DEPARTMENT OF THE INTERIOR

UNITED STATES GEOLOGICAL SURVEY

GEOKGE OTIS SMITH, DIRECTOR

BULLETIN 389

THE MANZANO GROUP

OF THE

RIO GRANDE YALLEY, NEW MEXICO

BY

WILLIS T. LEE

AND

GEORGE H. GIRTY

WASHINGTON

GOVERNMENT PRINTING OFFIGE

1909

CONTENTS.

Page.

I3TRATIGRAPHY OF THE MANZANO GROUP, BY WlLLIS T. LEE................. 5

Introduction........................................................... 5

Purpose of report................................................... 5

Preliminary statement of results..................................... 5

Field work......................................................... 7

Location and character of area............................'............... 7

Formation names. ..................................................:.: 8

Explanatory statement............................................. .8

Magdalena group.............................'...................... 9

Sandia formation.................................................. 9

Madera limestone. . .............. '. ................................. 10

Manzano group.................. '. ................................. 10

Abo sandstone...................................................... 12

Yeso formation.............. '. ...................................... 12

San Andreas limestone................................................ 12

Stratigraphic relations.................................................. 13

Underlying rocks.................................................. 13

Subdivision of the Manzano group:................................. 14

Overlying rocks.................................................... 15

Generalized section................................................. 15

Descriptive details of sections........................................... 18

Galisteo Canyon........ . .......................................... 18

Sandia Mountains. ................................................. 19

Abo Canyon...................................................... 20

Mesa delYeso...................................................... 21

Alamillo........................................................... 24

Blackinton's ranch. .............................................. 24

Carthage............................................. : ............ 24

Fra Cristobal Mountains:.......................................... 25

Nogal Creek....................................................... 26

Engle............................................................ 27

Elephant Butte................................................... 27

Caballos Mountains................................................. 28

San Andreas Mountains............................................. 28

Extension of Manzano group to the northeast............................ 30

Introductory statements............................................. 30

Apache Canyon................................................... 31

Rowe.............................................................. 33

Bernal............................................................. 35

Las Vegas.......................................................... 36

Summary.............................................................. 39

3
4 CONTENTS.

Page.

PALEONTOLOGY OP THE MANZANO GROUP, BY GEORGE H. GIRTY............ 41

Introduction.......................................................... 41

Description of species................................................... 50

Coelenterata........................................................ 50

Echinodermata..................................................... 50

Bryozoa............................................................ 52

Brachiopoda...................................................... 53

Pelecypoda...................................................;.... 72

Scaphopoda....................................................... 95

Gasteropoda....................................................... 96

Cephalopoda...................................................... 112

Ostracoda....:.................................................... 115

Trilobita........................................................... 118

Register of localities................................................... 119

INDEX. ................................................................... 137

ILLUSTRATIONS.

.Page. 

PLATE I. Map of the Rio Grande region in New Mexico.................... 8

II. A, Caballos Mountains; B, Gypsum beds in Galisteo Canyon....... 10

III. Columnar sections showing relations of the Manzano group to neighboring formations.............................................. 14

IV. A, Mesa del Yeso; B, Saddle Peak, Fra Cristobal Mountains....... 22

V. A, Western face of Fra Cristobal Mountains; B, Fault plane at the

western base of Fra Cristobal Mountains......................... 26

VI-XII. Fossils of the Manzano group.................................. 124-136

FIGURE 1. Partial section of sedimentary rocks exposed in Galisteo Canyon

west of Cerrillos............................................... 18

2. Section of a part of the beds exposed at the north end of the Sandia

Mountains, near Tejon......................................... 19

3. Section near Mesa del Yeso, 12 miles northeast of Socorro........... 22

4. Section 2 miles north of Carthage................................. 25

5. Section at Saddle Peak, near the south end of Fra Cristobal Mountains. ......................................................... 26

6. Section in Caballos Mountains west of Upham..................... 28

7. Section near the north end of the San Andreas Mountains, near

Rhodes's ranch................................................ 29

8. Section of red beds 1 mile east of Rowe, N. Mex.................... 34

9. Section 5 miles northwest of Las Vegas, N. Mex.................. 37
THE MANZANO GROUP OF THE RIO GRANDE VALLEY,

NEW MEXICO.

STRATIGRAPHY OF THE MANZANO GROUP.

Bv WILLIS T. LEE.

INTRODUCTION.

Purpose of report. The purpose of the present paper is to describe 

the red beds of that part of the Rio Grande valley which lies between 

Santa Fe and Rincon, a distance of about 200 miles, and to establish, 

their position in the geologic column. The rocks, consisting of sandstone and shale, prevailingly red in color, and containing gypsum and 

limestone, constitute a part of the so-called "Red Beds" of the Rocky 

Mountain region. On account of their general similarity in color and 

composition to .the red beds that are exposed in the eastern foothills 

of the Rocky Mountains and that extend from the mountains eastward and southeastward into Kansas, Oklahoma, and Texas, they 

have been regarded as Permo-Triassic in age.

While my principal object is to present the evidence that tends to 

fix the geologic age of the red beds of the Rio Grande valley, the relation of these to other beds of similar nature is also considered, flowever, I have no intention to discuss the various aspects of the complicated "Red Beds" problem or even to review the numerous 

contributions to it. I purpose, rather, to confine attention to such 

phenomena as I have personally observed in the field and to such 

considerations as may have a direct bearing upon the interpretation 

of these observations.

Preliminary statement of results. The red beds of the Rocky Mountain region are unfossiliferous in many places, but on account of their 

stratigraphic relations have frequently been called " Jura-Triassic " 

a term still in common use. The name "Red Beds" has been so constantly applied to these rocks that it has come to have more or less 

of a time significance, and red sediments of undetermined age in the

5
6 MANZANO GROUP OF RIO GRANDE VALLEY.

Rocky Mountain region are sometimes referred to as the "JuraTriassic Red Beds." In the Texas-New Mexico region the occurrence 

of red sediments that are older than the recognized Triassic beds and 

that are referred by many geologists to the Permian has given the 

name " Permo-Triassic " to some of the red beds in the Southwest.

Investigation has shown that some of the red beds of the Rocky 

Mountain region are much older than Triassic and that others are 

much younger, the geologic age extending from Mississippian ("Lower 

Carboniferous") to late Cretaceous. I have formerly called attention to the fact that the base of the red beds in Perry Park, Colorado,0 

is of lower Carboniferous age, and the evidence presented in this paper 

shows that a large part of the red beds in central New Mexico is of 

upper Carboniferous or Pennsylvanian age. Furthermore, there are 

red beds of late Cretaceous age, called Galisteo sandstone by 

Hayden,6 and later described more fully by Johnson,0 that are similar in general appearance to the older red beds and that have sometimes been mistaken for them. I have shown d that red sediments of 

late Cretaceous age occur also near Engle, N. Mex., about 150 miles 

south of Galisteo Canyon, the type locality of the Galisteo red beds.'

The red beds of the Rio Grande valley, here called the Manzano 

group, are shown on faunal evidence to constitute the upper part- of 

the Pennsylvanian ("Upper Carboniferous") series. It is not certainly known that the Manzano group is the exact time equivalent 

of any part of the red beds of the Rocky Mountain or Plains regions, 

as it has not been traced continuously from the one region to the 

other. However, certain data recently obtained indicate that the 

base of the red beds south and east of the mountains are of lower 

Pennsylvanian age, and it is reasonable to assume that some part of 

these apparently conformable beds is to be correlated with the Manzano or upper Pennsylvanian group.

Although the upper part of the red beds of the plains of eastern 

New Mexico is known ( from contained fossils to be of Triassic age,e 

I am disposed, because of lithologic resemblance, to correlate the 

lower part with the red beds of the Rio Grande valley. This opinion 

has recently found support in certain investigations made by Beede/ 

who has described a collection of invertebrates found in the Quartermaster formation near the top of the red beds in western Oklahoma 

and in the Panhandle of Texas. Beede refers the formation to the 

.Permian; but after studying the Manzano fauna described in this

a Lee, W. T., The areal geology of the Castle Rock region: Am. Geologist, vol. 29,1902, p. 97.

bHayden, F. V., U. S. Geol. Survey Terr, for 1867 and 1869; reprint 1873, p. 166.

c Johnson, D. W., The geology of the Cerrillos Hills, New Mexico; Schpol of Mines Quart., vol. 24,1903, 

p. 36.

<JLee, W. T., Note on the Red Beds of the Rio Grande region in central New Mexico: Jour. Geology, 

vol. 15,1907, pp. 52-58.

eldem, p. 55.

/ Beede, J. W., Invertebrate paleontology of the upper Permian red beds of Oklahoma and the Panhandle 

of Texas: Bull. Kansas Univ. Sci., vol. 14,1907, pp. 115-171.
INTRODUCTION. 7

bulletin Girty finds that the Quartermaster fauna of Beede is more 

closely related to the Manzano than to the Guadalupian fauna,0 

which he has described as Permian and which, in turn, is younger 

than the Manzano. He correlates the Manzano and Quartermaster 

formations with the Hueco, which underlies the Guadalupian of 

Texas, and with the Gschelian, which is said to underlie the Permian 

beds of Russia.

. Field work. The investigations forming the basis of this jeport 

were carried on in the Rio Grande valley in central New Mexico 

during the summers of 1904 and 1905 in connection with economic 

work which required the greater part of my time. For this reason 

and also because of the intricate structure of the region, on account 

of which much detailed work would be required in order to map the 

formations, no attempt is here made to show the areal distribution 

of the rocks described. Parts of the various sections were not accurately measured where such measurements would have required considerable time, and the thicknesses are estimated, as indicated in 

the detailed descriptions. On account of their conspicuous red color 

and other physical peculiarities, the rocks are readily distinguished 

from both the underlying and the overlying formations and little 

difficulty is experienced in identifying them in the field, except where 

the younger or late Cretaceous red beds later referred to occur near 

them. Nevertheless, fossil collections were made wherever possible, 

and in every case the paleontologic evidence coincides with the physical in making the red beds of the Rio Grande valley a sharply defined 

group.

Field work was discontinued in 1905 before the relations oft the 

Manzano group to the "Red Beds" of the Great Plains region to the 

east could be determined, and a short reconnaissance was made two 

years later (1907) in the foothills east and south of the Rocky Mountains in New Mexico for the purpose of making correlations. .All 

of the work was rapid reconnaissance in character, and future investigations may require modification or change of opinions herein 

expressed.

LOCATION AND CHARACTER OF AREA.

The area examined is in the Rio Grande valley of New Mexico, 

mainly east of the river, and extends from Santa Fe southward to 

El Paso, a distance of about 275 miles. The rocks described are 

exposed at numerous places from Apache Canyon, at the north end 

of the region, southward beyond Rincon, a distance of more than 

200 miles. A few miles south of Rincon they disappear beneath the 

surface of the Jornada del Muerto. This disappearance is not due 

to any original thinning of the beds, for the evidence at hand indi-

» Girty, G. II., The Guadalupian fauna: Prof. Paper U. S. Geol. Survey No. 58,1908.
8 MANZANO GEOUP OF KIO GRANDE VALLEY.

cates that they originally thickened toward the south.' It is caused 

rather by recent erosion, which has removed the beds from the 

highlands, and by the accumulation of surface debris, which covers 

any remnants that may remain within the trough of the Jornada 

syncline.

The red beds are not continuously exposed, owing to profound 

displacements by faulting, some of the uplifted parts having been 

eroded and the downthrown parts covered with subaerial deposits. 

The exposures are not far enough separated, however, to make difficult the tracing of the formations or to render doubtful the identity 

of the beds, and in several places the beds are traceable continuously 

for long distances. The localities where the accompanying sections 

were measured and where fossils were collected are indicated by numbers on Plate I. The second set of numerals corresponds to the permanent lot numbers of fossils collected at the various localities and preserved in the collections of the United States Geological Survey.

The opportunities for stratigraphic study are exceptionally good 

throughout the Kio Grande region, owing to the occurrence of many 

small groups of mountains consisting of upturned blocks that expose 

to view rocks ranging in age from pre-Cambrian to Quaternary. 

The uplift of these mountain blocks was accomplished apparently 

in late geologic time, and the strata are exposed in scarplike faces, 

illustrated in Plate II, A. In this escarpment thicknesses of several 

thousand feet are exposed and the formations are traceable without 

break for long.distances.

FORMATION NAMES.

Explanatory statement. Several of the formation names used in 

this paper are new to science and others are so unfamiliar that definition is desirable. A number of papers have been published relating-to the geology of the region, but apparently little detailed work 

has been done in the field and many of the names used have not been 

defined with sufficient care to make them intelligible even to one 

familiar with the geology of the region. In some cases the same 

name has been applied apparently to different formations, as shown 

by Gordon,® and in others the description of beds and the application of names are too ambiguous to be interpretable.

The names previously applied to formations are retained where 

type localities and adequate descriptions have been given. But for 

the older group of the Pennsylvanian series (Magdalena) and for the 

subdivisions of the younger group (Manzano) it has been deemed 

advisable to introduce new names.

o Gordon, C. H., Notes on the Pennsylvanian formations in the Rio Grande valley, New Mexico: Jour. 

Geology, vol. 15,1907, pp. 805-816.
FORMATION NAMES. 9

The question of the nomenclature of the Carboniferous formations 

of New Mexico has been discussed by Gordon in the article just 

referred to, and will be treated more fully in a paper in preparation 

describing the geology of a part of central New Mexico, to which 

readers interested in this question are referred. It should be added, 

however, that Doctor Gordon was writing his description at the same* 

time that I was preparing this paper. Together we compared the 

literature relating to the geology of New Mexico, he making the suggestions and criticisms relating to the Magdalena group, while I am 

responsible for those relating to the Manzano group. The following 

classification is the result of our joint labor:

("San Andreas limestone. 

Manzano group . . . .< Yeso formation.

[Abo sandstone. 

Pennsylvania!! series...... T? i t -i. 3 Erosional unconformity.

Magdalena group: . e limestone. 

' ISandia formation.

Magdalena group. The, name Magdalena is derived from the Magdalena Mountains in New Mexico, where the formations are well 

exposed, and has been applied to the lower group of the Pennsylvanian series by Gordon, who describes them as consisting of sediments 

1,000 to 1,300 feet thick, made up of limestone with a subordinate 

amount of shale and sandstone. The Magdalena beds are found 

throughout the Rio Grande region and are readily recognized as the 

evenly bedded limestone formation intervening between the massive 

cherty limestone of Ordovician 'and Silurian age that forms the conspicuous cliffs, illustrated in Plate II, A, and the overlying red sediments of the Manzano group. The group is subdivided according to 

Gordon into the Sandia formation, a name given by Herrick a to 

the lower division, and the Madera limestone, a name applied by 

Keyes b to the upper division.

Sandia formation. The Sandia formation derives its name from 

the Sandia Mountains, east of Albuquerque, N. Mex. It is 500 to 

700 feet thick and consists of limestone, carbonaceous shale, and 

quartzitic sandstone. This character, however, is not constant. 

According to Gordon, the beds become more calcareous southward, 

until south of Socorro County the distinction between the Sandia 

beds and the overlying Madera limestone is apparently lacking.

" Herrick, C. L., Geology of the white sands of New Mexico: Jour. Geology, vol. 8, 1900, p. 115. Also, 

report of a geologic reconnaissance in western Socorro and Valencia counties, N. Mex.: Am. Geologist, 

vol. 25, 1900, p. 235.

'b Keyes, C. R., Unconformity of the Cretaceous on older rocks in central New Mexico: Am. Jour. Sci., 

4th ser., vol. 18, 1904, pp. 360-362. Also, Geology and underground-water conditions of the Jornada del 

Muerto, New Mexico: Water-Supply Paper U. S. Geol. Survey No. 123, 1905, p. 22.
10 MANZANO GROUP OF RIO GRANDE VALLEY.

Madera limestone. According to the best information available, 

the type locality of the Madera limestone is in the Sandia Mountains, 

at the town of La Madera. The only reference to the origin of the 

name is that -of Herrick,0 who states that the town " seems to be 

upon a plateau of limestone." This limestone the Madera here 

c constitutes the uppermost member of the Magdalena group. According to Gordon, the Madera is the uppermost member of the group 

also in the Magdalena Mountains, where it is 300 to 500 feet thick, 

and it is about 700 feet thick in the Socorro Mountains. Farther to 

the south, as previously stated, it is not readily distinguishable from 

the Sandia formation.

Manzano group. The name Manzano is derived from the Manzano 

Mountains, one of the semidetached ranges of the Rocky Mountain 

system southeast of Albuquerque, N. Mex. The name was first 

applied by Herrick,6 as follows:

At the top of the gray lime [Madera]' is a large series of coarse red quartzites and 

sandstones interbedded with dark* earthy limestones and shales. Th'ere are few 

fossils except petrified wood, and the few found still preserve a Carboniferous habitus. 

This Manzano series is everywhere in evidence where a sufficiently high horizon is 

reached, but is often removed from the crests of the range, while it occurs in the 

eastern faulted extension. Following this is the group of red quartzites, sandstones, 

shales, and marls which we have recognized as the equivalent of the "red series" 

of Texas and Kansas. Three divisions can be made out in all parts of the territory 

examined, which have been named from their prevailing characteristic color, though 

it is not to be supposed that the color mentioned is constant. The lower or "red 

bed'' division still retains some bands of limestone or lime breccias, the latter being 

a very characteristic element. Some 500 feet may be estimated as the average thickness of this division, and prior to the work recently done in the valley of the white 

sands we had no definite evidence as to the age of the entire division. We only 

knew that a narrow bed of quartzite near the base at a point east of the Sandia 

Mountains contained the well-known Permian forms, such as Bakeivellia parva,

Myalina attenwta, Pleurophorus subcuneatus, c etc. The major portion of the series

proved obstinately barren. At the top of this division there are found in the most 

widely distant parts of the Territory enormous deposits of gypsum and salt. In 

fact, the presence of salines may be said to characterize the series, but especially at 

the passage from the red into the chocolate beds above it. The chocolate series 

has a thickness of at least 600 feet, and passes through quartzites and gray and red 

sandstone layers into the loose vermilion marls and clays of the upper division. So 

far we have no positive evidence as to the age of the two upper divisions, but may 

presume the chocolate beds to be Triassic and the vermilion division to represent 

whatever of Jurassic time is accounted for in the Territory, or at least in the central 

portion. d

a Herrick, C. L., The geology of the San Pedro and Albuquerque districts: Bull. Univ. New Mexico, 

vol. 1,1889, p. 104.

6 Herrick, C. L., Geology of the white sands of New Mexico: Bull. Univ. New Mexico, vol. 2,1900, 

fas. 3, p. 4; also Jour.Geology, vol. 8,1900, pp. 112-128.

c There is room for doubt regarding the identity of these fossils.' It is possible that Herrick may have 

mistaken for Permian certain Pennsylvanian forms which closely resemble the species named, as shown 

by Girty in the accompanying paper, pp. 44-45.

d The name Manzano has been applied to other formations, as, for example, Keyes's recent usage of the 

name for the lower part of the Magdalena group. (See Jour. Geology, vol. 14,1906, p: 154.) Herrick was 

the first, however, to use the name in a definite manner, and, in accordance with the law of priority, his 

usage has been followed.
BULLETIN 339 PLATE 11

' - A. CABALLOS MOUNTAINS.

Showing the western escarpment, consisting of pre-Cambrian granite, the Shandon formation (Cambrian), 

the Ordovician limestone, and limestone of the Magdalena group.

21. GYPSUM BEDS IN GALISTEO CANYON. 

Showing the gypsum at the base of the Yeso formation, underlain by the Abo sandstone at the left-
FORMATION NAMES. . 11

It is clear from this and other writings of Herrick that he included 

in the Manzano group only the .three subdivisions mentioned, namely, 

the lower or red sandstone (Abo), with which he associated the 

overlying gypsum; the middle or chocolate-colored sediments; and 

the upper or vermilion beds, the last two of which are here combined 

as the Yeso formation. Herrick referred the lower division to the 

Permian because of the presence of certain fossils which he supposed 

to be Permian, although with these fossils he found well-known Pennsylvanian forms. He explains this occurrence on the ground that 

the Pennsylvanian fossils were contained in fragments of limestone 

derived from the older beds and cemented together by the lime that 

contains the forms which he interpreted as Permian.® Some grounds 

for this suggestion of a mixed fauna are found in the irregular texture 

of the limestone near the base of the Manzano group, and the argument might have force were it not for the fact that the same species 

of fossils are found at various horizons throughout the Manzano 

group.

The same writer in the article just quoted and also in collaboration 

with Johnson 6 states that the upper beds are unfossiliferous, and 

on "stratigraphic grounds" these authors assign the chocolatecolored beds to the Triassic and the. vermilion beds to the Jurassic. 

It should be stated in this connection that I found this threefold 

'subdivision based on prevailing color so uncertain that it could not 

safely be applied in the field. The color varies greatly from place 

to place, and in the light of paleontologic evidence the reference of 

the lowest division to the Permian and of the upper divisions to 

the Triassic and Jurassic breaks down, since the whole group proves 

to be Pennsylvanian.

In the quotation previously given from the article describing the 

white sands, and in other writings as well, Herrick states that the 

Manzano group contains beds of salt. I am not able to confirm 

this statement, although I looked for evidence of salt beds in the 

various sections examined. I't is possible that more careful examination may establish their presence, although it is not clear from the 

literature that Herrick actually found salt deposits in the red beds 

of the Rio Grande region. His statement in this connection, that 

enormous deposits of gypsum and salt "are found in the most widely 

distant parts of the Territory" of New Mexico, indicates that he 

may have had in mind the thick beds of gypsum of eastern New 

Mexico which overlie strata known from paleontologic evidence to 

be of Triassic age, and the salt and gypsum beds in the so-called 

Texas-Permian of southeastern New Mexico, as well as the gypsumo Herrick, C. L., The Geology of the San Pedro and the Albuquerque districts: Bull. Univ. New Mexico,' 

vol. 1,1899, p. 103.

& Herrick, C. L., and Johnson, D. W., The geology of the Albuquerque, New Mexico, sheet: Bull. Univ. 

New Mexico, vol. 2, 1900, p. 49. Also, Bull. Denison Univ. Sci. Lab., vol. 11,1900, pp. 175-239.
12 MANZANO GROUP OF KIO GRANDE VALLEY.

bearing beds which are here referred to the Pennsylvania!! series of 

the Carboniferous, but which he supposed to be of Permo-Triassic 

age.

The massive limestone which overlies the gypsiferous shale and 

sandstone and which is here described as the San Andreas limestone 

is not described in any of the literature of the Rio Grande. region, 

although Herrick includes it in his sections.0 It contains an. abundant fauna which clearly allies it with the red beds in the Pennsylvanian division of the Carboniferous, and is therefore included in 

the Manzano group, although it was not originally so included by 

Herrick.

Abo sandstone. The Abo sandstone derives its name.from Abo 

Canyon, at the southern end of the Manzano Range. It is the :basal 

member of the Manzano group and rests unconformably upon the 

Magdalena group. It consists of coarse-grained sandstone, dark red 

to purple in color and usually conglomeratic at the base, with a 

subordinate amount of shale, which attains prominence in some 

places. This sandstone, together with the overlying gypsum, 

apparently constitutes Herrick's "Permian." In the classification 

here adopted the upper limit of the Abo formation is drawn below 

the gypsum for the obvious reason that in many places the overlying 

or Yeso formation contains beds of gypsum and gypsiferous shale 

at several horizons, through a thickness in some places of 1,000 

feet or more.

Yeso formation. The Yeso formation derives its name from Mesa 

del Yeso, a small table-land 12 miles northeast of Socorroj N. Mex., 

where it is typically exposed. (See section, p. 22.) It lies with apparent conformity upon the Abo sandstone, and consists of 1,000 to 

2,000 feet of sandstone, shale, earthy limestone, and gypsum. The 

sandstone varies in color from gray to many shades of pink, yellow, 

red, and purple, and in texture from soft, coarse-grained, friable 

masses to fine-grained layers, evenly bedded and flinty. The shales, 

frequently gypsiferous, are soft, pink to yellow in color, and beds of 

massive white, gypsum 100 to 200 feet thick occur in many places.

San Andreas limestone. The third formation of the Manzano group 

derives its name from the San Andreas Mountains, at the north end 

of which it is typically developed, as described in the section on page 

29. It consists essentially of massive limestone, which is often cherty 

and poorly fossiliferous, although several localities were found where 

fossils are abundant. This limestone was not included in the Manzano group by Herrick. He refers to it, however, in his description of 

the region east of Socorro 6 as an unfossiliferous limestone overlying 

the Manzano red beds, and includes it in the illustration of his section.

"Herrick, C. L., A Coal-Measure forest near Socorro, N. Mex.: Jour. Geology, vol. 12,1904, p. 243. 

& Idem, pp. 237-251.
STRATIGRAPHIC RELATIONS. 13

The writer, however, found in it fossils which are said to be unquestionably of Pennsylvanian age and which prove that the San Andreas 

limestone should be included in the Manzano group.

So far as is known at present the San Andreas limestone is the 

uppermost member of the Manzano group, but it can not be confidently asserted without further investigation that no Pennsylvanian 

beds younger than the San Andreas limestone are to be found in the 

Rio Grande region, or that no Triassic rocks occur there. The red 

sediments near Carthage beneath the basal sandstone of'the Cretaceous and apparently above the San Andreas limestone (see p. 25) 

are the only ones known which may represent Permian or Triassic 

time. These sediments differ considerably in general appearance from 

the known Manzano, but nothing was found to indicate whether they 

belong in the Manzano group or represent a younger formation.

STRATIGRAPHIC RELATIONS.

Underlying rocks. The red sediments of the Manzano group rest 

unconformably upon the massive blue limestones of the Magdalena 

group. These limestones yield an abundant fauna, by which they 

are known to be of lower Pennsylvanian age, as will be shown in a 

forthcoming paper by G. H. Girty, of the United States Geological 

Survey. In the northern part of the region described the underlying 

limestone is the Madera, but in the southern part the Magdalena group 

is not readily separable into the Madera and Sandia formations, and 

the limestone, although probably equivalent in age to the Madera, is 

not yet definitely correlated with that formation and is here 'referred 

to as the limestone of the Magdalena group.

Throughout the Rio Grande Valley wherever the contact was seen 

the unconformity at the base of the Manzano group was noted. 

There is no marked discordance in dip, but the contact is sinuous, and 

in several places the underlying limestone clearly had been .eroded 

previous to the deposition of the Manzano. A conglomerate frequently occurs at or near the base of the Manzano, and contains fragments of blue limestone, obviously derived from limestone of the 

underlying Magdalena group, and at several places water-worn fragments of fossils were found in the conglomerate. For these reasons, 

and because of the abrupt change throughout the Rip Grande region 

from the massive blue limestone of the Magdalena to the conglomeratic red sandstone at the base of .the Manzano, the unconformity is 

regarded as indicating a time break of considerable .duration.

The evidence, as stated, of this period of erosion is supplemented 

by the occurrence south and east of the Rocky Mountains of red sandstone and shale of Magdalena age, as described on pages 33-38. In 

other words, the Madera is apparentlyjnot the.youngest member of 

the Magdalena group. This youngest member was probably red
14 MANZANO GROUP OP EIO GKANDE VALLEY.

sandstone and shale, and was eroded away in the Rio Grande region 

previous to the deposition of the Manzano.

Subdivision of the Manzano group. The Manzano group, as used in 

this paper, includes all Pennsylvanian rocks above the unconformity 

just described.. So far as now known, it consists of three formations 

the Abo sandstone, the Yeso formation, and the San Andreas limestone. Pennsylvanian beds younger than the San Andreas may exist 

near Carthage, as described on page 15, and the long time interval 

represented by the unconformity at the top of the group, described 

below, renders it possible that these as well as still younger formations may at one time have extended generally over the region and 

have been removed by erosion previous to the deposition of the Cretaceous sediments.

The oldest Manzano formation, the Abo sandstone, has a maximum 

estimated thickness of 800 feet, and is conspicuous in every locality 

examined. Its character is constant throughout the Rio Grande 

region and its fauna' is abundant and easily recognized, although the 

fauna has yet been found at only two horizons. The most conspicuous forms are the large pelecypods Allerisma capax and Allerisma 

terminate, which are very numerous in the limestone near the base.

The Yeso formation, consisting of alternating strata of gypsum, 

shale, friable sandstone, and earthy limestone, is more variable than 

the Abo sandstone in color, composition, and general appearance. 

The color varies from the pure white of the massive gypsum, through 

a great variety of shades in the shale and sandstone, to the dull black 

of some of the earthy limestones. The colors are usually subdued, 

contrasting strongly with the deep red and purple tones of the Abo 

sandstone. The beds vary greatly both laterally and vertically, and 

no stratum was found that could be traced with confidence for any

great distance. In composition, as in color, the Yeso formation contrasts strongly with the Abo. It is very fossiliferous at many horizons. The limestones in some places are composed mainly of shells, 

and furnished most of the material described by Girty in the accompanying paper.

Until further information is available the San Andreas limestone 

can not be definitely separated from the Yeso formation, except in 

its type, locality in the San Andreas Mountains, where it is 500 feet 

or more in thickness and is clearly separable from the underlying 

beds. In the Caballos and Fra Cristobal Mountains to the west, 

and at Carthage to the north, the uppermost limestone of the sections 

is correlated with some confidence on lithologic evidence with the 

San Andreas limestone; but since the San Andreas fauna is apparently 

not sufficiently characteristic for purposes of correlation, it is not 

known whether the capping limestone shown in the sections from 

other localities is the San Andreas or one of the limestones within the
U. S. GEOLOGICAL SURVEY 

VERTICAL SCALE 

9 .... soo looofeet

c

aKsteo 

i

W^M

= 

n

z

=r.::-

_==J.'i%Z_

=ITrF:

r^-V^r

v.v.v.

1 Mesa, del ^

4

Upper Cretaceous

Morrison ? ,--- x

Yeso formation

Abo sandstone

Unconformity^ 

Magdalena

m*

T^T^r

4-r-

~1 1 T

feso 

Cf

\

\\

\ \ 

* \?

\\

\ 

\

\

\

\

\

irtha.

7

 ? . .'.' ^':

1 1 1 1 1 1 1 1 1

1 i 

1 1 1 1 1

,1 1 1

1 * L-

 

i'-''.:'.-','.- .-.'

^

= e 

^~ s 

/

7 ,''

/

' C~&^

f\0°

m ' Qf ' ->/> ' 

2O 45 

COLUMNAR SECTIONS SHOWING THE RELATIONS OF THE MANZANO GROUP TO 
STEATIGKAPHIC KELATIONS. 15

Yeso formation. The large coiled shells of the genus EuompTialus, 

the long pencil-shaped scaphopods Plagioglypta canna and Dentalium mexicanum, and the genus Aviculipinna are conspicuous in 

the uppermost limestones provisionally correlated with the San 

Andreas, but are not entirely absent from the lower ones.

The San Andreas limestone differs from the older formations of the 

Manzano group in having a more restricted geographic range. The 

beds provisionally correlated with it are well developed in the southern 

part, but become less prominent northward and are not represented 

in the northern part of the region described.

Overlying rocks. In only two localities near Carthage, including 

Blackinton's ranch, and at the northern end of the region were 

rocks found between those of known Manzano and those of Upper 

Cretaceous age. The red beds between the San Andreas limestone 

and the base of the Cretaceous near Carthage may belong in the 

Manzano group or may be younger, as no evidence of age other than 

stratigraphic position was found. At the northern end of the region 

a considerable thickness of the upper part of the Manzano is missing. 

In the Sandia Mountain section the San Andreas limestone is wanting, but the gypsum-bearing shale and the friable sandstone of the 

upper part of the Yeso formation are characteristically developed, 

and are overlain by variegated beds that resemble the Morrison. 

The upper part of the Yeso and the San Andreas limestone are wanting in the northernmost section (Galisteo), and the Morrison (?) rests 

on the pink sandstone of the middle part of the-Yeso formation.

The Manzano group is therefore separated from the overlying 

formations by an unconformity that, except for the beds of doubtful 

age, represents a period of time extending from near the close of the 

Pennsylvanian division of the Carboniferous to the beginning of the 

Upper Cretaceous. These relations are shown graphically in Plate III. 

It should. be stated in this connection that, although the Cretaceous 

is shown in only three of the sections, it occurs above the Manzano 

throughout the region described. In every locality examined, with 

the exception of San Andreas Mountains, fossiliferous Cretaceous 

beds were found above the Manzano at no great distance from the 

place where the section was measured. In most cases an unfossiliferous sandstone, 10 to 75 feet thick, occurs at the base of the Cretaceous, and this is overlain by shale and limestone which yielded an 

abundant fauna at every locality described. The collections of fossils 

have been examined by T. W. Stanton, of the United States Geological Survey, and found to constitute a well-defined Benton fauna.

Generalized section. The position of the Manzano group in the 

geologic column and its relation to other formations occurring in the 

Rio Grande region are shown in the table. The type localities of the 

various formations and the authors of the formation names are also 

given for reference. .
Rock formations exposed near the Rio Grande in New 

System.

Quaternary.

Tertiary.

Upper Cretaceous.

Lower Cretaceous.

Jurassic ?

Triassic.

Carboniferous.

Series.

Comanche.

Permian.

Pennsylvanian.

Mississippian.

Group.

Manzano.p

Magdalena, » 1,000 

to 1,300 feet.

Formation.

Palomas.

Santa Fe.

Puerco.

Galisteo, 2,000+ feet.

Madrid, 2,000± feet.

Montana and Colorado.

Morrison ?

Not identified.

Not identified.

San Andreas, 500 feet. .

Yeso, 1,OOO+ feet.

Abo, 30O-800 feet.

Madera, 300-500 feet.

Sandia, 500-700 feet.

Lake Valley.

Author.

Gordon and Graton.a

Hay den. b

Cope.c

Hayden.d

Johnson, 1903. «

Hill, 1887./

Lee, 1908.A

Lee, 1908.A

Lee, 1908.ft

Keyes, 1905. i

Herrick, 1900.t

Cope, 1881. l

Near R

Rio G

Fe, N

Rio Ga

Madrid

San A

Rhod

Mesa 

N. M

Abo Ca

tains

La Ma

tains

Sandia 

Lake V
Devonian.

g SUurian.

T

W - 

pi Ordovician.o

CO

oo

<j;> Cambrian.

11 Pre-Canibrian.

Archean ?

Fusselman, 1,000 feet.

Montoya, 250 feet.

El Paso, 1,000 feet.

Bliss, 300 feet.? "

Richardson, 1908. 

Richardson, 1908."

Richardson 1904.P

Richardson, 1904.r

Frankl

selm

Frank

Mon

Frank

El P

Frank

Fort 

a Gordon, C. H., and Graton, L. C., Jour. Geology, vol. 15,1907, p. 92; also Prof. Paper U. S. Geol. Survey (unp

t> Cope, E. D., Notes on the Santa Fe marls: Proc. Acad. Nat. Sci., Philadelphia, vol. 20,1874, p. 147.

c Cope, E. D., Rept. Secretary of War to 44th Cong., vol. 2, pt. 2,1875, p; 1012;

d Hayden, F. H., U. S. Geol. Survev Terr, for 1867 and 1869, reprint 1873, p. 166.

« Johnson, D. W.,The geology of the Cerrillos Hills, New Mexico: School of Mines Quart., vol. 24,1903, p. 36

/ Hill, R. T., The Comanche series of the Texas-Arkansas region: Bull. Geol. Soc. America, vol. 2,1891, pp. 5

Section of the Cretaceous at El Paso, Tex.: Am. Jour. Sci., 4th ser., vol. 1,1896, pp. 21-26.

g Herrick, C. L., Geology of the white sands of New Mexico: Bull. Univ. New Mexico, vol. 2,1900, fasc. 3, p. 4; 

logic reconnaissance in western Socorro and Valencia counties, N. Mex.: Am. Geologist, vol. 25,1900, p. 337. A Co

1904, p. 244. . ' 

. ft Lee, W.T. This bulletin, p. 12.

 Gordon, C. H., Jour. Geol., vol. 15, 1907, pp. 805-816.

; Keyes, C. R., Geology and underground-water conditions of the Jornadadel Muerto, N.Mex.: Water-Supply 

C. L., The geology of the San Pedro and Albuquerque districts: Bull. Univ. New Mexico, vol. 1,1899, p. 104.

* Herrick, C. L., Jour. Geology, vol. 8, 1900, p. 115; Am. Geologist, vol. 25, 1900, p. 235; Am. Geologist, vol. 5

' Cope, E. D., Eng. and Min. Jour., vol. 34,1882, p. 214. Geology of the Lake Valley mining district: Am. 

m Richardson, G. B., Paleozoic formations in trans-Pecos Texas: Am. Jour. Sci., 4th ser., vol. 25,1908, p. 47

»Idem, p. 478. ' ' - . 

o Gordon, C. H. Ordovician limestone has also been described and correlated with thecherty limestones of th

P Richardson, G. B., Reconnaissance in trans-Pecos Texas: Bull. Univ. Texas Min. Survey, No. 9,1904, p. 29.

g Cambrian has been described also from the Caballos Mountains, near Shandon, from which it has been c

L. C., Jour. Geology, vol. 15,1907, p. 91.

f Richardson, G. B., Reconnaissance in trans-Pecos Texas: Bull. Univ. Texas Min. Survey, No. 9, 1904, p. 
18 MANZANO GROUP OF RIO GBANDE VALLEY.

I/

DESCRIPTIVE DETAILS OF SECTIONS.

GALISTEO CANYON.

A section (fig. 1) of the Manzano group was measured north of 

the Atchison, Topeka and Santa Fe Railway in Galisteo Canyon 

 west of Cerrillos (locality 1 of the map, PL I). The rocks are upturned 

and well exposed, as shown in Plate II, B. The Abo sandstone is 

overlain -by the massive white gypsum and the red and yellow 

sediments of the Yeso formation, which here consist mainly of sandstone, the shales so abundant farther south being imperfectly 

represented.

Lying with apparent unconformity upon the Yeso formation is a 

group of sandstones and shales that resembles the Morrison formation

Feet.

I!

Sandstone and shale containing fossils of Benton (Cretaceous) age. 

60 Sandstone (Dakota), coarse, white, friable, cross-bedded.

210 Shale, variegated, and sandstones, in thin alternating layers. The sandstones vary from fine-grained, flinty layers to coarse-grained, friable, 

cross-bedded masses.

Unconformity.

210 Sandstone and shale, pink and bud-colored, lighter toward the top. 

The sandstones greatly predominate and are well indurated, coarsegrained, and spotted. <

25 Shale, pink, and thin layers of blue limestone. 

140 Gypsum, white, massive.

5-10 Gypsum, black, shaly, carbonaceous, in thin irregular plates; strong 

petroleum odor.

225 Sandstone, red, massive, with a subordinate amount of shale.

(Base not exposed.) 

FIGURE 1. Partial section of sedimentary rocks exposed in Galisteo Canyon west of Cerrillos.

in color, composition, and general appearance, but no fossils were 

found to identify it. If these variegated sediments are correctly 

referred to the Morrison, the apparent unconformity must represent 

the time equivalent of the San Andreas limestone and all succeeding 

formations between it and the Morrison, and probably also an erosion 

interval of considerable importance.

The Morrison (?) is overlain by white, coarse-grained, cross-bedded 

sandstone, conglomeratic near the base and similar in general appearance to the Dakota, but without fossils so far as observed. This 

sandstone is succeeded in turn by f ossiliferous shale and limestone of 

Upper Cretaceous age, including equivalents of the Colorado and Montana groups. Collections of Cretaceous fossils were obtained, and
DETAILS OF SECTIONS. 19

these together with others made throughout the region described 

have been -examined bv T. W. Stanton.

SANDIA MOUNTAINS.

The second section (fig. 2) is located about 15 miles south of 

Galisteo Canyon, at the north end of the Sandia Mountains, near Te-.

Feet.

Limestones and dark-colored shales.

50 Sandstone, white, friable, cross-bedded, conglomeratic.

N/ J--

200 Shale, variegated, and sandstone. r

Probable unconformity.

Shale and friable sandstone, pink to yellow, with gypsum near the base 

(several hundred feet not continuously exposed).

400 Sandstone, shale, and earthy limestone, gray, pink, and yellow, variable

v in character, containing Monopteria marian, Schizodus wlieclcrif,

( Dcltopectcn corcyanus, Plagioglypta canna, Euphcmus subpapillosus?,

Sdlerophon majusculw., Euomphalus sp. b, Phanerotrcma manzanicumt, MurcMsonial tk/ebraf, Patdlostium all. nodicostatum.-

Possible unconformity of erosion.

700 Sandstone, red, massive, with partings of red shales. (Thickness 

estimated.)

2 Limestone, granular, earthy.

40 Sandstone, red, conglomeratic, with limestone pebbles at the base. 

Unconformity.

Limestone (Magdalena group).

FIGUKE 2. Section of a part of the beds exposed at the north end of the Sandia Mountains,

near Tejon.

jon, on the road between Bernalillo and the Hagan coal mines (locality 

2, PI. I). The strata are steeply upturned toward the east, and 

although they are well exposed it would require more time than I 

had at my disposal to make a complete detailed section.
20 MANZAISTO GROUP OF BIO GRANDE VALLEY.

The Madera limestone is overlain unconformably by the Abo 

sandstone, the contact being well exposed near the spring known as 

Ojo de San Francisco. A band of fossiliferous earthy limestone 1 

to 2 feet thick was found 40 feet above the basal conglomerate 

of the Abo. The fossils are abundant in some places, while in others 

none were found for considerable distances along the outcrop. Above 

this limestone the massive dark-red sandstone (Abo) occurs charac- 

' teristically developed, but was not examined in detail.

The Abo is overlain by 400 feet of lighter colored sandstone, shale, 

and fossiliferous earthy limestone. Some indication of an unconformity of erosion, probably of local importance only, was noted 

between these lighter colored beds and the underlying dark-red 

sandstone. In general' character and appearance the light-colored 

sediments resemble the pink and buff sandstone overlying the gypsum 

of the Galisteo section (fig. 1). If they are to be correlated with this 

sandstone a time break should be found here representing the gypsum of the Galisteo section which occurs between the light-colored 

sandstone of the Yeso and the dark-red sandstone of the Abo. 

On the other hand, about 2 miles northeast of Tejon gypsum 

similar in every way to the gypsum of the Galisteo section underlies 

the light-colored sediments.

There is a great thickness of red and yellow shale, friable sandstone, and gypsum above the light-colored sandstone of the Sandia 

section. These outcrop in a valley of erosion that runs parallel with 

the strike, and are not continuously exposed. The valley is about 

half a mile wide and the strata on either side dip steeply to the east. 

The gypsiferous sediments are overlain by the variegated shales 

provisionally referred to the' Morrison, and the latter in turn are 

overlain by the same succession of Cretaceous beds that occur in 

Galisteo Canyon.

ABO CANYON.

The next section in order southward is about 75 miles south of

$ Galisteo Creek, in Abo Canyon (locality 3, PL I), from which the 

Abo sandstone derives its name. The limestone of the Magdalena 

group occurs here in characteristic development and is overlain by 

650 feet of the dark-red Abo sandstone, the upper part having been 

removed by erosion. The basal conglomerate of the Abo lies unconformably upon the unevenly eroded surface of this limestone.' There 

are several thin layers of earthy limestone 30 to 50 feet above the 

base, which yielded the following fossils.
U. S. GEOLOGICAL SURVEY BULLETIN 889 PLATE I

o/^iOj ,; 20 30 *o so Mile s

MAP OF THE RIO GRANDE REGION IN NEW MEXICO, SHOWING LOCATIONS OF SECTIONS 

AND FOSSIL LOCALITIES..

The numerals in parentheses refer to the lot numbers of fossils in the Geological Survey collection.
DETAILS OF SECTIONS. 21 

Fossils from, earthy limestone near the base of the -Abo sandstone .in Abo Canyon.

Lophophyllum? sp. 

Septopora aff. robusta. 

Meekella striaticostata. 

Prodiictus cora. 

Productus nebraskensis. 

Composita subtilita. 

Edmondia gibbosa. 

Chaenomya leaven worthensis. 

Leda obesa.

Aviculipinna? peracuta. 

Aviculipinna nebraskensis. 

Monopteria marian. 

Pseudomonotis hawni?

Myalina apachesi. 

Schizodus wheeleri. 

Deltopecten occidentalis. 

Deltopecten manzanicus. 

Deltopecten coreyanus? 

Allerisma capax. 

Pleurophorus aff. subcostatus? 

Pleurophorus aff. oblongus. 

Patellostium aff. nodicostatum. 

Bucanopsis modesta? 

Naticopsis deformis. 

Soleniscus aff. altonensis. 

Orthoceras sp.

In 1905 G. B. Richardson, of the United States Geological Survey, 

made a reconnaissance trip from Belen eastward across the Territory,

along the line of the Belen cut-off of the Atchison, Topeka and 

Santa Fe Railway, and has kindly furnished the following information for this paper: In Abo Canyon he observed the Manzano group 

in the locality described above, and traced it eastward for a distance 

of 40 miles. At the east end of a mesa 5 miles south of Willard, a 

town on the.Santa Fe Central Railway, he measured the following 

section:

Section 5 miles south of Willard, N. Mex.

Feet.

Limestone, gray, cherty, containing fossils of Pennsylvanian age, as 

follows: Chastetes milleporaceus?, Schizodus sp., Myalina? sp., Bellerophon sp.................................................... 50

Sandstone, gray, friable.......................................... 300

Sandstone, red.. ..........................................^...... 10

Gypsum, massive, bluish white...............'.................... 100

Base not exposed.

Although the base was not exposed, Richardson thinks it probable 

that the gypsum rests upon the red sandstone exposed in Abo Canyon 

and described in this paper under the name of Abo sandstone. This 

accords with the relations shown in other sections described, where 

massive gypsum overlies this sandstone. The fossils from the limestone are Pennsylvanian, and this evidence, taken in connection 

with the character and succession of the beds, indicates that the 

gypsum and sandstone probably belong to the Yeso formation, with 

a possible representative of the San Andreas limestone at the top.

MESA DEL Y'ESO.

The next section to the south is 12 miles northeast of Socorro and 

about 100 miles south of Galisteo Creek (locality 4, PL I). Although 

the rocks in the vicinity of Socorro are profoundly faulted and
22 MANZANO GROUP OF BIO GRANDE VALLEY.

otherwise disturbed, an excellently exposed section of the Manzano 

group was found about 2 miles south of Mesa del Yeso (PI. IV, A; fig. 3), 

the location of which is shown on the Socorro atlas sheet of the 

United States Geological Survey. The rocks included in the section 

are exposed from Canyoncito de la Uva northward across the low 

hills at the east edge of the Socorro quadrangle. It is from this

Feet: 

75 Limestone, fossiliferous (top eroded).

i , i ~ r

171 ,1,1

200 Sandstone, pink and white.

150 Gypsurrr^with' a -subordinate amount of pink arid yellow shale.

300 Sandstone, red, arid gypsiferous shale with a subordinate amount of 

earthy limestone.

50 Limestone, fossiliferous.

550 Sandstone, red and purple, with a subordinate amount of shale, 

and earthy limestone.

5 Limestone, fossiliferous. 

10 Shale, blue. 

30 Not exposed.

20 Sandstone and shale, brown to pink. 

25 Conglomerate limestone pebbles in matrix of sand. 

Erosional unconformity. 

Limestone, massive (Magdalena group).

FIGURE 3. Section near Mesa del Yeso, 12 miles northeast of Socorro. (For fossil contents see section

on p. 23.)

mesa that the Yeso formation derives its name. The Abo sandstone 

here rests unconformably upon the Madera limestone. The basal 

conglomerate is 25 feet thick, and among the pebbles of various 

kinds of rock were found fragments of limestone and waterworn 

fossils apparently derived from the underlying Madera limestone. 

A thin limestone 85 feet above the base of the Abo yielded fossils, as 

shown in the following section:
U. S. GEOLOGICAL SURVEY BULLETIN 389 PLATE IV

A. MESA DEL YESO. 

Showing the character of the Yeso forma-tion.

B. SADDLE PEAK IN FRA CRISTOBAL MOUNTAINS. 

Showing the Yeso formation, overlain by the San Andreas limestone.
DETAILS OP SECTIONS. 23

Section near Mesa del Yeso, 12 miles northeast of Socorro.

Feet.

Limestone, fossiliferous (top eroded). Contains Productus ivesi, Clinopistha? 

sp., Myalina apachesi, Schizodus aff. magnus, Deltopecten coreyanus, Pleurophorusaft. taffi, Pleurophorus aff. subcostatus?, Astartella subqua'drata?, Plagioglypta canna, Murchisonia? aff. terebra, Patellostium aff. nodicostatum, Bellerophon majusculus, Naticopsis aff. altonensis, Orthonema sp. a, Temnocheilus sp. a?. ........................................................... 75

Sandstone, pink and white................................................. 200

Gypsum with, a subordinate amount of pink and yellow shale................. 150

Sandstone, red, and gypsiferous shale with a subordinate amount of earthy 

limestone............... I............................................... 300

Limestone, fossiliferous. Contains Productus ivesi?, Productus mexicanus, 

Productus nebraskensis, Squamularia perplexa?, Pugnax osagensis var. pusilla, . Composite subtilita?, Nucula levatiformis, Manzanella elliptica, Leda obcsa, 

Pteria sp., Myalina apachesi, Schizodus aff. magnus, Deltopecten coreyanus, 

Allerisma capax, Pleurophorus mexicanus, Pleurophorus aff. taffi, Pleurophorus aff. meeki, Astartella subqmdrata, Plagioglypta canna, Phanerotrema

' manzanicum, Phanerotrema? sp. a, Euphemus inspeciosusf, Patellostium aff. '' 

nodicostatum, Bellerophon majusculus, Zygopleura aff. rugosa, Orthonema ' 

socorroense, Orthonema sp. a, Coloceras mexicanum, Temnocheilus aff. winslowi, Temnocheilus sp. a, Domatoceras sp., Anisopyge inornata .............. 50

Sandstone, red and purple, with a subordinate amount of shale and earthy 

limestone............................................................... 550

Limestone, fossiliferous. Contains Meekella striaticostata, Productus nebraskensis, Productus cora, Edmondia gibbosa, Chsenomya leavenworthensis, Aviculipinna? peracutaf, Myalina apachesi, Deltopecten coryanus, Allerisma sp., 

Pleurophorus bipartitus, Pleurophorus sp., Plagioglypta canna?, Bellerophon 

majusculus, Temnocheilus sp. a. ............................................ 5

Shale, blue................................................................ 10

(Not exposed).............................................................. 80

Sandstone and shale, brown to pink........................................ 20

Conglomerate; limestone pebbles in matrix of sand ............:.............. 25

(Erosional unconformity.)

Limestone, massive (Magdalenagroup). ' 

1,415

The Yeso formation at this place is very fossiliferous at two 

horizons, one near the base, the other at the top of the exposure. 

The limestone near the base yielded one of the most extensive and 

well-preserved collections found in the Manzano group. The limestone at the top yielded a smaller fauna. This upper limestone apparently does not represent the top of the Yeso. Six miles farther south 

a limestone similarly situated with reference to the gypsum occurs 

within the Yeso several hundred feet from the top and is presumably 

the same as the one at the top of the Mesa del Yeso section, although 

the faunal basis of correlation is poor, Pleurophorus aft0 , subcostatus 

being the only fossil found. This limestone is overlain by gypsiferous 

shale and pink sandstone, which in turn underlie the massive San 

Andreas limestone.
24 MANZANO GROTJP OF HlO GRANDE VALLEY.

ALAMILLO.

In a small canyon cut into the Yeso formation 2 miles east of the 

Kio Grande (locality 5, PL I), opposite the Mexican village of Alamillo, the following fossils were collected:

Nucula levatiformis. 

Manzanella elliptica. 

Pteria sp.

Schizodus wheeleri? 

Pleurophorus aff. meeki. 

Astartella subquadrata.

Fossils from Yeso formation near Alamillo.

Phanerotrema manzanicum.

Euphemus inspeciosus. 

Zygopleura aff. rugosa. 

Orthonema socorroense. 

Coloceras mexicanum. 

Anisopyge inornata.

Plagioglypta canna.

BLACKINTON'S RANCH.

There is an exposure of the Yeso formation consisting of gypsum, 

gypsiferous shale, and earthy limestone near Charles F. Blackinton's 

ranch, 18 miles east of Socorro (locality 6, PI. I). From .a limestone 

near the top of the gypsum the following fossils were obtained: 

Edmondia gilbosaf, Schizodus wheeleri?, Pleurophorus aff. subcostatus, 

and Temnoclieilus aff. winslowi.

A limestone, 50 feet or more in thickness, lying stratigraphically 

above the gypsum is presumably the San Andreas limestone. The 

rocks are not well exposed at this place, and it was'not determined 

whether the space between the gypsum and the limestone is occupied 

by the light-colored sandstone which underlies the San Andreasdimestone in well-exposed sections. No fossils were found in the limestone, 

but stratigraphically above it there are beds of red sandstone and 

shale unlike any observed below the undoubted San Andreas limestone. Lying unconformably upon these upper red sediments is a 

coarse-grained light-brown sandstone, about 15 feet thick, that constitutes the base of the Cretaceous and grades upward into shale and 

limestone containing fossils of Benton age. No1 fossils were found 

in these upper red beds, and their relation to the underlying limestone was not determined. 'It remains an open question whether 

they belong to the Manzano group or are younger.

CARTHAGE.

The next section in order southward (fig. 4) was measured a few 

miles north of Carthage, about 120 miles south of Galisteo Canyon 

(locality 7, PI. I). The lower part of the section is not well exposed 

and the estimated thickness of 300 feet for the Abo sandstone and 610 

feet for the Yeso formation made in the field is probably too small, 

as these beds are known to be thicker both north and south of this 

place. The upper part of the Yeso is well exposed in a westward-
DETAILS OF SECTIONS.

ill . r Feet. 

150 

275

Limestone, massive, containing Schizodus 

wheeleri.

Sandstone, coarse, friable, pink to white, 

with a subordinate amount of shale.

75

25

25

10

200

facing cliff, in which an erosional unconformity also was noted, as 

shown in the section between the light-colored sandstone near the top 

and an underlying cherty limestone. But nothing was observed to 

indicate whether this unconformity is local or represents a time break 

of some importance.

The limestone at the top of the section is probably the San Andreas 

limestone, although no fossils were found in it at the point where 

the section was measured. But a little farther south, at the Carthage 

limekiln, the same limestone, here several hundred feet thick, yielded 

a few poorly preserved fossils, among which Schizodus wheeleri? was 

recognized. The limestone apparently underlies a bed of red shale, 

sandstone, and conglomerate. The contact was not observed. 

but the upper 200 feet 

of the red sediments 

are well exposed near 

the limekiln, where 

they are overlain unconformably by a 

coarse-grained yellow 

sandstone which constitutes the base of 

the Cretaceous beds 

and grades upward 

into fossiliferous limestone and shale of Benton age. No fossils 

were found in these 

upper red sediments 

and their age is a matter of conjecture. In 

physical character and stratigraphic position they resemble the upper 

red beds just described near Blackinton's ranch, a few miles to the 

north, and probably belong to the same formation.

FRA CRISTOBAL MOUNTAINS.

The next section to the south (fig. 5) was measured at Saddle 

Peak (see PL IV, B}, near the south end of the Fra Cristobal Mountains", about 165 miles south of Galisteo Creek (locality 8, PI. I). 

The northern part of the range consists of limestone of the Magdalena 

group, inclined toward the southeast. The Abo sandstone comprises the central part and the Yeso formation the southern part of 

the mountains, the youngest stratum exposed being a fossiliferous 

limestone which is probably a part of the San Andreas formation.

Possible unconformity. *^

Limestone, cherty.

Sandstone, gray.

Sandstone, red.

Limestone.

Gypsum, alternating with pink and yellow 

shales and fossiliferous limestone, containing 

Schizodus wheeleri?. (Thicknessestimated.)

300+ Sandstone, red, massive, 

mated.)

(Thickness estiUnconformity.

Limestone (Magdalena group).

FIGUBE 4. Section 2 miles north of Carthage.
26 MANZANO GROUP OF RIO GRANDE VALLEY.

The upper 1,000 feet are well exposed in the cliffs, and were easily 

measured by barometer. Although moderately well exposed the 

lower part was not measured, owing to lack of time, and the thicknesses are estimated.

The Fra Cristobal Mountains form a part of the western limb of 

the Jornada syncline and the strata are cut off abruptly on the west c 

by faults, as illustrated in Plate V. The photographs and the accompanying section show 

the structural condiII

II |"T

I I I

II

Feet.

200+ Limestone, massive, containing Marginifcraf

manzanica,Marginifcra?sv.,ComposUasubtilita?

Solenomya? nxnia, Clinovistha sp., Nucula

' levatiformis, Dentalium mcxicanum, Murchisoma? afl. terebra, Bcllcrophon majusculus.

175 Limestone, pink, thin bedded.

n-f fl-.£» rnrmn + ninc! Tn < >! llie mountains. ill

order Southward the

granite, thelimestone 

of the' Magdalena 

group, and finally 

the Manzano group,

200 Sandstone, pink and yellow, calcareous. , T i

plunge beneath the

75 Limestone containing Nucula levatiformis var. oetrital material ImobUqua/Schizoduswhecleri?, Astartclla subquad- ,',-, 

- .-, rota, and Euphcmus subpapillosus?. 1U6 

o i '- ', -j 10 Sandstone, yellow.

Wi/=ff''1/tt.7r 25 Limestone containing Scliizodus wheeleri? . 

50 Shale, gypsiferous.

NOGAL CREEK.

300 Gypsum, pink to yellow shale, and friable sand- nl

stone. (Thickness estimated.) A Small exposure.

of the Manzano group 

was visited on Nogal 

Creek west of the 

Rio Grande, opposite 

the north end of

400 Sandstone, red. (Thickness estimated.) , _. ~ . - ,

. . the Fra Cristobal

Mountains (locality 

9, PI. I). A thickatena group). ness of several hundred feet of red and

FIGURE 5. Section at Saddle Peak, near south end of Fra Cristobal yellow sandstone and 

Mountains. . i i -\ shale was observed

overlain by 300 feet of limestone. Near the middle of this limestone 

the following fossils were obtained: Schizodus wheelerif , Deltopecten 

coreyanus, Plagioglypta cannaf, Murchisonia? aff. terebra, Belleropkon 

majusculus, Orihonema sp. -a?, TemnocJieilus aff. concJiiferum.

Fifty feet higher in the same limestone "fossils were collected as 

follows : Productus ivesi, Productus leei, Productus mexicanus, EupJie-^ 

mus inspeciosusf , Murchisoniaf aff. terebra, Euomphalus sp. a?,- 

Orthonema sp. a.
U. S. GEOLOGICAL SURVEY BULLETIN 339 PLATE V

p.etritus.

A. WESTERN FACE OF THE FRA CRISTOBAL MOUNTAINS. 

Showing two faults, a and b.

7>'. FAULT PLANE AT THE WESTERN BASE OF FRA CRISTOBAL MOUNTAINS. 

Showing near view of a, above,
DETAILS OF SECTIONS. 27 

ENGLE. -

The next locality to the south at which the relations of the Manzano 

to the underlying and overlying formations were observed is near 

the north end of Caballos Mountains, at the head of Palomas Canyon, 

southwest of Engle (locality 10, PL I). A bed of red sandstone and 

shale here rests upon the massive limestone of the Magdalena group 

and dips gently toward the east. The red sediments are overlain 

by 300 feet of limestone, from which the following fossils were 

obtained:

Fossils from limestone near north end of Caballos Mountains.

Meekella mexicana. 

Productus leei. 

Pseudomonotis hawni? 

Pseudomonotis occidentalis? 

Schizodus wheeleri?? 

Deltopecten manzanicus.

Pleurophorus mexicanus. 

Plagioglypta canna. 

Euphemus inspeciosus? 

Bellerophon majusculus.

Euomphalus deformis. 

Sphserodoma aff. medialis.

This limestone is overlain by about 200 feet of shale, apparently 

gypsiferous although not well exposed where the observations were 

made, which in turn underlies fossiliferous limestone of Benton age.

The red beds at this point were observed before I became aware 

of their real significance and were not examined with the scrutiny 

that would later have been given them. Having in mind previously 

published descriptions," I regarded the fossiliferous limestone as a 

part of the Magdalena, brought up to the observed position by faulting, although I was unable to find evidence of faults which would 

explain the observed relations. The fossil evidence proves that the 

limestone,1 instead of belonging to the Magdalena, is a member of 

the Manzano group.

ELEPHANT BUTTE.

At the north end of the Caballos Mountains (locality 11, PI. I), 10 

miles north of the Engle locality, the Manzano lies between the steeply 

upturned limestones of the Magdalena on the west and the Benton 

(Cretaceous) sediments on the east. From one of the limestones 

near the top of the Manzano the following fossils were collected: 

Meekella mexicana, Schizodus wheeleri?, Aviculipinna nebraskensisf', 

Myalina apachesi, Deltopecten manzanicus, BelleropTion majusculus, 

Euomphalus sp. a, Euomphalus sp. If.

a Herrick, C. L., The occurrence of copper and lead in the San Andreas and Caballos mountains: Am. 

Geologist, vol. 22, 1898, p. 289. Keyes, C. R., Structures of basin ranges: Jour. Geology, vol. 13, 1905, 

p. 64.
28 MANZANO GROUP OF EIO GRANDE VALLEY.

CABALLOS MOUNTAINS.

J

The next section measured (fig. 6) is on the eastern slope of the 

Caballos Mountains, west of Upham and about 200 miles south of 

Galisteo Creek (locality 12, PI. I). As at Palomas Canyon, this section was observed before the true stratigraphic position of the red

Feet.

25 Limestone, blue,containing Productus led, Aviculipinna nebraskensis, Phanerotrema aff.

brazoense, Murchisoniaf terebraf, Murchisonia an*, terebraf, Euomphalus aff. pernodosus, Euomphalus sp. a, Orthonema sp. 6. 

50 Shale, red, sandy.

200 Limestone, blue, containing Echinacrinus cratis, Aviculipinna nebraskensis, Schizodus 

wheeleri??, DcntaUum mexicanum, Mogulia? sp., Bellerophon majusculus, Sucanopsis 

modesta, Sphxrodoma aff. mc.dialis, and Sphxrodoma an. texana.

200 Shale, red, and gypsum (not continuously exposed). 

10 Limestone.

Several hundred feet not well exposed.

10 Limestone. 

Not exposed.

800 Sandstone, red, massive. (Thickness estimated.)

Unconformity.

Limestone (Magdalenagroup). .

FIGUKE 6. Section in Caballos Mountains west of Upham.

beds was known and the examination was cursory, no effort being 

made to find fossils or recognize subdivisions of the beds. But 

although .the thicknesses as given in the accompanying section are only 

estimates, the beds are shown in their correct sequence. The limestone at the base belongs to the Magdalena group, as proved by fossil
DETAILS OF SECTIONS. 29

evidence, and the fauna of the.upper limestone is that of the upper 

part of the Manzano, presumably the San Andreas limestone.

\ I I

Feet.

500 Limestone, massive, containing Productus iyesif, 

Productus Iccif, Productus mexicanus?, Schizodus 

whecleri, Deltopectcn manzanicus, Bellerophon 

majusculus, Marginifera? manzanical, Marginifera? sp., Squamularia perplexaf, Composita mex* 

icana,. Euomphalus sp. ft.

200 Shale and sandstone, pink and yellow, soft,friable.

150 Gypsum.

J.O Limestone containing Aviculipinna ncbraskensis

and Schizodus wheelerif. 

150 Shale, alternating beds' of pink to yellow, and fossiliferous limestones (A). 

50 Limestone containing Parallelodon ail. obsolctus,

Pscudomonotis hawnif,Pseudomonotis occidentalis,

Myalina apachcsi,.Schizodus wheelerif, Pleurophorus ail. taffi, Pleurophorus sp.

700 Gypsum, red sandstone, and shale, and earthy 

limestone. (Thickness estimated, not continuously exposed.)

SAN ANDREAS 

MOUNTAINS.

Another section 

(fig. 7) was measured 

near the north end 

of the San Andreas 

Range, in the canyon through which 

the road passes from 

Ehgle to Rhodes's 

ranch (locality 13 ;P1. 

I). At the time the 

rocks were observed, 

I was influenced by 

the opinion of previous writers and 

supposed that the 

red beds belonged 

in the Permo-Triassic system. The fossils which prove 

them to be Carboniferous were discovered in the upper 

part of .the section 

as I was leaving the 

canyon, and no opportunity has been 

found since that 

time for making more 

extended collections. 

To judge from such 

observations as I 

was able to make, it 

is probable that one 

of the most complete 

sections of the Manzano group is to be 

found at this place.

The limestone of 

the Magdalena group 

at Rhodes's ranch is overlain by the dark-red Abo sandstone. These 

formations were observed hastily, as was also the lower part of the

700 Sandstone, red, massive (Thickness estimated.)

Unconformity.

Limestone (Magdalena group).

FIGURE 7. Section near north end of San Andreas Mountains, near 

Khodes's ranch.
30 MANZANO GROUP OF EIO GRANDE VALLEY.

Yeso formation, but fossils were found about 500 feet from the top 

of the red beds, and the upper part of the exposure was examined 

as carefully as the limited time would permit.

The San Andreas limestone, which derives its name from this 

locality,-.is the uppermost stratum exposed and has been .deeply 

eroded. However, on the western slope of the range, where some-, 

what like its original thickness remains, it is about 500 feet thick.

EXTENSION OF MANZANO GROUP TO THE NORTHEAST.

INTRODUCTORY STATEMENTS.

My purpose to confine attention principally to my own observations precludes any attempt at correlating the Manzano group with 

the red beds of western New Mexico and Colorado, since my observations have been confined mainly to the formations south and east 

of the Rocky Mountains.

As previously stated (p. 6), the Manzano group has been regarded 

as part of the so-called " Permo-Triassic " red beds of the Southwest, 

and I found nothing during the course of my field work to indicate 

that they are not correctly so regarded, but further investigation 

must be made before final correlations are possible. There are at 

least two lines of - investigation that promise good results by way of 

determining the relations of the Manzano to other red beds of the 

Southwest. (1) From the central and southern parts of the Rio 

Grande region the Manzano might be traced more or less continuously eastward and its relation to the Permo-Triassic rocks of eastern 

New Mexico be determined. (2) Its relation to the red beds east of 

the Rocky Mountains might be determined by tracing the latter 

around the south end of the mountains to the Rio Grande valley.

1. Although it is probable that the Manzano group is to be correlated with some part of the red beds of Texas and eastern New Mexico, 

as shown by Girty in the accompanying paper, little has been accomplished by way of tracing the formations. As previously stated 

(p. 21), Richardson traced the Manzano beds for a distance of 40 

miles east of the Manzano Mountains. He found, however, that 

still farther toward the east, for a distance of 15 miles, the sedimentary rocks are interrupted by crystallines, beyond which red .sediments 

again appear. But nothing was found to indicate whether the red 

beds east of the crystalline'rocks are of Pennsylvanian (Manzano), 

Permian, or Triassic age. Furthermore, it is not known whether the 

crystalline area results from a local uplift around which the sedimentary formations might be traced, or is a ridge forming a barrier between 

the Manzano group on the west and red beds of perhaps different 

age on the east.
EXTENSION OF MANZANO GROUP TO NORTHEAST. 31

2. During the summer of 1905 I had observed the rock formations 

of the Rio Grande Valley northward to Santa Fe and eastward to 

Glorieta Pass. During the autumn of 1907 I made a hasty examination of the rocks between Glorieta Pass and Las Vegas, N. Mex., 

for the purpose of determining the relation of the Manzano group to 

the red beds of the foothill region .east of the Rocky Mountains. On 

account of complicated structure the task proved to be a difficult 

one and unexpected results were obtained. Between Galisteo Canyon, 

where undoubted Manzano red beds occur, and Las Vegas, one of the 

localities at which Hayden 0 examined the so-called Jura-Triassic 

red beds'of the eastern foothills, the rocks were examined and sections measured in Apache 1 Canyon, near Rowe, and near Bernal 18 

miles, 30 miles, and 50 miles, respectively, east of Galisteo and near 

Las Vegas, 20 miles north of Bernal.

APACHE CANYON.

As described on page 18, the beds of the Manzano group in Galisteo 

Canyon dip steeply to the east beneath sediments of Cretaceous age, 

the upper member of which is the Galisteo or late Cretaceous red 

bed formation that occupies the plain between Lamy and Cerrillos. 

In Apache Canyon east of Lamy and about 2 miles southwest of 

Canyoncito an extensive series of red sediments occur in contact 

with the granitic core of the Rocky Mountains. These sediments 

are continuously exposed from Lamy eastward around the southern 

end of the mountains to Las Vegas and beyond. They are parts of 

the so-called "Red Beds" formation, but whether they are to be 

correlated with the older or Pennsylvanian red beds or with some 

younger group can not be definitely stated. They are not distinguishable without careful examination from the red beds of the 

lower Pennsylvanian (Magdalena group) of the Pecos Valley a few 

miles to the east, described on page 34, nor from the upper Pennsylvanian red beds (Manzano group) of the Rio Grande Valley to the 

west, nor from the Galisteo red beds of late Cretaceous age in the 

Lamy-Cerrillos region. However, they contain plant remains, as 

mentioned below, which apparently place them at a horizon much 

lower than the Galisteo.

In Apache Canyon the sedimentary rocks north of the railroad are 

upturned against the granitic mass of the mountains and dip about 

40° SE., or toward Glorieta Mesa. South of the railroad they are 

more nearly horizontal and form the bordering cliffs of Glorieta Mesa. 

The following section was measured by pacing across the upturned

a Hayden, F. V., Kept. U.S. Geol. Survey of Colorado and New Mexico, Washington, 1869 (Third Annual 

Report), 1873, pp. 162-166.
32 MANZANO GEOTIP OF RIO GRANDE VALLEY.

edges of the beds north of the railroad. Lying stratigraphically 

above the beds described in the section and outcropping at the 

bottom of the canyon are a few hundred feet of red sediments whose 

eroded edges are now obscured by valley accumulations. One 

thousand feet or more of still younger red beds are exposed in the 

cliffs forming the south wall of the, canyon.

Partial section of red beds exposed in Apache Canyon, New Mexico.

Feet. 

Sandstone, with partings of pink shale..................................... 150

Conglomerate, containing many subangular pebbles of blue limestone....... 10

Sandstone, .prevailingly red in color, with partings of red shale............. 170

Sandstone, conglomeratic, locally cemented to an iron stone by iron oxide 

and containing small iron concretions and silicified trees................. 50

Sandstone, conglomeratic, and shale alternating; red, yellow to white in 

color (thickness estimated).............................................: 1, 500

Sandstone, conglomeratic; pebbles mostly of limestone.................... 20

Shale, red.........,...............-.'.................................... 25

Sandstone, coarse, light colored, massive.................................. 35

Sandstone, brown, calcareous, containing plant remains (mentioned below).. 8 

Shale and sandstone, red:..:.............................................. 90

Conglomerate............................................................ 10±

Sandstone and shale, red, alternating........... 1............... J......... 100

Conglomerate, red, consisting of angular and subangular pebbles of various 

crystalline rocks and fossiliferous limestone lithologically similar to the 

limestone of the Magdalena group found in the Pecos Valley a few miles 

to the east............................................................. 10+

Granite.

The actual contact of the red beds and the granite was not seen at 

the point where the section was measured, but the hill against which 

the sedimentary rocks lie is granite and the field relations are such 

as to lead me to believe that the lowest conglomerate lies, upon the 

granite,, and its composition suggests strongly that it is a basal 

conglomerate.

The limestone of the Magdalena group, identified by its fossils, is 

represented in Apache Canyon by only small remnants. The formation is 1,000 feet or more in thickness both east and west of Glorieta 

Mesa and presumably is continuous beneath the mesa. The uniformity in thickness and character of the Magdalena group over 

wide areas, the narrowness of the space from which it is absent in 

the vicinity of Glorieta Pass, and the presence in the overlying conglomerates of pebbles of limestone, apparently derived from the 

Magdalena, are regarded as sufficient evidence that these beds once 

extended continuously over this region and were removed by erosion 

previous to the formation of the red beds.

The only identifiable fossils obtained from the red sediments in 

Apache Canyon are certain plants that I found 210 feet above the 

basal conglomerate and some collected by T. W. Stanton from about 

the middle of the. 1,500-foot member of the section. These have
EXTENSION OF MANZANO GROUP TO NORTHEAST. 33

been examined by F. H. Knowlton and David White, who state 

that the forms can not be satisfactorily identified, but express the 

opinion that they probably indicate Permian or Triassic age.

Since there are differences of opinion among paleontologists regarding the age of the so-called Permian beds of the Southwest, it is 

possible that these plant-bearing red beds -are to be correlated with 

the Manzano red beds, which, although here described on faunal 

evidence. as a group of the Pennsylvanian series, contain a fauna 

similar to that of the Quartermaster formation of Oklahoma, which 

Beede a and others regard as Permian. On the other hand, if "Permian" in this case is to be interpreted as indicating beds younger 

than the Manzano, it becomes difficult, in the light of the facts described in the following sections, to explain the observed relations, 

and if the beds are of Triassic age the problem is still more complex.

In any case, it is clear that something more than reconnaissance 

examination is necessary before final conclusions can be reached.

The collections of plant remains contain two types of coniferous 

cones a curious stem, branches, and branchlets of a conifer and 

-fragments of a fern pinnule. In their report on these forms Knowlton 

and White state that 

The coniferous branches and branchlets are probably to be referred to Walchia, of 

the group W. pinniformis, though somewhat slenderer than the usual forms of this 

species. We find fragments of cones which it does not seem possible with the material 

in hand certainly to separate generically from the cones of Walchia, and there are 

detached cone scales that apparently show the same affinity. There are also minute 

fragments of a fern pinnule that appear to belong to the genus Laccopteris. The 

larger cones are at least strongly suggestive of those of Voltzia, while the curious stem 

has somewhat the appearance of the pith of one of these ancient types. With -these 

strongly suggestive facts in mind we regard the age as probably Permian or Triassic.

ROWE.

A section of the rocks exposed between Pecos River and the top of 

Glorieta Mesa was measured 1 mile east of Rowe (fig. 8), a railroad 

station 10 miles east of Apache Canyon. A great thickness of limestone and shale of the Magdalena group is exposed in the Pecos Valley, but only the upper 600 feet are included in the part measured. 

. The red beds overlie the limestone with apparent conformity. The 

transitional bed is a subcrystalline limestone, 50 feet thick, in which 

are angular pieces of granite and yellowish pink feldspar like that in 

the granite of the mountains to the north. In some places the rock 

consists of nearly equal parts of feldspar and limestone.

Above this lime breccia occur the red beds, which through a thickness of 100 feet or more contain beds of fossiliferous limestone of

a Beede, J. W., Invertebrate paleontology of the upper Permian red beds of Oklahoma and the Panhandle of Texas: Bull. Kansas Univ. Sci., vol. 4,1907, pp. 115-171,

84259 Bull 3.89 09 3
34 MANZANO GKOUP OF RIO GRA2STDE VALLEY.

varying character. In some places the limestone is gray and massive, 

in others it occurs in subcrystalline layers separated by red shale. I 

obtained from the limestone fossils that Girty regards as more nearly 

allied to the Magdalena than to the Manzano fauna.

I.I.I

ill , T

i ' 

Feet. '

175 Sandstone, yellow, weathering to pink and brown, coarse-grained, 

massive.

2 Limestone, impure, cement-like.

350 Sandstone, dark red.

300 Sandstone, red and white beds alternating, coarse-grained, locally 

conglomeratic.

10± Conglomerate, gray, pebbles of crystalline and metamorphic rock.

Possible unconformity. 

100 Shale and sandstone, red.

100 Sandstone and shale, red, containing beds of subcrystalline, red to

gray limestone with irregular cement-like surface. 

50 Limestone, fragmental and subcrystalline, containing pebbles and 

angular fragments of quartz and feldspar.

400 Limestone, blue, massive.

200+ Shale with thin beds of coal; limestone and sandstone.

FIGURE 8. Section of red beds 1 mile east of llowe, N. Mex. (For fossil contents seef ollowing section.)

Two hundred feet above the base of the red beds, as shown in the 

following section, is a prominent conglomerate, which on further study 

.may be found to mark a time break, but no fossils were found above 

it, and the age of the upper beds is not known.

Section of red beds 1 mile east of Rowe, N. Mex.

Feet.

Sandstone, coarse grained, massive, yellow, weathering to pink and brown.... 175

Limestone, impure, cement-like........................................... 2

Sandstone, dark red....................................................... 350

Sandstone, coarse grained, locally conglomeratic, red and white beds alternating. ......................'........................................... 300
EXTENSION OP MANZANO GROUP TO NORTHEAST. 35

' Feet. 

Conglomerate, gray, pebbles of crystalline and metamorphic rock.............. 10±

Shale and sandstone, red.................................................. 100

Sandstone and shale, red, containing beds of subcrystalline red to gray limestone with irregular cement-like surface. This limestone yielded the fol-

 lowing fossils: Lophophyllum? sp., Polypora sp., Fenestella 3 sp., Cyclopora 

sp., Fistulipora sp., Derby a sp., Chonetes sp., Productus cora, Productus 

nebraskensis, Spirifer cameratus, Spiriferina sp., Composita subtilita, Pugnax 

osagensis, Dielasma bovidens, Myalina subquadrata, Myalina sp., Modiola 

subelliptica, Deliopecten occidentalism, Acanthopecten carboniferus, Aviculipecten sp., Parallelodon carbonarius, Pleurophorus? sp., Edmondia nebraskensis?, Schizodus sp., Pleurophorella costata, Euconospira sp., Bellerophon sp., 

Soleniscus altonensisf, Orthonema? sp., Naticopsis sp., Platyceras n. sp., 

Metacoceras? aff. walcotti, Nautilus sp., Tainoceras aff. ocddentale, Orthoceras 

sp., Phillipsia aff. scitula. ............................................... 100

Limestone, subcrystalline, containing pebbles and angular fragments of quartz 

and feldspar. Contains Composita subtilita. ............................... 50

Limestone, blue, massive. Contains Productus nebmshnsis, Spiriferina kentuckyensis, Squamularia perplexa, Composita subtilita, Cleiothyridina missouriensis, Hustedia mormoni, Cardiomorpha? sp., Astartella sp., Aviculipinna 

peracuta. ............................................................... 400

Shale with thin beds of coal; limestone and sandstone. Contains Fistulipora 

sp., Derbya? sp., Productus semireticulatus, Productus cora, Spirifer cameratus, 

Composita subtilita, Myalina wyomingensis?, Metacoceras aff. walcotti. ........ 200

BERNAL.

About 5 miles southeast of Rowe conglomeratic red sandstone 

lies unconformably upon limestone of the Magdalena group, and again 

about 20 miles southeast of Rowe, at a point on the railroad 6 miles 

east of Pecos River and 1 mile west of the Mexican village of Old 

Bernal, the same red conglomeratic sandstone lies unconformably 

upon the Magdalena, which was here arched and eroded previous to 

the deposition of the red sediments. At the point where the contact is best exposed the limestone dips 30° and the overlying red 

beds are horizontal. Their lowest member is a coarse conglomeratebreccia containing angular and subangular fragments, some of which 

are several inches in diameter, composed of igneous and metamorphic 

rocks, red sandstone, and blue limestone apparently derived from 

the underlying limestone of the Magdalena. The limestone pebbles 

contain crinoid stems and fragments of spirifers and other brachiopods. The composition of this conglomerate and its unconformable 

relation to the underlying beds are regarded as sufficient evidence 

that the.red beds at this point are younger than the lowest red beds 

at Rowe and at Las Vegas, which are conformable with the underlying limestone of the Magdalena, and although conglomeratic, do not 

contain limestone pebbles so far as now known. It is possible 

that this conglomerate may be the same as the one 200 feet above 

the base of the red beds at Rowe; a suggestion that finds support
36 MANZANO GEOUP OF EIO GRANDE VALLEY.

in the lithologic resemblance of the beds above the conglomerate 

at both localities and in their continuity in the cliffs between the two 

points. Furthermore, these upper beds are continuously exposed in 

the cliffs of Glorieta Mesa, and it is possible that the conglomerate in 

the sections at Bernal and at Rowe may be the same as the basal 

conglomerate in Apache Canyon. However this may be, the known 

facts apparently warrant the conclusion that after the oldest red 

beds were deposited an uplift of the mountains occurred and extensive erosion took place. It is probable that this period of erosion is 

the same as that during which the Magdalena beds were removed 

from the Apache Canyon region, and may prove to be the same as 

that represented by the unconformity between the Magdalena and 

the Manzano groups of the Rio Grande region.

The following fossils were collected from the limestone of the 

Magdalena group at Bernal:

Fossils from limestone of the Magdalena group at Bernal.

Lophophyllum profundum. 

Eupachycrinus sp. 

Septopora sp. 

Derbya sp.

Meekella striaticostata. 

Productus punctatus.' 

Productus nebraskensis. 

Productus nebraskensis? 

Productus semireticulatus. 

Dielasma bovidens. 

Spirifer cameratus.

Squamularia perplexa. 

Spiriferina kentuckyensis. 

Composita subtilita. 

Aviculipecten sp. 

Myalina sp. 

Bellerophon crassus? 

Platyceras nebraskense. 

Dentalium? sp. 

.Metacoceras? aff. walcotti. 

Orthoceras sp. 

Phillipsia aff. major.

Spirifer rockymontanus.

LAS VEGAS

Between Bernal and Las Vegas, a-distance of 20 miles, red sedimentary rocks are exposed continuously. A section was measured 

about 5 miles northwest of Las Vegas, in the foothills south of Hot 

Springs. This section differs from others described in having rocks 

of known age both below and above the red beds, which are here 

apparently conformable with the underlying limestone of the Magdalena group and are overlain by the Morrison shale and the Dakota 

sandstone. Fossils contained in the lower 200 feet of the red beds 

prove that the lowest beds are of Magdalena (lower Pennsylvanian) 

age, but no evidence other than stratigraphic position was found 

that tends to reveal the age of the higher beds. There are several 

conglomerates, some one of which may be continuous with the basal 

conglomerate at Bernal and Apache Canyon, although it was my 

impression when I was in the field that the erosion interval so conspicuous at these places is 'not represented by a hiatus in the
EXTENSION OF MANZANO GROUP TO NORTHEAST. 37

Las Vegas section. The sediments 

are like those of Glorieta Mesa 

in that they are red and consist 

of shale and conglomeratic sandstone, but I found no beds in the 

Las Vegas section that resemble 

those of Glorieta Mesa closely 

enough to warrant even a provisional correlation.

The red beds at Las Vegas are 

parts of the so-called "Jura-Trias" 

of the eastern Rocky Mountains 

and were described as such by 

Hayden a as early as 1873. Hayden's section was measured at Hot 

Springs, a mile or more north of the 

point where I measured the following section and where the strata 

are much less disturbed than they 

are near Hot Springs. Some of the 

upper members of the Las Vegas 

section are presumably equivalent 

to the red beds of the plains to 

the east in which Triassic fossils 

have been found, and the uppermost massive member is similar 

in appearance, composition, and 

stratigraphic relations to the Exter 

sandstone,6 which I have previously described as resting with 

angular unconformity upon the underlying red beds.

It is possible that between the lower Pennsylvanian red beds of the 

Las Vegas section and those of Triassic age may be found beds to be 

correlated with the upper Pennsylvanian or Manzano group of the Rio 

Grande Valley, and with the Permian of the Texas region, but no such 

subdivision of the section can be 

made without further examination.

a Hayden,F.V., Rept. U.S. Geol. Survey of Colorado 

and New Mexico, Washington, 1869 (Third Annual 

Report), 1873, pp. 162-166.

6'Lee, W. T., The Morrison shales of southernColorado and northern New Mexico: Jour. Geology, vol. 

10,1902, p. 45.

 i VcJe&'oCi- '.": i V.

150 (12)

Feet. 

25 (1) 

5 (2) 

50 (3)

250 (4)

150 (5)

5 (6) 

25 (7)

2,000 (8)

20 (9) 

5 (10)

600 (11)

Many hundreds of feet. (30)

FiG. 9. Section 5 miles northwest of Las Vegas, 

N. Mex. "Figures in parentheses refer to detailed section given in text. 
38 MANZANO GROUP OF RIO GRANDE VALLEY.

The character and succession of the beds of this section are shown 

graphically in figure 9, and their relations to older and younger rocks 

are as follows: ' .

Section 5 miles northwest of Las Vegas, N. Mex.

Feet.

(1) Sandstone (Dakota).................................................... 25

(2) Fire clay (believed to be northward extension of Comanche)0 ........... 5

(3) Sandstone (formerly referred to Dakota) 0................................ 50

(4) Shale and sandstone, variegated (Morrison)............................. 250

(5) Sandstone, massive, pink to brown (Exter?)............................ 150

(6) Limestone, black, finely laminated, smelling strongly of petroleum ...... 5

(7) Sandstone, light brown, massive....................................... 25

(8) Sandstone, red, with much red shale and several beds of conglomerate

(thickness estimated)............................................... 2,000

(9) Sandstone, gray, coarse grained, conglomeratic ......................... 20

(10) Conglomerate......................................................... 5

(11) Shale, sandy, red to purple (not continuously exposed)................. 600

(12) Sandstone, conglomeratic, pink to gray ................................ 150

(13) Shale and sandstone, red (not continuously exposed).................... 200

(14) Limestone, hard, brittle, containing crinoid stems....................... 2

(15) Not exposed......................................J................... 100

(16) Limestone, brittle, conglomeratic...................................... 3

(17) Shale, red and yellow................................................. 30

(18) Sandstone, conglomeratic............................................. 4

(19) Shale, red ........................................................... 10

(20) Limestone, sandy .................................................... 1

(21) Shale, red ........................................................... 10

(22) Limestone, brittle.................................................... 1

(23) Shale, red ........................................................... 10

(24) Limestone, hard, brittle, weathering to rounded bowlders. Contains Productus cora, Productus semireticulatus, Productus punctatus, Composita 

subtilita, Allerismd terminate? .......................................

(25) Shale, red, sandy......................................................

(26) Sandstone, arkose, pink to yellow, with beds of impure limestone.......... 40

(27) Sandstone, conglomeratic, consisting of coarse grains of quartz, pebbles of 

crystalline and metamorphic rocks, and angular fragments of feldspar 

and blue limestone; and subcrystalline limestone containing Lophophyllum profundum, Rhombopora sp., Cyclopora sp., Fenestella sp., Derby a 

.sp., Productus cora, Productus punctatus, Spirifer rockymontanus, Spirifer 

cameratus, Squamularia perplexa, Spiriferina Kentuckyensis, Composita 

subtilita, Dielasma bovidens, Aviculipecten sp., Myalina sp., Conularia sp. 10

(28) Limestone, subcrystalline, containing the same fossils as the limestone .

immediately above it.............................................. 15

(29) Sandstone arkose, coarse grained, pink to yellow......................... 75

(30) Pennsylvanian limestone, Magdalena group, many hundreds of feet, massive, blue, containing Produces cora, Productus nebraskensis, Squamularia 

per.plexa, Composita subtilita, Cleiothyridina missouriensis, Hustedia mormoni, Cardiomorpha? sp., Astartella sp., Aviculipinna peracuta.

a Stanton, T. W., The Morrison formation and its relations with the Comanche series and the Dakota 

formation: Jour. Geology, vol. 13,1905, pp. 657-669.
SUMMARY OF STRATIGRAPHY. 39 

SUMMARY.

Although the accumulation of red sandstone and shale began in 

Mississippian ("Lower Carboniferous") time at Perry Park and elsewhere in Colorado, in the mountain region of New Mexico it began 

in Pennsylvanian ("Upper Carboniferous") time, as shown by the 

occurrence of a Magdalena fauna in the oldest red beds near Rowe 

and Las Vegas.

In late Magdalena time (near the middle of the Pennsylvanian) some 

change, presumably uplift, occurred in the mountain region of New 

Mexico, which caused a change in character of the- accumulating 

sediments from limestone to red shale and coarse-grained red sandstone. The change was apparently slow, as evidenced by the gradual 

transition shown in the Rowe and Las Vegas sections, but was of such 

magnitude, as evidenced by the occurrence of the feldspar breccia 

of the Rowe section, that it brought the basal crystallines of the mountains into a position where they furnished sediments. In case the 

limestone of the Magdalena group originally extended continuously 

over the crystalline rocks at this place, as there is some reason to 

believe, there must have been an uplift of 1,000 feet or more and erosion to an equal depth before the granitic debris could be furnished. 

This suggestion finds some support in the character of the breccia. 

The feldspar crystals are but slightly water worn and were evidently 

derived from sources near by.

In the Rio Grande region there is evidence of uplift and erosion in 

mid-Pennsylvanian time, immediately preceding the deposition of the 

Manzano beds. This uplift may have occurred early enough to prevent the deposition of the lower Pennsylvanian (Magdalena) red beds, 

but their absence from the Rio Grande valley is probably better 

explained as a result of erosion. Because of the uncertainty as to the 

age of the beds above the basal conglomerate at Bernal, Rowe, and 

Apache Canyon, it is not known whether this movement is the same 

as that just mentioned as occurring in late Magdalena time, or is to 

be associated with the uplift which caused the more extensive erosion 

evidenced by the greater unconformity at the base of the red beds in 

Apache Canyon, which are said to be of Permian or Triassic age.

The mid-Pennsylvanian erosion was followed in the Rio Grande 

region by the accumulation of the Manzano group of red beds, which 

are described in this bulletin. They constitute a part of the so-called 

"Red Beds formation" of the Rocky Mountain region, and in composition, physical character, and faunal relations they are similar to 

some of the so-called "Permian Red Beds" of the Texas region, with 

which they are probably to be correlated, although they are here
40 MANZANO GROUP OF EIO GRANDE VALLEY.

described, as a group of the Pennsylvanian series, to which the fossils 

prove that they belong. They are also probably equivalent to some 

part of the red beds of the eastern Rocky Mountains, but final correlations can not now be made.

The San Andreas limestone, the youngest member of the Manzano 

group, is absent from the northern part of the region, but whether 

because of nondeposition or because of erosion is not definitely 

known. Near Carthage it is overlain by red beds, the lowest member 

of which is a basal conglomerate containing pebbles of crystalline 

and metamorphic rock that must have come from distant localities. 

In the northern part, where the San Andreas is absent, the variegated shales provisionally referred to the Morrison are in contact 

with the Yeso formation. It is probable that uplift and erosion 

followed the deposition of the Manzano group, removing parts of it, 

and that the red beds above the San Andreas near Carthage may be 

of Permian or Triassic age. Red-bed accumulation in the Rocky 

Mountain and Plains regions is now known to have covered a period 

of time extending from Mississippian to Jurassic, and the geologic 

history during this time was complex.
PALEONTOLOGY OF THE MANZANO GROUP.

By GEORGE H. GIRTY.

INTRODUCTION.

While by no means without intrinsic interest, the fauna of the 

Manzano group is perhaps more interesting for extrinsic reasons. It

contains a considerable number of undescribed species, but at the same 

time does not present that novelty of facies, when compared with our 

typical Pennsylvanian faunas, which is sometimes found in the West. 

Furthermore, the Manzano shells are liable to be fragmentary and 

much inferior in preservation to the Pennsylvanian fossils of the Mississippi Valley. Through some peculiarity of preservation they are 

too often obscured in sculpture and in outline.

Some 84 varieties have been discriminated in the collection examined, which from one point of view may be distributed into three 

classes: Species described for the first time, and these are reasonably 

numerous; identifications with known species which have a purely 

western distribution; and identifications with certain species which 

have a wide distribution and occur in the more eastern faunas also. 

The first group is of value for correlation purposes only prospectively; 

the second carries suggestions of certain correlations in adjacent areas, 

while the last may, when properly interpreted, indicate certain relationships with faunas of the Mississippi Valley Pennsylvanian.

Intrinsically there seems to be no marked difference between the 

assemblages of species which occur in the three divisions of the 

Manzano group that can be discriminated on lithologic grounds. 

Collections made at different horizons .in the same section show no 

greater faunal distinctions than collections made at the same horizon 

in different sections. Nevertheless, certain peculiarities of range are, 

in fact, indicated, and it may be restated in this connection, though 

almost a truism, that the tendency of imperfect material is always 

toward the obliteration of faunal differences. On the other hand, 

every collection must necessarily show certain idiosyncrasies, in failing 

to represent the real range and distribution of organic types. Tables, 

then, both in the differences which they indicate and in those which

41
42 MANZANO GROUP OF RIO GRANDE VALLEY.

they fail to indicate, are merely approximations that should be verified and. corrected by subsequent data.

The subjoined tables are arranged to show the species identified at 

each locality and their known range in the different sections where 

collections were made. It would appear that in but a single section 

(No. 4) are the three divisions faunally represented. The Abo arid 

Yeso faunas appear together only in section 4, while the Yeso and 

San Andreas appear together in sections 4, 7, 8, and 13. Much space 

might be covered in pointing out the species which are common to two 

or to all three formations and those which are restricted to one of 

them, but anyone who is interested can readily note these facts for 

himself in the table. The two species which are most persistent in 

all the sections and at all the horizons are those identified as Schizodus 

wheeleri and BelleropJion majusculus, but in these types the limit of 

error is especially great because of their imperfect preservation.

Regarding the fauna from the biologic rather than the stratigraphic 

side, it is perhaps worthy of remark that the Mollusca exhibit more 

than the usual abundance and differentiation, while the Brachiopoda 

are less abundant and differentiated than is usual- in the ordinary 

Pennsylvanian fauna.

Different as they are in physical aspect, it is highly probable that the 

Manzano and Hueco are equivalent formations. The Manzano faunas 

are more closely related to those of the upper Hueco than to those of 

the lower, in which brachiopods are abundant. Whether the Magdalena group, which underlies the Manzano, is represented in the 

Hueco has not been definitely determined. Faunally the Hueco 

presents many aspects not known in either the Magdalena or the 

Manzano.

In the Grand Canyon section the Manzano appears to find its representation in the Aubrey group. Probably both the upper and 

lower Aubrey correspond to the Manzano. The beds in these two 

areas have ,in common the three very characteristic species Productus 

ivesi, Allerisma capax, and Dentalium canna, while no doubt other 

types can be cited when the faunas have been worked out in detail. 

Upon this basis the limestone (Magdalena group) which underlies the 

Manzano would probably correspond .to the upper part of the Redwall 

limestone, from which a Pennsylvanian fauna is cited by Gilbert. a 

The lower part of the Redwall, with its lower Mississippian fauna, is 

more or less exactly equivalent to the Kelly and the Lake .Valley 

limestones of New Mexico, whose position is below the Magdalena.

In Colorado the equivalent of the Manzano is, I am now disposed to 

believe, the Rico formation. Lithologically, stratigraphically, and 

faunally the Hermosa and Rico formations show many points of 

resemblance to the Magdalena and Manzano. It is proposed to

a Gilbert, G. K., U. S. Geog. Surveys W. 100th Mer., Kept., vol. 3,1875, p. 178.
PALEONTOLOGY. 43

A >

speak of the Magdalena and Hermosa in another paper, but accepting/ « 

the equivalence as a working hypothesis, the correlation of the Manzano and Rico seems justified in view of the close proximity, geographically and the fact that both are "Red Beds" formations, occupying corresponding positions in the section. The faunas of the 

Rico and Manzano show a general resemblance in the limitation of the 

brachiopocl forms and the abundance of the pelecypods and gasteropods. Generically they exhibit a striking' correspondence, while a 

number of species are common to both faunas, such as Productus 

com, Composita subtilita, Deltopecten occidentals, Pseudomonotis . 

Jiawni, Aviculipinna nebraskcnsis, AUerisma terrrdnale, and Edmondia 

gilibosa. Besides these many instances could be cited of kindred forms 

and forms which upon revision might prove to be the same.

The correlations here adopted of the Manzano group with the 

Aubrey on the one hand and the Rico on the other naturally bring the

Arizona formation into alignment with that of Colorado in spite of 

the fact that the Rico fauna is very different from that of the Aubrey. 

Although none of the characteristic Aubrey forms has been found in 

the Rico, the Manzano fauna to a certain extent presents a combination of types which occur in the Rico, but not in the Aubrey, and those 

which occur in the Aubrey, but not in the Rico.

As to the relationship of the Manzano group to the Pennsylvanian 

section as it is developed in the Mississippi Valley, it would be inadvisable to write at length at present. The Manzano fauna differs 

considerably from any of the Carboniferous faunas known from that 

region, whether of Pennsylvanian or so-called Permian age. The 

assemblage of forms which perhaps more closely than any other suggests that contained in the Manzano beds occurs in the Whitehorse 

sandstone and Quartermaster formation of Oklahoma and Texas.a 

These rocks are, relatively speaking, not so very remote in the two 

areas, and the fact that in both cases they form part of the "Red 

Beds" makes the correlation a rather inviting one. Mr. Beede in his 

discussion of the Whitehorse and Quartermaster faunas seems to 

adopt this correlation with the Manzano group, at least in a general 

way. Although the two faunas contain some closely related and 

possibly equivalent-species, there is only one which at the time of 

writing seems to be identical in the two formations, namely, Deltopecten vanvleeti. The brachiopod element seems to be entirely lacking from the Quartermaster and Whitehorse faunas, and though 

fairly abundant in the Manzano the representation is distinctly 

limited.

On the whole, however, it seems rather probable that the Manzano 

and Whitehorse-Quartermaster horizons will prove to be in a general 

way equivalent, but if so, some remarkable and interesting relations

a Beede, J. W., Bull. Kansas Univ. Scl., vol. 4,1907, pp. 115-171.
44 MANZANO GBOTJP OF BIO GRANDE VALLEY.

between other formations are opened up. It would appear, in brief, 

upon this hypothesis, that if the Guadalupian beds are equivalent to 

the Russian Permian, the so-called Kansas Permian is much older; and 

if, on the other hand, the Kansas "Permian" is equivalent to that of 

Russia, the Guadalupian represents a distinct and still younger epoch. 

This involves, on the one hand, the equivalence of the Manzano beds 

and the Hueco formation and the superposition of the Guadalupian 

series upon the Hueco, and, on the other, the determination of the 

Whitehorse and Quartermaster rocks as higher than the highest fossiliferous "Permian" of Kansas. Given, then, the equivalence of 

the Manzano and the Whitehorse-Quartermaster horizons, as hypothetized above, the Guadalupian must be considerably younger than the 

Kansas "Permian."

As to the correlation of the Manzano and the Hueco, I feel at 

present very little doubt, and it is certainly true that the Manzano 

fauna is extremely unlike that of the Guadalupian beds. At present 

also it seems practically impossible that the stratigraphic relations 

of the Hueco and Guadalupian formations are different from what 

they have generally been considered to be that the former underlies 

the latter. Regarding the relations of the Whitehorse and Quartermaster rocks to the Kansas "Permian," I have no independent 

opinion to advance. The crux of the whole matter seems to lie in 

the relation of the Manzano beds to the Whitehorse and Quartermaster rocks. 'As to the probability of their being equivalent, two 

additional points may be noticed. In the first place, only the most 

remote relationship can be traced between the Guadalupian fauna 

and the faunas of the Whitehorse and Quartermaster. beds as at 

present known. In the second place, Beede remarks that the American types experience a decided decrease and the foreign ones a 

decided increase in passing from the Whitehorse to the Quartermaster horizons. . Already I have called attention to the striking foreign 

faeies which appears in the Hueco formation, from which circumstance the Hueco would appear to be no older at least than the 

Quartermaster beds.

I have spoken more fully elsewhere as to what seemed to me the 

probabilities' of correlation between the Hueco and Guadalupian 

series and the Russian Permian. The Hueco fauna in many respects 

is strikingly similar to the Gschel fauna, which underlies the Permian and Artinsk in Russia.

Herrick0 has employed the designation "Permian" for part of the 

Manzano group, citing as Permian forms the three following species: 

Bakewellia parva, Myalina attenuata, and Pleurophorus subcuneatus, 

which probably are Pteria sp., Myalina apachesi, and PleuropJiorus

oHerrick, C. L., Bull. Univ. New Mexico, vol. 2, fasc. 3, 1900, p. 4; Jour. Geology, vol. 8,1900, p. 115.
PALEONTOLOGY. 45

aff. subcostatus of the present report. He evidently has in mind in 

this correlation the "Permian" of Kansas and Nebraska. That 

there is any substantial evidence for correlating the Manzano with 

the Russian Permian I am not disposed to believe, but that it may 

be more or less equivalent to the Kansas "Permian" seems, as 

already stated, not improbable.

The accompanying table shows the range and distribution of the 

Manzano species thus far obtained by Mr. Lee, who made all the 

collections on .which this paleontologic account is based. The first 

series of columns show the local faunas, the numbers at the top 

being lot numbers, which refer to localities described in detail in the 

locality register given on pages 119-120. To the right are the composite faunas, in columns grouped under the formation names Abo, 

Yeso, and San Andreas. It seemed best to make a geographic subdivision of the formational faunas, and consequently the numbers

heading these columns stand for certain districts or sections, as used 

by Mr. Lee in his portion of the paper and shown on Plate I, to wit:

1. Galisteo Canyon.

2. Sandia Mountains.

3. Abo Canyon.

4. Mesa del Yeso.

5. Alamillo.

6. Blackinton's ranch.

7. Carthage.

8. Fra Cristobal.

9. Nogal Creek.

10. Engle.

11. Elephant Butte.

12. Caballos Mountains.

13. San Andreas Mountains.

The lots combined to make up the composite formational faunas 

in the different areas are as follows:

Abo sandstone:

Sandia Mountains (2), comprising lots 3796, 3797, and 3798.

Abo Canyon (3), comprising lot 3757a.

Meso del Yeso (4), comprising lot 3751. 

Yeso formation:

Mesa del Yeso (4), comprising lots 3751a, 3751b, and 3751c.

Alamillo (5), comprising lot 3751e.

Blackinton's ranch (6), comprising lot 3750.

Carthage (7), comprising lots 3753, 3747a.

Fra Cristobal (8), comprising lots 3743a, 3743b.

San Andreas Mountains (13), comprising lots 3742b, 3742c, 3742d, 3742e, and 3742g. 

San Andreas limestone:

Mesa del Yeso (4), comprising lot 3751d.

Carthage (7), comprising lots 3746, 3746a.

Fra Cristobal (8), comprising lot 3743.

Nogal Creek (9), comprising lot 3744, 3744a.

Engle (10), comprising lots 3595, 3740, 3740a.

Elephant Butte (11), comprising lots 3741, 3600. 

. Caballos Mountains (12), comprising lots 3738, 3738a.

San Andreas Mountains (13), comprising lots 3742, 3742f.
Range-and distribution of the fossil invertebrates found in the Manzano 

Meekella striaticostata. ............................. ..........

Productus mexicanus? ........................................

Productuscora................... ...... ..... . ..........

Squamularia perplexa. ........................... ..........

Edmondia gibbosa ............................................

Bellerophon maiusculus. ..........:...........................

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Range and distribution of the fossil invertebrates found in the Manzano group 

Pleuronhorus bioartitus. ..........................................

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PALEONTOLOGY. 49

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50 MANZANO GROUP OF EIO GRANDE VALLEY.

DESCRIPTION OF SPECIES.

CCELENTERATA.

LOPHOPHYLLUM ? sp.

Of this species our collection has furnished a single specimen 

embedded in matrix and partially weathered through. The corallum 

is small, straight, rather rapidly expanding, 15 mm. long, 8 mm. in 

diameter at the larger end. Tabulae and dissepiments wanting. 

Fossula large and distinct. Septa 19 in number. Their ends unite 

at the center, and with the sides of two of them form an apparently 

continuous wall around the fossula. Nevertheless, on close inspection 

they are, by reason of the union of their inner ends, distinctly divisible 

into three groups. Opposite the fossula three of the septa form a 

wedge-shaped mass, whose extremity projects somewhat farther 

toward the center than the other combinations of septa,, and doubtless form the pseudocolumella, if such a structure was present. 

Eight septa on each side, possibly divisible into two groups of four 

each, occur between the fossula and the wedge-shaped group immediately opposite, their ends uniting so as to be distinct from each 

other and also, to a less degree, from the third group, which lies 

between them.

Horizon and locality. Abo sandstone, Abo Canyon (station 3757a).

ECHINODEBMATA. 

ECHINOCRINUS Agassiz.

I am, with regret, employing the generic name Echinocrinus instead

of the more familiar and more appropriate Archxoddans, but if the 

facts have all come before me no other course seems open.

Echinocrinus was first introduced by Agassiz in 1841. No complete or formal description was given, but after mentioning a few 

characters the genus was stated to include Oidaris urii and one or 

two other forms. In 1844 McCoy 0 gave a very good discussion of 

the genus, under the title proposed by Agassiz, mentioning the fact 

that he had long before distinguished it in manuscript by the name 

Archceocidaris. Meek animadverts to this fact, saying that Echinocrinus has usually been passed over by naturalists because Agassiz 

supposed the form to be a crinoid and the name is inappropriate for 

an echinoid. 6

Though by some considered adequate ground for rejecting a name 

in zoology, the fact that a name is. inappropriate or suggests mistaken

a Syn. Carb. Foss. Ireland, Dublin, 1844, p. 173. 

b Kept. Geol. Survey Illinois, vol. 2,1866, p. 294.
PALEONTOLOGY. 51

biological affinities is not generally regarded as invalidating it, and 

more than one example can be brought forward to illustrate the confusion which would spring up were such a principle adopted.

It seems, therefore, that Archseocidaris has no real standing in 

nomenclature. McCoy himself evidently did not seek to introduce 

it. It is anticipated by Echinocrinus Agassiz, and if Agassiz's somewhat casual definition is thought insufficient to fix the name, Archseocidaris is still anticipated by McCoy's own definition of the genus 

under the title of Echinocrinus.

The genotype of Echinocrinus Agassiz would undoubtedly have to 

be Cidaris urii Fleming, while that of Echinocrinus McCoy would 

probably be the species which McCoy identifies as Echinocrinus mun~ 

sterianus De Koninck(?). The former has characters more like those 

of the American Carboniferous species usually referred to Archseocidaris. (Maris munsteriana is now regarded as belonging to the 

genus Eocidaris. Apparently, therefore, if the genus be given to 

McCoy at all, whether as Archseocidaris or Echinocrinus, by the 

method of generic fixation by type species whichever name is adopted 

passes to the group now called Eocidaris, that term falling into 

synonymy.

It has been a matter of some difficulty to ascertain the facts relating 

to the literature of Echinocrinus and Archseocidaris. McCoy states 

that Agassiz had anticipated him in naming the group in question, 

but gives no reference to Agassiz's work. In his Nomenclator, 

Agassiz cites the genus as described in the second o,f his Echinoid 

monographs (1841). Goeppert and Meyer give the same volume and 

date, and also name the page, which was not given by Agassiz. Goeppert and Meyer give page 15 of the introduction. In the volume 

which I consulted, that from the Library of Congress, the genus was 

discovered with difficulty in a part bound in with Monograph I, 1838. 

This arrangement, however, is erroneous, for the fascicle in question 

is subscribed "Neuchatel en juillet 1841." Although this date is the 

same as that of the second monograph, there is good reason to believe 

that it did not form part of that work, the evidence consisting partly 

of the fact that this fascicle has a separate title-page and independent 

pagination. There is reason to believe, indeed, that this fascicle, 

which is entitled "Observations sur les progres re'cens de 1'histoire 

naturelle des Echinoderms," appeared as a separate brochure between 

the first and second monographs, though intended to form a part of 

the Echinoderm volume. Goeppert and Meyer's reference is, therefore, incorrect, not only as to the volume, but also as to the statement 

that the description of Echinocrinus occurs in the introduction. 

Monograph II has both a preface and an introduction of its own, while 

the fascicle in which this description does occur bears neither the one 

title nor the other.
52 MANZANO GROUP OF BIO GEANDE VALLEY. 

ECHINOCEINUS CEATIS White.

1876. Archseoddaris cratis. White, U. S. Geol. Geog. Surv. Terr., Second Division,

Powell's Kept. Geol. Uinta Mountains, p. 109. 

Lower Aubrey group: Confluence of Grand and Green rivers, Utah. 

1880. Archseoddaris cratis. White, U. S. Geol. Surv. (F. V. Hayden in charge);

Cont. to Paleontology Nos. 2-8, p. 130, pi. 33, fig. 2a. 

Middle Carboniferous: Confluence of Grand and Green rivers, Utah. 

1883. Archseoddaris cratis. White, U. S. Geol. Geog. Surv. Terr., Twelfth Ann. Kept.,

for 1878, pt. 1, p. 130, pi. 33, fig. 2a.

Middle Carboniferous: Confluence of Grand and Green rivers, Utah. 

1895. Archseoddaris cratis. Keyes, Iowa Acad. Sci., Proc., vol. 2, p. 188.

Coal Measures (Lower Aubrey): Utah.

1903. Archseoddaris cratis. Girty, U. S. Geol. Surv., Prof. Paper No. 16, p. 331. 

Weber limestone: Crested Butte district, Colorado. 

Hermosa formation: Ouray, Colo.' 

Leadville district, Colorado. 

'1904. Archseoddaris cratis. Klem, St. Louis Acad. Sci., Trans., vol. 14, p. 47.

This species is represented in our collection by. only three or four 

fragmentary specimens, which have been worn about half way 

through as they lie flat on the rock surface. They are characterized 

by having a few stout spinules disposed at rather long intervals. So 

far as can be determined, they agree with E. cratis, except that they 

are larger, the largest having a diameter of 5 mm. In size and to a 

certain extent in other characters these specimens suggest E. triplex, 

but I have seen no evidence that the radicle was triangular in section, 

a characteristic feature of E. triplex, while the spinules are more prolonged and tapering.

Horizon and locality. San Andreas limestone, Caballos Mountains 

(station 3738a).

BRYOZOA.

SEPTOPOEA aff. ROBUSTA Ulrich.

This species is represented in our collection by two specimens 

exposed on blocks of limestone and for the most part considerably 

weathered. On this account it has been possible to determine their 

characters only in part. The Manzano form is a large, fine species, 

apparently having a flabellate shape, more or less flexuous. The 

larger specimen measures 60 mm. in one direction. The branches 

increase by division and by intercalation, and sometimes this process 

has been so much more active in one part of the zoarium than in 

another that there is wide variation from point to point in the number 

of branches which occur in a given distance. Ten is perhaps the 

average number in 10 mm., but the range is from 8 to 11 or 12. Some 

9 or 10 fenestrules occur in the same distance. The fenestrules vary 

from subcircular to transversely subquadrate, though the latter type 

is not common. Usually the length and breadth are approximately
PALEONTOLOGY. 53

equal and the shape roundish, for the characteristic construction of 

the dissepiments as formed by the union of two oblique' branchlets is 

only here and there obvious. The dissepiments are depressed, expanding at their ends and varying from larger to considerably smaller 

than the branches, many of which remain slender for a relatively long 

distance after their introduction. The obverse side is probably 

striated, and the branches also appear to have been swollen or nodose 

at their junction with the dissepiments.

On the reverse the branches contain two rows of cells apparently 

separated by a fairly well-defined carina. The zocecial apertures 

come about four to the fenestrule or two opposite the fenestrules and 

two more or less opposite the dissepiments. There are about 20 in a 

distance of 5 mm., and they are considerably less than their own 

diameter apart. On the dissepiments the apertures are irregularly

distributed in One to three rows. The number and distribution of the 

accessory pores have not been determined. This form is evidently 

related to 8. robusta, but almost as evidently not identical with it. 

It is somewhat less robust and has the obverse face marked by nodes. 

Horizon and locality. Abo sandstone, Abo Canyon (station 3757a).

BRACHIOPODA.

MEEKELLA MEXICANA n. sp.

Plate VI, figures 1-5.

Shell of medium size, growth usually regular. Ventral valve 

having a subtriangular or spatulate outline, subconical, more or less 

flattened and produced backward. Hinge narrower than the greatest 

width. Area high, moderately well denned at the sides. ' Pseudodel tidium occupying about one-fourth of .its width, sometimes more, 

sometimes less.

Dorsal valve transverse, subquadrate in outline, strongly inflated, 

especially in the umbonal region.

Plications rather fine and faint, sometimes obscure, often beginning 

some distance from the beak. Lirae fine and rigid, apparently thin 

and sharp when not exfoliated, 16 to 19 in 5 mm., generally subequal, 

sometimes distinctly and regularly unequal, and of three or four 

degrees of prominence.

Some of the variable features of this species have already been 

pointed, out. The area varies considerably in altitude and also in 

direction, from being nearly perpendicular to the plane of the aperture 

to almost in line with it. The width of the pseudodeltidium also is 

subject to variation as well as the degree of strength in the plications. 

In some cases the latter are so faint and begin so far from the apex 

that if only specimens were seen which were not quite mature one 

would feel compelled to place them in the genus Orihotlietina. (See
54 MANZANO GBOTJP OF EIO GRANDE VALLEY.

fig. 4, PI. VI.) Such seems in fact to be the case with our material 

from station 3742d, in which the largest specimens examined do not 

exceed 16° mm. in length and show no trace of plications. They agree 

so well in other respects with typical M. mexicana that I have referred 

them without much hesitation to that species.'

There can be little question that the present form is distinct from 

Meekella striaticostata of the Mississippi Valley Pennsylvanian. A 

number of differences at once appear when characteristic specimens 

are compared, and they remain rather constant in all comparisons. 

The area of the ventral valve is generally more strongly inclined backward, frequently more flat and less distorted. The plications are 

much less distinct. It is difficult to make a count of the lirse upon 

M. striaticostata owing to the plications, but they appear to be 

considerably finer and less regular.

Horizon and locality. San Andreas limestone, Engle (station 3740) 

and Elephant Butte (stations 3600 and 3741); Yeso formation, San 

Andreas (station 3742d).

MEEKELLA STRIATICOSTATA Cox.

Plate VI, figure 6.

1857. Plicatula striato-costata. Cox, Owen's Geol. Surv. Kentucky, Rept., vol. 3, p. 

568, pi. 8, fig. 7.

Coal Measures: Providence, -Hopkins County, Ky. 

? 1858. Orihisina Shumardiana. Swallow, Acad. Sci. St: Louis, Trans., vol. 1, p. 183.

Lower Permian: Valley of Cotton wood, Kans.

1858. Orthisina Missouriensis. Swallow, Acad. Sci. St. Louis, Trans., vol. 1, p. 219.

Upper Coal Measures: Dallas, Mo.; Kansas.

? 1859. Orthisina Shumardiana. Meek and Hayden, Acad. Nat. Sci. Philadelphia, 

Proc., p. 26.

Upper Coal Measures: Fort Riley, Kans.

1859. Orthisina Missouriensis. Meek and Hayden, Acad. Nat. Sci. Philadelphia,

Proc., p. 26.

Upper Goal Measures: Leaven worth, Kans. 

? 1859. Streptorhynchus (Orthisina) Shumardianus. Shumard, Acad. Sci. St. Louis,

Trans., vol. 1, p. 395.

Permian sandstone: Guadalupe Mountains. 

? 1863. Orthisina ocddentalis. Swallow, Acad. Sci. St. Louis, Trans., vol. 2, p. 82.

Upper Coal Measures: Caldwell County, Mo. 

1866. Orthis striato-costata. Geinitz, Garb, und Dyas in Nebraska, p. 48, tab. 3, figs.

22-24.

Upper Coal Measures: Crescent City, Iowa. 

1868. Meekella striato-costata. White and St. John, Chicago Acad. Sci., Trans., vol.

1, pp. 120, 122, figs. 4-6. 

Coal Measures: Iowa. 

1872. Meekella striato-costata. Meek, U. S. Geol. Surv. Nebraska, Final Rept., p. 175,

pi. 5, figs. 12a-c.

Upper Coal Measures: Nebraska City, Bellevue, Plattsmouth, Otoe City, and 

Aspinwall, Nebr.; Kentucky; Iowa; Missouri; Illinois.
PALEONTOLOGY. 55

1873. Meekella striato-costata. Meek and Worthen, Geol. Surv. Illinois, Kept., vol. 5,

p. 571, pi. 26, fig. 21. 

Upper and Lower Coal Measures: Caseyville and various localities in Illinois.

1875. Meekella striatocostata. White, U. S. Geog. Surv. W. 100th Mer., Kept., vol. 4,

p. 126, pi. 9, figs. 4a-e. (Volume published as a whole in 1877.) 

Carboniferous: Camp Cottonwood, Lincoln County, Nev.; Tenney's ranch, 

Kaibab Plateau, Arizona; Kanab Canyon; Meadow Creek, south of Fillmore; 

Le Verkins Creek, and at cliff east of Belleview, Utah.

1876. Meekella striatocostata. White, U. S. Geol. Geog. Surv. Terr., Second Division; 

Powell's Kept. Geol. Uinta Mountains, p. 90. Lower Aubrey group: Confluence of Grand and Green rivers, Utah.

1883. Streptorhynchus (Meekella) striatocostata. Hall, New York State Geol. Sec. 

Ann. Kept, for 1882, pi. (10) 40, figs.18-23.

1883. Meekella striatocostata. Kayser, Richthofen's China, vol. 4, p. 178, pi. 23,

fig. 8. 

Upper Carboniferous: Lo-Ping, China.

1884. Meekella striatocostata. White, Geol. Surv. Indiana, Thirteenth Kept., p. 130,

pi. 26, figs. 12-14.

Coal Measures: Western part of Vigo County, Ind. 

1892. Meekella striatocostata. Hall and Clarke, Int. Study of Brach., pt. ], pi. 17,

figs. 10-13.

Upper Coal Measures: Winterset, Iowa; Lawrence County, Kans. 

1892. Meekella striatocostata. Hall and Clarke, Geol. Surv. New York, Pal., vol. 8,

pt. 1, p. 265, pi. 10, figs. 18-23; pi. 11B, figs. 20-22. 

Upper Coal Measures: Winterset, Iowa; Lawrence County, Kans. 

1895. Meekella striatocostata. Keyes, Missouri Geol. Surv., Kept., vol. 5, p. 68, pi.

39, figs. la-c. (Date of imprmt 1894.) 

Upper Coal Measures: Kansas City, Mo. 

1900. Meekella striatocostata. Beede, Univ. Geol. Surv. Kansas, Rept., vol. 6, p. 65,

pi. 12, figs. 9-9c.

Upper and Lower Coal Measures: Fort Scott, Olathe, Kansas City, Eudora, 

Lawrence, Lecompton, Topeka, Beaumont, Grand Summit, Kans. Widely 

distributed but moderately rare throughout the Coal Measures and base of 

the Permian. Abundant near base of Permian.

1903. Meekella striaticostata. Girty, U. S. Geol. Surv., Prof. Paper No.-16, p. 350. 

Hermosa formation: San Juan region, Colorado. 

Carboniferous: Leadville district, Colorado.

A few specimens obtained at different localities from those at 

which M. mexicana was abundant possess characters which at the 

same time tend to discriminate them from that species and ally them 

with M. striaticostata. The beak of the ventral valve is twisted. 

The area is not very high and is nearly perpendicular to the plane of 

junction of the two valves. On the one hand, the surface is plicated 

more strongly than in M. mexicana, but, on the other, it ,is not as 

strongly folded as is often the case with M. striaticostata. The lirae 

are finer than in M. mexicana and tend to bend outward from the 

.bases of the sulci up onto their sides in a manner common to M. 

striaticostata but rare in M. mexicana. In one ventral valve the 

dental plates are very closely arranged, more so than is usually the 

case with M. mexicana.

Horizon and locality. Abo sandstone, Mesa del Yeso (station 3751) 

and Abo Canyon (station 3757a).
56 MANZANO GROUP OF RIO GRANDE VALLEY.

PRODUCTUS IVESI Newberry.

1861. Productus Ivesi. Newberry, Ives's Colorado Expl., Exped., Kept., p. 122, pi.

2, figs. 1-8.

Middle Carboniferous limestone: Banks of Colorado River, near mouth of Diamond River.

This species has sometimes been regarded as identical with P. 

semireticulatus or as a mere variety of it. P. ivesi belongs to the 

semireticulatus group, but is without much question specifically distinct from P. semireticulatus itself, or at least from the form found 

in the Pennsylvanian of the Mississippi Valley which passes under 

that name and which is probably closely allied to the original English variety. P. ivesi is narrower, with less regular sculpture and 

more numerous spines. It more nearly resembles the Pennsylvanian 

species which was designated, I judge, by Swallow as P. calhounianus, but I am quite in accord with Meek in believing the western 

form to be distinct. 0

For the time being at least I shall not include with P. ivesi the 

form from Nevada which Meek identified as P. ivesi?, with the 

reversional name of P. longus.

The fossils under consideration, though somewhat imperfect, 

appear to be typical in every way. \

Horizon and locality. San Andreas limestone, Nogal Creek (station 3744a), Mesa del Yeso (station 375Id), and San Andreas (station 

3742f?); Yeso formation, Mesa del Yeso (stations 3751a, 3751b, and 

3751c?).

PRODUCTUS LEEI n. sp. .

Plate VII, figure 1.

Shell rather small, subquadrate. Width slightly greater than the 

length and greatest at the hinge. Ventral valve strongly convex. 

Ears small, depressed, triangular, arched. Sinus gentle, more or 

less obscure.

Dorsal valve similar to the ventral, except that the visceral area 

is flattened or gently concave.

Surface of ventral valve marked by moderately strong costas, 

which are rather irregular, subangular, and separated by relatively 

wide rounded striae. The visceral area is somewhat regularly, 

strongly, and finely wrinkled. A few small spines are scattered 

over the surface, but along the hinge line they are large and directed 

obliquely away from the beak. The sculpture of the dorsal valve is 

similar to that of the ventral, but the ribs are more rounded and 

the striae more narrow and angular.

a Meek's comment really applies to the Nevada shell and not to typical P. ivesi. (King, Rept. U. S. 

Geol. Expl. 40th Par., vol. 4, 1877, p. 68.)
PALEONTOLOGY. 57

This form is related to other members of the semireticulatus group, 

being distinguished chiefly by the somewhat irregular, angular, 

widely spaced, and possibly evanescent ribs. Of the associated 

species, that identified as P. mexicanus is probably the most closely 

allied. The present form is larger, broader, with not only relatively 

but even absolutely finer costse. As to P. ivesi there can be little 

question of identity. The form which I described from the Hermosa 

formation of Colorado as P. Jiermosanus is probably more closely 

similar than any of the American Producti known to me: P. leei is 

smaller and has a different distribution of the spines. I am not sure 

that the Manzano form should be regarded as more than a variety of 

the other, but with these differences, in conjunction with different 

stratigraphic position and faunal association, it seems hardly wise 

to regard them as the same species.

Horizon and locality. San Andreas formation, Engle (stations 

3740 and 3595), Caballos Mountains (station 3738), Nogal Creek 

(station 3744a?), and San Andreas (station 3742f ?).

PRODUCTUS MEXICANUS Shumard? 

Plate VII, figure 4.

1858. Productus Mexicanus. Shumard, St. Louis Acad. Sci., Trans., vol. 1, p. 291. . White [Permian] limestone: Guadalupe Mountains.

1859. Productus Mexicanus. Shumard, St. Louis Acad. Sci., Trans., vol. 1, p. 389.

White [Permian] limestone: Guadalupe Mountains. 

?1877. Productus Mexicanus? White, II. S. Geog. Surv. W. 100 Mer., Kept., vol. 4,

p. 120, pi. 8, figs. Qa-c. 

Carboniferous: Camp Cottonwood, old Mormon road, Lincoln County, Nevada;

near Salt Lake, New Mexico. 

71883. Productus Mexicanus. Kayser, Richthofen's China, vol. 4, p. 182, pi. 28,

figs. 7a-b.

Upper Carboniferous: Lo-Ping, China. 

?1902. Productus Mexicanus. Tschernyschew, Com. Geol. [St. Petersburg], Mem.,

vol. 16, No. 2, p. 264, pi. 52, fig. 10. 

Schwagerina zone: Ural Mountains.

1908. Productus mexicanus. Girty, U. S. Geol. Surv., Prof. Paper No. 58, pp. 255^256. 

Capitan limestone: Guadalupe Mountains, Texas.

P. mexicanus was not figured by its author, and we must almost 

perforce go back to White's figure of the species, which agrees fairly 

well with Shumard's description. At the same time, as typical 

P. mexicanus was found in the Guadalupe Mountains in a faunal 

relation widely different from that in which White's specimen occurred 

it seems rather probable that the latter is not really identical with 

the Guadalupian form. Nevertheless, about the only difference 

that can be pointed out between White's specimen and Shumard's 

description is that the latter indicates a larger size than is possessed 

by the former.
58 MANZAKO GKOUP OF ElO GRANDE VALLEY.

The form here under consideration appears to be very closely 

related to, if not identical with, White's P. mexicanus. It is, however, a little larger, in this respect agreeing more closely with the 

typical variety, and it is frequently more elongate.

From observations here and elsewhere I have been led to believe 

that P. ivesi may represent one extreme of a varied group of forms 

other extremes of which have been called P. subJiorridus, P. mexicanus, and P. leei. P. mexicanus as here identified and as identified 

by White also may possibly be thought of as a small and narrow 

P. ivesi, in which the sculpture remains but little changed, the ribs, 

therefore, being relatively very large for the size. P. subJiorridus 

can be derived from the same stock through a tendency of the costse 

to become evanescent. Much variation is shown by all three species, and in given cases it is not easy to distinguish them satisfactorily.

This group of forms is abundant in the limestones at Cloudcroft, 

N. Mex., affording better opportunities for study than the collection 

in hand. One form hardly if at all to be distinguished from P. subJiorridus occurs in great numbers. The ribs are obsolete or obsolescent, and spines are more or less abundant. A closely related form, 

connected with it by intermediate types, is the same species which I 

am here identifying as P. mexicanus. It has more distinct and more 

closely arranged costse than P. subJiorridus. A small variety of 

P. mexicanus is indistinguishable from P. mexicanus as identified by 

White. The specimen from Fort Wingate figured by White as 

P. costatus is intermediate between P. subJiorridus and P. mexicanus. 

P. costatus of Marcou and P. occidentalis of Newberry also belong 

to this group.

Horizon and locality. Yeso formation, Mesa del Yeso (station 

375la); San Andreas formation, Nogal Creek (station 3744a) and San 

Andreas (station 3742H).

PRODUCTUS CORA d'Orbigny.

1842. Productus com. D'Orbigny, Voyage dans 1'Ameiique MeYidionale, Pal., p. 55,

pi. 5, figs. 8-10. 

Carboniferous: Above Patapatani, on an island in Lake Titicaca; Yarbichambi.

1845. Productus lyelli. De Verneuil, Lyell's Travels in North America, vol. 2, p. 221. 

Mountain limestone: Windsor, Horton Bluff, Shubenacadie, Gays River, Debert 

River, Minudie, and Cape Breton.

1847. Productus com. De Koninck, Soc. Roy. d. Sci. Lie'ge, Mem., vol. 4, p. 148,

pi. 4, fig. 4a, b; pi. 5, fig. 2a, b, c, d.

Lower Carboniferous limestone of Vise", of Chokier, and of Ratingen; in the 

shales of the median 6tage near Tournay, and in the Upper Carboniferous 

slates.of Epinoy near Binche (Hainaut); banks of the Missouri; Kendal, 

Westmoreland; Lowick; Yorkshire; Derbyshire; Ireland; banks of the Wilji, 

an affluent.of the Tarousa; on the banks of the Louja in the district of Medynsk, 

province of Kalouga; beyond Cosatchi-Datchi on the eastern side of the 

Urals; near Sterlitamack, between Perm and Serebriansk; on the west side of
PALEONTOLOGY. 59

the same chain from Kachira on the Oka, and from Unja near Kosimof; Flint 

Ridge, Zanesville, Guernsey County (Ohio); between New Harmony and 

Mount Vernon (Indiana); Windsor (Nova Scotia); Leavenworth (Ind.); on 

the Bolivian plateau, above Patapatani; in one of the islands of Lake Titicaca, 

and at Yarbichambi, South America.

1847. Producta com. De Koninck, Recherches sur les Animaux Fossiles, pt. 1, p. 50,

pi. 4, figs. 4a, 6; pi. 5, figs. 2a-d.

Carboniferous: Guernsey County, Flint Ridge, and Zanesville, Ohio; between 

New Harmony and Mount Vernon, Ind.; Leavenworth, Ind.; Windsor, Nova 

Scotia; Bolivia, etc., South America.

1848. Productus Martini. Christy, Letters on Geology, pi. 5, figs. 6, 8, 9.

[Carboniferous]: Pinckneyville,*Ill. 

1848. Productus sp. Christy, Letters on Geology, pi. 5, fig. 1.

[Carboniferous] sandstone above the Black shale: Elk River, Tennessee. 

1852. Productus semireticulatus. Hall, Stansbury's Exped. Great Salt Lake, Rept., 

p. 411, pi. 3, figs. 3, 5o, b.

Carboniferous: Near Fort Laramie; and Flat Rock Point and other places in the

neighborhood of Great Salt Lake. 

1852. Productus cora. Owen, Geol. Surv. Wisconsin, Iowa, and Minnesota, Rept.,

pp. 103,136, pi. 5, fig. 1.

Carboniferous: Missouri River, below mouth of Little Platte River. 

1852. Productus cora. Roemer, Kreid. von Texas, p. 90.

Carboniferous: San Saba Valley, Texas. 

1854. Productus cora. Marcy's Expl. Red River of Louisiana, Rept., p. 176.

Carboniferous: Washington and Crawford counties, Ark. 

1854. Productus cora. Norwood and Pratten, Acad. Nat. Sci. Philadelphia, Jour. (2),

vol. 3, p. 6. (Entire volume appeared in 1855.)

Mountain limestone: Chester, Rosiclare, and Warsaw, 111.; near Richmond, 

. Mo.; Carrsville, Ky.

1854. Productus Prattenianus. Norwood, Acad. Nat. Sci. Philadelphia, Jour. (2),

vol. 3, p. 17, pi. 1, figs. lOa-d. (Entire volume appeared in 1855.) 

Coal Measures: Crossing of Big Nemahaw River, about 85 miles northwest of 

St. Joseph, Mo.

1855. Productus Cora. Salter, Belcher's " Last of the Arctic Voyages," p. 387, pi. 36, 

fig. 12.

Carboniferous: Top of Exmouth Island. 

1855. Productus Lyelli. Dawson, Acadian Geology, p. 219, fig. g.

Lower Carboniferous limestone: Nova Scotia.

1858. Productus cora. Marcou, Geol. North America, p. 45, pi. 6, figs. 4, 4a.

Mountain limestone: Tigeras Canyon of San Antonio; Pecos village; summit of 

Sierra de Sandia, New Mexico.

1859. Productus Prattenianus. Meek and Hayden, Acad. Nat. Sci. Philadelphia,

Proc., p. 26.

Coal Measures: Indian Creek and Leavenworth, Kans. 

1863. -Productus Cora. Davidson, Geol. Soc. London, Quart. Jour., vol. 19, p. 174,

pi. 9, figs. 22, 23..

Lower Carboniferous limestone: Windsor, Horton Bluff, Shubenacadie, Gays 

River, Cape Breton, Pugwash, eastward of Cumberland, Lennox Passage, 

McKenzie's Mill, at eastern extremity of Wallace Harbor, etc., Nova Scotia. 

1866. Productus Flemingi. Geinitz, Garb, und Dyas in Nebraska, p. 52, tab. 4,

figs. 1-4. (Not P.flemingi De Koninck.)

Upper Coal Measures: Bellevue, Plattsmouth, and Nebraska City, Nebr. 

1866. Productus Koninclrianus ? Geinitz, Garb, und Dyas in Nebraska, p. 53, tab. 4,

fig. 5. (Not P. Konincldanus De Verneuil.) 

Upper Coal Measures: Nebraska City, Bennetts Mill, Nebr.
60 MANZANO GROUP OF RIO GRANDE VALLEY.

1866. Productus Calhounianus. Geinitz, Garb, und Dyas in Nebraska, p. 53. (Not

P. Calhounianus Swallow.)

Upper Coal Measures: Diamond Spring, Santa Fe, in Kansas. 

1866. Productus com. Geinitz, Garb, und Dyas in Nebraska, p. 50.

Carboniferous limestone and shales: Germany, Belgium, England, Ireland, 

Spain, Russia, North America, Bolivia, etc. .Belleview, Plattsmouth, Nebr.

1868. Productus com. Dawson, Acadian Geology, p. 297, figs. 98a, b.

Carboniferous limestone: Windsor, Horton Bluff, Shubenacadie, Gays River, 

Minudie, Cape Breton, Pugwash, east coast of Cumberland, Lennox Passage, 

McKenzie's Mill, Wallace Harbor, etc., Nova Scotia.

1869. Productus cf. cor a. Toula, Kais. Akad..der Wissensch, Wien, Sitzb., vol. 59,

1. Abth., p. 441.

Carboniferous limestone: 10 miles from Cochabamba, Bolivia. 

1872. Productus Prattenianus. Meek, U. S. Geol. Surv. Nebraska, Final Rept.,

p. 163, pi. 2, figs. 5a-c; pi. 5, fig. 13; pi. 8, figs. 10a-6. 

Upper Coal Measures: Nebraska City, Bennetts Mill, Cedar Bluff, Plattsmouth,

Bellevue, and Omaha, Nebr.; Kansas, Iowa, Illinois. 

Lower Coal Measures: Illinois.

1874. Productus Cora (?). Derby, Cornell Univ. (Science) Bull., vol. 1, No. 2, p. 49,

pi. 2, fig. 17; pi. 6, fig. 17. 

Coal Measures: Itaituba and Barreirinha, Brazil.

1875. Productus prattenianus (pars). White, U. S. Geog. Surv. W. 100th Mer., Rept.,

vol. 4, p. 113, pi. 7, figs. la-c. (Entire volume published in 1877.) 

Carboniferous: Near Santa Fe and Sandia Mountains, New Mexico; Piloncillo 

Range near Gavilan Peak, and at the confluence of White Mountain and Black 

rivers, Arizona; Egan Range, 35 miles south of Egan Pass; Fossil Hill, White 

Pine County; Robert's Creek Range, Lander County, and top of Grass Mountain, Ely Range, 35 miles north of Pioche, Nev.; near Beckwith Spring, 

Cedar Range; near top of Mount Nebo, and west face of Oquirrh Range, Utah.

1876. Productus prattenianus. White, U. S. Geol. Geog. Surv. Terr., Second Division;

Powell's Rept. Geol. Uinta Mountains, p. 90. 

Lower Aubrey group: Confluence of Grand and Green rivers, Utah.

1876. Productus Cora. Derby, Mus. Comp. Zool., Bull., vol. 3, p. 281. 

Coal Measures: Yampopata:

1877. Productus Prattenianus. Meek, U. S. Geol. Expl. 40th Par., Rept., vol. 4,

p. 72, pi. 7, fig. 7.

Carboniferous: Fossil Hill, White Pine district; Railroad Canyon, Diamond 

Mountains, Nevada.

1878. Productus com. Dawson, Acadian Geology, 3d edition, p. 297, fig. 98.

Carboniferous limestone: Windsor, Horton Bluff, Shubenacadie, Gays River,

Minudie, and Cape Breton, Nova Scotia; Pugwash, on the eastern coast of

Cumberland; Lennox Passage;. M'Kenzie's Mill, at eastern extremity of

Wallace Harbor, etc.

1884. Productus Cora. White, Geol. Surv. Indiana, Thirteenth Rept., p. 126, pi. 26,

figs. 1-3. 

Coal Measures: Fountain, Vermilion, -Parke, Montgomery, Clay, Owen, Pike,

Dubois, and Warrick counties, Ind. 

1884. Productus com. Waagen, Palseontologia Indica, ser. 13, vol. 1, p. 677, pi. 66,

fig. 3; pi. 67, figs. 1, 2.

Productus limestone: Katta, Omarkheyl, Shekh Budin, and Jabi, India. 

1886. Productus Cora. Heilprin, Second Geol. Surv. Pennsylvania, Ann. Rept. for

1885, p. 452; p. 440, figs. 1, la. 

Upper Coal Measures, Mill Creek limestone: Wilkesbarre, Pa.
PALEONTOLOGY. 61

1886. Productus Cora. Heilprin, Proc. and Coll. Wyoming Hist, and Ge'ol. Soc.,

vol. 2, p. 268, figs. 1, la. 

Upper Coal Measures, Mill Creek limestone: Wilkesbarre, Pa.

1887. Productus Cora. Herrick, Sci. Lab. Denison Univ., Bull., vol. 2, p. 47, pi. 2,

fig. 26. 

Coal Measures: Flint Ridge, Ohio.

1888. Productus cora. Keyes, Acad. Nat. Sci. Philadelphia, Proc., p. 227. 

Lower Coal Measures: Des Moines, Iowa.

1895. Productus cora. Keyes, Missouri Geol. Surv., Kept., vol. 5, p. 47, pi. 37,

figs. 2a-c. (Date of imprint 1894.) 

Coal Measures: Calhoun and Kansas City, Mo.

1896. Productus cora. Smith, Am. Phil. Soc., Proc., vol. 35, p. 238.

Upper Coal Measures: Poteau Mountain, Indian Territory.

? Archimedes limestone: Independence County, Ark.

? Marshall shale: Independence and Stone counties, Ark.

? Fayetteville shale: Independence County, Ark.

1896. Productus cora. Smith, Leland Stanford Junior University Pub., Cont. Biol. 

Hopkins Seaside Lab., No. 9, p. 28.

Upper Coal Measures: Poteau Mountain, Indian Territory.

? Archimedes limestone: Independence County, Ark.

? Marshall shale: Independence and Ston.e counties, Ark.

? Fayetteville shale: Independence County, Ark.

1900. Productus cora. Beede, Univ. Geol. Surv. Kansas, Kept., vol. 6, p. 75, pi. 11, 

figs. 1-lf.

Upper Coal Measures: Kansas City, Eudora, Lawrence, Lecomptou, Topeka,

Geary County, MelVern, Osage County, Kans. 

1900. Productus cora. Herrick and Bendrat, Am. Geol., vol. 25, No. 4, p. 240.

Coal Measures: Sandia Mountains, N. Mex. 

1903. Productus cora. Girty, U. S. Geol. Surv., Prof: Paper No. 16, p. 364, pi. 4.

Hermosa formation: San Juan region and Ouray, Colo.

Rico formation: San Juan region, Colo.

Weber and Maroon formations: Crested Butte and Leadville districts, Colo.

Only a few examples of this form have come to hand, all rather 

imperfect and badly worn. In general aspect they are like specimens 

of P. cora from the Mississippi Valley Pennsylvanian. One difference 

can be noted, namely, that while spines are not entirely absent they 

are decidedly less numerous on the forms from the Manzano group. 

Nor can this difference with much probability be ascribed to imperfect 

preservation. As to the presence of spines along the hinge, the 

Manzano specimens leave one in doubt.

Tschernyschew's figure of the type specimen of P. cora a makes 

it fairly clear that the Pennsylvanian species which has so often been 

called P. prattenianus in our literature is really the same as the South 

American form.

Horizon and locality. Abo sandstone, Mesa del Yeso (station 

3751), Abo Canyon (station 3757a), and Sandia Mountains (station 

3798).

a Tschernyscliew, Th., M6ni. Comit6 g<5ol. [Russia], vol. 16, No. 2, 1902, p. 622.
62 MANZANO GROUP. OF RIO GRANDE VALLEY.

PRODUCTUS NEBRASKENSIS Owen.

Plate VII, figures 5 and 6.

1852. Productus nebrascensis. Owen, Geol. Surv. Wisconsin, Iowa, and Minnesota,

Kept., p. 584, pi. 5, fig. 3.

Carboniferous limestone: Bellevue, Missouri River, Nebr. 

.1854. Productus Rogersi. Norwood and Pratten, Acad. Nat. Sci. Philadelphia, Jour.

(2), vol. 3, p. 9, pi. 1, figs. 3a-c. (Whole volume appeared in 1855.) 

Coal Measures: Near Huntsville, Mo. 

1854. Productus Nebrascensis. Norwood and Pratten, Acad. Nat. Sci. Philadelphia,

Jour. (2), vol. 3, p.' 21. (Whole volume appeared in 1855.) 

Coal Measures: Crossing of Big Nemaha, Nebraska Territory.

1856. Productus rogersi. Hall, Pacific Railroad Rept., vol. 3, p. 104, pi. 2, figs. 14,15. 

Carboniferous limestone: Pecos Village, N. Mex.

1859. Productus Rogersi. Meek and Hayden, Acad. Nat. Sci. Philadelphia, Proc.,

p. 26. 

Upper Coal Measures: Kansas River Valley, below mouth of Blue River, Kansas.

1860. Productus asperus. McChesney, Desc. New Spec. Pal. Foss., p. 34. 

' Coal Measures: Lasalle and Springfield, 111.

1861. Productus Rogersi. Newberry, Ives's Colorado River Expl. Exped., Rept.,

p. 121. 

Coal Measures: Pecos Village and Kansas.

1865. Productus asper. McChesney, Illustrations New Spec. Foss., pi. 1, figs. 7a-b.

1866. Strophalosia horrescens. Geinitz, Carb. und Dyas in Nebraska, p. 49. (Not

S. horrescens of Murchison, Verneuil, and Kayserling.) 

Coal Measures: Bellevue, Plattsmouth, Nebraska City, and Bennett's Mill,

Nebr. 

1868. Productus nebrascensis. McChesney, Chicago Acad. Sci., Trans., vol. 1, p. 24,

pi. 1, figs. 7a-b. 

Coal Measures: Lasalle and Springfield, 111.

1872. Productus Nebrascensis. Meek, U. S. Geol. Surv. Nebraska, Final Rept., p. 165, 

. pi. 2, fig. 2; pi. 4, fig. 6; pi. 5, figs, lla-c.

Upper Coal Measures: Nebraska City, Wyoming, Bennett's Mill, Rock Bluff, 

Plattsmouth, Bellevue, and Omaha, Nebr.

Coal Measures: Illinois, Missouri, Iowa, Kansas, New Mexico.

1873. Productus Nebrascensis. Meek and Worthen, Geol. Surv. Illinois, Rept., vol. 5,

p. 569, pi. 25, fig. 8. 

Coal Measures: Sangamon and Lasalle counties, 111.

1875. Productus Nebrascensis. White, U. S. Geog. Surv. W. 100th Mer., Rept., vol. 4,

p. 116, pi. 8, figs. 3a-d. (Whole volume published in 1877.) 

Carboniferous: Camp Apache and Carrizo Creek, Maricopa County, Ariz.; 

Rubyville, Schell Creek Range, and top of Grass Mountain, Ely Range, 

Nevada; Meadow Creek, south of Fillmore, Utah.

1876. Productus Nebrascensis. White, U. S. Geol. Geog. Surv. Terr.,"Second Division;

Powell's Rept. Geol. Uinta Mountains, p. 90. 

Lower Aubrey group: Confluence of Grand and Green rivers.

1877. Productus Nebrascensis. Meek, U. S. Geol. Expl! 40th Par., Rept., vol. 4, p. 65.

1883. Productus asperus. Hall, New York State Geol., Rept. for 1882, pi. (19) 50,

figs. 5-7. 

Coal Measures: Lasalle, 111.

1884. Productus Nebrascensis. White, Geol. Surv. Indiana, Thirteenth Rept., p. 122,

pi. 24, figs. 7-9. 

Coal Measures:- Fountain, Vermilion, Parke, and Vigo counties, Ind.
PALEONTOLOGY. 63

1886. Productus Nebrascensis? Heilprin, Second Geol. Surv. Pennsylvania, Ann.

Kept, for 1885, p. 453, fig. 4c; p. 440, figs. 4-4b. 

Upper Coal Measures, Mill Creek limestone: Wilkesbarre, Pa.

1886. Productus Nebrascensis? Heilprin, Wyoming Hist, and Geol. Soc., Proc. and

Coll., vol. 2, pt. 2, p. 268, figs. 4, 4b. 

Upper Coal Measures, Mill Creek limestone: Wilkesbarre, Pa.

1887. Productus Nebrascensis. Herrick, Sci. Lab. Denison Univ., Bull., vol. 2, p. 49,

pi. 2, fig. 30.

Coal Measures: Flint Ridge, Ohio. 

1892. Productus Nebrascensis. Hall and Clarke, State Geol. [New York], Eleventh

Ann. Kept., for 1891, pi. 22, fig. 7. . 

Coal Measures: La Salle, 111. 

1892. Productus Nebrascensis. Hall and Clarke, Geol. Surv. New York, Pal., vol. 8,

pt. 1, pi. 19, figs. 5-7. 

Coal Measures: La Salle, 111.

1895. Productus Nebrascensis. Keyes, Missouri Geol. Surv., Kept., vol. 5, p. 48; 

pi. 37,.figs. 3a-c. (Date of imprint, 1894.)

Upper Coal Measures: Kansas City, Mo. 

1900. Productus Nebrascensis. Beede, Univ. Geol. Surv. Kansas, Kept., vol. 6, p. 84,

 pi. 9, figs. 7-7/.

Upper Coal Measures: Kansas City, Turner, Eudora, Lawrence, Lecomptou,

Topeka, Manhattan, and Grand Summit, Kans. 

1900. Productus Nebrascensis. Herrick and Bendrat, Am. Geol., vol. 25, no. 4, p. 241.

Coal Measures: Sandia Mountains, N. Mex.

1903. Productus Nebrascensis. Girty, U. S. Geol. Surv., Prof. Paper No. 16, p. 370,

pi. 5, figs. 1, 2, 2a. . , 

Hermosa formation: San Juan region and Ouray, Colo. 

Rico formation: San Juan region, Colo. 

Weber formation: Leadville district, Colo.

1904. Productus Nebraskensis. Girty, U. S. Geol. Surv., Prof. Paper No. 21, p. 53,

pi. 11, figs. 7-9. 

Pennsylvanian (Naco formation): Bisbee quadrangle, Ariz.

The fossils from the Manzano group included under this title are 

so exfoliated that the detailed sculpture can not be made out. In 

general configuration they resemble P. nebraskensis, and in other 

ways also appear to be rather closely related to that species. The 

outline of the ventral valve is subcircular, the ears very small and 

depressed. The cardinal line is shorter than the width in front; the 

body of the shell is rather strongly convex, narrow, elongate. The 

sinus is obscure. The surface is marked by elongated spine bases, 

which end more or less abruptly below with the development of the 

spine which gives rise to them. They tend to produce irregular, 

interrupted costse. Obscure concentric striae are present also, some 

fine and some coarse.

The dorsal valve resembles the ventral in outline. It is gently 

concave, nearly plane over the visceral region, more strongly curved 

upward about the margins. The ears are small, flattened, on a 

level with the edges. The surface is marked by concentric wrinkles, 

especially distinct near the hinge, and by radially elongated pits.
64 MANZANO GROUP OF EIO GRANDE VALLEY.

This form lacks the strong, regular, concentric corrugations which 

cross the surface of typical P. nebraslcensis. I have seen no evidence 

of the second set of large spines, which in the latter project at right 

angles to the surface, though it seems to be true that in exfoliated 

specimens, even of typical nebraslcensis, these spines are not easily 

seen.

At one time I thought to discriminate this form from P. nebraslcensis as a distinct variety, but have withdrawn the name which was 

bestowed upon it. It is not certain that the characters in which the 

Manzano form seemed to differ are constant and real, though adequate if they prove to be so.

Horizon and locality. Abo sandstone, Abo Canyon (station 3757a), 

Mesa del Yeso (station 3751), and Sandia Mountains (station 3798); 

Yeso formation, Mesa del Yeso (station 3751a).

MARGINIFERA ? MANZANICA n. sp.

Plate VII, figure 3.

Shell small, outline subquadrate, slightly transverse.

Ventral valve strongly convex, with a shallow, indistinct sinus, 

which marks the anterior half of the shell or a little more. Hinge 

line slightly longer than the greatest width in front. Ears small, 

.depressed.

Surface marked by relatively coarse, somewhat irregular costse, 

about 18 in number. A few not very distinct wrinkles cross the posterior portion, while a small number of relatively large spines spring 

from the costse.

The dorsal valve is not known. A less typical specimen has this 

valve, gently concave over the visceral portion, strongly curved 

around the margin. The visceral area is marked by a number of

rather fine, regular, indistinct, concentric wrinkles, beyond which, 

toward the margin, are coarse, not very strong, radial ribs.

This little form is probably a Marginifera, but the data at hand 

do not show clearly whether it is a member of that group or of 

Productus.

It is, with little question, distinct from our common Pennsylvanian Marginiferas. It is smaller than M. wabasliensis, with coarser 

ribs and less pronounced sinus.' It is smaller than M. splendens, 

with a different shape and fainter sinus. M. Jiaydeniana is a similar 

form, though its shape is different and its ribs are finer. M. ingrata 

is perhaps more similar than any other species mentioned. It is, 

however, broader and has finer costse. The type which White identified as Productus mexicanus is also like the form under consideration, though broader and with distinctly coarser ribs. Nevertheless, 

Marginifera? manzanica is possibly only a member of that series of
PALEONTOLOGY. 65

closely related species of Productus which includes also P. ivesi, P. 

mexicanus, and P. subliorridus.

Horizon and locality. San Andreas formation, Fra Cristobal (station 3743) and San Andreas (station 3742f?).

MARGINIFERA? CBISTOBALENSIS n. sp. 

Plate VII, figure 2.

In general appearance this form much resembles that described as 

Marginiferaf manzanica, from which it is distinguished by being 

without radial costse. The ventral valve is very small, highly convex, somewhat flattened along the mesial line, but without a distinct 

sinus. The width is only slightly in excess of the length, the hinge 

line being probably a little longer than the width at any anterior

point. The ears are small, subquadratfy depressed. The surface is

crossed by fine, indistinct wrinkles over the visceral region. The 

costse seem to be altogether undeveloped. A number of rather small 

spines are distributed over the surface, springing directly from it 

without being mounted upon distinct bases.

This form differs from any of the American Marginiferas in its 

noncostate condition, and resembles, among the different species 

known to me, especially Productus latidorsatus and P. subliorridus var. 

rugatulus of the Guadalupian fauna, the latter more than the former. 

It is narrower and more globose than P. subhorridus var. rugatulus, 

with fainter sinus and less distinct wrinkles, besides being much 

smaller. I suspect that this also will prove to belong to that group 

of species of Productus of which P. subliorridus is a member.

Horizon and locality. San Andreas formation, Fra Cristobal 

(station 3743) and San Andreas (station1 3742f?).

PUGNAX OSAGENSIS var. pus.iLLA n. var. 

Plate VIII, figures 2 and 3.

We have this species from but one locality in the Manzano group, 

where, however, it appears to have been rather common. The eight 

specimens collected are uniformly of small size, nearly circular outline, and high convexity. The fold has three plications (in one 

instance four) and the sides three, one of them indistinct.

This form is closely related to the common P. osagensis (usually 

P. utah) of the Pennsylvanian fauna, and while differing in certain 

minor particulars from the common and typical form of P. osagensis 

it probably is indiscriminate from certain varieties which pass under 

that specific name. Because the specimens, from the Manzano group 

so uniformly present this more or less individual expression and are 

associated with a fauna considerably different from the typical

84259 Bull. 389 09 5
66 MANZANO GROUP OF EIO GRANDE VALLEY.

Pennsylvania!!, it seemed to me desirable to recognize them as a 

variety, though, only provisionally, since further collections may 

show variations merging them with the typical form.

Horizon and locality. Yeso formation, Mesa del Yeso (station 

3751b).

SQUAMULARIA PERPLEX A McChesney.

1855. Spirifer Uneatus. Shumard, Missouri Geol. Surv., Kept., p. 216. (Not Sp.

lineatus Martin.) 

Coal Measures: [Missouri].

1856. Spirifer lineatus. Hall, Pacific Railroad Kept., vol. 3, p. 101, pi. 2, figs. 6-8.

(Not Sp. lineatus Martin 1809.) 

Carboniferous: Pecos Village, N. Mex.

1858. Spirifer lineatus. Marcou, Geol. North America, p. 50, pi. 7, figs. 5-5c. (Not

Sp. lineatus Martin.) 

Mountain limestone: Pecos Village and Tigeras, N. Mex.

1859. Spirifer lineatus. Meek and Hayden, Acad. Nat. Sci. Philadelphia, Proc., p. 28. 

 Upper Coal Measures: Leaven worth, Kans.

1860. Spirifer perplexa. McChesney, Desc. New Spec. Pal. Foss., p. 43.

Upper Coal Measures: Almost every part of the country where rocks of that age 

occur.

1861. Spirifer lineatus. Newberry, Ives's Colorado River Expl. Exped., Kept., p.

127. (Not Sp. lineatus Martin.) 

Upper Carboniferous: Cherty limestone west of Little Colorado River; vicinity

of Santa Fe, N. Mex. 

? 1864. Spirifer lineatus. Meek, Pal. California, vol. 1, p. 13, pi. 2, figs. 6-6d

Carboniferous: Bass's Ranch, Shasta County, Cal. . 

1866. Spirifer lineatus. Swallow, Acad. Sci. St. Louis, Trans., vol. 2, p. 408. (Not

Sp. lineatus Martin.) 

Coal Measures: Mississippi Valley. 

1866. Spirifer lineatus var. perplexa. Swallow, Acad. Sci. St. Louis, Trans., vol. 2,

p. 408. 

Coal Measures: Mississippi Valley.

1866. Spirifer lineatus var. striato-limatus. Swallow, Acad. Sci. St. Louis, Trans.,

vol. 2, p. 408.

Upper and Middle Coal Measures: Missouri. 

1872. Spirifer lineatus? Meek, U. S. Geol. Surv. Nebraska, Final Rept., pi. 2, figs.

3a, 6.

Upper Coal Measures: Platte River, Nebraska. 

1874. Spirifera (Martinia) perplexa. Derby, Cornell Univ. (Science) Bull., vol. 1,

No. 2, p. 16, pi. 3, figs. 27, 39, 40, 45, 50; pi. 8, fig. 13. 

Coal Measures: Bomjardim and Itaituba, Brazil, and River Pichis, Peru.

1881. Spirifera (Martinia) lineata? White, U. S. Geog. Surv. W. 100th Mer., Rept.,

vol. 3, Appendix, p-. xii. 

Coal Measures: Upper Mississippi River region.

1882. Spirifer (Martinia) lineatus. White, Geol. Surv. Indiana, Eleventh Rept.,

p. 372, pi. 42, figs. 4-6. 

Coal Measures: Eugene, Irid. 

1884. Spirifer (Martinia) lineatus. White, Geol. Surv. Indiana, Thirteenth Rept.,

p. 133, pi. 27, figs. 4-6.

Coal Measures: Fountain, Park, Vermilion, Vigo, Sullivan, Gibson, Pike, 

Knox, Posey, Vanderburg, and Warrick counties, Ind.
PALEONTOLOGY. 67

1886. Spirifer lineatus? Heilprin, Second Geol. Surv. Pennsylvania, Ann. Kept, for

1885, p. 453. 

Upper Coal Measures, Mill Creek limestone: Wilkesbarre, Pa.

1886. Spirifer lineatus? Heilprin, Proc. and Coll. Wyoming Hist, and Geol. Soc., 

. vol. 2, pt. 2, p. 269. 

Upper Coal Measures, Mill Creek limestone: Wilkesbarre, Pa.

1887. Spirifera (Martinia) lineata? Herrick, Sci. Lab. Denison Univ., Bull., vol. 2,

p. 46, pi. 1, figs. 13a-c. 

Coal Measures: Flint Ridge, Ohio.

1888. Spirifera lineata. Keyes, Acad. Nat. Sci. Philadelphia, Proc., p. 230.

Lower Coal Measures: DesMoines, Iowa.

1891. Spirifer (Martinia) lineata. Whitfield, New York Acad. Sci., Ann., vol. 5, 

p. 603, pi. 16, figs. 3-5.

Coal Measures: Hocking County, Ohio.

1893. Spirifer lineatus. Hall and Clarke, Geol. Surv. New York, Pal., vol. 8, pt. 2, 

pp. 10, 11, 17, 21, 30, 39, pi. 38, figs. 2, 4, 7, 8. (Not Sp. lineatus Martin.,) 

(Advance distribution in fascicles.) 

Coal Measures: Iowa.

1894. Spirifera perplexa. Keyes, Missouri Geol. Surv., Kept., vol. 5, p. 84. (Date of

imprint, 1894.) 

Upper Coal Measures: Kansas City, Mo.

1895. Spirifera (Martinia) lineata. Whitfield, Geol. Surv. Ohio, Rept., vol. 7, p. 488,

pi. 12, figs. 3-5.

Coal Measures: Hocking County, Ohio. 

1895. Spirifer lineatus. Hall and Clarke, Geol. Surv. New York, Pal., vol. 8, pt. 2,

pp. 10,11,17, 21, 30, 39, pi. 38, figs. 2, 4, 7, 8. (Not Sp. lineatus Martin.) 

Coal Measures: Iowa.

1899. Reticularia perplexa. Girty, U. S. Geol. Surv., Nineteenth Ann. Kept., pt. 3,

p. 577, pi. 72, fig. la. 

Upper Coal Measures: McAlester quadrangle.

1900. Reticularia perplexa. Beede, Univ. Geol. Surv. Kansas, Rept., p. 102, pi. 12,

figs. 4-4c. 

Upper and Lower Coal Measures to base of Permian: Fort Scott, lola, Lawrence,

Topeka, Kans. 

1900. Martinia lineata. Herrick and Bendrat, Am. Geol., vol. 25, No. 4, p. 240.

Coal Measures and Lower Carboniferous: New Mexico. 

1903. Squamularia perplexa. Girty, U. S. Geol. Surv., Prof. Paper No. 16, p. 392,

pi. 6, figs. 8, 8a, 9-96, 10, 10a.

Hermosa formation: San Juan region and Ouray, Colo. 

Weber formation: Crested Butte and Leadville districts, Colo. 

Maroon formation: Crested Butte district, Colo. 

Robinson limestone: Leadville district^ Colo.

Of this species our collection from the Manzano group contains 

but two examples, one a small silicified ventral valve, the other an 

external mold in limestone, also of a ventral valve, which must when 

complete have been fully 25 mm. long. The former shows the surface characters very obscurely. The latter is characterized by fine, 

regular but obscure, transverse plications, which mark the position 

of closely arranged rows of very small spines. I am hardly prepared 

to state definitely that the Manzano form belongs to the Pennsylvanian species, though it would be difficult to discriminate them
68 MANZANO GROUP OF EIO GEANDE VALLEY.

under existing conditions. The larger specimen suggests by its size 

the Guaclalupian form Squamularia guadalupensis, and from this 

species also a separation will at present be difficult.

Horizon and locality. Yeso formation, Mesa del Yeso (station 

3751c); San Andreas formation, San Andreas (station 3742fj.

COMPOSITA MEXICANA Hall.

Plate VIII, figure 1.

1857. Terebratulamexicana. Hall, Emory's Rept. TJ. S. and Mexican Boundary Surv., 

vol. 1, pi. 20, fig. 2.

[Carboniferous: Texas?] 

1908. Composite, mexicana. Girty, U. S. Geol. Surv., Prof. Paper No. 58, pp. 389-390.

Delaware Mountain formation: Comanche canyon, Glass Mts., Texas.

The genus Composita is more or less abundant in several of our 

collections from the Manzano group, and the dominant form, there 

can be no question, is the same to which Hall gave the name Terebratula mexicana. It is characterized by its small size, rather transverse shape, and strongly developed fold and sinus. The bending 

downward of the sides near the fold tends to give the outline a 

pentagonal shape. These characters are, however, by no means constant. Occasionally the shape is narrow, instead of transverse, or 

the size somewhat larger than in the small typical variety. More 

often the fold and sinus are not as well developed as in the latter, 

sometimes scarcely developed at all.

I do not know whether precisely this variety occurs in the Mississippi Valley, but if so there is little doubt that it would in that 

region be called Composita subtilita (or argentea}. It probably is 

not common there, at all events, and, on the other hand, some of 

the distinguishable Pennsylvania!! varieties of Composita subtilita 

are not known from the Manzano. While availing myself of the 

specific designation introduced by Hall, I may state that there 

appears to be no well-marked boundary between 0. mexicana and 

G. subtilita.

Horizon and locality. Yeso formation, Mesa del Yeso (station 

3751b); San Andreas formation, San Andreas (station 3742f).

COMPOSITA SUBTILITA Plall?

1842. Terebratula Roissyi. D'Orbigny (non L'Eveille'), Voyage dans 1'Amerique

M^ridionale, Pal., p. 46. 

Carboniferous: Yarbichambi. 

1852. Terebratula plano-sulcata. Owen, Geol. Surv. Wisconsin, Iowa, and Minnesota,

Rept., pi. 5, fig. 9.

Carboniferous limestone: Near Council Bluffs. 

1852. Terebratula subtilita. Hall, Stansbury's Exped. Great Salt Lake, Rept., p.

409, pi. 2, figs, la, b, 2a, b. 

Carboniferous: Missouri River, near Weston.
PALEONTOLOGY. 69

?1853. Terebratula subtiliia. Shumard, Marcy's Expl. Red River of Louisiana, Rept., 

Thirty-second Congress, second session, Senate Doc. No. 54 (reprinted several 

times with different pagination), p. 202, pi. 4, fig. 8. 

Carboniferous: Washington County, Ark.

1855. Terebratula subtilita. Schiel, Pacific Railroad Rept., vol. 2, p. 108, pi. 1, figs.

2a, b. 

Carboniferous limestone: 8 miles west of Westport.

1856. Terebratula subtilita. Hall, Pacific Railroad Rept., vol. 3, p. 101, pi. 2, figs. 3-5. 

Carboniferous: Pecos Village, N. Mex.

1857. Terebratula (?) subtilita. Davidson, Mon. British Carb. Brach., Pal. Soc., p.

18, pi. 1, figs. 21, 22. 

Carboniferous: Mayen Wais, England.

1858. Terebratula plano-sulcata. Marcou, Geol. North America, p. 52, pi. 6, figs. 8, 86.

Mountain limestone: Tigeras, N. Mex.; Ohio; Indiana; Illinois; Kentucky;

Arkansas. 

1858; Terebratula roysii. Marcou, Geol. North America, p. 51, pi. 6, figs. 10, 106.

Mountain limestone: Salt Lake City, Utah; El Paso, Chihuahua; headwaters

of the Rio Colorado Chiquito.

185S. Terebratula subtilita. Marcou, Geol. North America, p. 52, pi. 6, figs. 9-9/. 

Mountain limestone: Sierra Madre; Sierra de Mogollon; Great Salt Lake; 

Tigeras and Pecos Village, N. Mex.; summit of Sierra de Sandia and Sierra 

de Mogollon; El Paso, Chihuahua; junction of rivers San Pedro and Gila, 

Arizona; sources of Rio Colorado Chiquito; Shasta County, Gal.; Vancouver 

Island.

1858. Terebratula subtilita. Hall, Geol. Surv. Iowa, Rept., vol. 1, pt. 2, p. 714.

Coal Measures: Ohio; Indiana; Illinois; Iowa; Missouri; Kansas; Nebraska 

and Pecos Village, N. Mex.

1859. Spirigera subtilita. Meek and Hayden, Acad. Nat. Sci. Philadelphia, Proc.,

p. 28.

Upper Coal Measures: Kansas. 

18fiO. Terebratula? subtilita. Davidson, Mon. British Carb. Brach., Pal. Soc., p. 86,

pi. 1, figs. 21, 22; pi. 17, figs. 8-10.

Carboniferous: Mayen Wais, England; Tournay, Belgium. 

1861. Athyris subtilita. Salter, Geol. Soc. London, Quart. Jour., vol. 17, p. 64, pi.

4, fig. 4. 

Carboniferous: Isthmus of Copacabana, in the Lake of Titicaca.

1861. Athyris subtilita. Newberry, Ives's Colorado River Expl. Exped., Rept., p. 126. 

Upper Carboniferous: Cherty limestone on banks of Colorado between Little 

Colorado and Diamond rivers; Pecos Village, east of Santa Fe.

1862. Terebratula (?) subtilita. Davidson, Mon. British Carb. Brach., Pal. Soc.,

p. 217, pi. 17, figs. 8-10.

Carboniferous limestone: Bolland; Kendal in Westmoreland.

1866. Atkyris subtilita. Geinitz, Carb. und Dyas in Nebraska, p. 40, tab. 3, figs. 7-9. 

Upper Coal Measures: Omaha City, Plattsmouth, Bennett's Mill,-and Nebraska;

City, Nebr. 

1869. Spirifera (Athyris) subtilita. Toula, Kais. Akad. der Wissensch. Wien, Sitzb.

vol. 59, 1. Abth., p. 438, pi. 1, fig. 5.

Carboniferous limestone: 10 miles from Cochebamba, Bolivia. 

1872. Athyris subtilita. Meek, U. S. Geol. Surv. Nebraska, Final Rept., p. 180, pi. 1,

fig. 12; pi. 5, fig. 8; pi. 8, fig. 4. 

Upper Coal Measures: Nebraska City, Bennett's Mill, Wyoming City, Cedar

Bluff, Rock Bluff, Plattsmouth, Bellevue, and Omaha, Nebr. 

Coal Measures: Illinois; Missouri; Iowa; West Virginia; Ohio; Kansas; Pecos 

Village, N. Mex.
70 MANZANO GROUP OF RIO GRANDE VALLEY.

1873. Athyris subtilita. Meek and Worthen, Geol. Surv. Illinois, Rept., vol. 3, p. 570,

pi. 25, fig. 14. 

Coal Measures: Illinois.

1874. Athyris subtilita. Derby (pars), Cornell Univ., (Science) Bull., vol. 1, No. 2, 

p. 7, pi. 1, figs. 5, 8 (hot fig. 7=Spirigerella Derbyi); pi. 3, figs. 8, 16, 19; pi. 6, 

fig. 2; pi. 9, fig. 4. 

Coal Measures: Bomjardim, Itaituba, and Paredao, Brazil.

1875. Spirigera subtilita. White, U. S. Geog. Surv. W. 100th Mer., Kept., vol. 4,

p. 141, pi. 10, figs. 6a-c. (Whole volume published in 1877:) 

Carboniferous: Carizo Creek, Maricopa County; Camp Apache; Tenney's Ranch; 

Kaibab Plateau; confluence of White Mountains and Black rivers; Grass 

Mountain, 35 miles north of Pioche, and foothills' of Dragoon Mountains, 

Arizona; Fossil Hill, White Pine County, and Camp Cottonwood, Nev.; 15 

miles south of St. George; near Ophir City; Rock Canyon, Wasatch range, 

near Provo; and near Minersville, Utah.

1876. Spirigera subtilita. White, U. S. Geol. Geog. Surv. Terr., Second Division;

Powell's Rept. Geol. Uinta Mountains, p. 90. 

Lower Aubrey group: Confluence of Grand and Green rivers, and near Echo

Park, Utah.

Upper Aubrey group: Beehive Point, near Horseshoe Canyon, Utah. 

1876. Athyris subtilita. Meek, Simpson's Expl. Great Basin, Utah, Rept., p. 350,

pi. 2, figs. 4a, b.

Yellow limestone, Coal Measures: Humboldt Mountains. 

1876. Athyris subtilita. Newberry, Macomb's U. S. Expl. Exped. Santa Fe to Grand

and Green rivers, Rept., p. 138.

Upper Carboniferous: On the Colorado;'west of the San Francisco Mountains; 

junction of Grand and Green rivers; in the Sierra la Plata; at Santa Fe; Pecos. 

1876. Athyris subtilita. Derby, Mus. Comp. Zool., Bull., vol. 3, p. 279. 

Coal Measures: Yampopata, Brazil.

1876. Athyris subtilita. Meek, U. S. Geol. Geog.'Surv. Terr., Bull., vol. 2, p. 355,

pi. 1, figs. 2, 2a. 

' Carboniferous: Katlahwoke, Rocky Mountains.

1877. Athyris subtilita. Meek, U. S. Geol. Expl. 40th Par., Rept., vol. 4, p. 83, pi. 8, 

figs. 6, 6a.

Carboniferous limestone: Ruby group; Moleen Peak, near Humboldt River,

Nevada. 

' 1884. Athyris subtilita. White, Geol. Surv. Indiana, Thirteenth Rept., p. 136, pi. 35,

figs. 6-9.

Coal Measures: Indiana. 

1887. Athyris subtilita. Herrick, Sci. Lab. Denison Univ., Bull., vol. 2, p. 44, pi. 1,

figs. 18 (16a-c?). 

Coal Measures: Flint Ridge, Ohio.

1887. Athyris subtilita. De Koninck, Muse"e Royal d'Histoire Naturelle de Belgique, 

Ann., vol. 14, p. 73, pi. 18, figs. 1-4, 7-10, 12-28; pi. 19, figs. 47-56.

1888. Athyris subtilita. Keyes, Acad. Nat. Sci. Philadelphia, Proc., p. 231.

. Lower Coal Measures: Des Moines, Iowa. 

1891. Athyris subtilita. Whitfield, New York Acad. Sci., Ann., vol. 5, p. 604, pi. 16,'

figs. 7-9. , .

Coal Measur.es: Hocking County, Ohio.

1893. Seminula subtilita. Hall and Clarke, Geol. Surv. New York, Pal., vol. 8, pt. 2, 

-p. 95, figs. 66,67 on p. 95, and figs. 58,59 on p. 86; pi. 47, figs. 17-31. (Advance 

distribution in fascicles.)

(?) Chester limestone: Caldwell County, Ky.; Chester, 111. 

Coal Measures: Manhattan and Miami County, Kans.; Kansas City and Chariton 

County, Mo.; Coppers Creek, and Winterset, Iowa; Ohio.
PALEONTOLOGY. . 71

1895. Seminula subtilita. Hall and Clarke, State.Geologist [New York], Fourteenth

Ann. Kept., for 1894, pi. 35, figs. 16-19.

Coal Measures: Chariton County, Mo.; Winterset, Iowa; near Kansas City, Mo. 

1895. Athyris argentea. Keyes, Missouri Geol. Surv., Kept., vol. 5, p. 92, pi. 39,

figs, lla-d. (Date of imprint 1894.)

Coal Measures: Kansas City, Lexington, and Clinton, Mo. 

1895. Seminula subtilita. Hall and Clarke, Geol. Surv. New York, Pal., vol. 8, pt. 2,

p. 95, figs. 66, 67, and 58, 59 on p. 86; pi. 47, figs. 17-31. 

Coal Measures: Manhattan, Kans.; Coppers Creek, Iowa; Chariton County, Mo.;

Winterset, Iowa; Miami County, Kans.; Kansas City, Mo.; Ohio. 

(?) Chester limestone: Caldwell County, Ky.; Chester, 111.

1895. Athyris subtilita. Whitfield, Geol. Surv. Ohio, Kept., vol. 7, p. 488, pi. 12,

figs. 7-9. Coal Measures: Falls Township and Webb Summit, Hocking County, Ohio.

1896. Athyris subtilita. Smith, Am. Phil. Soc., Proc., vol. 35, p. 241.

Upper Coal Measures: Sebastian County, sec. 12, T. 8 N., R. 32 W., Arkansas; 

Poteau Mountain, Indian Territory.

(?) Burlington or Lower Keokuk (Boone chert): Stone County, N. W. { SOC. 9,

T. 14 N., R. 10 W., Arkansas. 

1896. Athyris subtilita. Smith, Leland Stanford Junior Univ. Publ.; Cont. Biol.

Hopkina Seaside Lab., No. 19, p. 31. 

Upper Coal Measures: Sebastian County, sec. 12, T. 8 N., R. 32 W., Arkansas;

Poteau Mountain, Indian Territory. 

(?) Burlington or Lower Keokuk (Boone chert): Stone County, N. W. -J sec. 9,

T. 14 N., R. 10 W., Arkansas. 

1900. Seminula argentea. Beede, Univ. Geol. Surv. Kansas, Rept., vol. 6, p. 105,

text-fig. 3c.

Upper and Lower Coal Measures: Marmaton Station, Bourbon County, lola, 

Kansas City, Eudora, Lawrence, Lecompton, Topeka, Manhattan, Grand 

Summit, Kans.. 

1900. Seminula argentia. Knight, Univ. Wyoming, Wyoming Exp. Sta., Bull.

No. 45, pi. 3, fig. 6. 

1900. Athyris argentea (subtilita). Hernck and Bendrat, Am. Geol., vol. 25, No. 4,

p. 240. 

Coal Measures: Sandia Mountains, N. Mex.

1902. Seminula argentia. Beede, Kansas Univ. Sci. Bull., vol. 1; pp. 155-157, pi. 6.

1903. Seminula subtilita. Girty, U. S. Geol. Surv.; Prof. Paper No. 16, p. 403, pi. 7, 

figs. 1-16, 2, 2a, 3, 3a, 4-7, 7a, 8-10.

Molas formation: San Juan region, Colorado.

Hermosa formation: San Juan region and Ouray, Colo.

Rico formation: San Juan region, Colorado.

Maroon formation: Crested Butte district, Colo.

Robinson limestone: Leadville district, Colo. ' . .

Carboniferous: Glenwood Springs, Colo.

1904! Seminula subtilita. Girty, U. S. Geol. Surv., Prof. Paper No. 21, p. 53, pi. 11, 

 figs. 15, 16.

Pennsylvanjan (Naco limestone): Bisbee quadrangle, Arizona.

Associated in some cases with typical 0. mexicana are a number of 

examples which have a fold and sinus less strongly or even very 

faintly developed. Some of these are small and may perhaps correctly be regarded as immature examples of that species. In other 

cases the size is rather large and no such interpretation can be given 

them. They must either be mature examples of a species somewhat
72 MANZANO GROUP OF RIO GRANDE VALLEY.

different from G. mexicana or young ones of a much larger species. 

While no well-defined limits can be given to either one form or the 

other, it. seems expedient to assemble them under two different 

groups. The present group has been placed under C. subtilita, and 

would unquestionably be so called if found in the Mississippi Valley. 

While it, clearly does not represent the typical variety, I do not feel 

justified in attempting, especially from the Manzano material, to 

establish any new subdivision.

Horizon and locality. Yeso formation, Mesa del Yeso (stations 

3751b and 3751c); San Andreas formation, Fra Cristobal (station 

3743); Abo sandstone, Abo Canyon (station 3757a).

PELECYPODA.

SOLENOMYA? NJENIA Walcott.

1884. Sanguinolites? nxnia. Walcott, U. S. Geol. Surv., Mon. 8, p. 249, pi. 19, fig. 9. 

Lower Carboniferous: Eureka district, Nevada.

A single small specimen strongly resembling the form from the 

Eureka district, but only one-fourth as large. No better identification can at present be suggested. It is rather more probable that 

this form is a Solenomya than a Sanguinolites, in which genus Walcott provisionally placed it.

Horizon and locality. San Andreas formation, Fra Cristobal 

(station 3743).

CLINOPISTHA? sp.

Plate X, figure 5.

This form is represented in our collection by three specimens, none 

of them in Very good condition. They suggest at first sight C. 

radiata var. Isevis, and even a comparison of specimens shows few, 

and possibly not important or constant, differences. Such as have 

been noted are the more slender shape of the Manzano form, its less 

prominent anterior extremity, and the more contracted outline of 

the posterior extremity, which has less of a quadrate shape by reason 

of the lower margin's bending upward more gradually. Until more 

complete data are available about the Manzano form it seems inadvisable either to identify it with C. radiata var. Isevis or to describe 

it as new. In fact, sufficient is not yet known to determine whether 

it belongs to Meek and Worthen's singular genus or not. The general 

shape is suggestive of &Wucula, but so far as determined the hinge 

appears to be edentukfus, in which of course it agrees with Olinopistha. ' 

. Horizon and locality. San Andreas formation, Mesa del Yeso 

(station 3751'd) and Fra Cristobal (station 3743).
PALEONTOLOGY. 73

EDMONDIA GIBBOSA McCoy.

1844. Astarte gibbosa. McCoy, Syn. Garb. Foss. Ireland, p. 55, pi. 8, fig. 11.

Carboniferous: Ireland. 

1866. Astarte gibbosa. Geinitz. Garb, und Dyasin Nebraska, p. 16, Tab. 1, figs. 23, 24.

Carboniferous: Plattsmouth, Nebr.

1903. Edmondia gibbosa. Girty, TJ. S. Geol. Surv., Prof. Paper No. 16, p. 447, pi. 9, 

figs. 7,8, 9.

Rico formation: San Juan region, Col.

Cisco group: Graham Young Co., Tex.

The fossils from the Manzano group are unfortunately imperfectly 

preserved, but they appear to agree very closely with the form from 

Kansas which Geinitz identified as Astarte gibbosa, McCoy. In 1.903 

I identified with this same species a form from the Rico formation of 

Colorado which also appears closely allied to that under consideration. At that time I cited the name as Edmondia gibbosa Geinitz non 

Astarte gibbosa McCoy, which would 'unquestionably be the proper 

form if McCoy's original species were an Astarte, or any other genus 

than an Edmondia, to which the American form with little question 

belongs. But if one may judge by his figures McCoy's Astarte gibbosa 

is also an Edmondia and a form very similar to that from the Mississippi Valley which Geinitz identified with it. It seems probable 

that were good specimens of both brought into comparison distinguishing characters would be discovered, but I do not find it practicable on the strength of the poor fossils which have come under 

my observation to attempt to discriminate between them.

The form from the Manzano group has a subcircular or slightly 

transverse shape, with high convexity, rather gibbous, strongly 

down-curved umbones, and projecting anterior portion. The surface 

is marked by rather regular lamellose concentric ridges, which are 

more closely arranged in some specimens than in others.

This is not to be confused with the species described by Swallow 

and bearing the same name, Edmondia gibbosa. The latter is presumably a different form, and if it proves to be an Edmondia will 

have to receive another name.

Horizon and locality. Abo sandstone, Sandia Mountains (station 

3798), Abo Canyon (station 3757a), and Mesa del Yeso (station 

3751); Yeso formation, Blackinton's ranch (station 3750?).

CELENOMYA LEAVENWORTHENSIS Meek and Hayden.

1858. Allorisma? Leavemuorthensis. Meek and Hayden, Acad. Nat. Sci. Philadelphia,

Proc., p. 263.

Coal Measures: Leaven worth, Kans. 

1864. Chsenomya leayenworthensis. Meek and Hayden, Smithsonian Cont. Knowledge,

vol. 14, No. 172, p. 43, pi. 2, figs. la-c. 

Coal Measures: Leavenworth, Kans. 

1866. Allorisma Leavenworthensis. Geinitz, Garb, und Dyas in Nebraska, p. 15.
74 MANZANO GROUP OF RIO GRANDE VALLEY.

1872. Chssnomya Leavenworthensis. Meek, U. S. Geol. Surv. Nebraska, Final Kept.,

p. 216, pi. 2, fig. 9.

Upper Coal Measures: Rock Bluff, Nebr.; Leavenworth, Kans. 

Coal Measures: Iowa, Missouri, Illinois. 

1895. Chsenomya leavenworthensis. Keyes, Missouri Geol. Surv., Kept., vol. 5, p. 131.

(Date of imprint, 1894.) 

Upper Coal Measures: Kansas City, Mo. 

1900. Chxnomya leavenworthensis. Beede, Univ. Geol. Surv. Kansas, Kept., vol. 6,

p. 172, pi. 19, figs. 3-3b.

Upper Coal Measures: Kansas City, Lawrence, Kan.

1903. Chsenomya leavenworthensis. Girty, U. S. Geol. Surv., Prof. Paper No. 16, p. 436. 

Hermosa formation: San Juan region and Sinbads Valley, Colo.

This type is represented in our collection by two specimens, both 

of them in a rather unsatisfactory state of preservation: In their 

present obscured condition I am unable to discriminate them from 

the species cited above, and even more perfect specimens could 

hardly do more than show that they are very closely allied to it.

Horizon and locality. Abo sandstone, Abo Canyon (station 3757a) 

and Mesa del Yeso (station 3751).

NUCULA LEVATIFOEMIS Walcott.

Plate X, figures 7 and 8.

1884. Nucula levatiforme. Walcott, U. S. Geol. Surv., Mon. 8, p. 241, pi. 22, figs.

1, la. 

Lower Carboniferous: Eureka district, Nevada.

Shell small, seldom attaining a width of more than 7 mm. Shape 

subtriangular, width not greatly in excess of the height. Superior 

outline rounded. Inferior outline more strongly curved than the 

superior and converging with it toward the front, Anterior outline

narrowly rounded. Posterior outline subrectilinear, nearly perpen-1

dicular to that above and meeting it in somewhat of an angle defined 

by the umbones; sometimes joining the lower outline more or less 

abruptly. Convexity high. Posterior end of shell beneath the 

beaks rather abruptly deflected, or flattened. Surface marked by 

very fine, regular, concentric striae.

There are about 6 posterior teeth and 10 anterior ones, the 3 or 4 

nearest the beak being rather small and obscure.

I feel little doubt that this species is the same as Walcott's N. 

levatiformis. It also resembles N. parva, differing in having the 

superior outline convex, instead of straight or concave, so that it is 

somewhat broader behind.

Horizon and locality. rYeso formation, Alamillo (station 3751e) 

and San Andreas (station 3742d); San Andreas formation, Fra 

Cristobal (station 3743) and Engle (station 3595).
ttn® ~ QxA 

r

5 c) 5 cy a., o / ' 

J ^ ^ C/ f«UC 
PALEONTOLOGY. 75

NUCULA LEVATIFORMIS var. OBLiQUA n. var.

Plate X, figure 9.

At station 3743b occurs what appears from present indications to 

be a distinct variety of the Nevada species to which the other fossils 

have been referred. This form is distinguished by being much 

smaller and somewhat more oblique, so that the cardinal and anterior 

margins meet at an acute angle, whereas in typical N. levatiformis the 

angle is usually almost a right angle. All of the specimens agree in 

possessing this peculiarity, a fact which seems to warrant a partial 

separation from the typical form.

Horizon and locality. Yeso formation, Fra Cristobal (station 

3743b).

MANZANELLA n. gen.

Shell small, transverse, elliptical, wider at the anterior end. Umbones rather large, subcentral, distinctly turned toward the longer 

side. The thickened hinge posterior to the umbones bears a small 

number of taxodont teeth similar to those of Nucula. Anterior to 

the umbones there are developed two rather short, slightly diverging 

teeth which form an abrupt columnar thickening of the cardinal 

margin. In the right valve the lower of these two teeth is much 

larger and more prominent than the other. In the left valve the 

upper is the larger. A large muscle scar seems to be situated at the 

anterior .end of the shell at the foot of the columnar thickening which 

supports th.e two anterior teeth. The character of the pallial line has 

not been determined.

The orientation of this shell can not be positively made. On a 

number of specimens there are indications, often very indistinct it is 

true, of a ligamental area just above the row of taxodont teeth. 

The fceaks would therefore be normal in pointing toward the anterior 

end, but the present type would traverse the common run of pelecypod shells in having the anterior end longer than the posterior. 

This orientation is here adopted. ,

The relationship, of Manzanella to other .genera is a matter of much 

uncertainty, and I anticipate that it will ultimately prove advisable 

to make it the type of a new family. In its taxodont dentition, at 

least upon one side, and the fact that it is produced upon the anterior rather than the posterior end, this genus strongly suggests the 

Nuculidae, but ,the pair of stout anterior teeth is of course quite alien 

to the typical Nuculoid dentition. The absence of a chondrophore 

and the fact that the anterior extremity is broad instead of contracting are also minor points of difference.
76 MANZANO GEOUP OF EIO GRANDE VALLEY.

MANZANELLA ELLIPTICA n. sp.

Plate X, figures 3 and 4.

Shell small, transversely elliptical, slightly wider at the anterior 

end, otherwise nearly bilateral. The shape, which is in other respects 

rather regularly elliptical as outlined by the aperture, is interrupted 

by the umbo, which is large, strongly projecting, and distinctly 

turned toward the larger end of the shell. Although one end is 

clearly longer than the other, the beak is subcentral. The convexity 

is rather high.

The surface is nearly smooth, marked only by somewhat irregular 

concentric striae and by occasional inequalities of growth. In a few 

instances traces of regular, closely arranged concentric strisB have 

been noted.

'Upon the interior the hinge posterior to the beak is thickened and 

bears about four arched denticles (and four sockets), similar to those 

in Nucula. In front of the beak also the hinge is thickened and 

supports a rather small, longitudinal, platelike, anterior tooth. 

Springing from the bottom of the valve, though for some distance 

consolidated with its cardinal margin', a second anterior tooth is 

developed. It is very stout, and diverges somewhat with the other, 

so that a large socket is left between. In the other (left) valve the 

dentition is of course the complement of this. The upper of the 

two anterior teeth is in this case larger and more strongly projecting.

Horizon and locality. Yeso formation, Alamillo (station 375le).

LEDA OBESA White.

1879. Nuculana obesa. White, U. S. Geol. Geog. Surv. Terr., Bull., vol. 5, p. 216.

Carboniferous: Wild Band Pockets, northern Arizona, 15 miles south of Pipe 

Spring.

1880. Nuculana obesa. White, U. S. Geol. Surv., F. V. Hayden in charge, Cont. to

Pal. Nos. 2-8, p. 136, pi. 34, figs. 2o-c. 

Upper Carboniferous: Wild Band Pockets, northern Arizona, 15 miles south

from Pipe Spring. 

1883. Nuculana obesa. White, U. S. Geol. Geog. Surv. Terr.,. Twelfth Ann. Kept.,

for 1878, pt. 1, p. 136, pi. 34, figs. 2a-c.

Upper Carboniferous: Wild Band Pockets, northern Arizona, 15 miles south 

from Pipe Spring.

Although rather unsatisfactorily preserved, there is not much 

question but that the Manzano form belongs to White's species. 

One specimen retains part of the thick shell, thus showing the sculpture, which consists of delicate raised lines separated by flattened 

interspaces of much greater width. They are apt to be wavy, and 

they do not always follow the growth lines, running in some cases
PALEONTOLOGY. 77

oblique to them. The fossils in the present collection are all somewhat smaller than those upon which the species was founded.

Horizon and locality. Yeso formation, Mesa del Yeso (stations 

3751a and 3751c); Abo sandstone, Abo Canyon (station 3757a).

PARALLELODON aff. OBSOLETUS Meek.

Of this form but a single example has come to hand, preserved as 

an internal mold. It is of small size, about 18 mm. in width, and the 

posterior portion is marked by rather coarse radial ribs. The exact 

identification is at present hardly possible.

Horizon and locality. Yeso formation, San Andreas (station 

3742b).

AVICULIPINNA ? PERACUTA Shumard. 

1858. Pinna peracuta. Shumard, Acad. Sci. St. Louis, Trans., vol. 1, p. 214.

Upper Coal Measures: Iowa Point, Nebraska; Kansas. 

1860. Pinna adamsi. McChesney, Desc. New Spec. Pal. Foss., p. 74.

Coal Measures: Lasalle, 111. 

1872. Pinna peracuta. Meek, U. S. Geol. Surv. Nebraska, Final Kept., p. 198, pi.

6, figs, lla, b. 

Upper Coal Measures: Bennett's Mill, Wyoming; Nebraska City, Plattsinouth,

Rock Bluff, and Bellevue, Nebr.

Coal Measures: Iowa, Nebraska, Kansas, Missouri, and Illinois. 

1875. Pinna peracuta-(I). White, U. S. Geog. Surv. W. 100th Mer., Rept., vol. 4,

p. 151, pi. 11, fig. 5a. (Whole volume published in 1877.) 

Carboniferous: Near Relief Spring, Ariz. 

1884. Pinna peracuta. White, Geol. Surv. Indiana, Thirteenth Rept., p. 145, pi. 28,

figs. 1, 2. > 

Upper, Middle, and Lower Coal Measures: Indiana. 

1886. Pinna peracuta. Heilprin, Wyoming Hist, and Geol. Soc., Proc. and Coll., vol.

2, pt. 2, p. 272, fig. 12; p. 273, fig. 12a.

Upper Coal Measures, Mill Creek limestone: Wilkesbarre, Pa. 

1886. Pinna peracuta. Heilprin, Second Geol. Surv. Pennsylvania, Ann. Rept. for

1885, p. 455; p. 444, fig. 12; p. 454, fig. 12a. . 

Upper Coal Measures, Mill Oeek limestone: Wilkesbarre, Pa. 

1892. Aviculopinna peracuta. Hyatt, Boston Soc. Nat. Hist., Proc., vol. 25, p. 338.

Coal Measures: Kidder, Mo.; La Salle, 111. 

1895. Pinna peracuta. Keyes, Missouri Geol. Surv., Rept., vol. 5, p. 116, pi. 45,

figs. 2a, 6 (date of imprint, 1894). 

Upper Coal Measures: Kansas City, Mo.

1899. Pinna peracuta. Girty, U. S. Geol. Surv., Nineteenth Ann. Rept., pt. 3, p. 579. 

Upper Coal Measures: McAlester quadrangle; Atoka quadrangle, Ind. Ter.

1900. Pinna peracuta. Beede, Univ. Geol. Surv. Kansas, Rept., vol. 6, p. 144, pi.

17, figs. 3, 36.

Upper Coal Measures: Kansas City, Lawrence, Topeka, Kans. 

1903. Aviculopinna? peracuta. Girty, U. S. Geol. Surv., Prof. Paper No. 16, p. 432,

pi. 9, figs. 1, 2.

Hermosa formation: San Juan region, Colo. 

Weber formation: Leadville district, Colo.
78 MANZANO GEOUP OF BIO GRANDE VALLEY.

This form as it occurs in the Manzano group is represented primarily 

by a single specimen, which is distinguished by its very slender proportions and subparallel upper and lower margins. This fragmentary 

specimen has a length of 155 mm. The height at the small end is 

33 mm. and at the larger one about 45 mm. The rate of expansion 

is perhaps a little more gradual than in the specimen of Aviculopinna 

peracuta figured by Meek. It is preserved as an internal mold, and 

while at present there are no characters which satisfactorily distinguish it from the Pennsylvanian species, possibly when more complete data can be obtained it will prove not to be the same.

Horizon and locality. Abo sandstone, Abo Canyon (station 3757a), 

Mesa del Yeso (station 3751?), and Sandia Mountains (station 3798.?)

AVICULIPINNA NEBEASKENSIS Beede.

1901. Aviculopinna nebraskensis. Beede, Kansas Acad. Sci., .Trans., vol. 17, p. 186,

pi. 13, figs. l-ld.

Permian: Gage County, Nebraska. 

1903. Aviculopinna nebraskensis. Girty, U. S. Geol. Surv., Prof. Paper No. 16, p.

435, pi. 9, figs. 1, 2. 

Rico formation: San Juan region, Colorado.

The fossils referred to this species vary much in size, the largest 

fragment having a height at the larger end of 50 mm. They are at 

once distinguished from the form referred to A. peracuta in being 

broader and in tapering more rapidly. So far as can be told this is 

the same species which occurs in the Rico formation and to which I 

there gave the same identification. It is true, however, that the 

present specimens leave many points in obscurity. The apical angle 

is about the same as in A. nebraslcensis, but owing to exfoliation the 

sculpture and the posterior outline can often not be determined. In 

one or two instances the sculpture consists of regularly spaced 

lamellose lines having the character and direction shown by the 

Colorado specimens. Usually, however, though perhaps owing to 

preservation, they do not appear to be lamellose and are more or less 

obscure. Although attaining a size larger than heretofore known 

for the species, I can hardly do otherwise than identify the Manzano 

specimens with Aviculipinna nebraslcensis.

Horizon and locality. San Andreas formation, Caballos Mountains 

(stations 3738 and 3738a) and Elephant Butte (station 3600); Abo 

sandstone, Abo Canyon (station 3757a) and Sandia Mountains 

(station 3798?); Yeso formation, San Andreas (station 3742e).

MONOPTERIA MARIAN White.

1874. Monopteria Marian. White, U. S. Geog. Surv. W. 100th Mer.; Prel. Kept. Inv.

Foss., p. 22. 

Carboniferous (Coal Measures): Camp Apache, Arizona.
PALEONTOLOGY. 79

1877. Monopteria Marian. White, II. S. Geog. Surv. W. 100th Mer., Kept., vol. 4,

p. 151, pi. 11, figs. 4a-c.

Carboniferous: Camp Apache, Maricopa County, Arizona. 

1900. Limopteria Marian. Beede^ Univ. Geol. Surv. Kansas, Kept., vol. 6, p. 128,

pi. 16, figs. 5-5c. 

Upper Coal Measures: Turner, Topeka, Kans.

This species is represented in our Manzano collection by fragments 

merely, but there can be little doubt, in view of their angular and 

greatly prolonged posterior extension, that they belong to the species 

cited above. This feature is indicated as even more pronounced 

than represented in White's figure.

Horizon and locality. Abo sandstone, Sandia Mountains (station 

3796) and Abo Canyon (station 3757a).

PTERIA sp.

Our collection contains two specimens of this little form, too imperfect to permit of the determination of their specific relationship with 

any degree of certainty. They seem to resemble P. ohioensis more 

closely than any other species of Pteria found in our American 

Carboniferous rocks, but I would hesitate to identify them definitely 

with that species.

They closely resemble also Bakewellia? parva. It is true that the 

serially repeated resilium characteristic of Bakewellia can not be seen 

on these specimens, but that character is absent, so far as I have been 

able to observe, in the Pennsylvanian species also, so that the present 

form may prove to be identical, not only generically but also specifically, with B. parva.

Horizon and locality. Yeso formation, Alamillo (station 3751e).

PSEUDOMONOTIS HAWNi Meek and Hay den ?

PLATE IX, figure 4.

1858. Monotis Hawni. Meek and Hayden, Albany Inst., Trans., vol. 4, p. 76.

Permian: Near mouth of Smoky Hill Fork of Kansas River and Helena, Kans.

1859. Monotis Hawni. Meek and Hayden, Acad. Nat. Sci. Philadelphia, Proc., p. 28. 

Upper Coal Measures: South of Kansas Falls, Smoky Hill River, and Cottonwood Creek, Kansas. 

1864. Eumicrotis Hawni. Meek and Hayden, Smithsonian Cont. Knowledge, vol. 14,

No. 172, p. 54, pi. 2, figs. 5a-c. 

Permian: Near mouth of Smoky Hill Fork of Kansas River and between there

and Council Grove; also on Cotton wood Creek, Kansas. 

1884. Eumicrotis Hawni. White, Geol. Surv. Indiana, Thirteenth Rept., p. 142, pi.

30, fig. 10.

Upper Coal Measures: Indiana.

1886. Eumicrotis Hawni. Heilprin, Second Geol. Surv. Pennsylvania, Ann. Rept. 

. for 1885, p. 455. 

Upper Coal Measures, Mill Creek limestone: Wilkesbarre, Pa.
80 MANZANO GEOUP OF BIO GRANDE VALLEY.

1886. Eumicrotis Hawni. Heilprin, Proc. and Coll. Wyoming Hist, and Geol. Soc.,

vol. 2, pt. 2, p. 271. 

Upper Coal Measures, Mill Creek limestone: Wilkesbarre, Pa.

1899. Pseudomonotis cf. hawni. Beede, Kansas Univ. Quart., vol. 8, No. 2, p. 83, pi.

19, figs. l-l/.

Upper Coal Measures: Turner, Wyandotte County, Kans.; Clements, Topeka, 

Lawrence, Kans.

1900. Pseudomonotis Hawni. Beede, Univ. Geol. Surv. Kansas, Kept., vol. 6, p. 132, 

pi. 13, figs. 11-llc; pi. 15, figs, l-l/, 2, 2a.

Upper Coal Measures: Turner, Lawrence, near Topeka, Kans. 

1903. Pseudomonotis hawni. Girty, U. S. Geol. Surv., Prof. Paper No. 16, p. 427.

Hermosa and Rico formations: San Juan region, Colorado.

A few specimens, some of them found associated with P. sullsevis, 

are distinguished by having the sculpture much more strongly 

developed.

These shells seem to be very similar to P. hawni, but it is doubtful 

whether they should be referred to that species or should be regarded 

merely as young examples of P. subls&vis, in which the striation, 

always more pronounced at that stage than later, is more sharply 

developed than common.

Horizon and locality. San Andreas formation, Engle (station 

3740); Yeso formation, San Andreas (station 3742b); Abo sandstone, 

Abo Canyon (station 3757a).

PSEUDOMONOTIS SUBL^EVIS 11. sp.

Plate IX, figures 1-3.

Shell large. Shape subovate, rather irregular. Hinge shorter than 

the width below, ears small.

Surface of the left valve with obsolescent sculpture. In the umbonal region it is marked by fine, irregular, more or less wavy costae, 

a few of which, arranged at rather regular intervals, are somewhat 

larger than the others. In the course of growth the smaller costae as 

a rule soon die out, while a few of the; larger ones, from 1 to 12 or 

more in number, much increased in size, pass on to the ventral border. 

More rarely some of the smaller costse are persistent. The whole 

surface is also crossed by closely arranged, irregular, concentric, 

lamellose lines and wrinkles.

This species is related to P. hawni, but is distinguished by its 

obsolescent sculpture and by the rarity or absence of spinelike scales 

springing from the larger costse. These could hardly fail to be preserved upon our specimens if originally present, and they were 

apparently developed very rarely, perhaps not at all.

Horizon and locality. Yeso formation, San Andreas (stations 

3742b, 3742c, and 3742d); San Andreas formation, Engle (station 

3740?).
PALEONTOLOGY. 81

MYALINA APACHESI Marcou.

Plate IX, figures 6 and 7.

1858. Myalina apachesi. Marcou, Geol. North America, p. 44, pi. 7, figs. 6, Ga. 

Mountain limestone: Near Pecos Village, New Mexico.

As identified in the present collection this species has an elongate 

triangular shape, with rather short hinge line. The anterior outline, 

marking the edge of the umbonal ridge, makes an angle of about 

45° with the hinge, while the posterior outline makes an angle of 

from 60 ° to possibly almost 90 ° with the same margin. The anterior 

and. posterior outlines thus gradually approach each other below, 

where they round together in a regular curve. The umbonal ridge is 

very high in front, projecting in a long down-curved beak. It spreads 

out and flattens down toward the inferior border. The anteriorsuperior margin of the shell bends downward and inward below the 

umbonal ridge, which in this portion forms the outline of the shell 

when viewed from above. A distinct sinus occurs in this deflected 

portion, but it is scarcely visible except when the shell is looked at 

from the anterior side, instead of from above. The surface is marked 

by regularly disposed, deeply imbricating lamellae, the development 

of which produces concentric striae or corrugations, a very noticeable 

character even on internal molds. The largest specimen referred to 

this species is of large size. It is imperfect, but must have measured 

about 100.mm. along the umbonal ridge.

It is not quite certain that the Manzano form is the same as that 

which Marcou gave the name Myalina apachesi, for his specimens 

seem to have been imperfect and his illustrations poor. They show 

the same strongly elevated umbonal ridge and deflected anterior 

margin which is a striking feature of the form under consideration; 

and Marcou's description seems to refer to the. presence upon his 

specimens of the concentric striae due to the development of lamellaa, 

which is also a character of the Manzano species. Myalina apachesi 

was described from near Pecos village, N. Mex., and there is good 

reason for believing that the Manzano group outcrops near the railroad station called Pecos, in the Pecos Valley, in the immediate 

vicinity of which it is presumed 'Marcou found his specimens. On 

the other hand, Marcou recognized the present form as Carboniferous, 

whereas he everywhere refers the "Red Beds" to the Trias. Inferentially, therefore, he did not obtain his fossils in place, or they 

came from the underlying Magdalena group, or the Manzano had lost 

its characteristic "Red Beds" aspect. On the other hand, Marcou 

says that M. apachesi is associated with Productus semireticulatus and 

Spirifer striatus. P. semireticulatus of Marcou's report I believe to be 

P. ivesi, while Spirifer striatus has since become S. marcoui. Neither 

$. marcoui nor P. ivesi is known from the Magdalena group. P. ivesi

S4259 Bull. 389 09 6
82 MANZANO GROUP OF BIO GBAKDE VALLEY.

is a rather characteristic fossil of the Manzano, and S. marcoui, while 

at present not known from the Manzano, occurs in the Hueco formation, with which the Manzano is believed to be in correlation. The 

Magdalena group, however, furnishes a small Myalina very similar 

and perhaps identical with the form under consideration.

Of the figured specim.ens the larger retains evidence of a fairly welldeveloped anterior lobe, in this case partly broken away, and a similar 

structure has been restored on the smaller specimen also, which is 

likewise broken. This lobe is usually present, but in various degrees 

of development, while in the larger examples especially it is often 

'largely obscured, when the specimen is viewed from above, by the 

retraction of the anterior-superior margin and the overhanging of 

the umbonal ridge. Where the lobe is well developed and obvious 

this form looks less like M. apachesi and more like the type from the 

Rico formation of Colorado which I identified as M. wyomingensis. 

In the latter the anterior margin is more spread out, not vertical or 

retracted, but they may prove to belong to the same species.

Myalina apachesi as here identified appears to be closely similar 

to Myalina Jcansasensis of the Mississippi Valley Pennsylvanian. 

There is perhaps a certain amount of differenqe in the configuration, 

especially of the umbonal region, and the present form, so far as observed, is entirely without the frilled condition into which the lamellsB 

of the Kansas species usually develop.

Typical Myalina apachesi is very closely related to the form which 

Walcott subsequently described from the Eureka district, Nevada, as 

Myalina congeneris. The associated faunas are similar and it is very 

probable that the Nevada species will prove to be a synonym of that 

described by Marcou.

Horizon and locality. Yeso formation, Mesa del Yeso (station

3751c) and San Andreas (station 3742b); San Andreas formation,

Mesa del Yeso (station 3751d) and Elephant Butte (station 3600); 

Abo sandstone, Abo Canyon (station 3757a), Sandia Mountains 

(station 3798), and Mesa del Yeso (station 3751).

SCHIZODUS WHEELERI Swallow? '

Plate X, figure 6.

1858. Schizodus obscurus. Swallow, St. Louis Acad. Sci., Trans., vol. 1, p. 193.

(Not Axinus obscurus Sowerby, 1823.) 

Lower Permian: Kansas. 

1863. Cypricardia (?) Wheeleri. Swallow, St. Louis Acad. Sci., Trans., vol. 2, p. 96.

Upper Coal Measures: Caldwell County, Missouri. 

1866. Schizodus obscurus. Geinitz, Garb, und Dyas in Nebraska, p. 20, tab. 1, figs.

30, 31.

Nebraska City, Nebr. ' 

1872. Schizodus Wheeleri (pars). Meek, U. S. Geol. Surv. Nebraska, Final Kept.,

p. 209, pi. 10, figs. la-d. 

Upper Coal Measures: Caldwell County, Mo.; Nebraska City, Nebr.; Adams

and Union counties, Iowa. 

Coal Measures: Illinois.
PALEONTOLOGY. 83

1876. Schizodus Wheeleri. White; U. S. Geol. Geog. Surv. Terr., Second Division;

Powell's Kept. Geol. Uinta Mts., p. 91. 

Lower Aubrey group: Confluence of Grand and Green rivers, Utah.

1877. Schizodus Wheeleri. White, U. S. Geog. Surv. W. 100th Merid., Kept., vol. 4,

p. 154, pi. 11, figa. 6a, 6.

Carboniferous: Near Bear Spring, Camp Wingate, N. Mex. 

1884. Schizodus Wheeleri. White, Thirteenth Kept. Geol. Surv. Indiana, p. 147, pi.

30, figs. 3-5.

Coal Measures: Indiana (?). 

1886. Schizodus Wheeleri. Heilprin, Second Geol. Surv. Pennsylvania, Ann. Kept.

for 1885, p. 456, p. 442, fig. 7. 

Upper Coal Measures, Mill Creek limestone: Wilkesbarre, Pa.

1886. Schizodus Wheeleri. Heilprin, Wyoming Hist, and Geol. Soc., Proc. and Coll.,

vol. 2, pt. 2, p. 275; p. 270, fig. 7; p. 274, fig. 7a. 

Upper Coal Measures, Mill Creek limestone: Wilkesbarre, Pa.

1887. Schizodus wheeleri. Herrick, Bull. Sci. Lab. Denison Univ., vol. 2, p. 42, pi.

3, fig. 15. . Coal Measures: Flint Ridge, Ohio.

1895. Schizodus wheeleri. Keyes (pars), Missouri Geol. Surv., Kept., vol. 5, p. 123,

pi. 46, fig. 3c. (Date of imprint, 1894.) 

Upper Coal Measures: Kansas City, Mo.

1896. Schizodus wheeleri. Smith, Stanford Univ. Pub., Cont. Biol. IX, p. 36, pi. 22,

fig. 4. . 

Lower Coal Measures: Conway County, Ark.

1897. Schizodus wheeleri. Smith, American Phil. Soc., Proc., vol. 35, p. 36, pi. 22,

fig. 4.

Lower Coal Measures: Conway County, Ark. 

1900. Schizodus Wheeleri. Beede, Univ. Geol. Surv. Kansas, Kept., vol. 6, p. 155,

pi. 22, figs. 1-lc. 

Upper Coal Measures: Kansas City, Mo.

Shells belonging to the genus Schizodus are rather plentiful in the 

Manzano beds, but they occur so exfoliated and generally imperfect 

that it has proved impossible to make a special study of them. It is 

seldom that the true outline or configuration can be more than estimated. Several varieties can be discriminated, one of which is found 

at station 3742, and appears to be closely related to S. wheeleri 

Swallow; not the form which Meek identified with that species and 

to which I gave a distinctive name, but the typical one. Material 

from other points shows the same general character and appears to 

belong to the same species. One apparent difference is that the 

Manzano form has a very indistinct umbonal ridge, while that of 

typical S. wheeleri is subangular, but this condition is in part due to 

the fact that the former are internal molds and show the umbonal 

ridge less prominently than testiferous examples. The shells from 

station 3742, together with others referred to the same species, present a certain variation in the proportion of length and breadth, 

such that while the transverse forms resemble S. wheeleri the less 

extended ones suggest S. affinis Herrick and also S. curtiformis of the 

Eureka district, Nevada. Some specimens referred to S. wheeleri 

attain a very considerable size.
84 MANZANO GROUP OF EIO GRANDE VALLEY. .

Where the surface of these shells is preserved it is seen to be 

marked by regularly disposed concentric raised lines, about nine in 

5 mm. This seems to be a feature not found in typical S. wheeleri.

White has identified S. wheeleri from Fort Wingate, N. Mex., and 

his form is probably the same species as that here receiving the same 

reference.

Horizon and locality. Yeso formation, San Andreas (stations 

3742b?, 3742c, 3742d, and 3742e), Fra Cristobal (stations 3743a 

and 3743b), Alamillo (station 3751e), Mesa del Yeso (station 3751c), 

Carthage (station 3747a?), and Blackinton's ranch (station 3750); 

San Andreas formation, Elephant Butte (station 3741), Engle (stations 3595? and 3740), Caballos Mountains (station 3738a?), Nogal 

Creek (station 3744), San Andreas (station 3742), and Carthage (stations 3746? and 3746a?); Abo sandstone, Abo Canyon (station 

3757a) and Sandia Mountains (stations 3796? and 3797).

SCHIZODUS aft'. MAGNUS Drake.

What appears to be a second species of Schizodus is represented by 

a few specimens whose most striking characteristic is an elevated 

and very angular umbonal ridge. They are in addition considerably 

elongated posteriorly and abruptly truncated, and their size is considerable, though not notably larger than some of the shells referred 

to S. wheeleri. They strongly suggest the form which Drake described 

as S. magnus, except that the beak is not so nearly central and the 

anterior extremity in consequence is smaller. Even, however, if 

this proves a constant difference I feel that my Manzano material is 

almost too imperfect to justify describing it as new.

Horizon and locality. San Andreas formation, Mesa del Yeso 

(station 3751d); Yeso formation, Mesa del Yeso (station 3751c).

DELTOPECTEN OCCIDENTALIS Shumard.

1855. Pecten occidentalis. Shumard, Missouri Geol. Surv., Kept., p. 207, pi. C, fig. 18.

Coal Measures: Near Plattsburg, Clinton County, Mo. 

1858. Pecten Cleavelandicus. Swallow, Acad. Sci. St. Louis, Trans., vol. 1, p. 184.

Permian: Valley of South Cottonwood, Kansas.

1861. Pecten occidentalis. Newberry, Ives's Colorado River Expl. Exped., Kept., 

p. 128.

Coal Measures: Banks of the Stranger, above Easton, Kans.

1864. Aviculopecten ? Meek and Hay den, Smithsonian Cont. Knowledge, vol. 

14, No. 192, p. 50, pi. 2, fig. 10.

Permian: Near Chapman's Creek, 18 miles above Fo'rt Riley, Kans. 

1866. Aviculopecten occidentalis. Meek and Worthen, Geol. Surv. Illinois, Kept., 

vol. 2, p. 331, pi. 27, figs. 4, 5, 5a.

Upper Coal Measures: Saline Creek, Gallatin County, 111. 

1866. Pecten missouriensis? Geinitz, Garb, und Dyas in Nebraska, p. 35, tab. 2, fig. 18.

Upper Coal Measures: Nebraska City, Nebr.
PALEONTOLOGY. 85

1872. Aviculopecten octidentalis. Meek, U. S. Geol Surv. Nebraska, Final Kept., p.

191, pi. 9, fig. 10. 

Upper Coal Measures: Rock Bluff, Bennett's Mill, Wyoming, and Nebraska

City, Nebr.; Illinois, Missouri, Iowa, Kansas, Kentucky. 

Coal Measures: Black Hills, Dakota. 

.1876. Aviculopecten occidentalis. White, U. S. Geol. Geog. Surv. Terr., Second

Division; Powell's Kept. Geol. Uinta Mountains, p. 90. 

Lower Aubrey group: 2 miles above Belleview, Utah. 

1877. Aviculopecten occidentalis. White, U. S. Geog. Surv. W. 100th Mer., Rept.,

vol. 4, p. 146, pi. 12, figs. 8a, 6. 

Carboniferous: Camp Apache, Ariz. 

1884. Aviculopecten occidentalis. White, Geol. Surv. Indiana, Thirteenth Rept., p.

143, pi. 28, fig. 2.

Coal Measures: Pike and Gibson counties, Ind. 

1886. Aviculopecten occidentalis. Heilprin, Second Geol. Surv. Pennsylvania, Ann.

Rept. for 1885, p. 455, fig. 5a; p. 442, fig. 5. 

Upper Coal Measures, Mill Creek limestone: Wilkesbarre, Pa. 

1886. Aviculopecten occidentalis. Heilprin, Wyoming Hist, and Geol. Soc., Proc. and

Coll., vol. 2, pt. 2, p. 270, fig. 5; p. 271, fig. 5o. 

Upper Coal Measures, Mill Creek limestone: Wilkesbarre, Pa. 

1891. Aviculopecten occidentalis. White, U. S. Geol. Surv., Bull. No. 77, p. 29, pi. 4,

fig. 1. 

Permian: Military Crossing, Baylor County, Tex.

1895. Aviculopecten occidentalis. Keyes, Missouri Geol. Surv., Rept., vol. 5, p. 110,

pi. 42, fig. 3. (Date of imprint 1894.) 

Upper Coal Measures: Plattsburg and Kansas City, Mo.

1896. Aviculopecten occidentalis. Smith, Stanford Univ. Pub., Cont. Biol. IX, p. 34. 

Lower Coal Measures: Conway County and elsewhere, Arkansas.

1897. Aviculopeclen occidentalis. Smith, Am. Phil. Soc., Proc., vol. 35, p. 34. 

Lower Coal Measures: Conway County, Ark.

1899. Aviculopecten occidentalis. Girty, U. S. Geol. Surv., Nineteenth Ann. Rept.,

pt. 3, p. 578. 

Upper Coal Measures: McAlester quadrangle; Atoka quadrangle.

1900. Aviculopecten occidentalis. Beede, Univ. Geol. Surv. Kansas, Rept., vol. 6, p. 

 114, pi. 13, fig. 7. 

Upper Coal Measures: Turner, Eudora, Lawrence, Topeka, Wabaunsee County,

Kans.

1900. Aviculopectin occidentalis. Knight, Univ. Wyoming, Wyoming Exp. Sta., Bull. 

No. 45, pi. 3, fig..3.

1902. Aviculopecten occidentalis. Beede, Okla. Geol. Surv., Adv. Bull., First Bien.

Rept., p. 9. 

Red Beds: Whitehorse Springs, Okla.

1903. Aviculopecten occidentalis. Girty, U. S. Geol. Surv., Prof. Paper No. 16, p. 414,

pi. 8, fig. 1.

Hermosa and Rico formations: San Juan region, Colo. 

Maroon formation: Crested Butte district, Colo.

This species occurs in the Manzano group in considerable abundance at station 3757a, and though the specimens studied are exfoliated and imperfect it seems highly probable that the New Mexico 

specimens belong to Shumard's species. White has cited D. occidentalis from Camp Apache, and his specimens agree well with mine.

Horizon and locality. Abo .sandstone, Abo Canyon (station 

3757a).
86 MANZANO GROUP OF KIO GRANDE VALLEY.

DELTOPECTEN VANVLEETI Beede.

Plate IX, figure 5.

1877. Aviculopecten McCcyi. ^Vhite, U. S. Geog. Surv. W. 100th Mer., vol. 4, p. 149,

pi. 11, fig. 2a.

Carboniferous: Near Bear Spring, Camp Wingate, N. Mex. 

1902. Aviculopecten vanvleeti. Beede, Oklahoma Geol. Surv., Adv. Bull., First

Bien. Kept., p. 6, pi. 1, figs. 8-86. 

Red beds: Whitehorse Springs, Okla. 

1907. Aviculopecten vanvleeti. Beede, Kansas Univ. Sci. Bull., vol. 4, No. 3, p. 159,

pi. 5, figs. 2-2*. 

Upper Permian: Whitehorse Springs, Okla.; Dozier, Tex.

Shell attaining a rather large size, 50 mm. or more in length. 

Hinge line somewhat shorter than the greatest width. Outline of 

left valve contracting below the hinge and spreading again to its 

maximum, about one-third the whole length up from the lower 

margin. Axis nearly perpendicular to the cardinal line. Ears 

large, triangular, well defined, the anterior abruptly depressed.

Sculpture consisting of numerous fine radii, which increase in size 

from apex to lower margin. N;ew ones are rather irregularly introduced by intercalation, so that they are alternating and of many 

grades of size. About six primary ones are much larger than any of 

the others, and very much larger than what may be called the average. 

They stand at varying intervals, most widely separated near the 

middle, closer together laterally. There are also fine, concentric, 

lamellose lines which tend to form scalelike spines upon the costae, 

the size and frequency of the spines bearing a direct relationship to 

the size of the costse themselves. Those upon the large primary ribs 

are large, producing nodes upon them, and they are a long distance 

apart.

The posterior ear is defined by the last of the primary costse. It is 

marked by a few fine, widely spaced radii and by concentric lamellose lines. The anterior ear, as already stated, is strongly and rather 

abruptly depressed. It appears to be marked by fine, closely 

arranged, but subequal radii similar to those upon the body of the 

shell.

There is a broad oblique cardinal' area with a shallow triangular 

cartilage pit beneath the beak, an arrangement which characterizes 

the genus Deltopecten.

The foregoing description is based upon specimens from New 

Mexico, chiefly upon the one which White described and figured 

under the identification Aviculipecten mccoyi Meek and Hayden. 

While related to Deltopecten mccoyi, there can be little question that 

the Western form is a distinct species. In the type specimen of 

D. mccoyi the primary radii are very nearly the same size as those of 

the second degree, so that it is not easy to distinguish them in some 

cases. The intervening radii are therefore larger and less numerous
PALEONTOLOGY. 87

than in D. vanvleeti. As many as 13 intermediate ones occur between 

the median principal radii in the Manzano specimens of D. vanvleeti. 

The scalelike spines are also much smaller and less conspicuous in 

typical D. mccoyi.

. On the other hand, after having had the privilege of comparing 

the Manzano specimens with the types of D. vanvleeti, I have been 

led to the conclusion that they belong to the same sp>ecies. In point 

of sculpture no constant or important differences have been detected. 

The fossils from Oklahoma show a wide variation in shape, a feature 

of which the range is scarcely indicated by my rather fragmentary 

material from New Mexico. I would judge that the Manzano specimens were round and erect and that the elongate varieties shown by 

Beede's figure 2a of Plate V and the oblique variety shown by his 

figure 2c of the same plate are not represented among them. I can, 

however, hardly do otherwise than refer my fossils to Beede's species.

This author seeks to distinguish D. vanvleeti from D. mCCOyi by the 

distance from the apex at which the enlarged costse are conspicuously 

developed. He names 15 to 20 mm. for D. vanvleeti and 3 to 5 mm. 

for D. mccoyi. In the original of his Plate XV, figure 2a, the primary 

ribs are abruptly enlarged at a point about 20 mm. from the beak, 

but this peculiarity does not appear in other specimens. In them and 

in the Manzano material alike the principal ribs can be traced as 

larger than the others well-nigh to the apex, but they begin to be what 

I should call conspicuously larger about 8 mm. from the apex. I am 

somewhat doubtful as to the importance of this character within the 

limits named for the discrimination of the two species. The real 

differences which in my estimation differentiate D. vanvleeti from 

D. mccoyi as based upon the type specimen, with which comparisons 

have been made, are given above. It is possible that Beede has in 

mind a false D. mccoyi, for in citing this species in 1900 he used 

White's figure of a specimen probably from the Manzano group which 

I regard as almost certainly identical with the other Manzano specimens (and also with D. vanvleeti) and distinct from typical D. mccoyi.

Horizon and locality. San Andreas formation, Elephant Butte 

(station 3600), San Andreas (station 3742), and Engle (station 

3740); Abo sandstone, Abo Canyon (station 3757a).

DELTOPECTEN COREYANUS White.

1874. Aviculopecten Coreyana. White, U. S. Geog. Surv. W. 100th Mer.; Prel. Rept.

Inv. Foss., p. 21. 

Carboniferous (Coal Measures): East of Mount Taylor, 1 mile south of Pajnata,

N. Mex. 

1877. Aviculopecten Coreyanus. White, U. S. Geog. Surv. W. 100th Mer., Rept., vol. 4,

p. 147, pi. 11, figs, la, b. 

Carboniferous: Bear Spring, near Camp Wingate, N. Mex. 

1895. Aviculopecten coryanus. Keyes, Missouri Geol. Surv., Rept., vol. 5, p. 113.

(Date of imprint 1894.) 

Upper Coal Measures: Kansas City, Mo.
88 MANZANO GKOUP OF EIO GEANDE VALLEY.

This fine species is abundant in the Manzano group, but is usually 

imperfectly preserved, much inferior in that respect to the specimens 

upon which the species rests. But little can be added to White's 

description. It is possible, however, to give some data regarding the 

right valve. This is considerably less convex than the left, but by no 

means entirely flat. It has almost the same shape as the other, the 

byssal sinus being not as deep as in some species. The surface I am 

inclined to believe is destitute of any radial markings but crossed by 

fine lines of growth, some of which are sublamellose.

White describes the sculpture of the left valve as consisting of fine 

radiating costse marked by fine radiating striae, but I am rather disposed to doubt that this is the real sculpture. Amongst the typical 

material one specimen, with fairly well-preserved surface, shows 

rather delicate concentric striae but no radiating ones on the ribs. 

The specimens which show this particular feature are more or less 

worn, so that the concentric lines are obscured, while the fine radiating striae have much the appearance of having been produced by 

delicate, probably discontinuous tubules in the substance of the shell 

which, brought to view by wear or exfoliation, give the semblance of 

fine liration superimposed upon the costae.

D. coreyanus proves to have a broad beveled cardinal area, with a 

triangular cartilage pit beneath the beaks. This structure is characteristic of the genus Limipecten, which I now believe to be a synonym 

of Deltopecten.

D. coreyanus will need to be compared with Walcott's Orenipecten TiaXlanus. The types of both species, but especially of the 

Nevada form, leave the observer in doubt upon many points, but my 

comparisons seem to show that the two are extremely similar in 

specific characters. -

The broad hinge plate Of C. TiaTLanus bears transverse crenulations, 

a character not observed on Deltopecten coreyanus, but I have come 

to doubt whether this character of a crenulated hinge may not after 

all be an individual peculiarity or the result of some circumstance 

of preservation. A parallel case may be found in the genera Per.nipecten and Entolium, the former of which has a crenulated hinge and 

the latter not. Weller has made Entolium a synonym of Pernipecten, 

and I am adopting the same course. If in the case immediately under 

consideration the difference in the character of the hinge plate can 

for one reason or another be passed over, it appears probable at 

present that Orenipecten hallanus will prove to be a synonym of 

Deltopecten coreyanus.

Deltopecten coreyanus appears to be rather closely related to the 

form recently described as Aviculipecten oklahomensis Beede. Some 

of the specimens (all fragmentary) which I have placed with the 

former species resemble the latter in a striking manner. D. coreyanus
PALEONTOLOGY. 89

attains a size much, larger than any specimens of D. oldahomensis yet 

known, but despite this fact and the shape of the Oklahoma species, 

which if. not deformed by compression is considerably narrower, 

the two forms may yet prove identical. On the other hand, the 

small right valve which Beede figures as belonging to D. oklahomensis 

is very different in shape from the right valve which seems to belong 

to D. coreyanus. It appears to have the same characters as the right" 

valve of D. vanvleeti, and if it really belongs to D. olclaliomensis there 

can be little question that the latter is distinct from D. cor ey anus. 

In the Manzano specimens the right valves were in some cases found 

in natural position with the lefts, which, though badly exfoliated, 

seem to belong with D. coreyanus. Among the very imperfect Manzano fossils, some of which are probably identical with D. coreyanus, 

it may well be that more than a single species is included.

Horizon and locality Abo sandstone, Mesa del Yeso (stations

3751 and 3751a); Sandia Mountains (stations 3796, 3797, and 3798), 

and Abo Canyon (station 3757a?); Yeso formation, Mesa del Yeso 

(station 3751c) and San Andreas (station 3742d?); San Andreas formation, Mesa del Yeso (station 3751d) and Nogal Creek (station 3744).'

ALLEEISMA ,CAPAX Newberry.

1861. Allorisma capax. Newberry, Ives's Colorado Expl. Exped., Kept., p. 120, pi.

1, figs. 9-9a.

Upper Carboniferous or Permian limestone: Agua Azul, near base of Mount 

Taylor.

As at present known there is nothing to distinguish this form from 

A. terminale, save its rather more robust proportions, and especially 

the greater height in relation to the width. A. capax was described 

from the horizon of the Aubrey group and, as specimens usually occur, 

is badly preserved. It seems probable that when good specimens of 

both species can be. compared other differences will come to light in 

configuration or in sculpture.

Two types are found in the Allerismas of the Manzano group. 

They can be distinguished with reasonable ease on the basis of the 

proportion of length and breadth. The less slender ones with little 

question belong to A. capax, and reach a very considerable size. The 

largest could hardly have been less than 150 mm. in width.

Small and immature examples of this species resemble the form 

from the Rico formation which I referred with some hesitation to 

A. terminate,*1 and it may be that there, as well as in the Manzano 

beds, the two species occur in association. It should be noted, 

however, that as yet no mature typical examples of A. capax are 

known in the Rico.

Horizon and locality. Abo sandstone, Abo Canyon (station 3757a) 

and Yeso formation, Mesa del Yeso (station 3751c).

a Prof. Paper U. S. Geol. Survey No. 16,1903, PI. IX, fig. G.
90 MANZANO GROUP OF RIO GRANDE VALLEY.

ALLERISMA TERMINALE Hall.

1852. Allorisma terminalis. Hall, Stanbury's Exped. to Great Salt Lake, Kept., p.

413, pi. 2, figs. 4a, 6. 

Carboniferous: Big Blue River. 

1852. Allorisma regularis ? Owen, Geol. Surv. Wisconsin, Iowa, and Minnesota,

Eept., tab. 5, fig. 13.

Carboniferous: Missouri River at Wayne City. 

1858. Allorisma subcuneata. Meek and Hayden, Acad. Nat. Sci. Philadelphia, Proc.,

p. 263.

Upper Coal Measures: Leavenworth, Kans. 

1860. Allorisma ensiformis. Swallow, Acad. Sci. St. Louis, Trans., vol. 1, p. 656.

Coal Measures: Clay, Mo. 

1864. Allorisma subcuneata. Meek and Hayden, Smithsonian Cont. Knowledge, vol.

14, No. 172, p. 37, pi. 1, figs. 10a, b. 

Coal Measures: Leavenworth, Kans. 

1866. Allorisma subcuneata. Geinitz, Garb, und Dyas in Nebraska, p. 14.

Upper Coal Measures: Plattsmouth and Wyoming, Nebr.; Kansas. 

1872. Allorisma subcuneata. Meek, U. S. Geol. Surv. Nebraska, Final Rept., p. 221,

pi. 2, figs. 10a, 6.

Upper Coal Measures: Rock Bluff, 2£ miles southwest of Nebraska City, Wyoming, and Plattsmouth, Nebr.; Leavenworth and Atchison, Kans. 

Upper and Lower Coal Measures: Illinois.

1875. Allorisma subcuneata (var.). White-, U. S. Geog. Surv. W. 100th Mer., Rept.,'

vol. 4, p. 155, pi. 12, figs. 7a, b. (Whole report published in 1877.) 

Carboniferous: Near Agua Azul, N. Mex.

1876. Allorisma subcuneata. White, U. S. Geol. Geog. Surv. Terr., Second Division;

PowelPs Rept. Geol. Uinta Mountains, p. 91. 

Lower Aubrey group: Confluence of Grand and Green Rivers, Utah. 

1881. Allorisma subcuneata? White, Dept. Stat. and Geol. Indiana, Second Ann.

Rept., p. 518, pi. 8, figs, 1, 2. 

Coal Measures: Edwardsport, Knox County, Ind. 

1884. Allorisma subcuneata. White, Geol. Surv. Indiana, Thirteenth Rept., p. 148,

pi. 31, figs. 1-3. 

Coal Measures: Indiana.

1886. Allorisma subcuneata. Heilprin, Second Geol. Surv. Pennsylvania, Ann. Rept.

for 1885, p. 456, 457, fig. 10a; p. 444, fig. 10. 

Upper Coal Measures, Mill Creek limestone: Wilkesbarre, Pa.

1886. Allorisma subcuneata. Heilprin, Wyoming.Hist. and Geol. Soc., Proc. and Coll.,

vol. 2, pt. 2, p. 272, fig. 10; p. 276, fig. 10a. 

Upper Coal Measures, Mill Creek limestone: Wilkesbarre, Pa.

1887. Allorisma subcuneata. Herrick, Sci. Lab. Denison Univ., Bull., vol. 2, p. 34,

pi. 4, figs. 1, 2.

Coal Measures: Flint Ridge, Ohio. 

1895. Allorisma subcuneatum. Keyes, Missouri Geol. Surv., vol. 5, p. 129, pi. 47,

figs. 5a-c. (Date of imprint, 1894.) 

Upper Coal Measures; Kansas City, Mo. 

1900. Allorisma subcuneatum. Beede, Univ. Geol. Surv. Kansas, Rept., vol. 6, p.

169, pi. 20, figs. 1-lb. 

Upper Coal Measures: Westport (Missouri), Kansas City, Mont Ida (Anderson

County), Lawrence, Lecompton, Topeka, Elmont, Grand Summit, Kans. 

1903. Allerisma terminale. Girty,- U. S.'Geol. Surv., Prof. Paper No. 16, p. 437, pi. 9,

figs. 4, 5, 6. 

Hermosa and Rico formations: San Juan region, Colo.
PALEONTOLOGY. 91

This well-known species occurs quite plentifully in the Manzano 

group, but invariably in a poor state of preservation. The fossils so 

identified resemble A. capax, except that, they are distinctly and 

persistently narrower. It can not definitely be stated that they 

belong to A. terminale, but their shape, so far as can be told, is the 

same, and there is no reason for supposing that the other characters 

also would not be in agreement.

Horizon and locality. Abo sandstone, Sandia Mountains (station 

3798).

PLEUROPHORUS MEXICANUS n. sp.

Plate X, figure 1.

Shell large, very transverse. Greatest width about two and onehalf times the greatest height. Beak subterminal, slightly projecting. 

Cardinal line about two-thirds the entire width. Basal outline gently

rounded, bending upward behind, so that that portion is somewhat 

contracted. Posterior outline rather distinctly truncated in an 

oblique direction. In front the inferior outline curves strongly 

upward arid is withdrawn beneath the beak. The convexity is high; 

the umbonal ridge is strongly elevated, but not angular. A broad, 

obscure sinus or constriction marks off the anterior third of the shell.

The surface is crossed by fine concentric striae and coarser ones at 

more or less regular intervals. A strong angular costa passes backward nearly parallel to the hinge, probably demarking an elongate 

escutcheon, and a short distance from it another more obscure costa 

intervenes between this and the umbonal ridge, while' a third, hardly 

perceptible, one appears to be developed near the umbonal ridge 

itself.

Though several other fragmentary and immature examples have 

been provisionally referred to the same species, the foregoing description is based upon the type specimen alone.

Pleurophorus mexicanus is an unusually robust form, and appears 

to be most closely related to P. taffi, of the Carboniferous of Indian 

Territory. It differs from the latter species in having the anterior 

portion less extended and nasute, in contracting instead of expanding 

behind, and in having a less angular umbonal ridge.

This is possibly the species which Walcott described as ModiomorpJia? desiderata, but his specimens were so imperfect that a comparison can not be carried out. The anterior portion is shorter than 

in one of his types, and the postcardinal slope is costate, a feature 

which he does not mention and which perhaps could not be determined from his specimens.

A silicified right valve provisionally referred to this species shows 

some of the internal characters. The point of attachment of a nar-
92 MANZANO GKOUP OF EIO GRASTDE VALLEY.

row elongate ligament occurs just back of the umbo and.below the 

sharp angulation defining the escutcheon. A stout cardinal tboth 

with a socket immediately above it is situated just below the umbo. 

The anterior extremity was the site of a large anterior muscle whose 

scar is defined posteriorly by a high, strong ridge extending downward 

at right angles to the hinge line.

Horizon and locality. Yeso formation, Mesa del Yeso (station 

3751c); Abo sandstone, Sandia Mountains (station 3798?); San 

Andreas formation, Engle (station 3595).

PLEUEOPHORUS BIPARTITUS n. sp.

. Plate X, figure 2.

Shell of medium size, rather short and high. Outline subcuneate, 

somewhat contracting in front and abruptly truncated behind. 

Beak small and depressed. Anterior extremity moderately projecting; hinge line equaling about three-fourths the entire width.. The 

lower margin is convex, rounding gradually upward in front, where 

it is strongly retracted under the beak. Convexity rather high, especially toward the posterior portion. Umbonal ridge elevated into a 

coarse, strong costa, while another of about the same size lies between 

it and the hinge line, though somewhat farther from the latter. The 

anterior half of the shell is marked by broad concentric striae, leaving 

between them rather strong angular ridges. Apparently from the 

type specimen these do not pass beyond the umbonal ridge, but they 

may occur on the postcardinal portion and be somewhat fainter 

there.

This species is possibly identical .with one of the several forms 

which Walcott includes under Sanguinolites seolus in his'Eureka district report, especially figures 7 and 9 of Plate XX. Though some 

differences of configuration can readily be noted, especially about the 

anterior end, the general expression is certainly close. About the 

identity of the Manzano form with typical Sphenotus seolus there is, 

I think, call for little discussion. P. lipartitus also resembles Walcott's Sanguinolites retusus, but is a much more transverse species.

The type specimen is more or less of an internal mold, but seems to 

show the specific characters with reasonable clearness. A second, 

still less well-preserved specimen is also known, agreeing in all respects 

with the other so far as can be determined.

Besides the three types of Pleurophorus specifically mentioned in 

this report, there appear to be representatives of several other species 

of the same genus, but too imperfect for description.

Horizon and locality. Abo sandstone, Mesa del Yeso (station 3751).
PALEONTOLOGY. * 93

PLEUROPHORUS aff. TAFFI Girty.

This species is represented by some very imperfect and some immature examples. The largest specimen had a width of at least 55 mm. 

Its convexity is low and its umbonal ridge not strongly marked, but 

the specimen has evidently been more or less crushed. Another 

example referred here shows only the anterior portion, which is 

more strongly produced even than in P. tqffi. A third example is 

immature, with a rather prominent umbonal ridge and strongly projecting anterior extremity. None of the specimens examined seems 

to have any costse developed on the postcardinal slope save an, angular 

ridge near the cardinal line, presumably marking the limit of an 

elongated escutcheon.

This form suggests the species described by Walcott as Modiomorpkaf desiderata, but both are too imperfectly known to permit a 

determination of their relationship.

Horizon and locality. Yeso formation, Mesa del Yeso (station 

3751c) and San Andreas (station 3742b); San Andreas formation, 

Mesa del Yeso (station 3751d); Abo sandstone, Abo Canyon (station 

3757a?) and Sandia Mountains (station 3797?).

PLEUROPHORUS aff. MEEKI Walcott.

This species is represented by four imperfect silicified specimens, 

the largest of which is 10 mm. wide or about half the size of the type 

specimen. They are characterized by very small and very nearly 

terminal umbones and by a smooth surface devoid of costse. In this 

they are very suggestive of Walcott's species, but whether they 

expand as strongly toward the posterior end can not be determined. 

Apparently they do not. v

They also resemble Modiola subelliptica of the Pennsylvanian fauna, 

a species which should be carefully compared with P. meeki.

Horizon and locality. Yeso formation, Alamillo (station 3751e).

PLEUROPHORUS aff. OBLONGUS Meek.

Here belongs a single specimen having much .the general appearance of P. oblongus, though about twice the size. The anterior end 

is imperfect, so that a comparison of this part is impossible. The 

shape only moderately transverse, it would appear, expands behind, 

where it is subtruncated. The umbonal ridge is distinct, though not 

angular. There is perhaps a costa, extremely obscure, between the 

umbonal ridge and the hinge line, somewhat nearer to the latter.

This form also resembles P. tropidophorus, but seems to show 

stronger resemblance with the species named above, since it expands 

more strongly behind, has not an angular umbonal ridge, and has 

the postcardinal costa, if present at all, less distinct.

Horizon and locality. Abo sandstone, Abo Canyon (station 3757a).
94 MANZANO GROUP OF RIO GRANDE VALLEY.

PLEUROPHORUS aff. SUBCOSTATUS Meek and Worthen.

Under this title is included a group of forms which might prove 

rather heterogeneous if its constituents were less imperfect. All that 

it seems necessary to say of them at present is that, so far as can be 

told, in size and proportion they seem to resemble Meek and Worthen's species rather closely.

Horizon and locality. Yeso formation, Blackinton's ranch (station 

3750) and'Carthage (station 3753); San Andreas formation, Mesa del 

Yeso (station 3751d?); Abo sandstone, Abo Canyon (station 3757a?).

ASTARTELLA SUBQUADRATA n. Sp.

Plate X, figures 10-13.

Shell small, subquadrate, width and height sometimes almost equal, 

the width being, however, always slightly greater. Cardinal margin 

and lower margin gently curved, more or less distinctly contracting 

behind. Posterior outline nearly perpendicular to the upper and 

lower margins; gently convex, rounding into the lower margin, but 

meeting the upper one in an obscure angle. Beak small. Below it 

the outline is concave, extending downward and somewhat forward 

for about two-thirds or three-fourths the length of the shell. It then 

meets the upward-curving anterior end of the lower outline, usually 

in a rather distinct angle. Convexity low. No appreciable umbonal 

ridge.

The sculpture consists of regularly arranged concentric lamellae, of 

which 6 to 8 occur in 3 mm., though the number varies according to 

the size of the shell, since upon the same specimen the distance 

between the lamellae increases regularly from beak to margin.

In its small size and less transverse shape this species most resembles Astartella gurleyi, but it differs in a number of points. A. gurleyi 

usually expands posteriorly instead of contracting in that direction, 

and the anterior extremity is rounded and not pointed. The convexity is considerably greater, and there is a more or less distinct 

umbonal ridge. The characteristic concentric lamellae are also much 

more closely arranged, being, when compared with A. subguadrata, 

about in the ratio of two to one.

Horizon and locality. Yeso formation, Alamillo (station 3751e) and 

Fra Cristobal (station 3743b); San Andreas formation, Mesa del 

Yeso (station 375Id?). 
PALEONTOLOGY. - 95

SCAPHOPODA. 

DENTALIUM MEXICANUM n. sp.

Plate XI, figure 10.

Shell rather large; length not determined; greatest diameter observed 7 mm. Straight, very gradually tapering. Sculpture, consisting of longitudinal costae, from 25 to 30 in number, which are 

obscure, broadly rounded, and separated by shallow, narrow striae. 

Transverse striae fine or absent upon the younger portion, but the older 

portion has well-developed transverse striae, due to irregular growth. 

They are distinctly oblique. The intervening spaces have obscure 

striae running lengthwise of the shell, but they do not produce continuous costae.' The general effect is of costae finer and much more

numerous than upon the younger portion.

The characters of the older parts of the shell are not taken from the 

type specimen, but from an associated fragment supposed to belong 

to the same species. Other large fragments show only irregular incremental striae.

This form is more closely related to D. acutisulcatum and D. sublseve 

than to any other American species. It appears to be straight and 

not curved, and consequently differs from both in this particular. 

Furthermore, the ribs are more numerous than in D. acutisulcatum, 

and instea'd of consisting of sharp ridges with rounded striae the ridges 

are rounded and the striae narrow and angular. Growth lines seem 

to be wanting over, all but the older portions of the shell. Similar 

differences exist between D. 'mexicanum and D. sublseve, which closely 

resembles D. acutisulcatum.

Horizon and locality. San Andreas formation, Caballos Mountains 

(station 3738a) and Fra Cristobal (station 3743).

PLAGIOGLYPTA CANNA White.

Plate XI, figure 11.

1874. Dentalium canna. White, U. S. Geog. Surv. W. 100th Mer.; Prel. Kept. Inv.

Foss., p. 23. 

Carboniferous (Coal Measures): Near Salt Lake, N. Mex., and near Relief Spring,

Ariz. 

1877. Dentalium canna. White, U. S. Geog. Surv. W. 100th Mer., Rept., vol. 4, p.

156, pi. 12, figs. 6a, b.

Carboniferous: Near Salt Lake, N. Mex., and near Relief Spring, Ariz. 

1903. Plagioglypta canna. Girty, U. S. Geol. Surv., Prof. Paper No. 16, p. 452. 

1908. Plagioglypta canna? Girty, U. S. Geol. Surv., Prof. Paper No. 58, p. 450, pi. 23,

figs. 11 to 13. 

Delaware Mountain formation: Guadalupe Mts., Texas.
96 MANZANO GROUP OF RIO GRANDE VALLEY.

Though described by White as curved and marked by obscure 

longitudinal ribs, I am satisfied that P. canna was straight and 

without longitudinal markings. This is true both of the type specimen and of the material found in the present collection. It appears 

probable that he may have observed the longitudinal striae upon a 

specimen of Dentalium mexicanum, which occurs associated with P. 

canna in the Manzano group and doubtless elsewhere too. The type 

specimen of P. canna, so far as I can observe, is entirely without 

them. In the present collection silicified specimens show no traces 

of longitudinal costae, though delicate transverse lines and striae are 

obvious. In general appearance this form is almost like Dentalium 

mexicanum, which occurs in the same fauna, though of course when 

well preserved the costae of D. mexicanum afford a ready means of 

discrimination. In the case of internal molds it is hopeless to distinguish them. Some specimens show striae upon the interior, but as 

they are only local it is doubtful whether even specific importance 

can attach to them. In both species probably the shell is distinctly 

thicker toward the apex than toward the aperture, consequently 

internal molds taper more rapidly than the shell itself.

The hypothesis that the more slender portions of D. canna may 

bear costae, so that P. canna and D. mexicanum are founded upon 

different portions of the same type of shell, may be dismissed at once, 

since specimens of P. canna, even when very small, are entirely 

smooth, save for growth lines.

Horizon and locality. Abo sandstone, Sandia Mountains (stations 

3796 and 3797) and Mesa del Yeso (station 3751?); San Andreas 

formation, Mesa del Yeso (station 375Id), Nogal Creek (station 

3744?), and Engle (station 3595); Yeso formation, Ala-millo (station 

3751e) and Mesa del Yeso (stations 3751a and 3751c),

GASTEROPODA. 

PHANEROTREMA MANZANICUM n. sp.

PL XI, figures 3 and 4.

Shell of medium size, turreted, consisting of about seven volutions. 

Volutions angular, with depressed sutures. The upper third of the 

external portion of each volution is nearly flat and directed obliquely 

downward at an angle of about 60° from the axis. This upper portion is terminated by a carina, whose top is channeled and contains 

the slit band, which is bounded above and below by the sharp elevated 

edges. The remaining two-thirds of the outer half of the peritreme 

is marked by angular revolving lirae, about 10 in number, separated 

by broadly rounded striae. The latter gradually diminish in width 

toward the umbilicus, and that immediately below the carina is con-
PALEONTOLOGY. 97

spicuously wider than any of the others. It is also wider than the 

carina itself. The volutions are deeply embracing, the upper edge 

of one falling upon the first lirse below the carina or a little lower. 

There is no other sculpture than this, except obscure incremental 

lines, which are slightly deflected backward, both above and below 

the carina. These are not strong enough to produce nodes or crenulations upon the'lirse.

Umbilicus nearly closed. Inner lip practically undeveloped. 

Aperture subrhombic.

A single specimen referred to this species has* the upper surface 

(that between the suture and the carina) divided about midway by a 

distinct revolving lira.

After reviewing with some care the Carboniferous Pleurotomarioids 

hitherto described from North America, no doubt remains that this 

is a new species. In fact, I find it hard to name a species which is

closely related to it. It differs from a large number in having the 

upper surface of the peritreme without sculpture and in having upon 

no part of it those transverse lines which in so many forms produce 

nodes or crenulations upon the revolving lirae. Phanerotrema 

marcouianum is perhaps the most closely similar, but the differences 

mentioned exist also between it and P. manzanicum. The latter has 

a somewhat higher spire' and is a much larger shell.

Horizon and locality. Yeso formation, Alamillo (station 3751e) 

and Abo sandstone, Sandia Mountains (station 3796?).

PHANEROTREMA aff. BRAZOENSE Shumard.

This type is represented in our collection by a small, imperfect, 

silicified specimen. The characters shown are as follows:

Size small, about 7 mm. in height, somewhat less in diameter. 

Spire low, rapidly enlarging, deeply turreted. The outer portion 

of the volution is subquadrate in section. The upper surface is 

nearly flat and perpendicular to the axis, with a raised band just 

below the suture marked by a row of large nodes. The lateral 

surface is about as wide as the upper surface and nearly vertical. 

These two portions are separated by a thin, laterally directed carina 

of extraordinary prominence. It constitutes the peripheral portion of the shell and gives the lateral surface a concave, somewhat 

retreating effect." The junction of the lateral and inferior surfaces is 

also subangular. The inferior surface is gently convex, rounding 

rapidly inward, so that the three divisions are approximately equal in 

height. The lower surface is marked by nine sharp, strong revolving 

lirae, separated by intervals considerably wider than themselves, and 

they apparently tend to degenerate into rows of nodes near the umbilicus, which is small and open. Two or three fine lirse are developed 

84259 Bull. 389 09 7
98 MAETZANO GROUP OF RIO GBANDE VALLEY.

on the lateral surface. The lower portion of the peritreme, and possibly the upper also, seems to be crossed by fine sublamellose growth 

lines, which tend to produce crenulations on the revolving lirse. Each 

volution embraces the lower half of the preceding one up to the angulation which defines the lateral and lower surfaces.

Though very suggestive of P. Irazoense, this form differs in having 

the upper surface much less elevated and the carina more prominent.

Horizon and locality. San Andreas formation, Caballos Mountains 

(station 3738).

 WORTHENIA ALAMILLANA n. sp. 

Plate XI, figure 5.

Shell rather small, subconical, consisting of seven or eight gradually 

enlarging volutions. Spire about equal in height to the final chamber. 

Volutions carinated along the peripheral line, which is slightly above 

the middle, though in the spire the carina occurs a short distance 

above the suture. The outer surface above the carina is strongly 

oblique and slightly sinuous, being convex above, near the suture, and 

concave below, near the carina. The lower surface is gently convex.

The upper surface between the carina and suture is nearly smooth, 

marked, however, by fairly distinct, fine, closely arranged, regular 

transverse costse. A sharp lira passes around the peritreme just 

above the carina, defining with the latter a narrow rounded channel, 

but with this exception the upper surface seems to be without revolving lines. A rather wide sulcus, somewhat wider than the carina, 

occurs just below the latter, but beneath it the surface is regularly 

crossed by rather coarse, rounded stride and lirse of about equal size, 

nine or ten of each. The aperture is strongly oblique and subrhombic 

in shape. The inner lip is somewhat thickened.

This form rather resembles PJianerotrema manzanicum, with which

it is associated, but many differences besides the more elongate shape 

are disclosed by a detailed comparison.

Worthenia alamillana has a higher spire than either W. tabulata or 

W. subscalaris and a lower spire than W. marcouiana. In some 

respects it resembles the latter species not a little, but besides the configuration, which has already been mentioned, there are other differences, such as the complete covering by striae of the lower part of the 

whorls in W. alamillana.

Of the American species usually placed under Pleurotomaria few 

resemble the present form closely in configuration, and from these the 

absence of revolving lines on the upper half of the volutions will prove 

a distinguishing character.

This form resembles Beede's MurcJiisonia collingsworthensis, but 

is at once distinguished by having the lower portion of the volutions 

striated.

Horizon and locality. Yeso formation, Alamillo (station 3751e).
PALEONTOLOGY. 99

MURCHISONIA ? TEEEBEA White.

1879. Murchisonia terebra. White, U. S. Geol. Geog. Surv. Terr., Bull., vol. 5, p. 219. 

Carboniferous: Wild Band Pockets, northern Arizona, 15 miles south of Pipe 

Spring. - "

1880. Murchisonia terebra. White, U. S. Geol. Surv., F. V. Hayden in charge; Cont.

Inv. Pal., Nos. 2-8, p. 139, pi. 34, fig. 4a. 

Upper Carboniferous: Wild Band Pockets, northern Arizona, 15 miles south of

Pipe Spring. 

1883. Murchisonia terebra. White, U. S. Geol. Geog. Surv. Terr., Twelfth Ann. Rept.,

'for 1878, pt. 1, p. 139, pi. 34, fig. 4a. 

Carboniferous: Wild Band Pockets, northern Arizona. 

1895. Murchisonia terebra.. Keyes, Missouri Geol. Surv., vol. 5, p. 146, pi. 49, fig. 4.

(Date of imprint 1894.) 

Upper Coal Measures: Kansas City, Mo.

The best specimen referred to this species is an internal mold, but

the identification is made with some confidence. In the general

shape of the: whole, as well as in that of the whorl section, it agrees 

very closely with White's figure. The imprint of crenulations along 

the carina is shown in the clearest manner, but the spiral lines upon 

the upper part of the peritreme are not retained.

Horizon and locality. Abo sandstone, Sandia Mountains (station 

3796?); San Andreas formation, Caballos Mountains (station 3738?); 

Yeso formation, San Andreas (station 3742d).

MUECHISONIA? aff. TEREBRA White.

This form is represented in our collection by five or six specimens, 

but is still very imperfectly known. It closely resembles M. terebra, 

but for the following reasons I have been unwilling to identify it with 

that species. The spire seems to be more rapidly tapering, but as my 

specimens are fragments, or in some cases somewhat compressed, 

this can not be stated definitely. The volutions appear to have 

much the same shape as in White's species, with a strong carina at a 

point three-fourths to two-thirds the distance down from the upper 

suture, the surfaces above and below being fiat and oblique, but the 

carina is only obscurely nodose, if at all, and the surface above the 

carina is smooth, instead of marked by revolving lirse.

Horizon and locality. San Andreas formation, Mesa del Yeso 

(station 3751d), Caballos Mountains (station ( 3738?), Nogal Creek 

(stations 3744 and 3744a), and Fra Cristobal (station 3743); Yeso 

formation, San Andreas (station 3742d).

EUPHEMUS SUBPAPILLOSUS White.

1876. Bellerophon carbbnarius var. subpapillosus. White, U. S. Geol. Geog. Surv.

Terr., Second Division; Powell's Rept. Geol. Uinta Mountains, p. 92. 

Upper Aubrey Group: Beehive Point, near Echo Canyon, and near Echo Park, 

Utah.
100 MANZANO GROUP OF EIO GRANDE VALLEY.

1879. Bellerophon subpapillosus. White, U. S. Geol. Geog. Surv. Terr., Bull.,'vol.

5, p. 218.

Carboniferous: Wild Band Pockets, northern Arizona, 15 miles south of Pipe 

Spring.

1880. Bellerophon subpapillosus. White, U. S. Geol. Geog. Surv. Terr., Contributions to Paleontology Nos. 2-8, p. 138, pi. 34, fig. 3a. 

Upper Carboniferous: Northwestern Colorado and northern Arizona. 

1883. Bellerophon subpapillosus. White, U. S. Geol. Geog. Surv'. Terr., Twelfth Ann.

Kept, for 1878, pt. 1, p. 138, pi. 34, fig. 3a.

Upper Carboniferous: Northwestern Colorado and northern Arizona. 

1899. Euphemus subpapillosus. Girty, U. S. Geol. Surv., Nineteenth Ann. Rept. ?

pt. 3, p. 592.

1903. Euphemus subpapillosus? Girty, U. S. Geol Surv., Prof. Paper No. 16, p. 476. 

Bellerophon limestone: Diamond Peak, Uinta Mountains, Colo.

This very characteristic fossil was obtained in considerable abundance at several points in the Manzano group, but most of the specimens are imperfectly' preserved. It can readily be distinguished 

from E. carlonarius. The revolving costss are fewer and farther 

apart, and near the aperture develop into rows of nodes. The slit 

band, instead of being occupied by two or three of the costae, is 

smooth and defined upon each side by one of them.

Horizon and locality. San Andreas formation, Engle (station 

3740); Yeso formation, San Andreas (station 3742d) and Fra Cristobal (station 3743b?); Abo sandstone, Sandia Mountains (station 

3797?).

EUPHEMUS INSPECIOSUS White.?

1881. Bellerophon inspedosus. White, U. S. Geog. Surv. W. 100 Mer., Kept., vol. 3,

Supp. Appendix, p. xxx, pi. 4, figs. la-d. 

Carboniferous: Near Taos and at Taos Peak, N. Mex.

1889. Euphemus inspedosus. Girty, U. S. Geol. Surv., Nineteenth Ann. Kept., pt. 3, 

p. 592.

Only a small number of specimens belonging to this species have 

been found, and they are of rather doubtful affinity. E. carbonarius 

and E, subpapillosus may be dismissed from the comparison without 

comment. While of about the same size as E. nodicarinatus or a 

little smaller, they are narrower and lack the node-bordered slit band 

on the smooth outer lip. They are of course much smaller than E. 

inspedosus, and do not show the irregular curvature which characterizes that species. The irregular curvature, I am inclined to believe, 

is a character of the mature shell not found in the earlier stages, and 

the present specimens are referred to White's species on the hypothesis that they are immature.

Horizon and locality. Yeso formation, Alamillo (station 3751e) 

and Mesa del Yeso (station 3751c); San Andreas formation, Nogal 

Creek (station 3744a?) and Engle (station 3595).
PALEONTOLOGY. 4 101

BELLEBOPHON MAJUSCULUS Walcott.

Plate XI, figure 2.

1884. Bellerophon majusculus. Walcott, U. S. Geol. Surv., Mon. 8, p. 256, pi. 23,

figs. 1, la; pl.-24, fig. 6. 

Lower Carboniferous: Eureka district, Nevada.

Under this title are included a large number of Manzano specimens, 

but as many of them are internal molds the identifications are provisional. What is regarded as the typical form, as shown by the 

best preserved specimens, possesses the following characters. The 

size is large, but in no instance equal to that of the specimens upon 

which the species was based, and in most cases much smaller. The 

peritreme enlarges gradually and is not much expanded at the 

aperture. The umbilicus is only partially closed, at least in young 

specimens, by a fold of the shell. The section is somewhat narrow 

and helmet shaped, contracting rather gradually to the keel-like 

slit band. The surface is marked by not very distinct, regular, 

closely arranged ridges, whose direction follows that of the growth 

lines. They are sometimes nearly transverse, but at others, particularly, it may be, in young specimens, they are strongly bent 

backward on approaching the band.

This species is closely related to B. crassus, and is chiefly distinguished by the more pointed and highly carinated dorsum. As 

both forms vary a good deal, not only as individuals but at different 

stages of growth, it is doubtful whether the other differences which 

have been noticed, such as the character and direction of the sculpture, 

will be found valid. The other characters, however, appear to be 

independent of stages of growth.

Although my specimens are smaller, often much smaller, than 

those from Nevada upon which the species was based, I can not but 

make the identification with some confidence. They seem to agree 

with B. majusculus in just the points in which they differ from B. 

crassus.

Horizon and locality. San Andreas formation, Engle (stations 

3595 and 3740a), Elephant Butte (stations 3600 and 3741), San 

Andreas (station 3742), Fra Cristobal (station 3743), Nogal Creek 

(station 3744), Mesa del Yeso (station 375Id), and Caballos Mountains (station 3738a); Yeso formation, San Andreas (stations 3742d 

and 3742g) and Mesa del Yeso (station 3751a, 3751b, and 3751c); 

Abo sandstone, Mesa del Yeso (station 3751) and Sandia Mountains 

(station 3797).
102 MANZANO GROUP OF RIO GRANDE VALLEY.

PATELLOSTIUM aff. NODICOSTATUM Gurley.

Our collection contains nine specimens of this species, but they are 

so poorly preserved, retaining only here and there patches of the 

shell, that nothing but an imperfect description can be given. The 

peritreme is rather rapidly expanding, transverse, broadly rounded 

across the dorsum-. Slit band sharply defined but not much elevated. 

Outer lip deeply notched.

Sculpture consisting of fine revolving lirse, about 12 in 10 mm., 

which are subequal or slightly alternating, separated by narrow, 

rather indistinct striae. These are crossed by transverse undulations, 

which are regular, closely arranged, and when the surface is well preserved apparently angular. They occur usually about 6 or 7 in 5 mm. 

They vary somewhat in direction, being in some specimens nearly 

straight, in others strongly curved, and they are always more or less 

bent backward near the slit band. The revolving lirse sometimes 

produce nodes as they cross the transverse ridges.

It is hardly probable that this is the same form which occurs in the 

Eureka district and was there identified by Walcott as BelleropJion 

textilis?

Horizon and locality. Abo sandstone, Sandia Mountains (station 

3796) and Abo Canyon (station 3757a); San Andreas formation, 

Mesa del Yeso (station 3751d); Yeso formation, Mesa del Yeso 

(station 3751a).

MOGULIA? Sp.

The subject of this sketch is a single small specimen, silicified, and 

partially freed from matrix. It seems rather probable that the present characters, so far as they are observable at all, are true to the 

original condition, from which probably little has been lost or altered 

in course of fossilization. The fact, therefore, that the specimen is 

entirely smooth, without transverse or revolving striae and without 

a visible slit band, invests it with unusual interest. The section 

would be regularly and strongly rounded across the dorsum, the volutions rather rapidly expanding in the same plane. The aperture was 

probably sublunate, transverse. The inner lip was not thickened. 

The outer lip, unfortunately, is.broken, so that in the absence of any 

distinct growth lines its shape can not be even inferred. It projected 

at the sides and was much thickened, producing a solid axis and 

obscuring any trace of an umbilicus.

So far as can be determined the generic affinities seem to be partly 

with Mogulia, and partly with Warfhia, and the decisive evidence of 

the shape of the outer lip is unfortunately wanting. The shell has the 

general aspect, the solid axis, and the laterally projecting outer lip of 

Mogulia, but lacks the transverse plications of that genus, which 

follow the growth lines and betray the shape of the lip. In its lack of
PALEONTOLOGY. 103

sculpture it is like Warihia, but has the lateral expansion of the outer 

lip which is so common in other Bellerophons, but which seems to be 

absent in the Indian genus.

Horizon and locality. San Andreas formation, Caballos Mountains 

(station 3738a).

BUCANOPSIS MODESTA n. Sp.

Plate XI, figure 1.

Shell small, the largest specimen examined having a diameter of 9 

mm. Peritreme rather rapidly expanding, transverse, broadly 

rounded over the dorsum. Aperture sublunate. Outer lip not flaring. Slit narrow and deep. Umbilicus open. Inner lip imperfectly 

developed.

Slit band rather broad, not sharply defined, slightly elevated. Surface marked by fine revolving lirse, about 10 in 3 mm., which vary 

somewhat in appearance, being now apparently slender and somewhat widely separated, and now broader and more closely arranged. 

These varying appearances are probably due to preservation. There 

are also fine, obscure, transverse lines, which are chiefly visible upon 

the slit band.

I am not altogether satisfied that this form is an undescribed species, 

but it unfortunately happens that most of the types with which it 

would be desirable to compare it have not been figured, and it is 

impossible to make satisfactory comparisons with the descriptions 

alone. B. marcouiana, from figures of Geinitz;s fragmentary specimen, appears to be a distinct species, by reason of the different shape 

of the peritreme. The Mississippian species B. textilis is very suggestive, but has not so broad a whorl section.

It seems hardly probable that these are young examples of the form 

identified as Patellostium afL nodicostatum, as the liration is finer and 

the transverse costse are absent.

Horizon and locality. San Andreas formation, Caballos Mountains 

(station 3738a) and Abo sandstone, Abo Canyon (station 3757a?).

EUOMPHALUS aff. PERNODOSTJS Meek and Worthen.

This form is represented in our collection by fragments of one 

rather small specimen. It was found associated with Euomphalus 

sp. a; but while the latter species has nodes upon the upper surface 

the present one as clearly has them upon the lower, and therefore 

it resembles E. pernodosus. Whether it can definitely be identified 

with E. pernodosus can hardly be determined from the material at 

hand.

The Manzano specimen had a diameter of about 25 mm. The 

upper surface was probably nearly fiat, or slightly concave, the lower
104 MANZANO GROUP OF RIO GRANDE VALLEY.

broadly and somewhat deeply umbilicated. The upper surface of 

the peritreme was nearly plain, almost horizontal, slightly sloping 

downward from the outer margin, which was probably angulated, 

effecting a marginal or submarginal carina. The lower surface is also 

carinated about midway, the carina being marked by nodes 5 mm. 

apart. From the carina the lower surf ace'of the peritreme slopes 

upward rather symmetrically in either direction.

The characters thus briefly sketched indicate a species similar in 

a general way to E. pernodosus. So far as can be told, the lyianzano 

form has its upper carina more marginal and its lower one less marginal than the typical variety. Other specimens, however, might 

show that these characters are not constant or not quite as described. 

Considerable change also takes place with the growth of the shell, 

and the present seems to be an immature example.

Horizon and locality. San Andreas formation, Caballos Mountains (station 3738).

EUOMPHALUS sp. a.

This type is represented in our collection by two specimens, and 

although many of its characters can be determined so that it is without much question a new species, I hardly feel justified at present in 

introducing for it a new name. At first sight one would hardly fail 

to compare it with EuompJialus pernodosus, but a more careful examination shows that the nodes in the present instance are situated upon 

the upper instead of the lower surface. The size is large, at least 45 

mm. in diameter, the upper surface flat, or even slightly depressed. 

The under surface is scarcely known, but is probably broadly and 

deeply umbilicated. The volutions are about 5 or 6. They are flat 

above and descend gently toward the center. The'sides also are

flattened and nearly normal to the upper surface, with which they 

join in a pronounced angulation, marked at rather long intervals by 

large, moderately well-developed nodes. The latter are 8 or 9 mm. 

apart in one specimen, but are more closely arranged in the other. 

They are developed only upon the mature volution, premature and 

postmature whorls showing only the marginal angulation. The 

volutions overlap, so that the inner edge of the upper surface of 

one is a little lower than the outer edge of the upper surface of the 

other. The shape of the lower, portion of the volution is imperfectly 

known. The vertical lateral surface appears to be bent inward 

rather gradually until, about midway of the peritreme by an abrupt 

change of direction which results in a median carina, its course is 

inward and upward.

Horizon and locality. San Andreas formation, Caballos Mountains 

(station 3738), Nogal Creek (station 3744a?), and Elephant Butte 

(station 3741).
PALEONTOLOGY. 105 

EUOMPHALUS sp. &.

The species which is the subject of the following remarks constitutes a rather important feature of the Manzano fauna, but of the 

sundry specimens examined the majority are more or less completely 

reduced to the internal mold. Many are also fragmentary, and a few 

presumably belong to a small immature stage. The size is large, 

55 mm. or more in diameter, and in number of volutions 4 or' 5. The 

upper surface is gently and the lower surface deeply concave. The 

upper surface of the peritreme is marked by a strong angular carina, 

which in the younger volutions seems to be almost marginal, so that 

the upper surface is nearly flat and horizontal. In the older volutions 

it still tends to be marginal, but is situated nearer the center. The 

upper surf ace of the peritreme is then concave, and it descends strongly 

inward from the carina, which: is often considerably elevated above

the larval part of the shell. In these large volutions the lateral surface curves downward and slightly outward from the upper carina, 

then slightly inward, where it receives another abrupt deflection 

upward, thus producing a second carina on the lower surface, submarginal and more or less directly below that upon the upper surface. 

A sufficient extent of either the upper or the lower portion has not been 

observed to permit me to determine whether one or both of the 

carinae were nodose. So far as observed they were not, but may 

have had nodes at rather long intervals. The lower surface of the 

peritreme is nearly plane and strongly oblique. The peritreme section resulting from this configuration is strikingly triangular. '

The foregoing account is composite, made up from observations 

upon several fragments, but'it is probably true of most of the specimens placed in this group, rather, however, of the mature than of the 

younger stages. Still some of the fossils assembled here can not be 

definitely determined, for the carinae are produced by thickenings 

of the shell, which take up most of the inequalities of configuration 

and leave the internal mold almost circular in section. In some cases 

the carinse appear to have been hollow.

This form also seems to be an undescribed species, but the description which I have been able to compose is too incomplete and too 

open to question in some particulars to make the introduction of a new 

name desirable.

Horizon and locality. Abo sandstone, Sandia Mountains (station 

3797); San Andreas formation, Engle (station 3740a), San Andreas 

(station 3742f), Elephant Butte (station 3741?), and Caballos Mountains, (station 3738a?); Yeso formation, San Andreas (station 3742g).
106 MANZANO GROUP OF RIO GRANDE VALLEY.

NATICOPSIS DEFORMIS n. sp. 

Plate XI, figures 8, 9.

Shell small, globose. Volutions rapidly enlarging, ventricose, each 

one embracing almost the whole of the preceding, so that the spire 

projects little, and sometimes not at all, above the final whorl. In 

the largest specimen referred to this species, which has a height of 

12 mm. and a diameter very nearly the same, the final whorl is greatly 

inflated and irregular. It has broad, gently convex upper and lateral 

surfaces connected by more strongly rounded portions. The lateral 

surface abruptly turns upward at the oblique lower side, and is 

marked toward the margin by two angular plications, one about midway and the other some distance below. These plications may be 

due to crushing, but this does not seem to be the case. The surface 

is marked by fine transverse striae. In the smaller of the two figured 

specimens these are nearly perpendicular to the suture, or even are 

directed slightly forward. In the larger one they are directed 

obliquely backward.

I am not quite satisfied that the forms here distinguished as a new 

species are not in fact mere immature examples of that cited as 

Naticopsis aff. altonensis. In the smaller of the two figured specimens 

we note a slight sulcus just below the suture on the last volution. 

Otherwise, in the height of the spire, the direction of the growth lines, 

and in other points, it is very different from Naticopsis aff. altonensis. 

In the. larger specimen figured the direction of the growth lines is as 

in the species last mentioned, and, furthermore, the lirae are possibly 

somewhat fasciculated toward the suture. The spire appears to be 

much lower, but the last volution is not as deeply embracing as the

others, and if continued on in the same plane would leave a moderately high spire in'specimens the size of Naticopsis aff. altonensis.

No more than a passing reference is needed to other American species from which the present form is distinguished by its very low 

spire and inflated body whorl. Naticellall transversa Beede hardly 

needs to be named here, since while somewhat similar in configuration 

the sculpture is very different, and the spire distinctly higher.

Horizon and locality. Abo sandstone, Sandia Mountains (station 

3798) and Abo Canyon (station 3757a); San Andreas formation, 

Engle (station 3740a).

NATICOPSIS aff. ALTONENSIS McChesney.

Under this title are included two specimens; only one of them 

moderately perfect and well preserved. Both are much smaller than 

normal N. altonensis. The following brief account is taken from the 

better specimen:
PALEONTOLOGY. ' 107

The complete height was probably about 15 mm. The spire is low, 

about as in typical N. altonensis, the volutions rapidly enlarging, 

deeply embracing. The whorl section is elliptical, strongly oblique 

to the axis. The upper part of the peritreme just below the suture is 

flattened to a horizontal direction. The long lateral surface is also 

somewhat flattened, perhaps even slightly depressed above. It is 

oblique to the upper surface, which it joins in a distinct shoulder. 

The lower side is probably strongly and regularly rounded. The 

surface is marked by fine, regular liras, which are distinctly fasciculate 

on the upper half. Their direction is strongly oblique to the suture, 

from which they extend backward at an angle of at first about 45°. 

There are also fine, wavy, and irregular revolving striae on the lower 

half of the peritreme.

Naticopsis altonensis represents a rather distinct type among the

Ndticopsis forms of our American Carboniferous, by. reason not only 

of its. configuration and sculpture but because the shell as at present 

preserved is frequently of a brownish color, indicating either some 

peculiarity of composition or, somewhat more probably, as the color 

is apt to be superficial, an epidermis thicker or more persistent than 

that which occurs in other groups. This is the case with the Manzano 

specimens. The outer layer alone is brown, and when exfoliated 

contrasts strongly with the white shell beneath.

White cites Naticopsis altonensis also from New Mexico, but it is 

somewhat doubtful whether it is quite the same species or from the 

same horizon as the one under consideration.

The Manzano form is possibly the same species which Beede has 

recently described as Stropliostylus permianus, but his material is so 

imperfect that a determination of this point is not possible. The 

Manzano form appears to have a slightly lower spire and a higher, 

more laterally flattened body whorl, but as Beede's specimen is 

crushed and more completely reduced to an internal mold these 

differences may be misleading.

Horizon and locality. San Andreas formation, Mesa del Yeso 

(station 3751d).

ZYGOPLEURA aff. EUGOSA Meek and Worthen.

Our collection contains but a single specimen of this species, which, 

though poorly preserved, agrees closely in all its determined characters with the description and figures of Loxonema rugosum. White, 

has cited the same or a related species (as Loxonema rugosum} from 

Taos and Coyote Creek, New Mexico.

Horizon and locality. Yeso formation, Alamillo (station 3751e). 
108 MANZANO GROUP OF BIO CtBANDE VALLEY.

SOLENISCUS aff. ALTONENSIS Worthen.

Plate XI, figure 6.

1884. Macrochdlus sp.? Walcott, U. S. Geol. Surv., Mon. 8, p. 260, pi. 24, fig. 8. 

Lower Carboniferous limestone: Eureka District, Nev.

This species is represented in our collection by two specimens, 

but as they are internal molds for the most part, they form an 

unsatisfactory basis for comparison with species in the literature 

which have usually been described from testiferous examples. The 

present form is intermediate between the elongated and the subglobose species of the genus, and has little to characterize it. So 

far as can be determined it is related to several known forms, though 

I hesitate to identify it definitely with any of them.

One of those most closely resembling it is S. altonensis. In that 

species the point of greatest convexity is farther from the top of 

the peritreme, which gives to the volutions of the spire a less inflated 

appearance, and a slightly different shape to the whole. The same 

is true of S. Jiallanus, which is perhaps the same species as S. altonensis. 8. newberryi and 8. planus are alsp related, but appear to 

have a more elevated spire than the Manzano form. 

. The circumstance that the highest convexity of the volution in 

these specimens occurs so near the suture may be connected with 

their condition as internal molds and the thickening of the test, 

which usually occurs near the suture.

This is, with little question, the same form which Walcott identified 

from the Eureka district as Macrocheilus sp. ?

Horizon and locality. Abo sandstone, Abo Canyon (station 3757a).

SPILEKODOMA aff. MEDIALIS Meek and Worthen.

This species is represented in our collection by but two specimens. 

The better one, though otherwise excellently preserved, has the 

spire partly concealed by closely adhering chert. It is less than 

half the size, of the specimen figured by Meek and Worthen, but the 

shape is closely similar, especially to their apertural view, which 

seems to'be a little tilted, thus foreshortening the spire. My specimen has a lower spire than that shown in the opposite view of the 

type. The apertural view, which, in fact, corresponds rather badly 

with the other, is also somewhat more gibbous. Another related 

species, though also a much larger one, is S. intercalaris. The 

Manzano form is somewhat more gibbous and has a lower spire.

The second specimen, which is very imperfect, agrees with the 

first in everything except size. It is much larger, very nearly as 

large as the typical example.
PALEONTOLOGY. 109

The fossil under consideration has a fold or denticle on the columella near the lower extremity of the aperture, a feature which is 

rather characteristic of Soleniscus. Indeed, it is somewhat doubtful whether any but an artificial'line distinguishes Sphaerodoma from 

Soleniscus, as the two genera are at present recognized in the American Carboniferous faunas.

Horizon and locality. San Andreas formation, Caballos Mountains (station 3738a) and Engle (station 3595).

SPH^ERODOMA aff. TEXANA Shumard.

Plate XI, figure 7.

This form is represented by two specimens, one-of them in fairly 

good preservation. It seems to differ from 8. aff. medialis in being 

much smaller and rather more inflated. It is characterized by its 

low spire and gibbous body whorl, and in this particular suggests 

several described species, but perhaps is as near to White's identification, of S. texana as to any. , It is only about one-fourth the size of 

White's specimen, however, but otherwise agrees with it closely. 

Another species of the same general type, though greatly exceeding it in size, is S. primigenia. 8. ponderosa is likewise similar in 

configuration.

Like the specimen identified as Sphserodoma aff. medialis, the present one also has a denticle near the extremity of the columella.

Horizon and locality. San Andreas formation, Caballos Mountains 

(station 3738a).

ORTHONEMA.

The group of shells here assigned to the genus Orthonema was at 

first provisionally placed with Murchisonia, and it may even yet prove 

to be necessary to return them to the Pleurotomariidae. The carina 

in some examples of 0. socorroense has much the appearance of a slit 

band, and while it seems in reality to be a carina, a band may occur 

just below or even upon it. No structure definitely functioning as a 

slit band has, however, been discovered, while in their general appearance these Manzano forms are certainly more like the Orthonemas 

than any Pennsylvanian species of Murchisonia or Pleurotomaria.

i 

ORTHONEMA SOCORROENSE n. sp.

Plate XI, figures 12, 13.

Shell small, terete, elongate-conical. Height of a rather large 

specimen 15 mm., diameter at base 4 mm., volutions about 11. 

The sides of this gradually tapering shell are almost absolutely 

straight and smooth. The vojutions have a flat, oblique lateral 

face and, the upper edge of one being flush with the lower edge of the
110 MANZANO GKOUP OF BIO GEANDE VALLEY.

other, form a continuous surface from apex to aperture. The change 

of direction from lateral to inferior surface is abrupt. The inferior 

surface is gently convex and nearly normal to the axis, so that almost 

the entire height of each volution is seen. The angulation formed 

by the lateral and inferior surface is the position of a somewhat broad 

very low carina resembling a slit band, or, rather, its position is on 

the lateral surface just above the angulation. The volutions overlap 

only to the angulation, and consequently to the lower edge of the 

carina, so the latter is seen at recurring intervals, marking their junction, which otherwise might have been hardly visible. Aside from 

the carina, the volutions appear to have been without markings or 

sculpture of any sort. Even growth lines do not appear on the 

silicified specimens.

Figure 13 of Plate XI represents an extreme example, between 

which and the typical one there are intermediate gradations. The 

structure which in the typical variety has been referred to as a 

carina and is scarcely elevated above the general surface, in this 

specimen projects as a distinct ridge near the base of the peritreriie. 

It tends to appear as a spiral elevation throughout the whole length 

of the shell just above the suture.' The tendency of some of the 

whorls to have gently concave instead of flat lateral surfaces, and in 

some cases to meet the preceding one, not flush with its lower edge, but 

somewhat withdrawn beneath it, doubtless contributes to this effect.

The relation of this form to typical 0. socorroense is somewhat 

doubtful. At first I was disposed to regard it as a wholly distinct 

species, and perhaps it would have been at least preferable to give 

it rank as a variety. In many respects its relations to 0. socorroense 

are so close, however, that it seemed best for the present to consider 

it merely as a variation within normal specific limits. To a certain

extent this form may be said to be intermediate between typical 

0. socorroense and the much larger species designated Orfhonema-sp. 'a 

and Orihonema sp. &.

0. socorroense is closely related to 0. carbonarium, especially the 

variety with more projecting carina, but even so it is a less distinctly 

turreted, more evenly conical shell than 0. carbonarium, besides 

being much smaller, so that if of the same length it would have perhaps twice as many volutions.

This form is so much like 0. dozierense a that at first I was disposed 

to regard both as belonging to the same species. A detailed comparison, however, seems to indicate that they are really distinct. 

0. dozierense is based upon a smaller specimen, which if developed to 

the same size as 0. socorroense would have contained a considerably 

larger number of volutions. 0. socorroense has an appreciable carina 

at the junction of the lateral and inferior surfaces, and in some cases

a Beede, J. W., Kansas Univ. Sci., Bull., vol. 4, No. 3, 1907, p. 168.
PALEONTOLOGY. Ill

the carina is rather striking, while no such feature seems to be developed in 0. dozierense. Finally, the lower surface of 0. socorroense is 

smooth, while 0. dozierense has a revolving ridge or lira just below 

the angulations formed by the lateral and basal portions of the 

peritreme.

The irregular, strongly carinated variety of 0. socorroense resembles 0. texanum, but the lateral face of 0. socorroense is much flatter 

and the lower face deeper, and it is smooth instead of striated 

underneath.

Horizon and locality. Yeso formation, Alamillo (station 375le).

ORTHONEMA sp. a.

This species, which is best known from a fragmentary specimen, is 

somewhat similar to 0. socorroense in that the spire is elongate and 

terete, with but little to interrupt its almost continuous lateral surface. It is, however, very much larger and shows other differences 

as well, which indicate that it is a quite distinct species. In the present specimen the diameter of the last whorl is 15 mm. The lateral 

surface of the peritreme is very gently concave. Its junction with 

the lower surface is marked by a strong carina. The lower surface 

of the peritreme is gently convex and inclined but slightly to the axis 

away from the apex. The lateral surfaces of the volutions are, so 

far as observed, entirely without sculpture or markings of any sort, 

but the lower portion is crossed by 6 or 7 revolving striae, that below 

the carina being somewhat stronger than any of the others. The 

volutions overlap only to the carina, which is somewhat emphasized 

by the slightly concave lateral surfaces above and below.

This species also seems to be quite distinct from any described from 

the American Carboniferous, but my material is almost too imperfect 

to make the introduction of a new name justifiable.

While the foregoing description has been drawn from a specimen 

which though imperfect shows many of the superficial characters, 

there have been provisionally referred here a number of fragments 

more or less completely reduced to the condition of internal molds, 

some of which indicate a much larger size than the described specimen. 

The largest has a diameter of 33 mm., while the height from suture to 

suture is about 18 mm.

This form in some respects much resembles Orihonema texanum 

Beede. The prominence of the carina, which is greater than in 

0. socorroense, suggests 0. texanum, but the lateral surface is flatter. 

The lower surface is also striated, as in 0. texanum. On the other 

hand, if of the same size as Orihonema sp. a, 0. texanum would have 

two or three times as many volutions.

Horizon and locality. San Andreas formation, Mesa del Yeso (station 3751d) and Nogal Creek (stations 3744? and 3744a); Yeso 

formation, Mesa del Yeso (stations 3751a and 3751c).
112 MANZANO GROUP OF EIO GRAttDE VALLEY.

ORTHONEMA sp. I.

This species is represented by a single imperfect specimen, and is 

related to sp. a, though by no means to be considered identical with 

it. The specimen under consideration must have been, when complete, about 22 mm. long, the diameter at the base measuring 8 mm. 

Probably 10 volutions were present. The general shape of the shell 

is elongate, conical, but not regularly so, for the upper portion seems 

to have been more rapidly tapering than the lower, which is subcylindrical. The general shape of the whorls is as in Ortlionemal 

sp. a, the sides being gently concave, with the carina located where 

the lateral surface joins the lower one, this feature being more distinct 

upon the upper half of the. shell. No sculpture seems to have been 

present, and in this respect the present form differs from Orihonemal 

sp. a, in which the lower surface of the whorls is striated.

This also appears to be an undescribed species, but for the same 

reason as in other cases it has seemed best not to give it a new name.

Horizon and locality. San Andreas formation, Caballos Mountains 

(station 3738).

CEPHALOPODA.

ORTHOCERAS sp. 

Plate XII, figure 2.

Of this type our collection has furnished a single specimen preserving the living chamber and a few of the septal chambers below. 

The size is rather large and the taper rather rapid. The section is 

somewhat elliptical and the siphuncle distinctly eccentric. The 

smaller end is 20 mm. by 19 mm. in diameter. The longer diameter 

of the larger end must have been about 26 mm. The length of the 

fragment is 46 mm. On the smaller end the siphuncle is 12 mm. from

the farther side and 7 mm. from the nearer. It is. very small. The 

sutures are not straight, but have a well-developed, broad lobe upon 

what may provisionally be called the ventral side. It is this side 

near which the siphuncle is situated and upon which the flattening 

chiefly occurs. Upon the dorsal side the sutures are directly transverse, but laterally they naturally bend upward in process of-forming 

the ventral lobe. The normal height of the chambers at this size is 

4 mm., or one-fifth the larger diameter, as shown by the final chamber 

on the specimen as figured and by two imperfect detached chambers, 

but the chamber just below the living chamber is almost 8 mm., while 

there is some indication of another septum 22 mm. above that forming 

the base of what is here regarded as the living chamber. . This narrow 

groove upon the interior mold may indicate a septum, but is provisionally considered a varix of growth near the real aperture. At 

all events, the irregularity in the height of the chambers may probably
PALEONTOLOGY. 113

be interpreted as an indication that the specimen is mature, with a 

rather short chamber of habitation.

The specific relations of this form are in some doubt, but it may be 

said to be probably distinct from any of the species yet cited from 

our Western Carboniferous. By reason of its locality and horizon 

Marcou's Orihoceras novamexicanum would invite comparison; but 

Marcou's description and figure give very few of the really important 

characters. 0. novamexicanum is very much larger, however, and if 

the present specimen is indeed mature, it seems probable that it is a 

different species. Meek's 0. baculum is also similar in some respects. 

The siphuncle is larger and less eccentric.

Horizon and locality. Abo sandstone, Abo Canyon (station 3757a).

COLOCERAS MEXICANUM n. Sp.

Plate XII, figure 1.

Shell rather small, subglobose, rapidly expanding. Umbilicus of 

medium size. Diameter of type specimen about 55 mm., width at 

aperture about 35 mm., width of umbilicus 8 mm. Section subcircular or somewhat subquadrate. Umbilical shoulder distinct, the 

umbilical portions of the volutions being almost parallel to the 

axis. The sides are slightly flattened, contracting above and ro.unding 

gradually into the broad ventral surface, which is gently depressed 

or concave. .Surface smooth. Suture slightly sinuated. Indistinct 

lobes seem to occur upon the ventral and lateral surfaces, separated 

by equally obscure saddles, whose position is on the umbilical shoulder 

and the ventri-lateral shoulder. Height of the chambers 4 mm. 

Siphuncle situated below the middle, -about halfway between the 

middle and the dorsal surface.

This form probably belongs to the genus Coloceras, though the 

faintly impressed ventral surface and the presence of an obscure 

ventral lobe sustain some doubt on this point. C. mexicanum is certainly distinct from the two other American species, not only in possessing the two features just mentioned, but in being narrower as 

well.

Horizon and locality. Yeso formation, Alamillo (station 3751e).

TEMNOCHEILUS afL WINSLOWI Meek and Worthen.

The subject of this description is a single fragment having a closely 

quadrate section 35 mm. in both directions. The sides are straight 

and parallel. The ventral surface is gently convex. The dorsal side 

is concave for an undetermined distance, and runs upward rather 

strongly at the sides, making this surface on the whole more convex 

than the other. The umbilical shoulder probably not well defined. 

84259 Bull. 389 09 8
114 MANZANO GROUP OF RIO GRANDE VALLEY.

While the ventral and lateral surfaces are fairly distinct, they apparently do not meet in an angle. This line, however, is marked by 

a row of very large nodes, which are subcircular, somewhat elongate, 

basally at least, in the direction of revolution, and are probably 20 

mm. or more apart. The siphuncle is of medium size and is about 

7 mm. from the ventral border. The sutures are very nearly straight 

and very nearly transverse. There is perhaps a faint ventral lobe. 

The chambers are low, about 4 mm. in height along the ventral surface.

This form appears to be related to T. wnslowi, but is with little 

question distinct, one difference being the less transverse shape of the 

cross-section. The Manzano form is too incompletely known, however, to determine its relationship to other species. More perfect 

material would probably verify the foregoing description in the main.

Horizon and locality. Yeso formation, Blackinton's ranch (station 

3750) and Mesa del Yeso (station 375 Ic).

TEMNOCHEILUS aff. CONCHIFEKUM Hyatt.

This form, like the other, is represented by very fragmentary 

specimens, the following notes being taken from one of them:

The volutions appear to have been rather gradually enlarging, and 

but slightly embracing, so that the shape of the whole was discoidal, 

with wide umbilicus. The shape of the section is transversely elliptical, with a barely perceptible flattening of the sides. The width is 34 

mm. and the height 24 mm. The dorsal surface is impressed for 

about one-third the entire width. Indistinct traces of nodes have 

been observed along the obscure ventrilateral shoulder.

The character o'f the suture is not shown by the specimen furnishing 

the above data, and other examples too doubtfully belong to the 

same species to make it desirable to include here data derived from 

them.

This form suggests T. conchiferum in its section, but is a less rapidly enlarging species.

Horizon and locality . San Andreas formation, Nogal Creek (station 3744) and Yeso formation, Alamillo (station 3751e).

TEMNOCHEILUS sp. a.

The form included under this title appears to be closely related to 

the last, and may prove even identical with it when both come to be 

better known. The chief reason for distinguishing them has to do 

with the septa. In the best and most characteristic specimen 

referred to this division the height of the chambers is about 6 mm., 

or considerably more than in the other. The sutures are also more 

strongly curved. There is a distinct ventral lobe or sinus and a distinct lateral lobe, with saddles more or less well marked upon the 

ventrilateral and umbilical shoulders.
PALEONTOLOGY. 115

Not all the specimens referred here show nodes upon the ventrilateral shoulder, but, especially in the older whorls, those structures 

are largely taken up by the thickness of the shell, leaving often very 

indistinct elevations upon the internal mold, the condition in which 

most of our specimens are found.

Horizon and locality. Yeso formation, Mesa del Yeso (station 

3751a? and 3751c); Abo sandstone, Mesa del Yeso (station 3751?); 

San Andreas formation, Mesa del Yeso (station 375Id?).

DOMATOCERAS? sp.

This form is represented in our collection by .the merest fragments, 

but nevertheless seems of sufficient interest to warrant a brief mention. The shell was'probably rather small and the shape flat, discoidal, with large umbilicus (?). The section was tetragonal, with 

nearly flat sides and ventral surface. The sides converged toward the 

latter, and their abrupt junction with it is emphasized in the best 

fragment by a strong carina. The septa are closely arranged, the 

height of the chambers being 2 mm.

Horizon and locality. Yeso formation, Mesa del Yeso (station 

3751c).

OSTEACODA.

HOLLINA HERRICKANA n. Sp. ' 

Plate VIII, figures 10, 11.

Shell equivalve, subrhomboidal, nearly twice as wide as high. 

Dorsal border straight, two-thirds to three-fourths the entire width. 

Ventral border curved, subparallel to the dorsal, somewhat contracting toward the front and curving upward more and more strongly, 

so that the anterior cardinal angle is a right angle, or even somewhat 

rounded. The posterior end is obliquely truncated at an angle of 

about 120°. The higher and .thinner end of the shell is posterior. 

There is a large tubercle near the dorsal border a little anterior to the 

median line, and a considerably smaller tubercle somewhat farther 

from the dorsal margin and a little posterior to the median line. The 

two tubercles are separated by a deep sulcus. The median portion 

of the shell is occupied by a transverse ridge which seems to begin 

just below the large anterior tubercle, with which it is partially confluent, curving in its forward extension and following the outline so 

as to meet the dorsal margin behind the smaller tubercle, which it 

thus partially surrounds. In some cases it seems to be traceable 

around the anterior tubercle also, but it is depressed and indistinct. 

Near the margins there is a projecting platelike flange which extends 

from anterior to posterior cardinal border, but is narrower toward its 

ends. It is somewhat oblique to the plane of contact of the valves. 

The surface is smooth.
116 MANZANO GROUP OF RIO 'GRANDE VALLEY.

In some respects this species appears to be closely related to H. 

fcetoidea, especially in the topography of the shell. The shape, however, is different, and H.fo&toidea seems to lack the frill-like lamella 

which projects from H. Jierrickana near its margin. The English 

species H. radiata is also similar, but s.eems to be without the inflated 

ridgelike median portion which partially incloses the two tubercles. 

The projecting submarginal plate is broader and striated. Jones and 

Kirkby represent that structure as abruptly terminating on the posterior ejid, but although one or two of "the American specimens show a 

corresponding appearance it must in these cases probably be ascribed 

to breakage. Most similar of all, however, is II. emaciata from 

which it is distinguished by the extreme prominence of the ventral 

ridge and its continuation as such to the cardinal border behind the 

posterior tubercle. It seems to lack also the short ridge in the postdorsal angle and the rimlike border ascribed to H. emaciata. This is 

clearly a species of Hollina, resembling, perhaps, in its essentials, the 

Devonian II. Icolmodini rather than the Carboniferous species.

Horizon and locality. Yeso formation, San Andreas (station 3742d).

CYTHERELLA BENNIEI Jones, Kirkby, and Brady.

Plate VIII, figures 7-9..

1884. Cytherella Benniei. Jones, Kirkby, and Brady, Pal. Soc., Mon. British Foss. 

Biv. Entom. Carbf. form., pt. 1, No. 2, p. 70, pi. 6, figs. 3a, 6, 4a, b, 5a, 6; 

7a, 6; pi. 7, figs. I2a-d.

The shells referred to this species are rather small, seldom exceeding 1 mm. in diameter, very nearly elliptical, though occasionally 

with one end slightly narrower than the other. The convexity is 

low, thicker at one end, which is the wider end when difference of

width is developed. Surface smooth.

Two varieties of this species are already known from the American 

Pennsylvania!!, but the form under consideration is perhaps more 

nearly like the typical English form. It would be extremely difficult 

to point out constant' differentiating characters.

Horizon and locality. Yeso formation, San Andreas (station 3742d).

BAIRDIA OCCIDENTALIS n. sp.

Plate VIII, figure 6.

Shell very elongate transversely. Outline of dorsal border slightly 

sinuate. Ventral border convex, most strongly bowed in the middle. 

Anterior end bluntly rounded. Posterior end acuminate. Convexity high, so that the cross section is nearly circular. One valve 

strongly overlapping upon the straight border. Surface smooth.

This form differs from B. cestriensis, the only other American representative of the genus, but is extraordinarily similar to the Waverly 

species which Ulrich described as Pontocypris? acuminata, suggesting,
PALEONTOLOGY. 117

however, that it might be an elongated Bairdia. The Manzano form 

presents few differences from that found in Ohio, the most important 

which I am able to indicate being the more pointed anterior end of the 

latter. B. occidentals should perhaps not be considered as more than 

a variety of the other, but in view of their wide difference in geologic 

age it would be inexpedient to unite them completely.

Horizon and locality: Yeso formation, San Andreas (station 3742d).

ENTOMIS SHUMARDIANA n. sp.

Plate VIII, figures 4, 5. «

Shell small, subovate to subelliptical. Strorigly convex, distinctly 

thinner at one end, which is that having the greater height when 

any appreciable difference in height occurs. Dorsal border straight, 

ventral convex. A deep narrow sulcus begins a little below the

middle and extends to the dorsal border. On either side the inflated 

valve puffs up into two lobelike elevations. On the more convex 

side the elevations sometimes appear to be bluntly pointed, or, as it 

were, terminating in a little tubercle near the sulcus. The two valves 

are distinctly unequal, one overlapping the other along the ventral 

border, and to a certain extent at the ends. Surface smooth!

I am in some uncertainty as to the generic relations of this form 

'and also as to its orientation. The nuchal furrow suggests both 

Entomis and Primitia, by its strength perhaps the former more than 

the latter. While the present form is distinctly inequivalve, 

Primitia appears to have the two valves equal and Entomis nearly 

so. Typically Entomis is highly sculptured, though a group of 

smooth species is known. Perhaps the least important disagreement 

lies with Entomis. By analogy with both genera the border against 

which the furrow is directed is the dorsal. If the identification with 

Entomis is correct, the narrower, more inflated, possibly tuberculated 

end is anterior, since the tubercle of Entomis is said to be in front of 

the sulcus. It may prove desirable to withdraw shells of this5 type 

from Entomis into a distinct and possibly a new genus, because of 

their smooth surface and strongly inequivalve configuration.

No American species of Entomis are known from the Carboniferous, 

though an undescribed form from the Caney shale of Indian Territory 

appears to belong to that genus.

Two American species of Primitia resemble the form under consideration rather closely. I refer to P. cestriensis and P. simulans 

of the Kaskaskia. Both species are presumably more equivalve, and 

both have a flattened border or flange the like of which is not found 

in the Manzano form. They are also less inflated and less distinctly 

furrowed. P. simulans, however, though larger, is very similar in 

shape.

Horizon and locality. Yeso formation, San Andreas (station 

3742d).
118 MANZANO GKOUP OF EIO GRANDE VALLEY.

TRILOBITA. 

ANISOPYGE INORNATA n. sp.

Plate VIII, figure 12.

This species is founded upon the pygidium, of which the following 

description can be given.

Shape subtriangular, strongly convex, slightly wider than long. 

Lateral outlines gently convex, meeting behind in a bluntly rounded 

angle. Axis strongly elevated, sharply defined, extending almost 

to the posterior outline. Axial segments about 27 or 28, becoming 

narrower and less distinct toward the extremity; sharply defined 

by striae. The axis narrows posteriorly, but less rapidly than the 

pleural portions. Toward the front it occupies less than one-third 

the width. A fairly distinct groove occurs upon each side of the 

axis, less than one-fourth the width up from the axial furrows, and, 

being parallel one with the other, each meets the groove before 

reaching the posterior end. The axis spreads a little more rapidly 

below these grooves, and the segments, elsewhere directly transverse, 

make a backward turn and sometimes become less sharply defined 

at them. Nine broad, strongly oblique segments on the plural 

portion. Sometimes narrow raised lines occur in the striae which 

separate them. The segments terminate laterally in a smooth 

flattened border, defined on its inner side by a groove. Near its 

outer margin it is marked by the slender, oblique, irregularly inosculating lirae rather characteristic of crustacean tests. The border, 

from being nearly horizontal on the sides, bends downward posteriorly to a more vertical position, which makes the end of the axis 

appear almost terminal when the pygidiurn is viewed from above.

The Surface is finely granular, but without other ornamentation.

This species is closely related to A. perannulata Shumard. The 

sharpest distinction is in the absence of rows of granules along the 

crests of the segments. Other differences in configuration, such as 

the greater width and the persistence of the axial segments to the 

furrow, may also prove serviceable in distinguishing them.

Horizon and locality. Yeso formatior, Mesa del Yeso (station 

3751c) and Alamillo (station 3751e).
REGISTER OF LOCALITIES.

3595. East of Caballos Mountains, at entrance to Palomas Gap, west of Ward's ranch.

W. T! Lee. 1904. 

3600. North point of Caballos Mountains.

v W. T. Lee. 1904. 

3738. Pass through Caballos Mountains, west of Upham. Limestone overlying the

red beds. . . . W. T. Lee. 1905.

3738a. Same as 3738. Limestone within the red beds, and 100 feet below top of section. 

W. T. Lee. 1905.

3740.' Caballos Mountains. Palomas Gap, east end. From lime above red beds and

50 feet from top of lime. On wagon road west of Ward's ranch. 

W. T. Lee. 1905.

3740a. Same as 3740; 25 feet from top of lime. 

W. T. Lee. 1905.

3741. Caballos Mountains, north end. From lime above red beds, top of Manzano

group. 

W. T, Lee. 1905.

3742. San Andreas Mountains, east of Engle. Foothills at edge of Jornada.

W. T. Lee. 1905. 

3742b. Same as 3742. In red beds 700 feet above top of massive red sandstone.

W. T. Lee. 1905. 

3742c. Same as 3742; 50 feet above 3742b.

W. T. Lee. 1905. 

3742d. Same as 3742; 100 feet above 3742c.

W. T. Lee. 1905. 

3742e. Same as 3742; 10 feet above 3742d.

W. T. Lee. 1905. 

3742f. Same as 3742; lime above red beds, top of section.

W. T. Lee. 1905. 

3742g. Same as 3742. From slide, midway of section.

W. T. Lee. 1905.

3743. Fra Cristobal Mountains, opposite .mouth of Montocello Gap. At 5,500 feet.

W. T. Lee. 1905. 

3743a. Same as 3743; in 25 feet of lime, in upper part of (red beds) Manzano.

W. T. Lee. 1905. 

3743b. Same as 3743; 20 feet above 3743a.

W. T. Lee. 1905.

3744. Nogal Creek, west of Paraja; from about midway of 300 feet of lime, above

pink and red sandstones. 

W. T. Lee. 1905. 

3744a. Same as 3744; near top of lime,

' W. T. Lee. 1905. 

3746. Carthage. Massive lime near the kiln.

W. T. Lee. 1905.

3746a. Same as 3746; in massive lime south of kiln. 

W. T. Lee. 1905.

119
120 MANZANO GROUP OF EIO GRANDE VALLEY.

3747. Hills east of San Antonio. Lime in upper portion of red beds. T\vo miles 

north of limekiln at Carthage.

W. T. Lee. 1905. 

3747a. Same as 3747. Lime resting on gypsum division of red beds.

W. T. Lee. 1905. .

3750. Near C. F. Blackinton's ranch, about 15 miles east of Socorro. Lime near

top of gypsum series of red beds. 

W. T. Lee. 1905.

3751. Section measured south of Mesa del Yeso, near Socorro. Lime near base of

red beds. 

W. T. Lee. 1905. 

3751a. Same as 3751. Lime between massive part of base of red beds and upper or

gypsum series. 

W. T. Lee. 1905.

3751b. Same as 3751a, but 20 feet higher. 

3751c. Same as 3751a; same stratum as 3751a.

W. T. Lee. 1905. 

3751d. Same; lime above the gypsum of the red beds.

W. T. Lee. 1905.

3751e. Two miles east of river near Alamillo. 

3753. Hills 10 miles east of Socorro. Lime in upper red beds.

W. T. Lee. 1905.

3757a. At head of canyon south of railroad line and £ mile east of a deserted stone 

cabin. About 50 feet above base of red beds. Abo Canyon at south end of 

Manzano Mountains. 

W. T. Lee. 19.05.

3796. Two miles south of Tejon, middle of red beds. 

W. T. Lee. 1905.

3797. Road between Ojo de San Francisco and Tejon. Middle of red beds. Road

runs from Bernalillo to Hague coal fields. 

W. T.Lee. 1905.

3798. Ojo de San Francisco, north of Sandia Mountains. 

W. T. Lee. 1905.
PLATES VI TO XII.

PLATE VI.

123
PLATE VI.

MEEKELLA MEXICANA n. sp. (p. 53).

FIGURE 1. Ventral view of a characteristic specimen, 

la. Side view of same in outline. 

16. Dorsal view of same.

2. Ventral view having more the configuration of M. slriaticostata but with

very obscure plications. 

2a. Side view of same in outline. 

26. Dorsal view of same.

3. Ventral view of a somewhat distorted specimen with rather strong

plications.

3a. Side view of same in outline. 

36. Dorsal view.

4. Dorsal view of an immature specimen which has at this stage all the characters of an Orthothetina. 

4a. Ventral view. 

46. Side view in outline.

5. A large dorsal valve with very faint plications. 

5a. Side view of same in outline.

The originals of figures 1-4 are from station 3740; that of figure 5 is 

from station 3741.

MEEKELLA STRIATICOSTATA Cox (p. 54).

FIGURE 6. Ventral view gf a specimen referred to this species. 

.6a. Side view of same in outline. 

66. Dorsal view of same.

The original of figure 6 is from station 3751.

124
U. S. GEOLOGICAL SURVEY BULLETIN 389 PLATE VI

2b

3a

4a

3b

6a

THE MANZANO FAUNA
PLATE VII.

125
PLATE VII.

PEODUCTUS LEEI n. sp. (p. 56).

FIGURE 1. Dorsal view of the type specimen, 

la. Side view of same in outline. 

16. Ventral view of same. 

Ic. Posterior view of same.

The original of figure 1 is from station 3738.

MARGINIFERA ? CRISTOBALENSIS n. sp. (p. 65).

FIGURE 2. Anterior view of the type specimen, X2. 

2a. Posterior view of same, X2. 

26. Side view of same in outline. 

2c. Same, seen from above.

The original of figure 2 is from station 3743.

MARGINIFERA? MANZANICA n. sp. (p. 64).

FIGURE 3. The type specimen seen from above. 

3a. Posterior view. 

36. Side view of same in outline.

The original of figure 3 is from station 3743.

PRODUCTUS MEXICANUS Shumard? (p. 57).

FIGURE 4. An imperfect ventral valve referred to this species. 

4a. Same, side view in outline.

The original of figure 4 is from station 3744a.

PRODUCTUS NEBRASKENSIS Owen (p. 62).

FIGURE 5. A ventral valve, considerably exfoliated. 

5a. Same, side view in outline.

6. A dorsal valve reduced nearly to the condition of an external mold. 

6a. Side view of same, outline.

The originals of figures 5 and 6 are from station 3757a.

126
U. S. GEOLOGICAL SURVEY BULLETIN 389 PLATE VII

3a

2b

' ^aa&

2c

5a

THE MANZANO FAUNA
PLATE VIII.

]27
PLATE VIII.

COMPOSITA MEXICANA Hall (p. 68).

FIGURE 1. Anterior view of a characteristic specimen, 

la. Dorsal view of-same. 

16. Side view of same in outline.

The original of figure 1 is from station 3742f.

PUGNAX OSAGENSIS var. PUSiLLA n. var. (p. 65).

FIGURE 2. Dorsal view of a rather broad specimen, X 2. 

2a. Ventral view of same, X 2. 

26. Anterior view of same, X 2.

3. Dorsal view of a narrow specimen, X 2. 

3a. Ventral view of same, X 2. 

36. Anterior view of same, X 2. 

3c. Same, side view in outline, X 2.

The originals of figures 2 and 3 are from station 3751b.

ENTOMIS SHUMARDIANA n. sp. (p. 117).

FIGURE 4. Side view of a specimen with both valves, X 20. 

4a. Dorsal view of same, X 20. .

5. Side view of another specimen similar to the first, X 20. 

5a. Dorsal view of same, X 20.

The originals of figures 5 and 6 are from station 3742d,

BAIRDIA OCCIDENTALIS n. sp. (p. 116).

FIGURE 6. Side view of a specimen retaining both valves, X 20. 

6a. Dorsal view of same, X 20.

The original of figure 6 is from station 3742d.

CYTHERELLA BENNIEI Jones, Kirkby, and Brady (p. 116).

FIGURE 7.. Side view of a specimen referred to this species, X 20.

7a. Dorsal (?) view of same, X 20. .

8. Side view of a second specimen, X 20.

8a. Dorsal view of same, X 20.

9. Side view of another specimen, X 20.

The originals of figures 7-9 are from station 3742d.

HOLLINA HEREICKANA n. sp. (p. 115).

FIGURE 10. Exterior of a right valve, X 20. 

10a. Interior of same, X 20.

11. Side view of a small specimen retaining both valves, X 20. 

lla. Dorsal view of same, X 20. The anterior extremity, as represented in

the figure, is below. 

116. Anterior view of same, X 20.

The originals of figures 10 and 11 are from station 3742d.

ANISOPYGE INORNATA n. sp. (p. 118).

FIGURE 12. A silicified pygidium, X 2. 

12a. Side view of same, X 2.

The originals of figure 12 are from station 3751e. 

128
U. S. GEOLOGICAL SURVEY BULLETIN 389 PLATE VIII'

4a

10

3a

2a

'1

L_

3°

1 2a

11

THE MANZANO FAUNA
PLATE IX.

84259 Bull. 389 09 9 129
PLATE IX.

PSEUDOMONOTIS SUBLJEVIS 11. Sp. (p. 80).

 FIGURE 1. A very characteristic specimen.

2. A narrow specimen considerably exfoliated.

3. A small, nearly perfect specimen.

The originals of figures 1-3 are from station 3742b.

PSEUDOMONOTIS HAWNI Meek and Hayden? (p. 79).

FIGURE 4. A small specimen provisionally referred to this species. 

The original of figure 4 is from station 3740.

DELTOPECTEN VANVLEETI Beede (p. 86).

FIGURE 5. A fragment of the umbonal portion of a specimen referred to this

species, X 2.

5a. View of the hinge plate, showing the triangular ligamental pit. 

56. Side view of same.

The original of figure 5 is from station 3742.

MYALINA APACHE si Marcou (p. 81). 

FIGURE 6. A small specimen referred to this species.

7. A fragmentary specimen larger than the other but considerably smaller 

than the largest forms placed in this species.

The originals of figures 6 and 7 are from station 3757a. 

130
U. S. GEOLOGICAL SURVEY BULLETIN 389 PLATE IX

THE MANZANO FAUNA
PLATE X.

131
r~

PLATE X.

PLEUEOPHORUS MEXICANUS n. sp. (p. 91).

TIGURE 1. Side view of the somewhat imperfect specimen on which the description

was based, 

la. Cardinal view of same.

The original of figure 1 is from station 3751c.

PLEUROPHORUS BIPARTITUS n. sp. (p. 92).

FIGURE 2. Side view of the type specimen.

The original of figure 2 is from station 3751.

MANZANELLA ELLIPTICA n. gen. et sp. (p. 76).

FIGURE 3. Interior of a left valve, X 3.

4. Interior of a right valve, X 3. 

4o. Same, exterior, ad nat.

The originals of figures 3 and 4 are from station 3751e.

CLINOPISTHA? sp. (p. 72).

FIGURE 5. A form of doubtful affinities. ' 

The original of figure 5 is from station 3743.

SCHIZODUS WI-IEELERI Swallow? (p. 82).

FIGURE G. An imperfect specimen referred to this species. 

The original of figure 6.is from station 3742d.

NUCULA LEVATIFORMIS Walcott (p. 74).

FIGURE. 7. A specimen of the size usual in our collection. Side view of left

valve, X 2. . 

la. Posterior view in outline, X 2.

The original of figure 7 is from station 3751e.

8. Side view of an unusually large left valve, X 2.

Sa. Same, natural size in outline.

The original of figure 8 is from station 3743.'

NUCULA LEVATIFORMIS var. OBLIQUA n. var. (p. 75).

FIGURE 9. Side view cf a characteristic right valve, X 2. 

9a. Posterior view of same in outline, X 2.

The original of figure 9 is from station 37431).

ASTARTELLA SUBQUADRATA 11. Sp. (p. 94).

FIGURE 10. Interior of a characteristic right valve, X 4. 

10a. Exterior of same, ad nat.

11. A right valve of somewhat unusual shape.

12. Exterior of a characteristic left valve. 

12a. Anterior view in outline, X 2.

13. Interior cf a lol't valve, X 4.

14. Cardinal view of a specimen having the two valves in conjunction. 

The originals of figures 10-14 are from station 3751e.

132 '
U. S. GEOLOGICAL SURVEY BULLETIN 389 PLATE X

1 a

7a

8a

Q),

9a

14

10

11 12

10a

12a

THE MANZANO FAUNA
PLATE XI.
PLATE XL

BUCANOPSIS MODEST A n. Sp. (p. 103).

FIGURE 1. Dorsal view of a silicifiecl specimen, X 2. 

la. Side view of same, X 2.

16. Anterior view, showing character of the slit, X 2. 

Ic. Apertural view, X 2.

The original cf figure 1 is from station 3738a.

BELLEROPHON MAJUSCULUS Walcott (p. 101).

FIGURE 2. Dorsal view of a small specimen than which much larger, though less

perfect, ones occur in the collection, X 2. 

2a. Side view. 

26.'Apertural view.

The original of figure 2 is from station 3738a.

PHANEROTREMA MANZANICUM n. sp. (p. 96).

FIGURE 3. Side view of a large specimen with imperfect spire, X 2. 

3a. Opposite side of the same, natural size. 

4. Side view of a small specimen with complete spire.

The originals of figures 3 and 4 are from station 3751e.

WOBTHENIA ALAMILLANA n. Sp. (p. 98).

FIGURE 5. Side view of the type specimen. 

5a. Opposite side of same, X 2.

The original of figure 5 is from station 3751e.

SOLENISCUS aff. ALTONENSIS Worthen (p. 108).

FIGURE 6. Side view of a specimen reduced almost to an internal mold. 

The original of figure 6 is from station 3757a.

SPH^RODOMA aff. TEXANA Shumard (p. 109).

FIGURE 7. Side view of a specimen resembling Shumard's species, X 2. 

The original of figure 7 is from station 3738a.

NATICOPSIS DEFORMIS n. sp. (p. 106).

FIGUKE 8. A large specimen, seen from above. 

8a. Side view of same.

The original of figure 8 is from station 3757a. 

9. A small specimen, seen from above, X 2. 

9«. Same, side view, X 2.

The original of figure 10 is from station 374Qa.

DENTALIUM MEXICANUM n. sp. (p. 95).

FIGURE 10. Side view of the typical specimen, X 3. Associated fragments indicate

a considerably larger size. 

10a. Same, natural size in outline.

The original of figure 10 is from station 3738a.

PLAGIOGLYPTA CANNA White (p. 95).

FIGURE 11. The younger portion of a specimen, showing the straight shape and the 

absence of longitudinal stride, X 2.

The original of figure 11 is from station 3751e.

ORTHONEMA SOCORROENSE n. sp. (p.-109).

FIGURE 12. Side view of the type specimen, showing very regular growth, X 2. 

13. Side view of specimen of less regular construction.

The originals of figures 12 and 13 are from station 3751e. 

134
U. S. GEOLOGICAL SURVEY BULLETIN 389 PLATE XI

10

2a 2b

8a

9a

10a 13 12

THE MANZANO FAUNA

11
PLATE XII.

135
PLATE XII.

COLDCERAS MEXICANUM n. Sp. (p. 113).

FIGURE 1. Side view'of the type specimen, showing the septation.

la. Opposite side, which retains the shell and so shows the configuration. 

16. Ventral view of same.

The original of figure 1 is from station 3751c.

ORTHOCERAS sp. (p. 112).-

FIGURE 2. View of ventral (?) side of a specimen of undetermined affinities. 

2a. Side view of same, showing the curved suture. 

26. End view in outline.

The original of figure 2 is from station 3757a.

136
U. S. GEOLOGICAL SURVEY BULI.ETIN 389 PLATE XII

'.=r

1 a

THE MANZANO FAUNA
GENERAL INDEX.

Page. 

Abo Canyon, fossils in....................... 21

section in................................ 20-21

Abo sandstone, description of....... 11,12,14,20,22

fossils of........................... 21,23,45-49

A.gassiz, Louis, on Echinocrinus............. 51

Alamillo, fossils near..................... 24,45-49

Apache Canyon, fossils of.................... 32-33

rocks of................................... 31-33

section in............................... 32

Aubrey group, correlation of................. 42-43

Beede, J. W., on Quartermaster formation

fossils........................ 0-7,43,44

Bemal, fossils near.......................... 36

rocks near..........:.................... 35-36

Blackinton's ranch, fossils at.............. 24,45-49

Caballos Mountains, fossils of.......... 27,28,45-49

rocks of.................................. 14

section in................................ 28

figures showing...................... 14,28

view of.................................. 10

Carthage, fossils of........................... 45

rocks near......................... 13,14,15,40

section near............................. 24-25

figures showing....................... 14,25

Elephant Butte, fossils of................. 27,45-49

Engle, fossils near........................ 27,45-49

red beds near........I....'............... 0

Faults, views of............................. 20

Field work, extent of........................ 7,31

location of............................... 7-8

Formation names, adoption of............... 8-9

Formations, description of.. '. ................ 9-13

Fossil localities, list of...................... 119-120

location of, map showing..........'...... 8

Fra Cristpbal Mountains, fossils of........... 45-49

rocks of............................... 14,25-20

section in................................ 25-20

figures showing...................... 14,26

views in...............................;. 22,2C

Galisteo Canyon, fossils of................... 45-49

rocks in, view of.......................... 10

section in................................ 18-19

figures showing...................... 14,18

Galisteo sandstone, character of.............. 6

Girty, G. H., on Quartermaster fauna....... ' 7

on Manzano fossils....................... 136

Glorieta Mesa, rocks of...................... 31-32

Goeppert, II. R., and Meyer, H. von, on

Echinocrinus .................... 51

Gordon, C. H., stratigraphy by.............. 8-10

Gypsum beds, view of....................... 10

Hayden, F. V., on Las Vegas rocks.......... 37

Herrick, C. L., on Manzano group........ 10-12, 44

on San Andreas limestone............... 12-13

Page.

Herrick, C. L., and Johnson, D. W., on Manzano group...................... 11

Hueco formation, correlation of.............. 42,44

Johnson, D. W., .and Herrick, C. L., on

Manzano group................. 11

Knowlton, F. H., and White, David, fossils

examined by.................... 33

Lamy, rocks near......................... 31

Las Vegas, fossils near....................... 30,38

rocks near............................... 30-38

section near............................. 38

figure showing..................... 37

Lee, W. T., fossils collected by......... 45,119-120

stratigraphy by......................... 5-40

Madera limestone, description of........... 10,20

Magdalena group, fossils of.................. 35,36

descriptions of............... 9-10,32, C3,35,39

subdivision of........................... 9

Manzano group, a[;e of.................. 5-6,39-40

character of............................ 10-13

correlation of............................ 42-44

deposition of............................ 39-40

. distribution of................. 5,7-8,21,30-38

erosion of............................... 8,14

fossils of................................ 13-118

localities of...................:.... 119-120

plates showing.................... 121-130

relations of........................ 5,13-17,30

stratigraphy of.......................... 5-40

summary of........................ 39-40

study of................................. 5,30

subdivision of........................... 9,14

unconformity above..................... 15

unconformity below..................... 13

Map of Rio Grande region, showing fossil

localities........................ 8

McCoy, Frederick, on Echinocrinus ......... 50-51

Meek, F. B., on Echinocrinus............... 50

Mesa del Yeso, fossils of..................... 45-49

'section at.............................. 21-23

figures showing..................... 14,22

view of.................................. 22

Morrison formation, relations of............. IS

New Mexico, red beds of.................... 5-6

See also Manzano group. 

Nogal Creek, fossils at................... 20,45-49

rocks at.................................. 26

Pennsylvanian series, descriptions of........ 9-13

subdivisions of.......................... 9

Perry Park, Colo., red beds of.............. 0

Quartermaster formation, correlation of..... 43-44

Red Beds, problem of...................... 5

Sec also -Manzano group. 

Redwall limestone, correlation of............ 42

137
138 GENEEAL INDEX.

Page. 

Richardson, G. B., on Abo Canyon rocks.... 21,30

Rico formation, correlation of.............. 42,43

Rio Grande region, map of.................. 8

Rio Grande valley, red beds of. See Manzano group. 

Rowe, fossils near........................... 35

rocks near............................... 33-35

section near................... 4 ......... 34-35

figure showing..................... 34

Salt, occurrence of........................... 11

San Andreas limestone, description of....... 12-13,

14-15,30,40 

fossils of........................ 26,28,29,45-49

view of.................................. 22

San Andreas Mountains, fossils of ............ 45-49

rocks of................................. 12,14

section in.............................. 28-30

figures showing..................... 14,29

Sandia formation, description of.............. 9

'Page. 

Sandia. Mountains, fossils of................. 15

rocks of................................. 45-49

section in................................ 19-20

figures showing...................... 14,19

Stanton, T. W., fossils determined by....... 15

Stratigraphy, description of................. 13-43

summary of............................. 38-39

table showing........................... 16-17

Tejon, rocks near............................ 20

White, David, and Knowlton, F. II., fossils

examined by.................... 33

Whitehorse sandstone, correlation of......... 43-44

Willard, N. Mex., fossils near ............... 21

section near............................. 21

Yeso formation, age of....................... 11

description of....................... 11,12,14,23

fossils of............... 19,23,24,25,26,29,45-49

view of.........../...................... 22
INDEX OF FOSSILS.

Names in italic are synonyms; figures in italic denote illustrations; figures in black face indicate 

descriptions.

A. Pa,

Acamhopecten carboniferus................. 35

Allerisma capax................ 14,21,23,42, 89, 01

terminals................... 14,38,43,89,90-91

sp....................................... 23

Allorisma capax. ............................ 89

ensiformis ............................... 90

Leavenworihensis ........................ 73

regularis. ................................ 90

subcuneata... ............................ 90

subcuneatum.. ........................... 90

terminale................................. 90

Anisopyge inornata:............. 23,24,49,11.8, 128

perannulata............................. 118

Archteocidaris............................... 50-51

craiis.. .................................. 52

Astarte gibbosa ................................ 73

Astartella gurleyi............................ 94

siibquadrata............... 23,24,46,49,94,7S2

sp....................................... 35,38

A thyris argentea ............................. 71

subtilita.. ............................... 09,70

Avienlipecten mccoyi....................... 86

oklahomensis............................ 88

sp.................................... 35,36,38

Aviculipinna................................ 15

nebraskensis.......... 21,27,28,29,43,46,48,78

peracuta................. 21,23,35,38,46,48,78

Aviculopccten... ............................. 84

Coreyana ................................ 87

Coreyanus. .............................. 87

coryanus ................................ .87

Me Coyi ..................s.............. 86

occidcnlalis .............................. 84,85

vanvleeli ................................. 86

Aviculopcctin occidentalis............^...... 85

A viculopinna nebraskensis................... .78

peracuta ................................. 77,78

B. 

Bairdia..................................... 117

cestriensis............................... 116

occidentalis ................ 47,49,116-117, 128

Bakewellia.................................. 79

parva................................ 10,44,79

Bellerophon carbonarius var. subpapillosus ... 99 

crassus................................. 36,101

inspeciosus ............................. 100

inajusculus. 19,23,26,27,28,29,42,46,49,101, 134 

subpapillosus............................ 99

textilis.................................. 102

sp....................................... 21,35

Brachiopoda............................. 42,53-72

Bryozoa.................................... 52-53

Bucanopsis marcouiana..................... 103

modesta.................. 21,28,47,49,103,734

textilis.................................. 103

c- ' Page. 

Cardiomorpha sp............................ 35,38

Cephalopoda............................. 112-115

ChEenomya leavenworthensis... 21,23,46,48,73-74 

Chsetetes milleporaceus..................... 21

Chonetes sp................................. 35

Cidaris miinsteriana......................... 51

uri i..................................... 59,51

Cleiothyridinamissouriensis................. 35,38

Clinopistha................................ 72-

radiata var. Isevis....................... 72

sp......................... 23,20,40,48,72,^,3

Ccelenterata................................. 50

Coloceras................... ^................ 113

mexicanum.................. 23,24,49,113, ISO

Composita argentea......................... 68

mexicana............... 29,46,49,68,71,72, 128

subtilita.. 21,23,26,34,35,36,38,43,46,49,68-72 

Conularia sp................................ 38

Crenipecten hallanus........................ 88

Cyclopora sp................................ 35,38

Cypricardia Whecltri ........................ 82

Cytherella benniei.................. 47,49,116, 128

I). 

Deltopecten coreyanus.... 19,21,23,26,46,48,87-89

manzanicus.......................... 21,27,29

mccoyi ................................. 86,87

occidentalis................. 21,35,42,48,84-85

oklahomensis............................ 83

vanvleeti............... 43,46,48,86-87,89, ISO

Dentalium acutisulcatum................... 95

canna................................ 42,95,96

mexicanum.......... 15,26,2S, 46,49,95,96, 134

sublseve................................. 95

sp....................................... 36

Derbya sp............................... 35,36,38

Dielasma bovidens....................... 35,36,38

Domatoceras sp......................... 23,49,115

E. 

Echinocrinus............................... 50-52

Gratis. ........................... 28,46,48,52

iniinsterianus........................... 51

triplex.................................. 52

Echinodermata. ............................ 50-52

Edmondia.................................. 73

gibbosa.................. 21,23,24,43,46,48,73

nebraskensis............................ 35

Entolium.................................... 8S

Entomis.................................... 117

shumarcliana....................... 47,117, 128

Eocidaris.................................... 51

Euconospira sp.................:............ 35

Eumicrotis Hawni. .......................... 79,80

Euomphalus................................ 15

deformis................................ 27

pernodosus.................. -28,47,49,103-104

sp........... 19,26,27,28,29,47,49,103,104-105

139
140 INDEX OF FOSSILS.

Puge. 

Eupachycrinus sp........................... 36

Euphcnius earbonarius...................... 100

inspcciosus.............. 23, 24, 26, 27, 46,49, JOO

nodicarinatus... '........................ 100

subpapillosus................. 19,46,49,99-100

F. 

Fenestella sp................................ 35,3S

Fistulipora sp............................... 35

G. ' . 

Gasteropoda. .............................. 1)6-112

H.

Hollina emaciata............................ 116,

tetoidea................................. 116

herrickana. ................. 47,49. 115-116, 128

kolmodini./............................ 116

radiata.................................. 116

Hustediamormoni.......................... 35,38

L. 

Laccopteris................................. 33

Leda obesa..................... 21,23,46, 48, 76-77

Limopteria Marian.......................... 79

Lophophyllum profundum.................. 30,38

sp................................ 21,35,46,50

Loxonema rugosum......................... 107

Mv 

Macrocheilus sp.............................. 108

Afanzanella. ................................. 75-76

elliptica...................... 23,24, -'.8, 76, 132

Marginiferacristobalensis............ 46,49,65, 126

hay cleniana............................. 64

irrgrata................................... 64

inanzanica. ............. 26,29, ^6,49, 64-65, 126

splcndens............................... 64

wabashensis............................. 64

sp....................................... 26,29

Martinia lineata. ............................. 06,67-

Meckclla mexicana. ........ 27,46,48, 53-54, 55, 124

striaticostata........ 21,23,36,46,48, 54, 55, 184

striato-costata ............................ 54,55

Metacoceras walcotti........................ 35,36

Modiola subelliptica......................... 35,93

Modiomorpha desiderata..........:......... 91,93

Mogulia..................................... 102

sp............................ 28, 47,49, 102-103

Mollusca.................................... 42

Monopteria marian................ 19,21, 4$. 78-7i>

Monotls Hawni.............................. 79

Murchisonia................................. 109

collingworthensis,....................... 98

terebra................... 19,23,26,28, <6,49,99

Myalina..................................... 82

apachcsi....... 21,23,27,29,44,46,48,SI-82, ISO

attenuata............................... 10,44

congeneris. ............................... 82

kansasensis.............................. 82

subquadrata............................ 35

wyomingensis........................... 35

sp................................. 21.35,36,38

N. 

Naticella transversa......................... 106

Naticopsis................................... 107

altonensis... .................... 23,49, 106-107

deformis..................... 21,47,49,106, 134

sp....................................... 35

Fage. 

Nautilus sp.. .......<....................... 35

Nucula...................................... 72,75

Icvatiformc. ............................... 74

levatiformis.......... 23,24,26,46, 48, 74,75, 132

var. obliqua................: 46,48, 75, 138

parva. ................................... 74

Xuculaha obesa ...................... 75

0. 

Ortli.is sluato-costata ......................... 54

OrthmnaMissouriensis ...................... 54

occidcntalis ............................. 54

Shumardiana ........................... 54

Orthoccras baculur.i......................... 113

novame.xicanum........................ 113

sp. -.................; 21, 35, 36,49,112-113, 136

Orthonerna carbonarium ............. 110, 109-112

dozierense............................. no, 111

socorroense ............. 23,24,49, 100-111, 134

texanuin................................ m

sp ................. 23, 26,35,47,49,110, 111-112

Orthothef'ina............................... 53 124

Ostracoda. ................................ 115-117

P. 

Parallelodon carbonarius.................... 35

obsoletus.......,.....:........ 29,46,48,77-78

Patellostium nodicostatum. 19,21,23,47,49,102,103 

Pccten cleavdandicus. ........................ 84

missouricnsis......................'...... 84

occidcntalis.............................. §4

Pelecypoda. ................................ 72-94;

Peniipecten................................. SB

Phanerotrema brazoense........... 28,46,49,97-98

manzanicum ......... 19,23,24,49, 96-97, 98, 184

inarcouianum........................... 97

sp....................................... 23

Phillipsia major............................. 36

scitula.................................... 35

Pinna adamsi .............................. 77

peracuta ................................ 77

Plagiogiypta.............. 15,19,23,24,26,27,46,49

canna. .............................. 95-96, 134

Platyceras nebraskense...................... 36

. sp....................................... 35

Pleurophorella costata....................... 35

Pleurophoms................................ 92

bipartite .................... 23, 46, 48,92, m

meeki............................. 23,24,49,93

mexicanus.............. 23,27,46,48, 91-92, 132

oblongr.s................................ 21,49

subcostatus........... 21,23,24,44-45,46,49,94

subcuneatus............................ 10,44

taffi......................... 23,29,46,49,91,93

tropidophorus........................... 93

sp ..................................... 23,29,35

Pleurotomaria.............................. 98,109

Pleurotomariidse............................ . 109

Plicatula striato-costata...................... 54

Polypora sp................................. 35

Pontocypris acuminata...................... 116

Prirnitia..................................... 117

cestriensis...!........................... 11"

simulans................................ 117

Productus................................... 64

asper.................................... 62

aspcrus. ................................. 62
INDEX OF FOSSILS. 141

Page. 

Productus calhounianus ..................... 50, CO

cora................ 21,23,35,38,43,46,49,58-61

costatus................................. 58

Flemingi. ............................... 59

hermosanus............................. 57

ivesi......... 23,26,29,42,46,48,56,57,58,65,81

KonincJdanus........................... 59

latidorsatus......................'.-..I.- C5

leei............ 26,27,28,29,46,48,56-57,58, 126

longiis................................... 56

lyelli .................................... 58

Martini ................................. 59

mexicanus..... 23,26,29,46,48,57-58.64,65, 186

nebrasccnsis...........:................. 62,03

aiebraskensis...... 21,23,35,36,46,48,62-64, 186

occidentalis.............................. 58 

Pratteniartus.......................... 59,GO,61

punctatus................................36,38

Rogersi .................................. 62

semireticulatus.............. 35,36,3)5,56,57,81

subkorridus............................. 58,65

var. rugatulus ...................... 65

Pseudomonotis hawni. 21,27,29,43/46,48,79-80, ISO 

occidentalis............................. 27,29

subltevis......................... 46,48,80, ISO

Pteria ohioensis.....'......................... 79

sp.............................. 23,24,44,48,79

Pugnax osagensis............................ 35,05

osagensis var. pusilla....... 23,~46,48,65-66, ^25

Utah...................................... 65

R.

Relicularia perplexa. 

Ithombopora sp....

S.

Sanguinolites................................ 72

teolus................................... 92

retusus.................................. 92

Scaphopoda.....................;........... 95-96

Schizodus .................................. 83

afflnis .................................... 83

curtiformis.............................. 83

jiiagnus.............................. 23,48,84

obscurus...'.............................. 32

wheeleri................................. 19,

21,24.25,26,27,28,29,42,46,48, $2-84, 152 

sp....................................... 21,35

Seminula argentia. ........................... 71

subtilita ................................. 70,71

Septopora robusta.................... 21,48,52-53

sp....................................... 36

Soleniscus................................... 109

altonensis.................... 21,35,49,108, 134

hallanus................................. 108

Soleuiscus newberryi....................... 108

planus....................... i........... 108

Solenornya.................................. 20

ntenia............. '. ............... 26,46,48,72

SphiErodoma................................ 109

intercalaris........................'...... 108

medialis. ....... "........ 27,28,47,49,108-109

ppnderosa.....................'.......... 109

primigenia.............................. 109

texana....................... 28,47,49,109, 134

Sphenotus seolus ............................ 92

Spirifer cameratus........................ 35,36,38

lineatus. .................................. 66,67

var. perplexa........................ 66

var. striato-lineatus.................. 66

raarcoui................................. 81

perplexa ................................. 65

rockymontanus.......................... 36,38

striatus.................................. 81

Spirifera (Martinia) lineata.................. 66,67

(Martinia) perplexa ..................... 66,67

Spiriferinakenttickyensis................. 35,36,38

sp....................................... 35

Spirigcra subtilita............................ C9,70

Squamularia perplexa. 23,29,35,36,38,46,48,66-68 

Strcptorliynchus (Meekella) striatocostato ..... 54

Streptorhynchus (Orthisina) Shumardianus .. 54 

Stropalosia liorrescens........................ 62

Strophostvlus permianus.................... 107

' TTainoceras occidentale.................... 35

Temnocheilus conchiferum.......... 26,47,49,114

winslowi................. 23,24,47,49,113-114

sp........................... 23,47,49,114-115'

Terebratuli .................................. 68

mexicana ................................ 68

plano-sulcata ............................ 68,69

roysii.................................... 69

subtilita................................. 68,W

Trilobita.................................... 118

Voltzia. 33

W.

Walchia...................................... 33

pinniformis............................ 33

Warthia.................................. 102-103

Worthenia alainillana................... 49,98, 134

marcouiana........................... 98

subscalaris.............................. 98

tabulata................................ 98

Zygopleura rugosa.................... 23,24,49,107

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