, 7f

The Upper Paleozoic Madera Group 

in the Manzano Mountains, 

New Mexico

By DONALD A. MYERS

CONTRIBUTIONS TO STRATIGRAPHY

GEOLOGICAL SURVEY BULLETIN 1372-F
UNITED STATES DEPARTMENT OF THE INTERIOR 

ROGERS C. B. MORTON, Secretary

GEOLOGICAL SURVEY 

V. E. McKelvey, Director

Library of Congress catalog-card No. 72-600328

For sale by the Superintendent of Documents, U. S. Government Printing Office 

Washington, D. C. 20402

Stock No. 2401-00287
CONTENTS

Page

Abstract ________________________________ _______ Fl

Introduction __________________________________ 1

Madera Group _________________________________ 3

Los Moyos Limestone 4

Wild Cow Formation __________________________ 8

Sol se Mete Member _ _ _____________ 8

Pine Shadow Member ________________________ 9

La Casa Member _ _ 10

Bursum Formation ___ _ _ _________ ______ 11

References cited _ _ _ _ _ ____________________ 12

ILLUSTKATIONS

Page

FIGURE 1. Index map of the Manzano Mountains area showing location of described sections ___ _____ _ _ F2 

2. Type and reference sections for the Los Moyos and Wild

Cow Formations ____________________ _ 7

ill

CONTRIBUTIONS TO STRATIGRAPHY

THE UPPER PALEOZOIC MADERA GROUP

IN THE MANZANO MOUNTAINS,

NEW MEXICO

By DONALD A. MYERS

ABSTRACT

The Madera Limestone, of Middle and Late Pennsylvanian and Early 

Permian age, is raised to group rank in the Manzano Mountains, N. Mex., 

where it consists of three formations (ascending order): a sequence of 

massive cliff-forming limestone, named in this report the Los Moyos Limestone; a sequence of arkosic clastic rocks, shale, and locally cliff-forming 

limestones defined as members of the Wild Cow Formation, all of which 

are named in this report; and the Bursum Formation, a red-bed sequence 

newly assigned to the Madera Group in the southern Manzano Mountains.

INTRODUCTION

The Manzano Mountains lie along the east side of the Rio 

Grande Valley and extend about 45 miles south from the east side 

of Albuquerque to Abo Canyon and the A.T. & S.F. Railway. They 

are about 10 miles wide (fig. 1). The core of the mountain range 

is Precambrian metasedimentary and metavolcanic rocks that contain minor granitic intrusives. Middle Pennsylvanian rocks lie in 

depositional contact upon the Precambrian.

The sedimentary sequence here discussed is of Middle and Late 

Pennsylvanian and Early Permian age. The stratigraphic nomenclature proposed for these rocks is based on continuing fieldwork 

that began in 1962. Except where ruggedness of terrain made it 

physically impractical, I walked the distance covered by most of 

the contacts between the named units.

I thank Dr. Frank E. Kottlowski of the New Mexico State 

Bureau of Mines and Mineral Resources for his review of the 

manuscript.

Fl
F2 CONTRIBUTIONS TO STRATIGRAPHY

106M5' 106°

35°00' 

34°30' 

FIGURE 1. Index map of the Manzano Mountains area showing location of described sections. Triangle indicates type section; X reference section. ^
MADERA GROUP, MANZANO MOUNTAINS, NEW MEXICO F3

MADERA GROUP

The term Madera was first used by Keyes (1903, p. 48), who 

wrote as follows:

This great limestone formation forms a remarkable cornice on the Sandia 

mountains, clearly seen from the railroad station at Albuquerque. It is also 

an important part of the Manzano * * * ranges.

In the Sandia Mountains the several formations have been more clearly 

differentiated than perhaps anywhere else. The basal conglomerate and 

associate sandstones have been called the Sandia quartzites. For the lower 

black limestone the name Placitos [sic.] is proposed * * *.

The superior part of the great limestone formation the blue to gray 

beds contains an abundant fauna, that clearly points to an age of late 

Carboniferous. In the Sandia Mountains this formation is called the Madera 

limestone. It forms by far the most important portion of the Carboniferous 

in all of the ranges before mentioned.

Above the great blue limestones of the Carboniferous comes in an important sandstone and then a sequence of shales and sandstones conspicuous 

for their remarkable red coloration * * *.

In the Sandia Mountains the lower sandstone is called the Coyote sandstone from Coyote Springs and the upper member the Bernalillo shales.

As used by subsequent workers (for example, Read and others, 

1944), the Madera Limestone includes Keyes' (1903) Placitos and 

Madera Limestones, Coyote Sandstone, and lower part of the Bernalillo Shales. The upper part of Keyes' Bernalillo Shales was 

apparently included in the Bursum Formation and in the basal 

part or all of the Abo Formation.

In the report area, rocks previously considered as the Madera 

Limestone and Bursum Formation are placed in the Madera 

Group, thereby redefining the upper contact of the Madera and 

raising its stratigraphic rank in the Manzano Mountains. The 

Bursum is included in the Madera Group because it is depositionally continuous with the underlying rocks. The group consists of all 

rocks that overlie the Sandia Formation of early Middle Pennsylvanian age and that underlie the Abo Formation of Early Permian 

age. It consists of rocks assigned to the fusulinid zones of Beedeina and Triticites and to the lower part of the zone of 

Schwagerina.

The Madera Group in the Manzano Mountains includes rocks 

previously assigned there to the Magdalena Group. The Magdalena Group, as originally defined by Gordon (1907, p. 806-812) in 

the Magdalena Mountains, consists of all rocks between the 

Mississippian System and the basal red beds of the Permian System. Thus the Magdalena Group was considered to be mostly of 

Pennsylvanian age until 1946 (Wilpolt and others), when the 

Permian Bursum Formation was added to the group. The Magdalena Group in the area of this report consisted of all Pennsylvania^
F4 CONTRIBUTIONS TO STRATIGRAPHY

rocks and the Bursum Formation; its use in the Manzano Mountains is rejected. The Magdalena Group remains in good standing 

elsewhere.

Thompson (1942) defined and described several groups, formations, and members from the Pennsylvanian system in New Mexico. His descriptions of the various lithic units were from southcentral New Mexico and his correlations between the various units 

were apparently mostly paleontologic. Few or no data have been 

published that demonstrate the cartographic continuity of Thompson's units. His units could not be recognized as lithologic entities 

in the Manzano Mountains.

The lower part of the Madera Group is a sequence of massive 

cliff-forming medium- to light-gray cherty limestone with minor 

amounts of interbedded gray to black shale and lenticular beds of 

grayish-orange sandstone and conglomerate. This part of the 

Madera is here named the Los Moyos Limestone.

The middle part of the Madera Group is here named the Wild 

Cow Formation. It is a rhythmic-bedded sequence of arkosic sandstone and conglomerate, gray shale that becomes red in the upper 

part, and light-olive-gray and light- to medium-gray locally cliffforming limestone.

The upper part of the group is the Bursum Formation, a thin 

red-bed unit.

LOS MOYOS LIMESTONE

Los Moyos Canyon, the feature for which the limestone is 

named, is on the Isleta Indian Reservation in the Tajique and 

Bosque Peak quadrangles, Torrance County. The canyon is in 

sees. 11 and 12, T. 7 N., R. 5 E. (projected), where a nearly complete sequence of the Los Moyos is exposed (figs. 1, 2). However, 

as access to this area is difficult, the type section is designated as 

exposures on the walls of a ravine that drains into Priest Canyon 

through a hogback in the southwestern part of the Torreon 15- 

minute quadrangle, sec. 7, T. 3 N., R. 5 E., Valencia County (figs. 

1, 2). The sequence in Los Moyos Canyon and a sequence exposed 

at Sol se Mete (Myers and McKay, 1970) in the Mount Washington quadrangle, sec. 29, T. 9 N., R. 5 E., Bernalillo County (figs. 1, 

2), are designated as reference sections.

The Los Moyos Limestone is everywhere about 600 feet thick. 

The basal few feet of beds is gradational from the dark-colored 

calcareous shale and shaly limestone of the uppermost Sandia 

Formation. The lower 80-100 feet is cliff-forming olive- to 

medium-gray calcarenite containing large amounts of dark-brown
MADERA GROUP, MANZANO MOUNTAINS, NEW MEXICO F5

to black chert that weathers to a characteristic rusty brown. These 

basal beds are overlain by cliff-forming cherty gray limestone, thin 

beds of dark-colored shale, and minor amounts of grayish-orange 

to orange siltstone, sandstone, and conglomerate.

Sandy beds are present in the lower and upper parts of the limestone ; they are less common in the middle part. They are lenticular and grade laterally into arenaceous and argillaceous limestone; 

they range in texture from siltstone to conglomerate, and, in 

places, they appear to be channel deposits.

The top of the Los Moyos is the top of a cliff-forming calcarenite 

that in most places contains nodular masses of brown-weathering 

black chert.

Age and correlation. The lower 20 feet of the limestone contains Fusulinella cf. F. famula Thompson, 1948, Fusulinella aff. F. 

devexa Thompson, 1948, and a primitive species referred to the 

genus Wedekindellina. The occurrence of primitive species of 

Wedekindellina with Fusulinetta in the lowermost beds of the Los 

Moyos suggests that rocks of earliest Des Moinesian age are present in the Manzano Mountains. In the Joyita Hills, about 20 miles 

southwest, Kottlowski and Stewart (1970, fig. 5, p. 14, 29) reported that the lower part of their Des Moines sequence was 

missing. Somewhat higher but still in the basal beds are found 

Beedeina aff. B. arizonensis (Ross and Sabins), 1965, Eoschubertetta aff. E. bluensis Ross and Sabins, 1965, and other fusulinids 

that are apparently transitional between Fusulinella and Beedeina.

Fusulinids are generally sparse in the uppermost beds of the 

Los Moyos. Locally, Eowaeringella aff. E. ultimata (Newell and 

Keroher), 1937, has been found within 10 feet of the top; somewhat lower but still within 80 feet of the top, the fusulinids Beedeina cf. B. sulphurensis (Ross and Sabins), 1965, Beedeina novamexicana (Needham), 1937, Beedeina rockymontana (Roth and 

Skinner) 1930, Beedeina cf. B. bowiensis (Ross and Sabins) 1965, 

and Wedekindellina ellipsoides Dunbar and Henbest, 1942, have 

been found.

The Los Moyos was deposited during Des Moinesian and earliest 

Missourian time. It is approximately equivalent to the Strawn and 

Canyon (lowermost) Groups in north-central Texas and to the 

upper part of the Horquilla Limestone in southeast Arizona (Ross 

and Sabins, 1965). The Los Moyos is the lower gray limestone of 

Read, Wilpolt, Andrews, Summerson, and Wood (1944), the lower 

part of the Madera Limestone (Myers, 1966, 1967a, 1969, Myers 

and McKay, 1970, 1971, 1972), and is probably equivalent to the 

Gray Mesa Member of the Madera Limestone (Kelley and Wood, 

1946).
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F8 CONTRIBUTIONS TO STRATIGRAPHY

WILD COW FORMATION

The name Wild Cow Formation is here proposed for the sequence of rocks that overlies the Los Moyos Limestone and underlies the red-bed-limestone sequence of the Bursum Formation. 

Where the Bursum cannot be recognized, the red beds of the Abo 

Formation overlie the Wild Cow Formation. The Wild Cow consists of rhythmic sequences of arkosic sandstone and conglomerate, gray to yellow siltstone and shale, and thin- to thick-bedded 

gray limestone. It is divided into three members, in ascending 

order: Sol se Mete, Pine Shadow, and La Casa. The type section 

of the formation and its three members is designated as exposures 

on the west side of Priest Canyon in an east-draining ravine that 

cuts through a hogback in sec. 7, T. 3 N., R. 5 E., Valencia County, 

in the Torreon Southwest quadrangle (figs. 1, 2). Reference sections are in the Tajique quadrangle (fig. 2) and in the vicinity of 

Sol se Mete (fig. 2) in the northern part of the Manzano Mountains (Myers and McKay, 1970). The name is taken from Wild 

Cow Spring in the NE*4 sec. 19, T. 4 N., R. 5 E., Torrance County, in the southwestern part of the Torreon 15-minute quadrangle. 

It is the arkosic limestone member of the Madera Limestone (Read 

and others, 1944), it is probably equivalent to the Atrasado Member of the Madera Limestone (Kelley and Wood, 1946), and it is 

units B, C, and D of the upper part of the Madera Limestone 

(Myers, 1966,1967a, 1969; Myers and McKay, 1970,1971,1972).

SOL SE METE MEMBER

The basal sequence of rocks in the Wild Cow Formation is here 

named the Sol se Mete Member. The name is taken from a hill 

bearing that name in the SW^4 sec. 28, T. 9 N., R. 5 E., in the 

Mount Washington quadrangle, where there are good exposures. 

Inasmuch as Sol se Mete is on the Sandia Military Reservation and 

free access is not always possible, the type section is designated as 

exposures in Priest Canyon mentioned in the discussion of the 

Wild Cow Formation. The exposures on Sol se Mete are designated as a reference section.

The contact of the Sol se Mete Member with the underlying Los 

Moyos Limestone is marked by the base of a conglomerate, or 

coarse to fine sandstone, or siltstone. The thickness of the basal 

clastic unit ranges from about 15 to 100 feet or more. In many 

places the basal unit is arkosic and contains angular to subrounded 

fragments of metamorphic rock. Locally, petrified logs are common, some of which may be 8 feet or more in length. This basal 

conglomeratic unit is the Coyote Sandstone (Herrick, 1900, p. 

115) and is the Coyote Sandstone Member of the Madera. Inas-
MADERA GKOUP, MANZANO MOUNTAINS, NEW MEXICO F9

much as the Coyote is not a mappable unit, its use is herein 

abandoned.

The clastic unit is generally gradationally overlain by a poorly 

exposed sequence of calcareous gray shale that may contain 

nodules of limestone. Locally, near the top, minor amounts of red 

beds are present. The top of the member consists of 30-60 feet of 

gray limestone, locally cherty, that forms a cliff.

The thickness of the member averages about 200 feet, and it 

ranges from about 150 to about 300 feet. It appears to be thinnest in the southern part of the Manzano Mountains where much 

of the limestone has been replaced by siltstone and fine-grained 

sandstone.

The Sol se Mete contains species of Triticites that resemble 

those from the Canyon Group of north-central Texas (Myers, 

1960, 1967b) and from the Missourian Series of the midcontinent 

region. It is unit B of the upper part of the Madera Limestone 

(Myers, 1966,1967a, 1969; Myers and McKay, 1970,1971,1972).

PINE SHADOW MEMBER

The middle sequence of rocks in the Wild Cow Formation is 

here named Pine Shadow Member. The name is taken from Pine 

Shadow Spring near the head of Priest Canyon in the SW^ sec. 

16, T. 4 N., R. 5 E. The type section (fig. 2) is designated as exposures mentioned in the discussion of the Wild Cow Formation. 

Exposures near Sol se Mete (fig. 2; Myers and McKay, 1970, section 3) are designated as a reference section. In the central part 

of the Manzano Mountains, exposures in the Tajique quadrangle 

(Los Moyos section, fig. 2) are designated as reference section 

(Myers, 1966, section 5).

Throughout most of the Manzano Mountains, the base of the 

Pine Shadow is arkosic conglomerate that rests on the uppermost 

limestone of the Sol se Mete Member. The conglomerate, which 

weathers reddish brown, generally forms a steep slope and locally 

forms ledges. It is composed of cobble-sized rounded to subrounded fragments of metamorphic rocks in a poorly sorted 

arkosic matrix that contains fragments of fossil wood in many 

places. Bedding planes are commonly ripple marked. At the type 

section, and elsewhere in the southern part of the mountains, the 

basal unit is yellow to brown micaceous siltstone and fine sandstone that contains fragments of carbonized plant debris and 

sparse fragments of fossil wood. The basal clastic unit is generally 50-90 feet thick, although locally it may be as thin as 5 feet and 

as thick as 100 feet or more. The basal clastic beds are overlain
F10 CONTRIBUTIONS TO STRATIGRAPHY

by relatively thin beds of yellow to gray siltstone and minor 

amounts of shale that become calcareous toward the top.

The uppermost beds of the member are ledge to cliff forming. 

At the reference section near Sol se Mete (fig. 2), they consist of 

limestone in a single bed about 50 feet thick. Farther south, in 

the Tajique area, they consist of three beds of limestone separated 

by sandstone and calcareous shale, and at the type section they 

consist of two beds of limestone separated by siltstone. The limestone is mostly light-olive-gray calcarenite and is locally cherty. 

It is generally 50-70 feet thick but locally is as much as 130 feet 

thick. In the central and southern parts of the mountains, it forms 

a conspicuous bluff and locally forms a cliff.

The Pine Shadow Member contains species of Triticites that 

resemble those from the lower part of the Virgilian Series of the 

midcontinent region. The fusulinids have affinities to those from 

the Graham Formation of north-central Texas (Myers, 1960), to 

the faunas from the Gaptank Formation of west Texas (Ross, 

1965, beds G, H, I), and to the triticite fauna from the lower part 

of the Earp Formation in the Whetstone Mountains in southeast 

Arizona (Ross and Tyrrell, 1965). The Pine Shadow is unit C of 

the upper part of the upper Madera (Myers, 1966, 1967a, 1969; 

Myers and McKay, 1970,1971,1972).

LA CASA MEMBER

The sequence of rocks that overlies the Pine Shadow Member 

and underlies the Bursum Formation is here named the La Casa 

Member. The name is taken from La Casa Spring in the SW^4 

NE^4 sec. 6, T. 3 N., R. 5 E., Torreon quadrangle, Valencia County. The type section is the same as that for the Wild Cow Formation. The member, about 290 feet thick at the type section, is at 

the top of the Wild Cow Formation.

At the type section (fig. 2) the member, in ascending order, consists of about 120 feet of poorly exposed siltstone and shale, about 

100 feet of light-gray calcarenite, the lower 70 feet of which forms 

a pronounced ridge, and a thin sequence of red and gray shale and 

yellowish-green calcareous sandstone. The top of the member is a 

30-foot-thick bed of light-olive-gray calcarenite.

Farther north, the basal clastic beds are arkosic and locally a 

conglomerate. The beds are somewhat thinner than at the type 

section; in the Tajique area they are about 30 feet thick, and in 

the Sol se Mete area, about 50 feet thick. The 100-foot-thick bed 

of limestone mentioned in the preceding paragraph has been replaced by alternating sequences of limestone, siltstone, sandstone, 

and shale, and the top beds of the member have been stripped by
MADERA GROUP, MANZANO MOUNTAINS, NEW MEXICO Fil

recent erosion. The La Casa Member appears to thicken to the 

north, and if the preerosional surface were restored, the member 

would probably be about 320-350 feet thick in the vicinity of Sol 

se Mete.

The La Casa Member is unit D of the upper part of the upper 

Madera Limestone of Myers (1966, 1967a, 1969) and Myers and 

McKay (1970, 1971, 1972). Fusulinids from the member consist 

of species of Tritidtes that indicate deposition during middle and 

late Virgilian time. The member is approximately equivalent to 

the uppermost Graham and Thrifty Formations in north-central 

Texas, to the upper part of the Gaptank Formation in west Texas, 

and to the lower member of the Earp Formation in the Whetstone 

Mountains of Arizona (Ross and Tyrrell, 1965). Fusulinids similar to, but not conspecific with Tritidtes creekensis Thompson, 

1954, have been found in the uppermost beds of the member. The 

presence of these f usulinids suggests that the uppermost beds may 

be of earliest Wolfcamp age.

BURSUM FORMATION

The uppermost formation of the Madera Group, the Bursum, 

gradationally overlies the La Casa Member of the Wild Cow Formation. The Bursum was described (Wilpolt and others, 1946) 

for 28-234 feet of red and green shale, arkose, arkosic conglomerate, and gray limestone in the northern part of the Oscura Mountains. The limestone contains Schivagerina and obese Tritidtes 

ventricosus (Wilpolt and others, 1946).

In the southern part of the Manzano Mountains, the Bursum is 

a sequence of lenticular red, arkosic, hematitic sandstone, red and 

locally green shale, and greenish-gray calcarenite; it forms a gently sloping surface to the east and southeast. Exposures of the 

formation are generally poor, as most of it is masked by surficial 

deposits. The top of the Bursum is the top of the highest marine 

limestone that underlies the Abo Formation. The thickness is in 

excess of 100 feet in the Priest Canyon area.

Northward from Priest Canyon the formation either becomes 

thinner or is replaced by the overlying Abo Formation. In the 

vicinity of Red Canyon and in the Torreon 7 */% -minute quadrangle, 

the Bursum is not a mappable unit, and the beds have been included with the La Casa Member of the Wild Cow Formation.

In the northern half of the Manzano Mountains, the Bursum is 

absent in most places. Field evidence suggests that north of Pine 

Shadow Spring many of the red beds of the Bursum have been replaced by gray shale and limestone. If such replacement has oc-
F12 CONTRIBUTIONS TO STRATIGRAPHY

curred, then the uppermost beds of the La Casa Member include 

Bursum equivalents in the northern Manzano Mountains.

Fusulinids described by Thompson (1954, p. 18) include 

Schwagerina pinosensis Thompson, 1954, from the Bursum in 

Abo Canyon at the south end of the Manzano Mountains. On the 

basis of these and other fusulinids from the Bursum described by 

Thompson (1954), that formation is determined to be of Wolfcamp age.

REFERENCES CITED

Dunbar, C. 0., and Henbest, L. G., 1942, Pennsyjvanian Fusulinidae of

Illinois: Illinois Geol. Survey Bull. 67, 218 p. 

Gordon, C. H., 1907, Notes on the Pennsylvanian formations in the Rio

Grande Valley, New Mexico: Jour. Geology, v. 15, p. 805-816. 

Herrick, C. L., 1900, The geology of the white sands of New Mexico: Jour.

Geology, v. 8, p. 112-116. 

Kelley, V. C., and Wood, G. H., Jr., 1946, Lucero uplift, Valencia, Socorro,

and Bernalillo Counties, New Mexico: U.S. Geol. Survey Oil and Gas

Inv. Prelim. Map 47. 

Keyes, C. R., 1903, Geological sketch of New Mexico: Ores and metals, v.

12, p. 48. [Reference supplied by library, State Historical Society of

Colorado.] 

Kottlowaki, F. E., and Stewart, W. J., 1970, The Wolfcampian Joyita uplift

in central New Mexico: New Mexico Bur. Mines and Mineral Resources

Mem. 23, 82 p. 

Myers, P. A., I960, Stratigraphic distribution of some Pennsylvanian

Fusulinidae from Brown and Coleman Counties, Texas: U.S. Geol.

Survey Prof, Paper 315-C, p. 37-53.

 1966, Geologic map of the Tajique quadrangle, Torrance and Bernalillo Counties, New Mexico: U.S. Geol. Survey Geol. Quad. Map 

GQ-551.

 1967a, Geologic map of the Torreon quadrangle, Torrance County, 

New Mexico: U.S. Geol. Survey Geol. Quad. Map GQ-639.

 1967b, Fusulinidae from the Graford Formation and Winchell Limestone, Canyon Group, Upper Pennsylvanian, in Brown County, Texas: 

U.S. Geol. Survey Prof, Paper 573-C, 17 p.

 1969, Geologic map of the Escabosa quadrangle, Bernalillo County, 

New Mexico: U.S. Geol. Survey Geol. Quad. Map GQ-795.

Myeri, D. A., and McKay, E. J,, 1970, Geologic map of the Mount Washington quadrangle, Bernalillo and Valencia Counties, New Mexico: U.S. 

Geol, Survey Geol, Quad, Map GQ-886,

 1971, Geologic map of the Bosque Peak quadrangle, Torrance, Valencia, and BernaUlla Counties, New Mexico; U,S, Geol, Survey Geol. 

Quad, Map GQ-048,

 1972, Geologic map of the Capilla Peak quadrangle, Torrance and 

Valencia Counties, New Mexico i UJ, Geol, Survey Geol. Quad. Map 

GQ-1008.

Needham, C. E., 1937, Some New Mexico Fusulinidae: New Mexico Bur. 

Mines and Mineral Resources Bull. 14, 88 p.
MADERA GROUP, MANZANO MOUNTAINS, NEW MEXICO F13

Newell, N. D., and Keroher, R. P., 1937, The fusulinid, Wedekindettina, in 

mid-Pennsylvanian rocks of Kansas and Missouri: Jour. Paleontology, 

v. 11, no. 8, p. 698-705.

Read, C. B., Wilpolt, R. H., Andrews, D. A., Summerson, C. H., and Wood, 

6. H., Jr., 1944, Geologic map and stratigraphic sections of Permian 

and Pennsylvanian rocks of parts of San Miguel, Santa Fe, Sandoval, 

Bernalillo, Torrance, and Valencia Counties, north-central New Mexico: 

U.S. Geol. Survey Oil and Gas Inv. Prelim. Map 21.

Ross, C. A., 1965, Late Pennsylvanian Fusulinidae from the Gaptank Formation, west Texas: Jour. Paleontology, v. 39, no. 6, p. 1151-1176.

Ross, C. A., and Sabins, F. F., Jr., 1965, Early and Middle Pennsylvanian 

fusulinids from southeast Arizona: Jour. Paleontology, v. 39, no. 2, 

p. 173-209.

Ross, C. A., and Tyrrell, W. W., Jr., 1965, Pennsylvanian and Permian 

fusulinids from Whetstone Mountains, southeast Arizona: Jour. Paleontology, v. 39, no. 4, p. 615-635.

Roth, R. I., and Skinner, J. W., 1930, The fauna of the McCoy Formation, 

Pennsylvanian, of Colorado: Jour. Paleontology, v. 4, no. 2, p. 332-352.

Thompson, M. L., 1942, Pennsylvanian system in New Mexico: New Mexico 

Bur. Mines and Mineral Resources Bull. 17, 92 p.

 1948, Studies of American fusulinids: Kansas Univ. Paleont. Contr. 

4, Protozoa, art. 1, 184 p.

 1954, American Wolfcampian fusulinids: Kansas Univ. Paleont, 

Contr. 14, Protozoa, art. 5, 225 p.

Wilpolt, R. H., MacAlpin, A. J., Bates, R. L., and Vorbe, Georges, 1946, 

Geologic map and stratigraphic sections of Paleozoic rocks of Joyita 

Hills, Los Pinos Mountains, and northern Chupadera Mesa, Valencia, 

Torrance, and Socorro Counties, New Mexico: U.S. Geol. Survey Oil 

and Gas Inv. Prelim. Map 61.