SIR: I have the honor to transmit herewith the manuscript of a 

report on the geology and paleontology of the Judith River beds, by 

T. W. Stanton and J. B.-Hatcher, with a chapter on the fossil plants 

by F. H. Knowlton, and to recommend its publication as a bulletin.

The report embodies the results, of field' studies in Montana and 

adjacent regions during the season of 1903, and of a subsequent study 

of the collections. By combining careful stratigraphic observations 

with several lines of paleontologic investigation the authors have satisfactorily answered a much discussed question in Cretaceous stratigraptry, and the results stated in this report will have an important 

bearing on the geology of a large area in the Northwest. 

Very respectfully,

C. W. HAYES,

Geologist in Charge of Geology. 

Hon. CHARLES D. WALCOTT,

Director United States Geological Survey.

GEOLOGY AND PALEONTOLOGY OF THE 

JUDITH RIVER BEDS.

By T. W. STANTON and J. B. HATCHER."

INTRODUCTION.

During- the summer of 1903 we spent two months together in the 

field study of the Judith River and associated formations of northern and central Montana and adjacent areas of Canada. The principal results of this work were the accurate determination of the 

position of the Judith River beds in the Upper Cretaceous section, 

and the removal of all doubts as to the correlation of these beds with 

the Belly River beds of Canada, thus establishing more accurately the 

position of that Canadian formation. These results are offered as a 

slight contribution to the Mesozoic history of the north interior 

region, which is rendered more than usually difficult to decipher 

because land or nonmarine conditions prevailed during several 

recurring intervals, at least from the Upper Jurassic to the top of 

the Cretaceous. It is our purpose to give somewhat in detail the 

evidence on which our conclusions are based, restricting the descriptions to the areas which have been actually studied by us and which 

include practically all the known exposures of Judith River beds in 

Montana and the southeastern part of the Belly River area^including 

the bottom and the top of the formation) in Assiniboia. After a cursory review of previous work on the formations discussed, the local 

outcrops and sections in the different areas will be described. The 

descriptions of the areal and stratigraphic geology will be followed 

by brief accounts of the vertebrate fauna by Mr. Hatcher, of the 

invertebrate fauna by Mr. Stanton, and of the flora by Mr. Knowlton.

Working independently along different lines, we have long been 

interested in the stratigraphic and faunal problems connected with

a On July 4,1904, soon after this manuscript was finished, Mr. J. B. Hatcher died, at his home in 

Pittsburg, after a brief attack of typhoid fever. His death at the early age of 43 years is a serious 

loss to geology and paleontology, in which the important work he had already done gave promise of 

greater results in the future. T. W. S.

9
10 THE JUDITH EI7EE BEDS. [BULL. 257.

the Judith River beds, and both of us had previously visited the 

typical area near the mouth of Judith River. In 1888 and 1892 

Mr. Hatcher spent considerable time in collecting vertebrate fossils 

from the formation, making only incidental observations on the stratigraphy of the region. He traveled by wagon road, thus approaching 

the "badlands" exposures of these nonmarine beds from the higher 

divides, where he noticed outcrops of marine Cretaceous shales in such 

locations that he inferred that they might overlie the Judith River 

beds. He had also noticed similar relations of the outcrops on Willow 

Creek near Musselshell River. The study of the vertebrate fauna led 

him to the conclusion that it is older than the Laramie fauna of the 

uppermost Cretaceous. In the absence of data as to the exact age of 

the underlying formation, all of Mr. Hatcher's observations tended to 

place the Judith River beds well down in the Upper Cretaceous.

In 1894 Mr. Stanton spent a few days with Mr. W. H. Weed near 

the mouth of Judith River. They traveled by rowboat down the 

Missouri River from Fort Benton to Judith, passing over and studying the formations underlying the Judith River beds, beginning with 

the Fort Benton shales. Mr. Stanton confirmed the statements of 

previous observers that some of the strata beneath the Judith River 

beds contain a fauna that is elsewhere characteristic of the Montana 

group, or Fort Pierre and Fox Hills formations. He was especially 

impressed by the occurrence, in the upper part of these underlyingbeds, of a zone containing Cardiwn speciosum, Mactra alta, TancTedia 

americana, and other forms which in north-central Colorado are known 

to occur only in the Fox Hills beds immediately beneath the Laramie. 

No beds higher than the Judith River were seen, and the view was 

adopted that the Judith River overlies all of the Montana group and 

is referable to the Laramie. When a few days later the overlying

marine Cretaceous shales were seen in contact with upturned Judith

River beds near Havre, Mont., their apparent position was supposed 

to be due to faulting, of which there was abundant evidence in the 

neighborhood.

With th'ese divergent views concerning the age of the Judith River 

beds the writers participated in the renewed discussion on that subject during the winter of 1902-3, to which reference will be made 

later. Mr. Hatcher then decided to make a field investigation of 

typical areas of the Judith River and Belly River beds, under the 

auspices of the Carnegie Museum, in Pittsburg, in which he had 

charge of the department of paleontology. Mr. Stanton expressed 

the desire to cooperate in such an expedition, and afterwards arrangements were made under which the expenses of the joint field work 

were borne by the United States Geological Survey.
DESCRIPTIVE GEOLOGY.

THE STKATIGBAPHIC COLUMN.

In order that the review of previous work on the Judith Riverbeds 

may be made intelligible without too much circumlocution, it is necessary to introduce here a brief account of the stratigraphy of the Upper 

Cretaceous in this region. The principal facts, with the names of 

the new formations recognized, have been published in a preliminary 

note."

Benton shales. The lowest formation studied consists of dark clay 

shales with occasional intercalated bands of sandstone, especially in 

the upper portion. There are also frequent calcareous concretions, 

often of large size, which are usually fossiliferous. This is the wellknown and Avidely distributed Fort Benton formation of the Meek 

and Hay den upper Missouri section. The name is derived from the 

town of Fort Benton, on Missouri River about 100 miles above the 

mouth of Judith River, but the original description and especially 

the stratigraphic limits are based largely on exposures in another 

area in Nebraska, where the Benton rests on the Dakota sandstone and is overlain by the Niobrara limestone and calcareous 

shales. In the neighborhood of Fort Benton and in all the region 

now under investigation there is no limestone corresponding to the 

Niobrara, and as there is no evidence of an erosion interval or unconformity, it is probably represented by shales or sandstones. The 

paleontologic indications are that in this region the Niobrara is represented by dark shales not separable stratigraphically from the Benton. 

If this be true the Benton shales of the upper Missouri represent 

more than the formation known by the same name in Nebraska, in 

Colorado east of the Front Range, and at other places, and really 

include the whole of the Colorado group, so that it is more appropriate to call them Colorado shales, as Weed has done in the Fort 

Benton folio. These shales are characterized in their lower portion 

by Inoceramus- Idbiatus, Scapkites warreni, and a few other species, 

while toward the top they yield Inoceramus umbonatus, I. exogyroides, 

Pkoladomya papyracea, Scapkites ventricosus, Baculites asper (f), and 

many other forms. The species of Inoceramus and Baculites occur in 

the Austin limestone of Texas; which is correlated with the Niobrara, 

and some of them have been found in the upper Niobrara shales of

a Science, \\. s., vol. IS,1903, pp. 211-212.

11
12 THE JUDITH EIVEB BEDS. [BULL. 257

Colorado. The total thickness of the formation is estimated at 800 

feet, but on\j the upper portion, 200 to 300 feet in thickness, is 

usually seen in the sections examined.

Eagle formation. Immediately above the Benton shales is the 

Eagle formation, which was named by Weed from Eagle Creek. It is 

found along Missouri River for many miles above and below Eagle 

Creek, the exposures being continuous from a point less than 10 miles 

below the mouth of Marias River to the mouth of Arrow Creek. At 

its base it consists of laminated sandstones and shales grading down 

through 30 or 40 feet into the underlying formation, but its most 

conspicuous member is a heavy-bedded or massive, very light-yellowish 

to white cross-bedded sandstone 100 feet or more in thickness, which 

"weathers into cliffs or steep slopes with balcony ledges and strikingmonumental forms capped by ironstone masses." (See Pis. I and II.) 

These striking features of the landscape have been noticed and 

described bjr all the early explorers of the upper Missouri. In the 

neighborhood of Eagle Butte the sandstone is cut b}^ many igneous 

dikes, which, however, do not cause any vertical displacement.

Above the massive white sandstone are softer beds consisting of 

alternating sandstones, shales, and many beds and seams of lignite. 

At many localities bands of small, flat, black pebbles occur near the 

top. The total thickness assigned by Mr. Weed to the formation 

along the Missouri is 200 feet, but if the similar lignitiferous beds 

that are predominantly sandstones be included the thickness is 

probably more than. 300 feet. This greater thickness of beds that 

can not be consistently separated from the Eagle formation was 

observed especially on Dog Creek, and at other places in the neighborhood of Judith.

 At many places the Eagle formation seems to be barren of fossils. 

This is especially true of the thick sandstone member. One locality

on the Missouri, 7 miles below "Coal Banks," has yielded a few 

species of fossil plants, and a considerable invertebrate fauna has been 

collected, mainly from the upper portion, 5 or 6 miles below the 

mouth of Arrow Creek, and on Dog Creek and elsewhere in the 

neighborhood of Judith. The invertebrates include Cardium speciosum, Thetis? circularis, Mactra alta, Placenticeras whitfieldi (f), and 

undescribed species of Crenella, Leptosolen, Itaroda, Pholadomya, and 

Baculites, all of which show much closer relation with the fauna of 

the overlying beds of the Montana group than with that of the 

Colorado group. This horizon has also yielded a few dinosaurian 

remains, including the type of Ornithomimus gmndis, which was 

found near the mouth of Cow Creek, where the Eagle formation is 

brought up by faulting.

The formation has often oeen confused with several other horizons. 

In addition to the areas already mentioned it has been recognized in
A. EAGLE FORMATION. "STONE WALLS" ON MISSOURI RIVER BELOW MOUTH OF

EAGLE CREEK.

Igneous dike in middle distance.

K. EAGLE FORMATION. SANDSTONE AND OVERLYING LIGNITE-BEARING BEDS AT 

MOUTH OF EAGLE CREEK.
THE STEATIGKAPHIC COLUMN. 13

prominent outcrops on Flatwillow and Willow creeks, on the Yellowstone at Billings, and on Fish Creek near Musselshell River.

Claggett formation. -The beds to which the name Claggett formation has been given lie above the Eagle formation and below the 

Judith River beds. In the neighborhood of Judith (old Fort Claggett), where they are well exposed, they have a total thickness of 

about 400 feet and consist largely of dark clay shales with variable 

intercalated bands and beds of sandstone, especially in the upper half. 

The dark shales of the lower part of the formation contain many calcareous concretions, which yield G-ervillia korealis, Baculites ovatus, 

Baculites. compressus, and a few other forms, elsewhere regarded as 

characteristic of the Fort Pierre. The yellowish sandstone beds 

higher in the formation, especially one about 200 feet from the top 

and another near the summit, are often locally very fossiliferous, and 

bear an invertebrate fauna, of which the most conspicuous species are 

the following:

Species from upper part of Claggett formation.

Taricredia americana. 

Cardium speciosum. 

Sphteriola? endotrachys. 

Tellina eqnilateralis. 

Thracia gracilis.

Mactra formosa. 

Mactra alta. 

Lunatia subcrassa. 

Vanikoropsis tuomeyana. 

Baculites sp.

Liopistha (Cymella) undata.

This has long been considered a typical '' Fox Hills" fauna, and a 

number of its species do recur at the top of the marine Cretaceous 

immediately below the Lararnie in Colorado and elsewhere. It is 

now known that some of them also occur as low as the Eagle formation. The shale exposures of this formation in the neighborhood of 

Judith have been identified as Fort Pierre in previous publications. 

The ''lower dark shales" mapped by Dawson on Milk River near 

Pakowki Lake, Assiniboia, are the upper part of the Claggett formation. There is usually a gradual transition upward into the Judith 

River beds, so that it is often difficult to determine the exact boundary.

Judith Rwer beds. The lithologic and paleontologic features of this 

formation are fully described on subsequent pages. The beds are 

mostly of fresh-water origin, but Occasionally contain intercalated 

brackish-water layers, the most persistent of which is near the top of 

the formation. More rarelj7' there are local marine deposits in the 

upper part. The formation is prevailingly light colored and tends to 

weather into "badlands" forms. The thickness near Judith is little 

more than 500 feet.

JBearpaw shales. These shales rest on the Judith River beds, and 

have the lithologic character of the Pierre shales, part of which they 

represent. They consist chiefly of dark clays, which weather into 

rounded slopes and form an "adobe" soil. In certain zones there are
14 , THE JUDITH EIVEE BEDS. [BULL. 257.

numerous calcareous concretions, most of which are fossiliferous and 

and yield a varied invertebrate fauna. Among the more common 

forms are the following:

Species found in Bearpaw shales.

Liopistha (Cymella) undata. 

Anisoniyon centrale. 

Cinulia concinna. 

Anchura americana. 

Baculites ovatus. 

Baculites compressus. 

Placenticeras whitfieldi. 

Placenticeras intercalare. 

Scaphites nodosus.

Ostrea patina. 

Avicula nebrascana. 

Avicula linguiformis. 

Inoceramus sagensis. 

Inoceramus barabini. 

Leda (Yoldia) evansi. 

Lucina aubundata. 

Thetis circularis. 

Callista deweyi. 

Mactra gracilis.

This formation is named from the Bearpaw Mountains, around 

whose north, east, and south sides it is well developed.. It is evidently 

the equivalent of only a part of the Pierre formation, which in South 

Dakota, Colorado, and elsewhere is defined to include all the strata 

between the Niobrara limestone and the Fox Hills sandstone. Whether 

the Bearpaw also includes the representative of the Fox Hills sandstone has not yet been definitely determined. Its limits are precisely 

the same as those of the beds in Alberta and Assiniboia described by 

the Canadian geologists as "Pierre-Fox Hills" group, whose thickness is estimated at 750 feet. The thickness in Montana probably 

approximates the Canadian estimate, but no section where an accurate 

measurement could be made was studied.

Higher horizons. Along Musselshell River in the neighborhood of 

Musselshell post-office and between the Musselshell and the Yellowstone north of Billings and Bigtimber the Bearpaw shales are overlain 

by a thick series of beds in which sandstones predominate, with shales 

and several coal-bearing horizons. This series doubtless includes representatives of the Laramie, Livingston, and Fort Union formations 

as described by Weed in adjacent areas.

HISTORICAL REVIEW.

The earliest definite geologic descriptions of the region about the 

mouth of Judith River were by Dr. F. V. Hayden, who visited the 

area in 1854 or 1855, a and brought back collections of both invertebrate and vertebrate fossils. The invertebrates were described by 

Meek and Ha)^den in the Proceedings of the Academy of Natural 

Sciences, Philadelphia, beginning in 1856, while the few vertebrate

"The scenic features above the mouth of Judith River produced by the Eagle sandstone were 

described by Lewis and Clark (Expedition to the Sources of the Missouri, etc., 1814) and by Prinz 

Maximilian zu Wied (Reise in das Iiinere Nord-America in den Jahren 1832 bis 1834, Coblenz, 1839- 

1841). The latter gives excellent illustrations of some of the striking outcrops of the Eagle sandstone 

on pis. 34, 35, 41, and vignette 18.
....-^..ND] HISTORICAL REVIEW. . 15

remains were described by Doctor Leidy. ft These joint papers 

by Meek and Hayden, and others written by Hayden independently, contain many notes describing the geology of the Judith 

River country and varying opinions as to the age of the beds 

exposed there. The presence of many faults and other disturbances, 

the lithologic similarity of several distinct formations, and the 

apparently contradictory character of the evidence from different 

classes of fossils conspired to make the interpretation of the section 

difficult, and it is not surprising that the necessarily hasty and imperfect examination of the stratigraphy made by Doctor Hayden left 

him in doubt as to the relations of some of the beds, or that he made 

mistakes in attempting to correlate these beds with the Cretaceous section exposed on Missouri River several hundred miles to the east, 

where the lithologic 'development of. some parts of the section is very 

different. The members of that section had not then been named, and 

the formations subsequently called 6 Dakota, Fort Benton, Niobrara, 

Fort Pierre, and Fox Hills were known as Nos. 1, 2, 3, 4, and 5, 

respectively.

In these early papers the sandstone now known to form the most 

prominent member of the Eagle formation was doubtfully referred to 

" No. 1," but from the fossils that are cited it is evident that Hayden 

did not separate the sandstone bands of the Claggett formation from 

the underlying Eagle sandstone. The occurrence of flettangia americana (afterwards referred to Tancredia) was especially commented on 

because it was believed to be a Jurassic type of shell, though its asso- 

 ciation with Baculites and other Cretaceous types was taken as evidence 

that the horizon was really near the base of the Cretaceous. This 

marine horizon was recognized to be beneath the nonmarine beds 

whose invertebrate fossils were all described as Tertiary species. The 

vertebrate remains from the same region were declared by Leidy c 

to be reptiles and fishes of old types, " which remains, I suspect, 

indicate the existence of a formation like that of the Wealden." At 

that time it was not certain whether the vertebrates came from the 

same horizon as the nonmarine invertebrates or from a lower bed with 

"No. 1," though apparently Hayden's original opinion was that the 

bones and part of the fresh-water Mollusca came from the lower 

horizon and that other fresh- and brackish-water fossils came from 

Tertiary beds in the same neighborhood, as the following quotation d 

from the first published geologic description shows:

Some 4 or 5 miles below the mouth of Musselshell River a lower rock a sandstone rises above the water level. This is probably No. 1 of the series, No. 2 and

aProc. Acad. Nat. Sci. Philadelphia, 1850, pp. 72, 73, and Trans. Am. Philos. Soc., vol. 11, I860, pp. 

139-154.

6 Proc. Acad. Nat. Sci. Philadelphia, 1861, p. 419. 

cProc. Acad. Nat. Sci. Philadelphia, 1856, p. 73. 

rfMeek and Hayden, idem, p. 114.
16 THE JUDITH RIVER BEDS. [BULL. 257.

No. 3 not being represented here. It is worthy of note that out of two species of 

Maclra, two of Tellina, two of Inoceramus,' one of Pholadomya, two of Natica, and one 

Baculite found in this rock, not one is known to occur in any of the higher formations, and some of these species are not unlike Neocomian forms.

In consequence of the increasing inclination of the strata, this last-mentioned sandstone rises in the vicinity of North Mountain River [Little Rocky Mountain Creek] 

as much as 250 feet above the Missouri. Here, or near this, begins a wild and desolate region, known as the Mauvaises Terres or Bad Lands of the Judith. At various 

places in these Bad Lands a sandstone similar to No. 1 wag seen alternating with 

beds of clay and lignite, all of-which are upheaved and much distorted. It was 

found impossible to devote to the examination of these formations time enough 

to determine their relations to the Cretaceous and Tertiary strata of this region, 

without running the risk of being cut off from the party and murdered by the 

Indians. Among a few fossils that were collected here, however, Professor Leidy 

finds teeth which he refers to two or three genera of large Saurians allied to the 

Iguanodon, Megalosaurus, etc. There are also in the collection from some of these 

beds one or two species of Unio, one or more of Cyclas or Cyrena, and a few crushed 

specimens of Gastropoda, like Paludina and Melania. JFrom these facts we are strongly 

inclined to think with Professor Leidy there may be here, at the base of the Cretaceous system, a fresh-water formation like the Wealden. Inasmuch, however, as 

there certainly are some outliers of fresh-water Tertiary in these Bad Lands, we 

would suggest that it is barely possible these remains may belong to that epoch, 

though the shells appear to be all distinct species from those found in the Tertiary at 

other localities in this region.

In this paper the Judith River invertebrates are described as Tertiary species. In a subsequent paper published in the same volume a 

Meek and Hayden again discuss the marine sandstones containing 

Baculites and Hetta/ngia [Tancredia] americana, and suggest that they 

may be as old as Jurassic, though more probably Cretaceous. Their 

statement is as follows:

If not older than Cretaceous, we think, from these facts, as well as from the stratigrapical position of these beds, they probably represent some of the older members 

of that system. What relation they bear to the formations near the same locality 

in which the saurian remains were found, supposed by Professor Leidy to be allied 

to the genera Iguanodon and Megalosaurus, is still an unsettled question, b

In 1857 Hayden published his "notes explanatory of a map and 

section illustrating the geological structure of the country bordering 

on the Missouri River." Among the " basins of the Tertiary system" he lists c the "Bad Lands of Judith River, which occupy an area 

of 40 miles in length and 15 to 30 in breadth, reposing on a sandstone,

a Pp. 265-286.

6 It is noteworthy that in this article the terms " Judith Kiver beds" and "Judith River formations" are used in a general, untechnical sense to include all the formations occurring near the 

mouth of Judith River. In Leidy's paper of 1860 "Judith River formation" appears in the title 

and in the caption of a section. The term was used rather loosely for some years, and when applied 

strictly to the formation now known by that name it usually took the form "Judith River Estuary 

beds." In 1871 Hayden proposed "Judith group" (Ann. Rept. U. S. Geol. Surv. Terr, for 1870, p. 97) 

as a formation name. In subsequent papers by Cope, Meek, and others "Judith River beds!' was 

used with its present signification.

cProc. Acad. Nat. Sci. Philadelphia, 1857, pp. 109-116,
STHATCHEKND] HISTORICAL REVIEW. 17

the age of which has not been positively determined." This area is 

colored as Tertiaiy on the map, and is described as follows:

This exceedingly interesting deposit occupies a depression in a sandstone formation which rises to the water level at the month of Little Rocky Mountain Creek 

from beneath the well-known Cretaceous bed No. 4 of the vertical section. It presents perhaps the most rugged scenery on the Missouri River, the denudation and 

erosion having been much greater than at the Bad Lands of White River. But 

the most remarkable feature of this basin is the wonderful disturbance of the strata. 

So much are the beds disturbed and blended together by forces acting from beneath, 

that it seems almost hopeless to obtain a section showing with perfect accuracy the 

order of superposition of the different strata.

A paper by Meek and Hayden in the same volume a gives a further 

discussion of the subject and shows that the change of view was caused 

by the study of the invertebrate fauna, which seemed to show close 

relationship with that of the " Great Lignite basin " near Fort Union.

A Judith River species of turtle (Trionyw) had also been identified 

in a bed at the base of the "lignitic," which was then regarded as 

Miocene. Their rather guarded statement is as follows:

We would not for a moment hesitate in regarding the deposits of which we have 

spoken, near the Judith, as Tertiary, were it not for the fact that the saurian and fish 

remains occurring in these beds, as may be seen by reference to Professor Leidy's 

remarks respecting them, are allied to Wealden and older types.

In the midst of evidence of such a conflicting nature, it is, of course, unsafe to 

express any very positive opinion respecting the age of these formations. At the 

same time we are strongly inclined to the conclusion that they will prove not merely 

Tertiary, but about of the age of the lowest beds of the Great Lignite basin, or perhaps a little older. We have therefore placed them provisionally along with the 

Tertiary beds in the accompanying section of the Nebraska rocks.

A generalized section of the Judith River beds ,415 feet thick is 

described as follows:

This section embraces all the deposits, as we believe, seen in the Bad Lands of the 

Judith, in which" land and fresh-water shells are known to occur. They appear, as 

near as could be ascertained, to occupy a local basin in a series of marine deposits, 

consisting of beds of sandstone and impure lignite, which we have regarded provisionally as of the age of No. 1 of our general section. &

This view, however, evidently was not in harmony with some of 

Hayden's stratigraphic observations, for when explorations in the 

Black Hills brought to light a fresh-water fauna at the base of the 

Cretaceous section, in beds now generally referred to the Jurassic, the 

opinion as to the age of the Judith River beds was again changed, and 

in a new edition of Hayden's map c the area was colored as "Cretaceous No. 1," with the statement that the beds may be the American

« Pp. 117-148.

& This section and a general discussion of the geology of the region were also published by Hayden 

in Warren's "Report of explorations in Nebraska and Dakota," in report of Secretary of War, 

1858. reprinted as separate document in 1875.

cProc. Acad. Nat. Sci. Philadelphia, 1858, pp. 139-158.

Bull. 257 05 2
18 THE JUDITH RIVER BEDS. . [BULL. 257.

representatives of the Wealden. A fuller statement by Meek and 

Hay den a is as follows:

The occurrence of these forms at this horizon [in the Black Hills] also leads us to 

suspect that a considerable portion of the estuary beds at the mouth of Judith River, 

above Fort Union, in regard to the age of which we have been so much puzzled, may" 

be, as first suggested by Doctor Leidy, a representative of the Wealden, and as we 

were then inclined to suppose, belong to our No. 1.

The close similarity between the lithological characters of these deposits and 

those of some of the Tertiary formations of the Northwest, and the estuary character 

of their fossils, together with the analogy of many of the species of Mollusca found in 

one of the upper beds (which may be an outlier of Tertiary resting on older formations), taken in connection with the fact that amongst the fossils collected from one 

of the middle beds (see section p. 124, Vol. VIII, Proceedings, 1857) there were 

some fragments of a Trionyx, regarded by Doctor Leidy as identical with a species 

occuring in well-marked Tertiary deposits near Long Lake, below Fort Clark, led us 

subsequently to think the whole of these estuary beds near the Judith River might 

possibly be an outlier of Tertiary reposing upon deposits of the age of our No. 1. 

At the same time, in consequence of the occurrence in them of remains regarded by 

Doctor Leidy as analogous to Lepidotus, Iguanodon, and Megalosaurus, we stated that 

in the midst of evidence of such a conflicting nature, it is unsafe to express any very 

positive opinion respecting the age of these formations.

Since we know that there is a similar group of beds at the base of No. 1, as we now 

understand it, near the Black Hills, containing a mingling of fresh-water and marine 

fossils although we are not sure any of them are specifically identical with those 

found near the Judith we are inclined to think our first views in regard to these 

Judith River formations will prove to be correct, or, in other words, the beds from 

which the saurian remains, described by Doctor Leidy, were obtained, will yet prove 

to be a part of the series we include in No. 1 of the Black Hills section. This view 

receives additional support, too, from the fact that the Judith River fresh-water or 

estuary formations were often seen much upheaved and distorted, while around the 

Black Hills the Tertiary deposits appear to lie undisturbed upon the upheaved older 

rocks in such a manner as to indicate that the last period of disturbance amongst 

the strata of this region occurred after the close of the Cretaceous epoch, but previous 

to the deposition of the Tertiary.

In 1860 Hayden published 6 a paper entitled "A Geological Sketch of 

the Estuary and Fresh-water Deposit of the Bad Lands of the Judith," 

which contains perhaps the fullest connected account of the region 

that he printed. The statements as to the stratigraphic position of the 

Judith Riverbeds are somewhat equivocal, but show no definite change 

from the views expressed in the paper last cited. The sandstones of 

the Eagle formation are referred to "No. 1," and some of the sandstones of the Claggett formation are also referred to the same horizon, 

while the shales of the Claggett, which are called " No. 4," are said to 

rest on No. 1.

In the following year Meek and Hayden 6' published a review of the 

geology of the upper Missouri region as an introduction to a paleonto- : 

logic paper. Here they first gave the geographic names Dakota, Fort

.«Ibid., pp. 45, 46.

&Trans. Am. Philos.Soc., vol. 11, pp. 123-138. 

oProc. Acad. Nat. Sci. Philadelphia, 1861, pp. 416-447.
STHATCHERND] HISTORICAL REVIEW. 19

Benton, Niobrara, Fort Pierre, and Fox Hills groups to the five numbered divisions of their Cretaceous section and called the overlying 

beds near the mouth of the Yellowstone, and lower on the Missouri, 

the "Fort Union, or Great Lignite group," at the base of which they 

placed the Judith River beds. On page 417 the following statement 

is made:

At the time we published these facts [concerning the fresh-water Jurassic of the 

Black Hills], we were led by the discovery here of fresh-water shells, in such a position, to think that some estuary deposits of doubtful age, near the mouth of Judith 

River, on the Missouri, from which Doctor Leidy had described some saurian remains 

resembling Wealden types, might be older than the Tertiary. Later examinations, 

however, have demonstrated, that the Judith beds contain an entirely different 

group of fossils from those found in the rock under consideration, and that they are 

really of Tertiary age, and hold a position at the base of the Great Lignite series of 

the Northwest.

Concerning the marine beds near the mouth of the Judith previously 

assigned to " No. 1," the authors say that it would be unsafe to refer 

them to the Dakota group.

In another paper, published by Hayden ft in 1861, the Tertiary beds 

of the Northwest are classified as "first, estuary deposits; second, true 

lignite beds; third, Wind River Valley deposits; fourth, White River 

Tertiary deposits." Of the first class he says:

The estuary deposits, of which the Judith basin may be regarded as the type, are 

quite remarkable and of a most interesting character. Opinions of a somewhat conflicting nature have been entertained in regard to them, owing to the peculiar character oi: the organic remains, but recent observations have convinced me that they are 

all of Tertiary age, and that they are quite widely distributed throughout the' Far 

West.

In the subsequent writings of Hayden there are many brief references to the Judith River beds, in which he constantly referred them 

to the Tertiary, with an occasional expression of doubt as to their exact 

position. There is no record that he revisited the original Judith 

River area after his first observations were made, but when connected 

with the Raynolds expedition of 1859-60* he passed over the same 

horizons and in part recognized them in traveling from the Judith 

Mountains to the mouth of Bighorn River on the Yellowstone.

Judith group was definitely proposed by Hayden c as a formation 

name in 1871 when discussing the Tertiary as follows:

There is one other basin near the sources of the Missouri which has already 

yielded many fossils of great interest, but which seems to be isolated from the others. 

This is what I have called the Judith basin, and inasmuch as it seems to be one of the 

ancient lake deposits, and characterized by a peculiar group of organic remains, I 

will designate the strata as the Judith group. The sediments do not differ materially from those of the Fort Union group, and they contain impure beds of lignite,

a Am. Jour. Sci., 2d ser., vol. 31, pp. 229-245.

b Kept. Geol. Expl. of the Yellowstone and Missouri rivers by Dr. F. V. Hayden, 1869. See pp. 12, 

59, 93, and 94. 

c Prelim. Kept. U. S. Geol. Survey of Wyoming, p. 97.
20 THE JUDITH RIVEK BEDS. [uuLL.257.

fresh-water Mollusca, and a few leaves of deciduous trees. But the most remarkable 

feature of this group is the number and variety of the curious reptilian remains, of 

which we have only yet caught a glimpse. ,

In 1875 the announcement was made independently by Meek" and 

by Hayden* that the marine sandstones near the mouth of Judith 

River whose position had so long been in doubt had been correlated 

by means of fossils with the Fox Hills. This correlation was based 

on the discovery of a fauna in a sandstone occurring at several localities in the South Platte Valley within a few miles of Greeley, Colo. 

The sandstone was referred to the Fox Hills, doubtless correctly, on 

account of its position at the top of the marine Cretaceous and beneath 

the Laramie, and because a large majority of the seventeen molluscan 

species recognized in it were known to be characteristic of the Fox 

Hills elsewhere. With these Fox Hills species there were four forms, 

Ta/ncredia americana, Cardium speciosum, Mactraformosa, and Mactra 

alta, that had previously been known only from the Judith River coun-. 

try, in sandstones that we now refer in part to the Claggett formation, 

though part of the species range down into the Eagle. Meek says:

From this blending together of the Fox Hills species and those of the marine 

Cretaceous beds found at the mouth of Judith Eiver on the Upper Missouri it is evident, I think, that we can not be far wrong in regarding the latter beds as holding 

a position at the horizon of the top of the Fox Hills group.

The correlation was justified by the facts then available, but it is 

now known that some of these littoral species haye a vertical range of 

many hundreds of feet and are not distributed throughout that interval in any one section, but recur whenever the conditions were suitable.

In Meek's last work, c published in 1876, there is an excellent resume 

of the stratigraphy, in which he says: d

We have long regarded the Judith River beds as forming a distinct group older 

than the Fort Union deposits.

He again identifies the beds underlying the Judith River as upper 

Fox Hills, and thinks it highly probable that the Judith River beds 

are Cretaceous, while the Fort Union may be Lower Eocene.

Prior to this time E. D. Cope had begun his contributions to the 

discussion. In his paper entitled "Synopsis of the Extinct Batrachia, 

Reptilia, and Aves of North America " e he listed the Judith River 

vertebrate fossils as Upper Jurassic species, probably meaning by that 

the Wealden. In 1874/ he regarded the Judith River beds as the top 

of the Cretaceous and discussed them under the heading "Fort Union 

or Lignite group." Three 3^ears later, after a field season in the area,

aBull. U. S. Geol. and Geog. Surv. Terr., vol. 1, pp. 39, 40. 

b Idem, p. 403.

3 A report on the invertebrate Cretaceous and Tertiary fossils of the upper Missouri country: Kept. 

U. S. Geol. Surv. Terr., vol. 9. 

d Page xlvii.

eTrans. Am. Philos. Soc., vol. 14,1870, pp. 1-252. 

f Bull. U. S. Geol. and Geog. Surv. Terr., vol. 1, No. 2, pp. 6-8.
] HISTORICAL REVIEW. 21

Cope" published his "Report on the Geology of the Region of the 

Judith River, Montana," in which some stratigraphicandpaleontologic 

details are given. The Judith River beds are treated as a distinct 

formation, about 500 feet thick, immediately overlying the Fox Hills, 

and the dark shales now included in the Claggett formation are" called 

"Fort Pierre," while other areas of shales on the Missouri farther 

east, which doubtless overlie the Judith River, are not recognized as 

distinct or in a different position. The white sandstone of the Eagle 

formation is tentatively correlated with "No. 3," or Niobrara, on 

account of its stratigraphic position. Cope's view as to the age of 

the Judith River beds is expressed in the following quotation : &

The positive evidence, then, as to the age of the. Judith River fauna is that it is 

Cretaceous, but, as might be supposed from its position, with some Tertiary affinities.

Ti- * * * . * * *

I will remark in conclusion that it is probable that the Lignitic formation will 

come to be regarded as a primary division of the Cretaceous, and equivalent as a 

whole to all or part of the older marine series. It will include as subdivisions the Judith 

River and Fort Union epochs, as already defined by Mr. Meek from the invertebrate 

fossils, and probably the Laramie or Bitter Creek epochs as distinct from them.

Similar views as to the classification and stratigraphic succession of 

the beds were expressed by Edward S. Dana and George B. Grinnell, c 

who visited the region in 1875. They spoke of the disturbed condition of the beds, but erroneously attributed it to the effects of local 

landslides, denying that there were any real faults or uplifts.

The review given thus far is confined to work on the original area 

in Montana. Meanwhile, however, the area of similar formations not 

far to the north and west in Canada began to be investigated. The 

first paper having any important bearing on the present subject was 

by James Hector d and was entitled "On the Geology of the Country 

between Lake Superior and the Pacific Ocean (between the Fortyeighth and Fifty-fourth Parallels of Latitude)." He gives a general 

section of the Cretaceous formations, at the base of which he places a 

great lignite-bearing group, including in it all the coal-bearing strata 

observed, although he admits that it may contain two distinct horizons, 

one Upper Cretaceous or Eocene and the other Cretaceous in the position assigned to it at the base of the section. His map extends as far 

south as Missouri River, where all the areas now known to consist of 

Eagle, Claggett, and Judith River formations are colored as the lowest member of his section.

The same region was more fully described in 1875 by Dr. George 

M. Dawson," who then treated all the coal-bearing beds as Tertiary

a Bull. U. S. Geol. and Geog.-Surv. Terr., vol. 3, pp. 565-597.

sidera, pp. 570 and 577.

cGeological Report in Ludlow's Kept. Reconnaissance from Carroll, Mont., to Yellowstone 

National Park and Return, pp. 97-137, Washington, 1876.

''Quart. Jour. Geol. Soc. London, vol. 17,1861, pp. 388-445 and map.

eBritish North American Boundary Commission. Report on the Geology and Resources of the 

Region in the Vicinity of the Forty-ninth Parallel from the Lake of the Woods to the Rocky Mountains.
22 THE JUDITH RIVER BEDS. [BULL.257.

and of the same horizon, though he recognized considerable differentiation in the widely separated areas and made stratigraphic observations that suggested a lower position for some of them. He speaks of 

the striking resemblance of the eastern (Souris River) area of Lignite 

Tertiary4o the "typical Fort Union," while the badlands south of 

Wood Mountain have a somewhat different aspect, and westward from 

this point there is a gradual change until near the Buttes [Sweetgrass 

Hills] the appearance is entirety distinct. This western area includes 

the beds that were afterwards described as the Belly River series, whose 

correlation with the Judith River beds is first suggested a in the following words:

Though I have not yet had an opportunity of comparing the fossils obtained in 

the western marine and brackish-water beds of the Tertiary on the forty-ninth parallel with those from the Judith River beds of the Missouri, I have little doubt of 

the identity of the formations. The age of these Judith River beds has long been an 

unsettled question, and they have only lately been included by some geologists with 

the remainder of the Lignite Tertiary and called Cretaceous. Doctor Hayden was 

only prevented from calling them Fort Union Tertiary by the occurrence of certain 

vertebrate remains the meaning of which is now better understood. The lithological resemblance between these beds of the line and those of the Judith River is close.

A few vertebrate fossils are described in an appendix by Cope, who 

calls them Fort Union. Part of them are from Judith River beds on 

Milk River and the others from probably a much higher horizon near 

Wood Mountain.

In 1881 Dawson b described the Cretaceous section of the Peace River 

region in Athabasca and named the Dunvegan sandstone, a partly nonmarine formation, intercalated in the marine Cretaceous, which he 

correlated at that time with the Niobrara and later with the Belly 

River beds. Subsequent descriptions and references by McConnell c 

and by Whiteaves a indicate that its exact position is still uncertain,

and as it lies far north of the area we have examined it need not be 

further considered except to remark that it may represent either the 

Eagle or the Judith River formation.

Dawson returned to a more detailed study of the western plains 

immediately north of the international boundary and soon discovered 

that a part of the beds he had previously grouped under the Lignite 

formation as Tertiarj^ really underlies marine Cretaceous shales 

referred to the Fort Pierre. This lower formation was called the 

Belly River series, and in the preliminary announcements 6 was correlated with the Dunvegan, and also doubtfully with the Niobrara. In 

the official report just referred to the section shows Laramie at the

a Pp. 156,157.

bAnn. Rept. Geol. Surv. Canada, 1879-80, p. 115B. See also Am. Jour. Sci., 3d ser., vol. 21, pp. 391- 

394, and Canadian Naturalist, new series, vol. 10, pp. 20-22.

c Ann. Kept. Geol. Surv. Canada, 1890-91, n. a., vol. 5, pt. 1, pp. 54-55D.

<*Trans. Roy. Soc. Canada, vol. 11,1893, sect. 4, pp. 9,10.

eRept. Geol. Surv. Canada for 1880-81-82, pp. 1-23B, 1883. Trans. Roy. Soc. Canada, vol. 1,1883, sect. 

4, pp. 42, 43.
.STANTON 

HATCHER4ND ] HISTORICAL REVIEW. 23

top, consisting of the named subdivisions Porcupine Hills, Willow 

Creek, and St. Mary River, succeeded below by unnamed yellowish 

sandstones and shaly beds, with a mingling of fresh-water and brackish or marine mollusks, still referred to the Laramie. Beneath these 

are Fox Hills and Pierre beds. The lower part of the section, beneath 

the Pierre, is described as follows:

Belly River series. Sandstone, shales, and sandy clays, generally of pale grayish 

tints. Marine and fresh-water fossils.

Series apparently underlying the last on the Bow and Belly, but on the stratigraphical position of which some doubt yet remains owing to the resemblance of its 

estuarine fauna to that of the Judith River. Brownish and yellowish sands and 

clays.

The Judith River beds are treated as a part of the Laramie, and the 

correlation of the Belly River beds is indicated in the following statements:

The pale beds underlying the Pierre in this region represent, with little doubt, 

the Dunvegan sandstones of the Peace River section. They are also evidently identical with those described by Professor Cope as occupying a similar position on the 

Missouri [now known as the Eagle formation]. This subdivision, which appears 

most probably to hold the position of the Niobrara in the Nebraska section, is therefore one of great persistence in the Cretaceous.

The same correlations are made in the paper published, by the Royal 

Society of Canada.

In 1884 Dawson ft extended the Belly River beds downward to 

include the }7 ellowish and brownish sands and clays with a Judith 

River fauna, and repeated the correlation of the upper part of the 

formation with the Eagle sandstone, while suggesting a lower position 

for the Judith River beds. He says:

The upper part of the Belly River series evidently represents the pale, sandy beds 

which occur on the Missouri in a similar position with reference to the Pierre; and 

the latter holds coal or lignite at the base in this district, as described by Prof. E. D. 

Cope, on that river.

In reference to the fossils, he makes the following very proper 

suggestion:

The fossils of the Belly River series have not .yet been critically examined; but their 

resemblance to those of the Judith River is so complete that I am strongly inclined 

to revert to Messrs. Meek and Hayden's original views respecting the stratigraphy 

of the latter beds and to suggest, though with some hesitation, that the species 

figured on'pis. 37-39 of Meek's work on the Cretaceous and Tertiary fossils of the 

upper Missouri, as from a peculiar development of the Fox Hills group, have really 

been derived from beds underlying the Pierre.

The species referred to are-from near the mouth of Judith River

id ai 

tions.

"Science, n. s., vol, 3, pp. C47, G4S.

and are now known to have come from the Claggett and Eagle forma-
24 THE JUDITH KIVER BEDS. [BUM,257.

Dawson's final report" on the region in the vicinity of Bow and 

Belly rivers, Northwest Territory, published in 1885, gives detailed 

descriptions of the Belly River and associated formations and a full 

statement of the evidence for its accepted stratigraphic position 

beneath about 830 feet of marine Cretaceous correlated with the Fort 

Pier re and Fox Hills. The area mapped extends from a few miles 

south of the international boundary to latitude 51° 20' and from longitude 110° 45' to the Rocky Mountains. The Belly River beds are represented as covering a large area, broadening southward across the 

eastern portion of the map. West of this area of Belly River beds 

overlying formations occupy a low, broad syncline, while in the 

uplifted belt along the foothills of the Rocky Mountains all the Cretaceous formations are mapped together under one color, because the 

complex region was not studied in sufficient detail. In the general 

section Dawson assigns maximum thicknesses to the formations as 

follows: To the members of the Laramie 5,750 feet; Fox Hills, 80 feet; 

Fort Pierre, 750 feet; Belly River, 910 feet; "Lower dark shales," 

800 feet.

The conclusions as to the Belly River and Judith River beds are 

summarized in these words: 6

Briefly.stated, it would appear from the investigations now reported on that considerable areas of the beds which in 1874 I called "Lignite Tertiary" here and in 

previous announcements designated as Belly River series must be relegated to a 

position below the Pierre shales, or at least to one below an upper portion of these 

shales. The beds thus separated as the Belly River series were, in 1875, by me correlated with the Judith River series of the Missouri. Additional and extensive 

collections of fossils since obtained and now being worked out confirm and strengthen 

this correlation and lead to the presumption that the so-called Judith River series 

must also occupy a position well down in the undoubted Cretaceous. It may be

added that this was the view originally held by Messrs. Meek and Hayden, and supported, it would appear, not alone on the supposed analogies of the vertebrate 

remains examined for them by Professor Leicly, butalso on stratigraphical evidenceevidence which perfectly agrees with the impressions resulting from such cursory 

examination as I was able to make of.the Missouri sections from the deck of a 

steamer while ascending the river in 1881.

An incidental reference in a footnote on page 122c makes it evident 

that Dawson still failed to discriminate between the Eagle and the 

Judith River formations on the Missouri, and he did not recognize any 

horizon in his area corresponding to the Eagle formation. It seems 

remarkable that this formation, which is°so well developed on the 

Missouri only about 75 miles south of the Canadian boundaiy, should 

disappear completely from the sections in the Sweetgrass Hills and 

along Milk River near the boundary. Several facts gleaned from 

Dawson's careful descriptions and from the subsequent paleontologic 

report c favor the suggestion that the Eagle sandstone really occurs

aQeol. Surv. Canada, Kept. Prog, for 1882-1884, pp. 1-1090 and map.

&Mem, p. 119c.

cCont. Canadian Palaeont., vol. 1, pt. 1, 1885.
8TANTON 

HATCHEREARND ] HISTORICAL REVIEW. 25

hero and has been referred to the Belly River. The castellated sandstones along Milk River between Verdigris Coulee and Dead Horse 

Coulee, as described on page 40c and as figured" in an earlier report, 

resemble the Eagle sandstone much more closely than any part of the 

Judith River or any other horizon in the general region. This same 

sandstone horizon was recognized in Rocky Spring Ridge and on the 

west flank of West Butte (Sweetgrass Hills) resting on dark shales 

which at the last-named localit}r have an estimated thickness of 800 

feet. Now, this thickness is much too great for the shales of the 

Claggett formation, which underlies the Judith River and is the same 

as that of the Fort Benton shales beneath the Eagle. Dawson 

expressly states 6 that the dark shales of these" two localities do not 

agree very satisfactorily with those farther east on Milk River, at the 

mouth of Fakowki Coulee, which we now recognize as belonging to 

the Claggett formation, and the fossils reported from them at both 

West Butte and Rocky Spring Ridge include Baculites asper and 

Scapkites warreni, of which, the latter especially is a characteristic 

Fort Benton species. As the writers have not visited the localities 

nor seen the fossils in question, they can only suggest that possibly 

the structure has been misinterpreted and that part of the area mapped 

as Belly River really belongs to the Eagle formation.

.The invertebrate fossils of the Belly River beds and associated formations have been described by Prof. J. F. Whiteaves, 6' and the fossil 

plants have been treated by Sir William Dawson,d with stratigraphic 

notes by Dr. George M. Dawson. Their general conclusions as to 

the evidence of the fossils are expressed in the following quotations. 

Whiteaves says:

Judging by their respective invertebrate faunas, it would seem impracticable to 

separate the "Belly River series" from the Laramie, and more especially from the 

"Judith River group," on purely paleontological evidence. 6

The invertebrate fauna of the " Belly River series " seems to be essentially the 

same as that of the "Laramie" of the United States and Canada, unless more 

than one formation has been confounded under the latter name, and * * * it is 

at present scarcely possible to separate the "lower dark shales" of Doctor Dawson's Bow and Belly River report from the " Fort Pierre and Fox Hills" groups, on 

purely paleontological grounds./

Sir William Dawson states in the first and third papers cited that, 

"it scarcely seems possible to distinguish by fossil plants alone the 

lower Laramie beds from those of the Belly River." He also remarks 

that the Dunvegan series of the Peace River region probably corre-

"Rept. Prog, for 1880-1882, frontispiece of Doctor Dawson's report. 

6Geol. Surv. Canada, Kept. Prog, for 1882-1884, p. 125c. 

eCont. Canadian Palseont., vol. 1, pt. 1,1885.

dTrans. Roy. Soc. Canada, vol. 3, sec. 4, pp. 1-22,1886. Idem, vol. 4, sec. 4, pp. 19-34, 1887. American Naturalist, vol. 22, 1888, pp. 953-959. 

eCont. Canadian Palteont., vol. 1, pt. 1,1885, p. 55. 

/Idem, p. 89. . . 
26 THE JUDITH KIVER BEDS. [BULL.257.

sponds in time with the Niobrara. The paleontologic evidence and 

relationships will be fully discussed on later pages.

Additional areas of Belly Kiver beds on the east and north of Dawson's area were described and mapped by R. G. McConnell a and by 

J. B. Tyrrell, 6 respectively, who confirmed Dawson's conclusions concerning the stratigraphic position of the formation so far as the overlying beds were concerned, but still left the exact age of the underlying formation undetermined.

In the United States the discussion concerning the age of the 

Laramie continued long after Meek and Haj7 den's publications ceased; 

and since the Larainie was generally held to include or to be the equivalent of the Judith River beds, the age of the latter was frequently 

involved in the discussion. The paleobotanists Newberry, Lesquereux, and Ward contributed many articles to this controvers}r, but 

they had no direct bearing on the Judith River question because no 

definitely described fossil plants were known from the Judith River 

beds.

From 1877 to 1891 -Dr. C. A. White published many papers in 

which the invertebrate paleontology and the geologic relations of the 

Judith River beds are more or less fully treated. At first 6 the 

Judith River was treated as a separate formation immediately underlying the Fort Union and holding the same relative position as the 

Laramie in southern W}^oming, but in the following year the term 

"Laramie" was used in a broader sense, as follows:

The Laramie group includes as either subordinate groups or regional divisions 

both the Judith Eiver and Fort Union series of the Upper Missouri River; the Lignitic series east of the Rocky Mountains in Colorado; the Bitter Creek series of 

southern Wyoming and adjacent parts of Colorado; and also the Bear River Estuary 

beds, together with the Evanston coal series of the Valley of Bear River and adjacent

parts of Utah.** * * * . . Some of the known portions of this great group doubtless represent different 

stages of the Laramie period, but the members'just designated arej as a rule, 

understood to represent different geographical developments of its strata with 

modifications of its fauna rather than separate successive epochs of time in the 

geological period which is represented by the whole great group. The'broof of the 

identity of these widely separated portions of the Laramie group consists in th.e 

recognition of various species of fossil moll asks in all of them that are found in some 

one or more of the others, thus connecting the whole by faunal continuity. Similar 

proof has also been obtained by Professor Cope in the discovery of certain species of 

vertebrate fossils in more than one of these geographical members of the Laramie 

group. fSo far as the Judith River, Fort Union, and Bitter Creek beds are 

concerned these views are consistently held in all of White's subse-

« Ann. Kept. Geol. Surv. Canada, n. s., vol. 1,1880, pp. l-78c.

bldem, vol. 2, pp. 1-152E, 1887.

cBull. U. S. Geol. and Geog. Surv. Terr., vol. 3,1877, pp. 608-609.

dldem, vol. 4,1878, p. 721.

eldem, p. 865.
] ' HISTORICAL EEVIEW. 27

quent papers. Tn 1883, accompanied by Prof. Lester F. Ward, he 

visited the Judith River and Fort Union areas along the Missouri, but 

he did not see any reason for changing the later conclusions of Meek and 

Hay den and of Cope, and his stratigraphic observations were not fu\\y 

published. Concerning the Fort Union area he made the following 

statement: a

During the,summer of 1882 I gave especial study to the geology of the region about 

Fort Union, extending up the Yellowstone Valley, and including all the localities 

from which Doctor liayden obtained the fossil plants here referred to [Fort Union 

plants described by New berry]. The result of that study has been to ascertain that 

only one formation, namely, the characteristic Fort Union group, Avhich is nothing 

more or less than a part of the great Laramie group, occupies that whole region. 

That is, with the exception of one or two small exposures of the Fox Hills Cretaceous group, upon which the Laramie strata rest conformably, no other than Laramie 

strata are to be found there.

In the excellent correlation paper on the Cretaceous, White 6 gave a 

general discussion of both the Laramie 0 and the Belly River*' formations, with a review of the literature. He still included the Judith 

River, Fort Union, etc., in the Laramie and held that it was deposited 

in a great land-locked sea of mainly brackish waters.

Concerning the Belly River beds he states that "certain observed 

conditions of strata exposed along the Missouri River in northern 

Montana apparently indicate its presence there. It also seems not 

improbable that some of the strata in the upper part of the valley of 

the Musselshell River, in Montana, which have been' referred to the 

Laramie, 6 really belonged to the Belly River formation." The first 

reference is evidently to the occurrence of the Eagle formation 

between Fort Ben ton and Judith, and the second reference is probably 

to an actual occurrence of Judith River beds which will be referred to 

again. The position of the Belly River formation is thus stated:

The marine strata which overlie the Belly Eiver are certainly referable to the Montana formation, but whether they represent the whole o.^ that formation or not it is 

at present impossible to say. That is, it is not yet certainly known whether the 

Belly River formation is interposed between the top of the Colorado and the base of 

the Montana, or 'between a large upper and a small lower part of the last-named 

formation. The'former condition is assumed to exist, although it is not yet certain 

that some of the'fossil species discovered beneath the Belly River strata do not also 

occur in the Montana formation.

From the intimate relationship between the Belly River and Laramie 

faunas,, especially the specific identity of'certain gill-bearing Mollusca 

in both, White inferred that there must have been physical continuity 

between the formations. The assumed relations of the Belly River to

a Am. Jour. Sci., 3d ser., vol. 26,1883, p. 121. 

>> Bull. U. S. Geol. Survey No. 82,1891.

a Pages 145-153.

rf Pages 173-177.

eSee.Lindgren, W., Tenth Census of tlie United States, vol. 15, pp. 743-74f>.
28 THE JUDITH EIVEE BEDS. [BULL. Hi?!

the associated formations are shown diagrammatically by representing 

the Belly River formation as a wedge inserted between the Colorado 

and Montana groups, gradually thickening so as to replace more and 

more of the Montana, until in some hypothetical area it becomes continuous with the overlying Laramie and is not separable from it.

In 1886 Mr. W. Lindgren" published a description, with sections, of 

a region between the Yellowstone and Musselshell rivers in Montana 

that is now known to contain Judith River beds. The section as 

described is remarkable for the ver}^ great thickness (8,600 feet) of 

beds assigned to the Laramie, and for the intercalation of marine beds 

with Placenticeras and Baculites within the Laramie. The AVliters 

have traveled along the line of Lindgren's section that extends northeasterly from Billings, and according to their interpretation the sandstone forming the cliffs at Billings, which he referred to the Fox Hills, 

really belongs to the Eagle formation, and his Laramie must include 

the Claggett, Judith River, and Bearpaw, as well as the Laramie and 

probably some overlying formations.

Cope b briefly discussed the Belly River beds of Canada in 1887. He 

stated that the flora and the fauna, vertebrate and invertebrate, are 

identical or nearly so with the Laramie, and expressed a suspicion 

that there had been some error of observation.

About this time horned dinosaurs began to be recognized at various 

localities in the West, and the beds yielding them were called l>y Prof. 

O. C. Marsh c Ceratops beds and referred to a single horizon of the 

Laramie. Mr. J. B. Hatcher, who had done the field work in collecting the vertebrate faunas of these beds, maintained that there was 

paleontologic and stratigraphic evidence that they include at least two 

horizons. His views are expressed in the following quotations: ^

The actually known area of the Ceratop8 beds is indeed very limited, and from 

these areas we should exclude certainly the Judith River or upper Missouri, and 

very likely the Black Butte locality in southwestern Wyoming. The beds of the 

former certainly and those of the latter almost certainly belong to an older horizon 

than those of the Denver or Converse County localities; the latter may be considered as the typical locality for the Ceratops beds. All of the dinosaurs from the 

Judith River country are smaller, less specialized forms than those from the Converse 

County and Denver localities, as has already been observed by Marsh.

Speaking of the Converse County locality, he says:

It would doubtless be better to restrict the limits of the Ceratops beds to those 

strata in which horned dinosaurs occur, and to consider the underlying 400 feet of 

barren sandstones as the equivalent of the Judith River beds. * * *

The terms Fox Hills and Laramie as now used can not be taken to represent distinct and different periods of time, for,.as has been shown by G. M. Dawson,

a Tenth Census United States, vol. 15, pp. 743-746. ,

6 American Naturalist, vol. 21,1887, pp. 171,172, and 445-462.

c Am. Jour. Sci., 3d sen, vol. 38,1889, p. 501. Marsh definitely referred the Judith River beds to the 

same horizon as the Ceratops beds of Converse County, Wyo., in the Geology of the Denver Basin: 

Mon. U. S. Geol. Survey, vol. 27,1896, p. 478.

rf American Naturalist, vol. 30, 1896, pp. 31 C, 117.
] HISTORICAL REVIEW. 29

Selwyn, and McConnell in the Belly Kiver region in Canada, and frequently 

observed by the writer on the upper Missouri in Montana, marine beds with typical Fox Hills fossils have been found interstratified with fresh and brackish water 

beds containing characteristic Laramie fossils, showing conclusively that the' two 

periods were in part at least contemporaneous; the one representing the marine 

and the other fresh or brackish water forms existing at the same time and in not 

widely.separated regions, these alternations in the nature of the fauna in the same 

locality having been brought about by successive encroachments and recessions of 

the sea.

In 1896 Mr. Whitman Cross a discussed the age of the Arapahoe and 

Denver formations and referred to related beds in other regions, 

especially those yielding horned dinosaurs, lie suggested that "the 

Judith River strata may perhaps represent the Arapahoe or some other 

post-Laramie formation, and not the true Laramie of Colorado and 

Wyoming." He quoted from the manuscript notes of Mr. T. W. 

Stanton the description of a section on Dog Creek, near Judith, Mont., 

which includes the lower 300 feet of Judith River beds and underlying strata then referred to the Fox Hills, but now designated as the 

Claggetl: and the upper part of the Eagle formation.

Mr. W. H. Weed 6 has described the section in the region of the 

Crazy Mountains between Yellowstone and Musselshell rivers, where 

the Judith River beds are now known to exist, but he failed to recognize the formation. It is very probable that the brackish-water fossils cited 6 as coming from the Livingston formation north of the 

Crazy Mountains were collected from an outcrop of Judith River 

beds. .

In the Fort Benton folio/* published in 1899, Weed named and 

described the Eagle formation, stating that it rests on the Colorado 

shales and is overlain by 2,000 feet of marine beds referred to the 

Montana formation, and that it has yielded fossil plants similar to 

those of the Belly River beds. The area mapped on the Missouri is 

west of all the outcrops of Judith River beds.

A few fossil plants from the Eagle formation near "Coal Banks" on 

the Missouri were described by'Dr. F. H. Knowlton* in treating the 

flora of the Montana formation. These were described as Belly River 

species, and in justification of this correlation a brief manuscript note 

by Stanton, giving his views on the stratigraphy and correlation of 

that part of-* the section, was published. The concluding portion of 

Stanton's note is as follows:

It is evident from the stratigraphy and from the marine invertebrate fauna of the 

underlying and overlying strata that the sandstones and the associated coal beds and

. "Geology of the Denver Basin: Mon. U. S. Geol. Survey, vol. 27, pp. 239-241.

/'The Laramie and the overlying Livingston formation in Montana: Bull. U. S. Geol. Survey 

No. 105,189;!. The Fort Union formation: Am. Geologist, vol. 18,1896, pp. 201-211.

"Bull. U. S. Geol. Survey No. 105, p. 33.

d Geologic Atlas of the United States, folio 55.

cBull. U. 3. Geol. Survey No. 163,1900. This paper was submitted for publication before the Fort 

Benton folio was issued, and consequently the name Eagle is not used for the formation.
30 THE JUDITH BIVEE BEDS. [BULL. 257.

plant-bearing horizons in the neighborhood of Coal Banks on the Missouri River are 

on essentially the same horizon to which the Belly River series was assigned by Dr. 

G. M. Dawson, and to which a part of the Canadian beds so named undoubtedly 

belong. But in Doctor Dawson's full and careful description of the Belly River 

series it is pointed out that in certain areas referred to that series the stratigraphy is 

not clear, and the beds may overlie the Montana shales instead of underlying them. 

It happens that most of the Belly River fauna, which consists chiefly of Laramie 

species, was collected in those doubtful areas. I suspect that in Canada two distinct 

formations, separated by marine beds, have been confused under the term Belly 

River series, and that a large part of the fauna, and possibly also of the flora, was 

collected from the upper horizon, which included the Laramie and possibly even 

later beds.

In 1902 Mr. Earl Douglas a described a formation under the local 

name Fish Creek beds, which he correctly correlated with the Belly 

River. The locality is a few miles east of the Crazy Mountains area 

previously described by Weed. The Eagle formation also occurs in 

the section, but was called Niobrara.

In the same year the vertebrate fauna of the Belly Riverbeds in 

Canada was reviewed and described by Prof. H. F. Osborn 6 and Mr. 

L. M. Lambe, the former contributing the general discussion and the 

latter the paleontologic descriptions. The conclusions as to correlation and stratigraphic position were more concisely stated in an 

abstract by Osborn,c from which the following brief extracts are taken:

The [Canadian] Survey had established beyond question, geologically, that the 

Belly River series is mid-Cretaceous, that it underlies the Montana or Fort PierreFox Hills group, and overlies the Fort Benton and Dakota groups. * * ' * It soon 

appeared * * * that the Belly River vertebrates were of decidedly different and 

apparently of older type than those from the Laramie beds of Converse County, 

Wyo., described by Marsh, and were rather to be compared with those described by 

Leidy, Cope, and Marsh, from Montana, chiefly from the Judith River beds, which

overlie the Fort Pierre in a region by no means distant geographically.

* * * * * * *

The fossil land vertebrates hitherto described from Montana probably are, in part

at least, of mid-Cretaceous or Belly Kiyer age, although the true Judith River beds

certainly overlie the Fort Pierre and are of more recent age.

Hatcher a commented on the paper last cited, correcting a statement 

concerning the locality of certain fossils, and giving reasons for 

believing that the stratigraphic position of the Judith River beds is 

lower than the horizon to which he assigned them in 1896. Stanton 6 

replied to this note, asserting that the formation in question overlies 

the Pierre and Fox Hills, called attention to the Eagle formation, and 

again suggested that two or more horizons may have been confused in 

the Belly River beds of Canada.

«Proc. Am. Philos. Soc., vol. 41, pp. 210,211. The section is partly described in an earlier note. 

(Science, n. s., vol. 15, 1902, pp. 31-32.)

& On Vertebrata of the mid-Cretaceous of the Northwest Territory: Cont. to Canadian Palseont., 

vol. 3, pt. 2,1902.

cScience, n. s., vol. 16, 1902, pp. 673-676.

d Idem, pp. 831-832.

e Idem, pp. 1031-1032.
8THATCHEB? D ] GENERAL FEATURES OF THE ORIGINAL AREA. 31

Prof. S. W. Williston" contributed to the discussion in a note on 

the Laramie of Converse County, Wyo., holding that these deposits as 

well as the Judith River are contemporary, in part at least, with the 

Fox Hills, and that the fauna presents in some respects "a startling 

resemblance to that of the Judith River and Belly River series."

Additional notes bearing on various phases of the discussion were 

published, during 1903 by Osborn, b Hatcher, c C. H. Sternberg, d and 

0. P. Hay," and ending with a brief note by Hatcher and Stanton/ on " the stratigraphic position of the Judith River beds and their 

correlation with the Belly River beds," in which they give the principal results of the field work which is fully described in the present 

paper.

DESCRIPTION OF JUDITH RIVER BEDS, BY AREAS.

ORIGINAL AREA.

GENERAL FEATURES.

The histoiy of the exploration of the region along Missouri River 

near, the mouth of Judith River and of the description of its geologic 

and topographic features by Dr. F. V. Hayden has been briefly 

given in preceding pages. While some of Doctor Hayden's determinations and correlations have since been shown to be erroneous, 

as Avas to be expected from the pioneer nature of his work, the reader 

of his most extended sketch/ if familiar with the region, can not fail 

to be impressed with his ability as an observer and the fidelity and 

clearness with which he describes the chief geologic features of the 

country;

The following extracts from Doctor Hayden's paper are quoted here 

as bearing directly upon the stratigraphic limits and geographic distribution of the Judith River beds as originally understood and defined 

by that author:

Near the mouth of the Judith River, not far from the sources of the Missouri, in 

latitude 47° 30/ , longitude 109° 30/ , is a wild, desolate, and rugged region which I 

have called the "Bad Lands of the Judith," in contradistinction to those of White 

River. No other portion of the upper Missouri country exhibits the effects of erosion 

and denudation on so large a scale, and to add to the picturesque effect of the country 

the variegated strata are distorted and folded in a wonderful manner by the action 

of the subterranean forces that have elevated, the mountain masses in the vicinity. 

The surface of the country occupied by the deposit I am about to describe is cut up 

into ravines and canyons, with nearly vertical sides, rising to a height of 400 to 600 

feet above the bed of the river, with scarcely a tree or shrub to greet the eye of the

u Science, n. s., vol. 16, 1902, pp. 952-953.

l> Idem, vol. 17, pp. 356,357.

cldem, pp. 471, 472, and Am. Geologist, vol. 31, pp. 369-375.

d Science, n. s., vol. 17, pp. 870-872.

e Am. Geologist, vol. 32, pp. 115-120.

/Science, n. s.,vol. 18, pp 211-212.

(/Trims. Am. Philos. Soc.-, 1860, pp. 123-138, witlui map.
32 THE JUDITH KIVER BEDS. [BULL.267.

explorer. A few scattering pines cap the summits of the hills and draw a scanty 

nourishment from a thin, dry soil, but it may be regarded for the most part as an 

inaccessible desert suited only as a retreat for the buffalo and mountain sheep.

The area occupied by this peculiar basin I could not determine with precision, but 

have estimated it at about 40 miles from east to west and from 15 to 30 from north 

to south, and it is separated into two nearly equal portions by the Missouri. The 

Judith River rises in the Judith Mountains, pursues a course nearly due north, for 

the most part through Cretaceous strata, and empties into the Missouri in latitude 

48°, longitude 106°. The Judith River forms the north [western] boundary of this 

basin. The Muscleshell River also rises near the Judith Mountains, but takes a 

course a little east of north, flows through Cretaceous formation No. 4, and empties 

into the Missouri near latitude 47° 30X and longitude 108°. That portion of the "Bad 

Lands" which is formed of the estuary deposit under consideration lies between 

these two streams. About 30 miles north of the entrance of the Judith River into 

the Missouri is the Bear's Paw Mountain, a small range, the highest.peak of which 

is elevated about 2,000 feet. On the same side of the Missouri and in nearly a northeasterly direction are the Little Rocky Mountains, a range similar to the Bear's Paw, 

though apparently disconnected from it. On the south side-of the Missouri, about 

15 miles southwest of the mouth of the Judith, the Square Buttes may be seen rising 

400 or 500 feet above the surrounding prairie, and are the nearest upheaval of trappean rocks to the Missouri in this region. From 30 .to 50 miles south is quite an 

extensive range, called the Judith Mountains, which have not yet been explored 

geologically. Here comparatively small local upheavals seem to represent the dying 

out of the intense subterranean forces which uplifted the vast Rocky Mountain chain. 

It will be important to understand the geographical position of these mountains in 

order to fully appreciate the sources of the power which has disturbed the strata of 

the more recent fossiliferous rocks, a point which will be again referred to in this 

paper. i

Lewis and Clarke, in their interesting account of an expedition to the sources of the 

Missouri, gave a brief but accurate description of the physical features of thisremark- 

 able region, but dwell more in detail on the picturesque portions near the "Stone 

Walls," which are composed of a basis strata upon which the estuary deposits of the 

"Bad Lands" of the Judith rest, which are doubtless of the age of Cretaceous 

formation No. 1, or upper Jurassic.

In the above description there are some errors relating to the 

geography, such as the statement that Musselshell River rises near

the Judith Mountains; and the sandstones ("Stone Walls" of Lewis 

and Clarke) upon which, according to Hay den's statement, the estuary 

deposits of this region rest, were erroneously identified with Cretaceous No. 1, although they are now known to represent the Eagle 

formation and to be immediately underlain by the Benton and overlain by the Claggett formation. However, the stratigraphic limits of 

the Judith River beds are fixed with reasonable accuracy, while the 

geographic limits of the type exposure is very accurately outlined 

on the map accompanying his paper.

From Doctor Hayden's paper and the personal observations of the 

present authors the original area of the Judith River formation may 

be defined as lying between the mouths of Judith River on the west 

and Little Rocky Mountain Creek on the .east and extending both 

north and south of Missouri River for an average distance of about 20
STANTON AND! HATCHBB J GENERAL FEATURES OF THE ORIGINAL AEEA. 33

miles. Throughout almost this entire region typical and characteristic exposures of these beds are everywhere observable. They rest, 

with at least apparent conformity, upon the darker-colored marine 

sandstones and shales of the Claggett formation, and in certain favored 

localities are overlain by material resembling the typical Pierre shales, 

in this region known as the Bearpaw shales. As these shales are soft 

and friable they yield readily to erosion, and over large areas, especially in the vicinity of Missouri River, where erosion has been most 

rapid, they have been completely carried away and the Judith River 

beds appear as the uppermost of the series. This fact, together with 

the resemblance between the lithology and fauna of the underlying 

marine sandstones and those of the Fox Hills sandstones in the regions 

farther south, for years caused many geologists to mistake the true 

stratigrapbic position of the Judith River beds, and to refer them 

unhesitatingly to the Laramie. In certain localities, however, the 

Bearpaw shales have resisted erosion and are seen in their normal position conformably above the harder and lighter-colored beds of the 

Judith River formation. This is especially true on Cow Creek, a 

small northern tributary of the Missouri rising in the eastern end 

of the Bearpaw Mountains. At many places along this stream the 

Bearpaw shales rest upon the Judith River beds, and along the old 

Fort Benton and Cow Island trail between Cow Creek and the southeastern extremity of the Bearpaw Mountains the Judith River beds 

are overlain by about 600 feet of these shales.

The Judith River beds of this region consist of light ash-colored 

sandstones, alternating with usually darker colored and more friable 

shales and clays mingled with frequent seams of lignite, which in places, 

more especially toward the top of the series, attain considerable 

importance, not infrequently forming beds of fairly pure lignite with a 

thickness of several feet. The most important and most constant of 

this series of lignite seams occurs very near the top of the Judith 

River beds and is frequently overlain by a shell breccia from 1 foot 

to 3 feet thick, and in most instances is composed almost entirely of 

the shells of Ostrea subtrigonalis, although at some places Corbicula 

cyth&riformis, Corbula subtrigonalis, and other brackish-water forms 

are common.

The average thickness of the Judith River beds in this region is about 

500 feet, if there is included in them the brackish (sometimes apparently purely marine) beds at the top and bottom of the series. These 

brackish beds are lithologically very similar to the intermediate freshwater deposits, which are frequently rich in the remains of fresh-water 

Mollusca, and contain also in some abundance, but usually in a very 

fragmentary condition, the bones and teeth of fresh-water fishes and 

reptiles and of terrestrial dinosaurs. Everywhere through these beds

Bull. 257 05 3
34 THE JUDITH K1VER BEDS. [BULL.257.

fossil plants are found in considerable abundance, but usually are not 

well preserved.

The frequency with which the different strata of sandstones and 

clays replace one another, both laterally and vertically, together with 

the great disturbances that have taken place subsequent to the deposition of the Judith River beds, renders it extremely difficult, if not 

impossible, to fix upon any definite horizons or strata within the limits 

of the fresh-water series that may be followed and recognized with 

certainty, even in reasonably adjacent sections. A detailed section 

taken at any point is of little value, since a similar section made at a 

distance of only a mile or two would give a quite different sequence 

of the alternating strata of sandstones and shales.

Almost every traveler has noted the complicated folding and faulting. Grinnell and Dana a attributed these disturbances to landslides 

due to the action of water, but Cope 6 pointed out the error of this 

view. No better description of the frequency of these disturbances, 

and the difficulties they have caused the stratigrapher, can be given 

than that of Doctor Hay den, which is as follows : c

It presents perhaps the most rugged scenery on the Missouri River, the denudation and erosion having been much greater than at the Bad Lands of White Kiver. 

But the most remarkable feature of this basin is the wonderful disturbance of the 

strata. So much are the beds disturbed and blended together by forces acting from 

beneath that it seems almost hopeless to obtain a section showing with perfect accuracy the order of superposition of the different strata.

EXPOSURES ON DOG CREEK.

Although the deposits under consideration were named from Judith 

River, they are rather poorly represented on that stream. They 

are well shown in the bluffs of Dog Creek, a small tributary emptying into the Missouri from the south, about 2 miles below the 

mouth of Judith River. The exposures on Dog Creek and on the 

north side of Missouri River immediately opposite the mouth of Dog 

Creek have been most frequently visited by geologists and paleontologists, and are therefore the best known of all the areas of the Judith 

River beds. Here, unfortunately, the beds are not of much value to 

the paleontologist, and are even more unsatisfactory to the stratigrapher, since the overlying Bearpaw shales are not adequately 

represented.

Dog Creek, or Dog River, as it is given on some maps, rises in the 

Moccasin Mountains, a small outlier of the Judith Mountains. After 

leaving these mountains it flows for perhaps 25 or 30 miles in a northerly direction through a narrow and shallow valley with rolling, 

grass-covered table-lands on either side. At intervals along the banks

iGeol. Kept, in Ludlows's Kept, on a Reconnoissance from Carroll, Mont., to Yellowstone National 

Park, 1876, pp. 97-137.

5 Bull. U. S. Geol. and Geog. Surv. Terr., vol. 3, pp. 565-597. 

o Proc. Acad. Nat. Sci. Philadelphia, 1857, pp. 115-116.
EXPOSURES ON DOG GREEK. '35

of the stream and its tributaries and on the slopes of the steeper hills 

exposures of the sandstones and shales of the Judith River beds may 

be seen. About 12 or 15 miles above its mouth the stream leaves this 

comparatively open country and enters a deep, rugged canyon. The 

surrounding country now suddenly changes from a rolling, grasscovered plain to a wild, desolate, but picturesque region, deeply dissected by numerous canyons, presenting mile after mile of almost 

perpendicular walls with jutting headlands capped with spires and 

minarets or flanked perhaps by numerous pillars detached from the 

perpendicular sides of the canyon wall, each threatening at any 

moment to add its towering mass to the talus-covered slope below. 

About the crest of the bluffs are considerable forests of pine and 

spruce which formerly afforded a sufficient supply of fuel for the 

river steamers that plied between Fort Benton and the lower Missouri. 

A few of these trees may also be seen clinging even to the perpendicular cliffs of the canyon walls, while on the less rugged slopes 

there is a sparse and scattered growth of small shrubs and bushes 

belonging for the most part to the genus Arternisia. In favored 

localities, especially at the summits of landslides, where disturbances 

in the beds have formed small basins which receive and retain the 

moisture brought by heavy rains, the chokecherry, Prunusvirginiana, 

often forms considerable thickets. In the bottom of the canyons the 

banks of the streams are fringed with broad and long-leaved cottonwood, while scattered about and often forming impenetrable thickets 

are buffalo or bullberry bushes. Such are the badlands of the upper 

Missouri. The nature of the topography made this region the last 

retreat for the larger game animals of this district. The inaccessible 

nature of the region afforded these animals their greatest protection, 

and they lingered here long after they disappeared from the surrounding plains and mountains. This was especially true of the deer and 

bighorn or mountain sheep, both of which animals were still abundant 

when the region was first visited by one of the present writers in 

1888. During our visit the past season, however, the mountain sheep 

seemed to have been nearly or quite exterminated, while only a few 

deer remained.

Dog Creek flows through this badland country in a deep and rugged 

canyon until it emerges upon the narrow valley of the Missouri, about 

a mile above its mouth. The walls of the canyon on either side are 

composed for the most part of the light ash-colored sandstones and 

darker shales and clays of the Judith River beds. This is especially 

the case in the upper portion of the- canyon. In the lower half of the 

canyon the darker buff-colored sandstones and dark sandj7" or black 

clay shales of the underlying Claggett formation constitute a considerable portion of the bluffs. For considerable distances the Judith 

River beds are nearly or quite horizontal, and conformably overlie
36 THE JUDITH RIVER BEDS. [BULL. 257.

the Claggett formation in such a manner that it is difficult to determine 

where one formation ends and the other begins, although in the field 

a bed of yellowish brown sandstone varying in thickness from 1 foot 

to 20 feet or more was regarded as the upper limit of the Claggett 

formation. This bed of sandstone appeared fairly constant, not only 

in this, but in other areas of the exposures, and it was referred to in 

our notes as the Tancredia sandstone, owing to the presence in it in 

considerable abundance of fossil shells belonging to that genus. From 

the persistence of this sandstone and from the fact that it marked the 

beginning of a decided change in the lithology of the underlying and 

overlying beds it would certainly form a convenient delimitation 

between the two series of deposits, and should perhaps be considered 

as the uppermost member of the Claggett formation, notwithstanding 

that in a number of instances typically marine fossils extended for 

some distance above in the basal members of those lighter-colored 

sandstones and shales usually referred to the Judith River beds and 

generally considered as entirely of fresh- or brackish-water origin.

At frequent intervals along the canyon of Dog Creek the beds are 

much disturbed by faults and folds, and at several places not only the 

Claggett formation is exposed, but the underlying Eagle sandstones 

have been thrust up and appear as prominent cliffs. (See PI. II.)

On the east side of Dog Creek 1 mile above its mouth the Eagle 

sandstones are seen near the bottom of the valley dipping westward at 

various angles. They continue to appear at frequent intervals for 2 

miles farther up the creek, and at a distance of 1 mile above the mouth 

of the canyon on the west side of the creek they cap the higher bluffs. 

In this vicinity the Eagle formation is composed of an upper and a 

lower stratum of light-colored, heavy-bedded sandstone, separated by 

a series of lignites and shales, the latter near the bottom bearing 

Baculites and other marine invertebrates. Above the upper and below 

the lower strata of sandstones are arenaceous shales and thin-bedded 

sandstones and lignites. The upper of these bear Cardiwn speciosum 

and Mactra alta in great abundance. On the west side of the creek 

the crest of the divide between Dog Creek and Judith. River is composed entirely of the Claggett and Eagle formations and the underlying Benton shales. The Benton shales are not well exposed in any 

section seen in this vicinity.

At the point where Dog Creek leaves the canyon and opens into the 

valley of the Missouri, a prominent cliff or butte of upper Eagle sandstones is seen on the east side of and not far from the creek. It is very 

fossiliferous, and from it the following invertebrates were secured:

Species found on Dog Creek. 

Cardium speciosum.

Tellina montanaensis.

Baroda? sp.

Callista sp. cf. C. deweyi.

Mactra alta. 

Mactra formosa. 

Lunatia subcrassa.
U. S. GEOLOGICAL SURVEY BULLETIN NO. 257 PL.

CLIFF OF UPPER EAGLE SANDSTONE NEAR MOUTH OF DOG CREEK.
EXPOSURES ON DOG CREEK. 37

A little farther up and on the same side of the creek the following

section was obtained:

Section on Dog Creek.

Feet.

9. Lower Judith Eiver beds with a heavy bed of brown sandstone at base resembling the Tancredia sandstone mentioned above, but apparently destitute 

of fossils. The overlying lighter-colored beds yield many fresh-water 

invertebrates....................................................... 200

8. Black shales weathered in gentle slopes with numerous concretions containing Baculites ovalus, Placenticeras, Inoceramus, and other marine invertebrates. The whole referred to the Claggett formation. The sandstone 

bands of the upper half with Tancredia, etc., are not well exposed in 

this section ........................................................ 300

7. Cross-bedded, sometimes finely laminated, light-colored sandstones and fine 

conglomerates with harder layers and concretions weathering brown-, and 

lenses containing Cardium speciosum, Mactra alta, etc., especially abundant toward the top. An additional 20 feet of soft sandstones and arenaceous shales forms the transition to the Claggett formation............ 100

6. Light, soft sandstone and shale ..........'................................. 90

5. Arenaceous shale with 1 to 3 foot band of very impure lignite in middle...... 10

4. Yellowish sandstones consisting at base of 1 to 3 foot band of hard sandstones with ferruginous masses, overlain by 8 feet of finely laminated 

sands and thin lignite seams, passing above into 30-foot bed of yellow, 

massive, coarse sandstone with thin seams of lignite, overlain by 1 foot 

of lignitic sands, followed by 20 feet of soft buff sandstones........... 60

3. Soft sandstones and shales consisting at base of 10 to 15 feet of soft, usually 

light-colored sandstones, passing upward into more shaly material having 

at top a few feet of light sands. More shaly layer yielded Placenticeras 

whitfieldi ........................................................... 60

2. Sandstone with Thetis? tircularis, Leptosolen, Baroda, Pholadomya, Lunatw,

Placeniiceras, Baculites, etc., regarded as base of Eagle '. ................ 3-5

1. Benton shales with very hard grayish concretions. Lower 40 feet consists of 

rather soft shales, the upper 35 feet of more arenaceous and harder 

shales; no fossils ................................................... 75

For a distance of between 5 and 8 miles from the mouth of Dog 

Creek the beds in the bluffs of the creek continue practically horizontal and undisturbed. The light ash-colored sandstones and shales of 

the Judith River beds are exposed to a thickness of from 300 to 400 

feet and form the greater portion of the can}^on's walls, but the. upper 

members of the Claggett formation are still seen at the bases of the 

cliffs. AVhile in this portion of the canyon the rocks appear undisturbed, not far to the east of the creek two prominent folds may be 

seen extending for several miles in a northwest-southeast direction, 

and along the crest of these the sandstones and shales of the Claggett 

formation appear flanked on either side by the Judith River beds.

A little farther up Dog Creek, in undisturbed areas, the Claggett formation disappears beneath the bed of the stream and the bluffs of the 

canyon are formed entirely of the Judith River beds, which have a 

maximum thickness here of perhaps 500 feet and are composed below 

of alternating layers of light ash-colored sandstones and darker shales
38 THE JUDITH RIVER BEDS. [BULL. 257.

abounding in numerous fresh-water Mollusca. Such invertebrates as 

TJnio, Anodonta, Sphserium, Physa, Planorbis, and G-oniobasis are 

common, while the remains of Trachodon, Ceratops, Monoclonius, 

Deinodon, Paldsoscincus, Ischyrotherium, Trionyx, Emys, Crocodilus, 

Lepidotus, Myledapkus, etc., represent the vertebrate life of the period. 

Toward the top of the series the characteristic light-colored sandstones and shales of the Judith River beds give way to darker-colored 

lignites and shales, which are usually overlain by a stratum of shell 

breccia or marl ranging from a few inches to 3 feet in thickness, and 

composed for the most part of the shells of Ostrea subtrigonalis, indicative of brackish waters and a later return of marine conditions. 

These upper beds are well shown on Dog Creek where it leaves the 

grass-covered plain and enters the canyon, and also on its tributaries. 

In the plains country to the south the highest hills are capped with the 

Ostrea siibtrigonaUs layer of the upper Judith River beds. The upper 

part of the Judith River beds in this region has the same general 

appearance as on Cow Creek, about the foot of the Bearpaw Mountains, 

near Havre on Milk River, and on Sage Cr^eek in Canada. It is well 

shown on an eastern tributary of Dog Creek, where, a few miles from 

its junction with the main stream, a heavj^ bed of lignite 5 to 10 feet 

thick is underlain and overlain by 10 to 15 feet of light, soft sandstone capped by the Ostrea subtrigonalis laj^er, which in some places 

contains shells of Corbicula cytheriformis, Covbula subtrigonalis, G-oniobasis convexa, etc., in considerable abundance. In some exposures 

there is a thinner bed of lignite above or below the main lignite seam, 

with an Ostrea layer immediately capping it. About 3 miles east of 

Dog Creek and on the south side of the tributary mentioned above the 

uppermost Ostrea bed is overlain by about 30 feet of black shales 

with concretions, but no fossils were found in them. These shales 

resemble very closely the Bearpaw shales, and doubtless represent the 

base of that formation.

EXPOSURES ON BIRCH CREEK.

Birch Creek rises in'the Bearpaw Mountains and flows south, emptying into Missouri River nearly opposite the mouth of Dog Creek and 

about 2 miles below the mouth of Judith River. A short distance 

below the point at which it leaves the mountains it enters a canyon, 

which, like Dog Creek Canyon, is deep and rugged and is cut in the 

Judith River and underlying formations. Above this canyon the hills 

on either side of the creek are formed of the Bearpaw shales.

The creek leaves the mountains by two branches, the east and west 

forks, known respectively as Birch Creek and Little Birch Creek. On 

the east side of Little Birch Creek, near the foot of the mountains and 

just below the Fort Benton-Cow Island road, the Judith River beds 

are brought to the surface by a prominent northeast-southwest anti-
U. S. GEOLOGICAL SURVEY

A. BIRCH CREEK CANYON FROM TOP OF BLUFFS NEA;. .'.: _ 

Looking toward Bearpaw Mountains. Shows full thickness of Judith River beds and top of Claggett formation

BROKEN ANTICLINE OF EAGLE SANDSTONE ON NORTH SIDE OF MISSOURI 

RIVER 1 MILE BELOW MOUTH OF BIRCH CREEK.

, Judith River beds form the more distant cliffs on right
] EXPOSURES ON BIRCH CBEEK. 39

cline and protrude from beneath the Bearpaw shales. On either side 

of this anticline the Judith River beds dip gently and soon pass beneath 

the Bearpaw shales.

A few miles west of Little Birch Creek, 1 mile above the bridge on 

the east fork of Eagle Creek, locally known as Dog Creek, a ridge of 

Judith River beds runs in a northeast-southwest direction and dips 

northwesterly, toward the mountains, at a high angle and soon passes 

beneath the Bearpaw shales.

Between the point where Birch Creek enters the canyon and Missouri River the adjacent country is deeply dissected. It is a typical 

badland region and presents all the features already described as prevailing in the badlands of Dog Creek on the opposite side of the 

Missouri (PI. Ill, A). The beds composing the canyon walls have in 

some places been much faulted and folded, often in such a complicated 

manner as to render difficult the determination of the proper sequence 

of the strata.

One mile above its mouth Birch Creek has cut its way through a 

prominent anticline which extends for several miles in a north of west 

by south of east direction, and brings to the surface the Eagle and 

Benton formations. About 1 mile below Birch Creek this anticline is 

faulted and in the bluffs of a small canyon opening into the Missouri 

about 300 feet of Benton shales appear beneath an escarpment of yellowish-brown Eagle sandstones which here forms a most conspicuous 

topographic feature (see PI. Ill, B). At this locality the upper Eagle 

sandstone is in places very fossiliferous, and such forms as Cardium 

specioswn, Thetis (?) circularis> Callista, Leptosolen, Baroda, Pholadomya, and Baculiles are very common. Above the Eagle sandstones 

are about 400 feet or more of shales and sandstones belonging to the 

Claggett formation. The lower 200 feet or more consist of dark shales 

weathering to soft clay on the slope and containing Baculites ovatus, 

Placenticeras whitfieLdi, and Gervillia l)orealis. About 200 feet below 

the top of the formation is a band of brown sandstones and shales 

about 30 feet in thickness, with Avicula nebrasccma (f), Sphadriola 

endotrachys, Tancredia americana, Tellina equilateralis, and Lunatia 

siibcrassa. Above this bed are frequent bands of sandstone intercalated in the shales, and one of these, about 160 feet higher and therefore very near the upper limit of the formation, yielded practically 

the same fauna, as follows: Oardiwn speciosum, Tancredia americana, 

Sphs&riola (?) endotrachys, Mactra formosa, Liopistha (Cymella) 

undata, Lunatia siibcrassa^ and Baculites sp.

The upper portion of the Claggett formation is well exposed on the 

east side of Birch Creek H miles above its mouth, at the first bend in 

the creek, just above the point where a difficult and little-used trail 

descends from the east. At this point about 20 feet of dark, sandy, 

and rather compact shale at the base are overlain by 10 to 15 feet of
40 THE JUDITH RIVER BEDS. [BULL. 257.

yellowish-brown sandstone with sharks' teeth, Tancredia a?nericana, 

and other invertebrates in abundance. Then come 30 feet of arenaceous shales, followed by 5 feet of sandstone overlain by 40 feet of 

shale. Then 3 feet of sandstone is separated by about 40 feet of shale 

from the 5-foot stratum of Tanwedia sandstone which has been taken 

as the upper limit of the Claggett "formation. This exposure is well 

shown in PL IV, B, where the trees mark the limit between the 

Claggett formation and the overlying Judith River beds, which here 

have a thickness of 510 feet from the Tancredia sandstone at the base 

to the Ostrea subtrigonalis layer at the top. The overlying Bearpaw 

shales are not represented in this immediate region, having been 

entirely removed by erosion. It was from the sandstones near the 

base of the Judith River beds near the mouth of Birch Creek that 

Professor Cope in 1876 secured the type of Monodonius crassus. 

From this point for a distance of 2 or 3 miles up Birch Creek the 

Judith River beds are quite undisturbed and present a continuous sec 

tion from their base to the Ostrea siibtrigonalis zone.

EXPOSURES ON MISSOURI RIVER BETWEEN BIRCH AND COW CREEKS.

On either side of Missouri River between Birch and Cow creeks the 

country is deeply dissected and presents the appearance of a wild badland region (see PI. IV, A). As on the lower courses of Dog and 

Birch creeks, the rocks belong to the Judith River beds and the underlying Claggett formation, save at intervals where disturbances in the 

strata have brought to the surface the Eagle sandstones and underlying Benton shales. Everywhere in the vicinity of the river in this 

region the overlying Bearpaw shales have been removed by erosion. 

In places, however, not far from the river, especially on the south 

side near Cow Island, these shales overlie the Judith River beds, while 

they occur almost continuously along the old Benton and Cow Island 

trail along the southern foot of the Bearpaw Mountains between Birch 

and Cow creeks. From Bearpaw Springs, at the southeastern base of 

these mountains, this trail continues westward over the Bearpaw shales 

with only occasional exposures of the undertying Judith River beds at 

intervals in the blufi's of the coulees. At Black Coulee, about 6 or 8 

miles west of Bearpaw Springs, the Judith River beds outcrop from 

beneath the Bearpaw shales only a half mile below the point where 

the road crosses the bed of the coulee, and 1£ miles farther down 

the coulee is a larger similar exposure. At the upper of these two 

exposures a section on the east side of the creek shows at the top a 

1-foot bed of shell breccia with Ostrea subtrigonalis, OorMcula, Corbula, 

and Anomia, underlain by 20 feet of light sandy clays followed by 10 

feet of lignite underlain by an ash-colored sandstone with thin seams of 

lignite to bed of creek. These beds have av northerly dip of about 15°
U. S. GEOLOGICAL SURVEY IULLETIN NO. 257 PL. IV

A MISSOURI RIVER BELOW MOUTH OF BIRCH CREEK. 

Looking downstream.

B. CLAGGETT FORMATION AND OVERLYING JUDITH RIVER BEDS ON BIRCH CREEK. 

The contact is marked by the small pine trees.
8THATCHi4ND ] EXPOSURES ON COW CREEK. 41

and are overlain by the Bearpaw shales with nodules containing Baculites ovatus, Placenticeras whitfieldi^ and Inoceramus. At the next 

lower bend in the creek the beds are still inclined to the north, but in 

the succeeding exposure the crest of a low anticline appears, and below 

this the beds dip to the south and soon pass beneath the Bearpaw shales, 

which occupy a basin between this and the more important exposure 

of Judith River beds already spoken of as occurring farther down the 

creek. The upper exposures of these Judith River beds contain 

Ostrea subtrigonalis, Anomia gryphorhynchus, and Corfiicula cytheriformis, and a bed a few feet lower yielded Sphceriumplanum, Campeloma vetula, Goniobasis invenusta, and other fresh-water forms.

Just to the left of the point where the Benton and Cow Island trail 

begins its descent into the valley of Sand Creek in going west toward 

Benton the upper Judith River beds dip northward at an angle of 30° 

and pass beneath the Bearpaw shales. A stratum of brown sandstone 

a few feet thick and about 100 feet below the top of the Judith River 

beds yielded Sphaeriwn planum, Splia&rium recticordinole, Goniobasis 

sublwms, and Campeloma vetula(f}. Farther down the creek better 

exposures of the Judith River beds are to be seen, and at several places 

along the Benton trail near the forks of Sand Creek the Judith River 

beds are overlain by the Bearpaw shales, while 2 or 3 miles still 

farther downstream extensive exposures of the Judith River beds are 

capped by the Bearpaw shales.

EXPOSURES ON COW CREEK.

Cow Creek flows in a deep, rugged canyon from a place a short distance below the point where it leaves the Bearpaw Mountains to its 

confluence with the Missouri. On the east side of Cow Creek and at its 

mouth there is a prominent exposure of Eagle sandstone (see PI. V). 

At this point these sandstones have been uplifted and form a conspicuous ledge extending for several miles in a nearly north-south 

direction and dipping to the west at an angle of about 45°. These 

sandstones at this locality yielded the type of Ornithomitnus grandis 

Marsh. Another nearly parallel and very similar exposure of the 

Eagle sandstones crosses 2 miles above the mouth of Bull Creek, a 

small tributary of the Missouri just below Cow Creek.

The bluffs on both sides of Cow Creek for several miles above its 

mouth are made up largely of rocks belonging to the Claggett formation overlain by the lighter-colored materials of the Judith River 

beds. The rocks here do not differ materially from those already 

described as belonging to the same formations on Dog and Birch 

creeks farther up Missouri River. At frequent intervals the beds are 

much faulted and disturbed and the underlying Eagle sandstones and 

Benton shales are exposed.

Abouc 6 or 7 miles above its mouth Cow Creek is crossed by a dike
42 THE JUDITH RIVER BEDS. [BULL.257.

of igneous material, in places attaining a thickness of 10 feet. On the 

east side of Cow Creek about a mile below this dike is a section in 

which are exposed about 200 feet of Judith River beds overlain by 

the Bearpaw shales, and which is different from all other sections 

examined, as it contains a strictly marine horizon well within the 

limits of the Judith River beds. The section is as follows:

Section on east side of Cow Creek.

Feet.

12. Dark shales of the Bearpaw formation ................................... 200

11. Similar ash-colored sands or arenaceous clays............................. 25

10. Ash-colored sands with many Ostrea subtrigonalis ......................... 1

9. Lignite ................................................................ 4

8. Soft ash-colored sandstone................................................ 40

7. Lignite ................................................................. 1-4

6. Very soft buff sandstone ................................................ 10

5. Ash-colored arenaceous clays with bands and nodules of brown sandstone

and occasional nodules of clay-ironstone in lower portion................ 40

4. Yellowish, more or less lenticular sandstone with teeth of sharks and other

fishes and bones of marine and fresh-water turtles...................... 2-5

3. Soft, friable, ash-colored argillaceous sandstone, the upper 2 or 3 feet containing numerous vertebrate remains, including sharks' teeth, mosasaur 

bones, vertebrae of Palseoscincus, Ischyrotherium, and a horn core of Ceratops montanus (1)..................................................... 30

2. Yellowish sandstone weathering into large nodular masses................. 10

1. Soft, friable, light-gray or ash-colored sandstones not well exposed. A band 

about 20 feet from the top yielded Leda, Nucula, Tellina, Liopistha (Cymella) undata, Mactrawarrenana (?), Lunatia, and Placenticeras (?). These 

are mostly not specifically determinable, but they indicate a strictly marine 

fauna................................. .............................. 30

The upper lignite and the Ostrea bed (Nos. 9 and 10) may unquestionabl}7 be assigned to the horizon that has been recognized throughout this region as belonging near the top of the Judith River formation, and all of the beds below No. 12 must be assigned to that 

formation on account of their stratigraphic position and general lithologic character. The land and fresh-water vertebrates found 100 

feet below the Ostrea bed belong to the Judith River fauna, while the 

marine rnosasaurs found with them and the marine invertebrates 

occurring 60 feet lower show plainly that locally the conditions under 

which the formation was deposited were different from those that 

generally prevailed. As these marine beds appear to pass horizontally 

into fresh-water deposits within a short distance, it is probable that 

they were laid down in a narrow bay or inlet which was not very farwest of the ocean.

Farther up Cow Creek the Judith River beds form an increasing 

proportion of the walls of the canyon, and about 13 miles above its 

mouth the bluffs are composed of them exclusively, save at intervals 

where disturbances have brought the underlying marine deposits to 

the surface.
U. S. GEOLOGICAL SURVEV 

FAULT COts LV iNv, LiNbU EAGLE bANU:, I ONE WITH HORIZONTAL JUDIT
] EXPOSURES ON COW CREEK. 43

About 10 miles above the mouth of Cow Creek, at the point where 

the old Fort Benton and Cow Island freight road leaves the creek and 

turns westward toward the Bearpaw Mountains, there is a conspicuous 

fault in the Judith River beds, which is .shown on PI. VI, B. North 

of the fault for some distance up the creek and almost uninterruptedly 

westward to the base of the Bearpaw Mountains the Bearpaw shales 

conformably overlie the Judith River beds. This is the locality mentioned by Hatcher a , where, in 1888, he observed about 400 feet -of 

what appeared to be Pierre shales overlying the Judith River beds.

Immediately south of the fault mentioned above, a prominent ridge 

composed of sediments belonging to the Judith River beds projects 

into the valley of the creek. The type of Ceratops montanus was 

obtained near the summit of this ridge, and the beds yielded also the 

remains of Trackodon mirabilis; turtles, crocodiles, and fishes of 

Judith River types and a considerable number of fresh-water invertebrates, including Unio danae, Unw primxvus, Splise,riwn planwn, 

Sphs&rium recticardinale, Ooniobasis invenusta, G-oniobasis judithensis, 

Physa copei, Hyalina occidentalis, and Valvata montanaensis.

Near our camp, at the point where a new trail enters the valley from 

the west, 2 or 3 miles above the point where the old Fort Benton 

and Cow Island trail leaves the valley, is an area that is extremely 

interesting and will therefore be described with some detail. On the 

summit of the bluff west of Cow Creek, just to the left of the Benton 

trail, a short distance above its junction with the new trail, is an 

important fault running N. 15° E. and bringing the Judith River 

beds up on a level with the Bearpaw shales. This fault strikes across 

the head of one of the tributaries of Cow Creek, and a mile or two 

below in the valley on either side of this tributary undisturbed Judith 

Riverbeds underlie the Bearpaw shales in a nearly horizontal position. 

An aneroid measurement gave a thickness of 535 feet for the Bearpaw 

shales, assuming them to be horizontal. Just above our camp, on Cow 

Creek, a sharp anticline crosses the creek in a northwest-southeast 

direction. Save for this local disturbance the Judith River beds in 

the immediate vicinity of camp on both sides of the valley of Cow 

Creek are undisturbed and lie beneath the Bearpaw shales. The 

base of these shales is here composed of about 25 feet of light-colored 

shales and sands^ 10 feet of rather dark shale at base, and 15 feet of 

ash-colored arenaceous shales above, with numerous large clay stone 

concretions weathering yellow. The sands contain Liopistha 

(Cymella) undata, Mactra ivarrenana, Lunatia subcrassa, and Placenticeras whitfieldi. Above these come 535 feet of typical Pierre (Bearpaw) shales with their characteristic fossils. Below these marine 

beds, at the base of the hill directly-in front of our camp, are exposed

aScience, n. s., vol. 1(i, 3902, pp. 831-832.
44 THE JUDITH RIVER BEDS. [BULL.257.

75 feet of the upper Judith River beds, consisting of 25 feet of ashcoJored sandstones with numerous very large, irregularly conical brown 

sandstone concretions, underlain by 10 feet of lignite, very impure at 

base, which in turn is underlain by 40 feet of light-colored sandstones. 

These beds contain remains of turtles and dinosaurs. At the point of 

junction between the Judith River beds and the overlying Bearpaw 

shales there is a 1-foot stratum of shell breccia composed of Ostrea 

subtrigonalis with Goniobasis convexa var. impressa, Panopaea simulatrix, Corlula siibtrigonalis, Anomia, gryphorhynchus, Corbicula cytheriformis, and Corbicula occidentals (1). The same horizon at another 

locality in the neighborhood yielded Viviparus conradi associated with 

Corbicula, Ostrea, and Anomia.

One mile below camp on the east side of the.creek there is an 

important uplift, bringing up the entire Judith River series and several 

hundred feet of the lower marine beds. The section to which the 

Bearpaw shales are added from exposures west of camp is as follows:

Section on east side of Cow Creek.

Feet. Feet.

5. Bearpaw shales, including the marine light-colored sands and 

shales at base, but not allowing for westerly dip, which, if 

continuous, as shown in front of exposure on west side of 

Cow Creek, would give a thickness of nearly, or quite, 700 

feet ................................................... 560

4. Judith Elver beds, the middle portion covered in bed of creek. 

One hundred and fifty feet of lower Judith Eiver beds are 

continuously exposed in the upper section, and one-half 

rnile east, where the Judith River beds are horizontal, a 

thickness of 490 feet was measured, but the base is not exposed at this point. A shale bed about 30 feet above the 

base of the formation yielded many leaves of Trapa? microphylla, together with abundant fresh-water Mollusca, including Sphserium planum, Spliserium recticardinale, Physa 

copei(f), and Goniobam suUortuosa. Another horizon about 

300 feet from the top, in the exposure one-half mile east of 

the section, yielded Sphssrium planum, Anodonta propatoris, 

Unio danse (?), Unio primnevus, Valvata montanaensis, Hyalina? 

evansi, Hyalina? occidentals, Planorbis amplexus, Physa cope\ 

Goniobasis suUortuosa, and Goniobasis gracilenta. ........... 490

3. Claggett formation:

c. Light-colored shales or sandy clays with band of brown sandstone containing Tancredia americana in middle. Top of 

marine ................................................ 50

b. Yellowish-brown sandstones, generally soft, but with harder 

layers and lenses, with Tancredia americana, Cardium speciosum, Tellina equilateralis, Liopistha (Cymella) undata, Lunatia 

subcrassa, Baculites sp., and fragment of vertebrate jaw.... 20

a. Dark shales with concretions bearing Baculites ovatus, B. compressus, Nucula cancellata, Leda.( Yoldia) evansi, and Gervillia 

borealis. These shales weather much as the Bearpaw, but 

with a reddish tinge. The concretions are different and
U. S. GEOLOGICAL SURVEY

A. UNDIbTUKnc.j jui.'iih RIVER BEDS WITH OVERLYING BEARPAy

COW CREEK.

The contact is below the pine trees on ridge in middle distance.

IS. FAULT CONTACT OF JUDITH RIVER BEi:b //: 1 H BEARPAW SHALES ON COW 

CREEK 10 MILES ABOVE MOUTH,
U. 8. GEOLOGICAL SURVEY BULLETIN NO. 257 PL. VII

A. INDURATED OR CONCRETIONARY MASS IN UPPER PART OF JUDITH RIVER BEDS 

ON COW CREEK 13 MILES ABOVE MOUTH.

H. UPPER PART OF JUDITH RIVER BEDS WITH HEAVY BED OF LIGNITE ON COW

CREEK.

 .. Opposite to view on PI. VI, A.
EXPOSURES ON COW CREEK. 45

3. Claggett formation Continued. Feet. Feet, 

with fewer fossils and not so great a variety. These beds 

become lighter toward the top, the upper 50 feet containing two seams of thin brown sandstone, each 2 to 3 feet

.....i.......................................... 30(MOO

Total thickness of Claggett formation.................. 370-470

2. Eagle formation. No fossils:

e. Cross-bedded and finely laminated sands with thin seams of

lignites, in places becoming more massive................ 125

d. Very light-colored, fine, heavy-bedded sandstone.......... 40

c. Heavy-bedded buff sandstones, soft at base, but harder 

above, and with indurated lenses and numerous large concretions, weathering brown at top. The thickness of b and 

c is very variable....................................... 50

b. Heavy-bedded buff sandstones with lenses of lignite and

shales sometimes exhibiting cross-bedding ............... 30

a. Kegularly-bedded buff sandstones with several thin seams

of dark shales. ......................................... 20

Total thickness of Eagle formation..................... 265

1. Dark Benton shales with Baculites and other invertebrates in 

concretions, and containing several layers of sandstones in 

upper 100 feet. The following fossils were found in these 

shales near the base: Inoceramus sp., fragments of a thickshelled form; Prionotropisfsp., fragment; Scaphites ventricosus; Baculites sp., a slender, strongly nodose form. Several 

genera of invertebrates not specifically determinable were 

collected in the upper portion....................... .... 300

Above our camp for several miles the bluffs of Cow Creek show 

important exposures of the Judith River beds, everywhere overlain by 

the Bearpaw shales. These shales are everywhere more or less fossiliferous and near Hedge Brothers ranch, on upper Cow Creek, the following species were obtained:

Gervillia borealis. 

Inoceramus barabini 

Leda (Yoldia) evansi. 

Lucina subundata. 

Thetis? circularis. 

Lunatia.

Anchura americana. 

Cinulia.

Fossils obtained on upper Cow Creek.

Anisomyon centrale. 

Anisomyon alveolus. 

Baculites ovatns. 

Baculites compressus. 

Scaphites subglobosus. 

Scaphites nodosus. 

Placenticeras whitfieldi.

Pis. VI and VII show well the chief lithologic and stratigraphic 

^features displayed by the various horizons in this region.

AREA NEAR HAVRE, MONT.

The most extensive exposures of the Judith River beds in this area 

are on the north side of Milk River from 1 to 4 miles above the town 

of Havre, a small station on the Great Northern Railway just north of
46 THE JUDITH RIVER BEDS. [BULL. 257.

the Bearpaw Mountains. This is perhaps the most accessible of all 

the exposures of these beds. Here is a rather large and picturesque 

badland region composed entirely of the Judith River beds. On the 

north side of Milk River about one-half mile above Havre the road 

crosses a deep gulch by a small bridge. At the point where this 

gulch emerges from the bluffs into the river valley, about 80 yards 

above the bridge, there is on its right side a cut bank, some 20 feet in 

height, showing two seams of impure lignite. The lower and thicker 

of these is about 6 feet above' the bed of the gulch; the upper is 

thinner and less pure and is about 10 feet higher than the lower. 

These two lignites are overlain by the Bearpaw shales, though these 

shales are probably not in position and are somewhat more arenaceous 

than usual. In them were found in place two limestone concretions, 

one of which contained shells of Ostrea patina and the other Inoceramus sagensis. Immediately beneath, in the wash at the bottom of the 

gulch, but evidently derived from the shales, was found a similar 

limestone concretion containing Placenticeras whitfieldi.

Up the river these lignite seams outcrop at frequent intervals in 

the bluffs. They rapidly assume a more elevated position and show 

at this point a decided easterly dip, amounting to perhaps 4° or 5°.

About 100 yards west of the exposure just described a prospecting 

tunnel has been driven into the lower and more important lignite 

seam, and between it and the overlying seam is a light horizontally 

cleaving sandstone.

Three hundred or 400 yards farther west these lignites are no longer 

visible, having perhaps passed above the present upper limits of the 

bluffs and been carried away by erosion,

A half mile farther up the river the bluffs on the north side present 

a picturesque badland area, consisting at the base of 150 to 200 feet 

of usually light-colored sandstones and cla,ys, with brown sandstone 

concretions and occasionally thin seams of lignite. (See PI. VIII, A.) 

In these beds at several horizons were found in considerable abundance dinosaur bones, crocodiles, garpike scales, turtles, and other 

vertebrates with fresh-water Mollusca, including Unio danse, Unio 

supenawensis, Anodonta propatoris, Sphserium planum, Physa copei, 

Goniobasis subtortuosa, Goniobasis- invenusta, Goniobasis juditliensis, 

etc. The assemblage of fossils as well as the lithologic features of 

these beds are those of the Judith River beds.

Above these light-colored, fresh:water deposits are two lignite seams 

which are very similar to those occurring at the locality where the 

marine fossils were found and bear the same relation to each other. 

This badland exposure continues for 3 or 4 miles farther up Milk 

River and the beds in every way resemble the Judith River beds at 

the type locality.

On the south side of Milk River for 3 miles west of Havre, or to a
U. S. GEOLOGICAL SURVEY ULLETIN NO. 257 PL. VIII

A, BADLANDS EXPOSURES OF JUDITH RIVER BEDS ON NORTH siut uF MILK 

RIVER NEAR HAVRE, MONT.

21. UPPER PART OF JUDITH RIVER BEDS AND OVERLYING BEARPAW SHALES ON 

SOUTH SIDE OF MILK RIVER 3 MILES WEST OF HAVRE, MONT.
.....-......")] EXPOSURES ON COW CREEK. 47

point about 1 mile above the mouth of Beaver Creek, are frequent 

exposures of the Judith River beds, overlain by the Bearpaw shales. 

The strata in these exposures have suffered much disturbance and are 

inclined at varying angles, in two or three places being nearly vertical. The exposures are not sufficient to reveal the structure completely, but in general the beds seem to have been folded sharply 

and faulted to some extent. Wherever the top of the Judith River 

formation is exposed it is overlain by the Bearpaw shales, with their 

characteristic fossils. This is especially noticeable in the bluff just 

below the mouth of Beaver Creek. Here the beds are inclined at a 

very high angle, perhaps 60°, with a southwesterly dip. At the bottom they are composed of about 200 feet of light-colored sandstones 

and arenaceous shales resembling the upper Belly River beds, as 

described by Dawson. These light sandy materials are succeeded by 

a series of light-colored clays and shales with 8 or 10 seams of lignite, 

which become thicker and purer toward the top and are overlain by a 

bed of Ostrea subtrigonalis, about 2 feet in thickness. This upper 

series of light-colored shales, lignites, and oysters has a thickness of 

about 60 or 75 feet and appears to represent the extreme top of the 

Judith River formation. It is overlain by dark marine Bearpaw 

shales, best seen at the foot of the exposure facing Beaver Creek and 

on the south side of the railroad track, and containing Inoceramus, 

Avicula linguiformis, Modiola meekii, and Baculites compressus.

Below the mouth of Beaver Creek a high ridge that faces Milk 

River continues a mile or more toward Havre. The upper part of the 

exposure is composed of the light-colored sands and shales of the 

Judith River beds. For perhaps half a mile there is exposed a lower 

thick stratum of heavy-bedded brown sandstone, which outcrops just 

above the railroad tracks and contains numerous spherical and irregular concretionary masses. This brown sandstone has an observed 

maximum thickness of about 30 feet. No fossils were found in it, but 

near its eastern extremity it is immediately overlain by some brown 

cherts with the shells of Corbula subtrigonalis in great abundance. 

This sandstone may be the top of the Claggett formation.

Above Beaver Creek, in the narrow ridge between this creek and 

Milk River, the sequence and relative positions of the fresh-water 

Judith River formation and overling Bearpaw shales are well shown. 

(See PI. VIII, J3.} In the valley of Milk River a short distance above 

the mouth of the creek there is a small uplift with the axis running 

in a northwest-southeast direction. Above this for a distance of 300 or 

400 yards, in the bluffs facing Milk River, there is a shallow syncline, 

the trough of which at its deepest portion is filled with Bearpaw shales 

containing Ostrea patina, Liopistha (Cymella] undata, Baculites compressus, and Placentic&ras whitfieldi. In the uplift just mentioned and 

in the eastern and central portion of the syncline only the upper por-
48 THE JUDITH RIVER BEDS. [BULL. 257.

tion of the Judith River beds as seen below the mouth of the creek 

is shown. The lignites and overlying' oyster bed, which here contains Ostrea subtrigonalis, Corbicula cytheriformis, Anomia gryphorhynchus, and Goniobasis convexa, >are especially prominent. On the 

western limb of the sjmcline the lower and more arenaceous members 

appear. Here the entire series is inclined at a higher angle and is 

clearly seen to pass beneath the Bearpaw shales.

Owing to the disturbances in the beds about Havre, it is not easy to 

determine in a perfectly satisfactory manner the sequence of the different horizons. This is especially true of the above-described exposures in the bluffs above the town, where, unless one is familiar with 

the character of the different formations and has determined their true 

sequence in less disturbed regions, the confusion is indeed perplexing. 

The most satisfactory locality for studying the Judith River beds in the 

vicinity of Havre is on the south side of Milk River about 6 miles 

below Havre, on Boxelder Creek, about 2 miles south of Toledo, a 

small station of the Great Northern Railway. Here the tops of the 

high hills are capped with 25 to 50 feet of Bearpaw shales conformably 

overlying the Judith River beds. Considerable disturbance is noticeable in the bluffs of the creek at this point, but in the hills 1 mile to 

the north the sequence of the strata is quite evident.

At the Black Diamond Coal Company's mines, 9 to 11 miles southeast of Havre, in a draw on the west side of Boxelder Creek, there is, 

in the uppermost Judith River beds, a coal vein 6 to Y feet thick. It 

has a gentle southerly dip and is overlain by 20 feet of Judith River 

deposits and 160 feet of Bearpaw shales, from which were collected 

Inoceramus sagensis, l^lacenticeras whiifieldi, Placenticeras intercalare, 

and Baculites ovatus. From this point a range of hills, composed at 

the base of Judith River beds and capped with the Bearpaw shales, 

extends in a northwesterly direction to near the mouth of Boxelder 

Creek. The Bearpaw shales here, as elsewhere, in weathered exposures 

show loose black shales with limestone concretions. Some of the concretions are 12 to 15 feet in diameter and very symmetrical.

EXPOSURES ON MILK EIVEH FROM HAVRE TO THE INTERNATIONAL

BOUNDARY.

Above Havre the Judith River beds are exposed almost continuously in the bluffs on either side of Milk River to and beyond the 

international boundary. There are also occasional exposures of 

the underlying Claggett formation and less frequently of the overlying Bearpaw shales. Although the region is a plains country, the 

strata have been much disturbed and are faulted and folded in a 

remarkable manner. In many narrow belts the disturbances are as 

great as those, usually encountered in an intensely mountainous country, though in the larger areas between the disturbed zones the beds
U. S. GEOLOGICAL SURVEY ULLETIN NO. 257 PL. IX

A. UPTURNED JUDITH RIVER BEDS AND BASE OF BEARPAW SHALES ON MEILI 

COULEE NEAR HAVRE, MONT.

B. CLAGGETT SHALES AND BASE .,," .,,....:,- .;, , ^ii :,£. :, ON MILK RIVER ONE- 

. v HALF MILE BELOW PENDANT D'OREILLE, ASSINIBOIA,
OTHATCHERND ] EXPOSURES ON MILK RIVER. 49

are practically horizontal. Since the uplifts occurred the country has 

been planed off by erosion and covered with thin Pleistocene deposits, 

so that it is only along the modern drainage courses that there is any 

evidence of such disturbances, and it is not always easy to determine 

definitely the exact relations of the various strata.

About 5 miles above Havre a small tributary known as Meili Coulee 

enters the Milk River Valley from the north, about half a mile above a 

conspicuous red butte, the color of which is due to burned-out lignite 

seams. At the mouth of Meili Coulee are prominent exposures of the 

Judith River beds dipping northward at a high angle and overlain by 

the Bearpaw shales. (See PL IX, A.) For half a mile before entering the valley of Milk River the bluffs on the east side of this coulee 

show the folloAving section:

Section on east side of Meili Coulee.

Feet.

4. Bearpaw shales with Baadiles ovalus and Placenticeras wltiljieldi, etc.......... 50

3. Shales underlain and overlain by shell breccia composed largely of Ostrea vubtrigonatis, forming the top of the Judith River beds..................... 20

2. Lignites, shales, and sandstones........................................... 40

1. Light-colored sandstones and shales of the Judith River beds with their characteristic fossils ...................................................... 250

The beds up to this point are inclined at a high angle and dip to the 

north, and the sequence and relations of the strata are quite evident, 

but above this point the beds have a different character and are much 

more nearly horizontal, although they are still gently inclined to the 

north. At this point in the section the beds have been faulted and the 

sandstones and shales of the Claggett formation abut against the Bearpaw shales, having been elevated far above their normal position 

relative to these shales.

Farther up the draw from this point the following section is seen in 

the bluffs on the east side:

Section on east side of Meili Coulee.

Feet. Feet.

2. Judith River beds .....................................................

f. Light-colored sandstones and shale with lignite and stratum of

shell breccia at the top......................... .... ........ TOO

e. Sandstones, shales, and thin seams of lignite .................. 130

d. Shell breccia ........................................^...... 3

c. Shales and lignite ........................................... 20

b. Ostrea subtrigonalis bed........................ J.............. 2

a. Lignite and shales ...;....................................... 20

 275 

1. Sandstones and shales of the CLaggett formation with marine invertebrates. 160

A little way above its mouth Meili Coulee is crossed by the fault 

mentioned above. This fault bears N. 60° W. by S. 30° E., and above 

it the sandstones and shales of the Claggett formation dip gently to the 

north until, at a distance of perhaps half a mile farther up the coulee, 

they pass beneath the Judith River beds, In a yellow sandstone layer 

Bull. 257 05 4
50 THE JUDITH EIVEE BEDS. [BULL. 257.

near the top of the Claggett formation were collected Tancredia ainericana, Mactra formosa, and a few other invertebrates.

Just north of the red butte situated below the mouth of Meili Coulee 

is a rather extensive exposure of Judith River beds with numerous 

sandstone Jenses and concretions exhibiting cross-bedding and other 

evidences of strong currents. From these we secured remains of 

Trachodon mirabilis, Palseoscincus costatus, and the mammal jaw shown 

in fig. 1 (p. 100).

In various small draws or coulees between Meili Coulee and Supenaw Coulee, 6 miles farther up the river, conditions similar to those 

prevailing in Meili Coulee were observed. The fault that crosses 

Meili Coulee near its mouth is continuous and crosses each of these 

coulees with about the same trend of N. 60° W. by S. 30C E. This fault 

crosses Supenaw Coulee about a mile above its 'mouth and just above 

Thackeray Brothers' reservoir. Above the fault the sandstones and 

shales'of the Claggett formation dip gentty to the north and soon pass 

beneath the Judith River beds, which here attain their normal development, and at a distance of about 3 miles, or near the head of the west 

fork of the Coulee, the lignite series at the top of these beds appears 

in much the same manner as in the other regions described. In Supenaw Coulee the lignite beds are partly burned out and the adjoining 

clays and sandstones are baked red. They were still burning when 

visited. Interstratified with these lignites are beds of fresh-water 

Mollusca, Campeloma vetula, and Unios, associated with Oorbulaperundata, and three strata of Ostrea subtrigonalis.

At the head of Browns Coulee, about 12 miles farther up the river, 

the Judith River beds are well developed, and on this coulee, about 2 

miles above its mouth, is an area of much disturbance, in which a brown 

sandstone of the lower Judith River beds appears in a steep anticline. 

There are here two sandstones separated by 30 feet of shales. In the 

upper of these we obtained shells of Hyalina occidentals and H. evansi, 

dinosaur bones, and fragments of a very large turtle. About 100 

yards below this anticline there is a second and larger fold affecting 

the Claggett formation, which on the north side passes beneath the 

Judith River beds. The northern limb of this anticline dips at an 

angle of 45°, while the southern is nearly or quite perpendicular, the 

sandstones and shales having the appearance of a vertical dike with its 

southern border resting against the lower brown sandstones of the 

Judith River beds, which are here only moderately inclined. There 

is thus unmistakable evidence of a fault as well as a fold at this point.

From Browns Coulee the bluffs of Milk River exhibit frequent evidences of disturbances as far as Simpson's ranch, about 9 miles nearly 

due south of Wild Horse Lake, which is on the international boundary. 

About 1£ miles below Simpson's ranch the Judith River beds are well 

exposed, and we secured remains of Cemtops, Aublysodon, and Acipen-
STANTON 

HATCHER,,4ND ] EXPOSURES ON MILK RtVEE. 51

ser, with Unio sp., Sphs&rium planwn, Goniobasis invenusta, Goniobasis judithensis, Pkysa copei, and Viviparus.

Above Simpson's ranch, to and beyond the international boundary, 

disturbances in the beds are less frequent, and the bluffs of the river, 

which have an average height of about 200 feet, are composed almost 

entirely of the light-colored sandstones and shales of the Judith River 

beds.

At Black Butte, a low prominence on the north side of Milk River 

about 7 miles west of south of Wild Horse Lake, the river valley has 

a width of scarcely more than a mile and a depth of perhaps 250 feet. 

The butte stands on the crest of the bluff and, on account of the levelness of the surrounding country, is visible from a considerable distance 

and forms a rather conspicuous landmark, notwithstanding its low altitude. At the top of this butte are 75 feet of glacial material, beneath 

which there are about 175 feet of the Judith River beds. At about 

the middle of the exposure are several feet of shell-marl and in this 

we secured numerous teeth of Trac/wdon, L&laps, and other dinosaurs, 

lizards, fishes, etc., together with Unio prisons (?), Unio primdevus, 

Sphs&rium planum, S. recticardinale, Goniobasis suUaevis, and G. subtortuosa.

There are also local developments of cross-bedded brown sandstones 

with numerous concretions, and these afforded'a few vertebrae, teeth, 

and other remains of Trachodon, Ceratops, and Lsdaps.

No lignites were seen here. The upper lignites, so characteristic of 

the Judith River beds, are wanting in this section and have doubtless 

been eroded away. They were last seen on the summit of the highest 

hills about the head of Cottonwood Coulee, 18 miles from Wild Horse 

Lake, on the road from Havre.

EXPOSURES ON MILK RIVER NORTH OF THE INTERNATIONAL BOUNDARY.

For some distance beyond the international boundary Milk River 

flows through a narrow and picturesque valley, about 200 feet in depth, 

carved out of the Judith River beds. A few miles below Pendant 

d'Oreille, a northwest mounted police station on Milk River about a 

mile below the mouth of Pakowki Coulee, the uppermost members of 

the "lower dark shales," as described and mapped by the late Dr. 

George M. Dawson, appear above the level of the river and occupy 

successively more elevated positions in the bluffs until, at a distance of 

about 1 mile above the police station, these shales and sandstones, constituting the Claggett formation, form almost the entire bluffs of the 

river, the overlying Judith River beds having here been almost entirely 

removed by erosion. In a bluff on the north side, and at the first bend 

of the river below Pendant d'Oreille, about 160 feet of beds are exposed 

(PI. IX, J5). The lower 100 feet of this exposure are composed of
52 THE JUDITH EIVEE BEDS. [BULL. 257.

-V

the Claggett formation, the "lower dark shales" of Dawson, while the 

upper 60 feet belong to the Judith River beds, "Belly River series" 

of Dawson. The section is as follows:

Section on Milk River near Pendant d' Oreille.

. Feet.

8. Light sandstones and soil ................................................ 10

7. Light sandstones with Unib at top......................................... 5

6. Light sandstones with shells of Corbula at top.............................. 19

5. Ostrea sublrigonalis breccia............................................I.... 4

4. Light-yellow sandy material...........................................:.. 10

3. Impure lignite and shell breccia with Corbula subtrigonalis, C. perundata, Corbicula cytheriformis, Unio prisons (?), and Neritina ....................'. 4

2. Light-colored arenaceous shales .......................................... 20

1. Dark shales belonging to the Claggett formation with limestone concretions 

and bands of sandstone containing Nucula, Leda, and Liopistha (Cymella) 

undata. ............................................................ 100

Nos. 2 to 8 belong to the base of the Judith River beds.

The bluffs of Milk River at the mouth of Pakowki Coulee, immediately above the police camp, are formed almost entirely of marine 

deposits, consisting, at the base, of dark shales with bands and nodules 

of limestone and at the top of light-yellow soft sands and arenaceous 

shales with harder layers of blue sandstones, weathering brown. The 

latter yielded Baculites asper (?), Lunatia subcrassa, Tancredia, americana, Cardium- speciosum, Tellina(l) sp., and Mactra. On the highest 

points these beds are capped b}^ about 3 feet of impure lignite overlain by light sandy shales with a few Unios and turtle fragments. In 

the marine sandstones underlying these lignites, along with the invertebrates just mentioned, were found several species of sharks' teeth.

Two and a half miles below the police station, in the bluff on the 

north side of the river, is a bed of well-preserved shells, about 2 feet 

thick, immediately overlying the 4-foot lignite seam seen in the bluff 

just below the police station. In this shell bed we collected Unio subspatulatus, Unio supragibbosiis (?), Modiola, CorMcula occidentalis, 

Corbicula cytheriformis (?), Corbula subtrigonalis, Corbula perundata, 

Rliytopliorus gldber, and Gonwbasis-invenusta, all in a good state of 

preservation. This shell bed is overlain b}^ about 10 feet of arenaceous shale, which is light at the base and dark above, and is followed 

by a 3-foot vein of lignite.

In a canyon tributary to Milk River about 8 miles below Pendant 

d'Oreille the following section is shown:

Section in canyon tributary to Milk River 8 miles below Pendant d' Oreille.

2. Judith River beds: Feet. Feet, 

d. Light-colored sandstones and shales with a variable upper member of yellow, cross-bedded, concretionary sandstone which 

shows a maximum thickness of 100 feet in the upper course of 

the canyon ................................................ 300
STHATCHERND] EXP09UBES ON SAGE CREEK, ASSINIBOIA. 53

2. Judith Eiver beds Continued. Feet. Feet, 

c. Sandstones, lignites, and shales with several layers of Ostrea 

subtrigonalis and some fresh-water shells. The principal lignite 

bed, 6 to 8 feet in thickness, is at the base.................... 50

b. Light-colored sandstones, becoming yellow toward the top...... 50

a. Buff arenaceous shales with remains of turtles and fragments of

dinosaur bones............................................. 25

 425

1. Marine beds belonging to the Claggett formation, consisting of dark 

shales with bands and lenticular layers of brown sandstone, 

containing Tancredia americana, Tellina (?) sp., and Vanikoropsis tuomeyana, with an admixture of such brackish-water forms 

as Ostrea glabra, Corbula subtrigonalis, and Melania ? whiteavesi, 

about...................................................... 100

From Pendant d'Oreille to Hooper's ranch, on Many Berries Creek, 

about 5 miles northwest of Pakowki (Badwater) Lake, the Judith 

River beds are exposed at frequent intervals in the slopes of the hills 

a few miles east of the trail. They also appear in the bluffs of the 

creek both above and below the ranch. Some miles northeast and 

east of Hooper's ranch there is a high ridge forming the divide 

between Sage Creek and Many Berries Creek (Big Timber Creek of 

some maps). Along the western slope of this ridge the Judith River 

beds are extensively exposed and are overlain by the Bearpaw shales.

SAGE CREEK AREA, ASSINIBOIA.

On Sage Creek, a small stream from the overflow of which Wild 

Horse Lake has its origin, there are important exposures of the Judith 

River beds, which have been described and mapped b}^ Mr. R. G. 

McConnell. These occur north of the lake on the west side of the 

road, about 8 miles north of the international boundary, and also 

about 2 miles below Can-oil's ranch, on Sage Creek. At the place last 

named some excellent exposures of the Judith River beds in the bluffs 

of a western tributary of tfye creek yielded Sphcerium planum, GonioItasis sublssvis, Viviparus, and plant fragments, including a cone. 

The lignite-bearing strata at the top of the Judith River beds are not 

represented here, but just above Carroll's house, on the west side of the 

creek, they appear, and they are frequently exposed for several miles 

in the bluffs of Sage Creek and its tributaries with characteristic vertebrate and invertebrate fossils. About 5 miles above Carroll's ranch 

and a mile or two above the mouth of the West Fork, Sage Creek flows 

through a deep, narrow gorge, the hills being much higher on the west 

side than on the east, and somewhat higher than the plain to the 

southeast. In the upper part of this bluff are about 50 feet of Bearpaw shales with Baculites ovatus, Placenticeras whitfieldi, Callista 

deweyi, Cyprina ovata, and Ostrea patina. Underlying these shales 

are about 150 feet of the upper Judith River beds, with the lignites at
54 THE JUDITH BIVER BEDS. [BULL. 267.

the top and light ash-colored and brown sandstones at the bottom (see 

PI. X, JB). In a brown sandstone about 10 feet above the creek are 

Unios and other fresh-water invertebrates, and 75 feet above the creek, 

near the base of 15 feet of light ash-colored sandstones overlying a 

bed of impure lignite, we found a considerable portion of a Trachodon 

skeleton. (See PL X, A.)

The following is a section from the bed of the creek to the top of 

the hill as displayed at this place:

Section on Sage Creek, Assiniboia.

Feet.

4. Bearpaw shales with characteristic fossils, Ostrea patina, Placenticeras whitfieldi, and Baculites ovatus, etc ....................................... 50

3. Finely banded shales with 4 feet of impure lignite at base and several feet of

same at top. Occasional thin seams of lignite in main body of shales.. 50

2. Light ash-colored sandstones with Trachodon skeleton at base............... 15

1. Sandstones and shales with lignites, the latter especially well developed 

toward the top. Ten feet from the base is a heavy bed of hard sandstone, weathering brown, with Unio dame, Anodontapropatoris, Sphierium, 

Physa, and Hyalina occidentalis. In the middle there is an exposure 

of about 10 feet of light ash-colored sandstones with ferruginous nodules 

and lenses of brown sandstones. The nodules have numerous fragmentary plant remains. This is overlain by 15 feet of arenaceous shales and 

lignites ............................................................ 75

About 4 miles farther up Sage Creek, in the vicinity of McClean's 

ranch, are important exposures of the Bearpaw shales with such characteristic fossils as Baculites ovatus, Placenticeras whitfieldi, Ostrea 

patina, and Inoceramus sagensis. This is a typical development of the 

Bearpaw shales, consisting of dark, finely laminated shales with limestone nodules inclosing numerous specimens of Baculites and Placenticeras. These shales are clearly seen to be the same as those overlying the Judith River beds farther down the creek. The aneroid 

gave them a thickness of 110 feet, but the base was not shown. On 

the west side of the creek, a mile below McClean's fence, there is a small 

exposure of the Judith River beds just at the bottom of the creek bluff. 

This is the uppermost member of these beds, the main bod}^ having 

here passed beneath the level of the stream. About 65 feet of the 

uppermost lignitiferous beds are represented.

Opposite McClean's ranch, on the south side of Sage Creek, 100 feet 

of upper Judith River beds overlain by 200 feet of Bearpaw shales 

form a range of hills 3 miles west of south of McClean's house. The 

Bearpaw shales at this locality yielded Baculites ovatus, B. compressus, 

Placenticems whitfieldi, P. intercalare, Nautilus dekayi, Ostrea patina, 

Cyprina ovata^ Callista deioeyi, gasteropods, and crustaceans. No fossils were found in the Judith River beds, which here consist of the 

uppermost 100 feet of that formation and carry much impure lignite. 

The Bearpaw shales are here cut by two or three sandstone dikes, each
U. S. GEOLOGICAL SURVEY BULLETIN NO. 257 PL. X

.1. EXPOSURE OF JUDITH RIVER BEDS ON SAGE CREEK, ASSI N I BO! A. 

Showing remains of Trachodon skeleton.

CONTACT BETWEEN JUDITH RIVER BEDS AND OVERLYING BEARPAW SHALES 

ON SAGE CREEK, ASSINIBO1A.
EXPOSURES ON SAGE CBEEK, AS3INIBOIA. 55

about 10 inches wide and several hundred yards in length. These 

dikes have a northwest-southeast direction and dip 60° NE. At 

this locality the Bearpaw shales are very fossiliferous and present four 

distinct white alkali bands. From this point northward the divide 

between Sage Creek and Willow Creek, along the road to the Cypress 

Hills, consists of Bearpaw shales covered by a thin veneer of glacial 

drift.

On Willow Creek, a small stream rising in the western end of the 

Cypress Hills, are extensive exposures of Bearpaw shales containing 

J3aculites compressus, Anckura americana, Cinulia concinna, Lucina 

subundata, Pecten (Chlamys) nebrascensis, and Amcula linguiformis. 

Just below John Heed's ranch, on Willow Creek, a heavy bed of brown 

sandstone caps these shales. In no place in this vicinity were we able 

to find the base of the shales exposed, so that we were unable to estimate* their thickness. As one ascends Willow Creek the brown sandstones mentioned above rapidly increase in prominence and at the head 

of the creek form the greater portion of the western extremity of the 

Cypress Hills. They constitute the highest marine horizon seen in the 

Cretaceous of this region and on account of their stratigraphic position and lithologic features are comparable with the Fox Hills sandstones of South Dakota. We collected from them a considerable 

number of marine invertebrates, including Leda (Yoldia] evansi, Amcula 

nebrasoana, Protocardia borealis, Tancredia americana, Callista nebrascensis, and Scapliites nodosus var. quadrangular is. Part of these 

species are known from the Fox Hills beds in other regions, and most 

of them occur also in the Pierre and Bearpaw shales. It has long 

been known that the faunas of the Fox Hills and Fort Pierre are too 

closely related to be considered really distinct.

Toward the summit of the Cypress Hills, on the western end, are 

about 60 feet of soft, light-colored, yellow sandstones with a 6-foot 

vein of lignite near the base. These beds may belong to the Laraniie 

as it has been mapped by McConnell, although we were unable to find 

any fossils in them by which to determine their age.

The exposures examined by us in Canada are all in the southeastern

portion of the large, continuous area of Belly River beds mapped by

 Dawson, McConnell, and Tyrrell. They include both the top and the

. bottom of the formation, as well as good exposures of the overlying

and underlying beds, and hence give a fair idea of the formation as

described by Dawson. The principal localities that have yielded the

Belly River vertebrate fossils described by Lam be are on Red Deer

River some distance north of the most northern point visited by us,

but we have no doubt that they are on the same horizons that we

studied.
56 THE JUDITH KIVEE BEDS. [BULL. 257. 

WILLOW CREEK AREA,'IN CENTRAL MONTANA.

In addition to the above-described exposures of the Judith River beds 

in northern Montana and southern Canada, there are others in central 

Montana, first observed by Hatcher in 1888. One of these occurs 

between Musselshell River and Flatwillow Creek. Near Flatwillow 

post-office a conspicuous ledge of yellow sandstone forms an almost 

continuous and in places perpendicular wall, extending for miles up and 

down the south side of the creek. These sandstones weather into 

pyramid-like forms, dip gentty to the southeast, and form the roadbed 

for about 2 miles along the old freight road from Fort Maginnis to 

Junction City, where they pass beneath the Claggett formation. In 

weathering, color, and lithologic character these sandstones resemble 

the brown phase of the Eagle formation as developed at the type 

locality at the mouth of Eagle Creek on Missouri River, about 20 

miles above the mouth of Judith River. Their stratigraphic position 

between the Benton and Claggett formations also favors this correlation. Some obscure fragments of Baculites were the only fossils 

yielded by them.

After passing over these sandstones, which have an estimated total 

thickness of 200 feet, the Claggett formation is reached where the 

road crosses the first coulee, 2£ miles south of Flatwillow. The 

Claggett overlies the Eagle sandstones and dips gently to the southeast. The shales of this formation yielded Baculites sp., B. ovatus, 

Placenticeras sp., Inoceramus bambini, Lucina occidentalis, and Nucula. 

Both species of Baculites were very abundant. Other fossils were rare. 

About 10 miles from Flatwillow the road crosses a broad, deep coulee 

which occupies the trough of a wide synclinal fold, and in the bottom of 

which may be seen considerable exposures of the lower 100 feet of the 

Judith River beds resting upon the Claggett formation. From the 

Judith River beds at this point we collected remains of turtles and 

dinosaurs, and saw a number of more or less fragmentary bones and 

much petrified wood.

For a mile or more the road crosses the trough of this syncline, and 

there are beautiful exposures of the Judith River beds on either side. 

It then once more traverses the shales of the Claggett formation for 

7 miles, or until Willow Creek is reached. From the higher points 

along the road the Eagle sandstones appear in prominent bluffs on the 

right at a distance of several miles. In this locality the Claggett 

formation can scarcely have a thickness of less than 500 feet. At 

Nolan and Archer's ranch, on Willow Creek about 10 miles north of 

Musselshell River, the Judith River beds again rest on the shales of 

the Claggett formation, and a series of exposures, on the south side of 

the creek form a low, broken wall. The beds have a slight dip (2° or 

3°) southeastward, and consist of light-colored argillaceous sandstones
STHATCHEKND ] EXPOSURES ON WILLOW CREEK. 57

and sandy claj^s with occasional lenses and masses of hard brown 

or gray sandstone. The sandstones are nearly all strongly crossbedded. The rocks are weathered into typical badland forms and 

have a thickness of 75 to 100 feet in the principal bluffs and buttes. 

(See PI. XI, A.) There are some lower beds not so well exposed, as 

well as higher strata to the southeast that are usually covered, but it is 

probable that the total thickness of Judith River beds does not exceed 

200 feet. Vertebrate remains are common in almost every exposure. 

Silicified wood is common also, and at one point about a mile east of 

the wagon road a local deposit of well-preserved plants was found, 

from which all the plants credited to Willow Creek and described by 

Dr. F. H. Knowlton in this paper were obtained. These plants were 

all collected in an area of 3 or 4 square yards, from a bed about 1 foot 

in thickness. About 2 feet below the plants in the same exposure the 

femur, tibia, and fibula of a large Trachodon were obtained. Half a 

mile east of this locality and on about the same horizon fresh-water 

Mollusca are common, including Goniobasis sublaevis, Anodonta propatoris, Sphseriwn, and three or four species of Unio.

West of the wagon-road crossing of Willow Creek the strata immediate^ underlying the Judith River beds are scarcely at all exposed, 

but about 6 miles west of the road there are conspicuous bluffs of light 

brownish or yellowish sandstonej dipping 5° or 6° NE., that probably 

belongs to the Eagle formation. South of the creek is a line of cliffs 

several miles long that often show vertical exposures 75 feet in height. 

At the base of the cliffs there are small exposures of dark shales, like 

the Benton, near the top of which an imperfect specimen of Placenticeras was collected. The overlying sandstones are exposed to a 

thickness of about 100 feet, and after a covered interval of 50 feet 

these are succeeded by 15 feet of similar sandsto~he. In the lower 25 

feet these sandstones are strongly cross-bedded and weather into large, 

rounded masses. These are succeeded by 50 feet of more massive 

sandstone, overlain by 25 feet of thicker bedded sandstone. Fossils 

are rare except in occasional nodules, some of which yield numerous 

specimens. Near the base of the formation we collected Pecten, Avicula linguiformis, Nucula, Lucina subundata, Cinulia, Nautilus 

dekayi (?), Scaphites related to 8. hippocrepis, and young individuals of 

a small, slender faculties that occurs in the Eagle formation on the 

Missouri. About 75 feet higher specimens of Inoceramus, related to 

I. /Tagilis, were obtained.

About 2 miles east of the road, in a bend of the creek, is a good 

exposure showing the contact of the Judith River beds with the Claggett formation. In a distance of about 5 miles along the road from 

Willow Creek to Musselshell post-office there is obtained a complete 

section from the base of the Judith River beds up through the Bearpaw shales into the overlying formations, which latter we did not study
58 THE JUDITH EIVEE BEDS. [BULL. 257.

in detail. All the beds dip gently to the southeast. The dip increases 

in the upper part of the section, being greater in the upper Bearpaw 

shales than in the Judith River beds, which are here clearly seen to pass 

beneath the Bearpaw shales. These shales, especially the upper portion, are rich in marine invertebrates, including the following species:

Fossils obtained from Bearpaiv shales near Musselshell post-office.

Ostrea pellueida. 

Syncyclonema rigida. 

Pecten (Chlamys) nebrascensis. 

Avicula nebrascana. 

Avicula linguiformis. 

Inoceranms barabini. 

Nucula subplana (?). 

Nucula planimarginata (?). 

Nucula cancellata (?). 

Leda (Yoldia) evansi. 

Trigonarca exigua. 

Lucina subundata. 

Protocardia rara. 

Cuspidaria ventricosa.

Liopistha (Cymella) undata. 

Thetis? circularis. 

Anchura americana. 

Acmsea occidentalis. 

Vanikoro arnbigua. 

Lunatia occidentalis (?) 

Haminea subcylindrica. 

Cinulia concinna. 

Baculites compressus. 

Baculites ovatus. 

Scaphites nodosus var. brevis. 

Placenticeras whitfieldi. 

Placenticeras intercalare.

Immediately above the Bearpaw shales is a very thick series of sandstones with intercalated shales and occasional lignite beds, which we 

were unable to study in the limited time at our disposal, though we 

made a brief fruitless search for fossils in the lower portion. At the 

base the dip is 15° to 20° to the south, and higher in the section it 

increases to 30° or more, these tilted beds forming a belt about 2 miles 

in width and consequently several thousand feet thick. From a point 

about 2 miles north of Musselshell post-office southward to Musselshell River similar beds occur with very low dips, and we saw such 

exposures of the same formation for many miles along the Musselshell above the post-office, The only paleontologic evidence of the 

age of the formation overlying the Bearpaw shales in this region was 

found at two localities about 14 and 17 miles west of Musselshell postoffice, where we obtained a' few plants from a horizon probably high 

in the section. Doctor Knowlton has identified among them Taxodium occidentalis Newberry, Populus speciosa Ward, Populus related 

to P. cuneata Newberry, Platanus, VImm rhamnifolia f Ward, Sapindus grandifolius f Ward, Coccuhis haydenianus Ward. Concerning 

them he says: "These species are typically Fort Union and 1 do not 

hesitate to refer them to this horizon."

The beds between this horizon and the top of the Bearpaw shales 

should, from their stratigraphic position, contain the equivalent of the 

Fox Hills and the Laramie as well as the Livingston formation, which 

was described by Weed in the Crazy Mountains, less than 100 miles to 

the west.
U. S. GEOLOGICAL SURVEY

A. JUDITH RIVER BEDS ON WILLOW CREEK 10 MILES NORTH OF MUSSELSHELL,

MONT.

IS, JUDITH RIVER BEDS ON FISH CREEK, MONT.
STANTON 

JIATCH1 'HKR!-D ] DESCRIPTION OF THE BEDS, BY AREAS. 59

FISH CREEK AREA.

There is a considerable exposure of the Judith River beds between 

Fish Creek and Mud Creek, small tributaries of Musselshell River 

near Melville, Mont., a few miles northeast of the Crazy Mountains. 

These exposures were first discovered by Mr. Earl Douglass and were 

described by him under the name of the Fish Creek beds, with the 

suggestion that they are the probable equivalents of the Belly River 

beds. Not being familiar with the Judith River beds, Mr. Douglass 

was unable to recognize the identity of the Fish Creek and Judith 

River outcrops. In their stratigraphic position as well as in their 

lithologic and fauna! characters thejr are almost identical with the 

Judith River beds farther north and should be referred to that formation.

These beds are best exposed on Crawford's ranch between Fish and 

Mud creeks, where they occur in a typical badland region of limited 

extent. (See PI. XI, _#.) Throughout most of this area the Judith 

River beds have a very gentle southerly dip. This is especially true on 

the slope looking toward Fish Creek, but at the divide between Fish 

and Mud creeks the beds are faulted, the fault running irregularly in 

an east-west direction. Immediately south of this fault the Judith 

River beds are nearly horizontal, while to the north they are much 

inclined, in places being nearly vertical or dipping southwesterly at 

angles varying from 30° upward, so that they appear to be unconformable with and to pass beneath the Judith River beds to the south 

of the fault. The upper part of the disturbed series is clearly Judith 

River, and it is evident that the strata have been faulted and that the 

unconformit}7" is only apparent. To the south and west of this badland 

area the Judith River beds are overlain by Bearpaw shales bearing 

the same fauna that has been listed from Willow Creek and other 

localities. These have an aggregate thickness of several hundred feet 

and occupy most of the region to the west between the two creeks. 

South and west of Fish Creek these shales are overlain by marine 

Cretaceous sandstones and by a thick series of beds that have been 

referred to the Laramie, Livingston, and Fort Union formations. The 

Judith River beds in this region are very similar to those on Willow 

Creek, Dog Creek, a'nd the Missouri at and below the mouth of Judith 

River. They contain remains of Trackodon, Ceratops, turtles, and 

crocodiles of Judith River types in fair abundance, much petrified 

wood, and beds of fresh-water Mollusca. The beds are usually light 

ash-colored sands and sandy shales with frequent bands of impure lignite and black ferruginous concretions. In a small draw or canyon 

running west by north from the badlands to Mud Creek (the draw in
60 THE JUDITH BIVEE BEDS. [BULL. 257.

which the Crawfords get their coal) the following section is exposed, 

commencing at the fault mentioned above and going down the draw:

Section in small draw north of Mud Creek.

Feet. 

4. Lower Judith Kiver beds................................................ 200?

3. Claggett beds (sandstones and shales with Inoceramus and Baculites) ....... 300?

2. Eagle sandstones and shales, with thick, bed of coal 100 feet from the base.. 400? 

1. Benton shales, base not exposed......................................... 300?

The above thicknesses are mere guesses and can not be considered 

even as an estimate. No. 3 is probably much below the actual thickness.

The Claggett beds are here made up very largely of sandstones, 

though there are several beds of shales which are usually poorly 

exposed.

The Eagle sandstones present the usual characters of that formation, and the lignite is especially good.

The passage from the Eagle to the Claggett formation and from the 

Claggett to the Judith River beds is so gradual that it is difficult to 

say where the one commences and the other ends. The Bearpaw 

shales are well differentiated from the underlying Judith River beds, 

and the line of demarcation between the Benton and the Eagle formations is likewise very distinct. Northward down the draw toward 

Mud Creek the dip of the Benton gradually decreases and a few calcareous and ferruginous nodular layers are seen here arid there, always 

more or less fossiliferous with Scaphites ventricosus, Baculites asper(f], 

Inoceramus wnbonatus, I. exogyroides, and Pholadomya papyracea,

The influence of the various horizons on the topography is marked. 

South and southwest of Widdecombe Creek, a branch of Fish Creek, 

the alternating sandstones and shales of the formations overlying 

the Bearpaw have produced a' rugged topography characterized by 

a series of low sawtooth ridges of harder sandstones, separated by 

gentle valleys occupied by the intervening beds of shales and other 

soft material. Between this creek and the Crawford badlands there 

is an area of low rolling hills about 6 miles wide that is composed of 

weathered Bearpaw shales. Northward, in the area of the Judith 

River, Claggett, and Eagle beds, is another series of rugged ridges 

separated by narrow valleys. Still farther north is .a low rolling country which extends northward to and beyond Musselshell River and 

which is the result of the erosion and weathering of the Benton shales.

Two miles west of the small draw mentioned above, where Mud 

Creek has cut its way through the upturned beds of the Judith River, 

Claggett, and Eagle formations, a fairly good section is shown from 

the Bearpaw shales down through the above-mentioned formations 

into the Benton. Through most of this section the beds are'inclined 

to the northwest at an angle of about 609.
STHATCHERND] DESCRIPTION OF THE BEDS, BY AREAS. 61 

OTHER PROBABLE AREAS.

Along Milk River the Judith River formation is known to extend 

far east of Havre, where we studied it. Its limits in that direction 

have not been determined. It is very probable that this area is connected with the Cow Creek area by almost continuous exposures 

across the divide separating the drainage of the Missouri from that of 

Milk River east of the Bearpaw Mountains. On our journey from 

Havre to Cow Creek, we passed through the eastern foothills of these 

mountains and crossed several areas of igneous rocks, but on Bean 

Creek near Lloyd post-office we saw outcrops apparently belonging 

to the Judith River beds, and if our route had been a few miles farther 

east we could probably have had the formation in sight all the time.

A few miles north of Billings, on the road from Roundup post-office 

Oil the Musselshell to Billings, Mont., we noticed outcrops that almost 

certainly belong to the Judith River formation. This area is along 

the line of a section described by Lindgren in volume 15 of the Tenth 

Census and was referred by him to the Laramie.

About 50 miles farther east on the Yellowstone, near the mouth of 

Bighorn River, Hayden has described exposures that may also belong 

to the Judith River formation. ,

There are certainly other areas of Judith River beds in the valley 

of Musselshell River north and west of the Fish Creek area which we 

have described. One of these is indicated by Lindgren's "description 

of the occurrence of marine Cretaceous above so-called Laramie beds 

near the mouth of Swimming Woman Creek. Another of these probable areas is indicated by the reported occurrence of Judith River 

species of brackish-water Mollusca at a locality north of the Crazy 

Mountains, where the beds containing them were referred by Weed & 

to the Livingston formation.

In this connection attention may be called to the occurrence of nonmarine coal-bearing beds within the Montana group at Coalville, Utah, 

at Point of Rocks, Wyo., and at several points on the Laramie Plains, 

southern Wyoming/ These beds are probably not very far from the 

horizon of the Judith River beds, but it is not believed that the facts 

would justify their reference to that formation.

"Tenth Census U. S., vol. 15, p. 743. 

bBull. U. S. Geol. Survey No. 105, p. 33.

cSee Stanton and Knowlton, Stratigraphy and paleontology of the Laramieand related formations 

in Wyoming: Bull. Geol. Soc. America, vol. 8, pp. 127-156.
62 THE JUDITH RIVER BEDS. [BULL.257.

RESUMli: A1STD CONOLTJSIOlSrS.

Our field studies in the original Judith River area have established 

the stratigraphic succession of the Upper Cretaceous section and show 

that the Judith River beds lie beneath several hundred feet of marine 

Cretaceous shales with a characteristic invertebrate fauna, and that 

they rest upon another marine formation which also bears an abundant 

fauna. The overlying formation we have called the Bearpaw shales, 

because it is well exposed in the area south, east, and north of the 

Bearpaw Mountains. The name Claggett formation has been given 

to the underlying beds because they are well developed around the 

site of old Fort Claggett, near the mouth of Judith River. Wherever 

the exposures in this region show lower beds the lignite and conspicuous sandstone ledges of the Eagle formation are seen, and still 

lower the dark Benton shales with a characteristic fauna are revealed. 

The Judith River formation itself has yielded a fauna of both vertebrates and invertebrates, most of which are peculiar to it. Its lithologic features also are different from those of any other formation in 

the section and make it easily recognizable.

Beyond the typical area, we found on Milk River in the neighborhood of Havre a similar succession of formations from the Claggett to 

the Bearpaw, inclusive. The formation occupying the position of the 

Judith Riverbeds here has the same lithologicand paleontologic characteristics as in the original area, with Avhich it probably has direct 

connections around the east end of the Bearpaw Mountains. It is therefore unhesitatingly identified with the Judith River beds. From Havre 

this formation was traced by means of practically continuous exposures 

and without essential change of lithologic and paleontologic characters 

into an area of Belly River beds mapped by Dawson. Here again the 

underlying Claggett formation was recognized by its fossils and lithologic features, and above the Judith River (Belly River) beds the Pierre 

shales of the Canadian geologists are clearly identical with the Bearpaw shales of our Montana section.

In other areas studied by us in Montana the same succession of 

formations was observed. Two horizons in this region are especially 

well characterized by marine invertebrates one in the upper part of 

the Benton shales and the other in the Bearpaw shales. Wherever 

these were both present in one section the succession and recognition 

.of the intervening formations were unmistakable.

The stratigraphic relations are more clearly shown in the following 

diagrammatic arrangement of comparative sections:
STANTON 

HATCHESEKND | RESUME AND CONCLUSIONS.

Sections in South Dakota, Montana, and Assiniboia.

63

Montana group.

Colorado group.

South Dakota 

section.

Lararnie.

Fox Hills.

Pierre.

Niobrara. 

Ben ton.

Dakota.

Central and northern 

Montana section.

Laramie?

Fox Hills?

Bearpaw. 

Judith River. 

Claggett. 

Eagle.

Ben ton.

Dakota?

Southern Assiniboia 

section.

Laramie?

Fox Hills?

Bearpaw.

Belly River 

(Judith River). 

Claggett.

CO

(?)

(?)

The Montana and Colorado groups are generally recognized as 

larger subdivisions of the strata lying between the Dakota and the 

Laramie. The South Dakota and Nebraska section is the Meek and 

Hayden section with the Laramie added, while the other two columns 

represent the sections studied by us. The queries in the lower part 

of the columns indicate formations not seen by us in the regions mentioned, and the queries in the upper part of the column indicate our 

doubts as to the correlation of any particular horizon in these sections 

with the Fox Hills, and as to the limits of the Laramie and its relationship with overlying formations that have been described in the region.

A few words of explanation are necessary concerning the general 

correlations expressed and the introduction of new formation names. 

In the first place, the entire Upper Cretaceous section as described 

by Meek and Hayden along Missouri River in South Dakota and 

Nebraska is very much thinner than the Montana section, and in some 

portions the lithologic development is not at all similar. Consequently 

the comparison of individual formations or horizons is in several cases 

made difficult.

Beginning the examination at the base of the section and leaving 

the Dakota out of consideration at present, the first difficulty is in 

connection with the Benton, especially as to its upper limits. In the 

upper Missouri section near Fort Benton a continuous body of shales 

extends up to the base of the Eagle sandstone, and so far as is noAV 

known there is no lithologic basis for a division in it. There are,
64 THE JUDITH KIVER BEDS. [ButL.267.

however, two well-marked faunal zones a lower one characterized by 

Inoceramus labiatus, Scaphites warreni, and the keeled ammonite 

genera Prionotropis and Prionocychis, and an upper zone with 

Inoceramus umbonatus, Inoceramus exogyroides, and Scaphites ventricosus. In the section farther east in South Dakota and Nebraska the 

shales referred to the Benton are limited above by the Niobrara limestone, and their fauna corresponds closely to that of the lower zone 

above mentioned. If it is assumed that the upper limit of the Benton 

shales in the two sections is identical, and that the sequence upward 

is continuous in both cases, then it must follow that the Eagle sandstone is or includes the equivalent of the Niobrara limestone, and 

should be correlated with it, though, of course, distinctive formation 

names are necessaiy. But all the paleontologic evidence is opposed 

to their correlation. On the one hand, the fauna in the upper Benton 

zone of the western section has its nearest representative in Colorado 

and Texas in beds that are referable to the upper Niobrara, and on 

the other hand the fauna of the Eagle formation is much more closely 

allied to the fauna of the overlying marine formations than to the 

Benton fauna, and consequently the formation belongs to the Montana 

rather than to the Colorado group. The objection may be raised that 

the Eagle is a littoral formation,'and that its fauna would therefore 

be different from the Niobrara faunas, but there are littoral faunas 

known at the top of the Benton in Colorado, northern Utah, and southwestern Wyoming, and these are wholly different from the Eagle 

fauna. The most reasonable view seems to be that the Fort Benton 

of the western section includes the representatives of both the so-called 

Fort Benton and the Niobrara of the eastern section.

The second serious difficulty in the Montana section is in determining the exact equivalent of "the Pierre shales. This formation was 

named from Fort Pierre on the Missouri, now Pierre, S. Dak., and

was defined as dark clays, limited above by the Fox Hills sandstone 

and below by the Niobrara limestone, with exposures along the Missouri for some distance both above and below Fort Pierre. Meek and 

Hayden's estimate of the thickness was 700 feet, but more recent 

estimates by Darton in the same general region place it at 1,200 to 

2.000 feet. It contains a large and characteristic invertebrate fauna. 

In the Montana section the shales we have called Bearpaw shales are 

very similar to the Pierre in lithologic character, and they bear a 

fauna composed in the main of identical species, showing an assemblage 

especially similar to that of the upper fossiliferous zone of the Pierre. 

The thickness possibly also approaches that of the Pierre in the 

typical area.

That the Bearpaw shales represent a part of the Pierre is unquestionable, but if they are strictly equivalent to the Pierre, so that they 

should be called by the same name, then in the South Dakota section
STANTON AND 

HATCHERND ] RESUME AND CONCLUSIONS. 65

there is a long unrepresented interval between the Mobrara and the 

Pierre, for, as we have shown, there is considerable evidence that the 

Eagle formation is later than the Mobrara. The overlying Claggett 

and Judith River formations certainly come within the Montana group. 

It is true that Meek and Hayden observed some evidences of erosion 

at the top of the Mobrara, but it does not seem probable that erosion 

or nondeposition could have continued throughout the time represented by the three formations just named without showing greater 

effects than have been observed. It is well known that along the 

western margin of the Great Plains in Colorado there is a great 

thickening of the Pierre, or at least of the formation in the corresponding position, so that in the Denver region it attains the thickness 

of 7,000 feet, while farther south, in the Arkansas Valley, its thickness is over 4,000 feet. Although in all this great thickness several 

zones have been more or less clearly recognized by minor differences 

in the fauna and in lithologic features, no basis for separation into 

distinct formations has been found. In the Montana section the shaly 

portion of the Claggett formation does not differ very greatly in 

lithologic character from the Bearpaw shales, and though the fossils 

are less numerous they are all of species that occur in the Bearpaw 

and the Pierre, while the sandstone members of the Claggett bear a 

littoral fauna that is closely related to that of the Fox Hills and even 

contains many of the same species. It is very probable, therefore, 

that the Claggett would not have been separated from the Bearpaw as 

a distinct formation if the totally different Judith River beds had not 

been interpolated between them, for the intermingling of Fox Hills 

and Pierre species has long been known elsewhere.

In view of the facts above stated it seemed expedient to give the 

local name Bearpaw shales to the formation immediately overlying 

the Judith River beds, rather than to regard it as the strict equivalent 

of the Pierre and to call it by that name, although we do not doubt 

that the one formation can be traced directly into the other and that 

some zones in both are identical. The Claggett formation is a stratigraphic unit, distinct and easily separable from the previously defined 

formations above and below it, and hence it required a new name.

Returning to the correlation diagram (p. 63), we wish to leave the 

question open whether the Pierre fills all of the space corresponding 

to that occupied by the Bearpaw, Judith River, Claggett, and Eagle 

formations, although we are confident that all of these belong to the 

Montana group. The identification of the Fox Hills formation in the 

Montana section is left in doubt partly because we did no detail work 

on that part of the section, and more especially because we have 

found that many of the Fox Hills species have a great vertical range, 

throughout which they may be expected to occur wherever suitable

Bull. 257 05 5
66 THE JUDITH EIVEE BEDS. [BULL.257.

conditions are found, so that paleontologic identification of the formation without the most careful stratigraphic work is extremely 

unreliable. The problem of the Laramie and associated later formations in this region is a veiy complex one, to which we were able to 

devote very little time, and consequent^ we do not desire to express 

any definite opinions concerning it.

Our principal conclusions from the season's work may be summarized as follows:

1. The Judith River beds are distinctly older than the Laramie, 

being separated from the latter by at least several hundred feet of 

marine shales identical in their faunal and lithologic features with the 

Pierre to which we have given the local name Bearpaw shales, from 

the Bearpaw Mountains about which they are well exposed.

2. The Belly River beds of Canada are identical with the Judith 

River beds of Montana. The name Judith River beds, having priority, should be the accepted name for this formation and the terms 

Belly River and Fish Creek beds should be dropped.

3. The marine sandstones and shales immediately underlying the 

Judith River beds do not represent either the Benton, as some Canadian geologists have supposed, or the Fox Hills and upper Pierre, 

as most geologists of the United States who have examined them have 

believed, but they constitute a distinct horizon within the Montana 

group which we have called the Claggett formation, from old Fort 

Claggett at the mouth of Judith River, near which they are well 

developed.

4. The Eagle formation, from its stratigraphic position and faunal 

relations, marks the.base of the Montana group in this region.

5. The Bearpaw shales, the Judith River beds,1 the Claggett and the 

Eagle formations all belong to the Montana group, and together probably form the equivalent of the Pierre as that term is generally understood, though the possibility is recognized that in the typical area the 

Pierre may have more restricted limits.

6. Faunas similar to that of the Fox Hills sandstone have a great 

vertical range and are likely to be found at any horizon within the 

Montana group where a littoral or shallow-water facies is developed. 

The use of the term Fox Hills as a formation or horizon name outside of the original area in South Dakota is therefore of doubtful 

propriety, as experience has shown.
VERTEBRATE FAUNA.

By J. B. HATCHER.

Leidy, Cope, Marsh, Osborn, and Lambe have been the chief contributors to our knowledge of the vertebrate fauna of the Judith River 

beds. A considerable number of genera and species pertaining to 

all five of the known classes of vertebrates have been described. 

Unfortunately these genera and species are for the most part based on 

exceedingly fragmentary and unsatisfactory material, and it has been 

quite impossible to determine with accuracy even the principal osteological or dental characters of most of the genera or to compare them 

intelligently with related forms from older or more recent formations. 

As an aid to future students there is given here a list of the various genera and species of vertebrates that have been described by various 

authors, with a reference to the original description and a brief statement concerning the nature of the types upon which they were based.

PISCES.

Altogether six genera and eight species of fish have been described 

from deposits referred by us to the Judith River beds. These genera 

and species are known only from detached scales, teeth, and bones. 

They doubtless represent only a small fraction of the fish fauna of 

these beds. While they give an indication of the character of some of 

the fishes that inhabited the waters of this region in Judith River times, 

they are at present known from such insufficient material as to render them of little value for purposes of correlation, as is abundant!}' 

evidenced by the apparent similarity existing between the fish remains 

known from these beds and those from the Laramie. This similarity 

is so striking that some paleontologists have been led, largely from such 

evidence, to correlate the Judith River beds with the Laramie, disregarding the more important evidence afforded by the dinosaurian 

fauna and the stratigraphy.

LEPIDOTUS OCCIDENTALIS Leidy.

Lepidotus occidentalis Leidy, 1856, Proc. Acad. Nat. Sci. Philadelphia, 1856, p. 73. 

Leidy described the species as follows:

A species proposed on five specimens of thick lozenge-shaped scales, with the root 

prolonged in the direction of the long diameter. The enameled surface of the scales 

is smooth and shining. The largest one has its sides about 4 lines long, the smallest 

one about 2£ lines long.

67
68 THE JUDITH ELVER BEDS. [BOLL.257. 

LEPIDOTUS HAYDENI Leidy.

Lepidotus haydeni Leidy, 1856, Proc. Acad. Nat. Sci. Philadelphia, 1856, p. 73. 

The original description of the species was as follows:

A species proposed on a single specimen of a thick oblong square scale, the long 

sides of which measure 5 lines and "the short 3J lines. The root projects forward 

from one of the long sides, and the enameled surface of'-the scales is covered with 

parallel square lines.

CEBATODTJS ERUCIFERUS Cope.

Ceralodus eruciferus Cope, 1876, Proc. Acad. Nat. Sci. Philadelphia, 1876, p. 259. 

This species was described by Cope as follows:. .

A basal lamina separable from the dentigerous lamina. The latter supports ribs 

which diverge from a single marginal rib which extends along one side. The marginal rib is separated by a deep groove from the radiating ribs, which is continuous 

with the grooves between the latter. The ribs are of irregular diameter and not 

perfectly straight; they are interrupted by weak transverse ridges, which project 

beyond the margin. The ridges rise abruptly from their common base and are separated distally by notches of the margin.

Measurements.

M.

Long diameter of dental surface ....................... ....... 0. Oil

Short-diameter of dental surface............................... . 007

Thickness of plate............................................ .003

There are six ridges in the length.

CERATODUS HIEROGLYPHTJS Cope.

Ceratodus hieroglyphics Cope, 1876, Proc. Acad; Nat. Sci. Philadelphia, 1876, p. 260.

This species was described by Cope as follows:

The dentigerous plate is thin and dense, and has the appearance of a shorttoothed comb with a handle. The tooth-like points are the extremities of low 

ridges, which are arranged nearly at right angles to a wide longitudinal elevated half 

of the osseous base. They are separated by shallow grooves from each other, and 

are not continuous with the basis just mentioned, which rises abruptly above them. 

They are smooth. The "handle" above alluded to is triangular in section, having 

two-bevels on the side supporting the tooth ridges. The lower face of the bone is 

smooth. &

Measurements.

M.

Total length ................................................ 0.013

 Length of dentigerous portion................................ . 010

Total width................................................. .0045

Width of dentigerous portion................................. . 0020

There are thirteen teeth in the length.

MYLEDAPHTJS BIPARTITTJS Cope.

Myledaphus bipartitus Cope, 1876, Proc. Acad. Nat. Sci. Philadelphia, 1876, p. 260.

This species is founded on detached and isolated teeth. Teeth of 

this pattern and of varying size are abundant both in the Judith 

Eiver beds and in the Laraniie. It would be quite impossible to identify either genera or species from teeth of such simple form.
HATCHER.] VETCTEBRATE FAUNA. 69

HEDRONCHUS STERNBERGII Cope.

Hedronchus sternbergii Cope, 1876, Proc. Acad. Nat. Sci. Philadelphia, 1876, p. 259. 

Cope described this species as follows:

Char. Gen. The bone on which this genus reposes has the appearance of the crown 

of a young tooth. Its central cavity is large and expands to the margin of the basis; 

its apex is unworn. It appears to be too protuberant for the position of a dermal 

tubercle. It may be distinguished as a short crown on a shorter slightly constricted 

portion or neck. The crown culminates in three crests, which together form a letter 

T, arid which descends toward the neck. There is no investment of cement or 

enamel, and the material of which it is composed resembles dense bone.

Char. Specif.- The faces on each side of the stem of the T are concave and divided 

by an oblique crest, which descends from the common apex. The other face isgently convex, and the inferior part of each of its bounding crests projects ear-like. 

The base is an oval.

Measurements.

M.

Elevation of crown........................................... 0.006

Diameter of bage{longitudinal................................. .005

Urans verse. ................................... . 004

ACIPENSER ALBERTENSIS Lambe.

Adpenser cdbertensis Lambe, 1902, Cont. Canadian Palseont, vol. 3, pt. 2, p. 29..

This species is founded on a detached keeled dermal shield from the 

Judith River beds of Red Deer River, Canada. Similar ossifications 

are common in the Judith River beds arid in the Laramie of Converse 

County, Wyo., and probably represent more than one species.

DIPHYODUS LONQIROSTRIS Lambe.

Diphyodus longiroslris Lambe, 1.902, Cont. Canadian Pakeont, vol. 3, pt. 2, p. 30.

This species is founded on a jaw fragment from the Judith Riverbeds of Canada, with numerous tooth scars which show the teeth to 

have been simple and conical and ankylosed with the jaw. Fragments 

of similar jaws are common both in the Judith River beds of Montana 

and in the Laramie deposits of Converse County, Wyo.

AMPHIBIA.

Two genera and five species of tailed Batrachia have been described 

from the Judith River beds. All of these have been founded on vei\y 

fragmentary and insufficient material, consisting for the most part of 

detached vertebrae, with an occasional limb bone or jaw fragment. 

Similar remains, for the most part undescribed, are common also in 

the Laramie.

All five of the species of Batrachia mentioned were described by 

Cope from material secured in the Judith River beds of Montana. 

Lambe a has reported Scapherpeton tectum Cope from the same beds on

(i Oont. Canadian Palseont., vol. 3, pt. '2, p. 31.
70 THE JUDITH KIVEE BEDS. [BULL. 257.

Eed Deer River in Canada. From the fragmentary nature of the 

types on which were based Cope's descriptions of the various genera 

and species, it will readily appear how extremely difficult it will be to 

refer any material with certaintjr to any of his species. Moreover, the 

fragmentary nature of all the remains of Batrachia thus far recovered 

from this formation renders them of little value for purposes of correlation, and were these remains better preserved it is improbable that 

they would afford any very reliable evidence as to the exact or relative 

age of the deposits, owing to the apparently slight modification which 

has taken place in these Batrachia throughout Cretaceous and Tertiary 

times. The Batracia of the Judith Biver beds can not be regarded as 

of any special value in determining the age of the deposits or in correlating them with other formations.

SCAPHEEPETON Cope.

Scapherpeton Cope, 1876, Proc. Acad. Nat. Sci. Philadelphia, 1876, p. 353. 

This genus was described by Cope as follows:

Vertebrae deeply biconcave, with opposed, but not continuous, foramina for the 

chorda dorsalis. Neural arch with zygapophyses, and well-developed neural spine. 

Centrum with vertically compressed, short diapophysis near the posterior extremity, 

a prominent hypapophysial keel, and prolonged neural spine. Supposed proximal 

limb bone with a branch-like trochanter. Supposed teeth in several rows, attached 

in shallow alveoli, those of the marginal series larger; the crowns obtusely conic and 

simple.

SCAPHERPETON TECTTJM Cope.

ScapJierpeton tectum Cope, 1876, Proc. Acad. Nat. Sci. Philadelphia, 1876, p. 355.

This species is founded on a single vertebra accompanied by a fragment which, according to Cope, "resembles the articular portion of 

the mandible."

SCAPHERPETON LATICOLLE Cope.

Scapherpeton laticolle Cope, 1876, Proc. Acad. Nat. Sci. Philadelphia, 1876, p. 356.

This species was founded on an atlas and several dorsal vertebras of 

different individuals, which latter, according to the author of the 

species, may pertain to the preceding species. An imperfect limb bone 

was found associated with the neural arch of a vertebra of the character 

ascribed to this species, and was described by Cope in connection with 

the type.

SCAPHEEPETON EXCISTJM Cope.

Scapherpeton excisum Cope, 1876, Proc. Acad. Nat. Sci. Philadelphia, 1876, p. 357.

This species was founded on scattered vertebra from three individuals of different sizes.

SCAPHEEPETON FAVOSUM Cope.

Scapherpeton favosum Cope, 1876, Proc. Acad. Nat. Sci. Philadelphia, 1876, p. 357. 

This species is founded on a single vertebra.
HATCHER.] VERTEBRATE FAUNA. 71 

HEMITRYPUS JORDANIANUS Cope.

Hemitrypus jordanianus Cope, 1876, Proc. Acad. Nat. Sci. Philadelphia, 1876, p. 358. 

This genus and species were founded on a single vertebra from the 

Judith River beds. This genus is distinguished from the preceding 

genus by the position of the foramen chordae dorsalis.

The Reptilia are far better represented in the Judith River beds 

than the other classes of Vertebrata. Not only are most of the larger 

subdivisions of the group represented, but the fauna is rich also in 

genera and species which in Judith River times were evidently undergoing a rather rapid development and acquiring a considerable degree of 

specialization. Genera and species such as these, which may be termed 

progressive types, afford the most reliable paleontological evidences 

upon which to base accurate correlations. The more specialized Reptilia offer more trustworthy evidence as to the age of these beds than 

any other group of vertebrates. Furthermore, from the abundance 

and condition of the remains the reptilian fauna of this formation and 

of other formations can be more carefully compared than is practicable 

with other classes of vertebrates.

PLESIOSAURIA.

While the Judith River beds are for the most part of fresh- and 

brackish- water origin, it is evident that at certain periods during their 

deposition the sea had access to limited areas of the region over which 

these beds are distributed. At certain localities like that mentioned 

on page 42, remains of typically marine invertebrates and vertebrates 

occur well within the limits of the Judith River beds. From such 

marine deposits we obtained shark's teeth pertaining to a number of 

distinct species, and remains of plesiosaurs and chelonians, some of 

which latter appear also to belong to marine species.

CIMOLIASAURUS MAGNUS Leidy.

Cimoliasaurus magnus Leidy, 1853, Proc. Acad. Nat. Sci. Philadelphia, 1853, p. 325. 

Smithsonian Contrb. to Knowl., vol. 14, p. 25.

Lambe ft has reported vertebrae pertaining to this genus and species 

from the Judith River beds of the Red Deer River, Canada. The 

original description of this genus and species was based on vertebras 

from the Greensands of New Jersey, for the most part of much larger 

size than those described by Lambe, and it is not improbable that the 

material described by the latter may pertain to a distinct genus and 

species. In some respects they more nearly resemble the vertebrae 

on which Leidy based his description of Ischyroth&rium antiquum. 1

«Cont. Can. Pal., vol. 3, pt. 2, 1902, p. 32. bProc. Acad. Nat. Sci. Philadelphia, 1856, p. 89.
72 THE JUDITH EIVEE BEDS. [uuLL.257.

URONAITES CETIFORMIS Cope.

Uronaites cetiformis Cope, 1876, Proc. Acad. Nat. Sci. Philadelphia, 1876, p. 346.

Founded on "cervical, dorsal, and caudal vertebras, portions of 

limb, and rib bones" found near the top of the Claggett or base of the 

Judith River beds near Armell's (Amell's) Creek, a small tributary of 

Missouri River in northern Montana, at about the eastern limits of 

the Judith River basin as defined by Hay den.

ISCHYKOTHERITTM cf. ANTIftTJTTM Leidy.

Ischyrotheriumci. antiquum Leidy, 1857, Proc. Acad. Nat. Sci. Philadelphia, 1856, p. 89.

We collected a number of vertebral centra from the marine horizon 

mentioned on page 42 as occurring within the usually recognized limits 

of the Judith River beds, which closely resemble those described and 

figured by Leidy a as the type of the present genus and species and 

which were obtained between Moreau and Grand rivers in South 

Dakota. Although Leidy states in his description that they were 

obtained "from an outlyer of the Great Lignite Tertiary formation" 

of that region, it is more than likely that the exact horizon was more 

nearly that of the Fox Hills or Pierre. However this may be, the 

vertebras collected by us doubtless are from beds older than those 

which yielded the type of the genus and species. Whether the vertebrse in question pertain to Ischyrotheri-um, to one of the two previously 

mentioned genera of plesiosaurs, or to a distinct genus can be determined only by cai'eful comparisons with the types, and the material is 

so incomplete that even then a fairty conservative paleontologist could 

not feel sure of his determination.

The plesiosaurs, like the fishes and the batrachians in the Judith 

River beds, afford very scanty and unsatisfactory evidence as to the 

age and proper correlation of the deposits.

CHELONIA.

Remains of chelonians are common in the Judith River beds. 

Altogether eight genera and fourteen species have been described 

from these deposits; most of these, unfortunately, are known from 

very fragmentary material, consisting for the most part of fragments 

of the carapace or plastron. In only a few instances is anything 

known of either the skull or the endo-skeleton.

TEIONYX FOVEATUS Leidy.

Trionyx foveatus Leidy, 1857, Proc. Acad. Nat. Sci. Philadelphia, 1856, p. 73.

The type of this species was collected by Doctor Hayden in the 

Judith River beds. The nature of the material upon which Leidy's

"Trans. Am. Philos. Soc., vol. 11, p. 150.
HATCH!*.] VERTEBEATE FAUNA. 73

description of the species was based can be best appreciated by quoting his original description, which is as follows:

The species is founded on fragments of several costal and sternal plates. The 

exterior surface of the costal plates is covered with pits, excepting close to the margins; and the pits are small and round at the vertebral extremity, and gradually 

increase in size outwardly and become antero-posteriorly oblong, oval, and reniform. 

A Arertebral fragment of a third or fourth costal plate, a little over an inch in length, . 

is 11 lines wide and 2 lines thick. Small fragments of the sternal plates present an 

exterior surface covered with broken vermicular ridges and tubercles separated by 

wide intervals. Fragments of a hyposternal plate are 3 lines in thickness.

In a later paper a Doctor Leidy figures the type material and associates with it remains of another specimen collected by Hayden in the 

"Great Lignite Tertiary [probably Laramie] basin, near Long Lake, 

below Fort Clark," on Missouri River. He says of these remains 

that, they are " not distinguishable from Trionyx foveatus," but adds 

that " the specimens are too imperfect positively to determine whether 

they actually belong to the same species." Considering the difference 

in the age of the deposits, it is quite probable that had better material 

been at the disposal of Doctor Leidy he would have found them to be 

at least specificalty distinct.

Lambc ?> has described and figured much better material which he 

refers to this genus and species. His material was secured from the 

Judith River beds on the Red Deer River in Canada.

TRIONYX VAOANS Cope.

Trionyx vaganx Cope, 1874, Ann. Kept. U. S. Geol. and Geog. Surv. Terr, for 1873, 

p. 453.'

The original description of this species was as follows:

Represented by a number of costal bones and perhaps of sternals also. The former 

are rather light or thin for their width, and are marked with a honeycomb pattern 

of sculpture, in which the ridges are thin and much narrower than the intervening 

pits. They incline to longitudinal confluence at and near the lateral sutures. 

Several arete are not infrequently confluent in a transverse direction near the middle 

of the bone.

Measurements.

M.

Width of costal bone ........................................ 0.0370

Thickness of costal bone ..................................... .'0045

Four and five arete in 0.010 m.

This species differs from the T. foveatus Leidy in the much narrower interareolar 

ridges and larger arete, and in their Iqngitudinal confluence at the margins, characters 

exhibited by'numerous specimens.

Lignite Cretaceous of Colorado; near the mouth of the Bighorn Eiver, Montana; 

Long Lake, Nebraska; found at the last two localities by Doctor Hayden.

aTruns. Am. Philos. Soc., vol. 11, 1800, p. 148, PI. XI. 

bCont. Canadian Palseont., vol. 3, pt. 2,1902, p. 33, PI. I.
74 THE JUDITH EIVEE BEDS. [BujL.257.

Latnbe a has described and figured from the Judith Eiver beds of 

the Red Deer River in Canada remains of a turtle which he refers to 

this species. By reference to his figures, however, it will be apparent to all that the specimen described by Lambe pertains to a species 

distinct from T. vagans. According to Lambe's figures the ridges on 

the surface sculpturing, instead of being "thin and much narrower 

than the intervening pits," as described by Cope, are heavy and 

broader than the intervening pits. There are other differences also 

of no less importance. It seems clear, therefore, that so far as our 

present knowledge goes the distribution of this species is limited to 

the Laramie, and -that it should not be considered as a Judith River 

form.

PLASTOMENUS COALESCENS Cope.

Plastomenus coalescens Cope, 1875, Kept. U. S. Geol. Surv. Terr., vol. 2, p. 93, PI. VIII. 

This species is founded on fragments of plastron and carapace collected by George M. Dawson near Milk River, in Canada, from beds 

referred by Cope to the "Transition series, probably the Fort Union 

or Lignite epoch," but now known to belong to the Judith River 

series. - The type material is extremely fragmentary and it would be 

difficult to identify other material by a comparison with Cope's description, his figures, or the type.

PLASTOMENUS COSTATUS Cope.

Plastomenus costatus Cope, 1875, Kept. U. S. Geol. Surv. Terr., vol. 2, p. 94, PL VIII. 

Founded on fragments of carapace and plastron collected by Doctor 

Dawson in the same region and from the horizon from which he 

secured the type of the preceding species. The observations made 

concerning the preceding species apply also to this. While we do 

not doubt that the remains upon which these two species have been 

founded are specifically distinct, yet from their exceedingly fragmentary nature they are of little value in determining other material. 

It would scarcely be possible to definitely refer any material with 

certainty to either species, so imperfect are the types.

PLASTOMENUS PUNCTULATUS Cope.

Plastomenus punctulatus Cope, 1874, Ann. Kept. U. S. Geol. and Geog. Surv. Terr, 

for 1873, p. 453; 1875, Kept. U. S. Geol. Surv. Terr., vol. 2, p. 94, PI. VI.

This species was "established on a costal bone found in association 

with the preceding species and referred to the genus Plastomenus provisionally, and with a possibility that it will be found not to pertain 

to it when fully known." Cope reports it also from the Lignite Cretaceous of Colorado and from Long Lake, Nebraska. The type of 

the present species is even more fragmentary than the types of the 

last two species.

oCont. Canadian Palseont., vol. 3, pt. 2,1902, p. 36, PI. I.
HATCHER.] VERTEBRATE FAUNA. 75 

PLASTOMENTTS INSIGNIS Cope.

Plastomenus insignia Cope, 1874, Ann. Rept. U. S. Geol. and Geog. Surv. Terr, for 

1873, p. 454'; 1875, Kept. U. S. Geol. Surv. Terr., vol. 2, p. 95, PI. VI.

This species is founded on "a portion of the right hyposternal bone 

of a tortoise about the size of the last species and from the same 

locality." A reference to the figure of the type published by Cope 

will serve to further emphasize the extremely fragmentary nature of 

the material upon which he based his description and the absolute 

hopelessness of referring with any degree of cejtainty other and 

better preserved material to this species.

Cope is not at all clear as to the localit}^ or horizon from which the 

types of the last two species were derived. In describing P. punotulatus he says the type was found in association with the preceding 

species (P. costatus). The only locality given by him for the latter 

species is south of Woody Mount, near latitude 49°, British America. 

Then, in describing P. insignis, he says that the type was found in 

the same locality as the last species (P. punctulatus), the inference 

being, therefore, that it also was found near Woody Mount. At the 

close of his description of P. punctulatus he adds "Lignite Cretaceous 

of Colorado ; also several fragments from Long Lake, Nebraska, 

from Doctor Hay den," while after the description of P. insignis he 

says, "Lignite Cretaceous of Colorado" in neither instance making 

an}7 reference to the Canadian locality. Now the localities given in the 

body of his descriptions of both these two species and those appended 

at the close are not only widely separated geographically, but the beds 

referred to are now known also to occupy very different stratigraphic 

positions. It would seem best to relegate both these species to the 

paleontologic scrap basket, since they are valueless from both a biologic and a stratigraphic standpoint.

ADOCUS LINEOLATTIS Cope.

Adocus lineolatus Cope, 1874, Bull. U. S. Geol. and Geog. Snrv. Terr., vol. 1, No. 2, 

p. 30; 1875, Rept. U. S. Geol. Surv. Terr., vol. 2, p. 92, PI. VI.

According to Cope, this species was "established on a number of 

fragments from different exposures of the lignite beds primarily on a 

vertebral and sternal bone. 1 ' The locality is given as "from lignite 

of Colorado, and mouth of Bighorn River, Montana," at neither of 

which localities are there any known exposures of the Judith Rivei 

beds. The types were almost surely secured from the Laramie.

Lambe fl has reported this species from the Judith River beds of 

Canada, and Cope 6 has included it in a list of vertebrates from, the 

Judith River beds of Montana. Since in his several descriptions of 

material referred to this species Cope has nowhere mentioned any of

aCont. Canadian Palteont., vol. 3, pt. 2, 1902, p. 38.

&Bull. U. S. Geol. and Geog. Surv. Terr., vol. 3,1877, p. 573.
76 THE JUDITH RIVER BEDS. [BULL.257.

it as having been derived from the Judith River beds, it is more than 

probable that its appearance in Cope's list of Judith River vertebrates 

is due to an oversight. Considering the difference in age between the 

Judith River beds and the deposits which yielded the types of the 

species, together with the extremely fragmentary nature of the latter, 

as will readily appear from an examination of Cope's figures, it would 

seem quite probable that Lambe's identification of the "two well preserved fragments" from the Judith River beds of Canada, as pertaining to this species, may be incorrect, notwithstanding his remark that 

"this species is readily recognized by its neat and characteristic sculpture."

BASILEMYS OGMITJS (Cope).

Compsemys ogmius Cope, 1875, Rept. U. S.-Geol. Surv. Terr., vol.2, p. 91. 

Compsemys variolo'sus Cope, 1876, Froc. Acad. Nat. Sci. Philadelphia, 1876, p. 257.

This genus and species is based on fairly good material discovered 

by the Canadian Boundary Survey near Milk River, Canada, and supplemented by other material discovered by Mr. Charles H. Sternberg 

in the Judith River beds of Montana. Cope's original description 

was as follows:

Compsemys ogmius Cope. Represented in the collections of the British-American 

Boundary Commission by portions of the carapace and plastron. These are massive, 

and indicate a species of large size. As in other species of the genus, the external 

surface is a dense layer of cement or allied substance, which is sculptured with 

shallow pits.

A portion of the costal bone is concave and increases rapidly in thickness in one 

direction. The suture is .coarse, but neither gomphosial nor squamosal. A portion 

of the plastron is thinner, not curved, and displays a very coarse median suture, in 

part squamosal in character. The sculpture consists of shallow pits not wider than 

the low, smooth ridges which 'separate them. There are deep superficial grooves 

marking the boundaries of dermal areas, a feature in which this tortoise differs much 

from the P. coalescens and resembles the species of Compsemys. Should marginal 

bones be found to exist in the P. oymius, its reference to that genus will be further 

established.

From 6 miles west of first branch of Milk River, near latitude 49°.

The material discovered in Montana was referred to a distinct species, Compsemys variolosus, and described as follows:"

One of the most abundant and the largest species of the Fort Union beds. The 

carapace is convex and the plastron flat; the marginal bones are heavy and strongly 

convex on the inferior side. The margin of the plastron is thickened and heavy 

characters which also belong to all parts of the carapace. The sutures of the dermal 

scuta are deeply impressed, and the surface of the bone is strongly sculptured above 

and below and even on the superior face of the thickened margins of the free lobes 

of the plastron. The sculpture consists of round fossae, which are deeply impressed 

and are arranged quincuncially, so that their borders never form straight lines. The 

latter are also more or less angulate on the edge, so that the surface has a more than 

usually rugose character.

The typical specimen equals those of the large land tortoises of. the Eocene in 

dimensions.

aProc. Acad. Nat. Sci. Philadelphia, 1876, p. 257.
HATCHER.J VEETEBEATE FAUNA. 77

Lambe" has described and figured material pertaining to this species 

from the Judith River beds of Canada. He has also reported it from 

the Willow Creek division of the Canadian Laramie. It is not improbable that the latter reference is incorrect. Lambe has placed this 

species in the genus Adpcus, but Hay 6 has made it the type of a new 

genus, Basilemys. Both these authors have accepted the specific name 

variolosus Cope, making ogmius Cope a synonym of variolosiis, although 

ogmlus was described a year before variolosus. W'e collected remains 

of this species at several localities.

BASILEMYS IMBRICARITJS (Cope).

Compsemys imbricarius Cope, 1876, Proc. Acad. Nat. Sci. Philadelphia, 1876, pt 257. 

This species is based on material from the Judith River beds of 

Montana. The original description was as follows:

This species like the others of the genus, has the scutal sutures well defined, and

the superficial surface of the carapace sculptured. The character of this sculpture 

distinguishes the species, and in the present instance in a special manner. It consists 

in the C. imbricarius,. of excavations bounded on the sides by a short ridge each, 

which alternate with each other. Thus each bounding ridge terminates'abruptly at 

the fundus of one of the fossse, while the other end of the fossa rises and contracts to 

another ridge. The result is precisely that seen in the interior sculpture of Saracenic 

domes or niches, and is one which is quite unique among tortoises. The direction 

of the ridges is at right angles to the costal dermal sutures. This species was about 

as large as the snapping tortoise (Chelydra serpentina).

Measurements.

M.

Thickness of a costal bone.................................... 0.0050

Three fosstemeasure{ len8thwise ---------------------------- °065

I- crosswise ............................. . 0050

POLYTHOKAX MISSTJRIENSIS Cope.

Polythorax mismriensis Cope, 1876, Proc. Acad. Nat. Sci. Philadelphia, 1876, p. 258. 

This genus and species was described by Cope from the Judith River 

beds of Montana. From his description, which is quoted below, it 

would appear to have been founded on ample material.

Char. Gen. Plastron with contracted fixed lobes and wide bridge; carapace with 

well-developed marginal bones; mandibular ram us narrow; alveolar face with acute 

external margin; the symphysis neither produced nor recurved. Dermal scuta everywhere distinct, those of the plastron the usual ones, with the addition of the two 

marginal intergulars, and two large interhunierals. The latter scuta are separated 

from the humerals by sutures running parallel with the humeral margin of the anterior lobe between the gular and pectoral scuta.

In the possession of interhumeral scuta, Polythorax differs from any known genus 

of Testudinata. The general structure is much like that of Adocus and Baena, with 

nearer resemblance to the latter in its double intergular scuta. It is impossible to 

ascertain whether there are intersternal bones, as the plastron is ossified throughout.

a Ottawa Naturalist, vol. 15, p. 63, Pis. III-VI, and Cont. Canadian PaUeont., vol. 3, pt. 2, 1902, 

p. 39, PI. II. 

6 Bull. U. S. Geol. Survey No. 179,1902, p. 445.
78 THE JUDITH EIVER BEDS. [BULL. 257 .

The presence or absence^of intermarginal scuta can not yet be determined, although it 

is clear, that if existing, their position is quite external.

This genus is interesting as connecting in its stratigraphical position allied types of 

Cretaceous No. 5 (Adocus), with those of the Wahsatch and Bridger Eocenes (Baena).

Char. Specif. Carapace with openly dentate posterior border. The surface is irregularly swollen, especially on the median line near the margins of the vertebral scuta. 

The vertebral scuta are wide, the costals short, and the marginals narrow. The anterior lobe of the plastron is a little shorter and more contracted than the posterior; 

its base is narrower than the antero-posterior extent of the bridge, its extremity is 

rounded, while that of the posterior lobe is truncate with rounded angles. The gular 

and intergular scuta are each wider than long, while the interhumerals are much longer 

than wide. The numerals are narrow, while the pectorals are wide from the anterior 

position of the pectero-humeral suture. Each anal scutum is longer than wide.

The surface of the plastron is obsoletely but coarsely rugose; the roughness greatest 

anteriorly, where it consists of short raised lines irregularly disposed.

Measurements.

M.

Length of plastron ........................................... 0.183

Length of anterior lobe....................................... . 049

Length of bridge............................................. .076

Width of bridge ............................................. .076

Width of extremity of posterior lobe......................... . 035

Thickness of inguinal region.................................. . 010

From our present knowledge concerning the stratigraphic position 

of the Judith River beds it is evident that Cope was in error in supposing that this genus was intermediate between certain forms (Adocus) 

from the Fox Hills (Cretaceous, No. 5) and others pertaining to the 

genus Baena, from the Wasatch and Bridger Eocenes.

BAENA ANTIQJJA Lambe.

Baena antiqua Lambe, Cont. Canadian Palseont., vol. 3, pt. 2, 1902, p. 44.

This species is founded on portions of carapace and plastron, probably pertaining to a single individual, from the Judith River beds of 

the Red Deer River, Canada. Lambe's description, of the species is as 

follows:

What is preserved of the carapace ig in an excellent, state of preservation. Five 

neurals in<all are represented, with five pairs»of costals'. The sutures are sinuous and 

fine, but can be traced with ease. The sulci are. very distinct.

The neurals are rather irregular in shape and of nearly equal size. The costals 

partake of theirsame irregularity of outline. The-outersurface is almost smooth, the 

only unevenness being due to a few striations and depressed, roughened markings 

erratically disposed. Striations also occur at right angles to the sutures, forming an 

obscure border sculpture. The vertebral shields are broader than long, more especially the first one. The rib heads are well developed. There is a strong and abrupt 

thickening in the axillary region, but elsewhere the shell is thin. The anterior 

border is evenly rounded.

The front end of the plastron is rather broad in proportion to the length of its 

component parts, of which the epiplastrals, the entoplastral, and small portions of the 

hypoplastrals are preserved. The entoplastral, seen from below, is diamond shaped, 

a little broader than long, and placed far forward on account of the shortness of the
HATCHEE.] VEKTEBBATE FAUNA. 79

suture between the epiplastrals in front. Seen from above, or within, the entoplastral is much longer than broad, its breadth being reduced and its posterior half being 

prolonged backward. Similar extensions of the posterior border also occur in the 

upper surface of the epiplastrals. Sulci, as indicated in the figure, define the boundaries of the gular and intergular shields.

BAENA HATCHERI Hay.

Baena hatcheri Hay, Annals Carnegie Museum, vol. 1, p. 325.

The type of the present species was described by Hay from the 

Laramie deposits of Converse County, Wyo. It has been reported 

by Lambe" from the Judith River beds of Canada. Considering the 

difference in size, the variation shown in the different elements of the 

plastron as figured and described by Lambe, and the difference in 

stratigraphic position, there can be little doubt that Lambe was in 

error in referring his material to the present species, which may therefore be very properly excluded from the known species of the Judith 

River fauna. The material referred by Lambe to B. hatcheri should 

either be included in B. antiqua or made the type of a new species.

NEURANKYLUS EXIMITJS Lambe.

Neurankylus eximius Lambe, Cont. Canadian Palseont., vol. 3, pt. 2, 1902, p. 42.

This genus and species is based on portions of the posterior half .of 

a carapace from the Judith River beds of Montana. According to 

Lambe, "the great development of the last neural by apparent coalescence with a suprapygal, the resulting compression of the pygal region, 

and the addition of a ninth pair of bones to the series of costals form 

a combination of characters that is both interesting and unique." The 

genus is considered by its author to show "greater affinity to the 

Chelydridte than to any other group."

In addition to the forms mentioned above, Osborn 6 has mentioned 

Oompsemys victus Leidy and 0. obscurus Leidy as occurring in the Cretaceous of Montana, which might be taken as evidence that they also are 

Judith River forms. In no descriptions of either of these species can 

I find any suggestion that remains of either have been described from 

Montana. The tj^pes of both were from the Cretaceous near Long 

Lake, on Missouri River below Fort Clarke.

From the above remarks concerning the turtles of the Judith River 

beds it will be seen that while several of the included species have 

been founded on very fragmentary material, a few of them have been 

based on fairly complete specimens of either the carapace or plastron, 

or both. While some of the genera mentioned, like Baena and Adocus, 

are of such persistent types that they may be "considered, at present at 

least, as of comparatively little value for purposes of correlation, nevertheless when the chelonian fauna of these beds is known from more

a Cont. Canadian Paloeont., vol. 3, pt. 2,1902, p. 43. 

bIbid., p. 12.
80 THE JUDITH EIVEE BEDS. [BULL. 257.

\

complete material and is thoroughly studied it will doubtless prove to 

be quite different from that of the Laramie.

RHYNCOCEPHALIA.

CIIAMPSOSAURUS Cope.

Champsosaurus Cope, Proc. Acad. Nat. Sci. Philadelphia, 1876, p. 348.

This genus was described by Cope from material consisting for the 

most part of detached and scattered vertebrae from the Judith River 

and Claggett beds of Montana. Vertebrae pertaining to representatives of the genus are common almost everywhere in the Judith River 

beds. They are perhaps the most abundant of the vertebrates of these 

beds. The vertebras are easily recognized, though, as a rule, only the 

centra are preserved. These are biconcave or amphiplatyan, slightly 

keeled below and flat above, with a broad rib facet situated on the 

upper border and at about the middle of the centrum. Cope has distinguished four species of Ckampsosaums from remains found in 

these beds.

CHAMPSOSAURUS PROFUNDUS Cope.

Champsosaurus prqfundus Cope, Proc. Acad. Nat. Sci. Philadelphia, 1876, p. 350.

This, the type species, of the genus, was founded on a cervical, three 

dorsals, and a sacral, presumably from the same individual, from the 

Judith River beds. Distinguished chiefly b}^ the great development 

of the inferior keel.

CHAMPSOSAURUS ANNECTENS Cope.

Champsosaurus annectens Cope, Proc. Acad. Nat. Sci. Philadelphia, 1876, p. 351.

In describing this species Cope remarks that "the greater number 

of vertebras obtained belong to this saurian, which may therefore be 

looked upon as the type of the genus." Since, however, the preceding 

species was described first, it would perhaps be better to follow the 

regular rule in such cases and regard it as the type of the genus, as 

was done by Hay in his Catalogue of American Fossil Vertebrates. 

The species is founded on several vertebras, of which Cope remarks: 

"I can not certainly connect the vertebras of a series as those of a 

single individual."

This species has been reported by Lambe a from the Judith River 

beds of Canada.

CHAMPSOSAURUS BREVICOLLIS Cope.

Champsosaurus brevicollis Cope, 1876, Proc. Acad. Nat. Sci. Philadelphia, 1876, 

p. 352.

This species is founded on a single cervical- vertebra, of which Cope 

remarks as follows:

The evidence for the existence of this species must, be allowed to rest at present on a 

cervical vertebra, with free hypapophysis. This body differs from the corresponding

«Cont. Canadian Palseont., vol. 3, pt. 2, 1902, p. 45.
HATCHEK.] VEBTEBRATE FAUNA. 81

one in the C. annectens in its greater brevity as compared with its length. The vertical 

and transverse diameters exceed the longitudinal in the C. brevicollis, while in the 

C. annectens the length exceeds both. The inferior aspect of this centrum is broadly 

rounded, not carinate as in C. annectens. The value of this character is uncertain, 

but a centrum similarly rounded below (above alluded to) has the more elongate 

form of the C. annectens.

CHAMPSOSATJRUS VACCINSTJLENSIS Cope.

Champsosaurus vaccinsulensis Cope, 1876, Proc. Acacl. Nat. Sci. Philadelphia, 1876, 

p. 353.

This species is founded on a single vertebra. It is defined by Cope 

as follows:

This reptile is indicated by a posterior dorsal vertebra in which the common base 

of the neural arch and diapophysis is decurved to below the middle of the side of 

the centrum. This surface has somewhat the outline of the section of a T-rail, the 

inner portion being on the superior face of the centrum. The centrum is shorter

than the corresponding ones of the C. annectens and C. profundus, so that the basis of

the neural arch approaches near the borders of the articular faces above. The centrum is perforated by two vertical foramina as in most Sauropterygia. The osseous 

tissue of the bone is quite dense and the surface is smooth.

Measurements.

M. 

fantero-posterior ........................ 0.026 . Diameter of centrum.] vertical ...... .......................... . 029

[transverse .............................. . 045

Besides the much larger size, this species differs from those previously referred to 

this genus in almost all details of proportion, etc.

From Cope's description of the vertebra which constitutes the type 

of this species it would appear not unlikely that it pertains to a genus 

distinct from Champsosaurus, though from the nature of the type it 

must be evident to all that it is impossible to properly define either 

the genus or the species to which it pertains.

Of the three preceding species of Champsosaurus it may be remarked 

that, while it is more than probable that several species pertaining to 

this genus are represented in the-Judith River beds, yet, owing to the 

fragmentary and disarticulated nature of the remains upon which Cope 

based his descriptions, he was unable to properly define any of the species, and it would be quite impossible to refer an}r material with certainty to any of the species described by him. It has yet to be shown 

that most of the characters mentioned by Cope as distinguishing his 

species are not present in vertebras from different regions of the vertebral column in the same individual. Mr. Barnum Brown has been 

recently engaged in making a study of some most excellent skeletons 

of Champsosaurus collected by himself in the Laramie. When the 

results of his studies are published we shall doubtless know more of 

the structure of the Cretaceous rhyncocephalians and be able to 

arrive at a more definite conclusion concerning the nature and validity

Bull. 257 05 6
82 THE JUDITH RIVER BEDS. [BULL. 257.

of the various species named by Cope. Owing to the fact that these 

Judith River forms are known almost exclusively from disarticulated 

vertebral centra, and considering the usually very simple structure of 

these throughout the entire vertebral column in this group, it may at 

present be considered difficult, if not impossible, to distinguish the 

Judith River forms from one another or from the later Laramie 

forms. Vertebree of the character now known to pertain to Ohampsosaurus were first described and figured by Leidy a as belonging to 

Palseoscincus costatus. They are now, however, known to have been 

associated with teeth entirely different from those described and figured as the type of that genus and species.

CROCODILIA.

CROCODILTTS HUMILIS Leidy. 

Crocodilus humilis Leidy, 1857, Proc. Acad. Nat. Sci. Philadelphia, 1856, p. 73.

This species was founded on a number of teeth from the Judith 

River beds of Montana. Leidy's original description was as follows:

The species is founded on ten specimens of shed crowns of teeth, apparently of a 

small species of crocodile. The largest specimen is 7£ lines long and 3£ lines in 

diameter at base, which is nearly circular. Another specimen is 7 lines long and 2£ 

lines in diameter at base, and a third specimen is 6 lines long and 3£ lines in diameter 

at base. These are all moderately curved conical, nearly circular in transverse section, with the two usual internal acute ridges, and with the intervening surfaces 

slightly striate or nearly smooth. The crown of a posterior tooth is compressed, 

mammillary in form, 2£ lines long and 2£ wide at base, with the summit obtuse, and 

the sides finely and longitudinally rugose.

From the above description it will readily appear that the simple 

conical teeth upon which the species was based furnish no characters 

for the positive identification of other material.

BOTTOSAURUS PERRUGOSUS Cope.

Bottosaurus perrugosus Cope, 1874; Bull. U. S. Geol. and Geog. Surv. Terr., vol. 1, 

No. 2, p. 26.

This species is founded on " numerous fragments with vertebrae and 

portions of skull" from Laramie deposits of eastern Colorado.

Lambe* has reported this species from the Judith River beds of the 

Red Deer River in Canada. Considering the fragmentary nature of 

the type material and the difference in the age of the deposits, Lambe's 

identification may be incorrect. It would seem better to accept it 

as only provisional until such time as the Crocodilia of the Judith 

River beds and the Laramie have been studied from more perfect 

material.

aTrans. Am. Philos. Soc., vol. 2, p. 146, PI. IX. 

bCont. Canadian Paleout, vol. 3, pt. 2,1902, p. 48,
HATCHER.] VERTEBRATE FAUNA. 83

DINOSAURIA.

A number of genera and species of dinosaurs- have been proposed 

by Leidy, Cope, and Marsh, based upon detached teeth from the 

Judith River beds, although nothing definite is known concerning the 

nature of the animals to which the}7 pertained. Some of these have 

been considered as pertaining to the Lacertilia, others to the Dinosauria, and still others to the Mammalia. 1 shall consider them collectively, however, as doubtfully pertaining to the Dinosauria. They 

are all founded on such fragmentary material as to be of little value 

except as bearing evidence of the diversity of the fauna.

TROODON FOKMOSTJS Leidy.

Troodon formosus Leidy, 1857, Proc. Acad. Nat. Sci. Philadelphia, 1856, p. 72; 1860, 

Trans. Am. Philos. Soc., vol. 11, p. 147, PI. IX.

This genus and species was founded on the crown of a single tooth 

from the Judith River beds of Montana. Teeth of very similar size 

and pattern are not uncommon in the Laramie of Converse County, 

Wyo. Lambe a has reported the genus and species from the Judith 

River beds of Canada.

DEINODON HORRIDUS Leidy.

Deinodon horridus Leidy, 1857, Proc. Acad. Nat. Sci. Philadelphia, 1856, p. 72; 1860, 

Trans. Am. Philos. Soc., vol. 11, p. 143.

This species was originally founded on a number of detached teeth 

from the Judith River beds, evidently pertaining to more than one 

genus and species, as was subsequently recognized by Leidy & when he 

made the more problematical of the teeth at first referred to this 

genus and species the type of a new genus and species, Aubl/ysodon 

mirandus. The remaining teeth referred by Leidy to the present 

genus clearly pertain to members of the carnivorous Dinosauria.

ATTBLYSODON MIBANDTJS Leidy. 

Aublysodon mirandus Leidy, 1868, Proc. Acad. Nat. Sci. Philadelphia, 1868, p. 198.

This species was founded on detached teeth from the Judith River 

beds of Montana. These teeth are variable in size and character. 

Their nature is problematical. Marsh has suggested that some of 

the smaller forms might possibly be mammalian. It seems more 

probable, however, that they are all reptilian and that they pertain to 

some form of carnivorous dinosaur. In general form the teeth are 

subconical, flattened on one side and convex on the other, with a rather 

blunt apex. Teeth of this "character are fairly common both in. the 

Judith River beds and the Laramie. Marsh c has named without

«Cont. Canadian Palreont., vol. 3, pt. 2, 1902, p. 47.

&Proc. Acad. Nat. Sci. Philadelphia, 1808, p. 198.

o Am. Jour. Sci., 3d ser., vol. 44,1892, pp. 174 and 175, PI. III.
84 THE JUDITH RIVER BEDS. [BULL. 257.

describing two species of the present genus, A. amplus and A. cristatus, from material found "in the Ceratops beds of Montana and 

Wyoming." Since neither of these species was properly described 

by Marsh, they may as well be abandoned. While, as remarked 

above, teeth of the same pattern as" those described and figured by 

Leidy are common in both the Laramie and the Judith River beds, 

they do not of themselves afford characters of sufficient importance 

to distinguish either genera or species.

PARONYCHODON LACUSTRIS Cope.

Paronychodon lacuslria Cope, 1876, Proc. Acad. Nat. Sci. Philadelphia, 1876, p. 256.

This species was founded on detached teeth with subconic crowns, 

"one side of which is convex and the other,side plane." After a comparison of Cope's description of the present genus and species with 

Leidy's description and figures of the preceding, it is evident that 

the teeth described by Cope are of the same form as those described 

by Leidy. Since Cope's material was derived from the same general 

locality in the Judith River beds as Leidy's, the last-named genus and 

species may well be considered a synonym of the first.

ZAPHSALIS ABRADUS Cope.

Zaphsalis abradus Cope, 1876, Proc. Acad. Nat. Sci. Philadelphia, 1876, p. 344.

This speqies was founded on detached teeth from the Judith River 

beds of Montana. The meager description given by Cope without 

figures renders it impossible to certainly identify any of the forms of 

teeth known from these deposits with those referred to by Cope in his 

description. It seems probable, however, that his description was based 

on certain small teeth found not very abundantly in both the Laramie 

and the Judith -River beds and characterized by sharp, compressed 

crowns, broad at base and pointed above, flat on one side and gently 

convex on the other, with denticulate posterior and smooth anterior 

border. The flat surfaces of these teeth are distinctly striated and 

have the appearance of having been applied to one another in a manner like that of the inner surfaces of the anterior pair of incisors in 

some rodents. They evidently pertain to the Reptilia, and may represent anterior teeth which occupied a position in the jaw similar to 

that of the incisors in certain Mammalia. Their exact nature must, 

however, for the present at least, remain uncertain.
HATCHEE.] VERTEBRATE FAUNA.' 85

THEROPODA..

DEINODON Leidy. 

Deinodon Leidy, 1857, Proc. Acad. Nat. Sci. Philadelphia, 1856, p. 72.

Cope ft has pointed out that Deinodon Leidy was essentially preoccupied by Dinodon, applied by Durnf eril in 1853 to a genus of reptiles. 

Cope by reason of this substituted the genus Lsolaps, 1 founded in 1866 

on material from the Greensands of New Jersey, overlooking the 

fact, later pointed out by Marsh c , that Lselaps was also preoccupied, 

having been applied by Koch in 1835 to a genus of Arachnida. At 

the same time Marsh proposed the generic name Dryptosaurus to 

replace Lsdaps. Considering that Leid}7 's spelling of the name 

Deinodon differed from that of Dumferil, not a few naturalists would 

be in favor of retaining the former as a good generic name. It is

retained here for those carnivorous dinosaurs with teeth after the

pattern of those to which it was restricted by Leidy in 1859. Should 

this name be abandoned as preoccupied it would perhaps be best to 

give to these Judith River carnivorous dinosaurs a new generic name 

rather than to refer them to 'Dryptosaurus, founded, as we have seen, 

on material from the New Jersey Greensands.

Besides the type species, D. korridus, already mentioned as having 

been described Iry Leidy from detached teeth from the Judith River 

beds of Montana, a number of other specific names have been proposed, 

more especially by Cope, for fragmentary remains from these deposits. 

These so-called species have been referred sometimes to the present 

genus, sometimes to Ldelaps, AuUysodon, Drt/ptosa'iwus, etc. I shall 

refer to them all under the present genus.

DEINODON LATERALIS (Cope).

Aublysodon lateral-is Cope, 1876, Proc. Acad. Nat. Sci. Philadelphia, 1876, p. 248.

This species is founded on detached teeth from the Judith River 

beds of Montana. From Cope's description of this species it is evident that the teeth upon which it is based belonged to the genus 

Deinodon rather than AuMysodon, as those genera were restricted by 

Leidy. Considering the heterodont- nature of the teeth in those 

carnivorous dinosaurs, it is doubtful, if the present species is distinct 

from the type of the genus.

DEINODON INCRASSATUS (Cope). 

Livlaps incrassalus Cope, 1876, Proc. Acad. Nat. Sci. Philadelpia, 1876, p. 248.

. This species was founded on "two teeth, a larger and a smaller, 

which were found near each other, but not sufficiently so as to war-

- "Trans. Am. Philos. Soc., vol. 14, 1870, p. 117. 

b Proc. Acarl. Nat. Sci. Philadelphia, 1866, p. 27G. 

o Am. Jour. Sci!, 2d ser., vol. 14,1877, p. 88..
86 THE JUDITH EIVEE BEDS. [BULL. 257.

rant the belief that they pertain to the same individual." These teeth 

are probably from near the anterior and posterior extremities of the 

series in some representative of D. horrid/us Leidy.

DEINODON EXPLANATUS (Cope).

Lselaps explanatus Cope, 1876, Proc. Acad. Nat. Sci. Philadelphia, 1876, p. 249.

This species was founded on numerous teeth of an apparent^ small 

carnivorous dinosaur from the Judith River beds of Montana. So far 

as it is possible to determine its characters from the teeth alone, it 

appears to be quite distinct from any of the others. Teeth similar 

in character to those described by Cope are common in both the 

Judith River beds and the Laramie. Cope has described the crowns 

of these teeth as " strongly compressed and curved; one side is flat, 

the other gently convex." It is probable that the teeth described by 

Cope occupied a median position in the jaw and that the flat surface 

was the inner.

DEINODON FALCTJLTJS (Cope).

Lxlaps falculus Cope, 1876, Proc. Acad. Nat. Sci. Philadelphia, 1876, p. 249.

This species is founded on several teeth from the Judith River beds 

of Montana. According to Cope, they are of about half the size of 

those of the last-mentioned species and are relatively shorter, stouter, 

and less sectorial in character. They may represent anterior teeth of 

that species.

DEINODON HAZENIANUS (Cope).

Lwlaps hazenianus Cope, 1876, Proc. Acad. Nat. Sci. Philadelphia, 1876, p. 343.

This species is founded on seven detached teeth from different localities. Teeth of the character of those described by Cope are not 

uncommon in both the Lararnie and the Judith River beds. They 

appear to pertain to the anterior dentition of some of these carnivorous 

dinosaurs, probably of D. horridus.

DEINODON UEVIFRONS (Cope). 

Lsdaps Isevifrons Cope, 1876, Proc. Acad. Nat. Sci. Philadelphia, 1876, p. 344.

This species is founded on a single tooth from the Judith River beds 

of Montana. It is distinguished by the absolutely smooth character 

of the anterior edge, a character of doubtful value.

DEINODON CEISTATUS (Cope). 

Lselaps cristatus Cope, 1876, Proc. Acad. Nat. Sci. Philadelphia, 1876, p. 344.

This species is founded on detached teeth from the Judith River 

beds resembling those of Troodon in character and size, and possibly 

pertaining to that genus.
HATCHER.] VERTEBRATE FAUNA. ' 87

OBNITHOMIMUS Marsh. 

Ornithomimus Marsh 1890, Arn. Jour. Sci., 3d ser., vol. 34, p. 84.

The present genus was based upon material from the Laramie 

(Denver) beds of eastern Colorado. Other species referred to the 

same genus by Marsh were secured in Cretaceous deposits in the 

Judith River region of Montana.

OKNITHOMIMUS TENTHS Marsh. 

Ornilhomimus tennis Marsh, 1890, Am. Jour. Sci., 3d ser., vol. 34, p. 85.

This species is founded on a portion of a third metatarsal from the 

Judith River beds of Montana.

ORNITHOMIMUS GRANDIS Marsh. 

Ornithomimus grandis Marsh, 1890, Am. Jour. Sci., 3d ser., vol. 34, p. 85.

This species is founded on fragments representing a considerable 

portion of a skeleton from the Eagle sandstones near the mouth 

of Cow Creek, opposite Cow Island, on the north side of Missouri 

River, Montana. This species, which is much the largest of this genus, 

has been erroneously referred to the Judith River beds. Our researches 

in the season of 1903 demonstrated conclusively that the sandstones 

from which it was obtained belong to the Eagle formation and pertain to a horizon decidedly older than the Judith River beds. Hereafter it should be referred to the Eagle formation. It was a reptile 

of enormous proportions. The third metatarsal, according .to Marsh, 

has a length of 600 mm., and was 90 mm. in transverse and 80 mm. in 

antero-posterior diameter at its distal extremity.

ORNITHOMIMTJS ALTUS Lambe. 

Ornithomimus altus Lain be, 1902, Cont. Canadian Paloeont., vol. 3, pt. 2, p. 50.

This species is based on considerable portions of the skeleton from 

the Judith River beds of the Red Deer River region in Canada. 

According to Lambe's description of the species, the type may be considered as consisting of " a complete hind limb (including the foot), the 

phalanges of the left foot in place, a pubic bone, and an ischium, of 

one individual (No. 930 Can. Geol. Survey)." The present species 

appears, from Marsh's very meager description, to be very closely 

related to, if not identical with, that of 0. tennis Marsh, based upon 

material from the same beds in Montana.

Although the genus Ornithomimus represents the most highly 

specialized theropod dinosaurs found in these beds, they are at present 

represented in our various museums by such meager material that it 

is as yet quite impossible to determine many of the more important 

characters of the genus or to satisfactorily compare the various 

species with one another. Whenever by the discovery of more
88 THE JUDITH RIVER BEDS. [BULL. 257.

perfect material it shall become possible to make comparative studies 

of the various species of Ornithomimidae now reported from the 

Eagle formation, the Judith River beds, and the Laramie, they will 

doubtless prove to exhibit many anatomical differences, perhaps even 

of generic importance, and show various degrees of specialization 

which are at present not discernible.

PREDENTATA.

STEGOSAURIA. 

PALJEOSCINCUS COSTATUS Leidy.

Palasostincus costatus Leidy, 1857, Proc. Acad. Nat. Sci. Philadelphia,. 1856, p. 72. 

In proposing the genus and species Leidy remarks as follows:

The genus and species is founded on a single specimen of a tooth of a lacertian, 

discovered by Doctor Hayden.

The crown of the tooth is palmate, with eight radiating costae terminating at the 

margin in more or less developed points. 'The fang is flattened, cylindrical, and is 

hollow; and it expands into a ridge surrounding the base of the crown. Breadth of 

the crown 4 lines, length 2$ lines; width of the fang 2 lines, thickness 1 line. 

Whole length of the specimen 4 lines.

This tooth was subsequently figured and described a in greater detail 

by Doctor Leidy. In this description it was provisionally associated 

with certain vertebrae now known to belong to the rhyncocephalian 

genus Champsosaurus.

Teeth of the same general form and pattern as "that described and 

figured by Leidy are common in the Judith River beds and the 

Laramie. As yet they have only been found detached, so that nothing 

is positively known as to the nature of the animals to which they 

belonged. On account of their close resemblance to the teeth of

stegosaurian reptiles from the Jurassic, they have been very generally

considered as pertaining to representatives of the Stegosauridse.

Lambe 6 has reported this species from the Judith River beds of the 

Red Deer River region in Canada. We found teeth not specificalty 

distinguishable at various localities both in Canada and in Montana.

PALJEOSCINCUS ASPEE Lambe. 

Palseoscincusasper Lambe, 1902, Cont. Canadian Pakeont., vol. 3, pt. 2, p. 54, PI. XVII.

This species is founded on the crown of a single tooth'from the 

Judith River beds of the Red Deer River region in Canada. According to Lambe, the present species is distinguished as follows: "The 

serrations are more numerous, the sides more conspicuously ridged, 

whilst the double row of denticles at one end of the cutting edge, 

besides being novel, is most interesting and instructive, in that it is

aTrans. Am. Philos. Soc., vol. 11, I860, p. 146, PI. IX. 

6 Cont. Canadian Palseont., vol. 3, pt. 2,1902, p. 53.
HATCHER.] VERTEBRATE FAUNA. 89

suggestive of a progressive step toward the development of a double 

row of tubercles such as is found in the molars of the Multituberculates." I am of the opinion that the characters mentioned above may 

be due to age or the position occupied by the tooth in the jaw, 

rather than to any specific distinction.

STEKEOCEPHALTTS TTJTTJS Lambe.

Stereocephalus tutus Lambe, 1902, Cont. Canadian Palteont., vol. 3, pt. 2, p. 55, Pis.

XI, XII, XXI.

The present genus and species has been described by Lambe from 

remains pertaining to several individuals, for the most part found dissociated in the Judith .River beds of the Red Deer River region in 

Canada. Lambe's description was based on material believed by him to 

represent parts of the skull, the ribs, teeth, dermal scutes, and spines or

plates. He refers the genus to the Stegosauridae, and it appears more

than probable that the tooth figured by him in the text may pertain to 

some member of that family, though it remains to be shown that it is 

distinct from the previously mentioned genus. This tooth certainly 

resembles very closely a large and worn tooth of Palwoscincus.

The fragment of skull, together with the five-keeled bony scutes 

found in connection with it, ma}^ or may not pertain to the same genus 

as the tooth and detached dermal plate. There is considerable evidence, however, for referring them to the Crocodilia rather than the 

Dinosauria. Scutes very similar to those figured and described by 

Lambe, though of much smaller size, are common in the living cayman 

and other members of the Crocodilia, while remains of crocodiles of 

gigantic size are known to occur in the Judith River beds. It seems 

not impossible, therefore, that remains of reptiles pertaining to two 

distinct orders have been associated in the description of this genus.

CERATOPSOIDEA.

Marsh" proposed the family name Ceratopsidee, from the genus 

Cwatops, to include a group of quadrupedal horned herbivorous dinosaurs from the Judith River beds and the Laramie. This family 

included, perhaps, the most highly specialized members of the predentate dinosaurs. It reached its culmination in the Laramie, where 

it was represented ~by numerous individuals pertaining to several 

genera and species. In Judith River times, however, the family had 

already acquired a marked degree of specialization, and was represented 

by at least two or three genera and several species pertaining to 

decidedly more primitive types than the later Laramie forms. At

a Am. Jour. Sci., 3d ser., vol. 36, 1888, p. 478.
90 THE JUDITH EIVEE BEDS. [BULLET.

present two genera are clearly recognizable among the remains of 

Judith River Ceratopsidse. A number of other genera supposed to 

belong to this family have been referred to these beds. Some of these 

genera are based on such fragmentary material that it is quite impossible to identify them specificalty or to determine their relations. 

Some genera are known to belong to other families of the Dinosauria, 

and one or two have been referred by some authors to these beds the 

types of which it seems more than probable were derived from the 

Laramie, although no definite statement was made by their author as 

to their geographic or stratigraphic position beyond the fact that they 

were from the Laramie. This assertion might now be taken as meaning anywhere from the base of the Judith River beds to the top of the 

Fort Union.

DYSGANTJS 'Cope.

Dysganus Cope, 1876, Proc. Acad. Nat. Sci. Philadelphia, 1876, p. 250.

The present genus was the first to be proposed for these dinosaurs. 

Unfortunately it was based on such imperfect material that Cope was 

unable to describe it in such a manner that it can be identified with certainty. The genus was founded on a number of detached teeth pertaining both to members of the present family and to the Trachodontidae, a family of bipedal dinosaurs common also in the Judith River 

beds. Cope proposed four species based upon the remains of teeth 

referred to Dysganus. Since all of these species are unidentifiable, 

it is only necessary to mention them in this connection. They are as 

follows: Dysganus bicarinatus, D. encaustus, D. kaydenianus, D. 

peiganus.

MONOCLONIUS Cope.

Monoclonius Cope, 1876, Proc. Acad. Nat. Sci. Philadelphia, 1876, p. 255. 

This is perhaps the best known dinosaurian genus from the Judith

River beds. Although distinguished chiefly by its cranial characters,

the remainder of the skeleton is also fairly well known. Altogether 

seven species have been referred to this genus four by Cope and 

three by Lambe. After a careful study of the remains upon which 

these various species were based, it is evident that they pertain to more 

than one genus.

Considering Monoclonius crassus Cope, the first species described, 

as the type of the genus and basing our diagnosis of the genus upon 

the material used by Cope in defining. this species, the present genus 

may be distinguished by the following cnaracters: Parietals perforated by lateral fontanelles of moderate dimensions separated by a 

broad, thin, median parietal bar. Sutures for squamosals much abbreviated, indicative of short and proportionally broad squamosals. 

Supraorbital horn cores very short, straight, and triangular in cross 

section. Nasal horn long and curved backward.
HATCHES.] VERTEBRATE FAUNA. 91

MONOCLONITIS CBASSUS Cope.

Monoclonius crassus Cope, 1876, Proc. Acad. Nat. Sci. Philadelphia, 1876, p. 255. .

This species is founded on a sacrum, several vertebrae, limb bones, 

portions of skull, teeth, etc., from the Judith River beds of Montana. 

Owing to the imperfect nature of the material, together with the 

unusual form of some of the elements, which are so strikingly different 

from those in all other known reptiles, Cope's description of this species 

was erroneous in many respects, as will appear from the following 

quotation:

Sacrum with ten vertebrae, the last centrum much compressed, the dyapophyses 

extending horizontally from the neural arch above, and connected by a vertical 

lamina with the iliac supports; length, 27.33 inches. The bones of the limbs are 

robust, the hinder the longer, but not so much so as in some other genera. Length 

of femur, 22 inches; greatest diameter, proxirnally, 8 inches; distally, 7.25 inches. 

The three anterior dorsal vertebrae are coossified, and the first exhibits a deep cnp 

for articulation with the preceding vertebra. The episternurn is a T-shaped bone, 

thin and keeled on the median line belo>v. Length of transverse portion, 21 inches.

The three coossified vertebras are now known to be the anterior 

cervicles instead of the dorsals, while the " episternum" is in reality 

the parietal. Cope's description of the teeth and their method of 

replacement is likewise erroneous. The teeth in the present genus, 

instead of resembling those of Hadrosaurus and being replaced from 

in front as in that genus as stated by Cope, differ markedly from the 

teeth in any of the bipedal dinosaurs. The crowns of the teeth in 

Monoclonius, as in all the Ceratopsidae, are compressed and acuminate, 

There is a strong median vertical keel on the external wall in the upper 

teeth and a similar one on the internal wall of the lower teeth. In the 

unworn teeth the opposite walls of both the inferior and the superior 

teeth present a broad keel. The teeth are replaced from beneath and 

not from the "front," as in.Hydrosaiirus. All the adult teeth, save, 

perhaps, those at either extremity of the dental series, are two rooted.

MONOCLONITJS DAWSONI Lambe.

Monoclonius dawsoni Lambe, 1902, Cont. Canadian Palseont., vol. 3, pt. 2, p. 57, PI.

XVI, XIX, XX.

This species is founded on a considerable portion of a skull from the 

Judith River beds of Canada. The type (No. 1173, Can. Geol. Survey) 

consists of a very fragmentary skull with large and somewhat compressed nasal horn core curved backward, ovate in cross section with 

the broad end of the oval directed anteriorly. The orbit is nearly 

circular, and there still remains in the type the base of a small rudimentaiy supraorbital horn core, notwithstanding Lambe's statement 

that it shows no trace of a horn core. This rudimentary horn core is 

flattened on its external surface as in the cotype of Monoclonius crassus 

Cope. The apex of this horn is wanting in the present specimen. A
92 THE JUDITH EIVEE BEDS. ' [BULL.257,

fragment of the parietal is preserYed, showing three or four of the 

marginal undulations. These resemble those seen in the type of Monoclonius crassus Cope, and I am inclined to regard the present species 

as closely allied to, if not identical with, the M. crassus of Cope. The 

nasal horn and orbit are very large when compared with the occipital 

condyle, the maxillaries, and the quadrate.

The peculiar parietal associated by Lambe with the type of M. 

dawsoni may be regarded as pertaining to a distinct species and perhaps also to a distinct genus. The median parietal bar is very heavy 

and deeply emarginate posteriorly, where on either side it gives off an 

elongated process which is pointed and curves inward and slightly downward. The bases of these processes are separated from one another 

by a distance of 300 mm. They are each 109 mm. in length, have a 

breadth of 112 mm. at the base, and a thickness of 30 mm. They are 

acutely pointed, have rugose surfaces with deep vascular grooves, and 

in life were evidently ensheathed in horn. The posterior border of 

the parietal between the bases of these processes is very thick and 

rounded. On the superior surface, in the middle just in front of the 

posterior border, there is a rather deep concavity. The median bar of 

the parietal is very thick throughout its entire length. Its superior 

surface is marked by a number of very gentle elevations; it is rugose 

and;shows shallow vascular impressions. Besides the processes already 

mentioned as present on the posterior portion of the parietals, there is 

.on either side a series of seven emarginations on the parietal borders, 

separated by as many prominences. The posterior of these prominences are the larger, and they each bear evidence of having supported 

a distinct epoccipital bone during the life of the animal, save perhaps 

the two anterior, which appear to have been overlapped by the squarnosal, since the parietal in this region presents a rather distinct sutural 

surface for contact with the squamosal. The parietals on either side 

of the median bar present a large fontanelle, and the margin of bone 

inclosing this is very thin. These fontanelles have a length of 292 mm. 

and a breadth of 254 mm. The parietal bar is concave on its inferior 

surface, and more especjalty anteriorly. At its anterior extremity-it 

presents a number of cavities and articulates with the postfrentals.

One-half of a horn core, split longitudinally and found with this 

peculiar parietal (No. 971, Can. Geol. Survey) referred by Lambe, 

though 1 think erroneously, to M. dawsoni, appears to represent onehalf of a nasal horn of the type described by Cope as M. sphenocerus. 

Owing to the imperfect nature of this specimen it is not possible to 

determine positive^ whether it represents a nasal or a supraorbital 

horn core. It seems more than probable that this type of parietal 

was associated with a nasal horn similar to that of M. sphenocerus. 

If the horn core should prove to be a supraorbital the evidence 

would be equally in favor of excluding it and the associated parietals
HATCHKK.] , VEETEBEATE FAUNA. 93

from the present species, whose very rudimentary supraorbital horn 

core is widely different. It seems quite probable that this peculiar 

parietal may pertain to M. sphenocerus. From the nature of the 

associated horn core it can not pertain to M. dawsoni.

MONOCLONIUS SPHENOCERUS Cope. 

Monoclonius sphenocerus Cope, 1889, Am. Naturalist, vol. 23, p. 716, PI. XXXIII.

This species is founded on a premaxillary, a nasal, and a nasal horn 

core from the Judith River beds. The nasal horn core of the present 

species is the largest and most powerful observed in the Ceratopsidai. It is perfectly straight and was directed upward and slightly 

backward. The anterior border is sharp throughout its entire length; 

the posterior is broadly rounded. No other portions of the skull are 

associated with the type, so that it is impossible to determine from it 

the character of the frill or parietal crest. As stated above, a portion 

of a horn core found associated with the peculiar parietal referred by 

Lambe to M- dawsoni resembles the nasal horn of the present species, 

and it is not improbable that the parietal figured and described by 

Lambe pertains to the present species rather than to M. dawsoni. If 

so, this would seem to emphasize the distinctive characters of the present species, which might then even be considered as generically distinct from the other known species.

MONOCLONIUS FISSUS Cope.

Monoclonius fissus Cope, 1889, Am. Naturalist, vol. 23, p. 717.

This species is founded on an imperfect pterygoid described as a 

squamosal. The type is not sufficient to afford an adequate description of the species, and the latter should be abandoned.

The three remaining species referred by their authors to this genus 

are here regarded as pertaining to the next genus.

CERATOPS Marsh. 

Ceratops Marsh, 1888, Am. Jour. Sci., 3d ser., vol. 36, p. 477, PI. II.

This genus was founded on an occipital condyle and a pair of supraorbital horn cores from near the summit of the Judith River beds in 

Montana. The horn cores toward the top are nearly circular in cross 

section instead of being flattened on the external side as in Monoclonius Cope. They are much longer than in the type of that genus and 

are somewhat curved, though not so much so in C. montanus Marsh, 

the type species, as in some of the other forms here referred to this 

genus. Combining the characters shown by the. types of the several 

species referred to the present genus, it may be defined as follows: 

Parietals reduced to a narrow median bar and slender posterolateral processes, inclosing on either side large elongated parietal foritanelles. External branches of parietals overlapped by the elongated
94 THE JUDITH BIVEK BEDS. ' [BULL. 257.

and triangular squamosals. Supraorbital horn cores well developed, 

circular in cross section except near the base, and curving backward 

and outward. Nasal horn core strong and curved forward instead of 

backward as in Monoclonius.

CERATOPS MONTANUS Marsh. 

Ceratops monlanus Marsh, 1888, Am. Jour. Sci., 3d ser., vol. 36, p. 477, PI. II.

This, the type species of the genus, was founded, as stated above, on 

an occipital condyle and a pair of supraorbital horn cores from the 

Judith River beds of Montana. The elongate supraorbital horn cores, 

circular in cross section, easily serve to distingush the present genus 

and species from Monoclonius crassus, and subsequent discoveries have 

shown that this type of horn core was associated with other distinctive 

cranial characters of still greater importance.

CERATOPS RECTJRVICORNIS (Cope).

Monoclonius recurvicornis Cope, 1889, Am. Naturalist, vol. 23, p. 716, PI. XXXIV 

[XXIV].

The species is founded on nasal and supraorbital horn cores and other 

parts of the skull pertaining to the same individual from the Judith 

River beds of Montana. The forward curve of the nasal horn, the 

presence of a rudimentary horn on the surface of the frontals a little 

in advance of the orbit, and the well-developed supraorbital horn cores 

are characteristic of this species. Owing to the immature age of the 

individual to which the type pertained, the supraorbital horn cores 

have not assumed their adult form and appear somewhat intermediate 

between those forms which are characteristic of C&ratops and those 

found in Monodonius, though they are decidedly nearer that of the 

former genus.

CERATOPS CANADENSIS (Lambe).

Canademis Lambe, 1902, Cont. Canadian. PaUeont., vol. 3, pt. 2, p. 63, 

Pis. XVII, XVIII.

This species is founded on a portion of a skull and a lower jaw. With 

the skull there is a nasal without the horn, erroneously considered by 

Lambe as a jugal part of the frontal region with the horn, a squamosal, 

and a portion of the slender external bar of the parietal. The supraorbital horn core in the present species is well developed, circular in 

cross section, and curves backward, all of which characters readily 

distinguish it from the short triangular horn cores of Monoclonius. 

The long triangular squamosal is quite different from that which the 

squamosal suture of the parietal would indicate as having been present 

in the latter genus. The fortunate discovery made by Mr. Lambe in 

the Judith River beds of Canada, in which he found the type of the 

present species, fixes with reasonable certainty the character of parietal 

and squamosal that were associated with the type of supraorbital horn 

seen in Ceratops montanus.
HATCHES.] VERTEBRATE FAUNA. 95

CEEATOPS BELLI (Lambe).

Monoclonius belli Lambe, 1902, Cont. Canadian Palseont., vol. 3, pt. 2, p. 66, PI. XX. 

This species is founded on a portion of a parietal from the Judith 

River beds of Canada. The portion of parietal found in place with 

the squamosal in the type of the preceding species is of such a character as to render it more than probable that the present species is 

not specificalljr distinguishable from 0. canadensis, as will appear 

from the following quotation taken from Lambe's description of the 

squamosal of Cemtops canadensis.

The lower surface near and parallel to the inner posterior end is broadly and 

shallowly grooved for the reception of a long, slender bone, triangular in section, 

that projects backward and inward, its outer edge continuing the curve of the 

squamosal. Probably this slender bone represents the anterior end of a forwardly 

bent, side extension of the parietal, such as occurs in the species Monoclonius belli.

The type of the present species would seem, therefore, to be of more 

value as furnishing direct evidence as to the character of the parietals 

in the genus Ceratops than as representing a new species.

CERATOPS PAUCIDUS Marsh.

Ceratops paucidus Marsh, 1889, Am. Jour. Sci., 3d ser., vol. 37, p. 336; 1890, Am. 

Jour. Sci., 3d ser., vol. 39, p. 83.

Founded on a fragmentary maxillary and premaxillary from the 

Judith River beds of Montana. These remains may very well pertain 

to some one of the species of Ceratopsidge previously described. It 

can not certainly be -determined whether they belong to Ceratops or 

to Monoclonius. Owing to the uncharacteristic nature of the type 

material, Marsh was unable to properly define the species, and it 

would be better to abandon it as a nomen nudiim.

Besides the above-mentioned genera and species of Ceratopsidae 

based on material from the Judith River beds there remain to be considered a number of others erroneously referred by some authors to 

this famity.

STEGOCERAS VALIDTJS Lambe.

Slegoceras validus Lambe, 1902, Cont. Canadian Palaeont., vol. 3, pt. 2, p. 68, PI. XXI. 

This species is based on two anomalous bones from the Judith River 

beds of Canada. Although both, these elements were referred by 

Lambe to a single species which he placed in the Ceratopsidse, it is 

evident upon examination that they pertain to two different species 

and belong to another family. Lambe says of these elements: " It is 

probable that these bones were situated in the median line of the head, 

in advance of the nasals." It seems more probable, after a careful 

study of them, that they represent the roof of the brain case and the 

frontal region of the skull of some unknown reptile. For the exact 

determination of their horjologies and the. nature of the reptile to 

which they belonged we must await the discovery of more complete 

material.
96 THE JUDITH EIVEE BEDS. [BULL. 267. 

MONOSPONDYLUS OIGAS Cope.

Monospondylus gigas Cope, 1892, Am. Naturalist, vol. 26, p. 757.

This species is based on two detached vertebral centra from the 

Cretaceous of South Dakota, referred by Cope to the Ceratopsidse, 

but now known to pertain to the Theropoda. The present'genus and 

species are referred to in this connection on account of their having 

been erroneously included byOsborn^in his list of genera and species from the Cretaceous of Montana. In showing these vertebrae to 

the writer Cope stated definitely that they were from the Laramie of 

South Dakota.

CLAOKHYNCHTIS TRIHEDRTJS Cope.

Claorhynchus trihedrus Cope, 1892, Am. Naturalist, vol. 26, p. 757.

This species is based on a rostral and predentary presumably from 

the- Laramie of South Dakota, although it is included by Osborii in 

his list from Montana. It has been referred by Cope to the Ceratopsida3, but the parts described differ materially from the' same elements 

in any known member of that family. From Cope's description they 

would appear to resemble more nearly the predentary and premaxillary of some member of the Trachodontidse. The types are not 

accessible and their nature and relations can at present only be judged 

by the description given by Cope. Unfortunately Cope omitted 

to state where they were found and nothing is positively known 

concerning either their geographic or their stratigraphic position.

ORNITHOPODA.

TEACHODON Leidy.

This genus is perhaps more abundant than any other dinosaurian

genus of the Judith River beds. Altogether five or six species, more 

or less distinct, have been described, while an equal number of species 

have been referred to other genera, some of which may prove to belong 

to Trachodon. Unfortunately the genus Trachodon and its included 

species, as well as the allied genera and species from the Judith River 

beds, are all based on such fragmentary material as to render their 

identification uncertain.

TRACHODON MIRABILIS Leidy.

Trachodon mirabilis Leidy, 1857, Proc. Acad. Nat. Sci. Philadelphia, 1856, p. 72.

Leidy states that this species is "founded upon specimens of teeth, - 

generally very much worn and in a fragmentary condition." Although 

the trachodonts are easily distinguishable by their teeth from the

aCont. Canadian Palseont., vol. 3, pt. 2, 1902, p. 15.
HATCHER.] VERTEBRATE FAUNA. 97

other Dinosauria of these beds, it is scarcely possible to identify 

the various species of this genus or the genera of the family from 

the teeth alone, although Lambe a has ventured to do so. The type of 

the present species was from the Judith River beds of Montana.

TBACHODON BREVICEPS (Marsh.) 

Hadrosaurus brevicejjs Marsh, 1889, Am. Jour. Sci., 3d ser., vol. 37, p. 335.

This species is founded on a portion of right maxillary, with teeth 

in an admirable state of preservation. The label accompanying the 

specimen states that it is from the Bearpaw Mountains. There is no 

doubt, therefore, that it is from the Judith River beds. In form and 

general character the teeth resemble very closely those of Trachodon 

selwyni Lambe from the Judith River beds of Canada, as will be seen 

by a comparison of the figures published by Marsh and Lambe.

TRACHODON SELWYNI Lambe. 

Trachodonfelwyni Lambe, 1902, Cont. Canadian Palaeont., vol. 3, pt. 2, p. 69, PI. III.

This species is founded "principally on the evidence of teeth," distinguished "from those.of T. mirabilis Leidy in being rounded oval 

above instead of terminating in a point." As stated above, in pattern 

and size the teeth of the present species as figured by Lambe agree 

very well with those of the type of T. Ireviceps, from the same beds 

in Montana as figured by Marsh, and it is quite possible that the 

present species is a synonym of T. breviceps.

TBACHODON MAKGINATUS Lambe.

Trachodon marginatus Lambe, 1902, Cont. Canadian Palasont, vol. 3, pt. 2, p. 71, 

Pis. III-X.

This species is based on numerous teeth and remains of the skeleton 

representing almost all the different elements, for the most part found 

dissociated in the Judith River beds of Canada. . That this species 

is based on material pertaining not only to different individuals, but to 

different species, genera, families, and even orders, is clear from a. 

reference to Lambe's figures and descriptions. The ischium figured 

on PI. X of his memoir as pertaining to the present species has 

nothing to do with the present genus, but is the ischium of some 

member of the Theropoda.

Of the abundant material figured and described by Lambe as 

belpnging to this species, none of it has been designated as the type, 

and the identification of the species might best be considered as resting 

upon dental characters alone. On page 77 of his memoir Lambe distinguishes this species by the teeth, which he says are "rounded 

above, with a marginal sculpture."

nCont. Canadian Palseout., vol. 3, pt. 2,1902, p. 77. 

Bull. 257 05 7
98 THE JUDITH KIVER BEDS. [BULL. 257.

TEACHODON ALTIDENS Lambe. 

Trachodon altidens Lambe, 1902,. Cont. Canadian Palseont., vol. 3, pt. 2, p. 76, PI. IV.

This species is founded on a left maxilla with the teeth from the 

Judith River beds of Canada. Distinguished by the small, narrow, 

elongate teeth "beautifully marked for a short distance above the 

apex of the crown, on the raised edges of the outer, enameled face by 

a few obliquely placed, transversely elongated embossments." The 

present species appears to represent one of the smaller members of 

the genus.

PTEEOPELYX GEALLIPES Cope.

Pteropelyx grallipes Cope, 1889, Am. Naturalist, vol. 23; p. 904.

This species is based on a considerable portion of a skeleton without 

skull or teeth, from the Judith River.beds of Montana. Distinguished 

from the preceding genus and species by its more slender proportions, 

pubis coossified with ischium, four digits in pes, and probably more 

elongate fore limbs.

Lambe a has distinguished the various species of Trachodon and 

Pteropelyx as follows:

Comparative table of teeth of species of Trachodon and Pteropelyx.

Trachodon mirabilis Leidy ..........

Trachodon (Pteropelyx) selwyni 

Lambe.

Trachodon (Pteropelyx) marginatus 

Lambe.

Pteropelyx grallipes Cope ...........

Trachodon (Pteropelyx) altidens

Lambe.

Teeth pointed above; margins smooth.

Teeth rounded oval above; margins 

smooth or with the faintest indications of oblique transverse strite.

Teeth rounded above; with a marginal 

sculpture.

Teeth. rounded above; with a border 

sculpture.

Teeth of small size, long in proportion 

to the breadth, and pointed above; 

with a border sculpture near the apex.

In this table Lambe has omitted Trachodon breviceps Marsh, which, 

as I bave already remarked, is probably identical with T. selwyni 

Lambe. While in the Trachodontidae, the teeth from various parts of 

the jaw of the same individual vary greatly in the form and markings, 

and great care should be taken in determining or proposing species 

from teeth alone, the teeth have certain characters, such as have been 

pointed out by Lambe in'the above table, by which they may, within 

certain limits at least, be distinguished specifically. Before accepting 

such dental characters as distinctive of the various species the cranial 

and skeletal features associated with each should be determined. If 

those species founded on dental characters alone are valid, such characters will doubtless prove to be supplemented hy other characters.

a Cont. Canadian Palseont, vol. 3, pt. 2, p. 76, PI. IV.
HATCHER.] VERTEBRATE FAUNA. 99

CIONODON (CINODON) Cope.

Oionodon (Cinodon) Cope, 1874, Bull. U. S. Geol. and Geog. Surv. Terr., vol. 1, 

no. 1, p. 10.

This genus is founded on detached teeth from the Laramie of 

northeastern Colorado. It was afterwards reported from the Judith 

River beds. It may be regarded as a genus based on insufficient material, and so poorly defined as to be indeterminable.

CIONODON STENOPSIS Cope. 

Cionodon stenopsis Cope, 1875, Proc. Acad. Nat. Sci. Philadelphia, 1875, p. 9.

This species is based on a maxillary and teeth from the Judith 

River beds near Milk River in Canada. According to Cope it is 

distinguished by the absence of a longitudinal keel on the lower part 

of the crown. It is quite probable that the present species is neither 

generically nor specifically distinct from some of the species of Traclwdon mentioned above.

DICLONIUS Cope.

Didonius Cope 1876, Proc. Acad. Nat. Sci. Philadelphia, 1876, p. 253.

This genus and three species D. pentagonus, J). perangulatus, and 

J}. calamarius were proposed by Cope from shed teeth found scattered throughout the Judith River beds of Montana. The genus 

should be, and has Arery generally been, considered as a synonym of 

Trachodon. From Cope's descriptions of the teeth referred by him to 

the various species mentioned above, it seems probable that more than 

one species were represented. In the absence of any figures, and 

considering the nature of the characters ascribed b}7 Cope to the various species, it is doubtful if any of them are at present identifiable 

without access to the. types, and since the latter seern no longer to be 

certainly determinate in the Cope collection, it would not be amiss to 

drop also the specific names referred to this genus.

CONIOENIS ALTUS Marsh.

Coniornis altus Marsh, 1893, Am. Jour. Sci., 3d ser., vol. 45, p. 82.

A single bird has been described from these beds. It was referred 

to the present genus and species. The type consisted of the distal 

portion of a tibia found near the base of the Judith River beds on 

Dog Creek, Montana. According to Marsh, its affinities are with 

Jfesperornis, a genus of toothed birds from the Mobrara chalk of 

Kansas.
100 THE JUDITH KIVER BEDS. [BULL. 257.

MAMMALIA.

Thus far only two species of mammals have been described from 

the Judith River beds. These were referred to tw.o genera, and both 

were described by Lambe from material collected by him in Canada.

PTILODUS PKIMJEVTJS Lambe. 

Ptilodus primzevus Lanibe, 1902, Cont. Canadian Palseont, vol. 3, pt. 2, p. 79, PI. XV.

This species is based on a fragment of a mandible with a first molar 

and fourth premolar in place. It is clearly related to, but somewhat 

more primitive than, Meniscoessus conqmstis Cope" from the Laramie 

of South Dakota.

BOREODON MATTJTINUS Lambe.

Boreodon matutinus Lambe, 1902, Cont. Canadian PaUeont, vol. 3, pt. 2, p. 79, PI. XV.

This species is founded on a single premolar from the Judith River 

beds of Canada, resembling in some respects, the teeth referred by 

Marsh to the genus Stagodon b from the Laramie of Converse County, 

W}7 o. The jaw shown here in fig. 1 was found in the Judith River 

beds on the north side of Milk River, about half a mile below Meili 

Coulee and directly north of the red butte mentioned on page 50. It 

was found in place in a lens of rather hard, cross-bedded sandstone. 

Associated with it were remains of Trachodon and turtles. It is provisionally referred to the present genus and species, although, from 

the absence of any teeth with which to make direct comparison, it is 

impossible to establish their identity.

FIG. 1. Posterior portion of right ramus referred to Boreodon matutinus Lambe. A, external view; 

B, internal; C, posterior; m, masseteric fossa; idf., inferior dental foramen.- Natural size.

The jaw is extremely heavy. While the coronoid process is imperfect, it is sufficiently preserved to show that it was high and .strong. 

The angle was inflected much as in modern marsupials. The masseteric fossa was deep. The inferior dental foramen is placed well back 

and opens far down on the floor of the inflected angle, as shown in 

fig. 1. There is no mylohoid or Meckelian groove. Unfortunately 

no teeth are preserved, though there are a number of alveoli. The 

appearance of these alveoli suggests that there was a last, small, tubercular, single-rooted molar preceded by a double-rooted molar of mod-

«Am. Naturalist, 1882, p. 830. b Am. Jour. Sci., 3d ser., vol. 43,1892, pi. 8, figs. 4, 5.
HATCHER.] VEETEBEATE FAUNA. 101

erate dimensions, while the preceding or first molar, assuming that 

there were three and only three true molars, was the largest of the 

series, as is indicated by its posterior root, which is still in place in the 

alveolus. It is laterally compressed and has the surface marked by 

faint striae similar to those seen on the root of the type of the species, 

though not shown in Lambe's figure. The jaw was broken-through 

the anterior alveolus of this tooth, and that portion of the ramus 

anterior to this is wanting.

SUMMARY.

From the foregoing review of the known vertebrates from the 

Judith River beds it will be seen that, while the fauna is one of considerable diversity, most of the genera and species are at present 

known from such insufficient and fragmentary material that it has not 

been possible hitherto to properly define them. It thus happens that 

a considerable number of genera and species that have been proposed 

for remains from these beds are not now determinable, and owing to 

the scanty material upon which not a few of these were originally 

founded it is quite impossible to refer to these with any degree o.f certainty, subsequently discovered and more perfect material, and thereby 

to further define and describe them. This is true to a greater or lesser 

extent of all 'the Vertebrata of these beds, but it is especially applicable 

to the fishes, amphibians, and by far the larger portion of the reptiles, 

while the birds and mammals of Judith River times are at present 

known from such exceedingly scanty material as of themselves to offer 

almost no evidence of the character of the avian and mammalian life 

of those times. Our knowledge of the vertebrate fauna of these beds, 

'now that their geographic distribution is known not to be so limited 

as had been previously supposed, Avill doubtless be greatly increased 

by more persistent collecting, aided by modern methods. At present, 

however, while we are in many cases unable to adequately define many 

of the genera and species, we know enough of the fauna as a whole to 

form a very good general idea of its character, and although we can 

not compare it closely with the related faunas of other horizons, yet 

enough is known of it to establish certain similarities and dissimilarities. These are especially pronounced in certain groups like the Ceratopsidse and the Trachodontidge, where there was already a high degree 

of specialization and where many of the different species are known 

from fairly satisfactory material.

When considered in its entirety, the vertebrate fauna of these beds 

is remarkably similar to, though distinctly more primitive than, that of 

the Laramie. Almost or quite all of the Laramie types of vertebrates 

are present, though, as a rule, they are represented by smaller and more 

primitive forms. The similarity between this fauna and that of the 

Laramie contrasts strongly with the great dissimilarity between the
10*2 THE JUDITH RIVER BEDS. [BULL. 257.

vertebrates of the Judith River and those of the Atlantosaurus beds, 

the next older fresh-water horizon in this region, containing also a 

rich and varied vertebrate fauna, but quite distinct from that of the 

beds in question.

The Dinosauria were the predominant vertebrates in Judith River 

times, and they, of all the vertebrates of these beds, afford the best 

basis for a comparison of the fauna of these deposits with that of the 

.Laramie above and the Jurassic below. The great group of Sauropoda, which formed so conspicuous a feature of the animal life at 

the close of the Jurassic and the beginning of the Cretaceous, is 

entirely wanting. Among the Predentata the Stegosauria, which had 

formed so striking a feature among the Jurassic dinosaurs, have 

almost or quite disappeared and are replaced entirely by the quadrupedal Ceratopsidse and the bipedal Trachodontidas. No unmistakable 

repesentative of the Stegosauria is certainly known from the Judith 

Riverbeds. Palseoscincus, referred to this suborder chiefly on the evidence of teeth alone, may or may not pertain to the Stegosauria; while 

Stereocephalus appears to have been founded on material belonging 

in part to the Crocodilia and in part to the Dinosauria. No evidence 

has as yet been produced to show that the large pointed shields 

described and figured by Lambe as pertaining to this genus may not 

have belonged to some member of the Theropoda or to the Ceratopsidse. That they really belonged to one or the other of these is most 

likely, since very similar plates have been met with in the Laramie 

also. No vertebrae or shield plates like those known to have belonged 

to Stegosa-urus are known from the Judith River beds.

The Trachodontidse had already attained to considerable diversity 

in Judith River times. Indeed, they appear to have been more abun-' 

dant, as regards both numbers of individuals and genera and species,

than they were in the Laramie. Judging- from the rather meager 

material at hand for comparison they were, however, somewhat-less 

specialized, as is evidenced by such characters as the presence of four 

digits in the pes of Pteropely% and the complement of teeth, which in 

the later Laramie forms seems to have been considerably greater than 

in the Judith River.

It is in the Ceratopsidse more than in any other group that we are 

at present-able to contrast the Judith River and Laramie forms. The 

chief differences are noticeable in the skull, and more especially in the 

structure of the parietal crest and the comparative size of the supraorbital and frontal horn cores. In the Laramie the supraorbital horn 

cores are always much larger than the nasal and the latter are frequently rudimentary, while in the Judith River beds conditions just 

the reverse prevail. In the Laramie the huge parietal fontanelles so 

common in the forms from the Judith River beds are known only in 

the single rare genus Torosaurus. There is some evidence also that 

the teeth in some of the Judith River forms are only in the process of
HATCHER.] VERTEBRATE FAUNA. 103

assuming that method of replacement which is common in later representatives of the group, and by means of which the single root of the 

embryo tooth early becomes bifurcated. The primitive nature of the 

Judith River Ceratopsidai, as compared with the Laramie, is especially 

seen in the smaller size of the individuals, the less perfectly developed 

armature of the skull, and the imperfectly developed parietal crest.

So little is at present actually known of the Theropoda of either the 

Laramie or the Judith River beds that it is quite impossible to make 

anything like an adequate comparison between them. The group, 

however, is represented in both formations by quite similar forms, 

though differing perhaps both generically and specifically. The 

Theropoda in the Judith River beds show much greater diversity than 

do those of the Jurassic, and judging from the remains available they 

represent quite different types.

Although much is desired in the way of better material before we 

shall be able to determine, even approximately, the character of the 

vertebrate fauna of the Judith River beds, enough is already known 

to suggest its diversity and to show that the fauna is similar to that 

of the Laramie and different from that of the Jurassic. The long 

period of time which had elapsed between the close of the deposition 

of the Atlantosaurus beds and the beginning of the Judith River was 

sufficient to accomplish a complete revolution in the vertebrate fauna 

of that region, though most of the later forms are clearly descended 

from the earlier. Scarcely a single vertebrate of strictly Jurassic type 

is found in this fauna, for, as mentioned above, Stereocephalus Lauibe, 

referred by that author and by Osborn to the Stegosauria, appears to 

have been founded on a composite type containing remains pertaining 

both to the Crocodilia and to the Dinosauria. The Dinosauria are not 

distinguishable from remains from the Laramie at present referred to 

the Ceratopsia, and the Crocodilia represent a group of crocodiles at 

present only known from the Judith River beds.

Briefly, the Judith River fauna, it is clear, is descended from the Jurassic and is the direct ancestor of the Laramie. Its relations with the 

former are not close, and several groups are absent in the one which 

are present in the other. Its relations with the Laramie are much 

closer, as should be expected, considering the stratigraphic position. 

With one or two possible exceptions all the families represented in 

either of these two later deposits are- present also in the other. 

Although several genera and species now appear to be common to 

both these formations, it is probable that when more perfect material 

is available they will be found, in most instances, to be quite distinct, 

though some pertaining to more persistent types may prove to be 

identical. In every case where any group of the fauna has been 

studied from sufficient material it has been found to be represented 

.by distinctly older and more primitive types than the related forms 

from the Laramie.
INVERTEBRATE FAUNA.

By T. W..STANTON.

The invertebrate fossils of the Judith Kiver beds have nearly all 

been adequately described and illustrated by Meek,ff White,5 and 

Whiteaves c in previous publications. For the present purpose, therefore, it will be sufficient to describe and illustrate a few new species 

and to give an annotated list of the others, with references to good 

figures. The systematic list will be followed by a brief discussion of 

the character and relationships of the fauna and of the evidence it 

affords as to the conditions under which the formation was deposited.

OSTBEA SUBTRIGONALIS Evans and Shumard.

Ostrea sublrigonalis Meek, 1876, Kept. U. S. Geol. Surv. Terr., vol. 9, p. 510, PI. XL, 

figs. la-Id.

The species was originally described from the vicinity of Owl Butte, 

between Grand and Moreau rivers, South Dakota, from beds that are 

now supposed to belong to the Laramie. From the fact that the types 

have never been figured and that no one has since studied them or 

other material from the type area, it may be questionable whether the 

Judith River form which Meek described under the same name is 

really identical. Whatever the final decision on that point may be, 

the form, figured by Meek is the most abundant and widely distributed 

of the Judith River invertebrates. In the exposures near the Missouri 

on Dog Creek, Birch Creek, and Cow Creek there is a bed from 1 to 2 

feet in thickness, at or very near the top of the formation, almost 

entirely composed of the shells of this species, with local accumulations 

of Corbicula cytheriformis, and less 'abundant specimens of Corbulo, 

siibtrigonalis, Anomia gryphorkynchus, and Goniobasis convexa. The

"Invertebrate Cretaceous and Tertiary fossils of the tipper Missouri country: Kept. U. S. Geol. Surv. 

Terr., vol. 9, 1870, pp. 509-592, pis. 42-43.

b Review of the nonmarine fossil Mollusca of North America: Third Ann. Kept. U. S. Geol. Survey, 

. 1883, pp. 411-550.

c Report on the Invertebrata of the Laramie and Cretaceous rocks of the vicinity of the Bow and 

Belly rivers and adjacent localities in the Northwest Territory: Cont. Canadian Palteont., vol. 1, 

pt. 1, 1885. The Belly River [Judith River] species are described on pp. 55-77.

104
STANTON.] INVEETEBBATE FAUNA. 105

same brackish-water fauna has a similar development at this upper 

horizon on Milk River in the neighborhood of Havre, especially near 

the mouth of Beaver Creek, 2 to 3 miles west of Havre, and at the 

head of Supenaw Coulee, on the north side of the river, 5 or 6 miles 

farther west. Ostrea subtrigonalis is reported by Whit eaves from 

about the same horizon at the mouth of St. Mary River and in Milk 

River Ridge, Canada, where the bed is referred to the " base of the 

shales of the Fort Pierre group."

Ostrea subtrigonalis also occurs in the upper part of the Claggett 

formation, on the north side of Milk River 4 miles west of Havre, 

Mont., and near Pendant d'Oreille, Canada, at both places associated 

with 0. glcibra, with which it seems to be connected by intermediate 

forms. It is reported from the lower Laramie and from the " Belly 

River " beds at several localities in Alberta and Assiniboia.

OSTREA GLABRA Meek and Hayden,

Ostrea glabra Meek, 1876, Kept. U. S. Geol. Surv. Terr., vol. 9, p.509, PL XL, figs.

2a-2d. 

Oslrea fjlabra White, 1883, Third Ann. Kept. U. S. Geol. Survey, p. 421, Pis. IX-XI.

The types of the species came from near the mouth of Judith River, 

but whether they occurred there in the Judith River beds or in the 

Claggett formation is not certainly known. In the present collection 

it was obtained from the upper part of the Claggett formation on Milk 

River 4 miles west of Havre, Mont., and in the neighborhood of Pendant d'Oreille, Assiniboia, and at the latter locality in the basal beds 

of the Judith River. Whiteaves reports it from several localities in the 

Canadian "Belly River" beds. It is also a very common species of 

the Laramie at many localities in the United States as well as in 

Canada, and apparently the same species occurs at several horizons in 

the Montana group.

ANOMIA GRYPHOBHYHCHUS Meek.

Anomia gryphorhynchus White, 1883, Third Ann. Kept. U. S. Geol. Survey, p. 422, 

PL XII, fags. 12-15.

The original locality is Point of Rocks, Wyoming, where the species 

occurs in a horizon now known to be in the Montana group, and probably not far from the horizon of the Judith River beds. It has also 

been recognized at Black Buttes, Wyoming; Crow Creek, Colorado, 

and various other localities in the Laramie. The species is not uncommon associated with Ostrea subtrigonalis near the top of the Judith 

River beds on Cow Creek, and near Havre, Mont., and at the base of 

the same formation or in the upper layers of the Claggett near Pendant d'Oreille, Assiniboia. It shows considerable variation in size and 

in the convexity of the upper valve.
106 - THE JUDITH EIVER BEDS. [Bui.i-.257.

ANOMIA MICRONEMA Meek.

Anemia micronema White, 1883, Third Ann. Rept. II. S. Geol. Survey, p. 422, PI. XII,

figs. 6-11. 

Anomia micronema Whiteaves, 1885, Cont. Canadian Palseont., vol. 1, p. 64.

This common Laramie species has been reported by Whiteaves from 

the Belly River beds of South Saskatchewan, half a mile below the 

forks of Bow and Belly rivers.

AVICULA NEBRASCANA Evans and Shumard.

Pteria (Oxytoma) nebrascana Meek, 1876, Rept. U. S. Geol. Surv. Terr., vol. 9, p. 34,

PL XVI, figs. 5a, 5b, and PI. XXVIII, fig. 11. 

Pteria (Oxytoma) nebrascana Whiteaves, 1885, Cont. Canadian Pakeont., vol. 1, p. 56.

Whiteaves reports this species from the "Belly River" beds in Milk 

River Ridge, Alberta. It is a common form in both the Claggett and 

the Bearpaw formations, and may therefore be expected in the Judith 

River beds wherever a marine stratum occurs.

MYTILUS SUBAECUATTTS Meek and Hayden.

Mytilus subarcuatus Meek; 1876, Rept. U. S. Geol. Surv. Terr., vol. 9, p. 69, PI

XXXVIII, figs. 2a, 2b. 

Mytilus subarcuatus Whiteaves, 1885, Cont. Canadian Pakeont., vol. 1, p. 56.

The typ& is from Dog Creek, Montana, probably in the Claggett formation. Whiteaves reports it from the "BellyRiver" beds on South 

Saskatchewan River 8 miles below Red Deer River, and our collections 

contain a single specimen doubtfully referred to the species from the 

top of the Judith River beds in Meili Coulee, 4 miles west of Havre, 

Mont.

MODIOLA sp.

Fragments of a species with rather coarse radiating sculpture were 

collected from the lower part of the formation on Milk River, near

Pendant d'Oreille, Assiniboia, and from the upper brackish-water bed

on Cow Creek, Montana, 13 miles above its mouth.

CRENELLA PARVTJLA Whiteaves.

Orenellaparuula Whiteaves, 1885, Cont. Canadian Palseont., vol. l,p. 57, PI. IX, fig. 1. 

This species is known only from strata referred to the "Belly 

River" beds in Milk River Ridge, Alberta.

NUCTTLA sp.

Imperfect specimens of an undetermined species of Nucula were 

seen in a bed of friable sandstone containing other marine fossils on 

Cow Creek, Montana, about 7 miles above its mouth. The horizon is 

about 150 feet below the top of the Judith River beds.

IEDA sp.

An imperfect specimen of a large species, probably undescribed, was 

collected on Cow Creek at the locality and horizon last mentioned.
STANTON.] INVERTEBRATE FAUJSTA. 107 

ANODONTA PKOPATOEIS White.

Anodonta propatoris White, 1883, Third Ann. Kept. U. S. Geol. Survey, p. 429, PI:

'XIX, figs. 6-9.

The types are from Judith River beds on Dog Creek and Birch 

Creek, Montana. This species is represented in our collections ,froni 

the neighborhood of the original localities and also from Cow Creek, 

Willow Creek, and near Havre, Mont., and somewhat doubtfully from 

Sage Creek, Assiniboia." Whiteaves reports the species, with some 

doubt as to identification, from many Canadian localities. It seems to 

be confined to the Judith River beds, and ranges throughout the whole 

formation except the brackish-water and marine layers. It is usually 

preserved in the form of casts and no perfect specimens are known.

ANODONTA PARALLELA White?

Anodonta parallela White, 1883, Third Ann. Kept. U. S. Geol Survey, p. 429, PI. XIX,

fig. 5.

Whiteaves has reported one doubtful specimen of this Laramie species from the "Belly River" beds on the South Saskatchewan 1 mile 

below the mouth of Bow River.

UNIO STTBSPATULATUS Meek and Hayden. 

PL XIII, fig. 1.

Unio subspatulatus Meek, 1876, Kept. U. S. Geol. Surv. Terr., vol. 9, p. 518, PI. XLI,

figs, la, 16.

The type from near the mouth of Judith River has the outer surface exfoliated so that the beak sculpture is not retained and the beaks 

are made to appear some what nearer the anterior end than they actually 

are. On Milk River 2 miles below Pendant cVOreille, Assiniboia, Mr. 

Hatcher collected many well-preserved specimens of a Unio that seems 

to be referable to this species from a stratum containing Corbula, Oorl)icula, and Modiola, near the base of the Judith River beds. Some 

imperfect specimens were collected at the mouth of Meili Coulee, on 

the north side of Milk River 4 miles west of Havre, Mont.

It is a rather slender, compressed shell, with nearly terminal, inconspicuous beaks and narrowed posterior end. The umbonal region is 

marked by a few distinct, undulating, concentric ridges, and the posterior umbonal slope bears two sharply elevated radiating lines that 

fade out about an inch from the beak. The shell is rather thin, and 

the teeth are correspondingly light.

Similar beak sculpture is found in several Cretaceous species of 

Unio, such as U. vetustus, U. prisons, etc., but the general form and 

proportions of the shell are different. It is a much lighter, less convex shell, with more nearly terminal beaks than Unio danse, and U. 

deweyanus, with which it has sometimes been supposed to be identical.
108 THE JUDITH. BIVER BEDS. [BULL.257. 

UNIO PRISCUS Meek and Hayden! 

PI. XII, fig 1.

Unio priscus Meek, 1876, Kept. U. S. Geol. Surv. Terr., vol. 9, p. 516, PL XLIII, 

figs. 8a-8d.

The type of this species is from the Yellowstone, 40 miles above its 

mouth, and presumably from beds of Laramie age. Meek also figured 

small specimens from Judith Elver, but it is somewhat doubtful 

whether they are really identical with the Yellowstone form which is 

represented in the National Museum collection by the single crushed 

specimen. All the specimens have an elongate form and beaks with 

strong concentric wrinkles, but those from Judith River and from the 

same formation on Milk River at Pendant d'Oreille, Assiniboia, and 

at a locality 5 miles south of Wild Horse Lake, on the Canadian boundary, have the posterior end somewhat broader and other slight differences in outline that may have specific or varietal importance. The 

specimen figured is from the locality last named.

UNIO PEISCTJS var. ABBREVIATES n. var. 

PI. XII, figs. 2-4.

This variety has the general aspect and sculpture of U. priscus, with 

the strong concentric wrinkles on the beaks and two elevated radiating 

lines on the posterior urnbonal slope, but it differs in having the posterior end relatively much shorter and somewhat broader, and it is 

apparently somewhat more convex. The shell is rather thin and th.e 

hinge teeth are light. The specimens figured are from Milk River, 

about 5 miles south of Wild Horse Lake.

UNIO DAN2E Meek and Hayden.

IMo dan% Meek, 1876, Kept. U. S. Geol. Surv. Terr., vol. 9, p. 517, PL XLI, figs.

3a-3c. 

Unio deweyanus Meek, 1876, Kept. U. S. Geol. Surv. Terr., vol 9, p. 519, PL XLI,

figs. 2a-2c.

The specimens described under the two names cited above all came 

from near Judith, Mont., and the differences on which the two species 

are based are d,ue to the state of preservation rather than actual specific characteristics. None of the types shows all of the specific features fully, but those of IL danae give a better idea of the outline and 

general proportions, while those of U. deioeyanus show part of the 

surface and details of the hinge, though giving an erroneous impression 

concerning the form. Our collections contain many specimens evidentl}7 belonging to one species, some of rwhich agree with one of 

these types and some with the other. The species attains a much 

larger size than the types, and apparently Meek was right in describing the beaks as unsculptured, in this respect differing from the form
STANTON.] INVERTEBRATE FAUNA. 109

which I have identified with Unib subspatulatus. We collected it on 

Sage Creek, Assiniboia; on Milk River, near Havre; on Cow Creek, 

Dog Creek, and at other localities in the original Judith River area. 

Apparently the same species, or if not, a closely related one that can 

not be separated with the imperfect material at hand, occurs in the 

Laramie at Black Buttes and on Lance Creek, Wyoming, near the 

mouth of the Yellowstone, and elsewhere in Montana. It has also been 

reported from the Laramie of Alberta.

T7NIO SUPENAWENSIS n. sp. 

PI. XIII, figs. 2 and 3.

Shell of medium size, obliquely subovate in outline, with relatively 

thick test and broad hinge plate; beaks very prominent, slightly 

incurved, very near the anterior end of the shell, and sculptured with 

distinct concentric wrinkles; the rest of the surface showing only 

ordinar}^ lines of growth and very faint radiating stride, which probably 

are not visible except when the actual surface is slightly exfoliated; 

dorsal and basal margins forming very gentle regular curves; anterior 

margin slightly excavated above in front of the beak and broadly 

rounded below; posterior end somewhat narrowly rounded; shell very 

gently convex in the umbonal and median portions, but abruptly 

descending toward the front and dorsal margins; cardinal teeth large, 

very irregular in form, and strongly corrugated; posterior lateral well 

developed, elongate.

Length of type, about 65 mm; height, about 55 mm; convexity of 

single valve, 22 mm.

The only Cretaceous species at all resembling this are Unio propheticus White and U. proavitus White, both of which were described 

from the Laramie at Black Buttes, Wyoming, and may well be considered as descendants of U. supenawensis. The resemblance is closer 

with U. propheticus, which is slightly smaller, with beaks nearer the 

anterior end, a more distinctly flattened band extending from the beak 

to the middle of the basal margin, more broadly rounded posterior 

end, and straighter basal margin.

Locality. The types were found near the top of the Judith River 

beds at the head of Supenaw Coulee, about 10 miles northwest of 

Havre, Mont, where the species is common.. Another specimen was 

obtained from near the same horizon on the north side of Milk River 

opposite Havre.

UNIO CEYPTQBHYNCHUS White.

Unio cryptorhynchus White, 1883, Third Ann. Kept. U. S. Geol. Survey, p. 431, PI. 

XIV, figs. 6, 7.

The types are from Dog Creek, Montana, and the species has been 

doubtfully identified in the Laramie at Black Buttes, Wyoming.
110 THE JUDITH BIVER BEDS. [BULL. 257.

TTNIO SENECTUS White.

Unio senectus White, 1883, Third Ann. Rept. U. S. Geol. Survey, p. 432, PI. XIX, 

figs. 1, 2.

From Dog Creek, Montana, and also reported by Whiteaves from 

the South Saskatchewan near the mouth of Bow River.

TTNIO PRIMAEVUS White.

Unio primaevus White, 1883, Third Ann. Eept. U. S. Geol. Survey, p. 432, PI. XIV, 

figs. 4, 5.

From Judith River beds near Cow Island, Montana. Also reported 

by Whiteaves from branch of east fork of Milk River, near the 

Canadian boundaiy. It occurs in our collections from Cow Creek 

and from Milk River 5 miles south of Wild Horse Lake.

Some of the specimens apparently belonging to this species are very 

much larger and more elongate than the type. It is probable that 

the two specimens figured by White represent two species, and if so, 

the smaller one, whose outer surface is figured, should be considered 

the type. The exterior of the other specimen is in a very poor state 

of preservation, so that its specific characters are not clearly determinable. It may possibly be the same as U. prisons var.. abbr&oiatus, 

described above.

UNIO CONSUETUS Whiteaves.

Unio consuetus Whiteaves, 1885, Cont. Canadian Palseont., vol. 1, p. 59, PI. IX, 

figs. 4, 4a.

Described from the "Belly River" beds of Alberta. Somewhat 

doubtfully identified in our collections from the Judith River beds at 

Willow Creek, Montana.

UNIO SUPKAGIBBOSUS Whiteaves.

Unio supragibbosus Whiteaves, 1885, Cont. Canadian Palteont., vol. 1, p. 66, PI. X, 

fig. 1.

Types from South Saskatchewan near mouth of Bow River. Represented in our collection from lower part of Judith River beds on 

Milk River 2 miles below Pendant d'Oreille, Assiniboia, associated 

with U. s'ubspatulatus.

UNIO sp.

There are several other species of Unio represented in ou;* collections by material too imperfect for satisfactory specific description. 

It is therefore thought better to await more complete collections. 

Several of the species already described, from the formation, are so 

imperfectly known that it is almost impossible to identify them, even 

by direct comparison with the types.
STANTON.] INVEBTEBKATE FAUNA. Ill

SPH.ERITJM FLANTTM Meek and Hayden.

Sphserium pfanum, Meek, 1876, Kept. U. S. Geol. Surv. Terr., vol. 9, p. 526, PI. XLIII, 

figs. 6«, 66.

This is one of the most common of the Judith River 'fresh-water 

species, occurring at many localities in the original area on Dog Creek, 

.Birch Creek, and Cow Creek, and on Milk River from Havre to the 

Canadian boundary. . The types came from near Grand Island, on the 

Missouri, below the mouth of Cow Creek, but they were at first erroneously reported to have come from near Grand River, Nebraska. The 

species attains a size considerably larger than the figured type. A 

similar but not identical form occurs in the Laramie of Converse 

County, Wyo.

SPHJERIUM RECTICARDINALE Meek and Hayden.

Sp'hivrium redicardinale Meek, 1876, Kept. U. S. Geol. Surv. Terr., vol. 9, p. 527, PI. 

XLIII, figs. 3d, 36.

' The types are from the same locality as the preceding, and the 

species, though not so abundant, also occurs sparingly at nearly all 

the localities where /S. planum is found. Large specimens are nearly 

half an inch in length.

SPHJERITJM FORMOSTTM Meek and Hayden J

Sphivrium formosum? Whiteaves, 1885, Cont. Canadian Pakeont., vol. i, pp. 6.1. and 68, 

PI. IX, fig. 3.

This form, from the Judith River beds of Alberta, is doubtfully 

referred to /£ formosum, which was originally described from Laramie 

or Fort Union beds near the mouth of the Yellowstone. The Canadian shell may possibly be the young of one of the preceding species.

CORBICULA OCCIDENTALS Meek and Hayden.

Corbicula occidental-is Meek, 1876, Kept. U. S. Geol. Surv. Terr., vol. 9, p. 521, PI. 

XL, figs. 6a-6c.

This form originally described from the badlands of the Judith,'is 

less abundant there than C. cytheriformis, with which it is associated, 

but on Milk River near Pendant d'Oreille, Assiniboia, it is very common near the base of the Judith River beds, where it is associated 

with specimens.that are intermediate in character between these two 

nominal species. It was collected on Cow Creek and near the mouth 

of Birch Creek, Montana, and forms that are apparently not specifically separable occur in the Laramie of "Wyoming and northwestern 

Colorado, as well as the " Western Laramie" of Canada.

CORBICULA CYTHERIFORMIS Meek and Hayden.

Corbicula cytlwriformis Meek, 1876, Kept. II. S. Geol. Surv. Terr., vol. 9, p. 520, 

PI. XL, figs. 5a-5e.

The remarks on the range and distribution of C, occidentalis apply 

to this form also, It is locally very abundant in the brackish-water
112 THE JUDITH RIVEK BEDS. [BULL. 257.

bed at the top of the Judith River on Cow Creek and near the mouth 

of Birch Creek, and it also occurs on Milk River 3 miles west of 

Havre. Forms that have been referred to the same species occur in 

, the Montana group at Point of Rocks, Wyoming, and in the Laramie 

at Black Buttes, Wyoming, and at various points in Wyoming and 

Colorado, as well as in Alberta. The type of Corbicula represented, 

by this and the preceding species may be said to range throughout the 

Upper Cretaceous, as similar forms are found in the Colorado group 

in Utah and in the Bear River formation in Wyoming.

TELLINA sp.

A single specimen of a medium sized Tellina was obtained from the 

marine stratum 150 feet below the top of the Judith River beds on 

Cow Creek, Montana, 7 miles above its mouth.

PANOP.ZEA SIMTJLATRIX Whiteaves.

Panopcea simulatrix Whiteaves, 1885, Cont. Canadian Palseont., vol. 1, p. 11, PI. II. 

fig. 2, 2a.

The types are reported from several localities in the "Western 

Laramie" area of Canada, but it is possible that some of those localities, if not all, are in the Judith River beds. We collected the species 

on Milk River 3 miles west of Havre, and on Cow Creek 13 miles 

above its mouth. In both cases it was associated with the brackishwater forms at the top of the formation.

LIOPISTHA (CYMELLA) TINDATA Meek and Hayden.

Liopistha (Cymella) undata Meek, 1876, Kept. U. S. Geol. Surv. Terr., vol. 9, p. 236, 

PI. XXXIX, figs. Id, 16.

Originally described from beds now known to belong to the Claggett 

formation near the mouth of the Judith, the species is also of common 

occurrence in the Bearpaw.shales, and it was found in the marine 

stratum 150 feet below the top of the Judith River beds on Cow Creek 

7 miles above its mouth.

MACTKA WARRENANA Meek and Hayden?

Mactra (Cymbophora) warrenana Meek, 1876, Kept. U. S. Geol. Surv. Ten?, vol. 9, 

p. 208, PL XXX, figs. la-Id.

A single specimen from the locality and horizon last mentioned is 

doubtfully referred to this Fox Hill species.

MACTRA (CYMBOPHORA) ALT A Meek and Hayden.

Mactra (Oymbophora) alta Meek, 1876, Kept. U. S. Geol. Surv. Terr., vol. 9, p. 210, 

PL XXXVII, figs. 2«, 26; Whiteaves, 1885, Cont. Canadian Paljsont., vol. 1, p. 62.

Whiteaves reports this species from the Judith River beds in the 

Milk River Ridge, Alberta. The occurrence may be in a local marine 

facies of the formation like that mentioned on Cow Creek, or it may 

be in the top of the Eagle formation, where it normally occurs.
STANTON.] INVEKTEBKATE FAUNA. 113

CORBTTLA SUBTBIGONALIS Meek and Hayden.

Corbula subtrigonalis Meek, 1876, Kept. U. S. Geol, Snrv. Terr., vol. 9, p. 529, PL 

XL, figs. 3a, 36.

This species was first described from the brackish-water bed at the 

top of the Judith River formation in the typical area. It has since 

been recognized at man}7" localities in the Western States and Canada, 

from the Benton- formation to the Laramie. In our collections it was 

found most abundantly in the lower gart of the Judith River near 

Pendant d'Oreille, Assiniboia, but it occurs sparingly wherever the 

brackish-water strata are found.

At the locality on Cow Creek, 13 miles above its mouth, a greatly 

elongated variety occurs with the typical form.

CORBULA PERUNDATA Meek and Hayden.

Corbula perundata Meek, 1876, Kept. U. S. Geol. Surv. Terr., vol. 9, p. 528, PI. XL,

figs. 4a-4d.

Originally described from the same locality as the preceding, it also 

occurs with it at many localities on Milk River from Havre, Mont., to 

Pendant d'Oreille, Assiniboia, and elsewhere in that territory and 

Alberta.

GASTEROPODA.

NEBITINA sp.

Velatetla baptista (White) Whiteaves, 1885, Cont. Canadian Palaeont., vol. 1, p. 73. 

Not Neritina (Velatella) baptista White, 1880, Twelfth Ann. Kept.' U.'S. Geol. and 

Geog. Surv. Terr., p. 89, PL XXIX, figs. 6a, Qb.

Specimens from Milk River near Pendant d'Oreille, in the neighborhood of some of Whiteaves's localities, on direct comparison with the 

types of Neritina baptista from the Laramie at Black Buttes, Wyoming, prove to be different in both form and color pattern, but the 

material in hand is not sufficient for specific description.

LUNATIA sp.

A small specimen of an undetermined species was collected with the 

other marine fossils 150 feet below the top of the Judith River formation on Cow Creek 7 miles above its mouth.

VIVIPARUS CONKADI Meek and Hayden.

Viviparus conradi Meek, 1876, Kept. U. S. Geol. Surv. Terr., vol. 9, p. 597, PL XLII, 

figs. 15a-15d.

This species was originally described f rom near the mouth of Judith 

River. We found it locally abundant near the top of the Judith 

River formation on Cow Creek, and Whiteaves reports it from a number of localities in Canada. It has been erroneously reported to occur 

in the Bear River formation.

Bull. 257 05 8
114 THE JUDITH EIVEE BEDS. [BULL. 257.

VIVIPARUS sp.

Imperfect specimens representing at least two or three species were 

found at a number of localities on the Missouri and on Milk River, but 

they were too much distorted and crushed for specific description. 

These forms seem to be closely allied to Laramie species, but apparently not identical with them.

CAMPELOMA VETULA Meek and Hayden.

Campdoma velula Meek, 1876, Eept. U. S. Geol. Surv. Terr., vol.9, p. 587, PI. XLIV, 

figs. 14o, 146.

Described from the Judith River, area. We found it most abundant 

and beautifully preserved in the upper part of the Judith River formation near the head of Supenaw Coulee, about 10 miles northwest of 

Havre. The specimens obtained here are clearly referable to C.vetula, 

though they are also very much like the typical form of G. multiiineata from the Laramie. The slight differences pointed out by Meek 

hold good, except that some of our specimens are slightly unbilicated, 

and these differences are probably of specific importance in spite of 

the fact that specimens not in a good state of preservation may be 

difficult to classify. The common Laramie form of G..multilineata 

with shouldered whorls is very distinct. The Laramie specimens 

from Black Buttes, Wj^oming, and elsewhere, that have been referred 

to G. vetula, so far as I have been able to reexamine them, are too 

imperfect for positive identification, and may well belong to G. 

multilineqta.

At.least a part of the specimens from the Canadian Judith River 

beds referred to G. multilineata by Whiteaves probably belong to G. 

vetula.

CAMPELOMA MULTILINEATA Meek and Hayden.

Campdoma multilineata Whiteaves, 1885, Cont. Canadian PaUeont, vol. 1, p. 77.

See remarks under C. vetula, above. No specimens referable to this 

species have been found in the Judith River beds of Montana, but it is 

one of the most common Laramie species, ranging probably as high as 

the Fort Union.

CAMPELOMA PKODUCTA White.

Campelomaproducta White, 1883, Third Ann. Kept, U. S. Geol. Surv., p. 469, PI. 

XXVI, figs. 21-27; Whiteaves, 1885, Cont. Canadian Pakeont., vol. 4, pp. 24, 28, 77.

This is also a Laramie species that has not been found in the Judith 

River beds of the United States, but has been reported by Whiteaves 

from both the Laramie and the Judith River of Canada.
STANTON.] ' INVERTEBRATE FAUNA. 115 

VALVATA? MONTANAENSIS Meek.

Valvata? montanaensis Meek, 1876, Kept. U. S. Geol. Snrv. Terr., vol. 9, p. 591, text 

figs. 81-83.

Described from mouth of Judith River. Represented in our collections from two localities on Cow Creek.

HYDROBIA ST7BCONICA Meek.

Hydrobia subconica Meek, 1876, Kept. U. S. Geol. Surv. Terr., vol. 9, p. 573, text 

. fig. 77.

Moiith of Judith River.

HYDROBIA SUBCYLINDRACEA Whiteaves. .

Hydrobia subcylindracca Whiteaves, 1885, Cont.-Canadian Pakeont., vol. 1, p. 75, PI. 

X, fig. 8.

Type from Belly River east of Driftwood Bend. WhiteaVGS also 

reports the species from Milk River near Pakowki Coul6e, and we 

collected it at Pendant d'Oreille, near the latter locality, where it was 

associated with Corbula subtrigonalis, C. perundata, and Hhytophorus 

glaber, near the base of the Judith River beds.

MELANIA] WHITEAVESI n. sp. 

PI. XIII, fig. 5.

Melania insculpla (Meek) AVhiteaves, 1885, Cont. Canadian Palseont., vol. 1, p. 73, PI.

X, fig. 6. 

Not Melania insculpla Meek, 1873, Sixth Ann. Eept. U. S. Geol. Surv. Terr., p. 515.

Shell of moderate size and rather robust form; whorls moderately 

convex, with the suture between them deeply impressed; surface 

marked by rather narrow, elevated, revolving striae, of which about six 

are visible on the spire, and by broader, more distant, curved ribs, 

which are more or less nodose at the intersections with the revolving 

lines. There are fifteen ribs on the last whorl of the specimen figured, 

which is considerably more strongly sculptured than the average. 

 Height, with apex restored, about 40 mm.; breadth, 13 mm.

The specimens studied show much variation in the strength of the 

sculpture, with every gradation from the nearly smooth forms like that 

figured by Whiteaves to the one illustrated here. The species differs 

from M. insculpta in the form of the whorls and in all the details 

of sculpture, both the ribs arid the spiral lines being more distant and 

less regular.

Some of the more strongly sculptured specimens of Goniobasis convexa 

M. & H. approach this form rather closely, and it is probable that they 

are related. Both are always found associated with brackish-water or 

marine species. The figured specimen of M. whiteavesi was obtained 

from near the base of the Judith River beds on Milk River 6 miles
116 THE JUDITH KIVEE BEDS. [BULL.257.

below Pendant d'Oreille, Assiniboia, and it was collected at several other 

localities near there, at one point ranging down into the top of the Clag - 

gett formation. Whiteaves reports it (under the name M. insculpta) 

from the same neighborhood, but his figured specimen is from the' 

South Saskatchewan 6 miles below the mouth of Bow River.

GONIOBASIS CONVEXA Meek and Hayden.

Goniobasis convexa Meek, 1876, Kept. U. S. Geol. Surv. Terr., vol. 9, p. 562, text figs. 

71, 72, and PI. XLII, figs. 2a, 26.

Described from mouth of Judith Eiver. Represented in our collections from Milk River near Havre, associated with Ostrea, Anomia, 

and other brackish-water forms at the top of the Judith River beds.

GONIOBASIS CONVEXA var. IMPRESSA Meek and Hayden.

Goniobasis convexa var. impressa Meek, 1876, Kept. U. S. Geol. Surv. Terr., vol. 9, p. 

563, PI. XLII, figs. 2c, 2d.

Occurs with the preceding at the type locality and in the brackishwater bed at the top of the formation on Cow Creek.

GONIOBASIS SUBLJEVIS Meek and Hayden.

Goniobasis sublsevis Meek, 1876, Kept. U. S. Geol. Surv. Terr., vol. 9, p. 567, PI. XLII, 

figs. 5a, 56.

Types from the fresh-water beds near the mouth of Judith River. 

Common on Cow Creek and Willow Creek, and along Milk River 

from Havre, Mont., to the Canadian boundary.

GONIOBASIS INVENTTSTA Meek and Hayden.

Goniobasis invenusla Meek, 1876, Kept. U. S. Geol. Surv. Terr., vol. 9, p. 564, PI. XLII, 

figs, la-le.

Occurs with the preceding and is somewhat more abundant, being 

found at most localities where fresh-water fossils occur in the Judith 

River beds, as far north as Pendant d'Oreille, Assiniboia.

GONIOBASIS GRACILENTA Meek.

Goniobasis gracilenla Meek, 1876, Kept. U. S. Geol. Surv. Terr., vol. 9, p. 568, text 

fig. 74,'and PI. XLII, fig. 3.

This species was found at the mouth of Judith River. It has also 

been reported from the Laramie at a number of localities in Wyoming 

and Colorado, but the state of preservation of all these specimens, as 

well as of the types, is such that their specific identity is doubtful.

GONIOBASIS 1 OMITTA Meek and Hayden.

Goniobasis? omitia Meek, 1876, Kept. U. S. Geol. Surv. Terr., vol. 9, p. 568, PI. XLII, 

figs. 4a-4c.

Mouth of Judith River.
STANTON.] INVERTEBEATE FAUNA. 117 

GONIOBASIS 1 SUBTORTUOSA Meek and Hayden.

Goniobasis ? subtortuosa Meek, 1876, Kept. U. S. Geol. Surv. Terr., vol. 9, p. 569, text 

figs. 75, 76, and PL XLII, figs. 17o, 176.

Described from near the mouth of Judith River, this is one of 

the most characteristic of the fresh-water species found in the formation. It has been collected at many localities in the original area, and 

along Milk River above Havre, Mont. Whiteaves reports it also from 

the South Saskatchewan, Bow, and Belly rivers in Alberta.

GONIOBASIS JTTDITHENSIS n. sp. 

PL XIII, fig. 4. .

Shell of moderate size, stout, consisting of seven or eight very convex whorls; aperture very slightly produced below; surface marked 

by narrow, sharply elevated revolving lines, of which four to six are

visible on the spire, separated by broader, flat bands which bear numerous minute revolving striae, and crossed by very fine growth lines.

Height of an average specimen, 22 mm.; breadth, 13 mm.

This species is probably the ancestor of G-o'niobasis tenuicarinata 

M. & PL, from which it differs in being larger, with more robust form, 

and with more narrow, more evenly distributed, and somewhat less 

prominent revolving lines or ridges.

It is common in the fresh-water beds of the Judith River on Dog 

Creek and at other localities near Judith, Mont., on Cow Creek, 

and on Milk River from Havre to the Canadian boundary. The figured specimen is from Simpson's ranch, on Milk River about 10 miles 

south of the boundary. .

RHYTOPHORUS T OLABER Whiteaves.

Rhytophorus? glaber Whiteaves, 1885, Cont. Canadian Palseont., vol. 1, p. 69, PL X, 

figs. 4, 4a-4c.

This peculiar little species, originally reported from a number of 

widely distributed points in Alberta and Assiniboia, we collected only 

from the brackish la}7 ers near the'base of the formation on Milk River 

in the neighborhood of Pendant d'Oreille, Assiniboia.

HELIX VETUSTA Meek and Hayden.

Helix vetusta Meek, 1876, Rept. U. S. Geol. Surv. Terr., vol. 9, p. 552, PL XLII, figs. 

7a, 76.

Mouth of Judith River.

HYALINAT EVANSI Meek and Hayden. 

Hyalina? mmstMeek, 1876, Rept. U. S. Geol. Surv. Terr., vol. 9, p. 548, text figs. 68-70.

Mouftr of Judith River; also in our collections from Cow Creek 

and at various points on Milk River from Havre to the Canadian 

boundary.
118 THE JUDITH EIVEE BEDS. [BOLL.257. 

HYALINA* OCCIDENTALIS Meek and Hayden.

Hyalina? occidentalis Meek, 1876, Kept. U. S. Geol. Surv. Terr., vol. 9, p. 547, PL 

XLII, figs. Qa-6d.

Somewhat more common than the preceding species and with the 

same geographic distribution.

THAUMASTTTS LIMN2EIFORMIS Meek and Hayden.

Thaumastus limnseiformis Meek, 1876, Rept. U. S. Geol. Surv. Terr., vol. 9, p. 553,

PL -XLIV, figs. 8a-8eZ. 

Thaumastus limnseiformis Whiteaves, 1885, Cont. Canadian Palseont., vol. 1, p. 72.

Originally described from Laramie or Fort Union beds near the 

mouth of the Yellowstone, and, so far as known, does not occur in 

lower horizons in the United States. Whiteaves reports the species 

from both the Laramie and the Judith River in Canada.

VITRINA! OBLIQ.UA Meek and Hayden.

Vitrina? obliqua Meek, 1876, Rept. U. S, Geol. Surv. Terr., vol. 9, p. 545, PL XLII, 

figs. 10o, 106. . 

Mouth of Judith River.

PLANORBIS (BATHYOMPHALUS) AMPLEXUS Meek and Hayden.

Planorbis (Bathyomphalus) amplexus Meek, 1876, Rept. U. S. Geol. Surv. Terr., vol. 

9,. p. 539, PL XLII, figs. 16a-16e.

Near mouth of Judith River. Represented in our collections from 

the same region and also from Cow Creek and on Milk River near 

Havre.

PLANORBIS PAUCIVOLVIS Whiteaves.

Planorbis 'paucivolvis Whiteaves, 1885, Cont. Canadian Palseont. vol.. 1, p. 71, PL X, 

fig. 5.

From Judith River localities on Belly River and South Saskatchewan, Alberta.

PHYSA COPEI White.

Physa copei White, 1883, Third Ann. Rept. U. S. Geol. Survey, p. 450, PL XXV, 

figs. 1,2.

Described from Judith River beds near Cow Island, Montana. The 

species is represented in our collections from Cow Creek, Dog Creek, 

and from several localities on Milk River from Havre to the Canadian 

boundary. Whiteaves reports it from many localities in both the 

Judith River and the Laramie of Alberta.

^BTTLINUS SUBELONOATUS Meek and Hayden.

Bulinus subelongatus Meek, 1876, Rept. U. S. Geol. Surv. Terr., vol. 9, p. 540, PL 

XLII, figs. 13a, 136.

Mouth of Judith River.
STANTON.J INVERTEBRATE FAUNA. llO

BULINUS ATAVUS White.

Bulinus atavus White, 1883,.Third Ann. Kept. U. S. Geol. Survey, p. 450, PI. XXV, 

figs. 6, 7.

Described from Dog Creek, Montana. Found also sparingly on 

Milk River near Havre.

CEPHALOPODA.

PLACENTICERAS sp.

Some fragments of a Placenticeras were seen in the marine stratum 

150 feet below the top of the Judith River beds on Cow Creek 7 miles 

above its mouth. Like the other purely marine fossils found here, 

this ammonite does not really belong to the Judith River fauna, but as 

it occurs within the stratigraphic limits of the formation it is worth 3^

of mention.

INSECTA.

Associated with the plants collected on Willow Creek 10 miles north 

of Mucselshell post-office a single wing of an insect was found which 

has been identified \>y the entomologists of the United States National 

Museum as belonging to a cockroach.

GENERAL COMMENTS ON THE INVERTEBRATE FAUNA.

The species enumerated in the above list fall into the three general 

categories of marine, brackish-water, and fresh-water forms, the latter 

including a few more or less doubtful land shells.

As the Judith River is essentially a nonmarine formation, strictly 

speaking its fauna should not be made to include the species cited 

belonging to Avicula, Crenella, Nucula, Leda, Tellina, Liopistha, 

Mactra, Lunatia, and Placenticeras, which were brought into the Judith 

River area by a local, temporary invasion of pure marine waters. In 

our field studies we saw only one occurrence of this kind, and that 

was on Cow Creek, Montana, where, as already described, the evidence 

seems clear that the marine beds are on the same horizon and strictly 

contemporaneous with fresh- and brackish-water beds in the same 

neighborhood. There is no mixture, of nonmarine with the marine 

invertebrates, but in an overlying stratum marine and land vertebrates 

are found commingled. The marine invertebrates found here belong 

to the faunas of the underl}7 ing and overlying formations.

The few marine fossils reported by Whiteaves from the Judith 

River beds in Canada may indicate a similar occurrence there, or possibly there has been an error in identifying the formation from which 

they came. With these exceptions no strictly marine fossils are 

known from the main mass of the Judith River, beds, but at the base
120 THE JUDITH EIVEE BEDS. [BULL. 257.

and the top there is ample evidence of continuity with the underlying and overlying marine formations. In many cases the lithologic 

change is not exactly coincident with the faunal change, so that the 

topmost layers containing the Claggett fauna and the lowest beds containing the Bearpaw fauna often closely resemble the Judith River 

beds in lithologic features.

The brackish-water fauna has a wide geographic distribution, occurring in practically every area in which the Judith River formation is 

found, but it is confined to thin beds intercalated in the upper and 

lower portions of the formation. On Milk River near Pendant 

d'Oreille, southern Assiniboia, these layers with brackish-water shells 

are unusually well developed near the base of the formation, and there 

are several intercalated bands extending up about 100 feet above the 

base. The individual beds are usually not more than 1 or 2 feet in 

thickness and the intervening strata contain fresh-water invertebrates. 

Farther south, near Havre, and in the area along the Missouri, brackishwater bands are seldom found in the lower part of the formation, but 

in the upper 25 feet there is a very persistent oyster bed, varying in 

thickness from 1 to 4 feet, closely associated with a heavy bed of lignite. In some places there are two or three of these brackish-water 

beds close together near the top of the formation. According to the 

Canadian reports, an oyster bed occurs at about this horizon in many 

places in Alberta.

The following species are confined to the brackish-water layers:

Species confined to brackish-water layers of Judith River formation

Ostrea eubtrigonalis.

Ostrea glabra.

Mytilus sp.

Modiola sp.

Anornia gryphorhynchus.

Corbicnla occidentalis.

Corbicula cytheriforrnis.

Corbula perundata. 

Panopsea simulatrix. 

Khytophorus glaber. 

Neritina sp.' 

Melania? whiteavesi.

Goniobasis convexa.

Goniobasis convexa var. impressa.

Corbula subtrigonalis.

The species of Corbula, Corbicula, and a few of the others apparent!}7 

ranged into nearly fresh waters, as they are sometimes found associated 

in the same layer with abundant specimens of Unio and Campeloma, 

while the oyster beds represent more nearly marine qonditions which 

did not permit the mingling of purely fresh-water forms. The three 

forms of gasteropods in this list, doubtfully referred to Melania and 

Goniobasis, occur in the oyster beds. It is noteworthy that the Laramie species, Melania f ^oyomingensis and M.f insculpta, also occur 

with brackish-water fossils, and the former has been found with marine 

associates in the upper layers of the Fox Hills.

By far the most abundant of the brackish-water forms is Ostrea subIrigonalis, which could probably furnish more individual specimens
STANTON.] INVEKTEBKATE FAUNA. 121

than all the rest of the Judith River fauna together. Next to it in 

abundance are the species of Corbula, Oorbicula, and Anomia, but their 

distribution is much more local and irregular. Ostrea glabra and a 

variety intermediate between it and 0. subtrigonalis are locally 

abundant, but the differences between these oysters are chiefly in the 

size, and the relationship between the different forms seems to be 

analogous to that between the local and commercial varieties of Ostrea 

virginica.

The five forms of Gasteropoda enumerated in our brackish-water 

list all appear to be confined to the Judith River beds, and the brackishwater faunule as a whole has a distinctive facies that is not exactly 

duplicated elsewhere, and yet when the comparison is made species 

by species almost all the other forms are represented in the Laramie 

by similar if not identical species, and some of them are represented 

in other formations as low as the Colorado group. In fact, they are 

persistent types that range throughout the Upper Cretaceous, and 

forms similar to some of them exist in the present seas. It is obvious 

that such species can not be safely used singly in correlating over 

great distances, but within limited areas, when comparison is made with 

an entire assemblage of forms and checked by stratigraphlc observations, their evidence is often to be depended upon, and is as convincing as any other paleontologic evidence. When full collections 

are compared it will usually be easy to distinguish between Judith 

River and Laramie from the brackish-water fossils alone, but if the 

collections are meager and fragmentary it may not be practicable to 

do so. This remark is based on experience with the two faunas in the 

United States. Comparing the oysters, in the Laramie the large 

Ostrea glabra is the common form, while in the Judith River 0. subtrigonalis is. by far the most abundant and most widely distributed. 

Corbicula also has a different development in the Laramie, the type 

represented by C. occidentalis and O. cytheriformis being comparatively rare, while there are many, other species that are much more 

abundant. In Canada the lists of brackish-water fossils from the 

" Western Laramie," as given by Whiteaves, include practically all 

of the Judith River forms, and indicate that the two faunules are 

indistinguishable. On examining the descriptions of the localities at 

which these fossils were collected it is found that in the majority of 

cases the strata have steep dips or show other evidence of much disturbance, suggesting the possibilit}^ that the fossils in question may 

have really come from the Judith River instead of the Laramie. 

Another explanation, which is perhaps as reasonable, is that the Judith 

River brackish-water Mollusca really persisted in the far northwest to 

Laramie time as a continuous and practically unchanged faunule, while 

in the United States the break in continuity and resultant necessary 

migrations caused greater modification.
122 THE JUDITH RIVER BEDS. [BULL.257.

After removing from our list of species the few sporadic marine 

forms and those that are confined to the brackish-water bands in the. 

upper and lower portions of the formation, there still remains a much 

larger number of fresh-water and land species of Mollusca. These 

characterize probably more than nine-tenths of the total thickness of 

the formation, though of course they are not uniformly distributed 

through it. Mention has already been made of the fact that Unios 

and other fresh-water shells are occasionally found in actual association with brackish-water species such as Corbula, Neritina, and 

Corbicula, but as a rule they are in distinct beds, even in the upper 

and lower parts of the formation, while the middle 300 or 400 feet 

contain none but fresh-water and land Mollusca, associated with 

vertebrates of similar habitat.

A considerable number of the fresh-water and land species are not 

found outside of the formation; A few apparently occur in the Laramie also, and others are represented in the Laramie by similar forms 

that are doubtless their direct descendants. Taken as a whole, the 

Judith River fauna is distinguished from that of the Laramie by the 

presence of inan}^ characteristic species that do not occur in the higher 

formation and by the absence of many of the most common and 

striking of the Laramie forms.

This difference is sufficiently conspicuous to have been recognized by 

all paleontologists who have studied the faunas, even when the forma- 

. tions were supposed to be nearly or quite contemporaneous.

In the systematic list, under the specific headings mention has been 

made of the fact that certain Judith River fresh-water species apparently recur in the Laramie and that others are represented there by 

forms so similar that they may be considered their direct descendants. 

We may cite as conspicuous examples of the first class Unio dance, 

U. prisons, II. cryptorhynchus, and Goniobasis gradient^ and of the second class U. Supenawensis, Spliseriumplanuin, Campelomavetula, Goniolasis judithensis, &ndPhysa copei. These, however, form a comparatively small proportion of the fauna, and there is a much larger list of 

forms that have not been recognized outside of the Judith River beds, and 

at least one form, Goniobasis f subtortuosa, conspicuous on account of 

its peculiar specific characters and wide distribution, has no near relative in the Laramie. On the other hand, there is an absence of many 

of the peculiar types of Unio and of such conspicuous forms as Viviparus trochiformis and Tulotoma tkompsoni, common in the Laramie.

Taken as a whole, the fresh-water faunas of the Judith River and 

the Laramie are somewhat more distinct than the brackish-water 

faunas of the same formations, and with fairly complete collections it 

should not be difficult to distinguish them in the laboratory.

From the facts that have been stated concerning the distribution of 

the different kinds of invertebrates within the Judith River beds, we
STANTON.] INVEETEBEATE FAUNA. 123

may reach some conclusions as to the conditions under which the 

deposits were found, for these animals were inhabitants of the waters 

in which the sediments were laid down, and they give clear testimony 

concerning the character of the waters and their relations with the sea. 

It is evident that after the deposition of the Claggett formation a considerable area in north central Montana and in Alberta and Assiniboia 

emerged from the sea and became the habitat of land and fresh-water, 

animals. Since there was no obvious break in the sedimentation, it is 

probable that the larger part of the area was covered by low-lying 

swamps and lagoons. For some time there were slight oscillations that 

occasionally for brief intervals brought large parts of the area down to 

sea level and gave the lagoons sufficient connection with the ocean to allow 

the growth of oysters and other brackish-water forms over areas that 

had been occupied by fresh waters. Then for a longer period, during 

which 300 or 400 feet of sediments were formed, there was no connection with marine waters, though it is not probable that the area was

ever very many feet above tide. During this epoch the general 

upward movement was reversed, and when the subsidence progressed 

more rapidly than deposition connection with the sea was soon again 

established, bringing in, first, brackish waters .with their oyster beds, 

over nearly the entire area, with probably local bays and straits having more open and direct oceanic connections, such as is indicated by 

the occurrence of marine fossils in the Judith River on Cow Creek. 

Finally marine conditions were fully established over the entire area, 

so far as known, and continued during the deposition of the Bearpaw 

shales.

PLATE XII.

125
PLATE XII.

Page. 

Fig. 1. Unio priscus Meek and Hayden?................................... 108

Figs. 2, 3, 4. Unio priscus var. abbreviatus n. var. ......................... 108

126
U. S. GEOLOGICAL SURVEY BULLETIN NO. 257 PL. XII

JUDITH RIVER MOLLUSCA.
PLATE XIII.

127
PLATE XII I.

Page, 

Fig. 1. Unio subspatulatus Meek and Hayden .............................. 107

Figs. 2, 3. Unio supenawensis n. sp.................................... ... 109

Fig. 4. Goniobasis judithensis n. sp........................................ 117

Fig. 5. Melania whiteavesi n. sp........................................... 115
BULLETIN NO. 257 PL. XIII

 fff

JUDITH RIVER MOLLUSCA.
FOSSIL PLANTS OF THE JUDITH RIVER BEDS.

By F. H. KNOWLTON.

DESCRIPTIONS OF SPECIES.

TEENS.

PI. XIV, fig. 1; PI. XV, fig. 7.

Aside from the species below described as Osmunda montanensis, 

the collection contains minute fragments of two other evidently quite 

distinct ferns, upon which I have not ventured to bestow even generic 

names. The first of these, shown on PI. XIV, fig. 1, is a fragment of 

what appears to be the extreme tip of a pinnule of an apparently very 

delicate fern. It is cut into several rounded lobes which are slightly 

decurrent along the stem or rachis. One of these, together with the 

terminal lobe, appears to have been toothed, but this is obscure. The 

frond seems to have been thick, and.is apparently covered with minute 

papillae. The nervation can not be made out satisfactorily. This fragment suggests the terminal portion of a pinnule of some of the lip 

ferns, Cheilanthes, but the material is not sufficient to warrant even 

generic determination, and it is only mentioned in the hope of calling 

attention to it in future.

On the same piece of matrix there are fragments of the terminal 

portions of several small pinnules, each being cut into several relatively strong lobes. The nervation is obscurely preserved, but appears 

to be only once forked. Its relationship is not apparent. It is shown 

on PI. XV, fig. 7.

OSMUNDA MONTANENSIS n. sp. 

PI. XIV, fig. 6.

Shape of frond unknown; pinnule linear-lanceolate, obtusely wedgeshaped at base, rounded at apex; margin obscure, but apparently finely 

and sharply serrate; midrib strong, straight; nervation strong, arising at an acute angle, forking in an almost dichotomous manner three 

or exceptionally four times, the ultimate branches entering the sinuses

between the marginal teeth.

129 

Bull. 257 05 9
130 THE JUDITH RIVER BEDS. [BULL.257.

Unfortunately this species is represented by a single pinnule only, 

which is linear or slightly linear-lanceolate in shape, with a very 

obtusely wedge-shaped base and a somewhat narrowed and rounded 

apex. The length is 22 mm. and the width about 7 mm. The margin 

is not very well preserved, but so far as can be made out it is finely 

and sharply serrate. The nervation as described above is well shown 

in the figure.

Among the few known living species this pinnule agrees most closely 

with those of Osmunda, regqlis, the well-known and widely spread 

Royal fern; in fact, the agreement is so close that with the limited 

material available it is impossible to note any essential difference in 

size, shape, marginal dentation, and nervation, the resemblance extending even to the ending of the ultimate nerve branches in the sinuses. 

But as we have no knowledge as to the shape of the whole frond, and, 

moreover, as the geologic horizon whence this comes is so remote 

from the present time, I have hesitated, even though, the resemblance 

is so close, to regard it as a fossil representative of the living species. 

It is hardly to be presumed that a species could come down from the. 

Cretaceous to the present without change. Additional material is 

much to be desired.

Some half a dozen fossil species of Osmunda have been described 

from North America, ranging in age from the Potomac to the Eocene. 

ThePotomac species described by Fontaine a may be dismissed at once, 

as they do not suggest the present form in the least. The species 

approaching it most closely in size is Osmunda obergianaHverb from 

the lower Atanekerdluk beds of Greenland, but this differs in having 

entire margins and only once-forked nerves; in nervation ours is nearest 

to 0. doroscJikiana Gopp. c (the 0. torrelli of Heer and Lesquereux), 

from the Miocene of Sachalin, but the size and margin are not in 

accord. Osmundites skidegatensis of Penhallow/ from the Lower 

Cretaceous of Skidegate Inlet, Queen Charlotte Islands, has the pinnules too fragmentary to admit of satisfactory comparison.

Locality. Willow Creek, Fergus County, Mont., about 12 miles 

north of Musselshell post-office and 1 mile east of road from Junction 

City to Fort Maginnis.

CYPERACITES sp.

On several pieces of matrix there are fragments of narrow grasslike or sedge-like leaves that require at least to be mentioned, although 

they are not of sufficient size or well enough- preserved to be of any 

value. The longest fragments are under 6 cm. in length and show a 

width of 3 or 4 mm., and are provided with numerous close, parallel

a Potomac flora: Mon. U. S. Geol. Survey, vol. 15,1889, pp. 145-147.

ft Fl. Foss. Arct., vol. 3, pt. 2, PL XXVI, figs. 9-96.

c Op. cit., vol. 5, pt. 3, PI. I, fig. 4.

rf Trans. Roy. Soc. Canada, vol. 8, sec. 4, pp. 3-29.
KNowi/roN.] FOSSIL PLANTS. 131-

veins. They have not been figured, as they are too characterless to be 

of value.

Locality. Willow Creek, Fergus County, Mont., about 12 miles 

north of Musselshell post-office and 1 mile east of road from Junction 

City to Fort Maginnis.

SEQUOIA REICHENBACHI (Oeinitz) Heer. 

PI. XIV. figs. 3-5.

This is by far the most abundant form in the collection, there 

being hundreds of specimens, while there is hardly a piece of matrix 

that does not show it in greater or less profusion. It is present 

from large branches nearly 2 cm. in thickness, from which nearly all 

the leaves have fallen, to great clusters of branchlets and even those 

just unfolding, and in one or two instances there are branchlets showing the male araents in a good state of preservation. 1 have selected 

for illustration a few to show the range of size and appearance.

Unfortunately this species is of little value in fixing age within 

narrow limits, as it is of almost world-wide distribution within the 

Cretaceous. In this country it occurs very abundantly in the Potomac, 

and "has been reported in greater or less abundance and with greater 

or less degree of certainty in the Kootenai of Great Falls, Mont., the 

Dakota group at Fort Harker, Kans., the Belly River series at Belly 

River, Canada, the clay marl at Cliffwood, N. J., the Amboy clay 

at Woodbridge, N. J., the Montana formation at Point of Rocks, 

Wyoming, the Livingston beds in the Bozeman coal field of Montana, etc.

I have very carefully compared these specimens with the illustrations of Sequoia reichenbachi in all the literature available, and I am 

not able to separate them from this form. As would be expected 

from such a mass of material, there are differences in size and to some 

extent in appearance, but these are connected by a.!l possible gradations and are undoubted!}' to be explained on the ground of robust and 

perfect development and the completeness of the suite of specimens.

Locality. Willow Creek, Fergus County, Mont., about 12 miles 

north of Musselshell post-office and 1 mile east of road from Junction 

City to Fort Maginnis.

SEQUOIA sp. 1? (cone). 

PI. XIV, fig. 2.

From the Judith River beds 10 miles northwest of Wild Horse 

Lake, Alberta, Mr. Stanton obtained a single, much-broken cone that 

appears to belong to Sequoia.. It is globular in shape, being about 

'6 cm. long arid nearly the same in width, but it is somewhat flattened 

and the exact dimensions can not be ascertained* with certainty. The
132 THE JUDITH RIVER BEDS. [BULL.257.

scales were very large and thick, apparently not more than five showing in a vertical view. No attachment for the cone is observable.

This cone appears to be very similar, except as regards size, to 

Sequoia heerii Lesq., a from the western Tertiary. This, however, 

does not exceed 1.5 cm. in long diameter, while the one in hand exceeds 

3 cm., which is too great a difference for reasonable specific variation. 

This also suggests certain cones of S. reichenbachi as figured by 

Heer & from the Kome and Pattorfik beds of Greenland, but it is too 

much broken to be positive.

Locality. Judith River beds 10 miles northwest of Wild Horse 

Lake, Assiniboia.

SEQUOIA HETEKOPHYLLA* Velenovsky. 

PL XVI, fig. 5.

Sequoia heterophylla Velenovsky, Gyinnosp. d. Bohm. Kreidf., p. 22, PI. XII, fig. 

12; PI. XIII, figs. 2-4, 6-9.

Among the hundreds of coniferous branches in this collection there 

is but a single one, together with its counterpart, that appears to 

belong to this species. It is a small piece, about 5 cm. in length, of 

the upper portion of a branchlet, and bears rather small, relatively broad and abruptly pointed leaves, which, in the lower part of 

the branchlet, are remote and approximately opposite. The leaves 

are slightly narrowed at the base and are decurrent for a considerable 

distance down the stem in fact, reaching down to and apparently 

overlapped by the leaves next below. In the lower portion of the 

branchlet the leaves are open and spreading, but they become closer 

and more erect at the tip.

The marked characteristics of this species as defined by its author, 

and as interpreted by Newberry from the Amboy clays, is the heterophyllous form of the leaves, those at the base of the branchlets being 

shorter, smaller, and more appressed; while above, the leaves are more 

scattered and spreading, though ordinarily not to the extent shown in" 

the lower portion of the Willow Creek specimens. This, however, compares very closely with figs. 2-4 of Velenovsky's PI. XIII (op. cit.), as it 

does with Newberry's PI. VI (op. cit.), figs. 3, 5, and 13. In the upper 

part of the branchlet, where the leaves become more erect, it is not possible to distinguish our specimen from the ordinary branchlets of S. 

heterophyllus. The lowest leaves preserved in the Willow Creek specimens are slightly smaller than those a little above, which is an indication that, had the whole branchlet been preserved, they would show a 

still further reduction. Thus I am convinced that the specimens in 

hand are correctly referred to the above species; yet, as there is but

aTert. Flora: Kept. U. S. Geol. Surv. Terr., vol. 1, PI. VII, fig. 13. Also Newberry, Later extinct 

floras of North America: Mon. U. S. Geol. Survey, vol. 35,1898, PI. XLVII, fig. 7. 

&F1. Foss. Arct., vol. 3, pt. 2, PI. XX, figs. 1, 2.
KNOWT/TON.] FOSSIL PLANTS. 133

a single example, and this not a complete branchlet, I have hesitated 

to record the identification as absolutely certain.

Sequoia heterophylla was described by Velenovsky from the Upper 

Cretaceous (Cenomanian and Senonian) of Bohemia, and in this country has been found abundantly in the Amboy clays by Newberry and 

sparingly in the Upper Cretaceous of Staten Island (Kreischerville) by 

Hollick," in the Tuscaloosa of Alabama by Smith, 6 and by Ward c in 

the so-called Lower and Upper Albirupean (Later Potomac) of Virginia. 

In some of the localities above enumerated, except in the Amboy 

clays, it is not present in numbers sufficient to remove all suspicion as 

to the correctness of the determination, although the material was 

perhaps as satisfactory in some cases as that now in hand.

Locality. Willow Creek, Fergus County, Mont., about 12 miles 

north of Musselshell post-office and 1 mile east of road from Junction 

City to Fort Maginnis.

THUJA CKETACEA1? (Heer) Newberry.

PI. XVI, figs. 3, 3a.

(

Thuja cretacea (Heer) Newberry, Flora Amboy Clays, p. 53, PI. X, figs. 1, la. 

Libocedrus cretacea Heer, Fl. Foss. Arct., vol. 6, pt. 2, p. 49, PI. XXIX, figs. 1, 2; 

PL XLIII, fig. Id.

The collection contains four small pieces which I am unable to distinguish from Thuja cretacea. These specimens show very well the 

size and arrangement of the branchlets, but unfortunately they are not 

sufficiently well preserved to show clearly the shape of the leaves, 

though in one small area their outline can be faintly made out. I can 

see no difference in the size and disposition of the branchlets, nor for 

that matter in the leaves, between them and Thuja cretacea, yet as 

there is a slight doubt, I.have questioned the specific determination.

Heer described his Libocedrus cretacea from the Ataneschichten of 

Greenland, and apparently the same form was identified by Newberry 

from the Amboy clays of South Ambo}r, N. J. The latter author 

changed the generic name to Thuja on what seems good grounds.

These specimens have some resemblance to Thuja interrupta Newb./' 

from the Fort Union beds near the mouth of the Yellowstone, but are 

distinguished at once by their more slender, graceful habit, and by 

not being enlarged at the extremity of the branchlets.

Locality. Willow Creek, Fergus County, Mont., about 12 miles 

north of Musselshell post-office and 1 mile east of road from Junction 

City to Fort Maginnis.

'aTrans. New York Acad. Sci., vol. 12, p. 30, PI. I, fig. 21. 

bGeol. Snrv. Alabama, 1894, p. 348.

cPotomac^formation: Fifteenth Ann. llept. U. S. Geol. Survey, p. 378 et seq. 

 JLater extinct floras of North America: Mou. U. S. Geol. Purvey, vol. 35, PI. XXVI, figs. B-5cZ.
134 THE JUDITH KIVEK BEDS. [BULL. 257.

DAMMARA ACICULARIS n. sp.

PI. XV, figs. 2-5.

Cone scales broad and very thick at apex, narrowed below into a 

broad, thick basal portion; apex broadly rounded, provided in the center with a long, slender, acute, apparently depressed awn; body of 

scale with several (8 to 10) strong apparently concentric ribs, which 

are pressed close together and pass down the narrowed basal portion 

as thin strise.

The collection contains a large number of these scales, evident^ from 

a large cone, all of them detached and most of them widely separated, 

though occasionally several of them are found near together or even 

overlapping. The smallest one observed has a width of 11 mm. at the 

distal end, while the broadest one noted is 16 or 17 mm.; the majority 

of them are 14 or 15 mm. broad. The slender, awl-shaped awn shows 

an extreme length of 5 mm., but the usual length is 3 or 4 mm.; it 

appears to have been directed downward in the perfect cone. The 

length of the scales is about 18mm., exclusive of the awn, and the 

width of the narrowed basal portion 3 or 4 mm.

This species shows unmistakable affinity with forms described by 

Heer from the Ataneschichten and Patootschichten of Greenland, but 

may be distinguished from them at once by the long, sharp awn. .In 

size it is perhaps nearest to Dammara microlepis Heer, a which shows 

a width of 14 mm., but it is described by its author as having an obtuse, 

rounded apex and an attenuated base. In shape and the disposition of 

the ribs or striae it is more like D. korealis Heer, 6 but this is 22 mm. 

broad and has a shorter, thicker basal portion.

Both the Greenland species are without the awn so characteristic of 

the specimens under consideration, though I). lorealis is stated by 

Heer to have the apex apiculate. Doctor Newberry identified c this 

latter species in the Amboy clays, where he states it to be abundant, 

but the only specimen he figures is as small as, or even smaller than, the 

smallest one observed from Willow Creek. The figure shows a short 

apiculate apex and is not unlike some of ours from which the awn has 

been broken, but as he has "found numbers of them sometimes associated together, often scattered," and makes no mention of the presence of an awn, it was probably not a character of the Amboy clay 

form. What is probably the same species, though mentioned under 

the name of Eucalyptus geinitzi Heer,rf was found by Mr. David 

White in the Cretaceous of Marthas Vineyard, but the figured specimen shows no evidence of the awn, nor is it mentioned, although Mr. 

White states that this species is one of the commonest forms present

aFl. Foss. Arct. vol. 6, pt. 2, p. 55, PI. .XL, fig. 5. 

bOp. cit, p. 64, PL XXVII, %. 5.

c Flora Amboy clays: Mon. U. S. Geol. Survey, vol. 20, p. 47, PI. X. fig. 8. 

 d Am. Jour. Sci.,3d.ser., vol. 39, 1890, p. 98, PI. II, fig. 10.
FOSSIL PLANTS. . 135

at that place. The reasons for regarding Heer's Eucalyptus geinitzi 

as at least generically similar to Daminara are well set forth by Newberry in his monograph on the Amboy clay, flora (p. 47).

The same form, or at least a form very closely allied to it, is 

described and figured by Velenoysky a from the Upper Cretaceous of 

-Bohemia, also under the name of Eucalyptus geinitzi, and it is also 

reported from the Cenomanian of Moravia. It would seem that these 

must all belong to one genus, and that a conifer.

Locality. Willow Creek, Fergus County, Mont., about 12 miles 

north of Musselshell post-office, and 1 mile east of road from Junction 

City to Fort Maginnis.

CUNNINOHAMITES ELEQANS (Corda) Endlicher. 

PI. XV, fig. 1.

Cunhinghamites ekgans (Corda) Endlicher, Synop. Coiiif.,p. 270.

Cunninghamia elegans (Corda) in Reuss, Verstein. Bohm. Kreidef., pt. 2, p. 93, PI. 

XLIX, figs. 29-31.

The collection contains portions of three or four thick branches, 

rather closely beset with long narrow leaves that I think must be referred 

without doubt to this species. The longest and best of these, shown 

on PI. XV, fig. 1, is about 15 cm. in length and shows a thickness of 1 

cm. While the leaves are not veiy well preserved, they are at least 3 

cm. long and 3 mm. or more in width, and the scars left on the branch 

by their fall are 5 rum. or more long and about 3 mm. broad; they 

are apparently 1-nerved.

The specimen here figured, together with another smaller one, is 

not to be distinguished from figures of this species given by Newberry b 

from the upper part of the Amboy clay at Keyport, N. J. It is of 

about the same size, and has the same large leaves and scars.

Cunninghamites elegans, first described from Moletein in Moravia 

and from Mseno in Bohemia, was also found by Heer c in the Patoot 

beds of Greenland, and according to him the forms from the lower 

Senonian of Westphalia referred by Hosius and von der Marck (/ to 

Cunning hamites squamasus should belong here also.

locality. ^Willow Creek, Fergus County, Mont., about 12 miles 

north of Musselshell post-office and 1 mile east of road from Junction 

City to Fort Maginnis.

aFoss. Fl. bohm. Kreidef., vol. 4, PI. II (XXV), figs. 8-li.

b Flora Arnboy clays: Mon. U. S. Geol. Survey, vol. 26, p. 48, PI. V, fig. 1.

cFl. Foss. Arct., vol. 7, PI. LI.II, fig. la.

dFl. d. Westf. Kreidef.: Palceontogr., vol. 26, PI. XXXVII.-
136 THE JUDITH RIVER BEDS. [BULL.267.

CTJNNINOHAMITES BECURVATUS1 Hoaius and von der Marck. 

PI. XVI, fig. 6.

Cunninghamites recurvatus Hosius and von der Marck, Fl. d. Westf. Kreidef.: 

Palseontogr., vol. 26, p. 179 (55), PI. XXXVII, figs. 143,144.

Associated with the last is the specimen here figured, which seems to 

belong to this species. It is a fragment from the middle of a branch; 

is between 8 and 9 cm. in length, and 3 or 4 mm. in thickness. The 

leaves are not very well preserved, but they are over 2 cm. in length, 

and, so far as can be made out, about 2 mm. in width at or near the 

base, and taper from near the middle to a narrow, acute point. The}r 

arise at a low angle and are somewhat decurved. The sCars left on the 

branch by their fall can not be determined, as the specimen is too poorly 

preserved at this point.

In view of the fact that this species is not only found in. the same 

beds with the last-mentioned species, but has a fragment of it on the 

same piece of matrix, it is entirely possible that this example is incorrectly determined. It may possibly be a smaller branchlet of O. 

elegans with the leaves slightly recurved, but it agrees almost perfectly 

with the figures given of 0. recurvatus, and I have referred it provisionally to this species. The type localit}r of C. recurvatus is the 

Scaphites binodosus zone of the lower Senonian of Westphalia.

Locality. Willow Creek, Fungus County, Mont., about 12 miles 

north of Musselshell post-office and 1 mile east of road from Junction 

City to Fort Magiunis.

CUNNINGHAMITES PTTLCHELLUS n. sp.

PI. XVI, fig. 1.

Branches apparently slender, leaves alternate, somewhat remote,

broad and thick at base, turning abruptly at right angles to the stem,

very long, narrow, sharp-pointed at apex, thick in texture and apparently deeply channeled above; leaf-bases large, oblong, obtusely acute, 

keeled and provided in the lower part with several fine striae.

This form is represented by several very well-preserved branches, 

the best of which is here figured. The greatest thickness observed in 

a branch is 6 or 7 mm., and the least about 3 mm. Lateral branches 

slender, arising at intervals of some 2 or 3 cm., alternate and nearly at 

right angles to the main branch. Leaves persistent for at least two 

seasons, disposed spirally, with enlarged bases closely appressed to the 

branch, just above which they turn abruptly at right angles and are 

then straight or sometimes slightly Repressed. Length of the leaves 

from 2 to 3 cm., and their width 2 mm. or less. As stated above, the 

leaves appear very narrow and stiff, their upper surface apparent^ 

being deeply channeled.

The specimen shown in PI. XVI, fig. 1, evidently represents portions of two seasons' growth, the lower segment, showing the origin
KNOWLTON.] . FOSSIL PLANTS. 137

of three lateral spurs, being clothed with shorter, more slender leaves, 

which are closer together, while the upper portion shows a period of 

more active growth, in which the leaves are slightly more scattered and 

larger and decidedly longer than those below. In all cases, however, 

the leaves just above their thickened base turn abruptly at right angles 

to the branch. By taking an impression of the branch with modeling 

clay or wax the original shape of the branch is approximately restored 

and the size and shape of the leaf bases become clear. It appears 

that the leaves are distributed on all sides of the branch in a regular 

spiral manner, a fact which is also shown in a fortunate fracture across 

the branch, showing the leaves going down into the matrix on what is 

now the underside of the stem. The thickened and ribbed base of a 

leaf is closely appressed to the branch, being overlapped at base by 

the leaves below and itself in turn partially overlapping the one next 

above. While there is no positive evidence to show how the leaves 

separated from the branch,.it is probable that they were cut off at or 

hear the point where the right-angled turn of the blade is made, which 

would leave behind the thick base. But, as already pointed out, it is 

certain that the leaves were persistent for some time, probably several 

seasons.

This fossil form has been very carefully compared with the only 

living species of Cunninghamia (0. sinensis) of China and Japan, and 

the points of agreement are so many as to leave no doubt regarding 

their generic identity. In the living species the leaves are distributed 

in a spiral manner and have the same thickened bases, which overlap 

and are in turn overlapped by others, as in the fossil. By taking an 

impression in clay of a branch of about the same size as some of the 

fossil branches, a mold is obtained which agrees in essential particulars with the fossil impression. By the strong curving of the leaves on 

the lower side of a branch they are made to assume a flat, more or 

less two-ranked disposition, and it is quite possible that a similar condition m&y have existed in the fossil. The leaves are evidently persistent for several years, as there is no evidence in any of the specimens 

available for study of a disposition to fall. The leaves in the living 

species, while of about the same size and shape as in the fossil, differ 

in having finely serrate margins and several faint parallel ribs, instead 

of what appears to be a channel in the middle.

So far as I have been able to find, the nearest approach among fossil 

forms to the one under consideration is the one which was called Al)ietites setigera by Lesquereux," but which has been later regarded as 

merely rootlets, a view I have myself held; but since seeing the material from Willow Creek I am decidedly of the opinion that Lesquereux's 

specimens actually represent a conifer. It seems quite impossible, 

however, that they could belong to Abietites on the ground of analogy

<«Ter. Flora: Kept. U. S. Geol. Surv. Terr., vol. 7, p. 82, PI. VII, figs. 17, 18.
138 THE JUDITH RIVER BEDS. [mu.Wi.

with the living Abies or Picea, since in both these the leaves fall with 

the greatest ease. In discussing his Abietites setigera, Lesquereux 

states that he had submitted it to Saporta, who informed him that he 

had an undoubtedly identical form from the Upper Cretaceous of St. 

Paulet, Gard, France. Saporta disagreed with Lesquereux as to the 

affinity of the fossil in question, but the latter does not mention what 

Saporta proposed to call it, nor have 1 thus far been able to find any 

mention of such a plant in Saporta's works, or of an account of the 

plants of St. Paulet.

Among species of Cunninghamites the one in hand appears to 

approach most closely to G. recurvatus Hos. and v. d. Marck,® from the 

Lower Serionian of Westphalia; in other words, to the preceding species. In that species the leaves, while somewhat recurved, arise at a 

considerable angle, whereas in this the leaves are at a decided right 

angle. This difference is really not great, yet the appearance of the 

two is very different, but it is possible that with a larger series of 

specimens of the former this apparent distinction might disappear. I 

have hesitated to think that there could be three well-marked species 

of so rare a genus in the same beds, }ret this is by no means without 

precedent.

Locality. Willow Creek, Fergus County, Mont., about 12 miles 

north of Musselshell post-office and 1 mile east of road from Junction 

City to Fort Maginnis.

POPTJLTJS CEETACEA n. sp. 

PI. XVII, figs. 1-5.

Leaves coriaceous in texture, ovate or elliptical-ovate in shape, very 

obtusely wedge-shaped, sometimes almost truncate, at base; rather 

obtuse or somewhat rounded at apex; margin entire at base, becoming 

coarsely undulate-toothed above, the teeth usually very much rounded, 

sometimes more nearly acute, occasionally with a small tooth between 

the larger ones; petiole slender, not fully preserved; midrib strong, 

passing straight to the apex; secondaries strong, 4 or 5 pairs, alternate, remote, lower pair arising at or a little above the top of the 

petiole, with several (3 or 4) branches on the outer or lower side, 

some of which pass directly to the margin, while others unite into 

broad loops and send small branches to the teeth; upper secondaries 

straight, or more frequently curved upward, often - forked, the 

branches passing to the teeth, or, especial^ in the upper part of the 

blade, with the secondaries uniting by broad bow well inside the margin and sending slender branches into the teeth; nervilles rather 

obscure, apparently irregular and mainly percurrent; finer nervation 

obscure.

This species, if I am correct in supposing that all here included 

actually belong to one form, is a very polymorphous one and

a PI. d. westf. Kreidef.: Palseontogr. vol. 26, p. 179, PI. XXXVII, figs. 143,144.
KNOWLTON.] FOSSIL PLANTS. , 139

shows considerable variation in size, shape, marginal teeth, arid 

nervation, and yet with the ample material in hand it seems impossible to draw any satisfactory line between them. What is assumed 

to be the typical form is shown in PL XVII, fig. 1. It is elliptical-ovate in general outline, with an abruptly and very obtusely 

wedge-shaped base and rather few, low, mostly rounded teeth, 

and has the lower pair of secondaries arising above the top of 

the petiole; its length is 6.5 cm. and its width about 4 cm. Agreeing 

with this in size and in the marginal teeth, but with a more nearly 

truncate base and the lower secondaries arising at the extreme base of 

the blade, is the form shown in fig. 5. Its length can not be ascertained, 

but the width is the same as that of the form first described. Of a 

smaller size and a more nearly elliptical outline is the leaf shown in 

fig. 3, in which the teeth are relatively larger and the lower secondaries apparently take their origin above the base of the blade. Its 

length is 4 cm. and its width 3 cm., and a little more than 1 cm. of 

the petiole is preserved. The smallest leaf regarded as belonging 

here is that shown in fig. IQd. It is only 2.5 cm. in length and a little 

over 2 cm. in width. The extreme in another direction is exhibited 

in fig. 2, which is more nearly ovate in outline and has an abruptly 

rounded base with a small deltoid extension down the petiole. Its marginal teeth are obscure, but so far as can made out the margin is 

merely undulate in the lower portion, but becomes regularly toothed 

in the upper part. The lowest pair of secondaries arise some distance 

above the base of the blade. The length of this example is about 

6.5 cm. and the width 5.5 cm. It is possible that this last may not 

belong with the others, but I have several specimens which seem to 

connect it with them, and it may at least provisionally bo regarded as 

the same.

I have been much puzzled as to the correct generic reference of 

these leaves, and had at first supposed that they belonged to Quercus, 

but a somewhat extended search among living and fossil forms has 

not disclosed anything that can be regarded as especially close. Thus 

at first sight they seem to suggest certain of the forms of Quercus westfalica Hos. and v. d. Marck/' from the Upper Senonian of Westphalia, 

but in these the secondaries are much more numerous and in no case 

do the lower pairs arise at the top of the petiole, nor are they branched 

on the lower side as in the Willow Creek leaves. I have finally concluded, on the ground of their obvious and close resemblance to the / o

leaves of the living Populus grandidentata Michx., that they are best 

referred to Populus. In looking through the specimens of the living 

species in the National Herbarium it is easy to select examples from 

many parts of the country in which the resemblance is really striking.

aFl. d. Westf. Kreidef.: Palceontogr, vol. 20, PI. XXIX and XXX.
140 THE JUDITH EIVER BEDS. [BULL.257.

They have the same ovate shape, with the rounded or obtusely wedgeshape base, and while the teeth vary somewhat in character, in many 

cases they are low and rounded, as in the fossil. The apex of the leaf 

is always pointed, but is more or less rounded in the fossil. The lowest 

pair of secondaries always arise at the very base of the 'blade, whereas 

in the fossil they may or may not do so. The other nervation is 

also quite like that in the "Willow Creek specimens, but it is more 

inclined to be camptodrome, though not infrequently the secondaries 

enter the teeth directly.

Locality. Willow Creek, Fergus County, Mont., about 12 miles 

north of Musselshell post-office and 1 mile east of road from Junction 

City to Fort Maginnis.

POPTTLTTS sp. 

PI. XIX, fig. 1.

The collection contains a single fragment that appears to belong to 

Populous, but it is, unfortunately, not well preserved. It is a small 

leaf, apparently almost circular in shape, being about 3 cm. broad 

and possibly a little less in length. The margin is uncertain, but 

appears to be undulate. The petiole is very long and slender, over 

2.5 cm. of it being preserved. The nervation consists of 5 ribs arising 

from the top of the petiole, the three middle ones being strong and 

once forked, the branches often uniting before reaching the margin, 

while the lateral ones on each side are slenderer and apparently 

unbr-anched. At the base of each of these outside ribs is a small 

secondary branch which has much the appearance of another rib. 

The nervilles, so far as can be made out, seem to be irregularly reticulated.

In size, shape, and the long petiole this fragment suggests Populm 

TOtundifolia Newb., a from the Fort Union beds of Montana, but the 

nervation, as well as can be determined, appears different, and the 

margin can not be compared. In size and shape, also, it is like P. 

flabellum Newb., 6 from the supposed Upper Cretaceous of Puget 

Sound, but the nervation is quite different. The status can not be 

fixed until more and better material is forthcoming.

Lacality. Willow Creek, Fergus County, Mont., about 12 miles 

north of Musselshell post-office and 1 mile east of road from Junction 

City to Fort Maginnis.

POPULITES AMPLTTS n. sp. 

PI. XVIII, fig. 1.

Leaf coriaceous in texture, apparently very broadly ovate in shape; 

base destroyed, but apparently truncate; apex very obtuse and

"Later extinct floras of North America: Mon. U. S. Geol. Survey, vol. 35, PI. XXIX, figs. 1-4. 

6Op. cit., PI. XX, fig. 4,
KNOWI/FON.] FOSSIL PLANTS. 141

rounded; margin with apparently one large, obtuse, lateral lobe, but 

others provided with obscure, faint, remote teeth; midrib of moderate 

strength, somewhat zigzag in the upper portion; secondaries four 

pairs, craspedodrome, the lowest pair straight, apparently opposite, 

and arising at or near the top of the petiole, provided with several 

branches on the lower side; upper secondaries remote, alternate, much 

arched upward, usually with two or three strong forks, all branches 

entering the margin in very slight marginal dentations; nervilles few, 

strong, and irregular.

The example figured is the only one contained in the collection, and 

unfortunately this is imperfect in that it lacks the basal portion. It 

is a large leaf of thick texture, and so far as can be made out is very 

broadly and obtusely ovate in outline, with a single rather large lobe 

on one side and faint indications of scattered marginal teeth. The 

length is about 9 cm. and the width nearly the same; possibly the 

length may have been a little more when the leaf 'was in perfect shape. 

From the appearance of the larger, lower pair of secondaries it would 

seem that the}7 were opposite and at or near the top of the petiole, 

giving rise to an obscurely 3-nerved condition.

This form seems to find its closest relationship with the genus Populites, as described by Lesquereux, from the Dakota group. For 

instance, it suggests in a general way P. letigiosus (Heer) Lesq., a being 

of approximately the same shape and with the same type of nervation, 

but it differs specifically in its much larger size and fewer, more arched, 

secondaries. In shape and disposition of the nerves it also suggests 

Populus? cordifolia Newb.,& from the Dakota at Blackbird Hill, 

Nebraska, which is figured as having a serrate margin.

Locality. Willow Creek, Fergus County, Mont.,"about 12 miles 

north of Musselshell post-office and 1 mile east of road from Junction 

City to Fort Maginnis.

BETTJLITEST HATCHEBI n. sp. 

PI. XVIII, fig. 3.

Leaf small, apparently of firm texture, approximately circular in 

outline, slightly heart-shaped at base, rounded at apex; margin rather 

coarsely toothed, the teeth broad and obtuse (petiole not preserved); 

midrib strong, irregular or zigzag; secondaries, about five pairs, 

strong, especially the basal ones, which arise at a nearly right angle, 

the others being at an angle of 30° or 40°; lower pair of secondaries 

with four or five slender tertiary branches on the lower side, which 

unite in a broad bow some distance inside the margin; upper secondaries forked at about two-thirds the distance between the midrib and

« Flora Dakota group: Mon. U. S. Geol. Survey, vol. 17, PI. VII, fig. 7; PI. VIII, fig. 5, etc. 

& Later extinct floras of North America: Mon. U. S. Geol. Survey, vol. 35, PI. Ill, fig, 7.
142 THE JUDITH KIVE.R BEDS. [BULL.257.

margin, the branches uniting and sending slender slips from the outside of the bows to the marginal teeth; nervilles numerous, very 

strong, mostly unbroken and at right angles to the secondaries.

This is another form represented by a single specimen, but it is well 

characterized by its small size, nearly circular or veiy broadly ovate 

outline, coarsely toothed margin, and peculiar strong nervation. The 

length is 2.5 cm. and the width about 3 cm. It is well shown in the 

figure.

I am uncertain as to the proper generic reference for this little leaf. 

Although differing greatly in size, the shape and general character of 

the .nervation are strongly suggestive of certain species of Viburnites 

from the Dakota group of Kansas. Thus V. cras'sus Lesq. a has a 

heart-shaped base and coarse-toothed margin as well as a strong nervation, but the teeth are lower and more acute and the secondaries after 

forking do not unite so distinctly, but pass directly to the margin. A 

similar criticism applies to Viburnites masoni Lesq., 6 though with less 

force. Certain of Lesquereux's species of Protophyllwn, which, by the 

way,' are hardly to be separated from some forms of Viburnites,, agree 

very well in shape, but have a more or less peltate base and distinctly 

forking secondaries, while in Populites the margin is somewhat different and the secondary nervation is strongly forked. Altogether this 

leaf seems to approach more closely to some of the forms of the 

highly polymorphous Betulites westii Lesq., c of the Dakota group. 

In size and shape it agrees very well with B. westii subintegrifolius, 

and in shape, size, and marginal teeth with B. westii reniformis. But 

in these forms, as well as in all but one of the other varieties, the secondaries usually fork and pass to the margin without uniting. In 

B. westii grewiopsideus,d however, the upper secondaries unite in 

exactly the same manner as in the leaf under consideration, and it is 

consequently referred to the same genus, although with a mark of 

interrogation. I do not think this leaf is sufficiently close to any of the 

forms of Betulites westii to warrant placing it with them, but, as above 

indicated, it does not seem generically distinct from them. In an}^ 

event it is a well-marked leaf and can easily be identified if found in 

future.

Locality. Willow Creek, Fergus Count}7 , Mont., about 12 miles 

north of Musselshell post-office and 1 mile east of road from Junction 

City to Fort Maginnis.

a Flora Dakota group: Mon. U. S. Geol. Survey, vol.17, PI. XLV, figs. 1-4. 

& Op. cit., PI. XLV, fig. 5. 

c Op. cit., Pis. IV and V. 

<*0p. cit., PI. LXIV, fig. 10.
KNOWI.TON.J FOSSIL PLANTS. 143

aUEECUS MONTANA n. sp.

PI. XVII, fig. 6.

Leaf of firm texture, ovate in shape, with a very obtusely wedgeshaped base and an obtuse apex; margin perfectly entire below along 

the wedge-shaped portion of the base, regularly and coarsely undulatetoothed above, the teeth obtuse and rounded; petiole slender, of moderate length; midrib of moderate strength, straight; secondaries, four 

or five pairs, rather slender, alternate or subopposite, remote, passing 

directly to marginal teeth or forking and the branches entering the 

teeth; nervilles numerous, mostly unbroken.

The example figured is all that can with certainty be referred to this 

form. It is ovate in shape, with a peculiarly straight and obtusely 

wedge-shaped base and coarse-toothed margin. The length is about 

6 cm. arid the width about 5 cm., while the petiole, which seems to be 

entirely preserved, has a length of a little more than 1 cm. The 

nervation is well shown in the figure.

I am uncertain as to the generic reference of this leaf, and it may 

possibly be an extremely aberrant form of what has been described as 

Populus cretacea (p. 138), but I do not think so. It has the peculiar 

base described above, very regularly toothed margins, and the lowest 

pair of secondaries arising at a distance above the top of the petiole, 

although at the extreme base of the blade is a pair of very thin secondary branches, which only proceed for a short distance.

Among fossil forms this seems to find its greatest aflinit}^ with 

Quercus suspecta Lesq., a from the Dakota group of Ellsworth County, 

Kans. The latter, however, is broader, being elliptical rather than 

ovate, more obtuse at apex, and has more numerous secondaries, 

which all seem to enter the larger marginal teeth. The finer nervation is not preserved in the Kansas leaf mentioned.

Lesquereux regards his species as being most closely related to Q. 

loilmsii Hos., and Q. latissima Hos., 6 from the Upper Cretaceous of 

Westphalia, but neither one seems to approach very closely to the 

form in hand.

Locality. Willow Creek, Fergus County, Mont., about 12 miles 

north of Musselshell post-office and 1 mile east of road from Junction 

City to Fort Maginnis.

ftUEBCTTS JUDITHS n. sp. 

PI. XVIII, fig. 2.

Leaf rather membranaceous in texture; apparently obovate in shape, 

truncate at base, and broadly rounded at apex; margin undulatetoothed, the teeth largest near the middle and becoming more shala Flora Dakota group: Mon. U. S. Geol. Survey, vol. 17, PI. XLVII, fig. 7. 

f>Dicotyl. Westf. Kreidef.: Palaeontogr., vol. 17, Pis. XII and XIII.
144 THE JUDITH RIVER BEDS. [BULL.257.

lowly undulate at the apex; midrib rather slender, zigzag, especially 

above; secondaries slender, five or six pairs, alternate, remote, forking, and sometimes ending in the marginal teeth, but usually joining 

the one above and sending thinner branches to the margin; finer 

nervation obscure, but apparently forming irregular meshes.

The specimen figured is all that was found in the collection, and 

unfortunately this is quite imperfect, lacking most of the sides below. 

As nearly as can be made .out it was obovate in outline, being about 

9 cm. in length and about 7 cm. in width. It seems to be allied to the 

preceding species and even to that described as Populus cretacea, but 

its obovate outline and somewhat different nervation are perhaps sufficient to characterize it.

Locality. Willow Creek, Fergus County, Mont., about 12 miles 

north of Musselshell post-office and 1 mile east of road from Junction 

City to Fort Maginnis.

SAPINDITS INEXPECTANS n. sp. 1! 

PI. XVII, fig. 7

Leaf small, membranaceous in texture, elliptical-ovate in shape, 

apparently .rounded at base, obtuse at apex; midrib slender, straight; 

secondaries stout, about six pairs, subopposite, at an angle of about 

45°, much curved upward, camptodrome, each joining the one next 

above; nervilles numerous, thin, mainly broken, and forming large, 

irregular areas.

This little leaf, the only one contained in the collection, is ellipticalovate in outline, about 3.5 cm. in length and 2.25 cm. in width. The 

nervation is shown in the drawing.

1 have not attempted much search for the close relatives of this species, as the single specimen available is of such a nondescript character 

that it would be difficult to work out satisfactorily its relationship.

Locality. Willow Creek, Fergus County, Mont., about 12 miles 

north of Musselshell post-office and 1 mile east of road from Junction 

City to Fort Maginnis.

TBAPA* MICKOPHYLLA Lesquereux.

From the base of the Judith River beds, at a point on Cow Creek 

about 13 miles above its mouth, Mr. Stanton has obtained about fifteen 

specimens of small detached leaves or leaflets that I am not able to 

distinguish from this species. While they are all smaller than the 

usual examples from the type locality (Point of Rocks, Wyoming), they 

agree well in shape and the marginal dentation, but unfortunately 

have not retained the nervation, or at most but slight traces of it. 

This species, or, at least, what has been so identified, has been figured 

by Dawson, in Tyrrell's collections from Bad Lands, Red Deer, and
KNOWLTON.] FOSSIL PLANTS. 145

Rosebud rivers, and Pincher Creek, Canada, the. age of which he 

regards as "Lower Larainie," and also a single doubtful example 

"from the Upper Laramie of Great Valley." fl

Professor Ward found this species abundantly at Burns ranch, on 

lower Yellowstone River, Montana, in beds supposed to be of Fort Union 

age; but, as I have shown in the Flora of the Montana Formation (p. 

63 et seq.), I can not believe that these should be referred to T. microphylla, for the reason that they are clearly compound leaves, rarely 

detached, whereas at the type locality and at all the points mentioned 

by Dawson they are always separated and show no evidence of having 

been compound. I found examples that are not to be distinguished, 

apparently, from the Burns ranch forms, on Wolverine Creek, in the 

Yellowstone National Park, in beds regarded as of true Laramie age, b 

and in 1896 Mr. Stanton and myself found a large number of detached 

leaves in Converse County, Wyo. j in clay beds in the lower portion 

of the true Laramie. c It may be that my presumption of two forms 

being mixed under this name is not valid, but it is certainly remarkable that at two localities they should always give evidence of being 

compound and at all the other localities appear as detached leaves, 

with no indication of being compound, especially as the material is 

ample in most cases. It must be confessed, however, that when dealing with isolated leaves or leaflets it is impossible to draw any satisfactory line between them.

Locality. Cow.Creek, Montana, 13 miles above its mouth.

TKAPA1 CUNEATA Knowlton.

Trapa? cuneata Knowlton, Flora Montana formation: Bull. U. S. Geol. Survey No. 

163, 1900, p. 64, PI. V, fig. 6.

The Willow Creek material contains a single, somewhat imperfect 

example, which is practically indistinguishable from my T. cuneata 

from Point of Rocks, Wyoming. It has the same obovate-cuneate 

outline, being broad and obtuse above and wedge-shaped below, 

and shows the same obtuse teeth confined to the upper third of 

the blade. It is slightly larger, being about 2.5 cm. long and a little 

over 1.5 cm. wide, while the Point of Rocks species is 2 cm. long and 

slightly over 1 cm. wide. The only point of difference is a very slight 

one in the midrib, this in the type specimen being " slender, somewhat flexuous, with several very slender, flexuous, often forking, 

branches," and in the one under discussion it is even less pronounced; 

in fact, hardly to be made out at all. But this character is perhaps not 

of much importance when considered in relation to the condition prevailing in Trapa ? microphylla Lesq., of which a great many speci-

«Cf. Trans. Roy. Soc. Canada, vol. 4, p. 31 (1886).

*>Mon. U. S. Geol. Survey, vol. 32, pt. 2, p. 661, PI. LXXVII, figs. 3, 4.

c Flora Montana formation: Bull. U. S. Geol. Survey No. 163, p. 63.

Bull. 257 05 10
146 THE JUDITH RIVER BEDS. [BULL.257.

mens have been found, and in which the midrib is sometimes quite 

distinct and at others very -faint or almost obsolete. The general 

nervation, however, is identical in the two specimens, and it seems 

safe to regard the Willow Creek example as the same as T. cuneata. 

It is not necessary to go into the question of the generic reference of 

these curious little leaves, as this has been done several times before. a 

' Locality. Willow Creek, Fergus County, Mont., about 12 miles 

north of Musselshell post-office and 1 mile east of road from Junction 

City to Fort Maginnis.

DIOSPYKOS JTTDITHJE n. sp. 

PL XVIII, figs. 4, 5; PL XIX, fig. 3.

Leaves membranaceous in texture, elliptical-lanceolate in shape, 

broadest at or near the middle, from which they narrow about equally 

to the acute base and acuminate apex; margin entire; petiole short; 

midrib of medium strength for the size of the blade, straight; secondaries five or six pairs, thin, alternate, irregular, camptodrome, arching 

well inside the margin and joining the one next above; lower secondaries very thin and forming a series of bows just inside the margin; 

nervilles numerous, very thin, mainly percurrent, and approximately 

at right angles to the secondaries.

This form is represented by about half a dozen examples, which show 

such a range in size as to suggest the possibility of two species being 

confused, but there seems no other line except that of size to be drawn 

between them. They all have the elliptical-lanceolate outline and are 

all about 'equally narrowed to both base and apex. The largest, shown 

in PI. XVIII, fig. 5, is about 6 cm. long and 3.5 cm. wide; it is quite 

imperfect, lacking the apex and most of one side. The next in size, 

shown in fig. 3, is 45 cm. long and 2.25 cm. wide; its petiole, seemingly entire, is 4 mm. in length. In fig. 4 is shown the smallest leaf, 

this being 3 cm. long and about 14 mm. wide.

These leaves are referred to the genus Diospyros from their agreement with certain leaves from the Dakota group of Kansas so referred 

by Lesquereux. For example, it is similar to some of the leaves 

referred to D. kansaseana Lesq., 6 but more particularly with D. primseva Heer, c which was'Originally from the Dakota group of Nebraska, 

but also since found in Kansas. In both.of these species, however, 

the secondaries are more numerous than in the Willow Creek specimens, and the petiole and midrib are much stronger.

It was at first supposed that these leaves should belong to the Celastracese.on account of their resemblance to certain forms of Celastrus^

«Cf. Flora Montana formation: Bull. U. S. Geol. Survey No. 163, pp. 62-64. 

f> Flora Dakota group: Mon. U. S. Geol. Survey, vol. 17, PI. XVII, figs. 1, 2, eto, 

c Op. cit., PI. XX, figs. 1, 2,
KNOWLTON.] FOSSIL PLANTS. 147

Euonymus, etc., but the resemblance is perhaps closer with Diospyros,- 

as above pointed out.

Locality. Willow Creek, Fergus County, Mont., about 12 miles 

north of Musselshell post-offlce and 1 mile east of road from Junction 

City to Fort Maginnis.

CA8TALIA STANTONI n. sp. 

PI. XIX, fig. 4.

Leaf large, evidently thick and of firm texture, approximately circular in outline; deeply cordate at base, the sinus rather broad and 

the lower lobes rounded; apex very obtuse and rounded; margins 

very faintly and obscurely toothed; petiole evidently thick and strong; 

nervation pinnate, the midrib relatively thin, straight; secondaries, 

five or six pairs, strong, subopposite, arising at an angle of about 45°, 

lowest secondaries with several (four or "five) branches on the lower

side, which fork two or three times and supply the lateral lobes, the 

branches passing to the minute marginal teeth; upper secondaries 

with one to three, occasionally uniting forks, the ultimate branches 

entering the marginal teeth; nervilles numerous, strong, mainly 

broken.

This splendid leaf, which is preserved practically entire, is the only 

One of its kind in the collection. It is nearly circular, the length from 

the top of the petiole to the apex being about 11 cm., and the width at 

the broadest point a little more than 12 cm.; the lateral lobes extend 

downward below the top of the petiole for a distance of about 2.5 cm. 

While the central or midrib is not particularly strong, the remainder 

of the nervation is abundantly so for the size of the leaf.

There seems to be little or no doubt as to the propriety of referring 

this leaf to the genus Gastalia, since, for example, it agrees very 

closely in size and shape with many leaves of 0. odorata of eastern 

North America or C. alba of the Old World. It has, however, a 

shallower, broader basal sinus than is.usual in most leaves of these 

species, and the lobes are more obtuse and rounded, yet in this respect 

it is not greatly unlike other species, such, for instance, as what has 

been called O. elegans (Hook.) from Guatemala. In most species of 

Gastalia the margin is perfectly entire, yet there are notable exceptions, as in C. ampla (Salsb.) of Mexico and the West Indies, C. lotus 

and G. thermalis of the Old World, and G. gigantea (Hook.) of Australia. In the fossil form under consideration the margin is very 

slightly but unmistakably toothed. As regards nervation, in most 

living species of Gastalia the secondaries after forking are more or 

less united, thus inclosing a large and one or two series of smaller 

areas, while in some e. g. G: ampla the secondaries are practically 

united from near the midrib into numerous series of large aerolse. In
148 THE JUDITH RIVEE BEDS. [BULL.267.

the splendid O. gigantea of Australia, however, the secondaries are 

little or not at all joined, but fork several times and send the ultimate 

branches to the margin. Thus, as regards marginal dentation and 

nervation, our fossil leaf seems to agree most closely with the Australian 

species mentioned.

The only other species of the genus thus far detected in this country is the doubtful Castaliaf duttoniana Knowlton a from the Montana 

formation at Dutton Creek, Laramie Plains, Wyo. This latter form, 

however, is a very different leaf, being hardly half the size of the one 

before us, broadly elliptical, very slightly heart-shaped at base and 

entire-margined; the nervation is also different, and it may not be 

correctly referred to Castalia.

Locality. Willow Creek, Fergus Count}', Mont., about 12 miles 

north of Musselshell post-office and 1 mile east of road from Junction 

City to Fort Maginnis.

PHYLLITES DENTICTTLATTTS n. sp. 

PI. XIX, fig. 2.

Leaf of small size and very thick texture; shape ovate, being apparently rounded at base and obtusely pointed at apex; margin entire 

at base, becoming strongly toothed above, the teeth being slender, 

sharp-pointed, and upward or outward turning; midrib rather slender, 

apparently zigzag; secondaries, three or four pairs, alternate, arising 

at a low angle and much curving upward, craspedodronie, entering 

the teeth, or forked and the branches entering the marginal teeth; 

finer nervation not observable.

This little leaf, the only one of its kind found in the collection, is 

evidently of thick texture, as the nervation can be made out with difficulty, It lacks both base and apex, but as nearly as can be determined its length was about 2 cm. and the width 1.5 cm.

1 am uncertain as to the generic relations of this leaf, and moreover 

the single example is hardly well enough preserved to warrant speculation on this point.

Locality. Willow Creek, Fergus County, Mont., about 12 miles 

north of Musselshell post-office and 1 mile east of road from Junction 

City to Fort Maginnis.

PHYLLITES INTKICATA n. sp. 

PI. XVIII, fig. 6.

The collection contains also another fragmentary example of a small 

leaf of doubtful affinity. It appears to have been rather membranaceous in texture, regularly ovate in shape with an apparently truncate 

or slightly cordate base and an acute apex. The margin is provided

« Flora, Montana formation; Bull, U. S, Geol, Survey No. 163, p. 55, PI. XIII, fig. 7.
.KNOWLTON.] FOSSIL PLANTS. 149

with a few relatively large, coarse teeth. The nervation is very thin, 

consisting of a slender, straight midrib, and two or three pairs of 

very thin secondaries which arise at an acute angle and are greatly 

curved upward, ending apparently in or just below the sinuses. The 

length of this little leaf was 2 cm. and the width about 1.25 cm.

This leaf suggests in a way certain herbaceous plants, but I am 

wholly at a loss as to its probable affinities, and simply present it in 

the hope that more material may subsequently be secured.

Locality. Willow Creek, Fergus County, Mont, about 12 miles 

north of Musselshell post-office and 1 mile east of road from Junction 

City to Fort Maginnis.

CARPITES JUDITHJE n. sp " 

PI. XVI, fig. 4.

Fruit evidently of firm texture, possibly a stone fruit; broadly 

obovate in shape, with a rather broad point of attachment and a regularly and obtusely rounded apex; fruit marked with numerous fine striae 

which arise at the apparent base, at which point they are slightly 

stronger, and after spreading slightly in the middle converge toward 

the apparent apex.

x The fruit here figured is all of its kind in the collection. It is perfectly preserved. It is rounded obovate, 14 mm. long and 11 mm. 

broad. It is provided. with numerous fine stride which converge at 

what is assumed to be the apex. The smaller end is presumed to be 

the point at which it was attached, as the stride or ribs are thicker at 

this place. Its affinity is unrecognized.

Locality. Willow Creek, Fergus County, Mont., about 12 miles 

north of Musselshell post-office and 1 mile east of road from Junction 

City to Fort Maginnis.

CARPITES PKTJNI n. sp.

PI. XV, fig. 6, 6a.

Fruit apparently of shelly or bony texture, broadly and obtusely 

ovate in shape, basal part rounded and apparently truncate; apex 

obtusely rounded; body of fruit marked with a marginal rib or thickened rim, and two or three longitudinal ribs.

This fruit is also, the only one of its form contained in the collection. 

It is broad or elliptical-ovate in shape, with a veiy broad base and an 

obtuse apex. The length is 13 mm. and the width 11 mm. It suggests in a remote way the stone of a Prunus, but its affinity is a matter of question.

Locality. Willow Creek, Fergus Countj7 , Mont., about 12 miles 

north of Musselshell post-office and 1 mile east of road from Junction 

.City to Fort Maginnis.
]50 THE JUDITH EIVEE BEDS. [BULL.257.

CAEPITES AIATUS n. sp. 

PI. XVI, fig. 2.

The collection contains two specimens of a very peculiar winged 

fruit that I am unable .to determine satisfactorily. The best example, 

shown in PI. XVI, fig. 2, is two-winged, the wings being broad and 

rounded, and separated by a deep, rounded sinus. The portion containing the nucleus extends as a long point, wingless (?) at the 

apex, but with the wings apparently arising below the apex 

and extending backward. The length over all is about 12 mm. and the 

greatest width about the same, the nuclear portion from the rounded 

sinus between the wings to its apex has a length of 6 mm., and the 

greatest width of the individual wings about 5 mm. In another 

example, which is presumed to be the same species, there is shown 

just one-half of the fruit, with the sharp-pointed nuclear portion and 

large rounded backward-extending wing. The dimensions are about 

the same as in the other. Neither shows any apparent point of 

attachment.

The other specimen, which has not been figured, is not unlike a 

single-winged coniferous fruit, such as Pinus, Abies, etc., while the 

figured one suggests the same, except that there is no evidence of a 

line of division between them, as should be the case if it is a double 

fruit. There seems to be only one nucleus or seed provided with a 

double wing in this specimen, but if the other example really belongs 

with it, it is probable that the idivision line is too obscure to be made out.

It is to be presumed that these are the fruits of a cone-bearing tree, 

possibly Pinus or something not greatly different, but in view of the 

anomalous features presented it is deemed best, .as the material is so 

scanty, to present it here under the name of Carpites and wait for 

future material to settle the question.

Locality. Willow Creek, Fergus' Count}', Mont., about 12 miles 

north of Musselshell post-office and 1 mile east of road from Junction 

City to Fort Maginnis.

DISCUSSION OF THE FLORA.

In 1900, when I published my paper entitled "Flora of the Montana Formation," I took occasion to describe a small collection of fossil 

plants from a point on the right bank of Missouri River about 7 

miles below the Coal Banks, just below the Great Bend of the Missouri. The beds whence these plants came were at the time supposed 

to be of Belly River age, as they appeared to be essentially in the 

position occupied by beds so called by the Canadian geologists, beyond 

the international boundary.

After setting forth briefly the then current though somewhat conflicting opinions regarding the areal extent and stratigraphic position
KNOWLTON.] FOSSIL PLANTS. 151

of the Belly River beds, I offered as an excuse for including the-plants 

in the Montana flora the contention of some writers, notably Dr. 

C. A. White, that these beds were synchronous in part at least with 

the Montana formation, instead of being wholly below it, as held by 

others. Subsequent events have proved that it was correct to include 

them in the Montana flora, though not within the Belly River beds as 

at present understood.

At the time my bulletin was in press Mr. W. H. Weed had in course 

of publication his Benton folio, a in which he separated the plantbearing beds in the vicinity of the Coal Banks under the name of the 

Eagle formation. He placed it between the Colorado and Montana 

groups, as separating them, but the subsequent investigations of 

Messrs. Hatcher and Stanton,& as already set forth in this bulletin, 

make it the lowest member of the Montana group, arid separated by

the Claggett formation from the Judith River beds, which are now

regarded as the complete equivalent of the Belly River beds.

The beds below the Coal Banks have afforded the following forms of 

plants:'

Thinnfeldia montana Knovvlton. 

Quercus? inontanensis Knowlton. 

Ficus missouriensis Knowlton. 

Juglans? missouriensis Knowlton.

Laurus? sp.

Liriodendron alatum Newberry MSS.

Hollick. 

'Platanua? wardii Knowlton.

As these plants were supposed at that time to belong to the Belly 

River beds, I assembled for purposes of comparison a list of all the 

known forms that have been found in beds regarded as of this age in 

the Canadian Belly River. The result was disappointing, for not one 

of the Coal Banks species was found to be identical with or to have 

special affinity with the Canadian Belly River, but on the other hand 

they did show an unmistakable affinity with the Dakota group, and 

two species (Thinnfeldia montana and Liriodendron alatum} were 

regarded as belonging to the true Laramie. The species of Liriodendron, with which the Coal Banks form seems identical, was described 

originally from very rich plant deposits at Florence, Colo., and while 

this material has not yet been worked up, I am of the opinion that it 

may prove to be older than the true Laramie, and on this point Doctor 

Hollick now agrees with me.

The other species (Thinnfeldia montana} I was not able to separate 

from examples found in the Laramie of the Bozeman coal field.

As regards the affinit}^ of the Coal Banks leaves with Dakota group 

forms, J probably underestimate rather than overestimate it; in fact, 

I should incline to regard what I then called Platamis f wardii as a

a Geologic Atlas of United States, folio 55.

bCf. Science, Aug. 1.4,1903, Vol. XVIII, pp. 211, 212.

c Flora Montana Formation, pp. 11-15, Pis. I, II. 
152 . THE JUDITH RIVER BEDS. [BULL.257.

species of Populites, possibly the same as Lesquereux's P. elegans a 

from the Dakota group at Fort Harker, Kans.; and further, it would 

not have done great violence to the facts had I identified my Ficus 

missouriensis with Ficus glascceana Lesq., and Laiirus sp. with Laurus 

knowltoni Lesq., both from the Dakota of Kansas.- There are slight 

differences, however, as I pointed out at the time, and it is perhaps 

best to regard them as distinct, at least until further material can be 

obtained.

So far as it seems possible to ascertain at the present time, it is 

more than likely that the Eagle formation will be found to be identical 

with the Dunvegan group of Dr. G. M. Dawson, 6 for the stratigraphic 

position, lithologic character, and fossil plants are similar.

From the Dunvegan group Sir William Dawson described c 19 

species of plants, of which number six or seven were regarded as 

identical with Dakota group species, and a number of others were 

quite close to forms well known in the Dakota. Although none of 

the species from the Dunvegan group are regarded as actually identical with those of the Eagle formation, there are several that are not 

distantly related.

Since the delimitation of the Eagle formation, which carried with it 

the only fossil flora supposed to belong to the Belly River beds south 

of the international boundary, there have been no known plant-bearing 

beds of this age in the .United States. The fortunate discovery by 

Messrs. Hatcher and Stanton of rich plant deposits in the Judith 

River beds on Willow Creek, Fergus County, Mont., about 12 miles 

north of Musselshell post-office and 1 mile east of the road from Junction City to Fort Maginnis, has now furnished a flora of at least 28 

forms, as follows: ''_

Fossil plants found in Judith River formation.

Fern, indeterminable.

Fern, indeterminable.

Osmunda montanensis n. sp.

Cyperacites? sp.

Sequoia reichenbachi (Gein.) Heer.

Sequoia heterophylla? Vel.

Sequoia sp.?

Thuja cretacea? (Heer) Newb.

Dammara acicularis n. sp.

Cunninghamites elegans (Corda) Endl.

Cunninghamites recurvatus Hos. and v.

d. M

Cunninghamites pulchellus n. sp. 

Populus cretacea n. sp. 

Populus sp.

Populites amplus n. sp. 

Betulites? hatcheri n. sp. 

Quercus montana n. sp. 

Quercus judithse n. sp. 

Sapindus inexpectans n. &p. 

Trapa? microphylla Lesq. 

Trapa? cuneata Knowlton. 

Diospyros judithse n. sp. 

Castalia stantoni n. sp. 

Phyllites denticulatus n. sp. 

Phyllites intricata n. sp. 

Carpites judithse n. sp. 

Carpites pruni n. sp. 

Carpites alatus n. sp.

a Flora Dakota Group, PI. XLVII, fig. 3. .

bQeol. Surv. Canada, Kept, of Progress, 1879-80 (1881), p. 116B.

cTrans. Roy. Soc. Canada, Vol. I, Sec. IV, pp. 20-23.
KNOWLTON.J FOSSIL PLANTS.

In order that this flora may be compared with that from the beds 

north of the international boundary, it will be desirable to first present 

a complete list of the latter as left by Sir William Dawson. The fol 

lowing enumeration is from Bulletin No. 163 (p. 15) and is believed to 

be complete:

Fossil plants found in Canada.

Pistia corrugate Lesq. (leaves).

Pinus or Abies, type of Pityoxylon

(Wood).

Sequoia, type of S. gigantea (Wood). 

Sequoia, type of S. sempervirens (Wood). 

Sequoia reichenbachi (Gein ) Heer 

 (leaves and branches). 

Thuja, type of T. occidentalis (Wood). 

Taxites, type of Taxus baccata (Wood). 

Ginkgo, type of G. biloba (Wood). 

Ginkgo? (fruit).. 

Lemna scutata Dawson (leaves).

Populus acerifolia Newb.? (leaf).

Populus latidentata Dawson (leaves).

Populus sp. (Wood).

Betula sp. (Wood).

ULmus sp. (Wood).

Gary a sp. (Wood).

Nel umbo dawsoni Hollick (Brasenia

antiqua Dawson) (leaves). 

Trapa cf. T. borealis Heer (fruit). 

Platanus nobilis Newb. 

Platan us ? sp. (Wood). 

Acer saskatchewense Dawson (leaf).

Much of this material is in the form of wood that has never been 

completely studied and is consequently of little value in an attempt to 

fix the age. If all of the remaining forms were correctly determined 

it would show the presence of a very remarkable association of species, but, as I have before suggested, it is more than likely that more 

than one horizon is represented. A reexamination of the evidence 

offered by Dawson leads me to place even less" confidence in the determinations, since it shows how meager and uncertain much of the evidence was. Thus, of the presence of Platanus nobilis in the same beds 

(near Medicine Plat) with Nelumlo dawsoni, Pistia corrugata, Lemna 

scutata, Trapa, etc., he says: a "There are also fragments of the great 

leaves of Platanus nobilis and the Populus and Acer described below." 

So far as I can find, this is the only mention of material referred to 

this species, yet in subsequent mention it takes its place in lists and 

elsewhere with unquestioned value. So also with Populus acerifolia 

Newb., the only mention of which is under his P. latidentata^ where 

he states that "in the same matrix with the above are fragments of 

leaves of another Populus, of the t}7 pe of P. acerifolia Newberry." 

Both of these species are typically Fort Union, and have never, so 

far as I know, been authentically identified in older beds, and 1 am 

consequently of the opinion that the present evidence is not sufficient to warrant regarding them as species of the Belly River or 

Judith River beds.

After dropping Platanus nobilis and Populus acerifolia^ as seems 

warranted, we have left but three duly authenticated species in the 

Canadian Belly River beds that enjoy an outside distribution, viz:

n Trans. Roy. Soc. Canada, Vol. Ill, Sec. IV, p. 16,1886. 

b Op. cit., p. 16. 
154 . . THE JUDITH BIVER BEDS. [BULL.257.

Pistia corrugata, which occurs in the Montana at Point of Rocks, Wyoming; Sequoia reichenbachi, which occurs widely throughout the 

Cretaceous of nearly all parts of the world, and Lemna scutata, which 

was described originally from the "Lignite Tertiary" near the fortyninth parallel, and subsequently detected by Professor Ward in the 

Fort Union at Burns ranch, Montana, and by Dawson in the Laramie 

at Wood Mountain and Pincher Creek, British Columbia. Lesquereux 

reported it from Point of Rocks, Wyoming, but, as I have shown in 

Bulletin No. 163," one of the examples he so identified is a small leaf of 

Pistia corrugata and the other a Nelumbo (N~. intermedia Knowlton).

As to the affinities of the other named species, it may be mentioned 

that Nelumbo dawsoni is very closely allied to my JV. intermedia f rom 

Point of Rocks, Wyoming, while the other two species (Populus latidentata and Acer saskatchewense) are not figured, nor are they described 

with sufficient fullness to permit of satisfactory comparison with other 

forms.

Turning now to the species described in this paper, mainly from 

Willow Creek, Montana, the reader will observe that the most striking 

feature of the list is the preponderance of conifers shown, since 8 of 

the 28 forms, or nearly one-third, belong to this group, and when the 

actual number of individual specimens is considered it is safe to say 

that fully nine-tenths belong to these species; and it may be added that 

the only species common to the Willow Creek locality and the Judith 

River beds north of the international boundary is /Sequoia reichenlachi. 

This species, as already pointed out, is exceedingly abundant at the 

Montana locality, and Dawson speaks b of it as being abundant also 

at Medicine Hat in the Canadian beds of this age. It is possible that 

if the dicotyledons described by Dawson were illustrated they would 

show affinity with some of those I have described from Willow Creek, 

but this can not be determined now.

Of the 28 forms enumerated in this paper the following species 

enjoy an outside dispersal:

Sequoia reichenbachi. 

Sequoia" heterophylla? 

Thuja cretacea?

Cunninghamites elegans. 

Trapa? microphylla. 

Trapa? cuneata.

Cunninghamites recurvatua.

As already mentioned, the first species (Sequoia reichenbachi) is very 

widely dispersed throughout the Cretaceous, occurring more or less 

abundantly in this country from the Potomac to the Livingston beds. 

Sequoia heterophylla, described originally from the Cenomanian and 

Senonian of Bohemia, has been found abundantly in the Amboy clays 

and sparingly at a number of other Upper Cretaceous localities. 

Thuja cretacea was first known from the Ataneschichten of Greenland,

« Flora Montana formation, p. 31.

6Trans. Roy. Soc. Canada, Vol. Ill, Sec. IV, p. 17 (under Salisbwia).
KNOWLTON.] FOSSIL PLANTS. 155

and has been found by Newberry in the Amboy clays, while Cunningkamites elegans occurs in the upper part of the Amboy claj^s, in the 

Patoot beds of Greenland, and in the Upper Cretaceous of Moravia, 

Bohemia, and Westphalia. Of the two species of Trapa, T. cuneata is 

known only from, and T.'m.icrophylla originally from, the Montana at 

Point of Rocks, Wyoming. As set forth under T. microphylla (p. 145), 

it has been found also in the true Laramie and in the Fort Union.

Of the species that 1 have described as new, Dammara acicularis is 

perhaps nearest to D. microlepis Heer, from the Atane and Patoot 

beds of Greenland, and also under the name of Eucalyptus geinitzi 

from the Cenomanian of Moravia and the Upper Cretaceous of Bohemia and Marthas Vineyard. Cunninghamites pulchellus seems to be 

nearest to 0. recurvatus, the distribution of which has already been 

given. The affinities of Populus cretacea are uncertain, but are perhaps closest with certain forms of Quercus described by Hoseus and

von d. Marck from the Upper Senonian of Westphalia, while Populus 

sp. is very suggestive of forms of this genus, such as P. rotundifolia, 

from the Fort Union beds. The single large leaf that I have described 

as Populites amplus is quite closely related to certain species of this 

genus from the Dakota group, and Betulites hatcheri is close to B. 

westii Teniformis Lesq., and Qu&rcus inontana approaches Q, suspecta 

Lesq., both from the Dakota. Sapindus inexpectans, based on a single 

small leaflet, has no very definite relationship, while the species of 

Phyllites and Carpites&r&m much the same state. Diospyrosjudithse 

is very suggestive of D. kansaseana Lesq., or more particularly D. 

primaeva Pleer, from the Dakota of Kansas and Nebraska, while the 

large leaf described as Castalia stantoni is quite unlike anything thus 

far obtained in this country.

From this review it appears that the flora of the Judith River beds 

that has thus far come to light shows very little affinity with the true 

Laramie or the Fort Union, but does exhibit an undoubted relationship with that of the.Dakota group or with the Cenomanian and 

Senoniau of the Old World, or, in broad terms, with the lower and 

middle portions of the Upper Cretaceous.

PLATE XIY.

157
PLATE XIV.

Page. 

Fig. 1. Fern, indeterminable, enlarged 3 times ............................. 129

Fig. 2. Sequoia sp.?. .......................................................^ 131

Figs. 3, 4, 5. Sequoia reichenbachi (Gein.) Heer............................ 131

Fig. 6. Osmunda montanensis n. sp., enlarged 2 times ........:............. 129

158
U. S. GEOLOGICAL SURVEY 1ULLETIN NO. 257 PL. XIV

JUDITH RIVER PLANTS.
PLATE XV.

159
PLATE XV.

Fig. 1. Cunninghamites elegans (Corda) Endlicher ......................... 135

Figs. 2-5. Dammara'aeicularis n. sp ....................................... 134

Fig. 6. Carpites pruni n. sp ............................................... 149

Fig. 6a. Carpites pruni n. sp., enlarged 3£ times............................ 149

Fig. 7. Fern, indeterminable, enlarged 3 times .............................. 129

160
U. S. GEOLOGICAL SURVEY BULLETIN NO. 257 PL. XV

JUDITH RIVER PLANTS.
PLATE XVI.

Bull. 257 05 11 161
PLATE XVI.

Page.

Fig. 1. Cunningharnites pulchellus n. sp................................... 136

Fig. 2. Carpites alatus n. ep............................................... 150

Fig. 3. Thuja cretacea? (Heer) Newberry .........................;........ 133

Fig. 3a. Same enlarged 3 times............................................ 133

Fig. 4. Carpites judithse n. sp.........................................'..... 149

Fig. 5. Sequoia heterophylla? Vel.....--..-...........--..--.-.-......-... 132

Fig. 6. Cunninghamites recurvatus ? Hosius and von der Marck ............. 136

162 .
U. 8. GEOLOGICAL SURVEY BULLETIN NO. 2o7 PL. XV

JUDITH RIVER PLANTS.
PLATE XVII.

163
P. LATE XVII.

Page. 

Figs 1-5. Populus cretacea n. sp........................................... 138

Fig. 6. Quercus montana n. sp.............................................. 143

Fig. 7. Sapindus inexpectans n; sp......................................... 144

164
U. S. GEOLOGICAL SURVEY BULLETIN NO. 257 PL. XVII

JUDITH RiVER PLANTS.
PLATE XVIII.
PLATE XVI11.

Page. 

Fig. 1. Populites amplus n. sp............................................. 140

Fig. 2. Quercus judithse n. sp ............................................. 143

Fig. 3. Betulites? hatcheri n. sp ....... ................................... 141

Figs. 4, 5. Diospyros judithse n. sp ........................................ 146

Fig. 6. Phyllites intricata n. sp............................................ 148

166 , .
JUDITH RIVER PLANTS.
PLATE XIX.

167
PLATE XIX.

Page. 

Fig. 1. Populus sp ...............-..------..-.-..............--...----.-. 140

Fig. 2. Phyllites denticulatus n. sp ........................................ 148

Fig. 3. Diospyros judithse n. sp.................. ^........................ 146

Fig. 4. Castalia stantoni n. sp............................................. 147

168 .
U. S. GEOLOGICAL SURVEY BULLETIN NO. 257 PL. Xl>

JUDITH RIVER PLANTS. .
INDEX.

Names in italic are synonyms; figures in black-face type denote pages on which descriptions are 

given; italic figures refer to illustrations.

A. Page. 

Abies....................................... 153

Acer saskatchewense Dawson............ 153-154

Acipenser albertensis Lambe ........... 50-51,60

Acmtea occidentals Meek and Hayden.... 58

Adocus lineolatus Cope..................... 75-70

Amphibia .................................. 69-71

Anchnra americtina Evans and Shumard.. 14,

45,55,57 

Anisomyon alveolus Meek and Hayden.... 45

centrale Meek.......................... 14,45

Anodonta parallela White ................. 107

propatoris White................ 46,54,57,107

sp....................................... 38

Anornia gryphorhyncus Meek.............. 41,

44,48,104,105,120

micronema Meek....................... 100

sp....................................... 40

Arapahoe formation, mention of........... 29

Assiniboia, section in ..........'...... 52,53,54, C3

Aublysodon mirandus Leidy............ 50,83-84

Austin formation, Niobrara correlated with. 11

fossils of................................ 11

Aves........................................ 99

Avicula linguiformis Evans and Shumard. 14,

47,55,57,58

nebrascana Evans and Shumard....... 14,

39,55,58,100

subarcutus Meek and Hayden.......... 10G

B.

Baculites asper Morton (?)........... 11,25,52,60

compressus Say ...... 13,14,44,45,47,64,55,58

ovatus Say.............................. 13,

14,37,39,41,44,45,48,49,53,54,56,58 

sp .............. 12,13,15,16,37,39,44,45,56,57

Badlands of Judith River, character and

location of................... 16,31-32

view of................................. 46

Baena antiqua Larnbe..................... 78-71)

hatcheri Hay........................... 7!)

Baroda sp ............................ 12,36,37,39

Basilemys imbricarius (Cope) .............. 77

ogmius (Cope)......................... 70-77

Batrachia................................... C9-70

Bean Creek, Judith River beds on.......... 61

Bearpaw Mountains, formation named

'from.............'............... 13,14

Bearpaw shales, correlation of.......... 14,63-65

fossils in.................... 14,45,47,54,55,58

occurrence and character of........... 13-14,

33,40-44,47,48,49,53-55,57-58,60,62

Page. 

Bearpaw shales, view of .............. 44, 4G, 48, 54

Beaver Creek, exposures on ................ 47

Belly River beds, character of .......... 23, 24, 27

correlation of ................... 9, 22, 27, 62, 63

identity of Judith Hi ver beds and ...... 66

occurrence of ........................... 24-27

Benton shales, correlation of ............ 63, 64, 66

fossils of..... ........................ 11,45,60

naming of .............................. 18-19

occurrence and character of ........... 11-32,

40,41,45,56,60,62,64 

Betulasp. (woodof)............ ............ 153

Betulites ? hatcheri Knowlton, n. sp....... 141,

152,1 55, 166 

Billings, Mont., Judith River beds near. ... 61

Birch Creek, Judith River beds on and

near ............................ 38-41

. location and character of .............. 38-39

view on ................................. 38, 40

Bitter Creek beds, inclusion of, in Laramie,

by White ....................... 26-27

Black Butte, Mont., Judith River beds in . . 51 

Black Diamond Coal Co., mines of......... 48

Boreodon matutinus:Lambe ............ 100-101

jaw of, figure showing ................. 100

Bottosaurus perrugosus Cope ............... 82

Boxelder Creek, Judith River beds on ..... 48

Brasenia antiqua Dawson .................. 153

Browns Coulee, Judith River beds on ...... 50

Bulinus atavus White...................... 119

subelongatus Meek and Hayden ....... 118

Callista deweyi Meek and Hayden. . . 14, 36, 53, 54 

nebrascensis Meek and Hayden ........ 55

sp ...................................... 39

Campeloma multilineata Meek and Hayden............................. 114

producta White...................'..... 114

vetula Meek and Hayden ..... 41, 50, 1 14, 122

Canada, Judith River plants from. . ........ 163

Cardium speciosum Meek and Hayden. . . . 10,

12,13,20,36,37,39,44,52 

Carpites alatus Knowlton, n. sp. . . . . 150, 152, 162

judithte Knowlton, n. sp........ 14!), 152,762

pruni Knowlton, n. sp .......... 149, 152, 760

Carya sp. (wood of) .................. ..... 153

Castalia stantoni Knowlton, n. sp ..... 147-148,

152, 155, 168 

Cephalopoda ............................... 119

Ceradotus crucif erus Cope ................. 08

hieroglyph us Cope ..................... 08

169
170 INDEX.

Page. 

Ceratops Marsh............................ 93-94

belli (Lambe) .......................... 95

canadensis (Lambe).................... 94

montanus Marsh ................... 42,43,94

paucidus Marsh........................ 96

recurvicornis (Cope)................... 94

validus Lambe ......................... 96

sp ................................ 38,50,51,59

..Ceratopsidae........................ 89-96,101-103

Champsosaurus Cope....................... 80

annectens Cope ....................... 80

brevicollisCope...... ................ 80-81

profundus Cope ........................ 80

vaccinsulensis Cope................... 81-82

Chelonia ................................... 72-80

Cimoliasaurus rnagnus Leidy .............. 71

Cinulia concinna Meek and Hayden.... 14,55,58

sp ....................................... 45,57

Cionodon (Cinodon) Cope.................. 99

stenopsis Cope.......................... 99

Claggett formation, correlation of ...... 63,65,66

fossils of.................... 13,37,39,40,44,56

occurrence and character of........... 13,

25,33,36,37-38,39,40,41,44-45,

47, 49, 50, 51, 53, 56, '57, 60, 62

view of ................................. 40,48

Claorhyncus trihedrus Cope................ 96

Coal, occurrence of......................... 48,61

Coalville, Utah, coal at..................... 61

Coculus haydenianus Ward ................ 58

Colorado group, subdivisions of............ 63

Colorado shales, occurrence and character

of............................... 11

Compsemys imbricarius Cope................ 77

obscurus Leidy.......................... 79

ogmius Cope............................ 70

variolosus Cope........................ 76-77

viclus Leidy ............................ 79

Coniornis al tus Marsh ...................... 99

Cope, E. D.,fossil found by................. 40

on Belly River beds .................... 28

on Judith River beds..................; 20-22

on vertebrate fauna of Judith River

beds............................ 20-21

Corbiculacytheriformis Meek and Hayden. 33,

38,41,44,48,52,104,111-112,120

occidentalis Meek and Hayden... 44,111,120

sp ...................................... 40

Corbula perundata Mee.k.......... 50,52,113,120

subtrigonalis Meek .................... 33,38,

44,47,52,53,104,113,120 

sp ...................................... 40,52

Cow Creek, Mont., dinosaur remains in

Eagle formation on............. 12

fault on................................. 43

fossils on................................ 45

Judith beds on and near ............ 40-45,61

location and character of............... 41-42

sections on .......................... 42,44-45

view on.................................. 42-44

Crenella parvula VVhiteaves................ 106

sp ...................................... 12

Cretaceous, Upper, assignment of Judith

Riverbeds to.................... 9,02

stratigraphy of, in Judith River region. 11-14

Crocodilia............................. 82,102-103

Page. 

Crocodilus humilis Leidy.................. 38,82

Cross, Whitman, on Judith Paver beds..... 29

C tinning/lamia elegans. ...................... 135

Cunninghamites elegans (Corda) Endlicher ............ 135,152,154-155, 160

pulchellus Knowlton, n. sp ........ 136-138,

152,155,162

recurvatos? Hosius and vender Marck. 136, 

152,154-155, 162

Cuspidaria ventricosa (Meek and Hayden). 58 

Cypcracites sp........................ 130-131,152

Cyprina ovata Meek and Hayden .......... 53,54

D.

Dakota formation, position of.............. 63

naming of.............................. 18-19

Dammara acicularis Knowlton, n. sp.. 134-135,

152,155, 160 

Dana, E. S., on Judith Riverbeds.......... 21,34

Dawson, G. M., on Belly River fossils........ 25,62

on Judith River region.............. 21-22,24

Dawson, William, on Belly River fossils.... 25

on Dunvegan sandstone................ 152

Deinodon Leidy............................ 38,85

.cristatus (Cope) ........................ 86

explanatus (Cope)...................... 86

falculus (Cope)......................... 86

hazenianus (Cope) ..................... 86

horridus Leidy ......................... 83

incrassatus (Cope)..................... 85-86

lateralis (Cope)......................... 85

laevifrons (Cope)........................ 86

Denver formation, Cross on age of.......... 29

Diclonius Cope............................. 99

Dinosauria...................... 83,83-84,102-103

Diospyros judithaeKnowlton, n. sp..... 146-147,

152,155, 166,168 

Diphyodus longirostris Lambe .........:.... 69

Dog Creek, Mont., fossils of Eagle formation on ......................... 36

Judith River beds on................... 34-38

location and character of............... 34-35

rocks on................................ 12

section on .............................. 37

view on................................. 36

Douglass, Earl, on Fish Creek beds......... 30,59

Dunvegan sandstone, correlation of.... 22,23,152

Dysganus Cope............................. 90

E.

Eagle Butte, Mont., rocks near............. 12

Eagle Creek, Mont., formation name derived from...................... 12

view on................................. 12

Eagle formation, correlation of ......23,63,66,152

fossils of....................... 12,36,37,39,57

occurrence and character of........... 12-13,

24-25, 27,31,36, 39,40,42, 45,56,57,60,62

view of........................... 12,36,38,42

Emys....................................... 38

F. 

Ferns......................... 129-130,152, 158,160

Ficus missouriensis Knowlton.............. 151

Fish Creek, Mont., Judith River beds near. 59-60
INDEX. 171

Page. 

Fish Creek, Mont., view on................. 58

Fish Creek beds, correlation of............. 59,66

location and character of ........... 30,59-60

Flatwillow, Mont., rocks near.............. 56

Flotwillow Creek, Judith River beds near. 56 

Florence, Colo., liriodendron from...'...... 151

Fort Ben ton, Mont., formation name derived from...................... 11

Fort Benton formation. See Ben ton shales. 

Fort Pierre formation. SeePierre formation. 

Fort Union formation, naming of.......... 19

occurrence of..................... 14,26-27,59

Fossils,.invertebrate, description of...... 104-123

plates showing........................126,128

Fossils, plant, description of............. 129-155

 plates showing ....................... 158-166

Fossils, vertebrate, description of......... 67-103

figures of ............................... 100

Fox Hills formation, correlation of ........ 64,66

fauna of, occurrence of.............. 10,13,20

naming of.............................. 19

occurrence of........................... 23,63

G. 

Gasteropoda................... 16,113-119,120-121

Geologic history, re'sumc' of later Cretaceous ........................... 122-123

Geology of north-central Montana and adjacent areas, sketch of.......... 11-66

Gervillea borealis Whiteaves......... 13,39,44,45

Gingko biloba..............'................ 153

sp....................................... 153

Goniobasis convexa Meek and Hayden.... 38,

44,48,104,110,120

convexa var. impressa Meek and Hayden.......................... 116,120

gracilenta Meek.................. 44,116,122

invenusta Meek and Hayden........... 41,

43,46,51,52,116 

judithensis Stanton, n. sp .............. 43,

46,51,117,122,^5 

omitta Meek............................ 116

subltevis Meek and Hayden.. 41,51,55,57,116 

subtortuosa Meek and Hayden.. 44,46,51,117 

sp....................................... 38

Grinnell, G. B., on Judith River beds...... 21,34

H.

Haminea subeylindrica Meek and Hayden. 58 

Hatcher, J. B., death of.................... 9

on Ceratops beds........................ 28

on Judith River beds................ 30,31,43

on vertebrate fauna................... 67,103

work of.................................. 9-10

Havre, Mont., Judith River beds near..... 45-48,

60,62 

rocks near.............................. 10

view near............................... 46,48

Hay, 0. P., on Judith Riverbeds........... 31

Hayden, F. V., on Judith River beds....... 14-20,

31-32,34,61 

Hayes, C. W., letter of transmittal by ...... 7

Hector, James, on Judith River region..... 21

Hedronchns sternbergii Cope .............. 69

Helix vetnsta,, Meek and Hayden.......... 117

Hemitrypus jordanianusCope ............. 71

Page.

Hettangiq americana Meek and Hayden'.... 15,16 

Hyalina evansi, Meek and Hayden.... 44,50,117

occidentalis, Meek and Hayden. 43,50,54,118 

Hydrobiasubconica, Meek................. 115

subeylindrica, Whiteaves............... 115

I. 

Ignanodon ................................. 16,18

Inoceramus barabini Morton ........ 14,45,56,58

exogyroides Meek and Hayden..... 11,60,64

fragilis Hall and Meek................. 57

labiatus Schlotheiin.................... 11,64

sagensis Owen.................... 14,46,48,54

umbonatus Meek and Hayden...... 11,60,64

sp.............................. 16,37,41,45,47

Insecta ..................................... 119

Ischyrotherium cf. antiquum, Leidy ... 38,42, 72

J.

Judith, Mont., rocks near.................. 12,13

Judith River, badlands of, location and

characterof................. 16,31-32

Judith River beds, age of................ 17,31,66

area of on Missouri River .............. 32-33

character of.......................... 13,33-34

correlation of............ 9-10,14-31,62,66,155

description of, by areas................. 31-61

identity of Belly River beds and ....... 66

marine fossils in........................ 42

name of ................................ 16,19

sections of................. I 37,42,44,49,52,54

description of....................... 17

study of................................. 9-10

. history of........................... 14-31

views of.......'.......... 40,42,44.46,48,54,58

Judith River region, geologic history of.. 122-123 

Juglans missouriensis Knowlton........... 151

K.

Knowlton, F. H., on Eagle formation fossils ............................. 29

on Fort Union fossils................... 58

on Judith River fossils ............ 57,129-155

work of................................. 9

L. 

Lxlaps. ..................................... 51,85

cristatus Cope........................... 86

. cxplanatus Cope ........................ 86

falculus Cope ........................... 86

hazenianus Cope...................... . 86

incrcssatus Cope........................ 85

lusvifrons Cope.......................... 86

Lambe, L. M., on Belly Riverbeds......... 30

on Judith River fossils ................. 67

Laramie formation, correlation of ...... 26,63,66

occurrence of........................ 14,69,61

fossils of, compared with Judith Rjver

fauna................. 101-102,120-121

Laurus ? sp ................................. 151

Leda (Yoldia) evansi Meek and Hayden... 14,

44,45,55,58 

sp..................................... 42,106

Leidy, Joseph, on Judith River palcontol-

 ogy ..................... 15,18,23,24,67

work of................................. 16
172 INDEX.

Lemna scutata Dawson................... 153-154

Lepidotus.haydeni Leidy................... 68

occidentals Leidy.................. 18,38,67

Leptosolen sp............................ 12,37,39

Lewis and Clark, description by............ 14

Libocedrus cretac'Ta Heer .................... 133

Lignite, occurrence of, in Eagle formation. 12

in Judith River beds ................ 19,33,.51

view of................................. 44

Lindgren, W., on Laramie of Montana..... 28,61

Liopistha (Cymella) undata Meek and

Hayden.. 13,14,39,42,43,44,47,58,112 

Liriodendron alatum Newberry............ 151

Literature, historical sketch of............. 14-31

Little Rocky Mountain Creek, rocks on .... 16,17

Livingston formation, mention of.... 14,58,59,61

Lloyd, Mont., Judith River beds near...... 61

Lucina occidentalis Morton................ 56

subundata Hall and Meek .... 14,45,65,57,58 

Lunatia occidentalis Meek and Hayden ... 58

subcrassa Meek and Hayden........... 13,

36,37,39,43,44,52

sp.................................. 42,45,113

M.

McConnell, R. G., on Belly River beds..... 26

on Dunvegan sandstone................ 22

Mactra (Cymbophora) alta, Meek and Hayden ............ 10,12,13,20,36,37,112

(cymbophora) warrenana Meek ......... 112

formosa Meek and Hayden.... 13,20,36,39,50

gracilis Meek and Hayden ............. 14

warrenana Meek and Hayden..... 42,43,112

sp....................................... 16,52

Mammalia................................ 100-101

Marsh, 0. C., on Ceratops beds............. 28

on Judith River fossils ................. 67

Meek and Hayden, on Judith River geology

and paleontology............ 14-20,24

section by .............................. 63

Megalosanrus............................... 16,18

Meili Coulee, fault on ...................... 49-50

Judith River beds on................... 49-50

sections on ............................. 49

view on ................................ 48

Melania insculpta (Meek) Whiteaves ........ 115

whiteavesiStanton, n. sp. 53,115-116,120, 128 

sp....................................... 16

Melville, Mont., Judith River beds near... 59 

Milk River, Judith River beds on and near. 46-53,

61,62 

location and character of.............. 51

rocks on................................ 25

sections on ............................. 52

view on................................. 46

Missouri River, view on............ '........ 38,40

Modiola meekii Evans and Shumard ...... 47

sp................................. 52,106,120

Mollusca ................................. 104-122

Monoclonius Cope.......................... 90

crassus Cope............................ 40,91

dawsoni Lambe ........................ 91-03

flssus Cope.............................. 93

sphenocerus Cope ...................... 93

sp....................................... 38

Monospondylus gigas Cope................. 96

Page.

Montana, general section of upper Cretaceous in ........................ 63

Montana group, subdivisions of............ 63

Mud Creek, Mont., Judith Riverbeds near. 59-60 

section on .............................. 60

Musselshell River, Mont., Judith River

beds near....................... 56

location of.............................. 32

rocks near.............................. 14,15

Myledaphus bipartitus Cope ............... 38,68

Mytilussp.................................. 120

N. 

Natica...................................... 16

Nautilus dekayi Morton.................... 54,57

Nelumbo dawsoni Hollick................ 163-154

Neritina sp............................ 52,113,120

Neurankylus eximius Lambe.............. 79-80

Niobrara formation,'correlation of. 22,23,63,64,65 

naming of.............................. 19

occurrence of..................... -...... 11

Nucula cancellata.......................... 44,58

planimarginata......................... 58

subplana ............................... 58

sp.................................. 42,57,106

0.

Ornithomimus altus Lambe ............... 87-88

grandis Marsh....................... 12,41,87

tenuis Marsh............................ 87

Ornithopoda............................... ^ 96-99

Osborn, H. F., on fauna of Belly River beds. 30-31 

on Judith River fossils ................. 67

Osmundamontanensis Knowlton, n.sp. 129-130,

152,i5S

Ostrea glabra Meek and Hayden..... 53,105,120

patina Meek and Hayden..... 14,46,47,53,54

pellucida Meek and Hayden ........... 58

subtrigonalis Evans and Shumard...... 33,

38,40,41,44,47,48,49,50,53,104-105,120 

sp..... ................................. 42

P.

Pakowki Coulee, rocks on.................. 52

Paleeoscincus............................... 102

asper Lambe........................... S8-89

costatus Leidy.......................... 50,88

sp....................................... 42

Paludina................................... 16

Panopaea sirnulatrix Whiteaves...... 44,112,120

Paronychodon lacustris Cope .............. 84

Pecten (Chlamys) nebrascensis Meek and

Hayden ........................ 55,58

sp....................................... 57

Pelecypoda ............................... 104-113

Pendant d'Oreille, Canada, rocks near..... 51-52

section near............................ 52

view near............................... 48

Pholadomyapapyracea Meek and Hayden. 11,60 

sp................................. 12,16,37,39

Phyllites denticulatus Knowlton, n. sp..... 148,

152, 168

intricata Knowlton, n. sp... 148-149,152, 166 

Physa copei White........... 43,44,46,50,118,122

sp....................................... 38,54

Pierre formation, correlation of...... 14,63,64-66
INDEX. 173

Page.

Pierre formation, fauna of, occurrence of.. 10,55 

naming of.............................. 19

occurrence of........................... 23

Finns....................................... 153

Pisces ...................................... 67-69

Pistia corrugata Lesquereux............... 153', 154

Placenticeras intercalare Meek and Hayden ....................... 14,48,64,58

whitfieldi Hyatt........................ 12,

14,37,39,41,43,45,46,47,48,49,53,54,58 

sp............................ 37,42,50,57,119

Planorbis(Bathyomphalus)amplexusMeek

and Hayden .................. 44,118

paucivolvis Whiteaves.................. 118

sp....................................... 38

Plastomenus coalescens Cope................ 74

costatus Cope........................... 74

insignis Cope ........................... 75

punctulatus Cope....................... 74

Platanus nobilis Ncwberry ................. 153

wardii KnowHon....................... 151

sp (wood of)........................... 58,153

Plesiosauria ................................ 71-72

Polythorax missuriensis-Cope ............. 77-78

Pdpulites ampins Knowlton, n. sp...... 140-141,

152,154, 166 

Populus acerifolia Newberry ?..,........'... 153

cuneatns Newberry..................... 58

cretacea Knowlton,n.sp. 138-140,152,155,167 

latidentata Dawson .................. 153-154

speciosa Ward.......................... 58

sp........................... 140,152,155, 168

Porcupine Hills formation, occurrence of.. 22-23 

Predentata.............................. 88-89,102

Prionocyclus ............................... 64

Prionotropis................................ 45,64

Protocardia borealis Whiteaves ............ 55

rara Evans and Shumard................ 58

Pteria (Oxytoma) ncbrascana Meek.......... 106

Pteropelyx grallipes Cope................ 98,102

Ptilodus primaevis Lambe.................. 100

Q.

Quercus Judith® Knowlton, n. sp...... 143-144,

152, 166

montana Knowlton, n. sp... 143,152,155, IG/t 

? montanensis Knowlton ............... 151

11. .. ' .

Red Deer River, Assiniboia, fossilson...... 55

Reptilia .................................... 71

Rhyncocephalia............................ 80-82

Rhyptophorus ? glaber Whiteaves.... 52,117,120

S.

Sage Creek, Assiniboia, Judith River beds

on .............................. 53-55

location and character of .............. 53

section on .............................. 54

view on ................................ 48

St. Mary River beds of Canadian Laramie,

mention of ..................... 22-23

Sapindus granditolius Ward................ 58

iuexpectans Knowlton...... 144, 152,155,^64

Sauropoda.................................. 102

Scapherpeton Cope......................... 70

Page. 

Scapherpeton excisum Cope ................ 70

favosurn Cope.......................... 70

laticolle Cope ....................'...... 70

tectum Cope ........................... 69,70

Scaphites hippocrepis (Dekay)............. 57

nodosus Owen....................... 11,14,45

var. brevis Meek.................... 58

var. quadrangularis Meek and Hayden............................. 65

subglobosns Whiteaves................. 45

ventricosus Meek and Hayden... 11,45,60,64 

warreni Meek and Hayden.......... 11,25,64

Sequoia gigantea (wood of) ................ 153

heterophylla? Velenovsky......... 132-133,

152,154,262 

reichenbachi (Geinitz) Heer........... 131,

152-154, 158 

sempervivens (wood of)...............- 153

sp........................... 131-132,152, 158

South Dakota, Cretaceous section in ....... 63

South Platte Valley, Fox Hills fauna of.... 20

 Sphajriola ehdotrachys Meek............... 13,39

Sphcerium formosum Meek and Hayden V.. Ill 

plannm Meek and Hayden............. 41,

43,44,46,50,51,53,111,122 

recticardinale Meek and Hayden ...... 41,

43,44,51,111 

sp. ........... :....................... 38,54,57

Stanton, T. W., on invertebrate fauna.... 104-123

on Judith River beds................... 30-31

section on Dog Creek, Mont., by........ 29

work of................................. 9-10

Stegoceras validus Lambe.................. 95

Stegosauria............................... 102-103

Stereocephalus Lambe ................... 102-103

tutus Lambe ........................... 89

Sternberg, C. H., on Judith River beds..... 3.1

Stratigraphy of Judith River beds ......... 11-14

Sweetgrass Hills, rocks of.................. 25

Swimming Woman Creek, Mont., Judith

River beds on................... 61

Syncyclonema rigida Hall and Meek ...... 58

T.

Tancredia americana Meek and Hayden... 10,

13,15,16,20,37,39,40,44,50,52,53,55

Taxites baccata ............................ 153

Taxodium occidentalis Newberry.......... 58

Tellina equilateralis Meek and Hayden. 13,39,44 

montanaensis (Whitfield)...........;.. 36

sp ............................ 16,42,52,53,112

Thaumastus linnajiformis, Meek & Hayden ............................. 118

Theropoda ......................... 85-88,102-103

Thetis? circularis Meek and Hayden ...... 12,

14,37,39,45,58 

Thinnfeldia montana Knowlton ........... 151

Thracia gracilis Meek and Hayden ........ 13

Thuja cretacea? (Heer) Newberry......... 133,

152,154, 162 

occidentalis (wood of).................. 153

Torosaurus .................................. 102

Trachodon Leidy........................... 90

altidens Lambe......................... 98

breviceps (Marsh)...................... 97

marginatus Lambe ................ 97,98
174 INDEX.

Page. 

Trachodon mirabilis Leidy ...... 43,50,96-97,98

selwyni Lambe ........................ 97, 98

sp ............................. 38,51, 5k, 57,59

Trachodontidae .................... 96-99,101,102

Trapa borealis Heer........................ 153

cuneata Knowlton...... 145-140,152,154-155

microphylla Lesquereux...........;... 44,

144-145,152,154-155 

Trigonarca exigua. ........................ 58

Trionyx foveatus Leidy.................... 72-73

vagans Cope............................ 73

sp ................................... 16,18,38

Troodon formosus Leidy ................... 83

Tyrrell, J. B., on Belly River beds. ........ 26

U.

Ulmus rhamnifoliaWard................... 58

sp....................................... 153

Unio consuetus Whiteaves ................. 110

cryptorhynchus White .............. 109,122

danse Meek and Hayden ............... 43,

44,46; 54,108-109,122 

deiveyanus Meek......................... 108

primsevus White......;............ 43,44,110

priscusMeek and Hayden?. 51,52,108,122, 1Z6 

var. abbreviatus Stanton........ 108, 126

senectns White ......................... 110

subspatulatusMeek and Hayden. 52,107, 1Z8 

supenawensis Stanton, n. sp . 46,109,122, 1$8 

supragibbosus Whiteaves............. 52,110

sp..................... 38,50-52,54,57,110,122

Uronaites cetiformis Cope.................. 72

V.

Valvata? montanaerisisMeek.......... 43,44,115

Vauikoropsis tuoraeyana Meek and Hayden............................. 13,53

Page. 

Velatctta baptista (White) Whiteaves......... 113

Vertebrates, description of, by J. B.

Hatcher ....................... 67-103

Vitrina? obliqua Meek and Hayden........ 118

Viviparus conradi Meek and Hayden .... 44,113

sp.................................. 51,53,113

W.

Ward, L. F., work of, on Missouri River ... 27

Weed, W. H., on Crazy Mountain region ... 29,61

on Eagle formation.................... 29,151

on Li vingston formation ............... 58

work of................................. 10,12

White, C. A., on Belly River beds ......... 27,151

on Judith River beds................... 26-27

White River Tertiary deposits, mention of.. 19 

Whiteaves, J. F., on Belly River fossils .... 25

on Dunvegan sandstone................ 22

Wied, Maximilian zu, description by ...... 14

Williston, S. W., on Judith River region... . 31

Willow Creek, Mont., Judith River plants

from.......................... 129-150

Judith River beds on and near......... 56-58

rocks on ................................ 55

view on................................. 58

Willow Creek beds of Canadian Laramie,

mention of ..................... 22-23

Wind River Valley deposits, mention of... 19

Y.

Yellowstone River, Mont., Judith River

beds on......................... 61

Zaphsalis abradus Cope .................... 84

o