Selected Annotated 

Bibliography of the Geology 

of Sandstone-type 

Uranium Deposits 

in the United States

GEOLOGICAL SURVEY BULLETIN 1059-C

This compilation was done on behalf 

of the U. S. Atomic Energy Commission 

and is published with the permission of 

the Commission

Selected Annotated 

Bibliography of the Geology 

of Sandstone-type 

Uranium Deposits 

in the United States

By ROBERT E. MELIN

SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY 

GEOLOGICAL SURVEY BULLETIN 1059-C

This compilation was done on behalf 

of the U.S. Atomic Energy Commission 

and is published with the Permission of 

the Commission

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1957
UNITED STATES DEPARTMENT OF THE INTERIOR 

FRED A. SEATON, Secretary

GEOLOGICAL SURVEY 

Thomas B. Nolan, Director

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

Office, Washington 25, D.G. - Price 33 cents (paper cover)
CONTENTS

Introduction.... _. _ .__. __ .._ .. _ 59

Explanation of the bibliography...... ............................ ........... 60

Bibliographies of uranium............................................................. 64

Annotated bibliography... ................................ . 65

Indexes.... ... .................................................................... 167

Authors................................................................................. 167

Subjects................................................................................ 170

Geographic areas. ..............-...... .................... .... 172

Formations......... ................................................................ 175

ILLUSTRATIONS

Page

FIGURE 4. Index map of the United States showing the location of 

some sandstone-type uranium deposits, groups of deposits, and districts..-.--...--..-...-_.............. ............ 62

III

SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

SELECTED ANNOTATED BIBLIOGRAPHY OF THE

GEOLOGY OF SANDSTONE-TYPE URANIUM DEPOSITS

IN THE UNITED STATES

By ROBERT E. MELIN

INTRODUCTION

Uranium is a vital and strategic metal in modern civilization. 

A large and steady supply of the fissionable material is essential 

to the use of atomic energy whether for peaceful or military 

purposes.

Today, uranium is mined in the United States principally from 

sandstone-type deposits such as those on the Colorado Plateau. 

In other parts of the world most uranium is mined from conglomerates as in the Witwatersrand of South Africa and the Blind 

River area of Ontario, Canada, and from vein-type deposits as at 

Shinkolobwe, Belgian Congo; Joachimsthal, Czechoslovakia; and 

at Great Bear Lake and Lake Athabaska in northern Canada.

Sandstone-type deposits of uranium and other metals are disseminated in continental sedimentary clastic rocks, and are localized primarily by stratigraphic rather than structural controls. 

The principal domestic source of uranium has been from sandstone-type uranium deposits on the Colorado Plateau where the 

bulk of uranium ore has been produced from the Chinle formation 

(Shinarump1 and sandstone members) of Triassic age and the 

Morrison formation of Jurassic age. These ores were mined first 

for radium, later for vanadium, and finally for uranium. Summaries of the geology of these deposits are given in reports by 

Fischer (1937, 1942, 1950, and 1955), Hess (1933), and Coffin 

(1921).

1 The Shinarump member of the Chinle formation now includes the strata fcxrmerly known 

as the Shinarump conglomerate.

59
60 SELECTED BIBLIOGRAPHIES OF TJEANITJM GEOLOGY

U. S. Geological Survey Map MR 2, by R. W. Schnabel (1955), 

shows the location of the more important uranium deposits in the 

United States, and U. S. Geological Survey Map MF 16, by W. I. 

Finch (1955), shows the location of deposits and occurrences of 

uranium on the Colorado Plateau.

The U. S. Geological Survey Bulletin 1030-A, "Search for uranium in the United States," by V. E. McKelvey (1955), is a report 

on the search for, and study of, uranium deposits and uraniferous 

rocks in the United States. The geology of many types of uranium 

deposits is reviewed, and the locations of the different types of 

deposits are indicated on small-scale base maps of the United 

States.

Irwin S. Parrish assisted the author in the compilation of the 

indexes and reviewed the entire report.

This compilation was done on behalf of the Division of Raw 

Materials of the U. S. Atomic Energy Commission.

EXPLANATION OF THE BIBLIOGRAPHY

The annotations in this bibliography are of selected reports 

that relate to the geology of sandstone-type uranium deposits in 

the United States that were available on June 30, 1955. Also 

included are pertinent reports contributed to the International 

Conference on Peaceful Uses of Atomic Energy, August 1955, 

at Geneva, Switzerland; these reports were published in 1956 by 

the United Nations as volume 6, "Geology of uranium and thorium," and were among those published by the U. S. Geological 

Survey as Professional Paper 300, "Contributions to the geology 

of uranium and thorium by the United States Geological Survey 

and Atomic Energy Commission for the United Nations International Conference on Peaceful Uses of Atomic Energy, Geneva, 

Switzerland, 1955."

The annotated reports have been selected on the basis of permanent value or interest. Because the Colorado Plateau is the 

center of the uranium mining industry in the United States, certain reports on the stratigraphy, structure, and general geology 

of parts of the Colorado Plateau have been included even though 

the discussions are not related directly to uranium deposits.

The annotations are arranged alphabetically by author; if an 

author has written more than one report, the reports are listed 

chronologically. Co-authors are indexed alphabetically under 

"Authors." The annotations are numbered consecutively for 

purposes of indexing.

The alphabetical indexes are an author index; a subject index;
BIBLIOGEAPHY OF SANDSTONE-TYPE TJBANTITM DEPOSITS 61

a geographical index of localities mentioned in the reports; and 

an index of formations. The numbers after each entry in an index 

correspond to the reference number. The index map shows the 

location of most areas mentioned in the annotations.

Geologic names listed are those of the various authors and do 

not necessarily follow the usage of the U. S. Geological Survey.
.58 62' . L_67_;.._.._ _ !

. . 

^Approximate boundary i 79. 

FIGURE 4. Index map of the United States showing the location of uranium-bearing sa

districts. For annotations concerning these localities see 
Localities shown in figure 4

Hawthorne area, Lincoln County, Nev.... 1

Lander County, Nev.. ....... 2

Virgin Valley opal district........ 3

Lyon County, Nev............................. 4

Tonopah area, Esmeralda County, Nev. 5 

Clark County, Nev.---------- . 6

Olancha, Calif. _ ._.........._.- ..-.. 7

Rosamond prospect ......... ---------- ..... 8

Taft-McKittrick area ---------- - 9

Ridenour mine . .-. ._ ... 10 

Aguila area ..-.- .......................... 11

Red Bluff prospect.....____..._-----__-. 12

Cameron area .. 13

Monument Valley (includes Copper Canyon, 

Hunts Mesa, Nokai Mesa, Hoskinninni Mesa 

and Monument No. 1, Monument No. 2, 

Skyline and Whirlwind mines) .. ..... 14

Black Mesa ._................................ 15

Carrizo Mountains area.-.----------.---------- 16

Chuska Mountains, Red Rock district and 

Lukachukai Mountains areas (includes Mesa 

V, Mesa VI, and Mesa VII mines)-------- 17

Cove Mesa and Kinusta Mesa areas. .-_ 18 

San as tee area, Grants district---.------------ 19

Becenti, Butler, Diamond 2, and Hogback 4 

mines, Grants district.- --- - - ... 20

Dakota, Silver Spur, Small Stake, and Section 9 mines, Grants district............ .. 21

Jackpile and Woodrow mines, Grants district 22 

Datil area .......... .-.. - 23

Guadalupita Coyote district .-........ 24

Colordo Plateau ..__............... ....... 25

Mike Doyle prospect. - - - 26

Shirley May Mine - 27 

Lucky Strike claim, Troublesome Creek area 28 

Meeker area ...... . - ............ 29

Skull Creek area... --.----.. ________________ 

Rifle and Garfield mines._._...______ 

Graysill mine, Placerville area............._ 

Uravan mineral belt (includes Atkinson 

Creek quadrangle, Bull Canyon quadrangle, 

Egnar-Gypsum Valley quadrangle, Gateway 

area, Long Park, Paradox Valley, Pine 

Mountain quadrangle, Roc Creek and 

Uravan district) . __....._ 

La Sal Creek and Wray Mesa (includes Gray 

Dawn mine) _ .. -- _ 

Big Indian Wash Lisbon Valley area (includes Mi Vida mine, Big Buck mine. 

Purple Paint claim, and Small Fry Claim) 

Montezuma Canyon ..... .................... 

Blanding district . .. .--.-.............. 

Happy Jack mine, White Canyon district .. 

Circle Cliffs area (includes Hot Shot and 

Yellow Jacket mines)..-.-................... 

Trachyte district, Henry Mountains...-..---. 

Bulloch group .... . ...... 

Silver Reef (Harrisburg) district, (includes 

Chloride Chief and Silver Point claims).... 

Capitol Reef (includes Oyler mine, Fruita 

area) ----__.______ --. __________ 

Little Wild Horse Mesa ..._...__________.__ 

San Rafael Swell (includes Brown Throne, 

Clifford Smith, Dalton, Dirty Devil, Dolly, 

Green Vein, Hard Pan, Hertz, Lone Tree, 

Pay Day, South Fork, and Wickiup claims, 

and Temple Mountain district) ..-..__._ 

Area southwest of Green River _____. 

"C" Group _____.__._______-----..---_ 

Indian Creek Lockhart Canyon area. __ 

Richardson area, Moab district........._.... 

Shinarump No. 1 mine, Seven Mile Canyon 
64 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

BIBLIOGRAPHIES OF URANIUM

Bibliographies that contain additional references to sandstonetype uranium deposits are listed below:

Alien, R. E., 1953, Uranium and its compounds, a bibliography 

of unclassified literature: U. S. Atomic Energy Comm. 

TID-3041, issued by U. S. Atomic Energy Comm. Tech. Inf. 

Service, Oak Ridge, Tenn.

Cooper, Margaret, 1953, Bibliography and index of literature 

on uranium and thorium and radioactive occurrences in 

the United States Part 1, Arizona, Nevada, and New 

Mexico: Geol. Soc. America Bull, v. 64, no. 2, p. 197-234.

Cooper, Margaret, 1953, Bibliography and index of literature on 

uranium and thorium and radioactive occurrences in the 

United States Part 2, California, Idaho, Montana, 

Oregon, Washington, and Wyoming: Geol. Soc. America 

Bull., v. 64, no. 10, p. 1103-1172.

Cooper, Margaret, 1954, Bibliography and index of literature 

on uranium and thorium and radioactive occurrences in the 

United States Part 3, Colorado and Utah: Geol. Soc. 

America Bull., v. 65, no. 6, p. 467-590.

Cooper, Margaret, 1955, Bibliography and index of literature on 

uranium and thorium and radioactive occurrences in the 

United States Part 4, Arkansas, Iowa, Kansas, Louisiana, Minnesota, Missouri, Nebraska, North Dakota, Oklahoma, South Dakota, and Texas: Geol. Soc. America Bull, 

v. 66, no. 3, p. 257-326.

Cooper, Margaret, 1953, Selected bibliography on uranium 

exploration and the geology of uranium deposits: U. S. 

Atomic Energy Comm. RME-4007, issued by U. S. Atomic 

Energy Comm. Tech Inf. Service, Oak Ridge, Tenn.

Postell, P. E., and Voress, H. E., 1953, Unclassified bibliographies of interest to the atomic energy program: U. S. 

Atomic Energy Comm. TID-3043, issued by U. S. Atomic 

Energy Comm. Tech. Inf. Service, Oak Ridge, Tenn.

Wallace, J. H., and Smith, H. B., 1955, Bibliography of U. S. 

Geological Survey trace elements and related reports to 

June 1, 1954: U. S. Geol. Survey Bull. 1019-B, p. 63-144.
BIBLIOGRAPHY OF SANDSTONE-TYPE UKANIUM DEPOSITS 65

ANNOTATED BIBLIOGRAPHY

Anderson, E. C., 1955, Occurrences of uranium ores in New Mexico:

N. Mex. Bur. Mines and Min. Res. Circ. 29,38 p. 

This publication is a directory of the uranium mines and prospects 

in New Mexico. The name, location, and ownership of the mines and 

prospects are given, and the lithology and host formation of each 

are indicated. The mines and prospects are indicated on a map of 

New Mexico at a scale of about 1:2,500,000. Occurrences in a number 

of counties are reported, and uranium minerals and guides to ore 

are listed.

Argall, G. 0., Jr., 1943, The occurrences and production of vanadium: 

Colo. School Mines Quart., v. 38, no. 4, 56 p.

This paper is a comprehensive study of vanadium, with emphasis 

upon the vanadium deposits of the Colorado Plateau. It describes the 

history, uses, production, occurrence, mining, and milling of vanadium 

and its ores. Because earnotite, one of the most important vanadium 

minerals in the deposits on the Colorado Plateau, also contains 

uranium, this report refers in part to uranium. The deposits occur 

mostly in sandstone of the Shinarump conglomerate of Triassic age 

and the Entrada and Morrison formations of Jurassic age. The widely 

scattered ore bodies form irregularly tebular masses that lie almost 

parallel to the sandstone beds, but do not coincide with the beds in 

detail. The ore occurs in lenses, flat tabular bodies, in well-defined 

channels, in rolls, and as zones of ore surrounding trees whose original 

constitutients have been replaced by silica or calcite or both.

The vanadium is recovered from carnotite by roasting the crushed 

ore with common salt in order to convert the vanadium to a watersoluble sodium vanadate. The calcine is then leached with water, 

and the vanadium is precipitated from solution by adjustment of the 

pH. Variations of this process are used for different types of sandstone ore. If the ore contains more than 6 percent of lime it is neutralized with acid before roasting.

An extensive bibliography on vanadium is included.

Argall, G. 0., Jr., 1954, Why Anaconda's uranium mines are unique:

Min. World, v. 16, no. 10, p. 54-59.

This report outlines the exploration and mining procedures used 

by the Anaconda Copper Mining Company in its uranium operations 

in the Grants district, New Mexico. The ore body at the Jackpile 

mine is in the Westwater Canyon member of the Morrison formation 

of Jurassic age, and is partly overlain by and partly cut by a post-ore 

diabase sill that is from 3 to 7 feet thick. The deposit is being mined 

by open-pit methods. The uranium deposit at the Woodrow mine 

occurs in the Morrison formation in a "ring fault" or "breccia pipe." 

The structure has the shape of an upright though slightly tilted 

cone with a diameter of about 30 feet at the surface. The central 

part has apparently dropped about 15 feet. The ore minerals, which 

are principally uraninite and coffinite, are associated with pyrite 

and asphaltic material.

Bain, G. W., 1950, Geology of the fissionable materials: Econ. Geology, 

v. 45, no. 4, p. 273-323.
66 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

Mineralogic and geologic characteristics of deposits of uranium and 

thorium are discussed. Occurrences are classified under primary or 

hypogene types, sedimentary or bedded deposits, and oxidized bodies. 

Primary deposits are now the principal source of supply, but all 

varieties of sedimentary occurrences give promise of large sustained 

production. Geology and resources of producing areas or potentially 

producing areas of the world are reviewed.

5 Bain, G. W., 1952, Uranium deposits in southwestern Colorado 

Plateau: U. S. Atomic Energy Comm. RMO-982(rev.) 59 p. 

issued by U. S. Atomic Energy Comm. Tech. Inf. Service, Oak 

Ridge, Tenn.

Part of the southwestern Colorado Plateau was studied to test 

results from experimental simulation of Colorado Plateau-type 

uranium deposits. The sedimentation pattern of the Shinarump 

conglomerate of Triassic age and the ore occurrences conform to 

laboratory experiments.

Almost all the uranium in the Shinarump is in a jasperoid conglomerate in the lowest part of ancient stream channels. Bain asserts 

that the uranium was originally contained in the jasperoid pebbles.

The deposits can be geographically zoned on the basis of their 

mineralogic character into an eastern vanadium-excessive zone, a 

central vanadium-sufficient zone, and a western and southern vanadium-deficient zone.

Many mines, prospects, and occurrences are described, including 

the Graysill mine near Placerville, Colo., the Monument No. 1, Monument No. 2, Skyline, and Whirlwind mines in the Monument Valley 

district, and the Yellow Jacket and Hot Shot mines in the Circle Cliffs 

area. The Graysill mine is a vanadium deposit in the Entrada formation of Jurassic age, and the other mines are uranium or vanadiumuranium deposits, in channel sediments of the Shinarump.

6 Bain, G. W., 1952, Uranium in the Dirty Devil Shinarump channel

deposit: U. S. Atomic Energy Comm. RMO-66, 40 p. issued by

U. S. Atomic Energy Comm. Tech. Inf. Service, Oak Ridge, Tenn.

Uranium occurs in the Shinarump conglomerate of Triassic age at

the Dirty Devil No. 6 mine, Emery County, Utah. The deposit is in

conglomeratic sediments which fill a channel cut into the underlying

Moenkopi formation of Triassic age. Although carnotite and tyuyamunite are present, hydrocarbons apparently contain most of the

uranium. Base-metal sulfides also are present. Bain suggests that

the uranium in the deposit was derived from jasperoid pebbles in the

Triassic river gravels, and that the pebbles were derived from a

leptothermal uranium deposit.

7 Baker, A. A., 1933, Geology and oil possibilities of the Moab district, 

Grand and San Juan Counties, Utah: U. S. Geol. Survey Bull. 

841, 95 p.

Exposed sedimentary formations in the Moab district range in 

age from Early Pennsylvanian to Late Cretaceous. Rock types include evaporites., limestone, shale, mudstone, sandstone, arkose, and 

conglomerate. One small igneous plug is present. The beds have 

been folded into low anticlines and shallow synclines during several
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 67

periods of deformation. Some of this deformation is due to the 

intrusion of salt plugs. The beds are cut by numerous small normal 

faults. The report includes a geologic map and a geologic structure 

map of the area at a scale of 1:62,500.

Disseminated deposits of uranium and vanadium minerals in the 

area are irregularly distributed in the Salt Wash sandstone member 

of the Morrison formation of Jurassic age.

Baker, A. A., 1935, Geologic structure of southeastern Utah: Am. 

Assoc. Petroleum Geologists Bull., v. 19, no. 10, p. 1472-1507. 

Southeastern Utah, lying within the Colorado Plateau, is characterized by several types of structural features, including (a) huge 

asymmetrical upwarps, (b) domes associated with laccolithic intrusions, (c) the southern edge of the Uinta Basin structural depression, 

(d) a north-trending zone of normal faults at the west edge of the 

Plateau, and (e) a group of numerous folds, faults, and faulted 

folds that are found in a limited area near Moab. Folding has occurred 

in the region several times since the end of the Mississippian, but 

the principal deformation that is reflected in the structure of the 

surface rocks took place at the end of the Cretaceous or early in 

the Tertiary and, therefore, was related to the Laramide orogeny. 

The large domical uplifts have a northerly trend and are strongly 

asymmetric, with the steep limb toward the east; they were formed 

at the end of the Cretaceous, possibly as a reflection in the surface 

rocks of more or less vertical uplifting along deep-seated reverse 

faults. The group of numerous smaller folds, faults, and faulted 

anticlines in the part of the region near Maob also is belived to have 

been formed near the end of the Cretaceous; the deformation is obviously related to the presence of the plastic salt-bearing beds of 

the Pennsylvanian Paradox formation beneath the surface rocks, because the structural features of this type near Moab are typically 

developed only within the area underlain by the Paradox formation 

and because the salt-bearing beds have been intruded into the overlying rocks at the crests of some of the folds. Events in the Tertiary 

structural history of the region include the intrusion of igneous 

rocks in four isolated, mountain groups, the downwarping of the 

Uinta Basin, and the development of the zone of normal faults at 

the west edge of the plateau; it is not possible to determine the 

order of these events, or to determine whether they represent different modes of expression of one period of crustal disturbance. 

 Author's abstract

Baker, A. A., 1936, Geology of the Monument Valley, Navajo Mountain region, San Juan County, Utah: U. S. Geol. Survey Bull. 

865, 106 p.

The geology of an area in southeastern Utah is described. Exposed sedimentary formations range in age from Pennsylvanian to 

Quaternary, have an aggregate average thickness of about 8,000 

feet, and most are of continental origin. Small volcanic necks and 

dikes of Tertiary age crop out at three places. The principal geological structure is a gentle westerly dip off of the Monument upwarp, but this is interrupted by several small transverse folds and 

the large dome of Navajo Mountain. The report includes a geologic map of the area at a scale of 1 : 96,000.
DO SELECTED BIBLIOGKAPHIES OF URANIUM GEOLOGY

Small copper deposits (and more recently uranium deposits) have 

been found in this area in the Shinarump conglomerate of Triassic 

age.

10 Baker, A. A., 1946, Geology of the Green River Desert, Cataract 

Canyon region, Emery, Wayne, and Garfield Counties, Utah: 

U. S. Geol. Survey Bull. 951,122 p.

Exposed formations in this region range in age from Pennsylvanian 

to Late Cretaceous and have an aggregate thickness of about 6,500 

feet. The rocks consist of interbedded marine and continental sedimentary formations; the formations are described. The most conspicuous structural feature in the area is the steeply dipping monocline along the east side of the San Rafael Swell. The southern 

part of the area includes part of the gently dipping northern end of 

the Monument up warp. The rocks are broken by numerous small 

normal faults, of which most have small displacements. The report includes a geologic map and a structural geologic map of the 

region at a scale of 1 : 62,500.

Uranium and vanadium deposits in the area include those at Temple 

Mountain in the Shinarump conglomerate of Triassic age and those 

southwest of Green River, which are in the Salt Wash member of 

the Morrison formation of Jurassic age.

11 Baker, A. A., Dane, C. H., and Reeside, J. B., Jr., 1936, Correlation 

of Jurassic formations of parts of Utah, Arizona, New Mexico, 

and Colorado: U. S. Geol. Survey Prof. Paper 183, 66 p. 

Jurassic formations on the Colorado Plateau and adjacent areas 

are described, redefined, and correlated. The rock units are subdivided into the Glen Canyon group (Wingate sandstone, Kayenta 

formation, Navajo sandstone), the San Rafael group (Carmel formation, Entrada sandstone, Curtis formation, Summerville formation), 

and the Morrison formation. Ten series of columnar sections are 

presented and discussed, the distribution and thickness of the formations are shown, and the conditions of deposition are interpreted.

12 Baker, A. A., Dane, C. H., and Reeside, J. B., Jr., 1947, Revised 

correlations of Jurassic formations of parts of Utah, Arizona, 

New Mexico, and Colorado: Am. Assoc. Petroleum Geologists 

Bull., v. 31, no. 9, p. 1664-1668.

The authors have modified the correlations proposed in their paper 

of 1936. The most important change concerns the Wingate and 

Entrada sandstones. The Wingate sandstone at its type locality at 

Fort Wingate, N. Mex., is now correlated with the Entrada. It is 

proposed that the name Wingate be retained for the sandstone forming the lower part of the Glen Canyon group, with the understanding that the original type locality of the Wingate be abandoned.

13 Bales, W. E., Bell, Henry, and Wilmarth, V. R., 1953, Uraniumvanadium deposits near Edgemont, Fall River County, S. Dak., 

[abs.]: Geol. Soc. America Bull., v. 64, no. 12, p. 1540. 

Uranium and vanadium minerals were found near Edgemont, Fall 

River County, in the southern part of the Black Hills, South Dakota, 

in the Lakota and Fall River sandstones of the Inyan Kara group
BIBLIOGRAPHY OF SANDSTONE-TYPE UKANIUM DEPOSITS 69

(Early Cretaceous). Uranium occurrences are known in the Deadwood formation and Minnelusa sandstone (Paleozoic) and have been 

reported from the Pierre shale (Late Cretaceous). Most highgrade deposits are in an area of approximately 20 square miles on 

the gently dipping southwest flank of the Black Hills uplift. Minor 

northward-trending anticlines lie east and west of the known mineralized area. These folds may be related to northward-trending 

shear zones of complex structure in the Precambrian rocks that 

crop out about 10 miles to the north.

The ore bodies apparently were localized by (1) thin bedding 

rather than massiveness of the sandstone beds, (2) local changes 

in dip, (3) minor faults, and (4) fracture zones.

The ore minerals are carnotite, tyuyamunite, rauvite(?), hewettite, metahewettite, autunite, and other unidentified uranium minerals. They form fracture fillings and disseminations through sandstones and shales, with a gangue of calcite, gypsum, and limonite.

Geologic guides useful in prospecting for uranium in the Edgemont area are (1) a brick-red staining of the sandstone near deposits of uranium and vanadium minerals, (2) abrupt, local changes 

of dip, (3) thin-bedded rather than thick-bedded sandstone, 

(4) abundant organic material in sedimentary rocks, and (5) proximity to northward-trending fracture zones. Authors' abstract

14 Barrett, D. C., 1953, Preliminary report of reconnaissance in the 

Bighorn Basin, north-central Wyoming and south-central Montana: U. S. Atomic Energy Comrn. RME-4027, 19 p., issued by 

U. S. Atomic Energy Comm. Tech. Inf. Service, Oak Ridge, 

Tenn.

Airborne and ground reconnaissance for uranium was conducted in 

the Bighorn Basin. No occurrences of economic importance were 

found. Sedimentary rocks ranging in age from Cambrian to lower 

Tertiary are exposed in the structural and topographic Bighorn 

Basin. Small occurrences of uranium were found in the Flathead 

sandstone of Cambrian age, the Chugwater formation of Triassic 

age, the Morrison and Cloverly formations of Jurassic and Cretaceous age, the Frontier and Mesaverde formations of Cretaceous 

age, and in the Wasatch formation of Eocene age.

15 Behre, C. H., Jr., and Barton, P. B., Jr., 1953, Progress report on 

interpretation and valuation of uranium occurrences in the Bird 

Spring and adjacent mining districts, Nevada: U. S. Atomic 

Energy Comm. RME-3057, 7 p., issued by U. S. Atomic Energy 

Comm. Tech. Inf. Service, Oak Ridge, Tenn.

Uranium occurrences in the Bird Spring and Spring Mountain 

Ranges, Clark County, Nev., are regionally and structurally of 

three types: (1) along fractures in a sandy zone in the Kaibab formation of Permian age; (2) in fractures and cement of Tertiary 

lavas, tuffs, and gravels and the immediately underlying Paleozoic 

rocks; and (3) in the oxidized parts of cupiferous and ferruginous 

fissure veins and replacement deposits. None of these occurrences 

is economically important.
70 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

16 Behre, C. H., Jr., and Barton, P. B., Jr., 1954, Interpretation and 

valuation of uranium occurrences in the Bird Spring and adjacent 

mining districts, Nevada: U. S. Atomic Energy Comm. RME3091, 35 p., issued by U. S. Atomic Energy Comm. Tech. Inf. 

Service, Oak Ridge, Tenn.

Uranium occurrences in the region southwest of Las Vegas, Clark 

County, Nev., are of two types: (1) those associated with basemetal vein deposits and (2) those occurring as superficial nearsurface disseminations and fracture coatings.

Small deposits of the second type are distributed widely in the 

area in Tertiary(?) tuffs and gravels and in Pennsylvanian and 

Permian sedimentary rocks. The uranium was probably derived 

from tuffs formerly overlying the area. Most of the occurrences 

are in cuts along the railroad, and none has present economic significance.

The uranium deposits in the base-metal mines are also described. 

These may have a different origin from the second type of deposits, 

and they merit further study.

17 Bell, Henry, 3d, Gott, G. B., Post, E. V., and Schnabel, R. W., 1956, 

Lithologic, structural, and geochemical controls of uranium deposition in the southern Black Hills, South Dakota: U. S. Geol. 

Survey Prof. Paper 300, p. 345-349; Geology of uranium and 

thorium, United Nations, v. 6, p. 407-411.

The uranium deposits in the southern part of the Black Hills in 

South Dakota occur in non-marine sandstone beds in the Inyan Kara 

group of Early Cretaceous age. The rocks in the area dip generally 

southward away from the Black Hills uplift. The principal ore 

minerals are carnotite and tyuyamunite; lesser amounts of corvusite and rauvite are present. Factors that influenced the localization of the uranium deposits include the lithologic, structural, and 

geochemical environments.

Uranium deposits have been found in three types of sandstone. 

They are a fine-grained sandstone, generally less than 5 feet thick, 

interbedded with laminated carbonaceous siltstone; a thick crossbedded noncarbonaceous sandstone, generally fine-to medium-grained, 

with many scour and fill structures; and lenses of fine-grained homogeneous sandstone separated by thin beds of mudstone.

Uranium deposits are most numerous in areas of abrupt changes 

in dip or in areas where abnormally low dips coincide with favorable 

lithologies. Most of the deposits have a halo of purplish-pink iron 

oxide stain, and, in a few deposits, a spatial relationship exists between carbonate-cemented sandstone and uranium minerals.

18 Benson, W. E., Trites, A. F., Jr., Beroni, E. P., and Feager, J. A., 

1952, Preliminary report on the White Canyon area, San Juan 

County, Utah: U. S. Geol. Survey Circ. 217, 10 p. 

Copper-uranium deposits in the White Canyon area in southeast 

Utah occur mostly in the Shinarump conglomerate of Triassic age, 

but some have also been found in the Moenkopi and Chinle formations, also of Triassic age. More than 2,000 feet of sedimentary 

rocks that range in age from Carboniferous to Jurassic(?) are 

present. The regional dip is l°-2° SW., and jointing is prominent
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 71

in some places. The Shiriarump conglomerate consists of lenticular 

beds of sandstone, conglomeratic sandstone, clay, and siltstone. Plant 

remains are common in the rocks that, fill channels cut into the underlying Moenkopi formation. The thickness of the Shinarump conglomerate ranges from a feather edge up to 75 feet. The largest 

concentrations of copper and uranium minerals occur in the lower 

part of the Shinarump conglomerate and seem to be controlled by 

ancient channel fills, fractures, and by carbonaceous material and 

clay. Unoxidized minerals include pitchblende and base-metal sulfides; 

oxidized copper and uranium minerals are found near the outcrops. 

The origin of the deposits is not knovm but is thought by the authors 

to be hydrothermal. The age of pitchblende from the Happy Jack mine, 

determined by the lead-uranium method, is 55 to 60 million years.

19 Beroni, E. P., 1954, Permian red-bed deposits, southwestern Oklahoma; in Geological investigations of radioactive deposits, Semiannual progress report, June 1 to November 30, 1954: U. S. 

Geol. Survey TEI-490, p. 213-216., issued by U. S. Atomic Energy 

Comm. Tech. Inf. Service, Oak Ridge, Tenn.

The most promising uranium-bearing localities in Oklahoma are 

in the Permian Red Beds in Tillman, Cotton, and Jefferson Counties. 

At a property in Cotton County a uranium-bearing zone about 25 

feet long and 2 to 4 feet thick is in a sandstone lens about 300 feet 

wide, 25 feet thick and 600 feet long. The lens projects about 10 

feet into the underlying rocks, and the mineralized zone is in this 

lower 10 feet.

20 Beroni, E. P., and King, R. U., 1952, The Mike Doyle carnotite deposit, El Paso County, Colo.: U. S. Geol. Survey TEM-133A, 

6 p., issued by U. S. Atomic Energy Comm. Tech. Inf. Service, 

Oak Ridge, Tenn.

The Mike Doyle carnotite prospect is located on a hogback in the 

foothills of the Colorado Front Range about 10 miles south of Colorado Springs. Carnotite occurs as coatings on fracture surfaces and 

on carbonized wood fragments in quartzitic sandstone of the Morrison formation of Jurassic age. The sandstone is commonly silicified along fractures, especially whesre carnotite is present, and the 

fractures contain slickensided iron-stained gouge. Uranium-bearing 

material also occurs in a carbonaceous shale underlying the sandstone. Samples of the rock contained from 0.052 to 0.068 percent 

uranium.

21 Beroni, E. P., and McKeown, F. A., 1952, Reconnaissance for urantferous rocks in northwestern Colorado, southwestern Wyoming, 

and northeastern Utah: U. S. Geol. Survey TEI-308A, 41 p., 

issued by U. S. Atomic Energy Comm. Tech. Inf. Service, Oak 

Ridge, Tenn.

A reconnaissance for uraniferous rocks was conducted in adjacent 

parts of Colorado, Wyoming, and Utah. No deposits were found 

that are commercially exploitable under present conditions.

Small copper-uranium deposits are associated with fossil plant 

material in sandstone and shale of the Uinta formation of Eocene 

age in the Uinta Basin in Utah; samples contained as much as 

0.01 percent uranium. A fresh-water limestone also in the Uinta 

formation, contained 0.019 percent uranium. The uranium deposits
72 SELECTED BIBLIOGRAPHIES OF UKANIUM GEOLOGY

at the Snow and Bonniebell claims, Uintah County, Utah, are in 

sandstone of the Mesaverde formation of Late Cretaceous age; 

samples contained as much as 0.09 percent uranium. Copper-uranium 

deposits near Skull Creek, Moffat County, Colo., are in sandstone 

of the Entrada and Curtis formations of Jurassic age and are associated with carbonaceous material; samples contained as much as 

0.16 percent uranium. The uranium deposits at the Lucky Strike 

claims, Grand County, Colo., are associated with iron and manganese 

stains on sandstone and clay of the North Park formation of Miocene(?) age; one sample contained 0.016 percent uranium. The 

uranium deposits at the Fair-U claims, Routt County, Colo., are in 

Precambrian crystalline rocks and contain as much as 0.04 percent 

uranium.

22 Beroni, E. P., McKeown, F. A., Stugard, Frederick, Jr., and Gott, 

G. B., 1953, Uranium deposits of the Bulloch group of claims, 

Kane County, Utah: U. S. Geol. Survey Circ. 239, 9p. 

Uranium deposits occur near the contact of the Dakota formation 

of Cretaceous age with the Summerville formation of Jurassic age 

on the Bulloch group of claims in southwest Utah. The area is part 

of the Markagunt fault block, and the rocks dip about 5° NE. 

Uranium minerals are finely disseminated in clay, fossil carbonaceous material, and in sandstone and conglomerate. Carnotite, tyuyamunite, and autunite were recognized, but another mineral (unidentified) probably contains most of the uranium. The deposits are 

small and of marginal grade. The uranium probably has been recently deposited or redistributed by ground water.

23 Black, R. A., 1956, Geophysical exploration for uranium on the Colorado Plateau: U. S. Geol. Survey Prof. Paper 300, p. 721-726; 

Geology of uranium and thorium, United Nations, v. 6, p. 766-771.

Geophysical investigations, other than radiometric, have been conducted in the Colorado Plateau region by both federal agencies and 

private contractors to test the applicability of standard geophysical 

methods in exploration for uranium. Field tests have been made of 

electrical, seismic, magnetic, gravimetric, and electromagnetic 

methods. Although the uranium deposits are found in many different stratigraphic horizons, most of the geophysical work has 

been in areas where the uranium is concentrated in the Morrison 

formation of Jurassic age and the Shinarump conglomerate of Triassic age.

Methods so far tested have not proved capable of directly detecting the uranium minerals because of the small percent of uranium 

ore in relation to the amount of host rock, but some have proved to 

be of value in the detection and delineation of such geologic guides 

to ore as thickening of the ore-bearing Salt Wash member of the 

Morrison formation and the channels filled with the Shinarump 

conglomerate.

24 Boardman, R. L., Ekren, E. B., and Bowers, H. E., 1956, Sedimentary features of upper sandstone lenses of the Salt Wash member and their relations, to uranium-vanadium deposits in the 

Uravan district, Montrose County, Colorado: U. S. Geol. Survey 

Prof. Paper 300, p. 221-226; Geology of uranium and thorium, 

United Nations, v. 6, p. 331-334.
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 73

A detailed study of the upper sandstone lenses of the Salt Wash 

member of the Morrison formation of Jurassic age in the Uravan 

district gives a general picture of the deposition, extent, and structure of these sandstone lenses and of the relation of sedimentary 

features to ore features throughout the area.

The individual sandstone lenses are commonly enclosed by relatively impermeable mudstone beds and are not extensive regional 

aquifers. The sedimentary trends in the Uravan district are, in 

general, east. The long axes of the ore bodies and the trends of 

favorable ground are nearly parallel to the strike of the sedimentary features. No direct correlation exists between fractures and 

faults related to regional structures and trends, or to features 

related to ore.

25 Bodine, M. W., Jr., 1954, Mineralogy of the Carlile deposit, Crook 

County, Wyo.; in Annual report for June 30, 1953 to April 1, 

1954, Columbia University, New York, New York; U. S. Atomic 

Energy Comm. RME-3096 (Pt. 1), p. 16-35, issued by U.S. 

Atomic Energy Comm. Tech. Inf. Service, Oak Ridge, Tenn. 

The Carlile uranium deposit is in the Lakota sandstone, the basal 

member of the Inyan Kara group of Early Cretaceous age. The 

area is on the northwest slope of the Black Hills uplift; the regional 

dip is about 3° NW. Carnotite is disseminated in the basal 8 feet 

of the upper sandstone unit of the Lakota sandstone, and is associated with, and forms halos around, fossilized carbonaceous material. The host rock is cross bedded and overlies a dense, impervious 

mudstone. An ore body in a slump block below and east of the 

open-pit and underground mine on the rim appears to have been once 

a part of the upper ore body. Coffinite(?), doloresite( ?), and rauvite(?) have been tentatively identified in specimens of carbonized 

wood from the deposit; also present are carnotite, metarossite, 

pyrite, aluminite, limonite, gypsum, calcite, manganese oxides, and 

alum minerals. Calcite, the original cement of the sandstone, has 

been almost completely removed. Secondary quartz overgrowths 

formed on quartz grains after removal of the calcite; later, carnotite 

and limonite coated and partially replaced the quartz grains and 

overgrowths.

26 Boutwell, J. M., 1905, Vanadium and uranium in southeastern Utah:

U. S. Geol. Survey Bull. 260, p. 200-210.

Uranium and vanadium deposits in certain areas in Utah are 

described. The deposits near Richardson contain carnotite and other 

vanadium minerals. The minerals coat fractures and impregnate 

or replace the sandstone host rock along a fracture zone. The host 

formation is probably of Jurassic age. The carnotite deposits about 

15 miles southwest of Green River are probably also in rocks of 

Jurassic age. The mineral impregnates the sandstone and is in close 

association with carbonaceous material. Several other uranium and 

vanadium deposits in the region have been reported.

27 Boyle, T. L., 1956, Airborne radiometric surveying: Geology of

uranium and thorium, United Nations, v. 6, p. 744-747. 

Established procedures and techniques of aerial prospecting, using 

light aircraft equipped with scintillation counters, designed to detect 

the emissions of gamma radiation by uranium daughter products,
74 . , SELECTED BIBLIOGRAPHIES OF URAXIUM GEOLOGY

are discussed. Flight elevations of 50 to 100 feet at an air speed of 

; 70 miles per hour have proved the most effective mode of flight.

Flight techniques used in airborne prospecting are applicable only 

,to exposed and nearly exposed mineralization and do not eliminate 

the need for .ground prospecting. A mantle of from 2 to 4 feet of 

barren soil will effectively absorb gamma radiation.

 28 Branson, C. C., Burwell, A. L., and Chase, G. C., 1955, Uranium in 

Oklahoma, 1955: Okla. Geol. Survey, Mineral Kept. 27, 22 p.

Uranium in Oklahoma occurs in sandstone lenses in Permian red 

beds, in asphaltic pellets, in phosphatic black shales, in oil field 

brines, and in some thin coal seams.

Sandstone lenses in the Garber formation of Permian age containing radioactive bituminous material occur locally beneath a crossbedded bituminous gray sandstone in the southwestern part of 

Oklahoma. In southern Cotton County, a lens of radioactive bituminous sandstone about 1 foot thick and 10 feet long lies within a 

lens of bituminous sandstone about 15 feet thick and 100 feet long. 

The larger lens thins laterally into red shales of the Garber forma-

* ' tion of Permian age. Carbonized wood and a green copper mineral 

are present in the radioactive lens. There is a similar occurrence 

in southern Jefferson County.

In Pawnee, Payne, Osage, and Noble Counties there are several 

small areas of non-commercial copper deposits with associated 

radioactive carbonized wood. These deposits are at several levels in 

red sandstones of Permian age.

29 Brooke, G. L., Shirley, R. F., and Swanson, M. A., 1951, Geological 

investigations of the Trachyte district, Henry Mountains, Utah: 

U. S. Atomic Energy Comm. RMO-912, 7 p., issued by U. S. 

Atomic Energy Comm. Tech. Inf. Service, Oak Ridge, Tenn. 

Uranium deposits occur in sandstone of the Salt Wash member 

of the Morrison formation of Jurassic age in the Trachyte district 

, . ,. on the east flank of the Henry Mountains. The Salt Wash member 

consists of alternating sandstone and mudstone; sandstone predominates and is commonly crossbedded. Carnotite and vanoxite are 

found along the edges of channels associated with fossil logs and 

carbonaceous trash. Locally, base-metal sulfides have been found. 

The vanadium-uranium deposits are small, and most of the material 

mined has been mineralized logs and the closely surrounding mineralized sandstone.

, 30 Bucher, W. H., and Gilkey, A. K., 1953, Fracture pattern and uranium ore of the Zuni uplift, New Mexico [abs.]: Geol. Soc. America Bull., v. 64, no. 12, p. 1402.

The Zuni uplift has a relatively flat top; its shape is due to more 

or less well-defined flexures, and in each structural unit of the uplift, the dominant joints in the sediments tend to parallel the nearest 

fault or flexure. This suggests that the Zuni uplift is the result of 

differential upward movement along faults cutting the crystalline 

basement.

The association of uranium with fluorite in the Todilto limestone 

in the Grants region, and the elongation of the ore-rich areas parallel to the local fracture pattern, suggests a causal relation between ore and fractures.
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 75

31 Burwell, Blair, 1920, Carnotite mining in southwestern Colorado:

Eng. Min. Jour., v. 110, no. 16, p. 755-758.

The exploration and mining procedures used in exploiting the 

carnotite deposits in the McElmo formation (Morrison formation) 

of Jurassic age in southwestern Colorado are described. The ground 

is prospected by drilling; selective mining practices are used to 

maintain the grade of ore. The deposits are irregular in size, shape, 

distribution, and grade of ore. The author suggests that the uranium and vanadium were originally disseminated in the mass of the 

host formation. A downward migration of uranium and vanadium 

took place in ground waters containing sulfates, and the metals 

were precipitated under the influence of carbonaceuos material. 

Inferred reserves of ore coataining more than 1.5 percent UsOg and 

4.5 percent V2 05 are 100,000 tons. "The carnotite region of southwestern Colorado possesses great potentialities for future production."

32. Burwell, Blair, 1932, Mining methods and costs at the vanadium 

mine of the United States Vanadium Corporation, Rifle, Colo.: 

U. S. Bur. Mines Inf. Circ. 6662, 9 p.

The mining methods, costs, and geology of this mine are described. 

The vanadium minerals are disseminated in sandstone of the McElmo 

formation of Jurassic age. (The host rock is now considered to be 

the Entrada sandstone of Jurassic age.) Most of the ore is in the 

lower part of a crossbedded gray sandstone that is from 50 to 75 

feet thick. The ore body ranges in thickness from a few inches to 

30 feet. A cross section through the mine shows -a close relation 

between the distribution of the ore and the crossbedding. The dip 

of the rocks is 15°-25° south, and the ore body trends northeast.

33 Butler, A. P., Jr., 1955, Some factors in the appraisal of part of 

domestic uranium resources: Mines Mag., v. 45, no. 3, p, 91-94, 

108.

The author discusses the rate of discovery of uranium deposits 

and some concepts useful in estimating the amount of uranium resources and in judging where the chances are best for finding concealed uranium deposits. Uranium resources, as defined in this 

paper, are those materials that might be marketed under present 

price schedules, if composition, size, and location, both geographically and in depth, make it economically feasible to do so.

The rate of discovery of uranium deposits since 1947 is two to 

three times the rate in previous years, and the rate of discovery of 

larger deposits is also greater. About 6 percent of the deposits 

contain about 70 percent of the reserves. If this applies to the bulk 

of the undiscovered resources, the major part of our uranium resources are in deposits big enough to look for, even if buried at 

considerable depth.

A method of estimating the ultimate uranium resources is presented. The method is based on the assumption that the proportion 

of the outcrop of a formation that is mineralized with ore-grade 

material more than one foot thick would correctly reflect the proportion of the whole area of the formation so mineralized.

The host rocks of the known uranium deposits have a number of
76 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

features in common. Except for the Todilto limestone near Grants, 

N. Mex., all the deposits are in clastic rocks, generally sandstones, 

deposited by flowing water, probably in a continental environment. 

Nearly all of the sandstones contain some mineral material other 

than quartz sand. Many of the formations contain considerable 

amounts of fine-grained volcanic ash or minerals derived from volcanic ash. Recognition of these and other features that may restrict 

the search will assist in converting hypothetical resources to usable 

reserves.

34 Butler, B. S., Loughlin, G. F., Heikes, V. C., and others, 1920, The 

ore deposits of Utah: U. S. Geol. Survey Prof. Paper 111, 672 p. 

The vanadium-uranium deposits and some of the copper, silver, 

and manganese deposits of Utah are characteristically lenticular 

bodies in sandstone and are associated with fossil plant remains. 

The sandstone is usually light gray and coarse grained to conglomeratic. Carnotite, the principal vanadium-uranium mineral, impregnates the sandstone and replaces the calcareous or clayey cement. 

The deposits are regarded as having been formed by circulating 

waters that collected the metals disseminated through the sedimentary 

rocks and deposited them on contact with carbonaceous matter, 

earlier sulfides, or other precipitating agents. The circulation in 

some places is believed to have been of artesian character and 

consequently controlled by structural features. Brief descriptions 

are given of uranium-vanadium deposits in the Richardson, Temple 

Mountain, White Canyon, Henry Mountains, La Sal Mountains, 

Fruita, and San Rafael River areas.

35 Butler, G. M., and Alien, M. A., 1921, Uranium and radium: Arizona

Bur. Mines, Bull. 117, 26 p.

This report is a brief general description of the history mineralogy, occurrence, uses, and recovery of uranium and vanadium. 

Carnotite deposits in the Carrizo Mountains, in Apache County in 

northeastern Arizona are in the lower part of the McElmo formation (now the Morrison formation) of Jurassic age. Some of the 

ore layers are a maximum of 4 feet thick.

36. Cannon, H. L., 1952, The effect of uranium-vanadium deposits on 

the vegetation of the Colorado Plateau: Am. Jour. Sci., v. 250, 

no. 10, p. 735-770.

Biogeochemical studies were conducted by the U. S. Geological 

Survey in the Thompson district, Grand County, Utah, to determine the effect of uranium-vanadium deposits on plants growing 

near those deposits. The deposits contain, in addition to uranium 

and vanadium, unusual amounts of selenium, and plants rooted in 

soils derived from the deposits accumulate small amounts of these 

metals. Plants growing on mine dumps and areas of mine seepage 

show physiological symptoms of ill health, but those rooted in undisturbed ore do not. A uranium tolerant flora has been recognized 

and a list of the plants compiled. The flora, characterized by selenium-indicator plants, can be used as a guide to exploration.

37 Cannon, H. L., 1953, Geobotanical reconnaissance near Grants, 

N. Mex.: U.S. Geol. Survey Circ. 264, 8 p.
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 77

The application of botanical methods of prospecting for uranium 

was investigated in uranium-bearing areas near Grants, McKinley 

County, N. Mex. The uranium minerals occur in the Todilto limestone and in the Westwater Canyon member, (this part of the 

Westwater Canyon member has subsequently been correlated with 

the Brushy Basin member of the Morrison formation) of the Morrison formation, both of Jurassic age. Samples taken from juniper 

and pinon trees rooted in the Todilto limestone were analyzed for 

uranium. It is concluded that this is a feasible method of exploration for uranium deposits in the Todilto limestone. Seleniumindicator plants may be used to prospect for uranium deposits in 

the Westwater Canyon member, but they apparently do not grow 

on the Todilto limestone. The geology of the area and the deposits 

are briefly discussed.

38 Cannon, H. L., 1954, Botanical methods of prospecting for uranium: 

Min. Eng., v. 6, no. 2, p. 217-220.

Botanical methods of prospecting for metalliferous ores are based 

on the premise that deposits at depth may affect surface vegetation. 

This may be manifested as unusual concentrations of the metals 

within the bodies of the plants growing on or near the deposits, or 

as the presence of particular plants which flourish in the anomalous 

geochemical environment. Both may be used in botanical prospecting for uranium.

The technique of prospecting for uranium by plant analysis consits of taking large samples of twigs or leaves from trees or shrubs 

of the same species at regular intervals throughout the area to be 

prospected. The samples are then analyzed for uranium. The 

laboratory analysis must be precise and is therefore time-consuming and costly. A uranium content of several parts per million is 

considered anomalous.

A plant may be used as an indicator in botanical prospecting if 

its distribution is controlled by any factor related to the chemistry 

of the ore deposit. Since some uranium deposits contain unusual 

concentrations of selenium and sulfur, selenium- and sulfur-indicator 

plants may be used as a guide to these ore deposits. Photographs 

of some species of these plants are included in the paper.

Botanical prospecting for uranium is useful wherever deposits are 

less than 70 feet from the surface and where selenium and uranium 

are readily available to plant roots.

39 Cannon, R. S., Jr., 1952, Geological Survey's work on isotope geology of uranium and thorium and their decay products: U. S. 

Geol. Survey TEI-209, 12 p., issued by U. S. Atomic Energy 

Comm. Tech. Inf. Service, Oak Ridge, Tenn. 

A program of research on the isotope geology of the uranium 

and thorium series is being carried on by the Geological Survey. 

Work is in progress on uranium-lead relationships in uranium ores 

of the Colorado Plateau region, on uranium-thorium-lead relationships in granite, on geological variations in the isotopic composition 

of lead, and on radon and helium in natural gas. A continuing program of systematic studies will try to establish methods in this 

field on a surer footing, and to apply the methods to the solution
78 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

of important geologic and mineral-resource problems. Author's 

abstract

40 Carithers, L. W., and Clinton, N. J., 1956, Uranium in shoreline 

sandstones of terrestrial and marine origin, Colorado Plateau: 

Geology of uranium and thorium, United Nations, v. 6, p. 383- 

386; see also, Clinton, N. J., and Carithers, L. W., 1956, Uranium deposits in sandstones of marginal marine origin: U. S. 

Geol. Survey Prof. Paper 300, p. 445-449.

At Black Mesa, Ariz., and in the San Juan Basin of New Mexico, 

uranium minerals occur in sandstones deposited in marginal marine 

or near-shore terrestrial environment in the Curtis formation of 

Jurassic age and in some members of the Mesaverde group of 

Late Cretaceous age. The occurrences are associated with local 

facies changes and with accumulations of carbonaceous material; 

all are in or near regions of post-Cretaceous tectonic disturbances.

41 Cater, F. W., Jr., 1954, Geology of the Bull Canyon quadrangle, 

Colorado: U. S. Geol. Survey Map GQ 33 (with text).

42 Cater, F. W., Jr., 1955, Geology of the Gateway quadrangle, Colorado: 

U. S. Geol. Survey Map GQ 55 (with text).

43 Cater, F. W., Jr., 1955, Geology of the Pine Mountain quadrangle, 

Colorado: U. S. Geol. Survey Map GQ 60 (with text).

The Bull Canyon, Gateway, and Pin© Mountain quadrangles are 

among eighteen 7%-minute quadrangles in the carnotite-producing 

area of southwestern Colorado that are being mapped as part of a 

. study of the carnotite deposits. The Atkinson Creek quadrangle has 

been mapped by E. J. McKay and his report is included in this bibliography. Reports on the other fourteen quadrangles are in preparation. The regional geology and the stratigraphy, structure and 

mineral deposits of the region are described in the text on each map; 

the texts are essentially similar.

The map area is underlain by sedimentary rocks that range in age 

from Late Paleozoic to Quaternary except in the northeastern part 

where crystalline Precambrian rocks crop out along the flanks of the 

Uncompahgre Plateau. Over most of the region the sedimentary beds 

are flat lying, but in places they are disrupted by high-angle faults 

or are folded into northwest-trending monoclines, shallow synclines, 

and strongly developed anticlines.

The uranium-vanadium deposits are mostly restricted to the upper 

layer of sandstone lenses in the Salt Wash member of the Morrison 

formation of Jurassic age. The ore consists mainly of sandstone 

impregnated with uranium- and vanadium-bearing minerals, but rich 

concentrations are also associated with thin mudstone partings, beds 

of mudstone pebbles, and carbonized fossil plant material. The ore 

bodies range from small irregular masses that contain a few tons of 

ore to large tabular masses containing many thousands of tons; 

most ore bodies are relatively small and contain only a few hundred 

tons. Margins of ore bodies may be vaguely or sharply denned. 

Layers of ore lie essentially parallel to the bedding; most of the 

deposits occur in the thicker parts of sandstone lenses and commonly 

near the base of the lenses. The trend of the long direction of the 

deposits and the trend of the rolls in the sandstone are roughly
BIBLIOGRAPHY OP SANDSTONE-TYPE URANIUM DEPOSITS 79

parallel to the trend of the fossil logs and to the average or resultant 

dip of the crossbedding in the sandstone.

44 Chase, G. W., 1954, Occurrence of radioactive material in sandstone 

lenses of southwestern Oklahoma: Okla. Geol. Survey, Mineral 

Kept. 26, 8 p.

Sandstone lenses of Permian age containing radioactive bituminous 

material occur in a few places beneath a gray crossbedded bituminous 

sandstone in the southern part of Jefferson and Cotton Counties, Okla. 

The sandstones are probably near the base of the Garber sandstone.

45 Chester, J. W., 1951, Geology and mineralization of Hunts Mesa, 

Monument Valley, Ariz.: U. S. Atomic Energy Comm. RMO-801, 

9 p., issued by U. S. Atomic Energy Comm. Tech. Inf. Service, 

Oak Ridge, Tenn.

Copper-uranium ore deposits on Hunts Mesa occur in the Shinarump 

conglomerate of Triassic age that fills ancient stream channels cut 

into the underlying Moenkopi formation. Secondary copper and 

uranium minerals are found in each of the two exposed channels. 

Even though the Shinarump conglomerate forms the cap of the 

mesa, the outcrops of the channels are poorly exposed.

46 Coffin, R. C., 1921, Radium, uranium, and vanadium deposits of 

southwestern Colorado: Colo. Geol. Survey Bull. 16, 231 p.

This paper is the result of a study of the carnotite region of 

southwestern Colorado. Separate chapters are devoted to geography, 

stratigraphy, structure, economic geology of the carnotite deposits, 

description of selected areas, and miscellaneous economic materials. 

Carnotite is an ore mineral of uranium, vanadium, and radium. At 

the time of this report, radium and vanadium were the metals 

sought.

Most of the carnotite deposits occur in one of two zones in the 

lower half of the McElmo formation of Jurassic age [redefined in 

part as the Morrison formation]. The lower zone is from 60 to 125 

feet above the base of the formation, and the more productive upper 

zone is from 275 to 325 feet above the base. The host rock is generally 

a light-colored massive crossbedded sandstone, and the ore is frequently underlain by beds of clay. Carnotite usually impregnates 

the sandstone and cements the sand grains, but it may also replace 

fossil wood or fill fractures and vugs. The carnotite deposits occur 

in the sandstone as lenses, seams, and irregular pockets whose long 

dimensions follow in general the bedding of the sandstone. The 

deposits are irregular in plan. Cylindrical masses of ore called 

"trees" or "logs" are found in the deposits,

The deposits have only a superficial relation to faulting, and they 

have no relation to depth. Structural relations, if any, are not clear. 

The age of the ore cannot be determined except within wide limits.

The author suggests that the minerals which eventually formed the 

present carnotite deposits were deposited with the sands of the 

host formation at the time of sedimentation. The character of the 

parent material is not clear. The minerals subsequently were transported and redeposited by waters which traveled laterally through 

the beds.
80 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

The report includes descriptions of several claims and groups of 

claims within the carnotite region.

47 Comstock, S. S., 1956, Scintillation drill-hole logging: Geology of

uranium and thorium, United Nations, v. 6, p. 722-725. 

The use of a scintillation-type drill-hole-logging unit is now a part 

of the uranium exploration drilling program. The scintillation logging 

unit, designed for efficient one-man operation, is mounted in a fourwheel drive Jeep station wagon. Gamma ray pulses detected by a 

subsurface probe are recorded on a paper chart. These gamma ray 

curves are used to obtain geological information and semiquantitative 

radiometric analysis of the mineralized zones.

48 Cook, K. L., and Moss, C. K., 1952, Geophysical observations in parts 

of the Grants district, McKinley County, N. Mex.: U. S. Geol. 

Survey TEI-244, 16 p., issued by U. S. Atomic Energy Comm. 

Tech. Inf. Service, Oak Ridge, Tenn.

Geophysical observations near Haystack Mesa in the Grants district had the dual objective of investigating the unusual occurrence of 

negative aeromagnetic anomalies in close association with airborne 

radioactivity anomalies and of investigating other geophysical methods which might assist in the search for uranium ores in the Grants 

district. Ground magnetometer tests indicate that the apparent correlation shown in the airborne data is fortuitous and cannot be attributed to a genetic relationship between uranium mineralization and 

the intrusion of dikes or the extrusion of the basaltic lava flow.

49a Craig, L. C., Holmes, C. N., Cadigan, R. A., Freeman, V. L., Mullens, 

T. E., and Weir, G. W., 1951, Preliminary report on the stratigraphy of the Morrison and related formations of the Colorado 

Plateau region: U. S. Geol. Survey TEI-180, 64 p., issued by U. S. 

Atomic Energy Comm. Tech. Inf. Service, Oak Ridge, Tenn.

49b Craig, L. C., and others, 1955, Stratigraphy of the Morrison and 

related formations, Colorado Plateau region, a preliminary report: 

U. S. Geol. Survey Bull. 1009-E, p. 125-168.

The Jurassic rocks of the Colorado Plateau region are divided into 

three units: Lower Jurassic Glen Canyon group, the Upper Jurassic 

San Rafael group, and the Upper Jurassic Morrison formation. The 

Glen Canyon group consists mainly of eolian and fluvial sediments, 

the San Rafael group consists of marine and marginal marine sediments, and the Morrison formation consists of fluvial and lacustrine 

sediments. Stratigraphic studies were concentrated on the Morrison 

formation.

The lower part of the Morrison formation consists of the Salt 

Wash and the Recapture members, and the upper part consists of the 

Westwater Canyon and the Brushy Basin members. The Salt Wash 

and the Brushy Basin members are present in eastern Utah, western 

Colorado, northeastern Arizona, and northwestern New Mexico, 

but the Recapture and the Westwater Canyon members are present 

only in northeastern Arizona, northwestern New Mexico and in 

relatively small areas in adjacent parts of Utah and Colorado. The 

Salt Wash and Brushy Basin members cannot be differentiated in 

central and eastern Colorado.
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 81

The Salt Wash, Recapture, and Westwater Canyon members are 

characterized by sequences of interstratified sandstone and red or 

green mudstone, but the Brushy Basin member consists mainly of 

variegated claystone with a few lenticular beds of conglomeratic 

sandstone. The Salt Wash, Recapture, and Westwater Canyon members were deposited as large alluvial plains or "fans" by systems of 

braided and aggrading streams. The Brushy Basin is composed 

largely of clay derived from volcanic ash that had been deposited in a 

lacustrine environment. The material in the Salt Wash sandstone 

member and in the fluvial part of the Brushy Basin shale member 

probably was derived from an area of sedimentary rocks in westcentral Arizona, and the material in the Recapture shale and Westwater Canyon sandstone members was probably derived from an 

area of intrusive and extrusive igneous rocks, metamorphic rocks, 

and sedimentary rocks in west-central New Mexico. The fluvial 

sediments become coarser as the source is approached, and the 

members are subdivided into facies on the basis of particle size.

The carnotite deposits of the Morrison formation are essentially 

confined to the Salt Wash member; these lie entirely within the 

sandstone and mudstone facies of the Salt Wash. Most of the carnotite deposits occur in areas where sandstones of the Salt Wash are 

relatively well sorted and probably have a relatively high permeability.

50 Curran, T. F. V., 1911, Carnotite in Paradox Valley, Colo.: Eng. Min.

Jour., v. 92, no. 27, p. 1287-1288.

Carnotite ore bodies in Paradox Valley crop out at about the same 

stratigraphic level, have a blanket form, and are a maximum 4 feet 

thick. The ore as mined contains from 6 to 15 percent uranium oxide. 

The economic geography of the area is discussed, and some of the 

mines and claims are briefly described.

51 Curran, T. F. V., 1913, Carnotite: Eng. Min. Jour., v. 96, no. 25,

p. 1165-1167, no. 26, p. 1223-1225.

The history of the carnotite industry on the Colorado Plateau is 

discussed. Carnotite ore bodies occur in a series of thin-bedded 

sandstones and shales (Morrison formation of Jurassic age). The 

best deposits are in western Montrose County, but the carnotite field 

encompasses an area of several thousand square miles in western 

Colorado and eastern Utah. The second part of the report is a 

discussion of the production, refining, and utilization of uranium and 

radium.

52 Dane, C. H., 1935, Geology of the Salt Valley anticline and adjacent

area, Grand County, Utah: U. S. Geol. Survey Bull. 863, 184 p.

Exposed sedimentary formations in this area range in age from

Pennsylvanian to Late Cretaceous; crystalline Precambrian rocks

are exposed on the Uncompahgre Plateau in the northeastern part

of the area. The Salt Valley anticline, a salt structure, is a prominent

fold broken by many faults; its crest is in part dropped into a

structural trough. For the most part the rocks are tilted at low angles

and warped into broad folds. The rocks in the eastern part of the

area are displaced by many normal faults. The report includes a
5Z SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

geologic map and a structure contour map of the area at a scale or 

1:62,500.

Vanadium-uranium deposits at Polar Mesa and in an area southeast 

of Thompson, Utah, are in the Salt Wash member of the Morriso^ 

formation of Jurassic age. Carnotite and other vanadium and uranium 

minerals replace carbonaceous material and impregnate light-colored 

lenticular sandstone beds.

53 Davidson, D. F., 1953, Distribution of coarse- and fine-grained rocks 

in the Wasatch formation and their relationship to uranium deposits, Powder River Basin, Wyo.: U. S. Geol. Survey TEM-676, 

12 p., issued by U. S. Atomic Energy Comm. Tech. Inf. Service, 

Oak Ridge, Tenn.

The Wasatch formation of Eocene age in the Powder River Basin 

apparently grades from predominantly coarse-grained rocks at the 

southern end to fine-grained rocks at the northern end of the basin. 

The uranium deposits occur in the central part of the basin where 

the two rock types are mixed. The significance of this relation is 

not known, and further studies are recommended.

54 Davidson, D. F., 1953, Reconnaissance for uranium in the Powder 

River Basin, Wyo.: U. S. Geol. Survey TEM-677, 32 p., issued 

by U. S. Atomic Energy Comm. Tech. Inf. Service, Oak Ridge, 

Tenn.

A reconnaissance was made for uranium deposits in a large part 

of the Powder River Basin, Wyo., other than the Pumpkin Buttes area. 

No uranium deposits of economic quality were found, but some rocks 

of the Tertiary Fort Union formation and the Cretaceous Inyan Kara 

group are sufficiently uraniferous to justify further search in these 

formations.

55 Davis, D. L., and Hetland, D. L., 1956, Uranium in clastic rocks of 

the Basin and Range province: U. S. Geol. Survey Prof. Paper 

300, p. 351-359; Geology of uranium and thorium, United Nations, 

v. 6, p. 387-391.

Uranium occurs in lake bed sediments and waterlaid tuffs of Tertiary age in several areas in the Basin and Range province of 

Nevada and California.

Rocks in the Virgin Valley in northwestern Nevada are waterlaid 

vitreous tuff and diatomaceous earth beds of early Pliocene age that 

contain discontinuous layers of opal. Carnotite occurs as fracture 

coatings or fine layers in the opal lenses, and a yellow fluorescent 

mineral, possibly schroeckingerite, is disseminated in the tuff. The 

volume of mineralized material is large, but the average uranium 

content is below commercial standards.

A deposit in Lander County, Nev., is in water-laid tuff which contains thin beds of opal. Uranium minerals have not been observed 

in hand specimens. The greatest radioactivity appears to be confined 

to minor fractures in the tuffs. Select samples from the deposit 

contain commercial amounts of uranium, but most of the material 

is submarginal.

Lake bed sediments of Miocene age near Tonopah, Nev., are finely 

stratified pyroclastic material and diatomaceous earth interbedded 

with discontinuous lenses of uraniferous opal. Uranium minerals
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 83

have not been identified, but anomalous radioactivity can be detected 

in an area about 1 mile wide and 8 miles long. A similar deposit 

in Lyon County, Nev., consists of a diatomaceous earth bed with 

carnotite coatings along minor fractures.

Near Hawthorne, Nev., a yellow secondary uranium mineral occupies a series of closely spaced vertical fractures in a tuffaceous 

sandstone. Yellow uranium minerals have been found in a thin bed 

of soft, waterlaid tuff in the Panaca formation of Pliocene(?) age 

in Lincoln County, Nev.

Near Olancha, Calif., the gently dipping Coso lake beds of Pliocene 

age contain autunite on fracture surfaces and in iron-stained zones.

56 Davis, W. E., 1951, Electrical resistivity investigations of carnotite 

deposits in the Colorado Plateau: U. S. Geol. Survey TEM-232, 

25 p., issued by U. S. Atomic Energy Comm. Tech. Inf. Service, 

Oak Ridge, Tenn.

Investigations of the use of geophysical methods in prospecting for 

carnotite deposits on the Colorado Plateau indicate that electrical 

resistivity methods, combined with other geologic data can be used 

successfully to locate areas favorable for drilling. Broad positive 

resistivity anomalies of small magnitude were observed over most of 

the deposits investigated, all of which are in the Salt Wash member 

of the Morrison formation of Jurassic age. The anomalies are related 

to thickening of the ore-bearing sandstone; mineralized ground in 

most places is also associated with this thickening. Electrical resistivity measurements can be successfully made at depths of as much as 

400 feet. The investigations were conducted on Calamity and Outlaw 

Mesas in Mesa County, and at Long Park in Montrose County, Colo.

57 Denson, N. M., Zeller, H. D., and Stephens, J. G., 1956, Water sampling as a guide in the search for uranium deposits and its use in 

evaluating widespread volcanic units as potential source beds for 

uranium: U. S. Geol. Survey Prof. Paper 300, p. 673-680; Geology 

of uranium and thorium, United Nations, v. 6, p. 794-800. 

In the western United States several thousand samples of water 

issuing from widespread volcanic units of Tertiary age and from 

the underlying sedimentary rocks were analyzed for uranium. These 

determinations have proved a useful guide in delimiting areas where 

uranium deposits are likely to occur. Most ground water contains 

less than 2 parts per billion uranium. However, water from seeps 

and springs in volcanic and tuffaceous sedimentary terranes as well 

as from areas of known uranium deposits may contain from 10 to 

250 parts per billion.

Although many of the volcanic rocks of Tertiary age contain appreciable amounts of uranium, not all of them make the uranium 

available to the ground water system in equal amounts. The ground 

water from units of Oligocene and Miocene age, irrespective of 

their geographic location, have a higher uranium content than does 

ground water issuing from other volcanic units.

58 deVergie, P. C., 1953, Preliminary drilling at the Nash Car area, 

White Canyon district, San Juan County, Utah: U. S. Atomic 

Energy Comm. RME-4032, 13 p., issued by U. S. Atomic Energy 

Comm. Tech. Inf. Service, Oak Ridge, Tenn.
84 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

Copper-uranium deposits in the Nash Car area occur in the Shinarump conglomerate of Triassic age in gray sandstone and conglomerate at or near the base of ancient stream channels cut into the 

underlying Moenkopi formation of Triassic age. The conglomerate 

is as much as 10 feet thick, is 100 to 150 feet wide, and is of unknown 

length. Chalcopyrite and pyrite replace carbonaceous material and 

are disseminated in the surrounding sandstone. Secondary copper 

minerals and limonite appear on the weathered outcrop. No uranium 

minerals are visible although in a few places the rock contains 

ore-grade quantities of uranium. The report includes a map that 

shows where drilling has been done, and geologic sections compiled 

from the logs of cores obtained during the drilling.

59 deVergie, P. C., and Carlson, W. A., 1953, Investigation of the "C" 

group area, San Juan County, Utah: U. S. Atomic Energy Comm. 

RME-4011, 13 p., issued by U. S. Atomic Energy Comm. Tech. 

Inf. Service, Oak Ridge, Tenn.

Uranium deposits on the "C" group of claims about 20 miles southwest of Moab on the west side of the Colorado River, are in sandstone lenses of the Shinarump conglomerate of Triassic age near the 

base of a large ancient stream channel cut about 50 feet into the 

underlying Moenkopi formation of Triassic age. Carbonaceous material is abundant in the ore zone, and uraninite and base-metal 

sulfides impregnate the sandstone and replace carbonaceous material. 

The host rock is a coarse- to fine-grained sandstone cemented by 

calcite. (What was formerly called Shinarump conglomerate in this 

area is now correlated with a sandstone member of the Chinle formation of Triassic age.)

60 Dix, G. P., Jr., 1953, Reconnaissance of the uranium deposits of the 

Lockhart Canyon Indian Creek area, San Juan County, Utah: 

U. S. Atomic Energy Comm. RME-4038, 20 p., issued by the U. S. 

Atomic Energy Comm. Tech. Inf. Service, Oak Ridge, Tenn. 

Copper-uranium deposits occur in the Bogus Tongue member of 

the Cutler formation of Permian age in the Lockhart Canyon Indian Creek area. Exposed consolidated sedimentary rocks in the area 

range in age from Permian to Jurassic, and the beds are essentially 

horizontal. The Bogus Tongue member, which is about 670 feet thick, 

is predominantly red and consists of siltstone, sandstone, and crossbedded arkose. The mineral deposits are associated, with discontinuous lenses of white arkose which, presumably, were once red. Small 

amounts of copper and uranium minerals occur as concretions and 

along bedding planes and arkose-mudstone contacts, but the better 

deposits are those in which the uranium and copper minerals are 

disseminated in the arkose lenses. The recognized uranium minerals 

are uranophane, zeunerite, and trogerite. Copper sulfides are present 

in the concretions, and secondary copper minerals are present in the 

other types of deposits.

61 Dix, G. P., Jr., 1954, The uranium deposits of Big Indian Wash, San

Juan County, Utah: U. S. Atomic Energy Comm. RME-4022

(Rev.), 15 p., issued by U. S. Atomic Energy Comm. Tech. Inf.

Service, Oak Ridge, Tenn.

Uranium deposits in the Big Indian Wash area have been found
BIBLIOGRAPHY OF SANDSTONE-TYPE UKANIUM DEPOSITS 00

in the Cutler formation of Permian age and in the Chinle formation 

of Triassic age. The area is on the southwest flank of the Lisbon 

Valley anticline, and the rocks dip about 15° SW. Formations exposed in the area range in age from Pennsylvanian to Cretaceous. 

The upper part of the Cutler formation consists of mudstone, siltstone, and lenses of coarse-grained arkosic sandstone. The uranium 

minerals, carnotite and becquerelite, are disseminated in the lenses 

of arkosic sandstone. Uranium deposits in the Chinle formation are 

in a gray, medium-grained micaceous sandstone near the base of 

the formation. The uranium minerals, uraninite, carnotite, and 

tyuyamunite, are associated with carbonaceous material, pyrite, 

montroseite, and roscoelite. The largest mine in the area, the Mi Vida 

mine, is in the Chinle formation. The deposits at the Big Buck mine 

and the Purple Paint and Small Fry claims are in the Cutler formation.

62 Dodd, P. H., 1950, Happy Jack Mine, White Canyon, Utah: U. S. 

Atomic Energy Comm. RMO-660, 23 p., issued by U. S. Atomic 

Energy Comm. Tech. Inf. Service, Oak Ridge, Tenn. 

The uranium deposit at the Happy Jack mine is in a lenticular, 

coarse-grained sandstone bed near the middle of the Moenkopi formation of Triassic age. Subsequent investigations (Benson, and 

others, 1952) have shown that the host bed is at the base of the 

Shinarump conglomerate of former usage of Triassic age. The 

porous, permeable sandstone bed thickens to about 20 feet at the 

portal of the mine; the thick section is presumably due to the filling 

of an ancient stream channel. This channel appears to be the major 

control of the deposit. Pitchblende and base metal sulfides occur 

in the unoxidized portion of the deposit, and secondary copper 

and uranium minerals occur near the outcrop. The uranium content 

is depleted near the outcrop due to surficial leaching. The mineral 

assemblage indicates the deposit may be of hydrothermal origin. 

Exposed consolidated sedimentary rocks in the area range in age 

from Permian to Jurassic, and dip l°-3° W.

63 Dodd, P. H., 1956, Some examples of uranium deposits in the Upper 

Jurassic Morrison formation on the Colorado Plateau: U. S. Geol. 

Survey Prof. Paper 300, p. 243-262; Geology of uranium and 

thorium, United Nations, v. 6, p. 615-633.

Important quantities of radium, vanadium, and uranium ore have 

been produced on the Colorado Plateau from the Morrison formation 

of Late Jurassic age. The Morrison formation still contains large 

reserves of ore.

The uranium deposits in the Morrison formation, although differing 

in detail, have many characteristics in common. The author describes 

several deposits to demonstrate the flat-lying tabular to irregular 

outline of the ore bodies, the concordance of ore bodies with bedding, 

the elongation of ore bodies in the direction of sedimentary structures, 

and the general correlation between ore bodies and types of lithology. 

Criteria for evaluating ore possibilities are discussed. Subsurface 

geologic maps based on drilled-hole data are presented.

A general hypothesis that explains the localization of the mineral 

deposits without recourse to speculation on origin and genesis of 

the deposits is presented to show the basis of current methods of 

exploration.
86 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

64 Droullard, R. F., and Jones, E. E., 1951, Investigations of uranium 

deposits near Sanastee, N. Mex.: U. S. Atomic Energy Comm. 

RMO-909, 7 p., issued by U. S. Atomic Energy Comm. Tech. Inf. 

Service, Oak Ridge, Tenn.

Uranium-vanadium deposits occur in the Recapture member of the 

Morrison formation of Jurassic age in the Sanastee area, San Juan 

County, N. Mex. Vanadium minerals and carnotite-type minerals, are 

disseminated in fine- to medium-grained sandstone in the upper part 

of the Recapture member. The deposits, which are generally less 

than 20 feet in outcrop length, are contained within slightly radioactive altered zones.

65 Duschatko, R. W., 1953, Fracture studies in the Lucero uplift, New 

Mexico, Final report: U. S. Atomic Energy Comm. RME-3072, 

49 p., issued by U. S. Atomic Energy Comm. Tech. Inf. Service, 

Oak Ridge, Tenn.

The Lucero uplift is a transitional tectonic element situated along 

the boundary of the Colorado Plateau and the Rio Grande graben 

belt of central New Mexico. The eastern margin of the structure has 

been complexly faulted during two (or more) periods of Tertiary deformation. Evidence is presented in support of the hypothesis that both 

stages of tectonic development involved primarily vertical movement 

along sharp monoclinal flexures possibly emanating from displacement along deep seated fracture zones. The composite fracture pattern developed over the uplift indicates that the faults and joints 

are essentially parallel and were produced by a common cause. The 

dominant fracture pattern is regional and indicates primary east-west 

lateral elongation with secondary north-south stretching- of the sediments due to bending of the rock between the primary fractures. 

 Author's abstract

66 Ellsworth, P. C., and Hatfield, K. G., 1951, Geology and ore deposits 

of Mesa VI, Lukachukai district, Arizona: U. S. Atomic Energy 

Comm. RMO-802, 12 p., issued by U. S. Atomic Energy Comm. 

Tech. Inf. Service, Oak Ridge, Tenn.

Vanadium-uranium deposits on Mesa VI are in a fine- to mediumgrained sandstone unit in the Salt Wash member of the Morrison 

formation of Jurassic age. The mineralized sandstone lies about 

60 feet above the base of the formation and is underlain by a bluegreen mudstone. Carnotite and vanoxite occur in mudstone seams 

and impregnate the sandstone. Light-tan sandstone, the most favorable host rock in the Lukachukai Mountains, is relatively scarce 

on Mesa VI. The most mineralized zone is part of a structural flat 

about 1,000 feet southwest of the axis of the Lukachukai syncline.

67 Ellsworth, P. C., and Mirsky, Arthur, 1952, Preliminary report on 

relation of structure to uranium mineralization in the Todilto 

limestone, Grants district, New Mexico: U. S. Atomic Energy 

Comm. RME-4020, 15 p., issued by U. S. Atomic Energy Comm. 

Tech. Inf. Service, Oak Ridge, Tenn.

Investigation of the structure of the Todilto limestone of Jurassic 

age in the Grants, district indicates a genetic relation between the 

folds in the Todilto limestone and the joints resulting from the Zuni 

uplift. Drill-hole data show that the larger ore bodies in the Todilto
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 87

limestone are on anticlines. The ore bodies are elongate in a manner 

that suggests control by a conjugate joint system; they appear to 

trend in general conformity with the folds.

68 Erickson, R. L., Myers, A. T., and Horr, C. A., 1954, Association of 

uranium and other metals with crude oil, asphalt, and petroliferous rock: Am. Assoc. Petroleum Geologists Bull., v. 38, no. 10, 

p. 2200-2218.

Some crude oil, natural asphalt, and petroliferous rock are appreciably radioactive, but little is known about the actual uranium content 

and the chemical nature of the uranium compound or compounds in 

these materials. Semiquantitative spectrographic analyses of the ash 

of 29 samples of crude oil, 22 samples of natural asphalt, and 27 

samples of oil extracted from petroliferous rock indicate that metals 

such as vanadium, nickel, copper, cobalt, molybdenum, lead, chromium, 

manganese, and arsenic are consistently present at some places in 

exceptionally high concentrations in this type of organic matter. 

The chemical analyses show that the uranium content of crude oil is 

consistently much lower than the uranium content of the natural 

asphalt and oil extracted from petroliferous rock. Author's abstract 

The association of uranium with organic materials may have a 

direct bearing on the genesis of some types of uranium deposits. 

Many uranium deposits in Utah, such as those in the San Raf ael Swell, 

Emery County; Circle Cliffs, Garfield County; and Capitol Reef, 

Wayne County, occur on the flanks of breached anticlinal structures 

that have served as geologic traps for the accumulation of petroleum.

69 Everhart, D. L., 1950, Reconnaissance examinations of copper-uranium 

deposits west of the Colorado River: U. S. Atomic Energy Comm. 

RMO-659, 19 p., issued by U. S. Atomic Energy Comm. Tech. 

Inf. Service, Oak Ridge, Tenn.

Several small copper-uranium, deposits have been found in southwestern Utah along the contact of the Shinarump and Moenkopi 

formations of Triassic age. The deposits are highly localized and 

and apparently erratic in their distribution. The deposits contain 

secondary copper, uranium, and copper-uranium minerals which impregnate sandstone and coat parting planes of shale. The deposits 

described are in the Capitol Reef, Circle Cliffs, Silver Reef and 

other areas. The deposits at Silver Reef are not at the ShinarumpMoenkopi contact, but higher in the section in the Silver Reef 

sandstone member of the Chinle formation of Triassic age. Exploration of the region had only begun in 1950, and the known 

deposits had not been exploited.

70 Everhart, D. L., 1951, Geology of uranium deposits a condensed 

version, with mineral tables by Muriel Mathez: U. S. Atomic 

Energy Comm. RMO-732, 34 p., issued by U. S. Atomic Energy 

Comm. Tech. Inf. Service, Oak Ridge, Tenn.

Uranium ore deposits have been found in many different geologic 

environments in igneous, metamorphic, and sedimentary rocks. In 

this report the deposits in igneous and metamorphic rocks and those 

in sedimentary rocks are described separately.

The carnotite deposits on the Colorado Plateau occur mostly in 

sedimentary rocks of Triassic and Jurassic age, and the copper-urani-
50 SELECTED BIBLIOGRAPHIES OF UBANIUM GEOLOGY

um deposits occur mostly in rocks of Triassic age. The carnotite 

deposits are irregular tabular bodies that in outline conform to the 

bedding, but cut across the bedding in detail. The deposits are 

associated with fossil vegetable material in ancient stream channels. 

The copper-uranium deposits are mostly at the base of ancient channels at the base of the Shinarump conglomerate of Triassic age. 

Pitchblende and base-metal sulfides are in the unoxidized parts of 

these deposits. Uraniferous asphalt deposits occur in Triassic rocks 

at Temple Mountain, Utah. Uranium deposits in limestone, uraniferous phosphorite, and black shale are discussed. Ore sampling procedures and the field use of radiation detection instruments are described.

71 Everhart, D. L., 1954, Origin of uranium deposits a progress report: 

Min. Eng., v. 6, no. 9, p. 904-907.

The uranium deposits of the world exhibit a broad variety of character and geologic environment. Uranium has a high solubility over 

a wide range in pH, temperature, and pressure, but there are a 

number of very effective precipitants, including carbonaceous matter 

and high base-exchange clays.

The origin of the uranium deposits in many geologic environments 

is reasonably clear. The disseminated deposits in sedimentary rocks, 

particularly those deposits on the Colorado Plateau, are in greatest 

doubt as to origin. The field relations of most of these deposits suggest that primary structures in the sediments were instrumental in 

localizing the deposits. In a few areas, however, field relations strongly suggest that the deposits may be genetically related to faults, 

fractures, or salt dome structures.

Two main hypotheses have been advanced to explain the origin 

of the Colorado Plateau ores. One is that the ores are penesyngenetic. The second hypothesis holds that the deposits are telethermal; 

that is, the ore-bearing solutions are presumed to have originated at 

depth from an igneous source, ascended along fractures, and mixed 

with ground waters from which the uranium was precipitated in 

favorable beds and sedimentary traps. A third idea is that ground 

waters removed the uranium from slightly uraniferous sedimentary 

rocks and transported it to an environment suitable for precipitation.

72 Faul, Henry, (ed.), 1954, Nuclear geology: New York, John Wiley and

Sons, Inc., 414 p.

This volume, a symposium on nuclear phenomena in the earth 

sciences, is a text covering the field between geology and nuclear 

physics. The first chapter is an introduction to nuclear physics and 

an outline of some techniques used in the study of radioactivity and 

isotopes. Chapters 2, 3, and 4 discuss the natural occurrence of radioactive elements. The thermal, physical, and chemical effects of radioactivity and nuclear methods of geophysical exploration and well 

logging are considered in chapters 5, 6, and 7, and techniques and 

results of absolute age determinations are discussed in detail in 

chapters 8 and 9. The last chapter discusses the origin of the earth.

73 Finch, W. L, 1953, Geologic aspects of the resource appraisal of 

uranium deposits in pre-Morrison formations of the Colorado 

Plateau an interim report: U. S. Geol. Survey TEI-328A, 35 p.,
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 89

issued by U. S. Atomic Energy Comm. Tech. Inf. Service, Oak

Ridge, Tenn.

A reconnaissance to determine uranium resources in pre-Morrison 

formations of the Colorado Plateau was made primarily of deposits 

in the Shinarump conglomerate of Triassic age. The uranium deposits 

in Triassic rocks may be divided on the basis of their principal metal 

content into three types vanadium-uranium (carnotite), copperuranium (uraninite and copper sulfides), and uranium (uraninite). 

The gangue minerals associated with nearly all the deposits are 

limonite, calcite, and gypsum. Most of the uranium deposits are 

irregular tabular bodies; the ore minerals have impregnated the 

host rock. Carbonaceous material is commonly associated with the 

ore. The most important guides to ore are the thickening of sandstone and conglomerate beds, alteration of associated mudstones, 

and the presence in the sandstone of carbonaceous material, iron 

oxide stains, clay and mudstone, and sulfides. Three belts of ground 

that may contain large uranium deposits have been outlined. One 

belt extends from the southern part of the San Rafael district to the 

Big Indian Wash area, Utah; another is in the White Canyon area, 

Utah; the third extends northwesterly across the Monument Valley 

district of Arizona and Utah.

74 Finch, W. I., 1954, Geology of the Shinarump No. 1 uranium mine, 

Seven Mile Canyon area, Grand County, Utah: U. S. Geol. Survey 

Circ. 336, 14 p.

The Shinarump No. 1 uranium deposit is about 12 miles north of 

Moab, Utah, on the west flank of the Moab anticline and about 700 

feet west of the Moab fault. The rocks dip about 8° NW; the formations are of sedimentary origin and range in age from Permian to 

Jurassic. Uraniferous material occurs mainly in three zones in the 

lower 25 feet of the Chinle formation of Triassic age. The Shinarump 

No. 1 deposit is in the lowest zone, which consists of from 5 to 10 

feet of siltstone with some interbeds of mudstone, sandstone, and 

conglomerate. The ore deposit is not in a channel fill but in flat-bedded 

sedimentary rocks that were deposited on an irregular surface. The 

deposit consists of discontinuous, irregular, lenticular layers of mineralized rock that, in general, follow the bedding. The ore minerals 

occur in the more poorly sorted parts of the siltstone and in stringers 

of coarse sand in the siltstone. The rocks near the deposits are bleached from red to gray and green. Uraninite, the principal uranium 

mineral, is associated mainly with chalcopyrite and pyrite. The 

uraninite occurs as small grains disseminated in the siltstone and 

as a replacement of wood. Rich concentrations of uranium occur in 

seams as much as half an inch thick along bedding planes. The 

uraninite was deposited later than or simultaneous with most of the 

sulfides; some of the chalcocite was deposited later than the uraninite. The Shinarump No. 1 deposit is thought to be of hydrothermal 

origin and to have been formed in Late Cretaceous or early Tertiary 

time. Guides to ore in the area are the presence of bleached siltstone, 

carbonaceous material, and copper sulfides.

75 Finch, W. I., 1955, Preliminary geologic map showing the distribution of uranium deposits and principal ore-bearing formations of
90 SELECTED BIBLIOGKAPHIES OF URANIUM GEOLOGY

the Colorado Plateau region: U.S. Geol. Survey Map MF 16 

(with text).

The locations of nearly 3,000 uranium deposits and occurrences on 

the Colorado Plateau are indicated on this map; those from which 

more than 1,000 tons of ore have been produced are distinguished by 

color.

The history of production, the general geology, the principal 

uranium-bearing formations, and the ore deposits are described in the 

text. The uranium is commonly associated with vanadium or 

copper and with carbonaceous material in rather well-defined irregular-shaped bodies. The ore minerals generally impregnate the host 

rock. The most important uranium-bearing formations are the Shinarump and Chinle formations of Triassic age, and the Entrada, 

Tod-lto, and Morrison formations of Jurassic age. Except for those 

in the Todilto limestone, most of the deposits are in light-colored 

sandstones.

76 Finch, W. I., 1956, Uranium in terrestrial sedimentary rocks in the 

United States exclusive of the Colorado Plateau: U. S. Geol. 

Survey Prof. Paper 300, p. 321-327; Geology of uranium and 

thorium, United Nations, v. 6, p. 600-604.

Large uranium deposits occur in Cretaceous sandstone formations 

in the Black Hills region of South Dakota and Wyoming and in 

Tertiary tuffaceous sandstone formations in several areas in Wyoming, Texas, and Nevada. Small deposits occur in terrestrial sedimentary rocks in Pennsylvania, Colorado, Oklahoma, New Mexico, 

and other places exclusive of the Colorado Plateau.

The carnotite deposits in the Black Hills are in sandstone beds in 

the Inyan Kara group of Cretaceous age. The deposits are generally 

similar to those on the Colorado Plateau. They consist of irregular 

tabular or lenticular layers that, in general, follow the bedding and 

have distinct boundaries. The Tertiary deposits occur most commonly as poorly defined bodies of disseminated uranium arsenate, 

silicate, and phosphate minerals in poorly bedded tuffaceous sandstone or sandy tuffaceous rocks. The relation of the deposits to sedimentary structures is obscure.

77 Fischer, R. P., 1937, Sedimentary deposits of copper, vanadiumuranium, and silver in southwestern United States: Econ. Geology, v. 32, no. 7, p. 906-951.

Widely distributed deposits of copper ("Red Beds" type), vanadiumuranium and silver, occurring in sandstones and shales of Permian, 

Triassic, and Jurassic age, exhibit many common features and are 

thought to have had a similar origin. Mineralization, although mostly 

discontinuous, is recurrent at certain stratigraphic horizons. Commonly the ore bodies are distinctly lenticular and in some cases it 

can be demonstrated that mineralization was restricted to a particular 

lens. Chalcocite pseudomorphs after plant fossils, show undeformed 

cell structure, suggesting mineralization previous to deep burial. 

Geologic structures, such as faults and folds appear to be postmineralization and show no genetic relationship to ore deposition.

This evidence opposes current ideas of mineralization by circulating meteoric waters or ascending thermal solutions, and it is believed
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 91

that the concentration of the metals occurred at the time of deposition of the enclosing sediments. It is suggested that these metals 

may have been concentrated from dilute solutions by organisms. 

 Author's abstract

The vanadium-uranium deposits include the carnotite and vanadiferous sandstone ores of Colorado and Utah. Workable deposits are 

restricted to three formations: namely, the Shinarump conglomerate, 

the Entrada sandstone, and the Morrison formation; and in limited 

areas the deposits are restricted to certain horizons within these 

formations. The ore bodies are commonly lenticular. The mass of 

the ore is. disseminated in sandstone, but the richest ore is associated 

with plant remains. Clay galls and thin shaly seams, rich in vanadium, are features common to many of these deposits. These ores 

show no apparent genetic relation to geologic structures such as 

faults and folds. Author's summary

78 Fischer, R. P., 1942, Vanadium deposits of Colorado and Utah, a preliminary report: U. S. Geol. Survey Bull. 936-P, p. 363-394.

Deposits of vanadium-bearing sandstone are widely distributed in 

western Colorado and eastern Utah and have been the principal 

domestic source of vanadium, uranium, and radium. Except during 

a few years when operations were relatively small, deposits at one or 

more places in this region have been intensively mined since 1909. 

Production has increased considerably each year since 1937.

Most of the deposits are in the Morrison formation, but there are 

two important deposits in the Entrada sandstone and several small 

deposits, in the Shinarump conglomerate. Recent X-ray studies indicate that the principal vanadium mineral, heretofore considered to be 

roscoelite, belongs to the hydrous mica group of clay minerals. This 

mineral, along with other vanadium minerals of minor importance, 

impregnates sandstone. Shale pebbles and clay films on bedding 

planes in ore-bearing sandstone are rich in absorbed vanadium, and 

fossil plants in and adjacent to ore bodies are richly mineralized 

with vanadium and uranium in places. Vanadium ore of milling grade 

contains from about 1 to 5 percent VsOs, and most of it contains less 

than 1 percent UsOg. Ore containing as much as 1% percent 

UsOs is usually sold as uranium ore. The vanadium-bearing hydrous 

mica is in part uniformly disseminated through the sandstone and in 

part concentrated along bedding planes and in thin zones that cut 

across bedding. As the zones that cut across bedding are curved or 

wavy, they are called rolls by the miners.

The ore bodies are spotty and form irregularly tabular masses that 

lie essentially parallel to the sandstone beds, but they do not follow 

the beds in detail. They range in content from a few tons of ore to 

many thousand tons. The trend of many elongate bodies is indicated 

by the orientation of the rolls within the ore, and this trend also suggests the probable alinement of any adjacent ore bodies; mapping 

of ore bodies and rolls is therefore an aid to prospecting and development.

No satisfactory explanation can yet be offered for the origin of 

these deposits. The ore bodies do not appear to have been localized by 

such geologic structures as fractures or folds, but within limited areas 

they are restricted to certain stratigraphic zones. Author's abstract
92 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

79 Fischer, R. P., 1944, Simplified geologic map of the vanadium region 

of southwestern Colorado and southeastern Utah: U. S. Geol. 

Survey Strategic Minerals Inv. Prelim. Map 3-226 (with text). 

The uranium-vanadium deposits in the Morrison formation of 

Jurassic age in southwestern Colorado and southeastern Utah are 

indicated on the map; the larger mines and groups of mines are 

named. The deposits in the northern part of the area are in a sandstone unit near the middle of the Morrison; the ore-bearing horizon 

is progressively lower in the section to the south. The ore bodies 

are irregularly tabular masses parallel to the sandstone beds, but 

they do not follow the beds in detail. The vanadium and uranium 

minerals impregnate the sandstone. Shale pebbles, clay layers, 

and fossil plants in or near the ore bodies may be richly mineralized.

80 Fischer, R. P., 1947, Deposits of vanadium-bearing sandstone; in 

Vanderwilt, J. W., Mineral resources of Colorado, p. 451-456: 

Colo. Min. Resources Board.

Deposits of vanadium-bearing sandstone occur in western Colorado and adjacent parts of Utah, Arizona, and New Mexico. The 

principal ore-bearing rocks are the Shinarump conglomerate of 

Triassic age, and the Entrada sandstone and Morrison formation of 

Jurassic age. The ore is sandstone impregnated with vanadium minerals, although some plant fossils are richly mineralized. The vanadium 

deposits form irregular, tabular layers whose long axes are nearly 

parallel to the bedding, but the deposits do not follow the beds in 

detail. The deposits are irregularly distributed and have a wide range 

in size. The limits of the vanadium-bearing sandstone generally are 

fairly well defined. Wherever the ore layer, or an edge of it, crosses 

the bedding in a smooth curve the structure is called a "roll." Fossil 

logs and the rolls in any one area usually have a common orientation. 

Attitudes of the host beds range from horizontal to steeply dipping, 

but most of the deposits are in gently dipping beds. Faulting is 

common, but the deposits apparently are not genetically influenced 

by faulting nor by Tertiary intrusive igneous rocks.

Origin and controls of the ore deposits have not been definitely 

established, but the deposits probably were formed by precipitation 

of the minerals from groundTwaters before regional deformation and 

perhaps shortly after deposition of the ore-bearing beds. The source 

of the vanadium is not known, but it may have been adjacent beds 

which were slightly vanadiferous and in great volumes.

(Because of security restrictions in effect at the time of publication, 

the report does not mention uranium. However the ores from most 

vanadium deposits on the Colorado Plateau also contain uranium.)

81 Fischer, R. P., 1949, Federal exploration for carnotite ore: Colo.

Mining Assoc., special pub., 14 p., Denver, Colo. 

The Geological Survey is conducting an integrated program of exploration and geologic studies in the carnotite region of southwestern Colorado and the adjoining states on behalf of the U. S. 

Atomic Energy Commission. Exploration will mainly test ground 

away from known deposits, ground that has not been tested and 

probably will not be tested by private industry because of the high 

risk of a poor yield. The geological studies are directed mainly at
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 93

determining conditions that localized the deposits, as a guide to 

ore-finding and an aid in evaluating the carnotite resources of the 

region.

A brief description of the carnotite deposits is. given, with particular reference to the geologic features that are useful in guiding 

exploration. Most deposits are in lenticular sandstone beds, mainly 

in or near the thicker, central parts of the lenses, where the sandstone is medium-grained and rather thickly though somewhat irregularly bedded. Thin-bedded and fine-grained sandstone on the thinning edges of the lenses is less favorable for ore. It is. suggested 

that ground-water solutions, from which the ore minerals probably 

were precipitated, circulated along the central parts of the sandstone 

lenses, and in doing so influenced the rock color, which is a useful 

guide in recognizing ground favorable for ore deposits. Most of the 

known deposits are in light yellowish-brown sandstone with associated mudstone or argillaceous material that has been altered from red 

to gray.

The general plan of exploration being used by the Geological Survey 

is described briefly. Author's abstract

82 Fischer, R. P., 1949, Origin of the Colorado Plateau vanadium deposits [abs.]: Washington Acad. Sci. Jour., v. 39, no. 3, p. 109.

The vanadium deposits of the Colorado Plateau occur in sandstone beds of Mesozoic age. Most of them are restricted to a few 

stratigraphic horizons, along which they have a wide but spotty 

areal distribution. All the deposits have many common characteristics.

The ore minerals mainly impregnate sandstone, partly or completely 

filling the pore spaces of the rock. The ore bodies are irregularly 

shaped in plan and in section they form tabular or lenticular layers 

that lie nearly parallel to the bedding. These layers do not follow the 

beds in detail, however, and for this reason the ore in its present 

form can not be syngenetic but rather had to have been precipitated 

from solutions after the sands had accumulated.

Though the geologic environment of the vanadium deposits differs somewhat from place to place, no definite relationship has yet 

been demonstrated between the spatial distribution or the character 

of the deposits and geologic structures such as faults, folds, and 

and igneous intrusions. Considering all factors it is difficult to 

rationalize the localization and character of the deposits as originating 

from hydrothermal or ground-water solutions that might have been 

introduced into the ore-bearing beds along through-going, vertical 

structures resulting from regional deformation or igneous activity.

Nevertheless, the habits of the ore and the location of the deposits 

show a close relationship to sedimentary structures and conditions 

that would certainly influence at one time or another the flow of 

solutions along or through the ore-bearing beds. Recognizing these 

features, and believing that mineralization after regional deformation is unlikely, it is therefore suggested that the vanadium ore was 

precipitated from ground waters moving along the beds during a 

period of active circulation shortly after the sands accumulated. 

Precipitation probably was caused by relatively slight changes in 

composition of the waters, resulting from reactions in an environment of decaying organic matter, reactions at a water table, or the 

mixing of two solutions. Author's abstract
94 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

83 Fischer, R. P., 1950, Uranium-bearing sandstone deposits of the Colorado Plateau: Econ. Geology, v. 45, no. 1, p. 1-11.

The uranium-bearing sandstone deposits of the Colorado Plateau are 

commonly referred to as "carnotite deposits." They have been the 

principal domestic source of uranium, radium, and vanadium. The 

deposits are largely restricted to a few stratigraphic zones, along 

which they have a wide but spotty areal distribution. The ore minerals mainly impregnate sandstone, though in places fossil plants are 

richly mineralized. Most of the ore bodies are small, but have a 

wide range in size, and within individual deposits the ore has a 

considerable range in thickness and grade. The deposits are irregularly tabular or lenticular, with their long axes nearly parallel to the 

bedding, but the ore does not f olow the beds in detail.

The ore is thought to have been precipitated from ground-water 

solutions after the enclosing sands had accumulated and before 

regional deformation. Sedimentary structures that seem to have controlled the movement of these solutions and the features that probably localized the ore deposits are described, and their application 

as guides to ore finding is explained. Author's abstract

84 Fischer, R. P., 1956, Uranium-vanadium-copper deposits on the Colorado Plateau: U. S. Geol. Survey Prof. Paper 300, p. 143-154; 

Geology of uranium and thorium, United Nations, v. 6, p. 605-614.

The uranium-vanadium-copper deposits of the Colorado Plateau 

region form a group of wide distribution and many common geologic 

characteristics. They have been the principal source of uranium and 

vanadium in the United States.

Structurally, the region has been relatively stable since Precambrian time. Exposed rocks consist mainly of late Paleozoic to Tertiary sedimentary strata that have been invaded by moderatesized stocks and laccoliths of early Tertiary or perhaps Late Cretaceous age. Laramide deformation is expressed by several broad folds 

and sharp flexures, but in most places the sedimentary beds lie 

nearly horizontal.

The early ore minerals consist of copper sulfides and low-valent 

oxides and silicates of uranium and vanadium. These minerals alter to 

higher valent oxides of vanadium and to vanadates and other secondary uranium and copper minerals. Sandstone is the principal host 

rock, and the ore minerals mainly fill pore spaces, through partly replacing sand grains and associated argillaceous and carbonaceous 

material.

Ore bodies range from small masses only a few feet across to 

deposits several hundred feet across. The large ore bodies are mainly 

tabular, forming layers a few feet to as much as 20 feet thick that lie 

essentially parallel to bedding, but the layers are undulant and cut 

across the beds in places. Many ore bodies in sandstone are slightly 

elongate parallel to the trend of the stream that deposited the sandstone; some of the ore bodies in limestone are markedly elongate and 

follow lines of deformation.

Although these deposits have been found in many formations, 

ranging from late Paleozoic to middle Tertiary in age, deposits that 

have yielded significant production are mostly restricted to the Shinarump conglomerate and Chinle formation of Triassic age and the
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 95

Todilto limestone, Entrada sandstone, and Morrison formation of 

Jurassic, age.

The deposits present peculiar problems of localization and genesis. 

In most places, the ore minerals were presumably introduced into 

their present positions by solutions moving laterally through the 

beds. Sedimentary structures, such as lenses, and associated argillaceous and carbonaceous material apparently influenced localization 

of many ore bodies. The regional distribution of deposits suggests to 

some geologists that regional deformation also influenced localization 

by providing pathways for vertical movement of solutions, and a few 

deposits show close association with such vertical pathways. Igneous 

activity and mineralization of definite hydrothermal origin are not 

closely associated with the deposits except in a few places.

Radioactive age determinations indicate that the deposits were 

formed in Late Cretaceous or early Tertiary time. If the ore metals 

were introduced into the host rock at this time, it seems likely that 

the metals were derived either from ascending hydrothermal solutions 

or by lateral or vertical secretion from the associated sediments. 

 Author's abstract

85 Fischer, R. P., Haff, J. C., and Rominger, J. F., 1947, Vanadium 

deposits near Placerville, San Miguel County, Colo.: Colo. Sci. 

Soc. Proc., v. 15, no. 3, p. 115-134.

The vanadium deposits near Placerville, discovered about 1900, 

occur in two belts in the Entrada sandstone of Late Jurassic age. 

The formations in the area are nearly horizontal sedimentary rocks 

of Permian to Cretaceous age which have been intruded by Tertiary 

igneous rocks and cut by numerous faults. The vanadium deposits 

seem to be older than the faults and intrusive rocks and thus not 

genetically related to them.

The ore, which is sandstone impregnated with vanadium minerals, 

forms a wavy layer within the upper 25 feet of the Entrada sandstone. The vanadium-bearing layer is nearly continuous and lies 

nearly parallel to the bedding but does not follow the bedding in 

detail. The layer averages a few inches in thickness, but locally it 

forms minable ore bodies from 1 foot to 20 feet thick. The ore bodies 

seem to be irregularly distributed and are either elongate or roughly 

circular in plan. Most of the elongate bodies occur where the vanadium-bearing layer cuts rather sharply across the bedding to form 

what the miner calls "rolls." The mineralization is believed to have 

taken place at a water table that existed before igneous activity and 

deformation. The genetic and structural conditions that controlled 

the localization of the ore bodies have not been definitely determined, 

and the exact locations of ore bodies cannot be predicted. A number 

of mines and prospects in the area are described.

86 Fischer, R. P., and Hilpert, L. S., 1952, Geology of the Uravan Mineral Belt: U. S. Geol. Survey Bull 988-A, p. 1-13. 

The name "Uravan mineral belt" is applied to a narrow, elongate 

area in southwestern Colorado in which carnotite deposits in the 

Morrison formation have a closer spacing, larger size, and higher 

grade than those in adjoining areas. The belt extends from Gateway 

through Uravan to Slick Rock.

The deposits within the belt tend to be clustered in patches of
96 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

favorable ground 1,000 feet or more in width and usually a mile or 

more in length. These patches of favorable ground, and the deposits 

within them, generally are elongate normal to the trend of the 

mineral belt. Similarly the fossil logs and the ore rolls within 

the deposits have a dominant orientation normal to the belt. The 

mineral belt probably was localized by geologic conditions extant 

during the time the ore-bearing Morrison formation was deposited. 

These geologic relations allow the projection of the belt under 

deep cover between points of exposure and offer the chance of discovering moderately large reserves of carnotite ore in the unexplored 

parts of the belt.

The U. S. Geological Survey has done intensive diamond-drill exploration in parts of the Uravan mineral belt since 1947. The concept of the geologic relations of the mineral belt and certain geologic 

features that can be recognized in drill core have been useful in 

guiding this exploration. These features, consisting of the thickness 

and color of the ore-bearing sandstone, the color of mudstone associated with the sandstone, and the presence of abundant carbonaceous 

material in the ore-bearing sandstone, are briefly described. Exploration is done in three stages. During the first stage, holes are drilled 

at a wide spacing, approximately 1,000 feet apart, to find and 

roughly delimit favorable ground. During the second stage, the 

favorable ground is drilled with holes at a moderate spacing, 100 

to 300 feet apart, to search for ore deposits. In the third stage of 

drilling, offset holes are drilled at 50- or 100-foot intervals around a 

discovery hole to extend and roughly outline the deposit. Author's 

abstract

87 Fischer, R. P., Stokes, W. L., and Smith, L. E., 1944, Geology of the 

Rifle Creek vanadium area, Garfield County, Colo.: U. S. Geol. 

Survey Strategic Minerals Inv. Prelim. Rept., 5 p. (mimeographed, 

limited distribution).

The vanadium deposits at the Rifle and Garfield mines, northeast 

of Rifle, Garfield County, Colo., are in the Entrada sandstone of 

Upper Jurassic age. The rocks in the area dip southward at moderately low angles, but this dip is locally disrupted by small folds 

and faults. Exposed formations include the Triassic "Red Beds," 

the Entrada sandstone and Morrison formation of Jurassic age, and 

the Dakota (?) sandstone and Mancos shale of Cretaceous age.

The ore is light-colored crossbedded fine-grained sandstone impregnated with vanadium minerals, the most important of which is 

a fine-grained micaceous mineral of uncertain composition. Fossil 

carbonaceous material has not been observed. The deposits occur in 

three layers which range in thickness from a feather-edge to a maximum of 30 feet and average about 5 feet. Generally the ore layers are 

nearly conformable to formation contacts; they normally cross inclined 

bedding. At the Rifle mine, the lower ore layer forms an elongate 

deposit that has been mined horizontally for nearly 5,000 feet. An 

altered zone at the top of the "Red Beds" is locally vanadiferous; 

the thicker parts of the altered zone are spatially related to vanadium 

deposits in the overlying Entrada sandstone.

88 Fix, Philip, 195&, Geochemical prospecting for uranium by sampling 

ground and surface waters: Geology of uranium and thorium,
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 97

United Nations, v. 6, p. 788-791; see also, Hydrogeochemical 

exploration for uranium: U. S. Geol. Survey Prof. Paper 300, 

p. 667-671.

Ground water and surface water take uranium into solution in 

amounts determined by the pH and chemical composition of the water 

and the composition and permeability of the geologic material with 

which the water is in contact If due regard is accorded these variables, the uranium content of the water will serve as a rough index 

of the uranium concentration in the geologic materials near the place 

where the sample was obtained.

The background concentration of uranium in large streams in the 

United States is commonly about 0.1 part per billion but may be 

higher or lower depending on the character of the geologic terrane 

traversed. Geological and chemical factors determine what point 

between 3 and 10 times the background shall be considered the 

threshold of significance. In most uraniferous areas the surface 

waters commonly contain from 1 to 10 parts per billion.

Analysis of water is a quick way of indexing the uranium possibilities in unexplored areas if the sampling of surface waters has been 

carefully planned. The analysis of water samples is also useful in 

guiding both physical exploration and detailed geologic work in 

known mineralized districts and active mines. Data from more than 

700 analyzed samples have established the validity of this method, 

and comparisons with geologic and geophysical methods of prospecting show excellent agreement.

89 Fleck, Herman, and Haldane, W. G., 1907, A study of the uranium and 

vanadium belts of southern Colorado: Rept. of the Colo. State 

Bur. of Mines, 1905-1906, p. 47-115.

The geology of the uranium and vanadium deposits in southwestern Colorado, the metallurgy of the ores, and the uses of the metals 

are discussed. Little is known of the geology of the deposits. They 

are in sandstone beds in a series of sandstone, shale, and conglomerate above the La Plata formation (Entrada sandstone) of Jurassic 

age and were formed subsequent to the deposition of the sandstone 

beds. Some writers (Hillebrand and Ransome, 1900) have suggested 

that the deposits were recently formed near the present surface as 

local concentrations of material already in the sandstone. Fleck and 

Haldane suggest that the deposits may be much older. A number 

of mines and prospects in the region are described.

90 Freeman, H. D., 1935, Vanadium and uranium deposits in the 

Triassic and Jurassic sandstones of the Plateau area of southwestern Colorado and southeastern Utah: Unpub. thesis, 

Princeton Univ.

Some of the vanadium and uranium deposits on the Colorado 

Plateau are described. The vanadium deposits at Placerville occur 

in the La Plata sandstone (Entrada) of Jurassic age at about 

the same stratigraphic horizon throughout the district. Roscoelite, 

the principal vanadium mineral, occurs in thin but rich (as much 

as 8.3 percent VzOs) horizontal seams with sparsely disseminated 

mineral in the sandstone above and below. The deposits range from 

less than 1 foot to 10 feet in thickness and may extend for several
98 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

hundred feet along the outcrop. Deposits of chromium occur in 

the same area, but not in association with the vanadium deposits.

The description of the uranium deposits in the Shinarump conglomerate of Triassic age at Temple Mountain, Utah, is taken from 

Hess, 1922 (see ref. 130).

Most of the uranium deposits in the Paradox Valley area are 

small bodies of carnotite-impregnated sandstone about 300 feet 

above the base of the Morrison formation of Jurassic age. The 

host bed, from 40 to 70 feet thick, is a crossbedded sandstone that 

contains mudstone lenses, numerous clay galls, and abundant organic 

debris.

The author reviews previous theories of origin, proposes that 

the deposits are syngenetic, and suggests that the metals were 

introduced with bits of clay or deposited by biochemical processes.

91 Friedel, Charles, and Cumenge, E., 1899, Sur un nouveau minerai 

d'urane, la carnotite: Soc. franc, mineralogie Bull., v. 22, 

p. 26-29, (In French); Bull. Soc. Chim. de Paris (3), v. 21, 

p. 328 (In French); Acad. des Sciences, Paris, Comptes Rendus, 

v. 128, p. 532 (In French) ; Chemical News, v. 80, p. 16. 

A powdery yellow substance from Montrose County, Colo., was 

received by the authors and found to be a new mineral species. 

The mineral, a hydrous potassium uranyl vanadate, was named 

carnotite in honor of M. Adolphe Carnot.

92 Gabelman, J. W., 1956, Uranium deposits in limestone: U.S. Geol. 

Survey Prof. Paper 300, p. 387-404; Geology of uranium and 

thorium, United Nations, v. 6, p. 338-345.

The Todilto limestone of Middle Jurassic age is present in northern 

New Mexico in an area which roughly coincides with the San Juan 

Basin. Throughout the basin the limestone is deformed by intraformational folds ranging in width from less than 1 inch to about 

35 feet. Folding may have begun contemporaneously with deposition, but it continued after lithification. Fold axes have two major 

directions and form a reticulate pattern which commonly coincides 

with the joint pattern.

The mineralized areas occupy the troughs of wide, shallow synclines which plunge down the northeast flank of the Zuni uplift. 

Ore deposits are confined to the crests of the small anticlines within 

the synclines and are, therefore, long and narrow. Ore trends coincide 

with the reticulate joint and fold pattern directions; the deposits 

occur close to the larger faults.

Uranium in considerably smaller quantities occurs in the Kaibab 

limestone of Permian age in Arizona, in the San Andres equivalent 

of that limestone in New Mexico, in calcareous parts of the Bidahochi formation of Miocene age in the Hopi Buttes area of Arizona, 

and in algal limestone in the Browns Park formation of Miocene age 

in Wyoming.

93 Gabelman, J. W., 1956, Uranium deposits in paludal black shales,

Dakota formation, San Juan Basin, N. Mex.: U. S. Geol. Survey

Prof. Paper 300, p. 303-319; Geology of uranium and thorium,

United Nations, v. 6, p. 422-429.

Uranium deposits are present in black shale at the base of the
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 99

Dakota sandstone of Cretaceous age in the San Juan Basin, northwestern New Mexico. The shales are of paludal and littoral origin 

and are richly carbonaceous. The shale beds are discontinuous 

lenses which interfinger with, and are enclosed by, discontinuous 

channel-sand lenses formed by ancient streams. Interbedded sandstone beds and lenses are gray, medium- to coarse-grained, and 

highly contaminated with carbonaceous trash.

Uranium is most common in the carbonaceous sandstone lenses 

which have the greatest lithologic variability. Yellow uranium 

minerals impregnate the most carbonaceous parts of the sandstone. 

Less commonly, beds of pure black carbonaceous shale or peat overlying ancient stream channel sands are mineralized rather than 

the neighboring sands. No uranium minerals are recognizable in 

the shales and the uranium is presumably absorbed by the carbon.

In the Gallup area, the Diamond No. 2 and Becenti deposits are 

in carbonaceous sandstone beds, and the Hogback No. 4 deposit is 

in black carbonaceous shale.

In the Grants area, the Silver Spur, Small Stake, and Dakota 

deposits are in the carbonaceous basal part of the Dakota sandstone 

which is enclosed by shale.

In the Nacimiento uplift, the Butler deposit is in a thin peat lens 

in the basal zone of interbedded black shales and sandstones in 

the Dakota formation. The Diamond No. 2, Hogback No. 4, and 

Butler deposits are described briefly.

94 Gale, H. S., 1906, Carnotite in Rio Blanco County, Colo.: U. S. Geol.

Survey Bull. 315-C, p. 110-117.

Carnotite deposits about 15 miles northeast of Meeker in Rio 

Blanco County are in sandstone of the Dakota sandstone of Cretaceous age. The carnotite coats fractures in the sandstone and 

is associated with fossil wood. The deposits are probably superficial.

95 Gale, H. S., 1908, Carnotite and associated minerals in western

Routt County, Colo.: U. S. Geol. Survey Bull. 340, p. 257-262. 

The carnotite deposits near Skull Creek in western Routt County 

occur in a white massive crossbedded coarse-grained sandstone of 

Jurassic age. Uranium, vanadium, copper, selenium, and chromium 

minerals impregnate the sandstone and coat fractures along a 

shear zone. The rock is heavily stained with limonite.

96 Garrels, R. M., 1953, Some thermodynamic relations among the 

vanadium oxides, and their relations to the oxidation state 

of the uranium ores of the Colorado Plateaus: Am. Mineralogist, 

v. 38, no. 11-12, p. 1251-1265; [abs.] Geol. Soc. America Bull., 

v. 64, no. 12, p. 1426.

Fields of stability of several vanadium oxides in water solution 

at 25° C have been calculated as functions of pH and oxidation 

potential. The bivalent VgOo is not expected under natural conditions; it should occur only at oxidation potentials below the 

breakdown potential of water. The oxide corresponding to the 

mineral montroseite V^Os^O or VOOH, is predicted to coexist 

with common metal sulfides and to oxidize to VgO* at about the same 

potential at which sulfide ion oxidized to sulfate. Owing to difficulties entailed by the complex chemistry of vanadium, V*5, no
100 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

attempt was made to calculate a boundary between VaO* and a 

higher oxide. Diagrams showing the fields of stability of the various 

oxides have been constructed, and contours showing the activities 

of the various vanadium ions have been superimposed. The stability fields of the vanadium oxides should be useful in deducing 

the environment of formation of the carnotite ores and the "blueblack" ores of the Colorado Plateaus. Author's abstract

97 Garrels, R. M., 1954, Thermodynamic relations among the uranium 

oxides, and their relation to the oxidation states of the uranium ores of the Colorado Plateaus [abs.]: Geol. Soc. America 

Bull., v. 65, no. 12, p. 1254-1255.

Fields of stability of uranyl hydroxide and uranous hydroxide 

in water solution at 25° C and 1 atmosphere pressure have been 

calculated as functions of Eh and pH. Equilibrium values of the 

activity of uranyl ion and of uranous ion also have been calculated 

and are shown as contours on the stability fields. Thermodynamic 

relations among the uranyl hydroxides, oxides, and hydrated oxides 

indicate that the free-energy differences among the various species 

are small. The data are interpreted to mean that a variety of such 

uranium (VI) compounds may form and even co-exist. Similar 

studies of the uranium (IV) hydroxide indicate that it is unstable 

relative to the oxide and might well be expected to invert to the 

oxide at a finite rate. Uranium (V) compounds probably have a 

transitory existence because of the instability of the U02+ ion; 

uranium (III) oxides and hydroxides would not be expected to 

occur naturally because the uranium (III) ion would decompose 

water. A comparison of the behavior of the low-valence vanadium 

hydroxides (III and IV) with uranium (IV) and (VI) hydroxides 

indicates that vanadium (III) hydroxide should oxidize to the vanadium (IV) hydroxide at a slightly lower potential than that required for the uranous to uranyl hydroxide pair. A speculative 

diagram showing probable fields of stability of many of the major 

minerals of the Colorado Plateaus is presented, and it is suggested 

that a consistent picture results if one assumes that the ores represent the superimposition of a weathering environment on a mineral 

assemblage formed in a primary reducing environment. Author's 

abstract

98 Garrels, R. M., 1955, Weathering of uranium deposits: Min. Cong.

Jour., v. 41, no. 5, p. 58-60.

The vanadium-uranium and copper-uranium ores of the "sandstone-type" deposits of the Colorado Plateau exhibit an extremely 

complex and varied mineralogy. The ores occur predominantly in 

sandstones of continental origin. The ore minerals characteristically are interstitial to or replacements of the sandstone particles. 

Before 1950, the metals contained in the ores mined were of a highvalent type, but since then low-valent ores from deeper mines have 

contributed significantly to the total production.

A consistent picture of the genesis and alteration of the minerals 

is obtained if it is assumed that the deposits originally consisted 

entirely of minerals containing uranium, vanadium, copper, and 

iron in their lower valence states, and that the present ores exhibit,
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 101

from place to place, every possible degree and range of oxidation 

of .this primary assemblage. The sequence of minerals formed 

during the process of oxidation and weathering is illustrated and 

explained.

99 Gilkey, A. K., 1953, Fracture pattern of the Zuni uplift Final 

report: U.S. Atomic Energy Comm. RME-3050, 34 p., issued 

by U. S. Atomic Energy Comm. Tech. Inf. Service, Oak Ridge, 

Tenn.

The objectives of this study have been to determine the nature 

of the major fracture pattern of the Zuni uplift; to analyze this 

pattern for evidence of the mode of origin of the uplift; and to 

compare the fracturing in the ore areas with that elsewhere on 

the uplift to see whether diagnostic features exist that might make 

it possible to indicate other favorable areas. Author's abstract 

The dominant set of fractures is roughly parallel to the long 

axis of the Zuni uplift, and a subordinate set is about normal to 

the long axis. These sets of joints and faults are present in both 

crystalline and sedimentary rocks. Gilkey concludes that the Zuni 

uplift was produced by up-warping of the crystalline core by large 

regional tectonic elements. The general area in which most of the 

uranium ore has been found is a prominently faulted part of 

the uplift with joints especially common near the faults. Some 

ore bodies show well-defined elongations in the directions of the 

principal fracturing; this suggests that the ore is related to fracturing.

100 Gill, J. R., 1953, Uranium minerals in Cedar Canyon, Harding 

County, S. Dak.; in Search for and geology of radioactive 

deposits, Semiannual progress report, December 1, 1952 to 

May 31, 1953: U.S. Geol. Survey TEI-330, p. 124-125, issued 

by U. S. Atomic Energy Comm. Tech. Inf. Service, Oak Ridge, 

Tenn.

A small deposit of a yellow uranium mineral, possibly carnotite, 

occurs in a channel sandstone at the top of the White River formation of Oligocene age in Cedar Canyon near the south end of the 

Slim Buttes. The mineral is most abundant in the sandstone near 

the base of the channel and is concentrated near fossil roots or stems 

and on the surfaces of fractures.

101 Gilluly, James, and Reeside, J. B., Jr., 1928, Sedimentary rocks 

of the San Rafael Swell and some adjacent areas in eastern 

Utah: U.S. Geol. Survey Prof. Paper 150-D, p. 61-110. 

The sedimentary formations of the San Rafael Swell area range 

in age from Permian to Late Cretaceous. Triassic and Jurassic 

formations are most widely exposed and are mostly of continental 

origin. Formations older than Late Cretaceous are predominantly 

sandstone. A few igneous dikes and sills are present in the southwestern part of the San Rafael Swell. The formations are described and a number of measured sections are presented.

102 Gilluly, James, 1928, Geology and oil and gas prospects of part of 

the San Rafael Swell, Utah: U.S. Geol. Survey Bull. 806-C, 

p. 69-130.
102 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

Sedimentary formations in this area of Emery County range 

in age from Permian to Late Cretaceous. A number of igneous 

sills and dikes are present in the southwestern part of the San 

Rafael Swell which is a huge asymmetric elongate dome. The dips 

on the north and west flank are gentle, but the south and southeast 

flanks are steeply dipping. Many minor folds are superimposed 

on the main structure, and small faults are present in many places. 

The report includes a geologic and structural map of the area at a 

scale of 1 : 126,720.

Vanadium-uranium ores have been mined at several places along 

the east flank of the swell, and carnotite stains were seen at several 

places on the west flank.

103 Gott, G. B., and Erickson, R. L., 1952, Reconnaissance of uranium 

and copper deposits in parts of New Mexico, Colorado, Utah, 

Idaho, and Wyoming: U. S. Geol. Survey Circ. 219, 16 p.

Copper and uranium are associated in several minable uranium 

deposits on the Colorado Plateau. Because of this association, a 

reconnaissance was made of several known deposits of copper disseminated in sandstone to determine whether they might be a 

source of uranium. Commercial-grade uranium is not associated 

with the copper deposits that were examined.

Uraniferous .asphaltite deposits in the Shinarump conglomerate 

of Triassic age in the San Rafael Swell were also examined. These 

deposits may be economic sources of uranium. The uraniferous 

asphaltite deposits contain a suite of trace metals similar to that 

contained in crude oil and other bituminous materials. The metals 

in the asphaltite may have been concentrated from petroleum.

104 Gott, G. B., Jones, R. S., Post, E. V., and Braddock, W. A., 1954, 

Black Hills, S. Dak.; in Geologic investigations of radioactive 

deposits, Semiannual progress report, December 1, 1953, to 

May 31, 1954: U.S. Geol. Survey TEI-440, p. 64-72, issued 

by U. S. Atomic Energy Comm. Tech. Inf. Service, Oak Ridge, 

Tenn.

The repeated occurrence in the Edgemont district of vanadiumuranium deposits in host rocks possessing particular characteristics 

was observed by the authors. These characteristics may be guides 

in predicting the occurrence of ore. The most favorable host rock 

appears to be the thickest sandstone in the lower part of the Lakota 

formation of Cretaceous age. The deposits generally occur where 

the sandstone contains numerous mudstone "splits." Many of the 

carnotite deposits occur on structural terraces. A characteristic 

purplish-pink iron oxide stain impregnates the sandstones adjacent 

to many of the deposits; this color appears to be one of the more 

useful guides to ore. Silica and carbonate cement are associated 

with the deposits in some places, but also are present in areas 

where ore is not known to exist.

105 Gray, J. R., and Tennissen, A. C., 1953, Uranium investigations 

near Aladdin, Crook County, Wyo.: U. S. Atomic Energy Comm. 

RME-4016, 13 p., issued by U. S. Atomic Energy Comm. Tech. 

Inf. Service, Oak Ridge, Tenn.

Uranium deposits occur in the Cretaceous Inyan Kara group in
BIBLIOGRAPHY OF SANDSTONE-TYPE UKANIUM DEPOSITS, 103

Crook County, Wyo. Carnotite-type minerals and possibly autunite and torbernite occur in sandstone as interstitial fillings and as 

coatings along bedding planes in four ore zones. Many areas of anomalous radioactivity are known. The radioactivity anomalies and 

mineralized areas are on the west flank of an anticline plunging north 

from the main part of the Black Hills uplift.

106 Gregg, C. C., 1952, Reconnaissance and investigational drilling on 

Hoskinninni and Nokai Mesas, San Juan County, Utah, and 

Navajo County, Ariz.: U. S. Atomic Energy Comm. RMO-987, 

10 p., issued by U. S. Atomic Energy Comm. Tech. Inf. Service, 

Oak Ridge, Tenn.

Diamond-drilling programs on Hoskinninni and Nokai Mesas 

demonstrated that these areas do not contain sufficient mineralized 

ground to justify further work by the Federal Government. The 

gross geology is similar to uranium-producing areas in Monument 

Valley. Sediments of the Shinarump conglomerate of Triassic 

age fill channels cut into the underlying Moenkopi formation, also 

of Triassic age. Copper and uranium minerals appear at places 

in sandstone and siltstone in these channels, but the size and grade 

do not satisfy the minimum requirements for ore.

107 Gregory, H. E., 1913, The Shinarump conglomerate: Amer. Jour.

ScL, Ser. 4, v. 35, no. 208, p. 424-438.

The Shinarump conglomerate is a gray to white siliceous sediment of continental origin. It consists of cross beds and lenses 

of pebble conglomerate, coarse sandstone, and fine sandstone. The 

structure and texture vary both vertically and laterally from place 

to place. The formation is resistant to erosion and forms cliffs, 

benches, and tables. Silicified fossil wood is found throughout the 

Shinarump. Though the formation has great areal extent, it is 

usually less than 100 feet thick. The Shinarump conglomerate, 

probably of Late Triassic age, apparently is conformably overlain 

by the Chinle formation of Late Triassic age. In most places it 

rests unconformably on the Moenkopi formation of Permian age 

(now considered Triassic).

108 Gregory, H. E., 1917, Geology of the Navajo country a reconnaissance of parts of Arizona, New Mexico, and Utah: U. S. 

Geol. Survey Prof. Paper 93, 161 p.

The geology of the Navajo country, an area in northeastern Arizona 

and adjacent parts of Utah, Colorado, and New Mexico, is described. 

Exposed consolidated sedimentary rocks in the region are mostly of 

Triassic, Jurassic, and Cretaceous age, but rocks of Precambrian, 

Pennsylvanian, and Eocene age also are present. Relatively large 

areas in the Carrizo Mountains and in the Hopi Buttes area are 

underlain by igneous rocks. Smaller bodies of igneous rocks are 

widely distributed. The sedimentary rocks in the region are horizontal or tilted at low angles except where they have been sharply 

folded into monoclines. Two major structural basins (now called San 

Juan basin and Black Mesa basin) and three major uplifts (now 

called Zuni uplift, Defiance uplift, and Monument uplift) are present 

in the region. The report includes a geologic map of the Navaio 

country at a scale of 1:500.000.
104 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

In Monument Valley a uranium-vanadium mineral, probably carnotite, was found among the pebbles of the Shinarump conglomerate and 

in association with petrified wood of the Chinle formation.

109 Gregory, H. E., 1938, The San Juan country, a geographic and 

geologic reconnaissance of southeastern Utah: U. S. Geol. Survey 

Prof. Paper 188, 123 p.

Exposed sedimentary formations in this region range in age from 

Pennsylvanian to Late Cretaceous. The formations are described, 

and a number of measured sections are presented. Relatively large 

masses of intrusive igneous rocks are present in the Abajo Mountains. 

The main structural features in the area are the Sage Plain downwarp, the Monument upwarp, and the intervening Comb Ridge 

monocline. Smaller folds locally modify these structures. The 

report includes a reconnaissance geologic map of the region at a 

scale of about 1:500,000.

110 Gregory, H. E., and Moore, R. C., 1931, The Kaiparowits region, a

geographic and geologic reconnaissance of parts of Utah and

Arizona: U. S. Geol. Survey Prof. Paper 164, 161 p.

The sedimentary rocks of the Kaiparowits region are chiefly of

Triassic, Jurassic, and Cretaceous age, but Eocene rocks cap the

highest plateaus, and Permian sandstones and limestones are present

in the upwarps. Extrusive igneous rocks of Tertiary age blanket

an area in the northwest part of the region. The Waterpocket

monocline and the East Kaibab monocline are the major flexures of

the region. The Circle Cliffs upwarp, the Kaibab upwarp, and

the Kaiparowits downwarp cover large areas and are modified by

small folds. The Paunsaugunt fault in the northwest part of the

region has a displacement of 1,500 feet. The report includes a

geologic map of the region at a scale of 1:250,000.

111 Grier, A. W., (ed.), 1954, Geology of portions of the High Plateaus 

and adjacent Canyon lands, central and south-central Utah: 

Intermountain Assoc. of Petroleum Geologists, 5th Ann. Field 

Conference [Guidebook], Salt Lake City, Utah, 130 p. 

This publication includes papers on the geomorphology, structural 

history, stratigraphic correlations, and the stratigraphy of the 

Carboniferous, Permian, Triassic, Jurassic, and Cretaceous and 

Tertiary rocks. Each of the formations is described. The stratigraphy and structure of the Capitol Reef area, the Kaiparowits 

region, and the Paunsaugunt Plateau region are described. The 

guidebook also contains papers on the oil and gas fields of the 

region and the uranium deposits at Temple Mountain. A number of 

geologic and structural maps and sections at various scales are 

included.

112 Griggs, R. L., 1953, A reconnaissance for uranium in New Mexico:

U. S. Geol. Survey Circ. 354, 9 p.

A reconnaissance for uranium in New Mexico was made in the 

Datil area in Catron and Socorro Counties, the Cerrillos and the 

Glorieta mining districts in Santa Fe County, the Las Vegas area 

and the Tecolote mining district in San Miguel County, and in an 

area in Colfax County. Significant uranium deposits were found
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 105

only in the Datil area, where one sample contained 0.056 percent 

UsOg. In this area, yellow uranium minerals associated with carbonaceous material and limonite occur in the Mesaverde formation 

of Cretaceous age at the base of sandstone beds which overlie shale.

113 Griggs, R. L., 1954, Datil Mountain area, New Mexico; in Geologic 

investigations of radioactive deposits, Semiannual progress report, June 1 to November 30, 1954: U. S. Geol. Survey TEI-490, 

p. 129-130, issued by U. S. Atomic Energy Comm. Tech. Inf. 

Service, Oak Ridge, Tenn.

Uranium deposits occur in the Mesaverde formation of Cretaceous 

age and in the Baca formation of Tertiary age in this area. The 

uranium is concentrated at the contact of porous sandstones with 

underlying impermeable shale beds and shale stringers. At one locality the uranium is in the thin edge of a lenticular sandstone in 

the Baca formation. Yellow uranium minerals are visible in some 

prospects but the uranium, in an unidentified form, is associated 

mainly with ferruginous and carbonaceous material in sandstone.

114 Gruner, J. W., 1951, Annual report for July 1, 1950 to June 30, 1951; 

part 2, Origin of the uranium deposits in the Shinarump formation A preliminary study: U. S. Atomic Energy Comm. RMO837, 27 p., issued by U. S. Atomic Energy Comm. Tech. Inf. Service, Oak Ridge, Tenn.

Features common to many or all of the uranium deposits in the 

Shinarump conglomerate of Triassic age are reviewed. Most of the 

deposits are associated with fossil carbonaceous material and are 

near the base of channels cut into the underlying rocks, which in 

most places are part of the Moenkopi formation, and are filled with 

irregular lenses and beds of conglomerate, sandstone, and clay. Commonly there is a thin bleached zone directly under the contact. The 

unoxidized parts of the deposits bear no relation to present-day 

topography. The uranium may be associated with vanadium or 

copper or neither, but pyrite is almost always present in the unoxidized ore.

Hypotheses that might explain the origin of uranium deposits in 

the Shinarump conglomerate are the hydrothermal, the concentration 

from the surface water that deposited the Shinarump conglomerate in 

Triassic time, and the concentration from circulating meteoric water 

since the deposition of the Shinarump conglomerate. Gruner favors 

the hypothesis that the surface waters that deposited the Shinarump 

conglomerate also deposited the uranium at the same time. Organic 

matter is thought to have been the precipitating agent.

115 Gruner, J. W., 1954, The origin of the uranium deposits of the 

Colorado Plateau and adjacent regions: Mines Mag., v. 44, no. 3, 

p. 53-56.

The uranium deposits on the Colorado Plateau are in essentially 

flat-lying sedimentary rocks that range in age from Permian to 

Tertiary, but most are in Triassic and Jurassic rocks. The uranium 

is associated with plant remains. The normally red rocks are bleached 

to gray near the uranium deposits, presumably by the same solutions 

which concentrated the uranium.

The rocks containing the ores are flood-plain deposits. Interstratj-
106 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

fied with them are thick volcanic ash beds, now mudstones and silts. 

The volcanic ash presumably contained a small amount of uranium 

which was easily leached by ground-water. During the Laramide 

revolution, tilting and doming of strata caused important changes in 

ground-water flow. At this stage much of the uranium was precipitated by the plant and hydrocarbon materials. The oxidation that 

changed the color of the ores from black to yellow is related to the 

present surface.

116 Gruner, J. W., 1956, A comparison of black uranium ores in Utah, 

New Mexico, and Wyoming: U. S. Geol. Survey Prof. Paper 300, 

p. 203-205; Geology of uranium and thorium, United Nations, 

v. 6, p. 530-532.

Unoxidized uranium deposits in four widely separated areas (Lisbon Valley, Utah; Temple Mountain, Utah; Poison Canyon, N. Mex.; 

and Gas Hills, Wyo.) are compared. The host rocks range in age 

from Triassic to Eocene, and all are poorly sorted arkosic sandstones which contain much organic carbon. Vanadium is not present 

in the deposits in Eocene rocks. The identified dark uranium-bearing 

minerals are uraninite and coffinite. The paragenetic sequence of 

minerals at all four deposits are very similar; the deposits were 

produced by nearly the same geologic processes. The "black ores" 

were deposited in a reducing environment, and they are primary in 

the sense that oxidized yellow ores are derived from them.

117 Gruner, J. W., Gardiner, Lynn, and Smith, D. K., Jr., 1953, Annual 

report for July 1, 1952 to March 31, 1953: U. S. Atomic Energy 

Comm. RME-3044, 58 p., issued by U. S. Atomic Energy Comm. 

Tech. Inf. Service, Oak Ridge, Tenn. 

This report is divided into six independent parts. 

In Part 1 preliminary results of field work in the White Canyon 

and San Rafael Swell areas of Utah are reported. The "flop-over" at 

Temple Mountain, Utah, is described, and the structure is interpreted 

as collapse due to an unknown cause.

In Part 2 four categories of uranium-bearing carbonaceous materials are discussed. They are: lignitic plant material, asphaltite, gilsonite, and liquid hydrocarbons. Uraniferous asphaltite is common 

in the Temple Mountain mines, where it occurs interstitial to sand 

grains and as globules. 

. . Part 3 deals with the synthesis of certain uranium minerals.

In Part 4 the changes in color from red to green of the silts and

shales associated with uranium deposits and uraniferous horizons are

discussed. The color change is due to the destruction of the red

coloring matter, hematite, either by reduction of the iron or by

- chemical reaction of the hematite with hydromicas.

Part 5 is a discussion of the quantity of disseminated uranium 

present in the sedimentary rocks of the Colorado Plateau, and how 

it could have been concentrated into ore bodies.

Part 6 is a discussion of the syngenetic and hydrothermal hypotheses of the origin of the uranium deposits of the Colorado Plateau. 

Gruner believes that the ore minerals probably were precipitated 

from acidic sulfate ground-water solutions. The uranium may have 

been derived from a magmatic source or, as Gruner believes, from a
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 107

sedimentary source. A number of observed facts that may be pertinent to the problem are presented.

118 Gruner, J. W., Gardiner, Lynn, and Smith, D. K., Jr., 1954, Mineral 

associations in the uranium deposits of the Colorado Plateau and 

adjacent regions Interim report: U. S. Atomic Energy Comm. 

RME-3092, 48 p., issued by U. S. Atomic Energy Comm. Tech. 

Inf. Service, Oak Ridge, Tenn.

The mineral associations and paragenetic sequence of the uranium 

ore minerals of the Colorado Plateau are similar in most of the deposits, notwithstanding the preponderance of vanadium-bearing 

minerals in some deposits and sulfides in others. "Black ores" containing uraninite and coffinite are unoxidized and are not necessarily 

of hydrothermal origin.

119 Gruner, J. W., Rosenzweig, Abraham, and Smith, D. K., Jr., 1954, 

The mineralogy of the "Mi Vida" uranium ore deposit of the 

Utex Exploration Company in the Indian Wash area, Utah; 

in Annual Report for April 1, 1953 to March 31, 1954: U. S. 

Atomic Energy Comm. RME-3094, p. 15-27, issued by U. S. 

Atomic Energy Comm. Tech. Inf. Service, Oak Ridge, Tenn. 

The "Mi Vida" vanadium-uranium ore deposit is in calcareous 

sandstone and mudstone lenses in the Chinle formation of Triassic 

age. The area is on the southwest flank of the Lisbon Valley anticline, and the rocks strike 15° - 30° NW and dip about 10° SW. 

The ore body is covered with impervious shale and siltstone. The 

mineralogy of the host rock and ore minerals is described, and the 

origin of the deposit is discussed. Uraninite is the major uranium 

mineral, but tyuyamunite and metatyuyamunite also are recognized. Montroseite, doloresite, and unidentified vanadium minerals 

are present. The ore minerals are associated with abundant carbonaceous material.

120 Gruner, J. W., Towle, C. C., and Gardiner, Lynn, 1951, Uranium 

mineralization in Todilto limestone near Grants, McKinley 

County, N. Mex. [abs.]: Econ. Geology, v. 46, no. 7, p. 802; Geol. 

Soc. America Bull., v. 62, no. 12, p. 1445.

Uranium ores have been found in Todilto limestone near Grants, 

N. Mex., about 75 miles west of Albuquerque. The rocks are a 

part of the southern rim of the San Juan Basin and dip gently 

northward. The Todilto is practically conformably underlain by 

Entrada sandstone. The Summerville formation overlies it. The 

limestone in the area under discussion varies from 3 to 20 feet in 

thickness. Usually, the upper part shows considerable recrystallization. It is in this portion that most of the mineralization is found. 

Here, the minerals carnotite, tyuyamunite, uranophane, and some 

amorphous, ill-defined uranium-vanadium compounds partly replace 

the calcite. Fluorite has been found in two places replacing calcite. 

Pitchblende in minute blebs has been identified. The lower, thinly 

bedded limestone contains uranium only along joints and fractures. 

Very minor amounts of uranium minerals have been discovered in 

the basal few feet of the overlying Summerville. It may be stated 

tentatively that the uranium content is probably of syngenetic origin. 

Diagenesis caused recrystallization of the upper Todilto and some
108 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

concentrations of the ore. Circulating ground water caused much 

later solution and reprecipitation in the ores. Authors' abstract

121 Grutt, E. W., Jr., 1955, Geologic notes on some Wyoming uranium 

districts: Mines Mag., v. 45, no. 3, p. 106-108.

Uranium in Wyoming occurs in veins in Precambrian rocks, in 

sedimentary rocks of Paleozoic and Mesozoic age, and in sedimentary rocks of Tertiary age. The deposits in sedimentary rocks of 

Tertiary age are most important.

In the Owl Creek Mountains, in the Pedro Mountains, and in 

the Laramie Mountains, uraninite occurs in hydrothermal veins in 

Precambrian rocks.

Carnotite deposits occur in sandstones of the Inyan Kara group 

of Early Cretaceous age on the northwest flank of the Black Hills.

Uranium deposits in the Powder River Basin occur in the 

Wasatch formation of Eocene age in two broad areas. In the Pumpkin Buttes area, there are two types of deposits: disseminated and 

concretionary. Both occur in coarse-grained arkosic sandstone but 

are not usually found together. The deposits in Converse County 

are mostly of the disseminated type.

The uranium deposits near Lance Creek, on the southeast margin 

of the Powder River Basin are mostly in arkosic sandstone in the 

White River formation of Oligocene age.

In the Gas Hills area, the majority of the deposits occur in gently 

dipping coarse-grained arkosic sandstone of the Wind River formation of Eocene age. A number of uranium minerals are disseminated in the host rock. In the Owl Creek Mountains, metaautunite is disseminated along seams or bedding in tuffaceous sediments of the Wind River formation.

In the Crooks Gap area in the Green Mountains, uranophane and 

other uranium minerals are disseminated in very coarse-grained 

sandstone and conglomerate in the lower part of the Wasatch formation of Eocene age.

Near Baggs, Wyo., and Maybell, Colo., uranium minerals are 

irregularly disseminated in sandstone of the Browns Park formation of Miocene age.

122 Grutt, E. W., Jr., 1956, Uranium deposits in Tertiary elastics in

Wyoming and northern Colorado: Geology of uranium and

thorium, United Nations, v. 6, p. 392-402; see also, Uranium

deposits in Tertiary sedimentary rocks in Wyoming and northern

Colorado: U. S. Geol. Survey Prof. Paper 300, p. 361-370.

Uranium deposits in the Wyoming sedimentary basins are in

medium- to coarse-grained and conglomeratic sandstones of Eocene,

Oligocene, and Miocene age. Torrential crossbedding is common;

the sandstones have calcareous, ferruginous, or phosphatic cement

and often contain carbonaceous material.

The important uranium minerals in deposits of the Powder River 

Basin are vanadates; the deposits in the Wind River Basin contain mostly phosphates and arsenates; and the principal uranium- 

^'- bearing minerals in deposits of the Green Mountains, Great Divide 

basin, and Washakie basin are silicates and sulphates. Uraninite 

*' has been identified in deposits in the Wind River, Powder River, and
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 109

Washakie basins.

Stratigraphic and lithologic guides to uranium deposits in the 

important districts are suggested. Structure plays an important 

but obscure role, and the size and shape of the deposits range within 

wide limits. The most promising deposits are those which contain 

uranium minerals disseminated in sandstone strata as grain coatings and interstitial fillings. The largest ore body of this type 

probably contains more than 50,000 tons of ore.

Representative deposits from the various areas are described and 

compared with other deposits in similar environments.

123 Gustafson, J. K., 1949, Uranium resources: Nucleonics, v. 4, no. 5,

p. 23-28.

The occurrence of uranium in nature, the potential supply of 

uranium, and the uranium procurement policy of the U. S. Atomic 

Energy Commission are discussed. Uranium deposits are divided 

into four main types: in igneous rocks, in veins of hydrothermal 

origin, in sedimentary rocks, and deposits of doubtful and perhaps 

complex origin. Within the fourth group are the carnotite-type 

uranium deposits of the Colorado Plateau. Tabular or lenticular 

bodies of carnotite-impregnated sandstone are found in certain 

parts of the Morrison and Entrada formations of Jurassic age 

and in the Shinarump conglomerate of Triassic age. The carnotite is commonly associated with other vanadium minerals and 

fossil plant material.

124 Hall, R. B., 1955, Recent uranium developments in the Black Hills: 

Mines Mag., v. 45, no. 3, p. 60,122-123.

The Black Hills is a relatively flat, domal uplift, elliptical in 

shape, and trends northwesterly. Crystalline Precambrian rocks 

are exposed in the core, and sedimentary rocks of Cambrian to 

Cretaceous age form a series of cuestas and hogbacks around the 

core. In the Edgemont district, Fall River County, S. Dak., the 

regional dip is to the southwest; the regional dip is interrupted 

by two large south-plunging anticlines and some minor structural 

features.

Uranium deposits in the Edgemont district, first discovered in 

1951, are mainly confined to the Inyan Kara group of Early Cretaceous age. The Inyan Kara group, in descending order, includes the 

Fall River, Fuson, and Lakota formations. Most of the deposits 

and all of the large producing mines are in areas where the rocks 

dip less than 5°, and generally where there is a sharp change in dip. 

The Gould ore body, the largest mine in the Black Hills, is in the 

basal part of the Fall River sandstone. Near the Gould mine, the 

ore-bearing rock is a buff to brown coarse- to very coarse-grained 

sandstone. The principal ore mineral, carnotite, occurs as interstitial fillings. Another large ore body was discovered during exploratory drilling done to test the validity of the concept of structural control. It is thought that lithologic controls combined with 

structural controls were instrumental in localizing the ore bodies.

An electrical resistivity survey in the drilling area demonstrated 

that a resistivity anomaly exists over the ore body. Resistivity 

techniques may be successful in delimiting favorable ground.
110 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

125 Hatfield, K. G., and Maise, C. R., 1954, Geologic reconnaissance 

of the Defiance uplift, Apache County, Ariz: U. S. Atomic 

Energy Comm. RME-71, 14 p., issued by U. S. Atomic Energy 

Comm. Tech. Inf. Service, Oak Ridge, Tenn.

A search for uranium deposits in the Defiance uplift was concentrated on the Chinle formation of Triassic age. No large deposits 

were found. A number of mineralized localities in the Chinle 

are associated with small concretions and carbonized logs. The 

deposits are surrounded by a zone in which the normal blue or 

purple color has been altered to gray or brownish-orange. Small 

uranium deposits may occur in formations other than the Chinle. 

Formations that range in age from Precambrian to Tertiary are 

exposed in the broad structural feature known as the Defiance 

uplift.

126 Hess, F. L., 1913, Carnotite near Green River, Utah: U.S. Geol.

Survey Bull. 530-K, p. 161-164.

The carnotite deposits near Green River occur in coarse-grained 

crossbedded sandstone of the Flaming Gorge formation (redefined 

in part as the Morrison formation) of Jurassic age. The carnotite 

impregnates the sandstone, coats fractures, and fills small irregular 

cavities. The mineral is associated with iron oxide stains and 

abundant fossil plant material.

127 Hess, F. L., 1913, Notes on the vanadium deposits near Placerville,

Colo.: U.S. Geol. Survey Bull. 530-K, p. 142-156. 

The vanadium mineral roscoelite occurs in a dark fine-grained 

sandstone in the La Plata formation (redefined in part as the 

Entrada sandstone) of Jurassic age. The mineral impregnates the 

sandstone in a few places at about the same stratigraphic horizon 

along several miles of outcrop. The individual deposits are tabular 

and have an outcrop length of as much as 700 feet. Carnotite, which 

is less plentiful than roscoelite, occurs locally along joints in the 

vanadium deposits, Mariposite, a green chromium mineral, is 

disseminated in sandstone and nearly envelopes the vanadium deposits. Inconclusive evidence suggests that the deposits were formed 

from hot water solutions of magmatic origin.

128 Hess, F. L., 1913, Uranium and vanadium: U.S. Geol. Survey, 

Mineral Resources, 1912, Pt. 1, p. 1003-1007.

This report is a brief study of the uranium and vanadium industry of the world in 1912 and a survey of the geology of deposits 

of uranium and vanadium. The deposits discussed are in southwestern Colorado, in Gilpin County, Colo., in several less important 

localities in the United States; and in Central Europe, England, 

Australia, Sweden, Norway, Portugal, France, Russia, East Africa, 

and Madagascar.

The uranium and vanadium minerals in the deposits in southwestern Colorado occur as interstitial fillings in sandstone. There 

are two types of deposits: carnotite and roscoelite. The roscoelite deposits contain a negligible amount of uranium.

129 Hess, F. L., 1914, A hypothesis for the origin of the carnotites of 

Colorado and Utah: Econ. Geology, v. 9, no. 7, p. 675-688.
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 111

The composition and areal occurrence of carnotite are described, 

and hypotheses of the origin of the carnotite deposits are reviewed. 

The carnotite deposits on the Colorado Plateau occur in nearly 

white, crossbedded medium-grained sandstone and are closely associated with carbonaceous fossil material. The carnotite impregnates the sandstone in aureoles around carbonaceous material and 

replaces plant debris and that part of fossil logs which evidently 

was most decayed at the time of burial.

Hess advances the hypothesis that the metals were weathered 

from veins and carried in solution to a shallow sea where they were 

absorbed by or precipitated by decaying organic matter. Upon the 

lifting, draining, and aerating of the rocks the minerals were oxidized to form carnotite and other minerals. During and after 

oxidation the carnotite moved slightly outward to form aureoles 

around the carbonaceous matter.

130 Hess, F. L., 1922, Uranium-bearing asphaltite sediments of Utah: 

Eng. Min. Jour., v. 114, no. 7, p. 272-276.

Uranium and vanadium minerals occur in and associated with 

asphaltite in the Shinarump conglomerate of Triassic age at Temple 

Mountain, Emery County, Utah, on the southeast flank of the 

San Rafael Swell. Fossil plant material is abundant. The asphaltite 

grains are detrital and are deformed around other sand grains. 

The metal-bearing asphaltite is notably harder and blacker than 

is asphaltite that contains no metals. Brightly colored uranium 

and vanadium minerals are conspicuous on the outcrop; they become markedly rarer a few feet from the surface. Ore shoots have 

an irregular ellipsoidal form that is probably due to weathering. 

The feature on part of Temple Mountain called the "flop-over" may 

be due to the action of sulfurous hot springs. Normally red or 

brown sediments are bleached to white; the structure is jumbled, 

and asphaltite is absent. Small masses of uranium ore occur in 

the "flop-over" in the Wingate sandstone of Jurassic age. The 

metals were probably leached from the asphaltite and redeposited; 

the volatile products were lost.

Hess suggests that the uranium and vanadium were picked up 

by the asphaltite grains before or during deposition of the surrounding sediments. The position, size, and shape of the ore shoots, although modified by weathering, are thought to be fortuitous. The 

possibility also exists that the metals were derived from the hot 

springs.

131 Hess, F. L., 1933, Uranium, vanadium, radium, gold, silver, and 

molybdenum sedimentary deposits; in Ore deposits of the 

Western States (Lindgren volume), p. 450-481, Am. Inst. Min. 

Met. Eng., New York.

Uranium and vanadium deposits are widely distributed on the 

Colorado Plateau in rocks of Triassic and Jurassic age. The vanadium may occur without visible plant fossils, but the uranium is 

nowhere found without either fossiliferous or petroliferous carbonaceous material in association.

The uraniferous asphaltite deposits at Temple Mountain, Utah, 

are in the Shinarump conglomerate of Triassic age. The asphaltite
112 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

was deposited with the sand as rolled grains some of which were 

hard enough to hold their shape. The beds contain abundant fossil 

plants. The uranium ore lies in distinct shoots that have an irregular ellipsoidal shape which may be due to weathering. Brightly 

colored uranium and vanadium minerals are also present, mostly 

near the surface. The asphaltite and its contained metals were 

locally corroded and redeposited or removed by hot sulfurous waters 

flowing upward along minor structures.

Large deposits of vanadium ore occur in very fine grained sand-^ 

stone of the La Plata (Entrada) sandstone of Jurassic age near 

Placerville, Colo. The vanadium mineral, roscoelite, impregnates 

the sandstone to form broad thinly lenticular ore bodies. The 

edges are enclosed in a halo of sandstone in which is disseminated, 

a chromium mineral, mariposite. Carnotite stains joints in the 

sandstone, particularly where the vanadium content is high.

The carnotite deposits in the Morrison formation of Jurassic age 

are in crossbedded sandstones in the lower part of the formation. 

Many deposits are confined to replaced logs and the halos around 

them. In some places carnotite forms tiny veinlets in fractures, and 

in others the mineralized rock stops abruptly at fractures. Locally, 

the ore bodies are bounded by smooth rounded "rolls" that cut 

across bedding planes.

The author suggests that the metals were removed from dilute 

solutions directly or indirectly by decaying carbonaceous matter 

at the time of deposition of the sediments.

132 Hewett, D. F., 1923, Carnotite in southern Nevada: Eng. Min. Jour.,

v. 115, no. 5, p. 232-235.

Small noncommercial carnotite deposits have been found in three 

areas in Clark County, Nev., southwest of Las Vegas. Near Sloan 

the carnotite occurs in vertical joints in a Tertiary rhyolite flow. 

The occurrences near Sutor are in a sandstone bed that immediately 

underlies the lowest Permian limestone bed, and those near Goodsprings are in a sandstone bed that overlies the lowest Permian 

limestone bed. The deposits probably were emplaced in relatively 

recent time by surface waters.

133 Hewett, D. F., 1925, Carnotite near Aguila, Ariz.: Eng. Min. Jour.,

v. 120, no. 1, p. 19.

Small noncommercial carnotite deposits occur in a lacustrine 

bentonitic tuff bed that is faulted, tilted, and intruded by dikes. The 

tuff beds overlie Precambrian granite and are overlain by basalt 

flows. The carnotite replaces clay blebs near poorly defined fractures in the tuffs. The deposits were probably formed recently 

by circulating ground water.

134 Hewett, D. F., 1925, Central Arizona holds deposits of carnotite:

Ariz. Min. Jour., v. 9, no. 7, p. 49-50.

Carnotite occurs as small patches along minor crosscutting fractures in drab thin-bedded Tertiary tuffs near Aguila in Maricopa 

County, Ariz. The tuffs are now largely bentonitic clays that total 

more than 200 feet in thickness. They are overlain by several hundred feet of vesicular basalt. The rocks are faulted and dip 10° - 

25° S. The carnotite probably has been deposited recently by circulating ground water.
BIBLIOGEAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 113

135 Hillebrand, W. F., and Ransome, F. L., 1900, On carnotite and associated vanadiferous minerals in western Colorado: Am. Jour. 

Sci., 4th ser., v. 10, no. 56, p. 120-144; 1905, U. S. Geol. Survey 

Bull. 262, p. 9-31.

The first part of this report describes some of the vanadiumuranium deposits in western Colorado, and the second part describes 

chemical analyses of the ores. The deposits were discovered only a 

few years before the report was published and little exploration and 

development had been done.

Vanadium deposits with minor amounts of uranium occur in the 

La Plata sandstone (Entrada sandstone) of Jurassic age near Placerville, Colo. Roscoelite impregnates fine-grained sandstone and may 

replace calcite cement. The vanadiferous material is fairly continuous over about 2,000 feet of outcrop but has no constant thickness; it locally splits into two or more layers. A thin discontinuous 

seam of sandstone impregnated with carnotite occurs near the base 

of the vanadiferous material.

The deposits at La Sal Creek are in massive nearly white sandstone 

in the McElmo formation (Morrison formation) of Jurassic age. 

Carnotite impregnates the sandstone along bedding planes and minor 

fractures. The deposits are small, discontinuous, and superficial. 

At the Roc Creek deposit carnotite impregnates sandstone and 

fills small openings along the hanging wall of a fault. At several 

other deposits in the region carnotite also impregnates the sandstone host rock.

The deposits of carnotite and roscoelite were formed subsequent 

to the deposition of the host rocks. The origin of the roscoelite 

deposits is not clear, but the carnotite deposits are thought to have 

been formed at the present surface of the ground by evaporation of 

uraniferous ground water. The metals were originally disseminated 

in the mass of the host formations.

136 Hilpert, L. S., and Freeman, V. L., 1956, Guides to uranium deposits 

in the Gallup-Laguna area, New Mexico: Geology of uranium and 

thorium, United Nations, v. 6, p. 346-349; see also, Guides to 

uranium deposits in the Morrison formation, Gallup-Laguna 

area, New Mexico: U. S. Geol. Survey Prof. Paper 300, p. 299-302.

Significant quantities of uranium ore have been produced in New 

Mexico; most of the total has come from the Gallup-Laguna area 

of McKinley and Valencia Counties where the ore occurs mostly in 

the Todilto limestone and the Morrison formation, both of Jurassic 

age. A large part of the reserves in New Mexico are in the Brushy 

Basin member of the Morrison formation in the Gallup-Laguna 

area.

The Brushy Basin member consists mostly of claystone with subordinate amounts of sandstone, conglomerate, and limestone; it ranges 

in thickness from a knife-edge to about 375 feet. The larger deposits in the Brushy Basin member generally occur in the thicker 

parts of relatively coarse grained sandstone units. Preliminary ore 

guides and methods of prospecting have been developed for two of 

these sandstones the so-called Poison Canyon and Jackpile sandstone units.
114 SELECTED BIBLIOGRAPHIES OF UEANIUM GEOLOGY

137 Hinckley, D. N., and Volgamore, J. H., 1953, Reconnaissance of

Little Wild Horse Mesa, Green River Desert, Emery County,

Utah: U.S. Atomic Energy Comm. RME-43, 14 p., issued by

U. S. Atomic Energy Comm. Tech. Inf. Service, Oak Ridge, Tenn.

Uranium occurrences on Little Wild Horse Mesa are in mediumto coarse-grained crossbedded sandstone near the middle of the

Salt Wash member of the Morrison formation of Jurassic age.

Two of the three mineralized localities may have some economic

importance.

138 Huff, L. C., 1955, Preliminary geochemical studies in the Capitol 

Reef area, Wayne County, Utah: U. S. Geol. Survey Bull. 

1015-H, p. 247-256.

A bleached zone at the base of the Chinle formation near the 

Oyler mine, Wayne County, Utah, was studied to establish whether 

there was a chemical relationship between bleaching in the Chinle 

and uranium mineralization in the Shinarump conglomerate. The 

preliminary results suggest that the bleaching was accompanied by 

a slightly reducing acid solution which deposited zinc and copper 

but no uranium in the bleached zone. A field test for heavy metals 

which has been devised for geochemical prospecting appears to be 

satisfactory for detecting and tracing such mineralization effects. 

It is hypothesized that the solution which bleached the Chinle also 

deposited uranium in the Shinarump, but more work is needed to 

clarify this relationship. Author's abstract

139 Huleatt, W. P., Hazen, S. W., Jr., and Traver, W. M., Jr., 1946, 

Exploration of vanadium region of Western Colorado and 

Eastern Utah: U. S. Bur. Mines. Kept. Inv. 3930, 30 p. 

Core-drilling on the Colorado Plateau from May to December 1943 

was done by the Bureau of Mines to stimulate wartime production 

of vanadium ore. Eight hundred ninety-five core-drill holes having 

an aggregate depth of 38,510 feet were distributed among 46 areas. 

Small maps, short descriptions of each area and assay data are included in the report.

The deposits explored are carnotite ore bodies in the Morrison 

formation of Jurassic age. The ore bodies are tabular, irregular 

in shape, and generally conform to the bedding. The uranium and 

vanadium minerals impregnate the sandstone and may locally replace fossil wood.

140 Hunt, C. B., 1953, Geology and geography of the Henry Mountains

region, Utah: U.S. Geol. Survey Prof. Paper 228, 234 p. 

The Henry Mountains are situated in a structural basin; exposed 

sedimentary rocks aggregate about 8,000 feet in thickness and include rocks of Permian, Triassic, Jurassic, Late Cretaceous, and 

Quaternary age. More than 80 percent of the pre-Cretaceous rocks 

are of continental origin; most of the Upper Cretaceous rocks are 

marine. Faults are generally uncommon. Each of the Henry 

Mountains is a structural dome produced by the injection of stocks 

and laccolithic masses. The report includes geologic and structural 

maps of the region at a scale of about 1:125,000, and geologic maps 

of Mount Killers, of Mount Holmes and Mount Ellsworth, and of 

Mount Ellen and Mount Pennell, all at the scale of 1:31,680.
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 115

Vanadium- and uranium-bearing minerals locally impregnate the 

sandstone and replace fossil plant remains in the lower part of the 

Morrison formation of Jurassic age on the east side of the Henry 

Mountains. Similar deposits, some of which contain copper, occur 

in the Shinarump conglomerate of Triassic age in areas adjacent 

to this region.

141 Huttl, J. B., 1954, New Mexico uranium: Eng. Min. Jour., v. 155,

no. 8, p. 96-99.

This report deals mainly with the uranium mining and milling 

operations of the Anaconda Copper Mining Company in the Grants 

district, New Mexico. The Anaconda's Section 9 mine near Grants 

is in the Todilto limestone of Jurassic age, and the Jackpile mine, 

also an Anaconda property, is in the Westwater Canyon member of 

the Morrison formation of Jurassic age. The carnotite ore body 

at the Jackpile mine is cut by a diabase sill.

142 Isachsen, Y. W., 1954, Ore deposits of the Big Indian Wash-Lisbon 

Valley area; in Uranium deposits and general geology of southeastern Utah: Utah Geol. Society, Guidebook to the geology of 

Utah, no. 9, p. 95-105, Salt Lake City, Utah.

Uranium deposits in the Big Indian Wash-Lisbon Valley area 

are mostly in the Chinle formation of Triassic age, but small deposits occur in the Cutler formation of Permian age. The 

uranium-producing area is on the southwest flank of the faulted 

northwest-trending Lisbon Valley anticline, which is probably a 

salt structure.

In the deposits in the Chinle formation, uraninite and montroseite 

replace calcite cement, and uraninite also replaces coalified logs and 

carbonaceous debris. Pyrite is fairly abundant. The deposits, all 

of which are in the lower part of the formation, are sometimes 

directly on the underlying Cutler formation. Ore does not follow 

the host rock uniformly, nor does it follow primary textures in detail 

The host rock includes siltstone, fine- to coarse-grained arkosic 

sandstone, and conglomerate. The most favorable host rock is 

gray-green fine- to coarse-grained arkosic sandstone cemented with 

calcite.

The deposits in the Cutler formation consist of carnotite and 

becquerelite disseminated in streaks, pods, and patches in fluvial 

arkose lenses.

143 Isachsen, Y. W., 1954, Uranium deposits, Big Indian Wash-Lisbon 

Valley area, San Juan County, Utah [abs.]: Econ. Geology, 

v. 49, no. 7, p. 804; Geol. Soc. America Bull., v. 65, no. 12, 

p. 1267-1268.

Extensive bedded uranium deposits have been discovered ... along 

the southwest limb of the Lisbon Valley salt anticline. The major 

ore bodies are confined to the lower portion of the Triassic Chinle 

formation which unconformably overlies the Permian Cutler formation. Arkosic, gray to black sandstone with intercalated lenses 

of gray-green mudstone and mudstone pebble conglomerate contain 

uraninite which has replaced carbonaceous material and calcite 

cement. Locally, solid masses of pure uraninite result from replacement of organic material. Montroseite occurs with uraninite
116 SELECTED BIBLIOGEAPHIES OF URANIUM GEOLOGY

in the major deposits discovered to date. Tyuyamunite frequently 

forms surface coatings along fractures. Thickness of ore in the area 

is generally sufficient to permit mining with little or no waste rock. 

In several areas known to contain ore bodies, the gray-green color 

of the lower Chinle formation extends upwards into the overlying 

red Chinle mudstones in the manner of an alteration halo. About 

100 feet beneath the Chinle ore horizon are arkosic lenses in the 

Cutler formation which contain, in some instances, low grade uranium mineralization. The ore minerals, carnotite and becquerelite, 

are disseminated in the arkose with greatest concentration adjacent 

to fractures. The oxidized state of these minerals coupled with 

the concentration near fractures suggests that the Cutler mineralization is due to leaching from uraninite ore bodies in the Chinle 

formation. Author's abstract

144 Isachsen, Y. W., 1956, Geology of uranium deposits of the Shinarump 

and Chinle formations on the Colorado Plateau: Geology of 

uranium and thorium, United Nations, v. 6, p. 350-367; see 

also, Isachsen, Y. W., and Evensen, C. G., 1956, Geology of 

uranium deposits of the Shinarump and Chinle formations 

on the Colorado Plateau: U. S. Geol. Survey Prof. Paper 300, 

p. 263-280.

Large uranium deposits are present in the Shinarump conglomerate of Triassic age in Monument Valley, Ariz., and White Canyon, 

Utah; and in the Chinle formation, also of Triassic age, near 

Cameron, Ariz., and in the Big Indian Wash-Lisbon Valley and 

Temple Mountain areas in Utah.

Both formations are of continental origin. The Shinarump conglomerate consists dominantly of light-gray sandstone with lenses 

of grit and conglomerate, and smaller quantities of interbedded 

mudstone. The base of the Shinarump conglomerate fills ancient 

stream channels cut into the underlying Moenkopi formation, also of 

Triassic age. Carbonaceous plant debris is common in the channelfills. The Chinle formation is predominantly a fluvial, sequence of 

red to brown siltstone and mudstone interbedded with sandstone 

and conglomerate. Carbonaceous plant remains are widely distributed in the formation; asphaltite occurs locally.

Copper, copper-uranium, and vanadium-uranium deposits have 

been found in both formations. Oxidized and unoxidized ore minerals frequently occur together; however, the principal uranium 

mineral in most deposits is uraninite. The ore minerals are disseminated in sandstone, siltstone, and conglomerate, and locally 

replace carbonaceous plant material and calcite cement.

Uranium deposits in the Shinarump conglomerate are restricted 

to ancient stream channels and are usually low on the flanks or 

in the bottom of the channels. The deposits in the Chinle formation 

are not restricted to channels nor to any one stratigraphic unit in 

the formation, but most large deposits occur in sandstone or coarser 

clastic rocks in the lower half of the formation. The principal ore 

controls in the larger deposits of the Chinle formation appear to be 

structural rather than sedimentary. Bleaching or other discoloration of red beds above and below the deposits in the Chinle formation may be used as an exploration guide.
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 117

Age determinations indicate that the uranium deposits are epigenetic, but the source of the metals is not known. Localization 

of ore in channel fills and other permeable clastic units which contain carbonaceous plant material suggests that transmissibility is 

an important local ore control and that carbonaceous material is 

the main precipitant.

145 Isachsen, Y. W., Mitcham, T. W., and Wood, H. B., 1955, Age and 

sedimentary environments of uranium host rocks, Colorado 

Plateau: Econ. Geology, v. 50, no. 2, p. 127-134. 

Uranium deposits have been found on the Colorado Plateau in a 

Tertiary monzonite porphyry and in 32 sedimentary units that range 

in age from Pennsylvanian to Tertiary. At least one example in 

each formation is briefly described. Ore has been produced from 

22 of these units. Host rocks represent all of the principal sedimentary environments except the glacial. The wide variation in 

age and depositional environments of the host rocks suggests an 

epigenetic origin for uranium ore on the Colorado Plateau.

146 Jobin, D. A., 1956, Regional transmissivity of the exposed sediments 

of the Colorado Plateau as related to distribution of uranium 

deposits: U. S. Geol. Survey Prof. Paper 300, p. 207-211; Geology 

of uranium and thorium, United Nations, v. 6, p. 317-320. 

A study of regional transmissivity of the sedimentary rocks of 

the Colorado Plateau has been made to relate variations in transmissivity to the position of known ore deposits. Transmissivity is 

defined as the capacity of a sedimentary rock as a whole to transmit 

fluids. The coefficient of transmissivity of sedimentary rock at a 

given locality is equal to the product of its thickness and mean 

permeability.

The sedimentary rocks on the Colorado Plateau may be divided 

into two groups on the basis of their transmissivity. Shales, mudstones, evaporites, and limestones are in effect nontransmissive because of their very low permeability. Conglomerates, sandstones, 

and siltstones are permeable and, therefore, the transmissive groups. 

The transmissive rocks may be separated into two groups: eolian 

sandstones of relatively uniform permeability and thickness, and 

fluvial sandstone, siltstone, and conglomerate which have a great 

range of permeability and thickness. The second group contains 

most of the uranium deposits in the Colorado Plateau. There is, 

however, no apparent correlation between position of ore deposits 

within a particular host rock and its regional permeability or 

transmissivity.

147 Jones, D. J., 1954, Sedimentary features and mineralization of the 

Salt Wash sandstone at Cove Mesa, Carrizo Mountains, Apache 

County, Ariz.: U.S. Atomic Energy Comm. RME-3093 (pt. 2), 

40 p., issued by U. S. Atomic Energy Comm. Tech. Inf. Service, 

Oak Ridge, Tenn.

Uranium deposits at Cove Mesa are in sandstone beds in the 

Salt Wash member of the Morrison formation of Jurassic age. 

Mineralized areas flank the curving trends of areas which have a 

high sandstone: shale ratio. The Salt Wash stream channels changed
118 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

direction from northwesterly to northeasterly in the Cove Mesa 

area. Areas marginal to Salt Wash channels, particularly where 

the channels changed direction, are apparently most favorable for 

the occurrence of uranium deposits. Cyclic repetition of rock types 

was observed in the Salt Wash member. The sequence includes a 

massive friable sandstone, capped by a thinner and strongly crossbedded sandstone, and is normally repeated three times. The uranium 

deposits are largely confined to the massive friable type of sandstone.

148 Joubin, F. R., 1955, Widespread occurrence and character of uraninite in the Triassic and Jurassic sediments of the Colorado

Plateau a discussion: Econ. Geology, v. 50, no. 2, p. 233-234.

This paper is a short comment on the paper of the same name by

Rosenzweig, Gruner, and Gardiner (Ref. no. 215). Joubin observes

that uranium is associated with hydrocarbons (thucolite) in a

number of localities in the Precambrian rocks of Canada, but is

absent from adjacent graphitic rocks. He suggests that the agent

active in the precipitation of uranium is not elemental carbon but

rather the hydrocarbon fraction (resin) that was once present.

149 Kaiser, E. P., 1951, Uraniferous quartzite, Red Bulff prospect,

Gila County, Ariz.: U. S. Geol. Survey Circ. 137, 10 p. 

Radioactivity is present in two zones in the silty upper part of 

the Dripping Spring quartzite of Precambrian age at the Red 

Bluff prospect in Gila County, Ariz. An unidentified uranium 

mineral, possibly pitchblende, is rather evenly disseminated through 

most of the rock in the deposits, but black streaks and fractures 

within the deposits contain a greater amount of uranium. Stratigraphic control of the radioactive zones is indicated by the restriction of the zones to two layers, each about 20 feet thick. The rock 

in the radioactive zones has been bleached and partly recrystallized. 

The uranium deposits are epigenetic and probably of hydrothermal 

origin.

150 Kelley, D. R., 1954, Drilling in the North Point No. 6 and Horn 

Channels, White Canyon, San Juan County, Utah: U.S. Atomic 

Energy Comm. RME-63, 33 p., issued by U. S. Atomic Energy 

Comm. Tech. Inf. Service, Oak Ridge, Tenn.

The Shinarump conglomerate of Triassic age in the North Point 

No. 6 and Horn channels was explored by drilling. Two of the 

52 diamond-drill holes penetrated ore-grade material. However, 

no ore bodies were found. Uranium silicates and secondary copper 

minerals are locally present in the channels. It is thought that 

the sediments contain too little carbonaceous material and that 

the sandstone is too fine-grained to be a suitable host rock.

151 Kelley, V. C., 1956, Influence of regional structure and tectonic 

history upon the origin and distribution of uranium on the 

Colorado Plateau: U.S. Geol. Survey Prof. Paper 300, p. 171- 

178; Geology of uranium and thorium, United Nations, v. 6, 

p. 299-306.

Although primary sedimentary structures are important factors 

in the localization of uranium in the rocks of the Colorado Plateau, 

the regional structure strongly influences the distribution and 

perhaps the origin of the uranium deposits.
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 119

Aspects of the regional structure are discussed in three parts. 

In the first of these, the structural elements are described and a 

tectonic subdivision of the Colorado Plateau made. In the second 

part, the geologic and tectonic history of the Colorado Plateau is 

interpreted from sedimentary thicknesses, the lithologic character 

of the rock, and unconformities. The third part is a discussion 

of tectonic influences on origin and distribution of uranium.

Geologic factors which may have been affected by tectonic events 

and which may have affected the distribution of ore include the 

geologic environments, paleohydrology, igneous activity, and erosional history.

152 Kelley, V. C., 1955, Regional tectonics of the Colorado Plateau 

and relationship to the origin and distribution of uranium: 

Univ. of N. Mex. publications in geology, no. 5, Univ. of N. Mex. 

Press, Albuquerque, 120 p.

The relationship between regional structure and regional concentration of uranium deposits was studied. The report of this 

study consists of three principal parts: (1) a description and analysis of the regional tectonics, (2) a geologic history, and (3) a 

discussion of the tectonic influence on distribution and origin of 

uranium.

In the first part the structural elements are described and tectonic 

subdivisions of the Colorado Plateau are made. Within the principal tectonic subdivisions are a host of minor structures such as 

folds, faults, joints, and intrusive centers which are described and 

discussed from a regional point of view.

In the second part the sedimentational and tectonic histories of 

the Colorado Plateau are outlined as interpreted from sedimentary 

thicknesses, the nature of the rocks and unconformities.

In the third part, which deals with the relation between regional 

structure and uranium distribution on the Colorado Plateau, the 

conclusion is reached that little if any direct relation exists. However, tectonic events have had an important bearing on other geologic features that may have contributed directly to the origin and 

distribution of uranium. These factors are included in a discussion 

of provenances and environments, paleohydrology, igneous activity, 

and erosional history.

153 Kentro, D. M., 1954, Processing uranium ores: Min. Cong. Jour., 

v. 40, no. 12, p. 58-60, 71.

The two basic methods of processing uranium ores from the 

Colorado Plateau are the acid leach and the carbonate leach. These 

hydrometallurgical processes are modified, when necessary, to fit 

the different types of ore. The details of many of the different 

steps are not revealed, and improvements on the processes are 

being made continually.

In the acid leach, the crushed ore may first be roasted to destroy 

carbonaceous material, thus reducing acid consumption. If both 

uranium and vanadium are to be recovered, salt is added to 

the roaster feed to convert the vanadium to a water-soluble compound; when the conversion is complete, the vanadium is removed 

by a water leach. The residue goes to the sulfuric acid tanks
120 SELECTED BIBLIOGBAPHIES OF URANIUM GEOLOGY

where leaching for from 1 to 24 hours at temperatures of 30° - 40° C 

is normally sufficient to dissolve the uranium. Separation of the 

leach solution from the solids is difficult, but baking the ores before 

leaching and adding certain chemicals usually improves filtering 

and settling rates sufficiently. The uranium may be separated 

from the leach solution by several methods.

The carbonate leach process is particularly useful on ores that 

have a high content of lime. A solution containing 5 to 10 percent 

sodium carbonate and 1 to 5 percent sodium bicarbonate is used. 

Leaching times of 4 to 24 hours at temperatures of 70° - 115° C 

are normally sufficient for good recoveries. The addition of an 

oxidizing agent is usually necessary. If sufficient vanadium is 

present in the ore, the metals can be precipitated from the leach 

solution by lowering the pH, and if not, caustic soda is added to 

precipitate the uranium. The uranium-bearing product from both 

processes may be shipped as yellow cake, or it may be fused and 

shipped as black oxide of uranium.

154 Keys, W. S., 1956, Deep drilling in the Temple Mountain collapse, 

San Rafael Swell, Utah: Geology of uranium and thorium, 

United Nations, v. 6, p. 371-378; see also, Keys, W. S., and 

White, R. L., 1956, Investigation of the Temple Mountain 

collapse and associated features, San Rafael Swell, Emery 

County, Utah: U. S. Geol. Survey Prof. Paper 300, p. 285-298. 

The collapse area at Temple Mountain is about 500 feet wide 

and 1,500 feet long; the maximum vertical displacement is about 

300 feet. The core obtained from deep drilling (500-900 feet) shows 

that the rock has undergone flowage, fracturing, and alteration. 

Minerals present include pyrite, galena, arsenopyrite, realgar, pitchblende, unidentified uranium and vanadium minerals, and abundant 

asphalt.

The Sinbad and Kaibab limestones are missing in the six holes 

completed to date. Absence of the limestones suggests that the 

solution of carbonate rocks was in part responsible for the collapse 

of overlying sediments.

A new ore layer has been found at the top of the Coconino sandstone in a conglomerate of chert geodes and nodules cemented by 

asphaltic sandstone. This conglomerate occupies the stratigraphic 

position of the Kaibab limestone and probably represents insoluble 

remnants of the Kaibab. Weakly mineralized layers, associated 

with hard asphalt, were noted at various depths within the collapsed 

area.

155 Kimball, Gordon, 1904, Discovery of carnotite: Eng. Min. Jour.,

v. 77, no. 24, p. 956.

In May, 1898, the author shipped 10 tons of carnotite ore containing 

21.5 percent UsOg and more than 15 percent "V^Os from claims on Roc 

Creek, Montrose County, Colo., to Denver, Colo., where it was sold 

for $2,600. The yellow ore occurs in white sandstone as disseminated 

grains, bedded veins, seams, occasional pockets, and vug fillings.

156 King, J. W., 1951, Geology and ore deposits of Mesa V, Lukachukai 

district, Arizona: U. S. Atomic Energy Comm. RMO-754, 17 p.,
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 121

issued by U. S. Atomic Energy Comm. Tech. Inf. Service, Oak

Ridge, Term.

Vanadium-uranium deposits on Mesa V are in the lower part 

of a fine-grained sandstone unit in the Salt Wash member of the 

Morrison formation of Jurassic age. The unit is from 65 to 95 feet 

above the base of the formation. The: light-tan limonite-stained 

sandstone is from 15 to 25 feet thick and contains thin mudstone 

beds which are bleached to gray near the ore deposits. The ore 

minerals, principally carnotite and vanoxite, impregnate the sandstone and coat the sand grains. Fossil carbonaceous material is 

locally abundant and at places is mineralized. The ore bodies on 

Mesa V are small but numerous; the deposits on Mesa Four-and-ahalf are generally similar but are more numerous and of higher 

grade.

157 King, J. W., 1951, Reconnaissance of Red Rock district, Cove Mesa, 

and Kinusta (Tree) Mesa, Ariz.: U.S. Atomic Energy Comm. 

RMO-755, 11 p., issued by U. S. Atomic Energy Comm. Tech. 

Inf. Service, Oak Ridge, Tenn.

All known vanadium-uranium ore deposits in the Red Rock district 

and the Cove Mesa and Kinusta Mesa areas are in the lower part 

of the Salt Wash member of the Morrison formation of Jurassic 

age. The Salt Wash member is about 200 feet thick and is composed of gray to brown fine-grained quartzose sandstone interbedded with red or green mudstone lenses a maximum of 5 feet 

thick. The small ore bodies are as much as 3 feet thick. Carnotite 

is the principal uranium mineral.

158 King, J. W., and Ellsworth, P. C., 1951, Geology and ore deposits of 

Mesa VII, Lukachukai district, Arizona: U. S. Atomic Energy 

Comm. RMO-803, 8 p., issued by U,, S. Atomic Energy Comm. 

Tech. Inf. Service, Oak Ridge, Tenn.

Carnotite and vanoxite impregnate a light-tan sandstone at one 

place on the rim of Mesa VII. The sandstone bed is in the Salt Wash 

member of the Morrison formation of Jurassic age and is about 40 

feet above the base of the formation. The ore exposure is less than 

1 foot thick and is underlain by a green mudstone bed. The Salt Wash 

member on Mesa VII is composed of predominantly pink fine- to 

coarse-grained quartzose sandstone and interbedded red mudstone.

159 Klemic, Harry,, and Baker, R. C., 1954, Occurrences of uranium in 

Carbon County, Pa.: U. S. Geol. Survey Circ. 350, 8 p.

Uranium vanadates, carbonates, and silicates occur in coarse 

graywacke conglomerate near the base of the Pottsville formation, of 

Pennsylvanian age, on the north limb of the Panther Valley syncline; 

and on the south limb, autunite and uranium silicates occur in graywacke sandstones near the top of the Catskill formation of Devonian 

age. Uraniferous graywacke sandstone occurs in the upper part of 

the Catskill formation near Butcher Hollow and near Penn Haven 

Junction in minor anticlines of the Broad Mountain anticline. Qmall 

amounts of kasolite and galena occur in the vicinity of Penn Haven 

Junction. Authors' Abstract

The three uranium deposits in the Catskill formation appear to be 

at about the same stratigraphic horizon. The uranium minerals coat
122 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

fractures and are disseminated in the rock in lenses in discontinuously 

radioactive zones. The occurrences are all in gray or greenish-gray 

rock that contains finely divided carbonaceous material rather than 

in the red parts of the formations.

160 Knoerr, A. W., and Lutjen, G. P., editors, 1954, UsOg Formula for

profits: Eng. Min. Jour., v. 155, no. 9, p. 87-118. 

This article is a collection of several papers by several authors and 

deals mainly with the economic aspects of the uranium industry on 

the Colorado Plateau. Exploration and development, mining, and 

milling of ore are covered. Diagrams illustrating various ore controls 

and ore guides are included in a generalized discussion of the geology 

of the ore deposits.

161 Koeberlin, F. R., 1938, Sedimentary copper, vanadium-uranium, and 

silver in southwestern United States: Econ. Geology, v. 33, no. 4, 

p. 458-461.

This short communication was prompted by R. P. Fischer's paper 

of similar title published in 1937 in Economic Geology. Koeberlin 

suggests that the metals may have been derived from pyroclastic 

material. As explained by W. H. Emmons, mineral-bearing fluids 

expelled from cooling magmas may collect in domes and cupolas 

near the roofs. If the magmatic extract enters fractures and permeable zones, veins are formed. However, if the roof is not strong 

enough to confine the magma, the material may be ejected into the 

atmosphere as volcanic ash. The metallic content of the ash beds 

would be easily available to surface- or ground-water solutions because of the minute size of the metal-bearing particles.

162 Laverty, R. A., and Gross, E. B., 1956, Paragenetic studies of uranium deposits of the Colorado Plateau: U. S. Geol. Survey Prof. 

Paper 300, p. 195-201; Geology of uranium and thorium, United 

Nations, v. 6, p. 533-539.

Detailed paragenetic studies have been made of several uranium 

deposits in Utah, Arizona, and New Mexico, and less detailed studies 

have been made of many other uranium deposits on the Colorado 

Plateau.

The composite paragenetic sequence is that expected in uranium 

ores deposited near the surface by juvenile water. 

Paragenesis of these deposits is similar in that: 

The uranium minerals occur as cement. 

The earliest uranium minerals are always the lower valence

oxides. 

The uranium minerals are usually associated temporally and

spatially with base metal sulfides. 

Oxidized uranium minerals are found only in the youngest

part of the sequence.

Similarities of the composite paragenetic sequence to that of the 

deposits of hydrothermal origin at Marysvale, Utah, are: 

Early silicification and fluoritization. 

Close association of uranium and sulfide minerals in both time

and space. 

Early U+4 minerals and late U+6 minerals.
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 123

163 Lindgren, Waldemar, 1933, Vanadium and uranium ores in sandstone; in Mineral deposits: 4th ed., New York and London, 

McGraw-Hill Book Company, Inc., p. 409-415.

Vanadium with some uranium and a trace of radium is common 

in gently inclined white crossbedded sandstones of the McElmo 

formation (Morrison formation) and La Plata sandstone (Entrada 

sandstone), both of Jurassic age, in western Colorado and eastern 

Utah. The three most important minerals are carnotite, vanoxite, 

and roscoelite. The carnotite ores are always associated with fossil 

wood. Lindgren suggests that the uranium and vanadium were 

concentrated by possibly tepid meteoric waters which leached the 

metals from terrigenous sediments derived from the disintegration 

of Precambrian igneous rocks and pegmatites.

164 Love, J. D., 1952, Preliminary report on uranium deposits in the 

Pumpkin Buttes area, Powder River Basin, Wyo.: U. S. Geol. 

Survey Circ. 176, 37 p.

Elongate concretionary bodies of uranium ore occur in sandstone 

beds in the Wasatch formation of Eocene age near the Pumpkin 

Buttes in northeastern Wyoming. Yellow and black uranium minerals are present but have not been specifically identified. Selected 

samples have contained more than 15 percent uranium. The host 

rocks are soft porous pink or tan medium- or coarse-grained crossbedded sandstones at several stratigraphic horizons and are persistent over a considerable area. The Pumpkin Buttes lie near the 

center of the Powder River Basin, a topographic and structural 

feature. The sedimentary rocks at Pumpkin Buttes are about 

16,000 feet thick. Several deposits are described in some detail. 

The author suggests that the uranium was leached from overlying 

tuffaceous sedimentary rocks (now largely removed by erosion) and 

redeposited in the present location by ground water.

165 Love, J. D., 1953, Preliminary report on uranium deposits in the 

Miller Hill area, Carbon County, Wyo.: U. S. Geol. Survey 

Circ. 278, 10 p.

Most of the erratically distributed uranium deposits in the Miller 

Hill area of southern Wyoming occur in an algal limestone marker 

bed in the Browns Park formation of Miocene (?) age. The Browns 

Park formation is more than 1,000 feet thick, and consists of basal 

conglomerate, tuffs, tuffaceous limy sandstones, and thin persistent 

radioactive algal limestone beds. The formation unconformably 

overlies Precarnbrian crystalline rocks and slightly tilted and truncated rocks of Paleozoic, Mesozoic, and Cenozoic age. The disseminated uranium in the limestone marker bed is thought to be partly 

syngenetic. No uranium minerals were noted. The highest analysis 

showed 0.15 percent uranium, but most samples contained much less. 

The geologic column and the sampled localities are described.

166 Love, J. D., 1954, McComb area, Wyoming; in Geologic investigations of radioactive deposits, Semiannual progress report, 

December 1, 1953 to May 31, 1954: U.S. Geol. Survey TEI-440, 

p. 175-178, issued by U. S. Atomic Energy Comm. Tech. Inf. 

Service, Oak Ridge, Tenn. 

The McComb area is in the northern part of the Wind River
124 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

Basin near the Owl Creek Mountains in Fremont County, Wyo. 

Most of the uranium deposits in the area are in the Tepee Trail (?) 

formation of late Eocene (?) age. Autunite, schroeckingerite, and 

other uranium minerals occur in bentonitic claystone, bentonitic 

sandstone, arkosic sandstone, and boulder conglomerate. The adjoining Precambrian granite is locally radioactive.

167 Love, J. D., 1954, Preliminary report on uranium in the Gas Hills 

area, Fremont and Natrona Counties, Wyo.: U. S. Geol. Survey 

Circ. 352,11 p.

Uranium deposits occur in the Thermopolis shale of Cretaceous 

age, in the Wind River formation of early Eocene age, and in rocks 

of middle Eocene age in the Gas Hills area of central Wyoming. 

The Cretaceous and older rocks are folded; the Tertiary rocks are 

almost horizontal. The Wind River formation was deposited on an 

irregular erosion surface developed on the Cretaceous and older 

rocks.

The uranium deposit in 'the Thermopolis shale is near the contact with the Wind River formation. The uranium was probably 

deposited in the shale from ground water solutions ponded by the 

erosion surface. The deposit is not of ore grade.

In most of the uranium ore deposits in the Wind River formation 

the uranium minerals meta-autunite(?), uranospinite(?), and an unidentified uranium mineral are disseminated in medium- to coarsegrained or conglomeratic sandstone, but some small low-grade deposits 

have been found in carbonaceous shale. Sonie of the deposits are in 

clayey sandstone, and some are associated with ferruginous concretions or beds. Samples selected from the deposits have contained 

as much as 10 percent uranium.

The uranium occurrence in the middle Eocene rocks is near the 

base of the sequence in a ferruginous coarse-grained conglomeratic 

sandstone. It does not contain ore-grade material.

The author suggests that uranium was leached from, younger 

tuffaceous Tertiary rocks by ground water and transported downward 

and laterally to environments favorable for deposition.

168 Love, J. D., 1954, Uranium in the Mayoworth area, Johnson County, 

Wyo. A preliminary report: U. S. Geol. Survey Circ. 358, 7 p. 

The uranium mineral tyuyamunite occurs in a hard gray oolitic 

marine limestone at the base of the Sundance formation of Jurassic 

age in the Mayoworth area, Wyoming. This limestone bed is about 

20 feet thick in the area, but it thins and disappears to the north 

and south. The rest of the Sundance formation is composed of 

marine sandstone and shale. The Sundance in this area is underlain by the Chugwater formation of Triassic age and is overlain 

by the Morrison formation of Jurassic age. The area is on the east 

flank of the Bighorn Mountains, and the rocks dip 10° - 15° NE. 

Metatyuyamunite coats fractures in the limestone and replaces the 

oolites. Selected samples contain as much as 0.71 percent uranium. 

Radioactivity is evident along some ferruginous brown clayey partings in the limestone. Dinosaur bones in the Morrison formation 

were radioactive wherever tested, but no significant amount of 

radioactivity was noted in the surrounding rocks. The uranium
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 125

was apparently deposited in the limestone from ground water solutions. The author suggests that the uranium was derived from the 

White River formation of Oligocene age which truncates the older 

rocks about 2,500 feet higher, structurally, than the uranium 

deposits.

169 Levering, T. G., 1954, Radioactive deposits of Nevada: U.S. Geol. 

Survey Bull. 1009-C, p. 63-106.

Uranium deposits in Nevada that were known before 1952 are 

described. Those which can be classed as sandstone-type deposits 

are included in this annotation. All known occurrences of this 

type are of low grade, and all are thought to have been deposited 

by ground waters.

Carnotite, associated with calcite and manganese oxide, forms 

fracture coatings and small veinlets in a rhyolite porphyry a few 

miles south of Sloan. Near Sutor and Goodsprings, carnotite associated with manganese oxide, calcite, and celestite forms joint and 

fracture coatings in sandstone of Permian age. Secondary uranium 

minerals occur as caliche in alluvium of Quaternary age between 

Erie and Arden. These four occurrences are in Clark County 

southwest of Las Vegas.

Discontinuous layers of uraniferous opal occur in vitric tuff and 

ash beds in the Virgin Valley opal district in northwestern Nevada. 

Carnotite occurs locally as fine coatings on parting planes and 

fractures in the opal.

170 Levering, T. G., 1955, Progress in radioactive iron oxides investigations : Econ. Geology, v. 50, no. 2, p. 186-195.

Many uranium and thorium deposits in the western United States 

are closely associated with zones of radioactive secondary iron minerals. As a result of a study of these radioactive "limonites," it 

was concluded that uranium minerals in an oxidizing sulnde environment go into solution in acid sulfate waters as uranyl sulfate in the 

presence of ferric sulfate. When these acid waters are neutralized, 

ferric sulfate hydrolyzes to form a colloidal ferric oxide hydrate 

which absorbs the uranyl ion and thus removes most of the uranium 

from solution. As the colloidal ferric oxide hydrate ages, it crystallizes to form goethite and in this process most of the uranium is 

expelled to form particles of secondary uranium minerals. Most 

thorium minerals are resistant to weathering and are still present 

in their original form in the thorian limonites (goethite).

171 Levering, T. S., Lakin, H. W., Ward, F. N., and Canney, F. C., 

1956, The use of geochemical techniques and methods in prospecting for uranium: U. S. Geol. Survey Prof. Paper 300, 

p. 659-665; Geology of uranium and thorium, United Nations, 

v. 6, p. 782-787.

The art of successfully applying the fundamental principles of 

geochemical dispersion of the elements to the practical problem 

of finding hidden ore bodies depends on establishing diagnostic 

patterns of dispersed metals near ore deposits. The techniques 

of using variations in trace amounts of metals to delineate such 

patterns or anomalies is being used in the search for uranium and 

thorium.
126 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

The anomalies most commonly investigated in geochemical prospecting are those formed at the earth's surface by agents of 

weathering, erosion, or surficial transportation. Analysis of soil 

derived from the direct weathering of rock in place gives the most 

reliable and consistent indication of ore lying just beneath the soil. 

Attention also is being given to primary anomalies found in bedrock, 

and several studies have indicated the presence of dispersion halos 

adjoining and overlying some blind ore bodies dispersions that 

are apparently related to the ore-depositing process.

Owing to the varying mobilities of different elements, some of 

these diagnostic halos, both primary and secondary, extend over 

a large area and form broad targets which are useful in general 

reconnaissance; others, which are restricted to the vicinity of the 

ore body itself, are more useful for detailed studies.

172 Lowell, J. D., 1953, Applications of cross stratification studies to

problems of uranium exploration: U. S. Atomic Energy Comm.

RME-44, issued by U. S. Atomic Energy Comm. Tech. Inf.

Service, Oak Ridge, Tenn.; 1955, Econ. Geology, v. 50, no. 2,

p. 177-185.

Uranium ore bodies in the lower part of the Morrison formation 

of Jurassic age in the Chuska Mountains area in northeastern 

Arizona are elongated in the direction of ancient stream channels. 

Intersections of ancient stream systems appear to be favorable loci 

for the deposition of uranium ore. These stream directions and 

intersections can be reconstructed and projected by mapping and 

analysis of cross stratification. Mineral-bearing solutions appear 

to have followed networks of filled channels and scours, moving 

through them along the path of greatest permeability. Where 

the velocity of the moving solutions was reduced by especially permeable rocks, uranium was deposited if a suitable geochemical environment existed.

173 Luedke, R. G., and Shoemaker, E. M., 1953, Tectonic map of the

Colorado Plateau: U. S. Geol. Survey TEM-301, open-file report.

The structure of the Colorado Plateau is characterized by broad

uplifts and basins, monoclinal folds, and salt anticlines. These

structures are locally modified by large and small faults and by

intrusive igneous rocks. Extensive areas of extrusive igneous

rocks occur near the margins of the Colorado Plateau. Each of

these features is discussed in the text. The map shows structural

contours and fault lines and indicates the areas of salt structures

and intrusive and extrusive igneous rocks.

174 McKay, E. J., 1955, Geology of the Atkinson Creek quadrangle,

Colorado: U.S. Geol. Survey Map GQ 57 (with text). 

The Atkinson Creek quadrangle is one of eighteen 7^ minute 

quadrangles in the carnotite-producing area of southwestern Colorado that are being mapped as part of a study of the carnotite deposits. Three other quadrangles (see Cater, F. W.) have been 

completed. The regional geology and the stratigraphy, structure, 

and mineral deposits of the area are described.

Rocks exposed in the eighteen quadrangles mapped consist of 

crystalline Precambrian rocks and sedimentary rocks that range
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 127

from Late Paleozoic to Quaternary. Crystalline rocks crop out 

only in the northeastern part of the area along the flanks of the 

Uncompahgre Plateau; the rest of the area is underlain by sedimentary rocks. Over most of the region the sedimentary beds are 

flat lying, but in places they are disrupted by high-angle faults or 

are folded into northwest-trending monoclines, shallow synclines, 

and strongly developed anticlines.

The uranium-vanadium deposits are mostly restricted to the upper 

layer of sandstone lenses in the Salt Wash member of the Morrison 

formation of Jurassic age. The ore consists mainly of sandstone 

impregnated with uranium- and vanadium-bearing minerals, but 

rich concentrations are also associated with thin mudstone partings, 

beds of mudstone pebbles, and carbonized fossil plant material. The 

ore bodies range from small irregular masses that contain a few 

tons of ore to large tabular masses containing many thousands of 

tons; most ore bodies are relatively small and contain only a few 

hundred tons. Margins of ore bodies may be vaguely or sharply 

denned. Layers of ore lie essentially parallel to the bedding; most 

of the deposits occur in the thicker parts of the sandstone lenses, 

and commonly near the base of the lenses. The trend of the long 

direction of the deposits and the trend of the rolls in the sandstones 

are roughly parallel to the trend of the fossil logs in the sandstone 

and to the average resultant dip of the crossbedding in the sandstone.

175 McKee, E. D., Evenson, C. G., and Grundy, W. D., 1953, Studies in 

sedimeritology of the Shinarump conglomerate of northeastern 

Arizona: U. S. Atomic Energy Comm. RME-3089, 48 p., issued 

by U. S. Atomic Energy Comm. Tech. Inf. Service, Oak Ridge, 

Tenn.

Studies of sedimentary features of the Shinarump conglomerate 

in northeastern Arizona . . . include analyses of composition, texture, 

and cross-stratification, examination of small-scale primary structures and of features of the basal contact, and the accumulation of 

data on stratigraphic relations and the controls of mineralization. 

 Authors' abstract

Much of the detrital sediment included in the Shinarump conglomerate was transported by streams from the south and southwest. 

The formation developed as a regressive sandstone, forming a 

blanket deposit across a surface of small hills, valleys, and stream 

channels. The types of deposition were rigidly controlled by water 

level.

Field relations indicate that lateral and downward moving solutions, following the paths taken by ground water today, introduced 

the mineral matter. Channels cut into the underlying Moenkopi 

formation appear to have determined the main directions of movement of the solutions; local sedimentary traps of several types 

within these channels have been responsible for ore accumulation. 

Carbonaceous matter and some varieties of clay deposits are associated with mineralization in many sedimentary traps.

176 McKelvey, V. E., 1955, Search for uranium in the United States: 

U.S. Geol. Survey Bull. 1030-A, p. 1-64.
128 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

The search for uranium in the United States is the most intensive 

ever made for any metal during our history. The largest part of 

this search has been concentrated in the Western States. No vein 

deposit of major importance by world standards has been discovered, but the search has led to the discovery of important minable 

deposits in sandstones in the Colorado Plateau, Wyoming, and South 

Dakota and in coals in South Dakota; of large low-grade deposits 

of uranium in phosphates in both western and Florida fields, in 

black shales in Tennessee, and in coals in the Dakotas, Wyoming, 

Idaho, and New Mexico; and of some promising occurrences of 

uranium in vein deposits.

The Colorado Plateau deposits contain carnotite and other oxidized minerals near the surface, but pitchblende and other dark 

uranium and vanadium minerals occur below the zone of oxidation. 

These minerals, along with hydromica, pyrite, and other sulfides, 

fill pore spaces in tuffaceous, arkosic, and quartzose sandstones 

and conglomerates and also replace clay galls, logs, and other wood 

fragments. Some of the deposits contain uraniferous asphaltic 

pellets and lenses. The ore deposits are tabular masses, generally 

elongated in the direction of the long axes of the sandstone or conglomerate lenses in which they occur. Near the ore, associated 

mudstone lenses are generally green or gray instead of the red 

generally found. Ore has been produced from about 20 formations 

on the Plateau, but the principle sources have been the Shinarump 

and Chinle formations of Triassic age, and the Entrada, Todilto, 

and Morrison formations of Jurassic age.

The report includes an extensive bibliography of uranium and a 

number of small maps of the United States showing the distribution 

of the different types of uranium deposits.

177 McKelvey, V. E., Everhart, D. L., and Garrels, R. M., 1956, Summary 

of hypotheses of genesis of uranium deposits: U. S. Geol. Survey 

Prof. Paper 300, p. 41-53; Geology of uranium and thorium, 

United Nations, v. 6, p. 551-561.

The origin and distribution of uranium in several geologic environments are discussed. The uranium deposits in sandstones on 

the Colorado Plateau are probably epigenetic. Certain studies 

have shown that the uranium probably came from a source deep in 

the earth, but it is possible that the uranium was derived from 

volcanic ash or other dispersed sources within the sedimentary pile 

and transported to the site of deposition by circulating waters or 

petroleum. Whatever the source, the path the ore solutions followed 

in the sandstones was determined mainly by sedimentary structures. 

The precipitation of uranium is probably caused by reduction due, 

perhaps, to decaying organic matter.

178 McKnight, E. T., 1940, Geology of area between Green and Colorado 

Rivers, Grand and San Juan Counties, Utah: U. S. Geol. 

Survey Bull. 908, 147 p.

Exposed sedimentary formations in this area range in age from 

Pennsylvania to Late Cretaceous. Most of the Permian, Triassic, 

and Jurassic formations are of continental origin; the Pennsylvanian 

and Upper Cretaceous formations are mostly marine. The dominant
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 129

structure of the area is a gentle regional dip to the north. Superposed on the regional dip are several folds, some of which may be 

due to the intrusion of salt. The report includes a geologic map 

and structural geologic map of the area, both at the scale of 

1:62,500.

179 Masters, J. A., 1951, Uranium deposits on southwest rim of Lukachukai Mountains, northeast Arizona: U. S. Atomic Energy 

Comm. RM0-911, 10 p., issued by U. S. Atomic Energy Comm. 

Tech. Inf. Service, Oak Ridge, Tenn.

Vanadium-uranium deposits on the southwest rim of the Lukachukai Mountains are in the Salt Wash member of the Morrison 

formation of Jurassic age. The Salt Wash member is composed 

of red and gray fine-grained quartzose sandstones interbedded with 

red and gray shales and siltstones. Carnotite and vanoxite are 

associated with carbonaceous material and impregnate crossbedded 

channel sandstone from 45 to 100 feet above the base of the Salt 

Wash sandstone. The host rock is light to dark gray; the rocks 

in other units are commonly red. However, not all gray sandstone 

is mineralized. The deposits extend from Dry Bone Mesa to Camp 

Mesa on the opposite side of the Lukachukai Mountains from the 

mineralized belt on the northeast rim.

180 Masters, J. A., 1953, Geology of the uranium deposits of the Lukachukai Mountains area, northeastern Arizona: U. S. Atomic 

Energy Comm. RME-27, 23 p., issued by U. S. Atomic Energy 

Comm. Tech. Inf. Service, Oak Ridge, Tenn.; 1955, Econ. 

Geology, v. 50, no. 2, p. 111-126.

A concentration of vanadium-uranium ore bodies occurs in finegrained to very fine grained sandstone of the Salt Wash member 

of the Morrison formation of Jurassic age in a north-south belt 

across the Lukachukai Mountains. The belt extends from Mesa I 

to Mesa V on the north side, and from Two Prong Mesa to Step 

Mesa on the south side of the mountains. The ore belt conforms 

to a lenticular sandstone and mudstone facies and is bounded 

on the west by a massive sandstone facies and on the east by a 

mudstone facies containing some sandstone.

Changes in permeability influenced the movement of mineralbearing solutions by causing their diversion, damming, and concentration. Permeability is greatest near ancient stream channels. 

The ore bodies, which lie in and are elongated parallel to these 

channels, tend to occur in clusters along the flanks. The presence 

of carbonaceous material and possibly of mudstone caused precipitation of uranium from solution. Ore most commonly occurs in 

gray and limonitic-brown sandstone; and, in the vicinity of ore, 

the associated mudstone is usually gray. The favorable color zones 

follow the ancient stream channels. The ore solutions presumably 

bleached the rocks from red to gray or brown. The ore bodies in 

the Lukachukai Mountains are generally smaller than, but otherwise similar to, those of the Uravan mineral belt. Carnotite and 

vanoxite impregnate sandstone and "trash piles," and replace fossil 

logs. Some ore bodies are rolls. The ore bodies in the Lukachukai 

Mountains and in the Uravan mineral belt are associated with 

bleached sandstone and mudstone.
130 SELECTED BIBLIOGEAPHIES OF URANIUM GEOLOGY

The Lukachukai Mountains lie on the east flank of the Defiance 

uplift, and the rocks dip 1° - 2° NE. The Lukachukai anticline, 

a northwest-plunging sharply asymmetric flexure, reverses this dip 

by 10 to 30°. The axis of the attendant syncline lies along the northeast edge of the Lukachukai Mountains.

181 Merritt, P. L., 1950, Uranium exploration in the United States: 

Rocks and Minerals, v. 25, no. 7-8, p. 363-370; Canadian Min. 

and Met. Bull., v. 43, no. 460, p. 438-443; Mines Mag., v. 40, 

no. 6, p. 36, 51-52.

The exploration program of the U. S. Atomic Energy Commission 

and the methods used by the Commission to stimulate private exploration are outlined. Generalized geologic descriptions are given 

of the types of environments in which uranium has been found 

in the United States. The uranium deposits on the Colorado Plateau 

are mostly in continental sandstone formations of Triassic and 

Jurassic age. The most important producing formation is the 

Salt Wash member of the Morrison formation of Jurassic age. 

The deposits are roughly tabular, irregular in outline, and in general 

conform to the bedding, although in detail they may cross, the bedding. The most important mineral is carnotite; it is usually associated with fossil organic material. Also described are pitchblende 

deposits in the Colorado Front Range; in the Coeur d'Alene district 

in Idaho; at Marysvale, Utah; in upper Michigan; and uraniferous 

phosphorite and black shale deposits in the United States.

182 Miller, L. J., 1952, Drilling in the Happy Jack mine area, White 

Canyon, San Juan County, Utah: U. S. Atomic Energy Comm. 

RME-4039, 14 p., issued by U. S. Atomic Energy Comm. Tech. 

Inf. Service, Oak Ridge, Tenn.

Diamond drilling in the Happy Jack mine area was done to locate 

copper-uranium deposits in the Shinarump conglomerate of Triassic 

age and to outline channels cut into the underlying Moenkopi formation of Triassic age. Eleven of the 26 holes penetrated ore, 

and the Sunrise, Gonaway, and Happy Jack channels were outlined. 

The ore occurs in the Shinarump conglomerate at or near the base 

of the channels and is characteristically in porous coarse-grained 

sandstone which rests on dense mudstone. The principal uranium 

mineral, pitchblende, is associated with carbonaceous material and 

in places replaces woody material. The host rock is erratically 

cemented with gypsum, calcite, and silica.

183 Miller, L. J., 1953, Ore textures of uraninite and associated minerals from the Colorado Plateau uranium deposits [abs.]: Geol. 

Soc. America Bull., v. 64, no. 12, p. 1453-1454.

Uraninite in the ore deposits of the Colorado Plateau is present 

as a replacement mineral. It replaces the clay cement of the quartz 

grains, the quartz overgrowths, asphaltite, organic matter, and in 

some cases sulfide minerals. The exsolution texture of chalcopyrite 

and bornite indicates deposition at a high temperature. A comparison of the large amount of alteration at the Marysvale (Utah) 

uranium deposit and the low amount of alteration of the Plateau 

deposits suggests a low-temperature deposition for the Plateau 

deposits. Authors abstract \
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 131

184 Miller, L. J., 1953, Uranium ore controls of the Happy Jack deposit, 

White Canyon, San Juan County, Utah: U.S. Atomic Energy 

Comm. RME-33, 34 p., issued by U. S. Atomic Energy Comm. 

Tech. Inf. Service, Oak Ridge, Tenn.; 1955, Econ. Geology, 

v. 50, no. 2, p. 156-169.

Miller, L. J., 1952, Uranium ore controls in the Happy Jack mine 

and vicinity, White Canyon, Utah [abs.]: Econ. Geology, v. 47, 

no. 7, p. 774; Geol. Soc. America Bull, v. 63, no. 12, p. 1280.

The copper-uranium deposit at the Happy Jack mine is in an 

ancient stream channel which contains sediments of the Shinarump 

conglomerate of Triassic age. The host rock is a coarse-grained 

to conglomeratic quartzose sandstone which contains abundant 

carbonaceous material. This unit is present only in the channels; 

it is overlain by an intrachannel mudstone unit of the Shinarump 

and is underlain mainly by dense mudstones of the Moenkopi formation of Triassic age. The ore is associated with organic material 

and sedimentary structures and is generally in deep areas within 

the channel. Lithologic controls include bedding planes, petrologic 

traps, scours within the Shinarump, and basal Shinarump mudstone. Uraninite and copper sulfides impregnate the sandstone and 

replace carbonaceous material and secondary overgrowths on quartz 

grains. The ore minerals are nearly contemporaneous. Secondary 

uranium and copper minerals are minor. The normally red sediments near the ore deposit have been bleached to green, but there 

is no other evidence of alteration within the deposit.

Channels within the Shinarump formation of Triassic age are 

thought to be the principal uranium ore control in White Canyon, southeastern Utah. Intrachannel controls include carbonaceous matter, lithologic changes, and bedding planes.

185 Miller, R. D., 1954, Reconnaissance for uranium in the Hualapai 

Indian Reservation area, Mohave and Coconino Counties, Ariz.: 

U. S. Atomic Energy Comm. RME-2007, 18 p., issued by U. S. 

Atomic Energy Comm. Tech. Inf. Service, Oak Ridge, Tenn. 

The only known occurrence of uranium in the Hualapai Indian 

Reservation is at the Ridenour mine. The workings are in bleached 

fine-grained sandstone members of the normally red Supai formation of Permian age. Copper minerals occur in a vein and breccia 

zone with pyrite and limonite. Vein quartz is absent, and uranium 

and vanadium are minor. Consolidated sedimentary rocks in the 

area range in age from Cambrian to Permian. Precambrian crystalline rocks are exposed in the deeper canyons. Large faults are 

prominent. The sedimentary rocks are either horizontal or gently 

dipping. The Supai formation and the Hermit shale, both of Permian age, appear to be the most favorable host rocks in the area 

for uranium deposits localized by stratigraphic control.

186 Mirsky, Arthur, 1953, Preliminary report on uranium mineralization in the Dakota sandstone, Zuni uplift, New Mexico: U. S. 

Atomic Energy Comm. RME-47, 21 p., issued by U. S. Atomic 

Energy Comm. Tech. Inf. Service, Oak Ridge, Tenn. 

Uranium deposits occur in sandstone and carbonaceous shale 

of the Dakota sandstone of Cretaceous age along the north and
132 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

northeast flank of the Zuni uplift. The Dakota sandstone regionally 

truncates older rocks. The sandstone units are buff to gray, fineto medium-grained, crossbedded, plane-bedded or massive, and are 

interbedded with blue or gray mudstone and carbonaceous shale. 

Most beds are lenticular; the formation is about 50 feet thick. 

The uranium mineral metatyuyamunite(?) is closely associated with 

carbonaceous material and iron oxides. The deposits are in or 

marginal to ancient stream channels. Joints may partially control 

the location of the deposits. Except for one deposit in carbonaceous 

shale, all are in sandstone.

187 Mitcham, T. W., and Evenson, C. G., 1955, Uranium ore guides, 

Monument Valley district, Arizona: Econ. Geology, v. 50, no. 2, 

p. 170-176.

The contact between the Shinarump conglomerate and the Moenkopi formation, both of Triassic age, is a marked erosional unconformity. Basal Shinarump sediments fill ancient stream channels 

incised into the underlying Moenkopi. *** Uranium ore deposits 

are commonly found in these stream channels. Paleostream channels are the prime guide to ore in the Shinarump. Twenty-seven 

others of varying degrees of usefulness are summarized. Authors' 

abstract

188 Moore, G. W., and Levish, Murray, 1055, Uranium-bearing sandstone in the White River Badlands, Pennington County, S. Dak.: 

U. S. Geol. Survey Circ. 359, 7 p.

Uranocircite is locally disseminated in the lower 2 feet of a channel sandstone in the Chadron formation of Oligocene age in the 

White River Badlands. The sandstone is yellowish gray and coarsegrained; it is directly underlain by an impermeable bed of bentonitic claystone.

Metatyuyamunite(?) was found at one place in a bed of freshwater limestone in the Chadron formation. At several places carnotite forms very thin coatings on the outer surfaces of chalcedony 

veins in the overlying Brule formation of Oligocene age.

The uranium was probably leached from the overlying volcanic 

ash beds by descending meteoric waters and carried by these waters 

to an environment favorable for deposition.

189 Moore, R. B., and Kithil, K. L., 1913, A preliminary report on 

uranium, radium, and vanadium: U. S. Bur. Mines Bull. 70, 

101 p.

Topics discussed in this report are the carnotite deposits of Colorado and Utah, the pitchblende deposits of the world, the vanadium 

deposits in the United States and Peru, methods of analysis of ore, 

methods of ore treatment, and uses of the metals. Carnotite deposits in the Green River and Thompsons districts in Utah, and at 

Skull Creek, Coal Creek, and in the Paradox Valley region of Colorado are described. The deposits are commonly associated with 

carbonaceous material in sandstone beds. Some vanadium minerals 

may be present. The deposits in the Paradox Valley region are in a 

light-colored sandstone of the McElmo formation (Morrison formation) of Jurassic age. The most typical ore is sandstone impreg-
BIBLIOGBAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 133

nated with carnotite and which contains small brown masses of 

vanadium-rich sandy clay. The deposits are invariably in pockets 

and are associated with gypsum, carbonaceous material, and red, 

brown, blue, and black vanadium minerals. Some of the mine 

workings are described as they appeared in 1912.

The authors suggest that the uranium was disseminated in the 

sandstone country rock and has been concentrated in ore bodies 

by the action of water.

190 Muilenburg, G. A., 1949, Notes on uranium: Mo. Div. Geol. Survey

and Water Res. Inf. Circ. 5, 18 p.

This circular briefly describes uranium minerals and methods of 

identifying them, different types of uranium deposits, and uranium occurrences in Missouri. Only specimen quantities of uranium 

minerals have been found in Missouri. Meta-torbernite has been 

found in a fire-clay in Franklin County, and carnotite has been 

found on a joint surface in limestone at a quarry near Ste. Genevieve. 

Several other localities are known.

191 Muilenburg, G. A., and Keller, W. D., 1950, Carnotite and radioactive

shale in Missouri: Am. Mineralogist, v. 35, no. 3-4, p. 323-324.

Carnotite and possibly other radioactive minerals have been found

in a quarry in the Spergen limestone of Mississippian age about

5 miles north of Ste. Genevieve, Ste. Genevieve County, Mo. The

carnotite forms a thin film along a joint in the limestone. A thin

parting of highly radio'active black shale overlies the occurrence; the

carnotite is thought to have been derived from this shale parting.

192 Mullens, T. E., and Freeman, V. L., 1952, Lithofacies study of the 

Salt Wash sandstone member of the Morrison formation [abs.]: 

Geol. Soc. America Bull., v. 63, no. 12, p. 1340.

The Salt Wash sandstone, the lower member of the Upper Jurassic 

Morrison formation in a large part of the Colorado Plateau, is the 

product of an aggrading fluvial system and consists of lenticular 

beds of light-colored cross-laminated sandstone and conglomeratic 

sandstone irregularly interbedded with mudstone, claystone, and 

horizontally laminated sandstone.

The fluvial deposits are divided into stream and flood-plain deposits: the stream deposits include all sediments interpreted as 

deposited from moving water; the flood-plain deposits include all 

deposits interpreted as deposited from slack water.

The lithof acies of the Salt Wash member is the total aspect of the 

thickness, relative proportions, and continuity of the two types of 

deposits. Areal variations in the Salt Wash lithofacies are shown 

by isopach and isolith maps.

Interpretations of the areal variations in Salt Wash lithofacies 

indicate piedmont-type deposition by a distributary drainage system 

from one principal source area. The distributary drainage radiated 

outward from south-central Utah and spread sediments to the north 

and east in a fan-shaped pattern. The total thickness of the deposits 

and relative proportion of stream deposits decrease rather uniformly 

away from the apex of the fan. In the Four-Corners area, where 

the Salt Wash member interfingers with the Bluff sandstone member 

of the Morrison, the development of the fan shape was interrupted as
134 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

the distributary streams encroached on the sand dunes of the Bluff 

sandstone member. Author's abstract

193 Nininger, R. D., 1954, Minerals for atomic energy: New York, D. Van

Nostrand Company, Inc., 367 p.

This book, written by the Deputy Assistant Director for Exploration of the Atomic Energy Commission, is a guide to exploration for uranium, thorium, and beryllium minerals. Part 1 describes 

the minerals and mineral deposits that are the sources and potential 

sources of these metals. Representative uranium deposits on the 

Colorado Plateau and in other areas are reviewed. Part 2 is a discussion of possibilities for new deposits in various areas of the world, 

and particularly in the United States. Part 3 covers prospecting 

equipment and techniques, the use of the Geiger and scintillation 

counters, evaluation of deposits, and details of prices, markets, 

and governmental controls. Appendixes include mineral identification tables, classifications of ore deposits, testing and analysis procedures, and other pertinent information.

194 Notestein, F. B., 1918, Some chemical experiments bearing on the 

origin of certain uranium-vanadium ores: Econ. Geology, v. 13, 

no. 1, p. 50-64.

The carnotite deposits of the Colorado Plateau occur as small 

lenticular bodies of mineralized light-colored sandstone within hard 

ledge-forming crossbedded sandstones of the McElmo formation 

(Morrison formation) of Jurassic age. The deposits generally 

conform to the bedding. Nearly all of the ore-bearing beds are rich 

in fossil carbonaceous material, and most also contain calcite and 

gypsum.

The three hypotheses of origin that have been advocated are summarized as follows:

1. Widely disseminated uranium and vanadium minerals have been 

dissolved from overlying rocks and transported by ground water; 

the metals were reprecipitated at the position where now found 

through some agency such as calcite or organic material or through 

oxidation near outcrops. Recency is implied. (Hillebrand and Ransome, 1905, see ref. 135).

2. The minerals carry vanadium and uranium were concentrated 

by ordinary processes of sedimentation at or near the present position, 

and the carnotite is an oxidation product of such minerals. (Fleck 

and Haldane, 1907, see ref. 89; Wherry, 1915, see ref. 276).

3. The uranium and vanadium were precipitated from sea water 

by the reducing action of decaying vegetable matter; carnotite is an 

oxidation product, nearly in place, of such precipitated salts. (Hess, 

1914, see ref. 129).

The author ascertained through laboratory experiments that carnotite is readily soluble in sulfate ground water, and that calcite will 

precipitate uranium and vanadium from sulfate solution. This precipitate is soluble in calcium bicarbonate solution but will be reprecipitated by loss of carbon dioxide.

The author suggests that descending sulfate waters took the 

disseminated uranium and vanadium minerals into solution. The 

metals precipitated when a calcitic bed was reached, and gypsum
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 135

and carbon dioxide formed. The carbon dioxide reached with calcite 

to form calcium bicarbonate which redissolved the uranium and part 

of the vanadium; the dissolved salts were then transported to an 

outcrop or some other suitable place where the loss of carbon dioxide 

caused reprecipitation of the metals.

195 Page, L. R., 1950, Interim report of geologic investigation, Lost Creek 

schroeckingerite deposits, Sweetwater County, Wyo.; U. S. Geol. 

Survey TEM-183A, 3 p., issued by U. S. Atomic Energy Comm. 

Tech. Inf. Service, Oak Ridge, Tenn.

Schroeckingerite occurs principally as rounded aggregates as much 

as 1 inch in diameter in green, brown, or purple clay, and also as 

tiny flakes disseminated in sand or sandy clay. The clays are early 

Eocene or younger in age and are interbedded with arkosic sands 

and grits. These beds are overlain by Pleistocene and Recent sands 

and gravels which conceal the ore-bearing material. The ore beds 

are relatively continuous along the strike, but the nature of schroeckingerite (an efflorescent mineral) indicates that the deposit does 

not extend to any great depth. The schroeckingerite deposits appear 

to be associated with the Cyclone Rim fault which is believed to have 

been the channel for the uranium-bearing solutions. Suggestions for 

prospecting are included.

196 Page, L. R., 1956, Geologic prospecting for uranium and thorium: 

U. S. Geol. Survey Prof. Paper 300, p. 627-631; Geology of 

uranium and thorium, United Nations, v. 6, p. 688-691. 

The search for uranium and thorium in the United States has emphasized the value of geologic guides in prospecting. The application 

of the guides discussed in this report in conjunction with radiometric, 

geochemical, botanical, panning, and geophysical techniques has 

greatly increased the rate of discovery. Prospecting for new districts 

is based on very general criteria; prospecting for individual ore 

deposits in new or old districts requires specific guides. Geologic 

guides to ore deposits vary for each of the principal uranium and 

thorium districts.

197 Page, L. R., and Redden, J. A., 1952, The carnotite prospects of the 

Craven Canyon area, Fall River County, S. Dak.: U. S. Geol. 

Survey Circ. 175, 18 p.

Carnotite deposits occur in the Lakota sandstone of Early Cretaceous age in Craven Canyon, Fall River County, S. Dak. The area 

lies on the southwest flank of the Black Hills uplift and the rocks dip 

gently to the southwest. The Lakota sandstone is a white to buff 

massive to thin-bedded sandstone containing many thin white to 

purplish-red shale beds. Throughout the area studied a dense black 

bed of carbonaceous shale from 1 to 3 feet thick is exposed and used 

as a marker bed. The carnotite occurs as impregnations of sandstone and as joint coatings and fillings; it is commonly associated 

with iron oxides and fossil carbonaceous material. The deposits are 

generally parallel to the bedding, but in detail they may cut across 

the bedding. Because there are few exposures little is known about 

the outline of the deposits, but they are probably tabular and quite 

small. The average thickness is about 2 feet. Eleven prospects are 

described, and suggestions for prospecting are included.
 136 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

198 Phair, George, and Levine, Henry, 1952, Notes on the differential 

- leaching of uranium, radium, and lead from pitchblende in 

H2S04 solutions: U. S. Geol. Survey TEI-262, 23 p., issued by 

U. S. Atomic Energy Comm. Tech. Inf. Service, Oak Ridge, 

Tenn.; 1953, Econ. Geology, v. 48, no. 5, p. 358-369. 

It has been noted that the radium: uranium ratios in weathered 

;,,. pyritic pitchblende ores are abnormally high. The complex solutions 

involved in the leaching of pitchblende in pyritic mines and dumps are 

characterized by a relatively high concentration of sulfuric acid. Laboratory experiments show that in an oxidizing and highly acid 

environment uranium is rapidly leached, and radium and lead tend 

to be residually concentrated. Further, UOs is preferentially leached 

with respect to UC>2.

199 Phoenix, D. A., 1956, Relation of carnotite deposits to permeable 

rocks in the Morrison formation, Mesa County, Colo.: U. S. Geol. 

Survey Prof. Paper 300, p. 213-219; Geology of uranium and 

thorium, United Nations, v. 6, p. 321-325.

The uppermost, almost continuous, sandstone layer in the Salt 

Wash member of the Morrison formation of Jurassic age contains 

most of the carnotite deposits in southwestern Colorado and southeastern Utah. It is composed of broadly lenticular strata of sandstone separated by fine-grained laminated sediments collectively 

called mudstone. Carnotite deposits are localized where the sandstone 

strata thicken and rest one upon another; they are not found where 

the sandstone strata are thin and the layer is mostly mudstone.

The permeability of sediments in the uppermost layer is influenced 

by the character of the original sediment and by the later effects of 

diagenesis. Laminated mudstone and siltstone are least permeable 

and bedded sandstone is most permeable except in places where the 

original porosity has been reduced by the interstitial clay, quartz 

overgrowths, and calcite and iron oxide cement. The sedimentary 

rocks are less permeable across bedding than parallel to bedding.

The coefficient of transmissivity, which is equal to the product of 

the thickness and mean permeability, was determined for samples 

from drill holes in Mesa County, Colo. Maps showing transmissivity 

indicate that carnotite deposits are localized where the rocks in the 

uppermost layer are most transmissive; they are uncommon where 

rocks in the uppermost layer are least transmissive.

200 Poehlmann, E. J., and King, E. N., 1953, Report on wagon drilling for

uranium in the Silver Reef (Harrisburg) district, Washington

County, Utah: U. S. Atomic Energy Comm. RME-2004, 24 p.,

issued by U. S. Atomic Energy Comm. Tech. Inf. Service, Oak

' Ridge, Tenn.

An exploratory wagon-drilling program revealed two new uranium 

ore bodies in the Silver Reef district. The uranium deposits in the 

Silver Reef district are near the faulted north-plunging nose of the 

Virgin anticline. Silver, uranium, vanadium, and copper minerals 

occur in 5 carbonaceous, sandy shale zones of the Leeds and Tecumseh members of the Chinle formation of Triassic age. The most 

important uraniferous zone is a carbonaceous crossbedded sandy shale 

which lies in the upper part of the Leeds sandstone. Mineralization
BIBLIOGRAPHY OF SANDSTONE-TYPE UBANITJM DEPOSITS 137

has favored areas where relatively close-spaced normal faults of very 

small displacement cut the favorable beds.

201 Poole, F. G., and Williams, G. A., 1956, Direction of transportation 

of the sediment constituting the Triassic and associated formations of the Colorado Plateau: Geology of uranium and thorium, 

United Nations, v. 6, p. 326-330; see also, Direction of sediment 

transport in the Triassic and associated formations of the Colorado Plateau: U. S. Geol. Survey Prof. Paper 300, p. 227-231. 

Clastic sediments develop characteristic features in certain depositional environments and these features reflect the direction in which 

the transporting medium was moving. These characteristic features 

are called sedimentary, primary, or original structures. Sedimentary structures that possess directional characteristics include channels, cross-strata, current lineation, and ripple marks. From these 

primary structures the direction of transportation can be determined 

and the direction of source can be inferred.

Studies of sedimentary structures have been made of rocks of the 

Colorado Plateau that range in age from Permian to Jurassic, and 

directions of sediment transportation of several formations have 

been determined. This information is useful in the exploration for 

uranium and vanadium deposits because the ore bodies, which are 

localized in channel-filling sandstones, generally are elongate in the 

direction of transportation of the sediments.

202 Proctor, P. D., 1953, Geology of the Silver Reef (Harrisburg) mining 

district, Washington County, Utah: Utah Geol. and Mineralog. 

Survey Bull. 44, 169 p.

The Silver Reef mining area in southwestern Utah contains the 

only known occurrence in the United States of commercial bodies of 

silver ore in sandstone. Minor amounts of copper, uranium, and 

vanadium minerals also are present in the ore. The ore bodies are 

restricted to the Silver Reef sandstone member of the Chinle formation of Triassic age, and they occur on the limbs and nose of the 

northeast-trending and plunging Virgin anticline and a subsidiary 

anticline and syncline. A north-trending normal fault and a thrust 

fault with a minimum eastward displacement of 1,500 feet repeat 

the ore horizon three times. No constant relation exists between 

mineralized ground and the folds or faults.

The deposits are associated with carbonaceous material in lenses 

of light-colored quartzose sandstone and may be localized in channels 

in the Silver Reef sandstone.

The author concludes that the metals in the Silver Reef deposits 

were derived from volcanic tuffs by ground or surface waters and 

precipitated in proximity to carbonaceous material in the Silver 

Reef sandstone. The silver was further concentrated by enrichment.

203 Proctor, P. D., Hyatt, E. P., and Bullock, K. C., 1954, Uranium: 

where it is and how to find it: Salt Lake City, Eagle Rock Publishers, 85 p.

This publication is a nontechnical guide to prospecting for uranium. 

Included is information on uranium minerals and deposits, areas of 

known deposits, equipment, and other topics of interest to a uranium 

prospector.
138 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

204 Rankama, Kalervo, and Sahama, T. G., 1950, Geochemistry: Chicago, 

Univ. Chicago Press, 912 p., see p. 632-639.

The geochemistry of uranium is discussed. Uranium is a member of 

the actinide series of rare-earth elements, has a large ionic radius, 

and is radioactive. The most important uranium mineral is the oxide, 

UC>2, found as uraninite and pitchblende. Other uranium minerals 

include hydroxides, phosphates, arsenates, vanadates, uranates, carbonates, silicates, and sulfates; these minerals are usually derived 

from the alteration or decomposition of uraninite and pitchblende. 

Uranium never occurs in the natural state and never forms sulfides, 

arsenides, or tellurides.

Uranium does not enter the crystal lattices of the rock-forming 

minerals during the crystallization of a magma because its ionic 

radius is too large; it is therefore enriched in residual solutions. It 

may crystallize in pegmatites or it may enter pneumatolytic and 

hydrothermal veins. Uranium is also concentrated, notably in the 

presence of vanadium, in minerals precipitated from ground waters; 

such uranium deposits are sometimes found in sandstones.

The cycle of uranium and the biogeochemistry of uranium are 

also discussed. Uranium is absorbed by biological substances. Some 

petroleum and associated brines contain uranium, and marine carbonaceous shales have a definitely higher uranium content than most 

other sedimentary rocks. Some coals also have a high uranium 

content.

The largest and most important uranium deposits are near Great 

Bear Lake in Canada, at Katanga in the Belgian Congo in West 

Africa, and in Czechoslovakia. They are all associated with hydrothermal veins. Important deposits also occur in continental sandstones in the western United States.

205 Rapaport, Irving, 1952, Interim report on the ore deposits of the 

Grants district, New Mexico: U. S. Atomic Energy Comm. RMO1031, 19 p., issued by U. S. Atomic Energy Comm. Tech. Inf. 

Service, Oak Ridge, Tenn.

Uranium deposits in the Grants district occur in the Todilto limestone and in the Morrison formation, both of Jurassic age. The deposits are on the northeast flank of the Zuni uplift and on the Lucero 

uplift. Unexposed deposits may exist in the intervening McCarty 

syncline. Exposed rocks range from Precambrian to Tertiary in age. 

The deposits in the Todilto limestone are in the upper coarse, 

crenulated, recrystallized part of the formation. Pitchblende is 

associated with calcite, pyrite, barite, and fluorite. Uranium vanadates, uranium silicates, and hematite are found in the oxidized parts 

of the deposits. Some of the deposits are associated with minor semicylindrical bulges or anticlines that have no intervening synelines. 

The deposits seem to be in a zone between the silty limestone facies 

to the south and the gypsiferous limestone facies to the north. Joints 

and faults also may have had an influence on the movement and emplacement of ore.

The uranium minerals in the Morrison deposits, mainly carnotite 

with some schroeckingerite, are associated with carbonaceous material and limonite. Carnotite impregnates sandstone, coats fractures, 

and replaces fossil logs. Ancient stream channels, diastems, intricate
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 139

facies changes, and the presence of organic material seem to localize the ore.

The uranium, iron, sulfur, barium, and flourine probably were 

transported in solution in hydrothermal waters to the place of deposition. The ore-bearing solutions moved laterally and undoubtedly 

were mixed with ground water.

206 Kapaport, Irving, Hadfield, J. P., and Olson, R. H., 1952, Jurassic 

rocks of the Zuni uplift, New Mexico: U. S. Atomic Energy 

Comm. RMO-642, 45 p., issued by U. S. Atomic Energy Comm. 

Tech. Inf. Service, Oak Ridge, Tenn.

The Zuni uplift is an asymmetrical elliptical dome in the southeastern corner of the San Juan Basin. It is about 65 miles long by 

40 miles wide and is elongated in a northwesterly direction. Precambrian crystalline and metamorphic rocks are exposed in the 

central part of the uplift. About 1,000 feet of Paleozoic and more 

than 3,000 feet of Mesozoic sedimentary rocks overlie the Precambrian rocks. Tertiary and Quaternary lava flows cover areas of 

moderate size.

Jurassic sedimentary rocks of this region, in ascending order, are 

the Glen Canyon group, the San Rafael group, and the Morrison 

formation. The Wingate formation is the only member of the Glen 

Canyon group. The San Rafael group consists of, in ascending order, 

the Carmel, the Entrada, the Todilto, the Summerville, and the Bluff 

formations. The Morrison formation is divided into the Recapture 

Creek, the Westwater Canyon, and the Brushy Basin members. Rock 

types include shale, siltstone, sandstone, and limestone. All Jurassic 

formations, except perhaps the Carmel, are of continental origin.

The regional stress responsible for the Zuni dome appears to have 

been mainly one of vertical uplift that occurred probably in early 

or middle Tertiary time. Structural relief is more than 6,600 feet. 

The joints and faults seem to be tensional and normal to the direction 

of most bending and to the bedding.

207 Rasor, C. A., 1952, Uraninite from Gray Dawn mine, San Juan

County, Utah: Science, v. 116, no. 3004, p. 89-90. 

Massive chunks of primary uraninite have been found intimately 

associated with carnotite-bearing ores from the Grey Dawn mine 

which is on a small tributary of La Sal Creek near the southeast 

flank of the La Sal Mountains, San Juan County, Utah. The host 

rock is a gently dipping sandstone bed in the Salt Wash member of 

the Morrison formation of Jurassic age. This is the first discovery of 

uraninite in the Salt Wash sandstone. The deposit is otherwise similar to other carnotite deposits in the Salt Wash sandstone. This occurrence of uraninite may make it necessary to modify the present 

concept of the origin of these ores.

208 Redmond, R. L., and Kellogg, J. P., 1954, Drilling at Polar Mesa,

Grand County, Utah, and review of favorability criteria used:

U. S. Atomic Energy Comm. RME-22 (pt. 1), 30 p., issued by

U. S. Atomic Energy Comm. Tech. Inf. Service, Oak Ridge, Tenn.

Vanadium-uranium deposits on Polar Mesa occur in a sandstone

unit of the Salt Wash member of the Morrison formation of Jurassic

age. This unit, called the "payoff sand," is a massive crossbedded
140 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

medium- to fine-grained yellow-brown sandstone that ranges from 10 

to 70 feet in thickness. The base of the ore-bearing zone is about 

270 feet above the contact of the Entrada and Summerville. Carnotite and roscoelite are associated with fossil trees and carbonaceous 

trash. The ore bodies are generally tabular, of irregular shape, and 

contain as much as 10,000 tons.

A drilling program was conducted near the northeast rim of the 

mesa. The "payoff sand" was correlated between holes on the basis of 

regional dip. A f avorability map of this area was constructed to guide 

further drilling. Factors considered favorable for uranium ore are 

the presence of either equal amounts of sandstone and mudstone or 

more sandstone than mudstone; of more yellow-brown than grey 

sandstone; and of blue-green mudstone.

209 Reinhardt, E. V., 1951, Reconnaissance of Henry Mountains area, 

Wayne and Garfield Counties, Utah: U. S. Atomic Energy Comm. 

RMO-753, 7 p., issued by U. S. Atomic Energy Comm. Tech. Inf. 

Service, Oak Ridge, Tenn.

Uranium ore deposits occur in sandstone of the Salt Wash member 

of the Morrison formation of Jurassic age in a strip about 3 miles 

wide along the east flank of the Henry Mountains. Tertiary laccolithic intrusive rocks in a structural basin form the core of the Henry 

Mountains. The uranium deposits are found from north to south, in 

the North Wash, the Trachyte, and the Little Rockies districts. The 

deposits are of good grade and apparently extensive, but many are 

thin. Development and production have been limited mostly by the 

cost of transportation to distant shipping points and buying stations.

210 Reinhardt, E. V., 1952, Practical guides to uranium ores on the 

Colorado Plateau: U. S. Atomic Energy Comm. RMO-1027, 13 p., 

issued by U. S. Atomic Energy Comm. Tech. Inf. Service, Oak 

Ridge, Tenn.

This report presents and discusses a list of guides to uranium ore. 

Items 1 through 4 are syngenetie features, and items 5 through 11 

are epigenetic. The order of listing does not reflect importance.

1. Presence of ancient stream channels.

2. Thickening of sandstone lenses.

3. Interfingering of mudstone and sandstone lenses.

4. Presence of carbonaceous material.

5. Proximity of ore.

6. Relation to mountain masses and large folds.

7. Bleaching of sandstone.

8. Bleaching of mudstone adjacent to sandstone lenses.

9. Presence of yellow iron-oxide stains.

10. Presence of bleached mudstone pebbles in the sandstone 

lenses.

11. Etched and corroded sand grains.

211 Reinhardt, E. V., 1952, Uranium-copper deposits near Copper Canyon, 

Navajo Indian Reservation, Ariz.: U. S. Atomic Energy Comm. 

RMO-902, 13 p., issued by U. S. Atomic Energy Comm. Tech. 

Inf. Service, Oak Ridge, Tenn.

Copper-uranium deposits in the Copper Canyon area of the Monument Valley district in Utah and Arizona occur in the Shinarump
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 141

conglomerate of Triassic age near the base of channels cut into the 

underlying Moenkopi formation of Triassic age. The deposits, which 

are relatively small, are all less than 20 feet above the base of the 

channels and the best concentrations are in the lower 5 feet. The 

ore contains as much as 0.68 percent UaOg. Carnotite, the principal 

uranium mineral, impregnates sandstone and replaces fossil carbonaceous material. The copper minerals occur similarly but also 

are found higher in the section. There is no constant ratio between the 

copper and uranium content of the deposits. Exposed consolidated 

sedimentary rocks range in age from Permian to Jurassic and dip 

l°-2° NW.

212 Reyner, M. L., 1950, Preliminary report on some uranium deposits

along the west side of the San Rafael Swell, Emery County,

Utah: U. S. Atomic Energy Comm. RMO-673, 31 p., issued by

U. S. Atomic Energy Comm. Tech. Inf. Service, Oak Ridge, Tenn.

Twelve uranium deposits along the western flank of the San Rafael

Swell were examined. The deposits are lenticular or tabular bodies of

mineralized sandstone, conglomerate, or shale, and all are near the

base of the Shinarump conglomerate of Triassic age. The uranium

is intimately associated with blebs, seams of asphalt, and small bits

of carbonized wood. Brightly colored secondary uranium minerals

are present at the outcrop. The author describes the Lone Tree,

Hard Pan, Dalton, Dexter, Wickiup, Dolly, South Fork, Pay Day,

Green Vein, Brown Throne, and Dirty Devil groups of claims, and

the Clifford Smith, Hertz No. 1, and Gardell Snow claims.

213 Robeck, R. C., 1954, Uranium deposits of Temple Mountain; in 

Geology of portions of the High Plateaus and adjacent Canyon 

Lands, central and south-central Utah: Intermountain Assoc. 

of Petroleum Geologists, 5th Ann. Field Conference (Guidebook), 

Salt Lake City, Utah, p. 110-111.

The uranium deposits at Temple Mountain, Utah, are in the 

so-called Mossback sandstone unit of the Chinle formation of Triassic 

age. The area is on the southeast flank of the San Rafael Swell. The 

uranium is associated with wood fragments and petroleum residue 

(asphalt) in the lower part of a 100-foot thick cliff-forming sandstone bed.

214 Rogers, K. J., 1954, Reconnaissance of the lower Chinle along the 

Colorado River between the Moab and Dewey bridges, Grand 

County, Utah: U. S. Atomic Energy Comm. RME-70, 17 p., 

issued by U. S. Atomic Energy Comm. Tech. Inf. Service, Oak 

Ridge, Tenn.

One small radioactivity anomaly was noted during a reconnaissance 

for uranium deposits in the lower part of the Chinle formation of 

Triassic age in an area north of Moab along the Colorado River. The 

lower Chinle in this area, is apparently unfavorable for the occurrence 

of uranium deposits.

215 Rosenzweig, Abraham, Gruner, J. W., and Gardiner, Lynn, 1954, 

Widespread occurrence and character of uraninite in the Triassic 

and Jurassic sediments of the Colorado Plateau: Econ. Geology, 

v. 49, no. 4, p. 351-361.
142 SELECTED BIBLIOGBAPHIES OF URANIUM GEOLOGY

Uraninite has been found in many uranium deposits in the sedimentary rocks of the Colorado Plateau. Although this mineral is not 

restricted to any one formation, most of the occurrences are in the 

Shinarump conglomerate and Chinle formation of Triassic age. The 

two principal modes of occurrence are with copper sulfides or in 

asphaltic bodies. Association with fossil plants is common. Uraninite replaces the cell walls of fossil plants and copper sulfides fill 

the cells.

216 Schlottman, J. D., and Smith, L. E., 1954, Preliminary report on 

uranium mineralization in the Troublesome formation, Middle 

Park, Grand County, Colo.: U. S. Atomic Energy Comm. RME1042, 14 p., issued by U. S. Atomic Energy Comm. Tech. Inf. 

Service, Oak Ridge, Tenn.

The uranium minerals carnotite, autunite, and schroeckingerite 

occur in conglomerates, sands, and clays of the Troublesome formation of Oligocene to Miocene age in Middle Park, Colo. Middle Park 

is a structural and topographic basin partly filled with nearly a 

thousand feet of fluvial and lacustrine sediments of the Troublesome 

formation. Underlying rocks range in age from Precambrian to 

Tertiary. The uranium deposits, distributed throughout several 

square miles, are limited stratigraphically to the lower 160 feet of 

the formation. They are lenticular and are controlled by faeies 

changes in the clays, sands, and conglomerates. Carbonized plant 

material, jarosite, and brown and green vanadium minerals are 

common in many of the deposits. The deposits are small and most are 

not in radioactive equilibrium.

217 Schnabel, R. W., 1955, The uranium deposits of the United States: 

U. S. Geol. Survey Min. Inv. Res. Appraisals Map MR 2 (with 

text)

This map shows the location of the more important uranium deposits in the United States. The deposits are classed according to 

their geologic environment. These classes include the deposits in 

sandstone which are mainly on the Colorado Plateau but also in 

South Dakota, Wyoming, and other States; deposits in phosphorite 

in Florida, South Carolina, and in the Northwest; deposits in lignite 

which are mainly in South Dakota, North Dakota, and Wyoming; 

uraniferous black shale deposits which are mainly in Tennessee, 

Kentucky, Alabama, and Georgia; placer deposits of monazite in 

southeastern United States and in Idaho; and deposits in igneous 

rocks, pegmatites, veins, and limestone. The geology of each class of 

occurrence is briefly summarized.

218 Sharp, W. N., McKay, E. J., and McKeown, F. A., 1954, Powder

River Basin, Wyo.; in Geologic investigations of radioactive

deposits, Semiannual progress report, June 1 to November 30,

1954: U.S. Geol. Survey TEI-490, p. 117-119, issued by U.S.

Atomic Energy Comm. Tech. Inf. Service, Oak Ridge, Tenn.

The uranium deposits in the Pumpkin Buttes area of the Powder

River Basin are associated with a zone of interbedded, dominantly

red sandstone lenses and claystone strata near the middle of the

Wasatch formation of Eocene age. The red color boundary locally

transects primary sedimentary features. Iron-manganese-uranium
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 143

concretions are scattered erratically in the red sandstone at most 

places, although in some places they are associated with primary 

sedimentary features. Disseminated uranium ore with some iron, 

manganese, and concentrations of carbonate is associated with a 

sharp color change from primarily buff and gray sandstone to red 

sandstone.

219 Sharp, W. N., McKeown, F. A., McKay, E. J., and White, A. M., 

1956, Geology and uranium mineral deposits of the Pumpkin 

Buttes area, Powder River Basin, Wyo.: U. S. Geol. Survey 

Prof. Paper 300, p. 371-374; Geology of uranium and thorium, 

United Nations, v. 6, p. 403-406.

The Pumpkin Buttes are in the Powder River Basin which is an 

asymmetrical syncline trending north-northwest. The Wasatch 

formation of Eocene age crops out over most of the basin. Older 

rocks are exposed along the perimeter of the basin and remnants 

of the White River formation of Oligocene age cap the Pumpkin 

Buttes. The regional dip in the Pumpkin Buttes area ranges from 

30 to 100 feet per mile to the northwest.

The uranium deposits in the Pumpkin Buttes area are spatially 

related to a zone of predominantly red sandstone within the normally 

buff or gray Wasatch formation. The contacts between red and 

buff or gray parts transect all sedimentary structures and rock 

types within a sandstone unit. Tyuyamunite and carnotite are disseminated in buff or gray sandstone near and at the contact with 

red sandstone. Calcite is abundant at the contact. Uranophane 

occurs chiefly in the cores of, and peripheral to, manganese-iron 

oxide concretions; these deposits are small but high grade.

It is suggested that the deposits of oxidized uranium minerals 

were derived from initial deposits which were formed under reducing and mildly alkaline conditions.

220 Shawe, D. R., 1956, Significance of roll ore bodies in genesis of 

uranium-vanadium deposits on the Colorado Plateau: U. S. Geol. 

Survey Prof. Paper 300, p. 239-241; Geology of uranium and 

thorium, United Nations, v. 6, p. 335-337.

Similarities between "roll" ore bodies and the more prevalent 

tabular ore bodies in sedimentary rocks on the Colorado Plateau 

suggest a common origin for the two types. Analysis and interpretation of details of roll ore bodies may clarify genesis of the 

vanadium-uranium ore deposits on the Colorado Plateau. Roll ore 

bodies are found principally in sandstone lenses and layers in the 

upper part of the Salt Wash sandstone member of the Morrison 

formation of Jurassic age commonly near the base of thick sandstone units where many thin well-defined mudstone layers are interbedded with thin sandstone layers. Roll ore bodies are generally 

layered deposits that crosscut sandstone bedding in sharply curving 

forms. The long axes of rolls generally coincide with primary sedimentary features and may extend for hundreds of feet. Rolls 

commonly terminate against an upper and lower mudstone layer 

and may be split into two distinct rolls by a third thin mudstone 

layer. The details of roll ore bodies suggest that they were formed 

by precipitation of minerals at an interface between solutions of
144 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

different composition and density, and that flow of the ore-bearing 

or active solution as it passed through connate waters in the sediments was influenced strongly by local sedimentary features.

221 Shoemaker, E. M., 1954, Structural features of southeastern Utah 

and adjacent parts of Colorado, New Mexico, and Arizona; in 

Uranium deposits and general geology of southeastern Utah: 

Utah Geol. Soc., Guidebook to the geology of Utah, no. 9, Salt 

Lake City, p. 48-69.

Structural features of southeastern Utah are considered in three 

main categories: major uplifts and basins; salt plugs and salt 

anticlines; and domes, laccoliths, dikes, and diatremes.

The principal uplifts of southeastern Utah are the San Rafael 

Swell, Circle Cliffs uplift, the Uncompahgre uplift, and the Monument uplift; the largest basins are the Kaiparowits basin, the Henry 

Mountains basin, and the Uinta Basin. Each of the uplifts and 

basins is an asymmetric fold bounded on one side by a large monocline.

Five series of salt structures, some of which have collapsed crests, 

occur mainly in a northwest-trending belt in Colorado and Utah. 

The structures resulted from the intrusion of plastic masses of salt 

and gypsum.

The laccolithic mountain groups in Utah the Henry, La Sal, 

and Abajo Mountains consist of stocks of igneous rocks from 

which radiate tongue-shaped masses. Sills, dikes, small laccoliths, 

and diatremes are distributed irregularly in parts of southeastern 

Utah.

The tectonic history of the region is reviewed. The regional 

pattern was established before Cambrian time. Slight folding during 

the Permian period probably initiated the intrusion of salt which 

continued until late in Jurassic time. During the Late Cretaceous, 

the area was inundated by the sea and covered with about 5,000 

feet of sediments. Probably by the end of Cretaceous time most of 

the larger structures had assumed their present form and the laccolithic mountain groups had been intruded. The entire area was 

uplifted during the late Tertiary.

222 Smith, J. F., Jr., Hinrichs, E. N., and Luedke, R. G., 1952, Progress 

report on geologic studies in the Capitol Reef area, Wayne 

County, Utah: U.S. Geol. Survey TEI-203, 29 p., issued by 

U. S. Atomic Energy Comm. Tech. Inf. Service, Oak Ridge, 

Tenn.

Small deposits of uranium occur principally in a thin clay bed 

at the base of the Shinarump conglomerate of Triassic age in the 

Capitol Reef area. The uranium minerals zippeite and metatorbernite are associated with copper minerals, carbonaceous material, 

a thick bleached zone at the top of the underlying Moenkopi formation, and channels or scours in the top of the Moenkopi. Consolidated sedimentary rocks in the Capitol Reef area range in age from 

Permian to Jurassic and have an aggregate thickness of more than 

3,000 feet. The stratigraphy is described in considerable detail. 

The area is on the northeast and east flanks of a topographic and 

structural dome.
BIBLIOGBAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 145

223 Staatz, M. H., and Bauer, H. L., Jr., 1951, Virgin Valley opal district, Humboldt County, Nev.: U. S. Geol. Survey Circ. 142, 7 p. 

Carnotite and uraniferous opal occur in a gently dipping series 

of vitric tuff and ash beds in the Virgin Valley opal district. The 

carnotite occurs as fracture coatings and fine layers in the opal. 

The opal layers, some of which are uraniferous, are discontinuous 

and irregular in extent and thickness; they parallel the bedding 

of the ash and tuff beds. One sample contained 0.12 percent UsOs; 

others contained less than 0.05 percent UsOg.

224 Steen, C. A., Dix, G. P., Jr., Hazen, S. W., Jr., and McLellan, 

R. R., 1953, Uranium-mining operations of the Utex Exploration 

Co. in the Big Indian district, San Juan County, Utah: U. S. 

Bur. of Mines Inf. Circ. 7669, 13 p.; 1954, Mines Mag., v. 44, 

no. 4, p. 16-28.

A large uranium-vanadium ore deposit was discovered in July 

1952 by C. A. Steen on the Mi Vida claim in the Big Indian mining 

district, San Juan County, Utah. The district lies on the southwest flank of the faulted northwest-trending Lisbon Valley anticline; near the Mi Vida mine the rocks dip about 15° SW. The 

deposit is in the Chinle formation of Triassic age which is underlain by the Cutler formation of Permian age and overlain by the 

Wingate sandstone of Jurassic age. The rocks of the Chinle formation consist of variegated mudstones and siltstones, intraformational conglomerates, and fine- to medium-grained crossbedded sandstones. The ore-bearing unit in the lower part of the Chinle formation is characteristically gray; the upper part of the formation 

is red. The ore body is irregularly tabular in shape and ranges 

from 10 to 23 feet in thickness. The deposit lies in a channel scoured 

in the Cutler formation to a depth of about 50 feet; the channel 

axis trends about N 30° W. Abundant carbonaceous trash in the 

channel is replaced by pyrite or uraninite or preserved as carbon. 

The highly variable lithologic character of the channel material 

provides a favorable host rock.

Steen believes that the deposit was emplaced by hydrothermal 

solutions derived from Late Cretaceous or early Tertiary intrusive 

igneous rocks such as are exposed in the La Sal Mountains, but 

there is a possibility that the solutions could have been ground 

water or a mixture of ground water and hydrothermal solutions. 

The position of the deposits may have been controlled by the Lisbon 

Valley anticline.

Exploration, development, the surface and underground plants, 

the mining methods, and production are described.

225 Stephens, J. G., 1954, Crooks Gap area, Fremont County, Wyo.; 

in Geologic investigations of radioactive deposits, Semiannual 

progress report, June 1 to November 30, 1954: U. S. Geol. 

Survey TEI-490, p. 120-122, issued by U. S. Atomic Energy 

Comm. Tech. Inf. Service, Oak Ridge, Tenn.

In the Crooks Gap area, uranium

fault zone in both the arkosic sandstones of the Wasatch(?) formation of Eocene age and in ferruginous limestone and shale of Cambrian age. No ore-grade deposits ha

occurs mainly along a thruste been discovered in the Cam-
146 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

brian rocks. The Wasatch(?) formation consists of iron-stained 

coarse arkose that contains thin lenses of carbonaceous sandy shale 

and mudstone and interbeds of giant-boulder conglomerate. The uranium deposits are in the lower part of the formation and are associated with fine-grained carbonaceous beds and with red and 

brownish-yellow iron stained sandstone. Uranophane is the principal uranium mineral.

226 Stewart, J. H., and Williams, G. A., 1954, Stratigraphic relations 

of the Triassic Shinarump conglomerate and a prominent sandstone unit of the Chinle formation in southeastern Utah [abs.]: 

Geol. Soc. America Bull., v. 65, no. 12, p. 1387.

Recent field work in southern Utah indicates that the Shinarump 

conglomerate is not so extensive as was formerly thought, and 

that rocks called Shinarump conglomerate in east-central and 

central Utah are actually a separate unit. Field relations indicate 

that the Shinarump conglomerate extends from the type section 

in northwestern Arizona to a northwest-trending line passing about 

10 miles north of White Canyon, in southeastern Utah, where it 

pinches out. The Shinarump conglomerate is generally less than 

100 feet thick and consists of light-colored coarse- to very coarsegrained cross-stratified conglomeratic sandstone.

A prominent sandstone in the Chinle formation lying 200 feet 

above the top of the Shinarump conglomerate in White Canyon 

correlates with the unit called Shinarump in central and eastcentral Utah. A new name for this unit will be proposed at a 

later date. The prominent sandstone averages about 50 feet in 

thickness and is composed of light-colored fine- to medium-grained 

cross-stratified conglomeratic sandstone. Northward from White 

Canyon this prominent sandstone overlaps the underlying part of 

the Chinle. The known distribution of this sandstone indicates 

that it was deposited as a mass about 60 miles wide and 150 miles 

long extending northwestward from southwestern Colorado to 

central Utah.

The Shinarump conglomerate and the prominent sandstone are 

both interpreted to be stream deposits formed by northwest-flowing 

streams. Authors' abstract

227 Stieff, L. R., and Stern, T. W., 1952, Identification and lead-uranium 

ages of massive uraninites from the Shinarump conglomerate, 

Utah: Science, v. 115, no. 3000, p. 706-708.

Age determinations were made on massive uraninites from the 

Happy Jack mine in White Canyon, San Juan County, Utah, and 

from the Shinarump No. 1 claim in Seven Mile Canyon, Grand 

County, Utah. Both are in the Shinarump conglomerate of Triassic 

age. The ages, as determined from the Pb206 /U238 and the Pb207/ 

U235 ratios, range from 65 to 75 million years.

If the ages calculated are close to the true ages of these ores, 

then these minerals were probably formed in late Mesozoic or 

early Tertiary time. This interpretation differs from an earlier 

belief that the ore bodies were formed during or soon after deposition 

of the host rocks in Late Triassic time.
228

229

230

231

BIBLIOGRAPHY OF SANDSTONE-TY

Stieff, L. R., and Stern, T. W., 1! 

Pb208/U238<Pb207 /U235 «Pb207/Pb20 

Geology of uranium and thoriui 

546; see also, Interpretation of 

uranium ores : U. S. Geol. Surv

The age of many

Pb206 /U238, Pb207 /U235,

pb206/U238 agg i

uranium ore 

and Pb207 /P$

than the Pb207/Pb206 age. Various 

of these ages as "the true age" in 

have interpreted the age sequence a 

of lead, failure to correct for origins 

in the U235/U238 ratio. The geologic 

which may be very significant in 

origin of uranium ores, are discussed.

terms

Stieff, L. R., Stern, T. W., and Mil 

determination of the age of som 

Plateaus by the lead-uranium 

Circ. 271,19 p.

Age determinations by leadruran 

samples of uranium ore from the ( 

age as determined by the Pb206/U m 

and the average age as determine 

about 82 million years. If these a 

of the ores, the uranium was introduced 

Late Cretaceous or early Tertiary 

ago. This interpretation differs ma 

that the present uranium deposits w 

and Late Jurassic sediments during 

sediments between 152 million and 

methods and difficulties of making c

Stieff, L. R., Stern, T. W., and Sherwood, A. M., 1955, Preliminary

description of coffinite a ne1

v. 121, no. 3147, p. 608-609. 

A new radioactive black mineral 

mines on the Colorado Plateau, and 

and several foreign countries. Th 

with some hydroxyl substitution, has 

of Reuben Clare Coffin.

Stokes, W. L., 1944, Morrison format 

adjacent to the Colorado Platea 

v. 55, no. 8, p. 951-992. 

The Morrison formation in and 

is discussed. The Salt Wash, Brush 

Westwater Canyon members are cor 

Morrison and are almost certainly oi 

group of Jurassic age and beds ten 

taceous are also considered, 

paleogeography of all units are dis 

clature and correlation are recommenc

>E URANIUM DEPOSITS 147

56, The interpretation of the 

age sequence of uranium ores: 

( United Nations, v. 6, p. 540- 

;he discordant age sequence of 

y Prof. Paper 300, p. 549-555. 

minerals calculated from the 

206 ratios do not agree. The 

r/U235 age which is much less 

nvestigators have selected one 

reference to the other two and 

a result of loss of radon, loss 

I radiogenic lead, or variations 

consequences of this selection, 

of the search for and the

ey, R. G., 1953, A preliminary 

uranium ores of the Colorado 

method: U. S. Geol. Survey

um methods were made of 41 

olorado Plateau. The average 

thod is about 71 million years, 

by the Pb207/U235 method is 

?es are close to the true ages 

into the sediments during 

time 55 to 80 million years 

sedly from the previous belief 

re formed in the Late Triassic 

or soon after deposition of the 

127 million years ago. The 

terminations are discussed.

v uranium mineral: Science,

las been discovered in several

Q Wyoming, Colorado, Arizona,

mineral, a uranous silicate

been named coffinite in honor

on and related deposits in and 

: Geol. Soc. of America Bull.,

ac iacent to the Colorado Plateau 

Basin, Recapture Creek, and 

sidered equivalent to the type 

Jurassic age. The San Rafael 

;atively classed as Lower CreLitholojfic character, distribution, and 

ussed, and changes in nomen-
148 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

232 Stokes, W. L., 1948, Geology of the Utah-Colorado salt dome region 

with emphasis on Gypsum Valley, Colorado: Utah Geol. Soc. 

Guidebook 3, 50 p.

The geology and origin of salt anticlines and related structures 

in the Paradox salt basin in Utah and Colorado are discussed.

Sedimentary rocks ranging in age from Pennsylvanian to Recent 

are exposed in the area and Precambrian rocks are exposed to the 

northwest in the Uncompahgre Plateau. The evaporite deposits 

of the Paradox formation of Pennsylvanian age are overlain by 

nearly 6,000 feet of younger rocks. The primary structural trend, 

northwest-southeast, was established before deposition of the Pennsylvanian evaporites. Intrusion and solution of the salt has produced 

long, narrow, collapsed anticlines. Salt flowage has been intermittent since Permian time.

233 Stokes, W. L., 1951, Carnotite deposits in the Carrizo Mountains 

area, Navajo Indian Reservation, Apache County, Ariz., and 

San Juan County, N. Mex.: U. S. Geol. Survey Circ. Ill, 5 p. 

Carnotite deposits occur in the Salt Wash member of the Morrison 

formation of Jurassic age in the area surrounding the Carrizo 

Mountains in northeastern Arizona and northwestern New Mexico. 

Tertiary intrusive igneous rocks form the core of the mountain 

mass, and Mesozoic sedimentary rocks surround the mountains. The 

Salt Wash member in this area is a light-colored fine-grained crossbedded lenticular sandstone interbedded with shale and is from 60 

to 220 feet thick. Carnotite may occur at any stratigraphic level 

within it. The ore bodies are irregular tabular masses a maximum 

of 15 feet thick and a few hundred feet wide, and are nearly parallel 

to the principal bedding of the sandstone. The ore bodies are 

generally clustered in ill-defined areas a few thousand feet across. 

The origin of the deposits is not clearly understood, but they are 

thought to have been formed from ground water solutions shortly 

after the sands accumulated.

234 Stokes, W. L., 1952, Uranium-vanadium deposits of the Thompsons 

area, Grand County, Utah, with emphasis on the origin of 

carnotite: Utah Geol. and Mineralog. Survey Bull. 46, 51 p.

The Thompsons area of about 200 square miles occupies most of 

the northeast flank of the Salt Valley anticline in north-central 

Grand County, Utah. The area has been a contributor of uranium 

and vanadium ores since about 1911. Exposed sedimentary rocks 

include the Navajo, Carmel, Entrada, Summerville, Morrison, 

Cedar Mountain, Dakota, and Mancos formations. The Morrison 

formation, which contains the ore deposits, consists of a lower unit, 

the Salt Wash sandstone member and an upper unit, the Brushy 

Basin shale member. Paleontology, paleogeography, and lithologic 

features of the Morrison formation indicate a fluvial origin on an 

aggrading flood plain.

The ore bodies consist of a concentration of various uranium 

and vanadium minerals in sand lenses. Most of the ore minerals 

occupy pore spaces in the sandstone. The largest and richest ore 

bodies are elongate and crudely semicylindrical "rolls" that occur 

in groups in the sand lenses. Studies of cross-bedding in the area
235

236

BIBLIOGRAPHY OF SANDSTONE-TYI

show that the long axes of rolls are ] 

of the water that deposited the em 

nearly always accompanied by orga 

limonite staining in associated sands 

alterations in the mudstones below the

It is assumed that the ore minera 

water in the vicinity of decaying o 

the enclosing sandstones accumulatei 

to be essential to ore formation, cc 

given to factors that favor the ao 

on flood plains.

It is concluded that the edges of th 

along meander curves, are favorable 

and hence for the formation of ore

Stokes, W. L., 1953, Primary sedinn 

plied to ore finding in the Cai 

New Mexico: U. S. Atomic Ene 

48 p., issued by U. S. Atomic Ent 

Oak Ridge, Tenn.

Field studies in three areas in the 

dicate that uranium deposits in the 

rison formation are more common ir 

marked shifts in fluvial trends within 

in stream directions may have been 

the confluence of ancient streams, 

such areas is thought to be due to 

plant debris deposited along the bend

Stokes, W. L., 1953, Sedimentary pat 

tion in the Morrison formation o 

Geol. Soc. America Bull., v. 64,

It is generally believed that the Salt 

up of coarser fractions deposited in t 

deposited on the flood plains. The o 

stone lenses usually in association 

ore bodies contain elongate masses o 

are called "rolls"; fossil logs, when 

associated rolls.

The current directions which prev 

the sandstones, can be determined thr 

tion and other primary features. D 

made in certain districts show that th 

the direction of flow of the depositing 

lamination. This is thought to mean 

which brought together the various c 

through the sand lenses in essentially 

tions as the original surface streams 

ultimate source of the constituents 

mineralization may also be solved b 

 Author's abstract

237 Stokes, W. L., 1954, Relation of sed 

tures, and ore deposits in the Blan

URANIUM DEPOSITS 149

arallel to the direction of flow 

osing sandstone. The ore is 

ic material of some kind, by 

ones, and by blue-green color 

eposits.

were deposited from ground 

ganic materials shortly after 

As organic material seems 

isiderable attention has been 

umulation of plant materials

cker sand channels, especially 

sites for plant accumulation 

jposits. Author's abstract

ntary trend indicators as aprizo Mountains, Arizona and 

gy Comm. RME-3043(Pt. 1), 

fgy Comm. Tech. Inf. Service,

Carrizo Mountains region inalt Wash member of the Morareas where there are wellhe Salt Wash. These changes 

ue to ancient structures or to 

?he increased favorability of 

,n increase in the amount of 

of streams.

erns and uranium mineralizathe Colorado Plateau [abs.]: 

o. 12, p. 1516.

Wash is a fluvial deposit made 

e channels and finer fractions 

e deposits occur in the sandwith fossil vegetation. Most 

higher-grade material which 

present, lie parallel with the

iled during the deposition of 

ugh mapping of cross-lamina- 

-ailed study of the ore bodies

rolls lie mostly parallel with 

streams as revealed by crossthat the subsurface solutions 

nstituents of the ore traveled 

the same patterns and direcOther problems such as the 

of the ore and the time of

aid of sedimentary studies.

mentary trends, tectonic feaing district, San Juan County,
150 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

Utah: U.S. Atomic Energy Comm. RME-3093(Pt. I), 40 p., 

issued by U. S. Atomic Energy Comm. Tech. Inf. Service, Oak 

Ridge, Tenn.

Field studies of the Salt Wash member of the Morrison formation in the Blanding district indicate a relation between tectonic 

features, river courses, the accumulations of fossil plants, and the 

formation of ore bodies. It is thought that the Monument upwarp 

exerted some influence on stream directions in Salt Wash time, 

and that the carbonaceous material which localized the uranium 

deposits was preferentially deposited at the bends of streams.

238 Stokes, W. L., 1954, Some stratigraphic, sedimentary, and structural relations of uranium deposits in the Salt Wash sandstone, Final report April 1, 1952 to June 30, 1954: U.S. 

Atomic Energy Comm. RME-3102, 50 p., issued by U. S. Atomic 

Energy Comm. Tech. Inf. Service, Oak Ridge, Tenn. 

Investigations of the Salt Wash member of the Morrison formation of Jurassic age in Arizona and Utah included the study of 

(1) nature and origin of primary structures and their use in tracing 

zones that are favorable or unfavorable to mineralization; (2) 

relation of sedimentary properties of Salt Wash sandstones to 

primary structures and ore formation; (3) occurrence and meaning 

of the repetition of rock types in the Salt Wash; (4) relation of 

fossil plants or other organic material to sedimentary patterns 

and ore; and (5) relation of sedimentary patterns to mineralized 

areas and to ancient structural features.

Environments favorable for the deposition of uranium minerals 

probably were created by buried organic matter. Growth and 

burial of plants in Salt Wash time was not uniform but was concentrated along old river bends which are now shown by curving 

patterns of sediments. The areas of pronounced bends and greater 

than average amounts of organic matter are thought to occur in 

places where normal directions of flow were changed or where deflections of current took place due to tectonic features. Such areas 

can be located and followed by the observation and analysis of 

primary structures and of other sedimentary features.

239 Stokes, W. L., 1954, Stratigraphy of the southeastern Utah uranium 

region; in Uranium deposits and general geology of southeastern Utah; Utah Geol. Soc., Guidebook to the geology of 

Utah, no. 9, Salt Lake City, p. 16-47.

Exposed sedimentary formations in southeastern Utah are of 

every system from Mississippian to Tertiary. Older sedimentary 

rocks may be present but are not exposed. Each of the exposed 

formations is described.

Uranium ore has been produced from 21 formations on the Colorado Plateau; 7 formations contain uranium deposits that have 

yielded more than 1,000 tons. The bulk of the production in southeastern Utah has come from the Shinarump and Chinle formations 

of Triassic age and from the Morrison formation of Jurassic age. 

These three formations are discussed in greater detail than the 

others.
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS 151

240

241

Stokes, W. L., (ed.), 1954, Uraniun 

of southeastern Utah: Utah Geol 

of Utah, no. 9, Salt Lake City, 115 

Two sections of this report are 

vanadium-uranium-radium industry 

uranium mineralogy of the region i 

that includes mineral tables. The 

the region are discussed separately 

in this bibliography are no. 239 and 

ium deposits of the Thompson area 

Indian Wash-Lisbon Valley area ir 

described separately (annotat5ons of 

142 respectively).

deposits and general geology 

Soc., Guidebook to the geology 

Pdevoted to the history of the 

the Colorado Plateau. The

described in another section 

tratigraphy and structure of 

(annotations of these reports 

221 respectively). The urann Grand County and the Big

San Juan County are also 

these reports are no. 241 and

member

Stokes, W. L., and Mobley, C. M., 

posits of the Thompson area, Gr 

deposits and general geology of 

Soc., Guidebook to the geology 

City, p. 78-94.

Uranium-vanadium deposits in the 

sandstones in the Salt Wash 

of Jurassic age. Rocks in the area 

east away from the Salt Valley 

munite replace fossil plant material 

surrounding sandstone. Corvusite 

eral are disseminated in the sandston 

occur with the uranium minerals, 

or lenticular, with their long axes p 

may be curved zones, called "rolls," 

cross the bedding planes. The 

ore bodies is dominantly light gray 

red, and the mudstone interbedded 

ore bodies is gray rather than the 

appears to be confined mainly to th 

sandstone lenses; the larger ore de 

of the lenses.

1954

anticline.

and

242 Stokes, W. L., and Phoenix, D. A., 

Gypsum Valley area, San Miguel 

U. S. Geol. Survey Oil and Gas 

The stratigraphy and structure of 

posed sedimentary rocks range in 

Quaternary; no igneous rocks are p 

Triassic, and Jurassic rocks are of 

tural trend is northwest-southeast; 

in part to Paleozoic time. From 

include the Dolores anticline, the 

Gypsum Valley anticline. The Dol 

intrusive salt, and the Gypsum Vail 

crest of the latter is extensively fau

243 Stokes, W. L., Russell, R. T., Fischer 

1945, Geologic map of the Gate 

and the adjoining part of the Grand

Geology and uranium dend County, Utah; in Uranium 

outheastern Utah: Utah Geol. 

of Utah, no. 9, Salt Lake

Thompson area occur in fluvial 

of the Morrison formation 

ip at low angles to the northCarnotite and tyuyaand are disseminated in the 

a micaceous vanadium minalso, but they do not always 

The deposits may be tabular 

rallel to the bedding, or they 

of mineralized material that 

sardstone enclosing most of the 

white rather than the usual 

with the sandstone near the 

normal red-brown. The ore 

thicker and more continuous 

osits are in the central part

to

1948, Geology of the Egnarand Montrose Counties, Colo.:

. Prelim. Map 93 (with text).

the area are described. Exage from Pennsylvanian to 

esent. Most of the Permian, 

ontinental origin. The strucgentle regional folding dates 

south to north, the structures 

Disappointment syncline, and the 

>res anticline may be due to 

jy anticline certainly is. The 

ted and collapsed.

Irv,

the

R. P., and Butler, A. P., Jr., 

ay area, Mesa County, Colo., 

County, Utah: U. S. Geol.
152 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

Survey Strategic Minerals Inv. Prelim. Map 3-173 (with text). 

The vanadium-uranium deposits in the Gateway area of Colorado 

are in a bench-forming sandstone unit in the lower part of the 

Morrison formation of Jurassic age. The sandstone in the deposits 

is partly or wholly impregnated with carnotite and other vanadium 

minerals, and some plant material is richly mineralized. The ore 

bodies are irregular in shape; the larger ones are tabular and lie 

generally parallel to the bedding but cut the bedding in detail. Some 

of the ore bodies, called rolls by the miners, have a roughly cylindrical shape. The rolls and the mineralized logs have a northeasterly orientation. A belt in which the ore bodies are relatively 

close-spaced trends northwestward through the area. The location 

of the deposits is shown on a map.

244 Stokes, W. L., and Sadlick, Walter, 1953, Sedimentary properties

of Salt Wash sandstones as related to primary structures 

part 2, Technical report for April 1, 1952 to March 31, 1953:

U. S. Atomic Energy Comm. RME-3067, 26 p., issued by U. S.

Atomic Energy Comm. Tech. Inf. Service, Oak Ridge, Tenn.

Field and laboratory studies of primary sedimentary structures

of the Salt Wash member of the Morrison formation of Jurassic

age in the Carrizo Mountains of Arizona indicate that uranium

deposits are most prevalent between the flood plain and the more

 central parts of the channel sands because this environment was 

most favorable to the plant growth and burial needed to create an 

environment favorable to ore deposition. This zone can be identified 

by reference to primary structures and by sedimentary analysis.

245 Strobell, J. D., Jr., 1954, Stratigraphic relations in the Carrizo 

Mountains area, northeastern Arizona and northwestern New 

Mexico [abs.]: Geol. Soc. American Bull., v. 65, no. 12, p. 1310- 

1311.

Formations exposed in the Carrizo Mountains area range in age 

from Permian to Eocene(?). The De Chelly sandstone member of 

the Cutler formation (Permian) is underlain by Cutler red beds 

and unconformably overlain by Shinarump conglomerate (Late 

Triassic); the Moenkopi formation (Early and Middle (?) Triassic) 

is absent. The Chinle formation (Late Triassic) is restricted to 

Gregory's lower three divisions; red siltstone of Gregory's "A 

division" is now the lower member of a twofold Wingate sandstone 

that is assigned to the Triassic system on evidence gained by J. W. 

Harshbarger and associates elsewhere in the Navajo country. The 

Kayenta formation (Jurassic?) and Navajo sandstone (Jurassic) 

thin southward and disappear within the Carrizo Mountains area. 

The San Rafael group (Middle and Late Jurassic) comprises five 

formations: Carmel formation, Entrada sandstone, Todilto limestone, Summerville formation, and Bluff sandstone. Carmel is 

present only in the western half of the area, and Todilto only along 

the eastern edge. Where Carmel pinches out, Entrada rests unconformably without detected angularity upon Wingate.

The Morrison formation (Late Jurassic) comprises four members

 Salt Wash, Recapture, Westwater Canyon, and Brushy Basin. 

Possible equivalents of the Burro Canyon formation (Early Cretaceous) are not differentiated from the Morrison. Dakota sandstone
246

247

248

BIBLIOGRAPHY OF SANDSTONE-TYPE

overlies

s lale

(Late Cretaceous) unconformably 

formably succeeded by marine Mancos 

kopi, convergence of Kayenta, Navajo. 

thinning and lithologic change in other 

mittent uplift during Mesozoic time, 

truncated, and subsequently covered by 

 Author's abstract

erosion.

Stugard, Frederick, Jr., 1951, Uraniim 

Reef (Harrisburg) district, WasMngto: 

Geol. Survey TEM-214, open-file report 

Uranium deposits of the Silver Reef 

occur in the Tecumseh sandstone member 

of Triassic age. The principal struc 

the northeast-trending and plunging 

been thrust-faulted and breached by 

dipping as much as 36° are developed 

The ore occurs in thin-bedded and 

shale and sandstone and is apparent!; 

plant material. Vanadium-uranium or 

Chloride Chief and Silver Point claims 

times as much vanadium as uranium, 

silver. The occurrences are similar 

were mined from 1875 to 1909. More 

staked in the area.

resources in the Silver 

n County, Utah: U. S. 

, 33 p.

district near Leeds, Utah, 

of the Chinle formation 

,ural feature of the area is 

Virgin anticline which has 

Hogbacks, or "reefs," 

on resistant sandstone beds, 

crossbedded fluvial lenses of 

associated with carbonized 

B has been shipped from the 

The ore contains several 

some copper, and traces of 

;o the silver deposits which 

than 150 claims have been

Stugard, Frederick, Jr., 1952, Two ur; 

Washington and Kane Counties, 

Bull., v. 63, no. 12, p. 1373.

Uranium, vanadium, copper, and 

lenticular deposits in sandstone of the 

age at Silver Reef, Washington County 

porphyry nearby is thought to be the 

hydrothermal solutions that formed the (

At the Bulloch properties in Kane 

constitutes a blanket deposit in Juras 

unconformity between the Jurassic 

source of the uranium is not known.

Stugard, Frederick, Jr., 1953, Physical 

during 1951 in the Silver Reef 

Utah: U.S. Geol. Survey TEI-254 

The Silver Reef district in southwestern 

eastward trending and plunging Virgin 

breached by erosion. Thirteen diamond 

were located around Pumpkin Point, v 

grade deposits were found. Carnotite 

in surface exposures in mined areas, 

have been mined in the Chinle forma 

sight. The chances of discovering significant 

the Silver Reef district are poor becaus 

closely faulted structure, and the obliteration 

bearing lenses during silver mining, 

tions of several mines and prospects

URANIUM DEPOSITS 153

the Morrison and is conNondeposition of MoenCarmel, and Todilto, and 

formations suggest interThese rocks were folded, 

huska sandstone (Eocene?).

,nium deposits in sandstone, 

Utah [abs.]: Geol. Soc. America

silver minerals occur as small 

Chinle formation of Triassic 

Utah. A mass of trachyte 

source of the metal-bearing 

eposits.

County, disseminated autunite 

ic sandstone just below the 

and Cretaceous systems. The

exploration for uranium 

district, Washington County, 

open-file report, 59 p.

Utah lies on the northanticline which has been 

-drill holes, 10 of which 

ere drilled in 1951; no oreand volborthite are present 

Small lenticular ore bodies 

tion, but no ore remains in 

uranium deposits in 

j of highly variable lithology, 

of shallow uraniumThe report includes descripin the area.
154 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

249 Tavelli, J. A., 1951, Review of airborne radioactivity survey techniques in the Colorado Plateau: U.S. Atomic Energy Comm. 

RMO-697, 12 p., issued by U. S. Atomic Energy Comm. Tech. 

Inf. Service, Oak Ridge, Tenn.

An airborne technique for rapidly prospecting for surface exposures of uranium deposits is being developed. It has been found 

that uranium concentrations of commercial grade can be detected 

by simple instruments from low-flying fixed-wing aircraft. Flight 

elevations of 50 feet at air speeds of about 60 miles per hour have 

produced successful results with commercially available scintillation 

equipment. The technique is applicable only to exposed deposits 

and does not eliminate the need for ground prospecting.

250 Thomas, H. D., 1954, Uranium in Wyoming: Mines Mag., v. 44,

no. 3, p. 81-82, 96.

Uranium deposits in Wyoming occur in sedimentary rocks that 

range in age from Cambrian to Recent. The deposits in the Black 

Hills are in the Lakota sandstone, Fuson shale, and Fall River 

sandstone, all of Cretaceous age. Carnotite fills small fractures 

and interstitial spaces in medium- to coarse-grained sandstone that 

contains abundant carbonaceous material.

Deposits of carnotite and uranophane occur in sandstone in the 

Wasatch formation of early Eocene age in the Pumpkin Buttes 

area. In the Miller Hill area a uraniferous limestone occurs in a 

series of several hundred feet of mildly radioactive tuffaceous rocks 

of Tertiary age. Most of the uranium deposits of the Gas Hills 

are in sandstone in the Wind River formation of early Eocene 

age. The uranium deposits in the McComb area are in rocks of 

middle or late Eocene age, those in the Saratoga area are in the 

North Park formation of Pliocene age, and deposits near Mayoworth are in limestone of the Sundance formation of Jurassic age. 

In the Red Desert area schroeckingerite occurs in the Wasatch 

formation and in younger alluvial material. The deposits near 

Baggs are in Tertiary sandstones.

251 Tourtelot, H. A., 1952, Reconnaissance for uraniferous rocks in 

northeastern Wind River Basin, Wyo.: U. S. Geol. Survey TEM445, 14 p., issued by U. S. Atomic Energy Comm. Tech. Inf. 

Service, Oak Ridge, Tenn.

Most of the radioactivity anomalies detected by airborne instruments were in Precambrian rocks, but some were in Paleozoic and 

Cenozoic rocks. None contained more than 0.003 percent uranium.

252 Towle, C. C., and Rapaport, Irving, 1952, Uranium deposits of the 

Grants district, New Mexico: Min. Eng., v. 4, no. 11, p. 1037- 

1040 [abs.]: Econ. Geology, v. 47, no. 1, p. 128.

Uranium mineralization along the north flank of the Zuni Uplift 

in northwest New Mexico was discovered ... in 1950. . . . Irregular 

blanket-type uranium deposits are in terrestrial Jurassic sediments. 

The principal ore-horizon is the upper recrystallized portion of the 

Todilto limestone. This limestone erodes as benches one-half to 

three miles wide, enabling relatively cheap exploration and open-pit 

mining. Ore deposits have also been discovered in the sand lenses 

of the Morrison formation, 500 to 800 feet stratigraphically above
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS

the Todilto. The Morrison erodes into s 

expensive exploration and mining method 

The uranium minerals in the Todilto 

and uranophane; finely disseminated pii 

deposits are removed from the effects of 

minerals are pyrite, hematite, calcite, 

fluorite. The sandstone ores in the Mo 

schroeckingerite, associated with limonite 

The ore deposits are believed to have ac 

the lateral percolation of slightly heatec 

however, may have originally been contributed 

authors' abstract

eep cliffs, necessitating more

253 Trites, A. E., Jr., Finnell, T. L., and T 

deposits in the White Canyon ares 

U. S. Geol. Survey Prof. Paper ; 

uranium and thorium, United Nati 

Uranium deposits in the White Canyon 

conglomerate of Triassic age in channel 

Moenkopi formation, which is also of 

channels are within a band from 8 to 

known high-grade uranium deposits are 

15,000 feet of the edge of the band c 

The principal intrachannel control of 

have been lithologic; the most favorabl 

stone which contains carbonized plant 

siltstone or mudstone.

aden, R. E., 1956, Uranium 

, San Juan County, Utah: 

00, p. 281-284; Geology of 

ns, v. 6, p. 379-382. 

area occur in the Shinarump 

that have been cut into the 

Triassic age. Most of the

miles wide, and all of the 

in channels that are within 

f Shinarump conglomerate, 

uilanium deposition appears to

host rock is clayey sandnaterial and which overlies

15

254 Troyer, M. L., McKay, E. J., Soister, P.

Summary of investigations of uranium 

Buttes area, Johnson and Campb 

Geol. Survey Circ. 338, 17 p.

Uranium occurrences in the Pumpkin 

antly in sandstones of the Wasatch 

Pumpkin Buttes area lies in the topogra 

River Basin. The Wasatch formation i 

is underlain by the Fort Union forma 

overlain by the White River formation 

for the thin capping of White River ro 

rocks exposed in the area are of the WE

The uranium occurrences are in gray 

closely associated with a red sandstone 

above the base of the Wasatch for 

this zone is typically massive and crosi 

grained, feldspathic, and friable to mode 

beds are tuffaceous.

The uranium occurrences are of two pi 

and disseminated. The concretionary 

masses in which the principal uranium ir 

also contain vanadium minerals and a 

manganese oxides. The uranium center 

percent. The deposits are as much as 10 

but are usually smaller and may occur ir

155

are carnotite, tyuyamunite, 

chblende is found where the 

uperficial oxidation. Gangue 

and traces of barite and 

rison contain carnotite and 

and organic material, 

ieved their present form by 

Tertiary waters. Uranium, 

during the Jurassic. 

., and Wallace, S. R., 1954, 

deposits in the Pumpkin 

11 Counties, Wyo.: U. S.

Buttes area are predominfortnation of Eocene age. The 

phic and structural Powder

about 1,500 feet thick, and 

tion of Paleocene age and

of Oligocene age. Except 

eks on the high buttes, the

atch formation, 

to buff sandstones that are 

zone 450 to 900 feet 

nation. The sandstone in 

bedded, medium- to coarseately well cemented; a few

incipal types: concretionary 

posits are small irregular 

ineral is uranophane. These

large amount of iron and 

t is locally as high as 15 

feet in maximum dimension,

clusters. The disseminated
156 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

deposits occur as irregular zones in which metatyuyamunite irregularly impregnates the sandstone; little or no iron or manganese oxide 

is visible. In general, the sandstone in the concretionary deposits 

is cleaner than that in the disseminated deposits.

Two geologic maps of the area are included. One shows the locations of uranium occurrences and radioactivity anomalies; the 

other shows the distribution of favorable sandstones in the eastcentral part of the area.

266 Tschanz, C. M., 1953, Guadalupita, N. Mex.; in Geologic investigations 

of radioactive deposits, Semiannual progress report, June 1 to 

November 30, 1953: U. S. Geol. Survey TEI-390, p. 81-90, 

issued by U. S. Atomic Energy Comm. Tech. Inf. Service, Oak 

Ridge, Tenn.

The copper and uranium deposits near Guadalupita occur in 

lenticular shale, sandstone, arkose, and limestone beds in the lower 

2,500 feet of the Sangre de Cristo formation of Pennsylvanian and 

Permian (?) age. Although the Sangre de Cristo is predominantly 

a "red bed" unit, all the known deposits in this area are in gray, 

green, dark-gray, or yellow-brown beds. Both copper and uranium 

are most abundant in the more carbonaceous sediments. The deposits 

are discontinuous.

256 Tschanz, C. M., 1954, Guadalupita, N. Mex.; in Geologic investigations of radioactive deposits, Semiannual progress report, December 1, 1953 to May 31, 1954: U. S. Geol. Survey TEI-440, 

p. 72-73, issued by U. S. Atomic Energy Comm. Tech. Inf. Service, Oak Ridge, Tenn.

The copper-uranium deposits in the Guadalupita area are in the 

steeply dipping Sangre de Cristo formation of Pennsylvanian and 

Permian (?) age in a sandstone member near the middle of the 

formation. The deposits are localized by sedimentary structures 

in stream-laid sandstone beds that overlie the members that contain 

most of the larger copper deposits. Particularly favorable for 

uranium deposits are those parts characterized by local cut-and-fill 

structures, carbonized plant remains, chalcopyrite, gray or black 

clay galls, visible copper or vanadium minerals, and distinctive 

pink sandstone. Most of the uranium in sandstone is in a black 

ferric (?) oxide, but metatyuyamunite is locally abundant.

257 U. S. Atomic Energy Comm. and U. S. Geol. Survey, 1956, Techniques for prospecting for uranium and thorium: Geology of 

uranium and thorium, United Nations, v. 6, p. 752-755; see also, 

Foote, R. S., and Page, L. R., 1956, Techniques for prospecting 

for uranium and thorium A summary: U. S. Geol. Survey 

Prof. Paper 300, p. 621-625.

Successful prospecting and physical exploration for uranium and 

thorium requires a thorough knowledge of geologic, geochemical, 

and geophysical techniques. The favorability of each distinct geological unit within any large unexplored area can be evaluated 

by the use of these techniques. Preliminary geophysical reconnaissance of the favorable areas is best made by gamma radiation detectors carried by the geologist-prospector on the ground or in a 

low-flying aircraft. These techniques locate only exposed or slightly
BIBLIOGRAPHY OF SANDSTONE-TYP

259

260

261

262

263

buried deposits, but they commonly : 

tricts where concealed deposits are f 

Where ore minerals are not expose 

soil, rock, water, and plant samples a 

ation and geologic criteria. Structural 

guides useful in the search for deeply 

termined for most uranium districts i 

these guides, such as the structural 

host rocks, have been effectively 

niques.

esult in opening up new disund by other methods. 

, panning and the analysis of 

 e useful supplements to radilithologic, and mineralogic 

buried deposits have been dethe United States. Some of 

and lithologically favorable 

delineated by geophysical tech258 U. S. Geological Survey, 1951, Prog 

Desert) area, Wyoming: U. S. 

issued by U. S. Atomic Energy 

Ridge, Tenn.

This report concerns the prelimina.ry 

during 1949 on the schroeckingerite 

Wamsutter, Sweetwater County, Wye 

as a caliche deposit along a fault zone 

derived from uraniferous lignite cut 

of about 500 feet. It is suggested 

along other fault zones that cut uranif e

ess report: Wamsutter (Red 

reol. Survey TEM-96A, 2 p., 

Oomm. Tech. Inf. Service, Oak

results of field work done 

deposits at Lost Creek near 

The schroeckingerite occurs 

The uranium may have been 

by the fault zone at a depth 

similar deposits may occur 

rous lignite.

that

U. S. Geological Survey, 1953, Search 

deposits, Semiannual progress 

31, 1953: U. S. Geol. Survey TE 

Atomic Energy Comm. Tech. Inf

U. S. Geological Survey, 1953, Geologi 

deposits, Semiannual progress re 

1953: U. S. Geol. Survey TEI-390 

Energy Comm. Tech. Inf. Service, (

U. S. Geological Survey, 1954, Geologi 

deposits, Semiannual progress 

31, 1954: U. S. Geol. Survey TE 

Atomic Energy Comm. Tech. Inf.

U. S. Geological Survey, 1954, Geologi 

deposits, Semiannual progress rej 

1954: U. S. Geol. Survey TEI-490 

Energy Comm. Tech. Inf. Service 

The Geological Survey, under the 

Energy Commission, has undertaken 

materials in the United States and A 

which are statements of progress mad 

gives the principal unclassified 

particular period.

Vickers, R. C., 1954, Belle Fourche 

S. Dak.; in Geologic investigations 

annual progress report, June 1 to 

Survey TEI-490, p. 209-210, iss 

Comm. Tech. Inf. Service, Oak Rid| 

The uranium deposits of the Bell

position of horizontal change in color

URANIUM DEPOSITS 157

:or and geology of radioactive 

report, December 1, 1952 to May 

1-330, 302 p., issued by U. S. 

Service, Oak Ridge, Tenn.

; investigations of radioactive 

tort, June 1 to November 30, 

280 p., issued by U. S. Atomic 

iak Ridge, Tenn.

c investigations of radioactive 

December 1, 1953 to May 

-440, 246 p., issued by U. S. 

Service, Oak Ridge, Tenn.

report

e investigations of radioactive 

ort, June 1 to November 30, 

299 p., issued by U. S. Atomic

Oak Ridge, Tenn.

sponsorship of the Atomic 

investigations of radioactive 

aska. Each of these reports,

during a period of 6 months, 

information compiled during the

area, Northern Black Hills, 

of radioactive deposits, SemiNovember 30, 1954: U. S. Geol. 

ed by U. S. Atomic Energy 

e, Tenn.

Fourche area are near the 

from pink or red to gray or
158 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

buff sandstone within the lower unit of the Fall River formation 

of Cretaceous age. In detail the pink to buff contact cuts across the 

minor structures, but in general it is parallel to the regional strike 

of the beds. The deposits also seem to be related to local structural 

features such as flattening or reversal of the dip.

264 Vine, J. D., and Prichard, G. E., 1954, Uranium in the Poison Basin

area, Carbon County, Wyo.: U. S. Geol. Survey Circ. 344, 8 p. 

Uranium deposits occur in sandstone in the Browns Park formation of Miocene (?) age in the Poison Basin west of Baggs, Wyo. The 

Browns Park formation overlies the slightly tilted Wasatch and 

Green River formations of Eocene age. The unit in which the deposits 

lie is a soft light-colored crossbedded quartzose fine- to medium-grained sandstone that contains small amounts of tuff aceous material. The 

uranium minerals, mostly uranophane and schroeckingerite, are 

associated with brown, green, gray, or yellow sandstone. The uranium 

minerals coat fractures and are disseminated in the sandstone. They 

were probably deposited by ground water solutions of unknown origin. 

The Browns Park formation in this area contains an exceptionly large 

amount of selenium.

265 Walker, G. W., 1953, Rosamond uranium prospect, Kern County,

Calif.: Calif. Div. Mines, Spec. Rept. 37, 8 p.

Small quantities of autunite and of another radioactive mineral 

occur in tuffaceous sedimentary rocks of the Rosamond formation 

of Miocene age at the Rosamond prospect about 10 miles south of 

Mojave, Kern County, Calif. The autunite occurs principally as 

coatings on fracture and joint surfaces and, to a lesser extent, as 

disseminations in the tuffaceous rocks adjacent to faults. A waxy 

reddish-brown to black radioactive mineral associated with iron 

oxides and chlorite(?) is found in small quantities on slickensided 

fault surfaces.

266 Walthier, T. N., 1955, Uranium occurrences of the eastern United

States: Min. Eng., v. 7, no. 6, p. 545-547.

Uranium occurrences in the eastern United States are in sandstone, 

arkose, black shale, coal, and crystalline rocks in several different 

geologic environments. In the Jim Thorp area of Carbon County, 

Pa., several small pods of uraniferous material have been found in 

fluvial sandstone and graywacke in the Catskill formation of Devonian age. Uranium occurs in the same area in siliceous conglomerate 

in the Pottsville formation of Pennsylvanian age. In Hunterdon 

County, N. J., and Bucks County, Pa., small amounts of uranium 

minerals have been found in arkosic redbeds of the Stockton formation of Triassic age, and in southwest Virginia, abnormal radioactivity has been found in the Price sandstone of Mississippian age.

267 Wantland, Dart, 1952, Geophysical investigations for United States

Atomic Energy Commission in the Colorado Plateau area: U. S.

Bur. Reclamation Geol. Rept. G-119, 151 p., issued by U. S.

Atomic Energy Comm. Tech. Inf. Service, Oak Ridge, Tenn.

Geophysical field investigations were conducted at King Tutt

Mesa in Apache County, Ariz., and at Bull Canyon in Montrose

County, Colo. The resistivity method was used in both areas; the
BIBLIOGRAPHY OF

potential drop ratio method was un 

Canyon area. Areas of high resistn? 

of ground favorable for the occurren 

procedures are described and resistr

268 Wantland, Dart, and Casey, R. D., 

States Atomic Energy 

geophysical method for tracing 

ment Valley area, Arizona: U. 

G-123, 68 p., issued by U. S. 

Service, Oak Ridge, Tenn. 

Seismic methods were tested to d 

used in the mapping of buried channels 

occur. It was tentatively concluded 

could be used to determine the outline 

tion method proved unsuitable for

952, Field tests for the United 

Commission on the use of the seismic 

'buried channels" in the MonuS. Bur. Reclamation Geol. Rept. 

Atomic Energy Comm. Tech. Inf.

that

269 Waters, A. C., and Granger, H. C., 

ferous sandstones, and its poss 

precipitation of uranium: U. S.

The relationships between uraniui 

Colorado Plateaus and volcanic 

host rocks suggest that the uranium 

origin and history, and that they wer 

deformation and igneous intrusion of

Volcanic debris, now altered to 

in the Salt Wash sandstone and 

Morrison formation and in the 

formation. Field studies and micro 

indicate a relationship between the o 

clay formed by devitrification of 

hydromica formerly called "roscoe] 

from montmorillonite.

A paragenetic sequence of events 

sections of the ore-bearing sandstoi 

the sand by calcite, followed by se 

grains. The new silica deposited 

grains was probably released by dev: 

material. At a later date the 

vanadium hydromica and uraniumDeposition of the ore minerals wa; 

in ground-water conditions brought

During devitrification of volcanic 

leached alkalis, uranium, vanadium, 

ash. The absence of blanket depo 

minerals however, implied either (1) 

bearing ground water, or, more 

bearing juvenile waters into the 

additional problems must be i 

can be reached. Authors' abstract

quartz

270 Weeks, A. D., 1951, Red and gray cl 

stone of the Morrison formation

'E URANIUM DEPOSITS 159

uccessful in a part of the Bull 

ty can be correlated with areas 

e of uranium deposits. The field 

ity depth curves are plotted.

itermine whether they could be 

in which uranium ore might 

the seismic refraction method 

of channels. The seismic reflechis purpose.

1953, Volcanic debris in uranible bearing on the origin and 

Geol. Survey Circ. 224, 26 p. 

n-vanadium ore deposits on the 

material that, in part, make up the 

and vanadium have a complex 

emplaced during the structural 

Tertiary time.

clay minerals, has been recognized 

Brushy Basin shale members of the 

Shinarump conglomerate and Chinle 

icopic examination of the ores 

e minerals and montmorillonite 

volcanic glass. The vanadium 

te" is believed to be derived

shown by examination of thin 

;s, begins with cementation of 

ondary enlargement of quartz 

as overgrowths on the quartz 

;rification of the glassy volcanic 

grains were dissolved and 

jearing minerals were formed.

probably related to a change 

about by igneous intrusion, 

ash, ground waters may have 

and other substances from the 

its of uranium and vanadium 

reactivated circulation of metal- 

(2) introduction of metalground-water system. Several 

before final conclusions

probably

inves' igated

underlying ore-bearing sandin western Colorado: U. S. Geol.
160 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

Survey TEM-251, 19 p., issued by U. S. Atomic Energy Comm.

Tech. Inf. Service, Oak Ridge, Tenn.

As a result of a preliminary study of the clays that underlie the 

ore-bearing sandstone of the Morrison formation of Jurassic age, 

the principal clay mineral has been tentatively identified as hydrous 

mica. Chemical analyses show that the red clay contains more iron 

than the gray clay, but that more of the iron in the gray clay is n 

the ferrous state. Spectrographic analyses of minor constituents show 

no significant difference between the red and gray clay except in iron 

content. Quartz and carbonate have a wide range in quantity that 

is not related to the color of the clay. Sufficient evidence is not 

available to indicate whether the gray color was produced by alteration of the red clay.

271 Weeks, A. D., 1953, Mineralogic study of some Jurassic and Cretaceous 

claystones and siltstones from western Colorado and eastern 

Utah: U. S. Geol. Survey TEI-285, 22 p., issued by U. S. Atomic 

Energy Comm. Tech. Inf. Service, Oak Ridge, Tenn. 

The clay minerals and water-soluble minerals identified in 50 

samples of siltstone and claystone from Jurassic and Cretaceous 

formations suggest some distinctive characteristics for these formations and some differences in source area or environment of deposition. 

Hydromica predominates in samples of the Summerville and Burro 

Canyon formations and of the Salt Wash member of the Morrison 

formation, but montmorillonite derived from volcanic ash is found in 

samples from the Brushy Basin member of the Morrison. Kaolinite 

in the Dakota sandstone is probably related to the regional unconformity at the base of the Dakota. Size analyses show that 

most of the samples are siltstones.

272 Weeks, A. D., and Thompson, M. E., 1954, Identification and occurrence of uranium and vanadium minerals from the Colorado 

Plateaus: U. S. Geol. Survey Bull. 1009-B, p. 13-62. 

This report gives physical properties, X-ray data, and in some 

instances results of chemical and spectrographic analyses of 48 uranium and vanadium minerals Also included are lists of mines in which 

the minerals have been identified.

273 Weeks, A. D., Thompson, M. E., and Thompson, R. B., Jr., 1953, 

Mineral associations and types of uranium ores on the Colorado 

Plateaus [abs.]: Geol. Soc. America Bull., v. 64, no. 12, p. 1489- 

1490.

Uranium ores from the Colorado Plateaus are classified as (1) 

uranium with vanadium, and (2) uranium with copper and other 

metals. Each type is subdivided into highly oxidized ore and relatively unoxidized ore

The vanadium-to-uranium ratio of the vanadiferous ores ranges 

from about 30:1 at Placerville and Rifle, Colo., to about 1:1 at 

Temple Mountain in the San Rafael district of Utah. The chief uranium minerals of the highly oxidized ore are the uranyl vanadates: 

carnotite, tyuyamunite, and metatyuyamunite.

The black unoxidized vanadiferous ores contain a new black uranium mineral, and pitchblende, montroseite, and at least two other low-
274

275

276

277

BIBLIOGRAPHY OF SANDSTONEvalence vanadium oxides. They 

sulfides.

The oxidized nonvanadiferous 

orange, or green uranium miner! 

erals.

The unoxidized nonvanadiferous 

blende, base-metal sulfides, and th 

above.

Weir, D. B., 1952, Geologic guide 

posits on Colorado Plateau: 

p. 15-27.

This report describes the geol 

appraise the favorableness of gr 

ploration for carnotite deposits in 

mation on the Colorado Plateau. '. 

the geologic logs of about 2,500 ho 

The most useful features consist 

ore-bearing sandstone, the altered 

bearing sandstone, and the abundance 

sandstone. Although each feature 

favorableness of the ground, an 

gether is more useful. A metho 

values is suggested.

The results obtained by the Geo 

guides appear to be at least twice 

obtained with little or no geologic

Wherry, E. T., 1915, Carnotite n 

Survey Bull. 580-H, p. 147-151 

Carnotite occurs thoroughly 

a 40-foot layer of coarse-grained 

Pottsville formation of Pennsyl 

Mauch Chunk. The outcrop ext 

road cut. The uranium and 

originally contained in detrital 

Circulating ground waters since 

the uranium and vanadium.

Williams, F. J., and Barrett, D 

reconnaissance in the Came 

Energy Comm. RME-4002, 10 

Comm. Tech. Inf. Service, Oal

YPE URANIUM DEPOSITS 161 

are associated with base-metal

ore is characterized by yellow, 

s and blue or green copper min-

»re is also black and contains pitch^ 

s new uranium mineral mentioned

to prospecting for carnotite deU. S. Geol. Survey Bull. 988-B,

cigic features that can be used to 

und in guiding diamond-drill exthe Upper Jurassic Morrison fort is based on a statistical study of 

es drilled by the Geological Survey, 

of the thickness and color of the 

mudstone associated with the oreof carbonaceous material in the 

can be used alone to appraise the 

ppraisal based on all of them toof expressing this in numerical

ogical Survey using these geologic 

as favorable as the drilling results 

guidance. Author's abstract

Wherry, E. T., 1912, A new occurrence of carnotite: Am. Jour. Sci.,

4th ser., v. 33, no. 198, p. 574-5 

Small' scattered occurrences of 

of conglomerate in the Pottsvilli 

near Mauch Chunk, Pa. The mim 

patches in the lower part of the be d 

feet along a roadway. The auth 

vanadium minerals were origina 

as detritus, and that the metals 

circulating meteoric waters.

0.

arnotite have been found in a bed

formation of Pennsylvanian age 

ral occurs in scattered streaks and

, which is exposed for about 2,600 

r suggests that the uranium and 

ly deposited in black shale beds 

ivere extracted and redeposited by

ar Mauch Chunk, Pa.: U. S. Geol.

but unevenly distributed throughout 

conglomerate near the base of the 

vanian age about a mile north of 

nds for about 2,000 feet along a 

adium are thought to have been 

minerals of the host formation, 

have dissolved and redistributed

C., 1953, Preliminary report of 

ron area, Arizona: U. S. Atomic 

p., issued by U. S. Atomic Energy 

Ridge, Tenn.
162 SELECTED BIBLIOGRAPHIES OP URANIUM GEOLOGY

Ground and airborne reconnaissance for uranium was conducted 

in the Cameron area, Coconino County, Ariz. The largest and best 

deposits are in the Petrified Forest member of the Chinle formation 

of Triassic age, but uranium also occurs in association with fossil 

logs in the Shinarump conglomerate, also of Triassic age. The 

uranium deposits in the Petrified Forest member are in silty mudstone and clay which contain scattered sand and carbonaceous material. The normal gray of the rocks has been changed to light tan 

or yellowish brown near the deposits. Uraninite and secondary 

uranium minerals are associated with pyrite, smaltite, calcite, 

gypsum and carbonaceous material. The deposits contain negligible 

amounts qf copper and vanadium.

278 Williams, G. 0., 1925, Radium-bearing silts of southeastern Utah:

Eng. Min. Jour., v. 119, no. 5, p. 201-202.

Radium-uranium deposits have been found in silt and clay beds 

of either Tertiary or Quaternary age on the floor of Montezuma 

Canyon in San Juan County, Utah. The author suggests that 

ancient carnotite deposits in an unknown host rock were eroded, 

washed downstream, and redeposited on the floor of the canyon.

279 Wilmarth, V. R., 1953, Garo, Colo.; in Search for and geology of 

radioactive deposits, Semiannual progress report, December 1, 

1952, to May 31, 1953: U. S. Geol. Survey TEI-330, p. 109-110, 

issued by U. S. Atomic Energy Comm. Tech. Inf. Service, Oak 

Ridge, Tenn.

The Shirley May uranium-vanadium-copper deposit near Garo, 

Park County, is on the northeast flank of the Garo anticline in 

the Maroon formation of Permian age. The minerals, principally 

tyuyamunite, carnotite, volborthite, azurite, and malachite, occur 

in three separate medium- to coarse-grained sandstone beds as 

disseminations, cementing material, and fracture fillings. The gangue minerals are calcite, manganite, and hematite. The localization of ore is mainly controlled by faulting and the porosity of the 

sandstones adjacent to the faults.

280 Winterhalder, E. C., 1954, Preliminary reconnaissance for uranium 

in the Green River Basin and the Rock Springs uplift, Sweetwater and Fremont Counties, Wyo.: U. S. Atomic Energy Contim. 

RME-1045, 10 p., issued by U. S. Atomic Energy Comm. Tech. 

Inf. Service, Oak Ridge, Tenn.

Reconnaissance for uranium deposits in part of southwestern 

Wyoming disclosed two areas of anomalous radioactivity. One area 

is northwest of Oregon Buttes in the southwest corner of Fremont 

County. Anomalous radioactivity is present in some micaceous and 

arkosic sandstones of the Tipton tongue of the Green River formation and the Cathedral Bluffs tongue of the Wasatch formation, 

both of Eocene age. The other area, the Red Creek basin, is south 

of Rock Springs, Wyo., near the Utah-Wyoming border. Here, 

some shale, carbonaceous shale, coal, and limestone beds in the 

Tipton tongue of the Green River formation are anomalously radioactive.

281 Witkind, I. J., 1954, Localization of uranium minerals in channel 

sediments at the base of the Shinarump conglomerate, Monu-
282

283

284

BIBLIOGRAPHY OF SAFDSTOFEment Valley, Ariz. [abs.]: Econ 

Geol. Soc. America Bull., v. 65, 

Uranium ore bodies in the 

in the conglomeratic sandstone o 

Triassic age that fills channels 

kopi formation which is also of 

from 15 feet wide and 10 feet 

deep. Fragments of trees were 

ments in the channels. Witkind £ 

conglomerate was invaded by 

minerals were deposited mainly 

plant material. The author also 

more likely to contain ore than long

. Geology, v. 49, no. 7, p. 804-805; 

no. 12, p. 1327.

Mcnument Valley area are localized 

the Shinarump conglomerate of 

cured into the underlying MoenTriassic age. These channels range 

deep to 2,300 feet wide and 70 feet 

deposited with Shinarump sediuggests that when the Shinarump 

mineralizing solutions, the uranium 

in and adjacent to decomposing 

suggests that short channels are 

channels.

into

Witkind, I. J., 1956, Channels and 

Shinarump conglomerate, 

Survey Prof. Paper 300, p. : 

thorium, United Nations, v. 6,

Vanadium-uranium ore deposits 

nel sediments at the base of the S 

age. The channels range in wid 

scoured a maximum of 75 feet i 

between channels and uranium d 

repeatedly that prospecting in th 

for, and exploring, these channels.

In some places a channel coincid< 

swale. The swales are too large 

parent on isopach maps. The 

miles, and have about 40 feet of r 

and outline concealed channels by

related swales at the base of the 

Monument Valley, Ariz.: U.S. Geol. 

33-237; Geology of uranium and 

. 368-370.

in Monument Valley are in chaninarump conglomerate of Triassic 

h from 15 to 2,300 feet and are

underlying strata. The relation 

posits has been demonstrated so

area has evolved into searching

Wood, H. B., and Grundy, W. D. 

exploration of Shinarump 

Geology of uranium and thor 

703; see also, Techniques and 

in Shinarump channels on 

Survey Prof. Paper 300, p. 651 

This paper discusses geologic 

ployed in the search for uraniurr 

glomerate of Late Triassic age in 

regions of southeastern Utah, an 

Utah and Arizona. The formati 

posits of Permian and Triassic age 

quality occur in Shinarump sed 

channels cut into the underlying

Wright, R. J., 1954, Prospecting wi 

Comm., 68 p., U. S. Government 

D. C. 

This report is a summary of

use of portable radiation detecti

prospecting for uranium, such as

counters.

YPE URANIUM DEPOSITS 163

s with the axis of a broad elongate 

'or visual observation but are apswales range in width from 1 to 3 

lief. It may be possible to locate 

exploration of the swales.

1956, Techniques and guides for 

channels on the Colorado Plateau: 

um, United Nations, v. 6, p. 701- 

guides in exploration for uranium 

the Colorado Plateau: U. S. Geol. 

657.

guides and drilling techniques emdeposits in the Shinarump conhe Circle Cliffs and White Canyon 

I the Monument Valley region of 

ns concerned are continental deUranium deposits of commercial 

ments which fill ancient stream 

rocks.

h a counter: U. S. Atomic Energy 

Printing Office, Washington,

nformation on the operation and 

n equipment suitable for use in 

Geiger counters and scintillation
164 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

285 Wright, R. J., 1955, Ore controls in sandstone uranium deposits of 

the Colorado Plateau: Econ. Geology, v. 50, no. 2, p. 135-155.

Wright, R. J., 1953, Lithologic ore controls in sandstone type uranium deposits, Colorado Plateau [abs.] : Geol. Soc. America Bull., 

v. 64, no. 12, p. 1495.

Marked lithologic control characterizes most uranium deposits in 

sandstone formations of the Colorado Plateau. Deposits in rocks 

ranging in age from the Cutler formation of Permian age to the 

Wasatch formation of Eocene age are primarily in 1) fluvial sandstones which, 2) contain carbonized plant matter, 3) are lightcolored or gray rather than red, and 4) contain feldspar or mica. 

In addition, 5) sandstones that are interbedded with or interfinger 

with shales or mudstones are particularly favorable. These features are also characteristic of most sedimentary copper deposits.

Most uranium deposits in sandstone formations show no immediate 

connection with tectonic features, but a general clustering of ore 

bodies around large positive structures is noted. The reason for 

this is not clear.

It is postulated that at least some of the uranium in the ores 

was derived from the same source as the host rocks. In this light 

the sandstone uranium deposits may be the continental analogue 

of uranium-rich marine black shales and phosphorites. Sedimentary copper deposits may have had a similar origin. Uranium 

moving seaward in streams, during erosion of a land mass, may 

be fixed on the continent in certain favorable fluvial environments. 

 Author's abstract

286 Wyant, D. G., 1952, Lost Creek (Wamsutter) schroeckingerite deposit, Sweetwater County, Wyo.: U. S. Geol. Survey TEM-10B, 

3 p., issued by U. S. Atomic Energy Comm. Tech. Inf. Service, 

Oak Ridge, Tenn.

Schroeckingerite deposits occur at Lost Creek, Wyo., in clays and 

sands of Eocene or younger age. The yellow platy micaceous mineral occurs as rounded aggregates in the clay beds, and as fine 

disseminations in the sand and sandy clay beds. The uraniferous 

beds are discontinuous and their areal distribution is erratic. The 

beds strike northwest and dip 14° - 27° NE. The area is part of 

the Continental Divide Basin.

287 Wyant, D. G., Beroni, E. P., and Granger, H. C., 1952, Some uranium deposits in sandstones; in Selected papers on uranium deposits in the United States: U. S. Geol. Survey Circ. 220, p. 

26-29.

The principal domestic source of uranium and vanadium has 

long been the carnotite and roscoelite deposits in sandstone of the 

Morrison and Entrada formations of Jurassic age on the Colorado 

Plateau. Other known uranium deposits occur in sandstones that 

range in age from Paleozoic to Recent; many of these differ from 

the carnotite deposits in mineralogy, host rock, localization, and 

possible origin. The deposits may be grouped on the basis of mineral or metal assemblage into (1) uranium-vanadium deposits; (2) 

copper-uranium-vanadium-carbonized wood deposits; (3) uraniferous
BIBLIOGRAPHY OF SANDSTONE-TYPE URANIUM DEPOSITS

288

289

290

asphalt deposits; and (4) 

deposits.

In general, these deposits occur 

stone or conglomerate interbedded 

materials are iron oxide, carbon, 

ization of some of these deposits a 

sedimentary features of the enclos 

osity, fractures, and proximity to 

minerals may have been deposited 

have formed by weathering and 

some may be hydrothermal in 

showing the location and types oi 

and briefly describes an example

miscellaneous deposits including carbonate

with 

and

the

orijnn

of each

in lenses of argillaceous sandshales. Commonly associated 

copper compounds. The localpears to be controlled by initial 

ng rock, that of others by porsurface. Some of the uranium 

from ground water, some may 

xidation of other minerals, and 

The report includes a map 

uranium deposits in sandstone, 

type.

Zareski, G. K., 1954, Reconnaissance

Mesa, San Juan County, Utah 

U. S. Atomic Energy Comm. 

U. S. Atomic Energy Comm. Te 

Reconnaissance examination was 

posits on Wray Mesa. The depos 

horizons in the Salt Wash memte 

Jurassic age, and in sandstone len 

Basin member of the Morrison 

carnotite, tyuyamunite, and black 

Exposed formations are of Jurass 

rocks dip about 3° NW.

Zeller, H. D., and Baltz, E. H., Ji 

deposits in the Coyote distric 

Geol. Survey Circ. 334, 11 p.

Uranium-bearing copper deposits 

tion of Pennsylvanian and Permia 

occur in lenticular carbonaceous z 

shale and arkosic sandstone. 

3 percent copper and contain as 

Metatyuyamunite is disseminated 

beds, and uraninite was identified 

nodules found in the shale. The s 

cipally of chalcocite with some bo 

chite. Some nodules replaced wood.

The copper and uranium were 

ments and concentrated into zones 

tion. Carbonaceous material in th 

vided the environment that precip 

mineral-charged connate waters

if uranium occurrences at Wray 

and Montrose County, Colo.: 

ME-69(Pt. 1), 15 p., issued by 

ch. Inf Service, Oak Ridge, Tenn. 

made of several uranium de- 

;s occur in sandstone at several 

r of the Morrison formation of 

es near the base of the Brushy 

formation. The ore minerals are 

ranium and vanadium minerals, 

c and Cretaceous age, and the

Anonymous, 1955, Uranium, a com 

in California and in the Colo 

Min. Inf. Service, v. 8, no. 5, p. 

Uranium deposits are known to o 

metamorphic rocks at about 100 

localities are indicated on a map. 

San Luis Obispo and Kern Counti 

uranium minerals coat fractures in

165

1954, Uranium-bearing copper 

Mora County, N. Mex.: U. S.

Samples

in the Sangre de Cristo formai age south of Coyote, N. Mex., 

ones in steeply dipping beds of 

from these zones average 

nuch as 0.067 percent uranium, 

i some of the arkosic sandstone

in some of the copper sulfide 

Ifide nodules are composed prinnite, covellite, pyrite, and malaprobably deposited with the sediduring compaction and lithificaSangre de Cristo formation protated uranium and copper from 

reed from the clayey sediments.

'arisen of its geologic occurrence

ado Plateau: Calif. Div. Mines,

-7.

:cur in igneous, sedimentary, and

localities in California. These

In the Taft-McKittrick area of 

s, carnotite and other secondary

shale beds of Tertiary age. In
166 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

the Rosamond-Mojave area of Kern County, secondary uranium 

minerals occur along fractures and bedding planes and as dissemminations in tuff aceous sedimentary and rhyolitic rocks of the Rosamond formation of Miocene age. In Kern Canyon in Kern County, 

autunite and other uranium minerals occur in and near shear zones 

in granitic rocks. Uranium deposits are also known in many other 

scattered areas in California.

Uranium deposits in other areas of the United States and the 

world are described in order to provide a general concept of geologic 

occurrence that might be useful in the search for uranium deposits 

in California. Descriptions of these deposits are taken largely 

from other publications. These include Finch (1955, see ref. 75), 

Nininger (1954, see ref. 193), Fischer and Hilpert (1952, see ref. 

86), Everhart (1951, see ref. 70), Fischer (1950, see ref. 83), and 

Bain (1950, see ref. 4).
INDEXES

AUTHORS

Index no, 

Alien, M. A..........................__ 35

Anderson, E. C. -_____.._......_ 1

Argall, G. O., Jr......................... 2,3

Bain, G. W, . 4-6

Baker, A. A................................ 7-12

Baker, R. C............................_ 159

Bales, W. E......_...................... 13

Baltz, E. H., Jr..... 289

Barrett, D. C....___................... 14, 277

Barton, P. B., Jr. ..................... 16, 18

Bauer, H. L. ______.___.___.__ 223 

Behre, C. H., Jr........................... 15, 16

Bell, Henry, 3d............................ 13, 17

Benson, W. E.............._........._ 18

Beroni, E. P.____....__...__18-22,287

Black, R. A............................... 23

Boardman, R. L.............______ 24

Bodine, M. W., Jr....................... 25

Boutwell, J. M.......................___ 26

Bowers, H. E. ____._________ 24 

Boyle, T. L.._.............._..___ 27

Braddock, W. A.........._.........._. 104

Branson, C. C.______._________ 28 

Brooke, G. L........................._... 29

Bucher, W. H. ........................._. 30

Bullock, K. S.-.-...-....._.........._ 203

Burwell, A. L......._................... 28

Burwell, Blair ............................ 31, 32

Butler, A. P., Jr........._........... 33, 243

Butler, B. S..._..............._...._ 34

Butler, G. M............................... 35

Cadigan, R. A............................. 49a

Canney, F. C.._....._........__.... 171

Cannon, H. L. __________.__.. 36-38 

Cannon, R. S.,Jr..-.-..________ 39 

Carithers, L. W......__._._._.._ 40

Carlson, W. A............................. 69

Casey, R. D.._....._._.__..____ 268

Cater, F. W., Jr......................... 41-43

Chase, G. C.......------.._.......___ 28

Chase, G. W. .. ._ 44

Chester, J. W.... ..__-.--.--..__ 46

Clinton, N. J.._..............__.____ 40

Coffin, R. C._..----.---.-._.._...... 46

Comstock, S. S.------.-..__ ...... 47

Cook, K. L.__---.-...._......_.._ 48

Craig, L. C.__._._............... 49a, 49b

Cumenge, E. ........ ...__..____ 91

Curran, T. F. V............... ... 50, 51

Dane, C. H. ......................... 11, 12, 62

Index no.

Davidson, D. F... .- . -68, 64 

Davis, D. L....--...---...----...-....--.. 65 

Davis, W. E.... . ........ ----- 66

Denson, N. M..-..____ . . 67 

deVergie, P. C.. ........................ 58, 59

Dix, G. P., Jr. .. - 60, 61, 224 

Dodd, P. H.... . 62, 63

Droullard, R. F. 64

Duschatko, R. W.- 65

Ekren, E. B.. 24

Ellsworth, P. C.----. . - 66, 67, 168

Erickson, R. L. 68, 103

Evenson, C. G. 177, 187

Everhart, D. L. 69-71. 179

Faul, Henry __ . 72 

Feeger, J. A. 18

Finch, W. L 73-76

Finnell, T. L. - 263

Fischer, R. P... 77-87, 248 

Fix, Philip . . . ...... 88

Fleck, Herman ....................... 89

Foote, R. S................... .... 257

Freeman, H. D. - ... 90 

Freeman, V. L. ..... 49a, 136, 193

Friedel, Charles ..- - .-- 91

Gabelman, J. W. - -- 92, 93

Gale, H. S. 94. 96

Gardiner, Lynn .. .... 117, 118, 120, 215

Garrels, R. M... . 96-98. 179 

Gilkey, A. K.... -- . 30, 99

Gill, J. R. 100

Gilluly, James . - . 101, 102 

Gott, G. B.. . ...... 17, 22, 103, 104

Granger, H. C.. ............. 269. 287

Gray, J. K............................. i06

Gregg, C. C. ...... 106

Gregory, H. E. ......... . . 107-110

Grier, A. W. HI

Griggs, R. L. 112, 113

Gross, E. B. - 162

Grundy, W. D... ... ... 176. 283 

Gruner, J. W. 114-120, 216

Grutt, E. W. 121, 122

Gustafson, J. K. ........ .. . 123

Hadfield, J. P......... . . 206

Haft, J. C................................. 86

Haldane, W. G. - 89

Hall, R. B. ........ ....... ..... 124

Hatfield, K. G... 66. 126
168 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

Index no. 

Hazen, S. W., Jr......---.___.__._.__.. 139, 224

Heikes, V. C. ........................ 34

Hess. F. L.-,.__............._.___126-131

Hetland, D. L..................._____ 55

Hewett, D. F................._.__._ 132-134

Hillebrand, W. F......................... 135

Hilpert, L. S._.................__...... 86, 136

Hinckley, D. N........................... 137

Hinrichs, E. N.._.....__...._____ 222

Holmes, C. N............._.__.___ 49a

Horr, C. A....._.__.___________ 68

Huff, L. C.-..-.-....-._....._._._. 138

Huleatt, W. P... . ..__.___....____ 139

Hunt, C. B................................. 140

Huttl, J. B................................. 141

Hyatt, E. P............................... 203

Isachsen, Y. W.....----.....-....---... 142-145

Jobin, D. A............................... 146

Jones, D. J.__________________ 147

Jones, E. E.__________________ 64

Jones, R. S............................... 104

Joubin, F. R.. ______. __________ 148

Kaiser, E. P.___________._____ 149

Keller, W. D............................... 191

Kelley, D. R.._..__.........__...... 150

Kelley, V. C........................... 151, 152

Kellogg, J. P......__.................. 208

Kentro, D. M.________________ 153

Keys, W. S........_____.________ 154

Kimball, Gordon ....._.............__ 155

King, E. N.-._..............__........_ 200

King, J. W....._...............____ 156-158

King, R. U.........._._----..____ 20

Kithil, K. L............................... 189

Kleraic, Harry ......______._._... 159

Knoerr, A. W.____........_.____. 160

Koeberlin, F. R.............__.____ 161

Lakin, H. W.-............................. 171

Laverty, R. A.________________ 162 

Levine, Harry ________________ 198 

Levish, Murray _______________ 188 

Lindgren, Waldemar ___________ 163 

Loughlin, G. F.________________ 34 

Love, J. D............................... 164-168

Lovering, T. G.__...________. 169, 170 

Lovering, T. S......_...._.___.__ 171

Lowell, J. D._....................___. 172

Luedke, R. G........................... 173, 222

Lutjen, G. P......_____............_ 160

MoKay, E. J................... 174, 218, 219,254

McKee, E. D.................._.......... 175

McKelvey, V. E........ .............. 176, 177

McKeown, F. A......--..-...... 21, 22, 218, 219

McKnight, E. T........................... 178

McLellan, R. R........................... 224

Maise, C. R............................... 125

Masters, J. A........................... 179, 180

Mathez, Muriel _.____________ 70 

Merritt, P. L............................. 181

Milkey, R. G............................... 229

Index no. 

Miller, L. J............................. 182-184

Miller, R. D...... . 185

Mirsky, Arthur 67, 186

Mitcham, T. W. 146. 187

Mobley, C. M. 241

Moore, G. W. 188

Moore, R. B. . 189

Moore, R. C.. HO

Moss, C. K..... - 48

Muilenburg, G. A...... .. . .. 190. 191

Mullens, T. E. - 49a, 192

Myers, A. T.... 68

Nininger, R. D. 193

Notestein, F. B............. .....------ 194

Olson, R. H. 206

Page, L. R. . 195-197, 257 

Phair, George ... ----- 198

Phoenix, D. A.-.-------- ---- - 199,242

Poehlmann, E. J. 200

Poole, F. G. -- 201

Post, E. V. -. 17. 104

Prichard, G. E. 264

Proctor, P. D...-. . . -.- 202, 203

Rankama, Kalervo -... -- ---- 204

Ransome, F. L..- -- I36 

Rapaport, Irving ....... . 205, 206, 252

Rasor, C. A. . 207

Redden, J. A. - 197

Redmond, R. L. - 208

Reeside, J. B., Jr.... ... 11. 12, 101

Reinhardt, E. V. 209-211

Reyner, M. L. 212

Robeck, R. C. 213

Rogers, K. J. 214

Rominger, J. F. 85 

Rosenzweig, Abraham 119, 215

Russell, R. T.. 243

Sadlick, Walter . 244

Bahama, T. G. - 204

Schlottman, J. D............... 216

Schnabel, R. W. 17, 217

Sharp, W. N. 218, 219

Shawe, D. R. 220

Sherwood, A. M... 230

Shirley, R. F.... ...... 29

Shoemaker, E. M. 178, 221

Smith, D. K., Jr. 117-119

Smith, J. F., Jr..... 222

Smith, L. B.. 87. 216

Soister, P. E. 254

Staatz, M. H. 223

Steen, C. A... . 224

Stephens, J. G. 67, 226

Stern, T. W.. 227-230

Stewart. J. H.. 226

Stieff, L. R............. 227-230

Stokes, W. L. 87, 231-244

Strobell, J. D., Jr..... ...-- 246

Stugard, Frederick, Jr. . . 22, 246-248 

Swanson, M. A. 29
INDEX 169

Tavelli, J. A..... 

Tennissen, A. C. 

Thaden, R. E... 

Thomas, H. D...

Index no. 

 249 

.... 105 

.... 253 

.... 250

Thompson, M. E....................... 272, 273

Thompson, R. B., Jr........._.___. 273

Tourtelot, H. A........................... 251

Towle. C. C.. ..................... 120, 252

Traver, W. M., Jr....................... 139

Trites, A. F., Jr......................... 18, 253

Troyer, M. L............................. 254

Tschanz, C. M. - --....... . 255, 256

U. S. Atomic Energy Commission.. _ 257 

U. S. Geological Survey ............. 258-262

Vickers, R. C._........................... 263

Vine, J. D. ............................. 264

Volgamore, J. H. _________.___ 137

Walker, G. W.. ........................ 265

Wallace, S. R.. ........................ 254

Walthier, T. N........................... 266

Index no. 

Wantland, Dart ........................ 267, 268

Ward, F. N............................... 171

Waters, A. C. - 269

Weeks, A. D.......-... .............. 270-273

Weir, D. B................................. 274

Weir, G. W. 49a

Wherry, E. T. .......................... 275,276

White, A. M..-._.. ..._____........ 219

White, R. L....... .. .... 154

Williams, F. J..... ... .. 277

Williams, G. A.......... .. 201, 226

Williams, G. O.~. ..................... 278

Wilmarth, V. R... . 18. 279 

Winterhalder, E. .-__.-_.--_. _.-.. 280 

Witkind, I. J............. 281, 282

Wood, H. B.. .....-.... .. 146, 283

Wright, R. J.................... 284, 285

Wyant, D. G. . 286, 287

Zareski, G. K............................. 288

Zeller, H. D.._.._..... . 67, 289

Anonymous ........................ ..... 290
170 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

SUBJECTS

Index no. 

Age determinations _------_ 18, 72, 227-229

Airborne radioactivity survey techniques _____________ 27, 249 

Asphalt and related substances 68, 103, 130, 213

Black ores ........... .............. 116, 118

Botanical methods of prospecting-.__-. 36-38

Cambrian ..----_--_...-----._______._. 13, 14, 225

Carbonaceous material ----------__.... 148

Carnotite ....--.--....---...--..-.. 50, 51, 91, 129

Channels and lenses.. 5, 6, 18, 44, 45, 68, 62, 81,

93, 106, 144, 147, 172, 174, 175, 179,

180, 184, 186, 188, 201, 210, 216, 224,

226, 234, 237, 241, 248, 281-283, 189.

Clay .-...-....----.......--....._. 134, 270, 271

Cofflnite -------_-_--..-.---_.-_--....-_... 230

Colorado Plateau

Distribution of deposits._._...... 75

Geology of areas

Area between Green and Colorado Rivers, Utah_______ 178 

Atkinson Creek quadrangle,

Colorado ..-..------...--...- 174

Bull Canyon quadrangle, Colorado ........ ......-.......... 41

Capitol Reef area, Utah.....--, Ill

Central and south-central Utah 111 

Egnar-Gypsum Valley area,

Colorado ____________ 242 

Gateway area, Utah and Colorado ____.__._______ 248 

Gateway quadrangle, Colorado.. 42 

Green River Desert-Cataract

Canyon region, Utah...... 10

Gypsum Valley, Colorado..--.. 232 

Henry Mountains, Utah. 140 

Kaiparowits region, Utah...... 110

Moab district, Utah __ . 7 

Monument Valley-Navajo Mountain area, Utah.... . 9

Navajo country, Arizona, Utah,

New Mexico ..---.-..-..-... 108 

Pine Mountain quadrangle,

Colorado ......-.--...-..---. 43

Salt Valley anticline, Utah.--. 52 

San Juan country, Utah-.--.. 109 

San Rafael Swell, Utah.... 101, 102

Southeastern Utah-. . . 8

Thompson area, Utah.--... . 242

Utah-Colorado salt dome region 233

Geology of uranium......._._.... 5, 77,

83, 84, 86, 131, 163, 243 

Geophysical prospecting ... .... 23

Ore controls __.....----_.. .. 281

Ore guides .....------..-..---- 86, 210, 274

Origin of deposits....._____ . 71, 77,

78, 82-84, 115,117, 129, 163, 194 

Structure --_... ..- 151, 152, 173, 221 

Tectonic map 173

Copper

Index no. 

.................... 9, 18, 21.

45, 58, 60, 69, 73, 77, 95,

98, 184. 185, 222, 246, 287

Devonian ._..........--.-.--.-....---.- 159, 266

Deposits, distribution of, maps

'Colorado Plateau .... . 75

Gateway area, Colorado and Utah 243 

Missouri .................... . ..- 190

New Mexico .. --.. 1 

Pumpkin Buttes, Wyoming 254 

Southwestern Colorado and southeastern Utah .-....-.-.---.-.-- 79

United States -....--..--.----.-.-..-- 217

Eocene ___-----___ 14, 21, 

53, 121, 164, 167, 218, 219, 250, 254

Exploration (also see Prospecting)

Drilling ............ 58, 81, 86, 139, 150, 182

General ........... .......... 81, 160, 181

Polar Mesa, Utah........ ......... 208

Shinarump channels 283 

Silver Reef district, Utah.-.-... 200 

White Canyon area, Utah..-. 58, 150, 182

Geobotanical prospecting. ( see under

Botanical methods)

Geochemical prospecting ... 57, 88, 171 

Geochemistry of uranium ...... 204

Geologic prospecting . 196, 257 

Geophysical prospecting

Bull Canyon, Colo...-..--.---.-. 267 

Calamity Mesa, Colo.____.____. 66 

Colorado Plateau .....-..----.. 23

Edgemont district, South Dakota..-. 124 

Grants district, New Mexico 48 

King Tutt Mesa, Ariz..... __ 267

Long Park, Colo. ----- .... .. 56

Methods

Airborne radioactivity surveys 27,

249 

Drill-hole logging ..--......---. 47

Electrical ..--......-..-_... 23, 267

Potential drop ratio.__.. 267 

Resistivity ___..... 56, 267

Seismic ----- .. .. 23, 268

Monument Valley, Arizona 268

Outlaw Mesa, Colorado. _ 56

Gold ..._ . 131

Isotopes _ _..-. .-... - 39, 72, 227-229 

Limestone .... 30, 67, 70, 92, 120, 132, 205. 252

Milling ...._ . . .. .. 2, 141, 153, 160 

Mineralogy (see specific mineral)

Identification and occurrence of

uranium and vanadium minerals 190,

272

Mineral associations 118, 273 

Ore textures ..................... 82-84,183
INDEX 171

Index no 

Mineralogy (Continued)

Paragenetic studies _________ 98, 162 

Radioactive iron oxides....._._ 170

Schroeckingerite .______ 195, 258, 286 

Synthesis of uranium minerals__ 11 

Weathering effects _____.____ 98 

Mining .................. 3, 31, 32, 141, 155, 16C

Miocene __---..-..-. 92, 121, 165, 264, 265, 29C 

Mississippian __--.-----.-..____ 191, 266

Molybdenum ................._.__.-- 131

Oligocene ........................ 100, 121, 188

Ore controls

Colorado Plateau _.._.______ 281 

Edgemont district, South Dakota_- 13, 17 

Ore guides (also see Prospecting and 

Exploration) 

Colorado Plateau -....--.-... 86, 210, 274

Edgemont district, South Dakota__ 13

10^ 

Monument Valley, Arizona and

Utah ............................ 18;

Ore textures --.--------.--..-...---..- 82-84, 183

Origin of deposits 

Epigenetic

General _._.--._----.--_.--._. 81, 84

133, 134, 144, 145, 175, 183 

220, 227-229, 264, 287. 

Metals derived from black shale 191

276 

Metals derived from deep-seated

source .. ..__ 18, 62, 

71, 127, 149, 162, 177, 205, 

224, 247, 269, 287.

Metals derived from petroleum 103 

Metals derived from surrounding rocks ._...__--.__ 31, 34, 

46, 115, 135, 189, 194, 219, 

252, 258, 276. 

Metals derived from volcanic

ash ........................ 16,

115, 161, 164, 167, 168, 188. 202 

Syngenetic

General .... . ... 163, 165, 285, 287

Metals deposited mechanically.. 5, 

6, 90, 278

Metals deposited biologically 77, 90 

Metals deposited chemically 114, 

120, 129-131 

Metals deposited during diagenesis . ......--...-..-- 82,

83, 85, 233, 234, 289

Petroliferous rocks ..----------.. 68

Petrology .......... 17, 24, 40, 53, 107, 145, 194

Pitchblende ........--....-..---.. 198

Pliocene 55 

Processing of ores 2, 141, 153, 160 

Prospecting

Airborne radioactivity survey techniques ............ 37, 249

Index no. 

Prospecting (Continued)

Botanical methods __________ 36-38 

General .................. 178, 193, 203, 285

Geochemical methods ..._ 57, 58, 88, 171 

Geologic methods .........__ 196, 257

Geophysical methods (see Geophysical prospecting)

Radioactive iron oxides.__.._..__ 170 

Radium .............................. 46, 51, 131

Resources ___._------ ____ 33, 73, 123

Roll ore bodies.--.------_______.__ 220

Schroeckingerite ____ 195, 258, 286 

Sedimentary features

Salt Wash member ... __ 24,

147, 172, 192, 235-238, 244

Shinarump conglomerate ... 175

Transmissivity ---------- -._ 146, 199

Sedimentary patterns and ores.-..---. 24, 238 

Selenium ............... .. 36-38, 95, 264

Shales __..-.__.--------.----.... 93, 181, 191

Silver ............-. ..... 77, 131, 246, 247

Source of metals.--------.-_------------ 161

Stratigraphy

Carrizo Mountains ....-_.......... 245

Central and south-central Utah.... Ill

Jurassic formations .-.--------. . 11, 12

Morrison formation .__ 49a, 49b, 231 

Salt Wash member.. . .... 238

San Rafael Swell. ............ 101, 102

Southeastern Utah ..-..-.--.---.- 239 

Triassic formations ... . 226 

Structure

Influence on uranium deposits.. 17,

151, 152

Colorado Plateau (see Colorado Plateau, geology) ........151, 152, 173, 221

Lucero uplift 65 

Southeastern Utah .-..-...-.--...-.. 8, 221 

Tectonic map of Colorado Plateau.. 173 

Todilto limestone .....-.-----..----.- 67

Synthesis of uranium minerals.. 117

Tectonic map of the Colorado Plateau.. 173 

Thermodynamic relations

Uranium oxides . . .. ----- 97

Vanadium oxides .. -.- 96 

Thorium .._____... ......... 4, 39, 196, 257

Transmissivity .-... .. ......... 146, 199

Tuffs and tuffaceous sediments 55, 133

United States, distribution of deposits 217 

Uranium minerals (see specific mineral) 

Uraninite ......................... 148, 205, 215

Uravan mineral belt ... .... 86

Volcanic debris . . ------ 270

Water, uranium content . _._ 5?! 88
172 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

GEOGRAPHIC AREAS

Index no. 

Arizona

Apache County (also see Monument 

Valley area)

Black Mesa ... 40 

Carrizo Mountains __._____ 35, 

147, 233, 235, 244, 245 

Chuska Mountains ..______ 172 

Cove Mesa ---....-..-..--..... 147, 157

Defiance uplift -...._______ 125

King Tutt Mesa.................. 267

Einusta Mesa ..._......___ 157

Lukachukai Mountains ---... 179, 180 

Mesa V -.--.-.......-...... 156

Mesa VI .................... 66

Mesa VII .............._. 158

Red Rock district................ 157

Coconino 'County

Cameron area -.-....-___.. 144, 277 

Hualapai Indian Reservation.. 185 

Ridenour mine ..____.._.... 185

Gila County

Red Bluff prospect--..-.----._ 150

Maricopa County

Aguila area .......___.... 134, 135

Mohave County

Hualapai Indian Reservation.. 185

Monument Valley area_____._ 5, 45, 

106, 108, 144, 187, 211, 268, 281-283 

Copper Canyon _______.. 211 

Hoskinninni Mesa --...----... 106 

Hunts Mesa ________ 45 

Monument No. 1 mine...___. 5, 

Monument No. 2 mine._____ 5 

Nokai Mesa -.-....._......... 106

Navajo County (also see Monument 

Valley area) 

Black Mesa ................__ 40

California

Kern County

Kern Canyon __....______ 290 

Rosamond Prospect _____ 265, 290 

Taft-McKittrick area ._------ 290

Olancha area ....._________ 55

Colorado

El Paso County

Mike Doyle prospect__.___ 20

Garneld County

Garfleld mine ...._............. 87

Rifle mine ..-.-...-..._....... 32, 87

Grand County

Lucky Strike claims--...-...... 21

Middle Park (Troublesome

Creek) area _________ 216

Mesa County

Gateway area ._________ 243 

Gateway quadrangle . 42 

Pine Mountain quadrangle 43 

Uravan mineral belt_____... 86

Moffat County

Skull Creek area..,.,,..,. 21, 95, 189

Index no. 

Colorado (Continued) 

Montrose County

Atkinson Creek quadrangle 174 

Bull Canyon quadrangle 41 

La Sal Creek............. . 135

Long Park . 46

Paradox Valley ............ 50, 51, 90

Roc Creek .._ - . - 155 

Uravan district .... .--- 24

Uravan mineral belt......------ 86

Wray Mesa ........ .. . 288

Paradox Valley 50, 51, 90

Park County

Garo area 279

Shirley May mine...... 279

Rio Blanco County

Meeker area --------- - 94

Routt County

Skull Creek area. - - 21, 95, 189 

San Miguel County

Bull Canyon quadrangle 41 

Egnar-Gypsum Valley area 242 

Graysill mine . 5 

Gypsum Valley area _ .. 86, 232 

Placerville area 5, 85, 

90, 127, 131, 135

Uravan mineral belt. - 86 

Utah-Colorado salt dome region.... 232

Colorado Plateau ....- 2, 5,

23, 36, 49a, 49b, 56, 63, 73, 75, 80-84, 

90, 96-98, 115, 118, 139, 144-146, 148. 

160, 173, 176, 177, 181, 183, 192, 194, 

201, 210, 215, 217, 220, 226, 229, 231, 

236, 249, 267, 272-274, 283, 285, 290

Missouri

Franklin County--. 190

Ste. Genevi«ve County. . 190, 191

Montana

Big Horn Basin. 14

Nevada

Clark County 15, 16, 169

Arden ----- - . 169

Erie 169

Goodsprings 169 

Las Vegas 169

Sloan 169

Sutor 169

Esmeralda County 76 

Tonopah area - 65 

Humboldt County

Virgin Valley opal district 55. 

169, 223

Lander County 55, 76 

Lincoln County 55 

Lyon County -------- 55

New Jersey

Hunterdon County - .- - 266
INDEX 173

Index no. 

New Mexico

Catron County

Datil area 112, 113

Grants district

Becenti mine . .. -. -. 93 

Dakota mine .. 

Diamond No. 2 mine ...- .. 98 

Hogback No. 4 mine .... 

Jackpile mine --_ .. _ 

Lueero uplift, structure. . 65 

Sanastee area....._ ....---.. 64 

Section 9 mine..__..__..__ 141 

Silver Spur mine_________ 93 

Small Stake mine... 1. . 93 

Woodrow mine __..._ -. 

Zuni uplift . . 30, 67, 99, 206

McKinley County (see Grants 

district)

Mora County

Coyote district __.__.___ 289 

Guadalupita area ..--__ 255, 256

Nacimiento uplift

Butler mine . 93

San Juan County

Carrizo Mountains______ 233, 245 

Sanastee area . 64 

San Juan Basin . 40

Santa Fe County

Cerrillos district .... . . 112 

Glorieta district . 112

Socorro County__.__._____ 112, 113

Valencia County (see Grants 

district)

Oklahoma

Cotton County.. ... ... 19, 28, 44 

Jefferson County. .. ... 19, 28, 44 

Noble County . . . 28 

Osage County .. . . 28 

Pawnee County ._ .. - .. 28 

Payne County . . 28 

Tillman County ._ __............ 19

Pennsylvania

Bucks County___ _ - 266

Carbon County ___._ 159, 266, 275, 276

Jim Thorp area - 266

South Dakota

Black Hills (also see Fall River

County) .... .-.. 76, 104 

Northern Black Hills..- 263 

Southern Black Hills (see Fall 

River County)

Butte County

Belle Forche area . . 263

Fall River County

Craven Canyon 197

Edgemont district _... .. 13,

17, 104, 124, 197

Gould lease .--...... ....... 124

Harding County

Cedar Canyon 100

Pennington County

White River Badlands. .. 188 

Badlands __ 189

Index no.

Karnes County .___....____ 76

Utah

Eastern part ..____________ 78, 80 

Emery County

Area southwest of Green River 26, 

34, 126, 190

Brown Throne group ___ 212 

Clifford Smith claim.. 212 

Dalton group.._____.___ 212 

Dirty Devil group... .. 212 

Dirty Devil No. 6 mine __ 6 

Dolly group..... .. ..._ 212

Green River Desert-Cataract

Canyon area . . 12 

Green Vein group.__ __ 212 

Hard Pan group___...___ 212 

Hertz No. 1 claim.. 212 

Hot Shot mine.___ _._ 5 

Little Wild Horse Mesa. 137 

Lone Tree.. ......_ ___ 212

Pay Day group 212 

San Rafael Swell (see Temple

Mountain) ____.___ 68, 73, 

101-104, 117, 212

South Fork claim_________ 212

Temple Mountain ._ .. 10,

34, 70, 117, 130, 131, 144, 154, 213

Wickiup claim ..._ 212

Garneld County

Circle Cliffs 5, 68, 69, 283

Henry Mountains ..._ 29, 34, 140, 209 

Trachyte district - 29 

Yellow Jacket claim 5 

Grand County

Gateway district «__ 86, 243

Polar Mesa . 52, 208

Moab district.. 7

Richardson area. 26, 34

Salt Valley anticline... 52

Seven Mile Canyon 74

Shinarump No. 1 mine 74, 227

Thompsons district 36, 52,

189, 234, 240, 241

TJravan mineral belt 86 

Kane County

Bulloch group 22 

Kaiparowits region.... .. 110, 111

Northeastern 21 

Salt Valley anticline___...... 52

San Juan County

Big Buck mine 61

Big Indian Wash-Lisbon Valley 61,

73, 119. 142-144, 224, 240

Mi Vida mine 61, 119, 224

B landing district____ 237

"C" group 59

Gray Dawn mine__ 207

Hoskinninni Mesa____ 106

La Sal Creek ......... 185, 207

Gray Dawn mine__ 207 

La Sal Mountains 34 

Lisbon Valley (see Big Indian 

Wash)
174 SELECTED BIBLIOGRAPHIES OF URANIUM GEOLOGY

Index no. 

Utah (Continued)

Lockhart Canyon-Indian Creek 60 

Mi Vida mine. ........ 61, 119, 224

Moab district............__ 7

Montezuma Canyon.-...__ _ 278 

Monument Valley ..------...-.. 5, 8,

73, 106, 108, 144, 283 

Hoskinninni Mesa..--..__ 106 

Nokai Mesa_....._...-.-. 106

Nokai Mesa _._---------__ 106

Purple Paint claim.--..- ...-. 61 

Skyline mine .. 5 

Small Fry claim................ 61

Whirlwind mine ................ 5

White Canyon ........-------. 18, 34,

58, 62, 73, 117, 144, 150, 182, 184, 

227, 253, 283.

Happy Jack mine .. 18,

62, 181, 184, 227

Wray Mesa ...-..-.....--....--.. 288

Southeastern .. ................ 8,77-

80, 83, 84, 163, 221, 239, 240 

Uintah County

Bonniebell claim --.-----..--..-- 21

Snow claims -------------------- 21

Washington 'County

Chloride Chief claim.---.-...-.. 246 

Silver Point.....-----.-.-.--..... 246

Silver Reef (Harrisburg) district .............. 69. 200, 202, 246, 248

Wayne County

Capitol Reef area..-...--.-__ 68, 69,

138, 222

Fruita area -------------- 34

Henry Mountains ..-..--. 34, 140, 209 

Oyler mine ....-----.--..--....-. 138

Virginia 266

Wyoming

Bighorn County

Bighorn Basin .. 14

Black Hills (also see South Dakota,

Black Hills) .............. 76, 121, 250

Aladdin area .-..--- -- 105 

Carlile area ... 25

Index no. 

Wyoming (Continued)

Campbell County

Pumpkin Buttes _-__-___ 121. 

164, 218, 219, 250, 254

Carbon County

Baggs area (Poison Basin area) 250,

264

Miller Hill area.-.. ... 165, 250 

Saratoga area. .. 250

Converse County ..--..... .. ... 121

Crook County

Aladdin area ...... .... 105

Black Hills ..-..... ........... 76

Carlile area .-. - ... 25

Fremont County

Crooks Gap .................. 121, 225

Gas Hills _.. 121, 167, 250 

Green Mountains -------------- 122

Lysite-McComb area . -... 166, 250 

Oregon Buttes 280

Owl Creek Mountains_______ 121 

Wind River Basin............ 122, 251

Great Divide Basin__________ 122 

Lost Creek-Wamsutter-Red

Desert 195, 258, 286

Green Mountains . 122

Green River Basin_____._._ 280

Johnson County (also see Powder River Basin) 

Mayoworth area --------- 168, 250

Natrona County

Gas Hills area.... -. 121, 167, 250

Niobrara County

Lance Creek area.. . 121

Powder River Basin .____ 53, 54, 122

Converse County area...._... 121

Pumpkin Buttes area . 121,

164, 218, 219, 250, 254

Red Desert area.......--..-.. 195, 258, 286

Rock Springs uplift.. ____.. 280

Sweetwater County

Lost Creek-Wamsutter-Red

Desert . . 195, 258, 289 

Rock Springs uplift- . 280

Washakie Basin ....... . . ... 122
INDEX 175

FORMATIONS

Index no. 

Baca formation.... ..... 113

Bidahochi formation .-.-..----....--.--. 92

Browns Park formation__. 92, 121, 164, 264 

Brule formation _..-.._--- .. 188 

Brushy Basin (see Morrison formation) 

Cambrian, undifferentiated ....... . 225

Catskill formation __ _______ 159, 266

Chadron formation ________.____ 188

Chinle formation -. .. 18, 61,

69, 74, 84, 108, 119, 125, 138, 142-144, 176,

200, 202, 213, 214, 224, 226, 246-248, 277.

Chugwater formation .................... 14

Coconino sandstone .-... .... 154

Coso Lake beds .---.-.. 55 

Cretaceous, undifferentiated . 231 

Curtis formation ____........ __ 21, 40

Cutler formation .............. 60, 61, 142, 143

Dakota group _________.___ 93, 94, 186 

Deadwood formation _...-. . 13 

Dripping Springs quarteite .. 149 

Entrada sandstone .--. 5, 21, 

32, 75, 77, 78, 84, 85, 87, 89, 90, 127, 

131, 135, 163, 176, 287. 

Fall River sandstone (see Inyan Kara

group)

Flathead sandstone ______ __ 14 

Frontier formation __. ..... . 14

Fuson shale (see Inyan Kara group) 

Garber formation ______............. 28, 44

Green River formation.- . . 281 

Inyan Kara group (includes Lakota,

Fuson, and Fall River formations).... 13,

17, 25, 76, 104, 105, 121, 

124, 197, 250, 263.

Jurassic, undifferentiated 11, 

12, 26, 49a, 49b, 206

Kaibab limestone __..._________ 15, 92 

Lakota formation (see Inyan Kara

group)

Maroon formation -.-_..-_.._..__ 280 

Mesaverde formation ...... 14, 21, 40, 112, 113

Minnelusa formation ._..____ __ 18 

Moenkopi formation _...-. 6, 18, 69, 187, 253 

Morrison-CIoverly formation ............ 14

Index no.

Morrison formation (includes Salt 

Wash, Recapture, Westwater Canyon, 

and Brushy Basin members) 3, 7, 

20, 24, 29, 31, 35, 37, 41-43, 46, 49a, 

49b, 51, 52, 63, 64, 66, 75, 77-80, 84, 

85, 87, 126, 131, 135, 137, 139-141, 147. 

156-158, 163, 172, 174, 176, 179-181, 189, 

192, 199, 205-209, 220, 231, 233-239, 241, 

243, 244, 252, 269-271, 274, 285, 287, 288.

Panaca formation ____ _______ 65 

Pierre shale __...._____............ 13

Pottsville formation _..--. 159, 266, 275, 276 

Price sandstone - 266 

Recapture member (see Morrison formation) 

Rosamond formation ........ 265, 290

Salt Wash member (see Morrison

formation) 

San Andres limestone-...........-.-...-. 92

Sangre de Cristo formation_... 255, 256, 289 

San Rafael group ............ 231

Shinarump conglomerate . ....- . 5, 6,

9, 18, 45, 58, 59, 62, 69, 70, 73, 75, 77,

78, 80, 84, 103, 106-108, 114, 130, 131,

138, 144, 150, 175, 176, 182, 184, 187,

211, 212, 222, 226, 253, 277, 281-283.

Spergen limestone 190

Stockton formation ..__ ....... 266

Summerville formation ... . 22 

Sundance formation __ ...... 168, 250

Supai formation -- .. 185 

Tepee Trail (?) formation. ...... 166

Thermopolis shale .. 167

Todilto limestone _____________ 30,

87, 67, 70, 75, 92, 120, 141, 205, 252

Troublesome formation .. 215

TJinta formation 21

Wasatch formation ...- 14,

53, 121, 164, 218, 219, 250, 254

Westwater Canyon (see Morrison

formation) 

White River group (includes Brule and

Chadron formations) .......... 100, 121

Wind River formation............ 121, 167, 250

Wingate formation .. 130

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