STUDIES RELATED TO WILDERNESS

DU NOIR ADDITION, 

WASHAKIE WILDERNESS, 

WYOMING

GEOLOGICAL SURVEY BULLETIN 1472 geh 3

Mineral Resources of the 

Du Noir Addition, 

Washakie Wilderness, 

Fremont County, Wyoming

By H. J. PROSTKA and J. C. ANTWEILER, U.S. GEOLOGICAL SURVEY, and 

C. L. BIENIEWSKI, U.S. BUREAU OF MINES

With a section on AEROMAGNETIC SURVEY

By M. DEAN KLEINKOPF, U.S. GEOLOGICAL SURVEY

STUDIES RELATED TO WILDERNESS

GEOLOGICAL SURVEY BULLETIN 1472

An evaluation of the mineral 

potential of the area

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1979
UNITED STATES DEPARTMENT OF THE INTERIOR 

CECIL D. ANDRUS, Secretary

GEOLOGICAL SURVEY 

H. William Menard, Director

Library of Congress Cataloging in Publication Data

Prostka, Harold J.

Mineral resources of the Du Noir Addition, Washakie Wilderness, Fremont County, Wyoming.

(Studies related to wilderness study areas)

(Geological Survey Bulletin 1472)

Bibliography: p. 35

1. Mines and mineral resources Wyoming Washakie Wilderness. 2. Washakie Wilderness, Wyo.

I. Antweiler, J. C., joint author. II. Bieniewski, Carl L., joint author. III. Title. IV. Series.

V. Series: United States Geological Survey Bulletin 1472.

QE75.B9 no. 1472 [TN24.W8] 557.3'08s [S53'.09787'63]

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

Washington, D.C. 20402 

Stock Number 024-001-03250-3
STUDIES RELATED TO WILDERNESS

In accordance with the provisions of the Wilderness Act 

(Public Law 88-577, September 3, 1964) and the Joint Conference Report on Senate Bill 4, 88th Congress, the U.S. 

Geological Survey and U.S. Bureau of Mines have been conducting mineral surveys of wilderness and primitive areas. 

Studies and reports of all primitive areas have been completed. Areas officially designated as "wilderness," "wild," or 

"canoe" when the Act was passed were incorporated into the 

National Wilderness Preservation System, and some of them 

are presently being studied. The Act provided that areas 

under consideration for wilderness designation should be 

studied for suitability for incorporation into the Wilderness 

System. The mineral surveys constitute one aspect of the 

suitability studies. This report discusses the results of a 

mineral survey of some national forest lands in the Du Noir 

area, Wyoming, that is being considered for addition to the 

Washakie Wilderness. The area studied is in northern Fremont County, northwestern Wyoming.

CONTENTS

Page

Summary ............................................................... 1

Introduction............................................................. 1

Previous studies ..................................................... 4

Present investigations ................................................ 4

Acknowledgments ...................................;............... 5

Geology ................................................................. 6

Permian Phosphoria Formation ....................................... 9

Cenozoic rocks ....................................................... 9

Indian Meadows Formation ....................................... 10

Absaroka Volcanic Supergroup .................................... 10

Tepee Trail Formation ........................................ 11

Wiggins Formation ........................................... 12

Pliocene basalt ................................................... 12

Pliocene(?) intrusive rocks ......................................... 13

Surficial deposits ................................................. 13

Structure ............................................................ 14

Aeromagnetic survey, by M. Dean Kleinkopf ........................... 14

Mineral resources ........................................................ 15

Setting .............................................................. 15

Mining claims and mineral production history .......................... 16

Geochemical sampling program and analytical methods ................. 17

Analytical results and resource potential............................... 21

Metallic minerals ................................................. 21

Coal, phosphate, and limestone .................................... 30

Oil and gas ....................................................... 32

Building stone, gravel, and sand ................................... 33

Geothermal resource potential......................................... 34

Conclusions ............................................................. 34

References cited ......................................................... 34

ILLUSTRATIONS

Page

FIGURE 1. Map showing location of Du Noir Addition, Washakie Wilderness,

Wyoming ................................................... 2

2. Photograph of Pinnacle Buttes and Kisinger Lakes ............... 3

3. Photograph of the Ramshorn and Frozen Lake Creek ............. 3

4. Geologic map of Du Noir Addition ............................... 6

5. Aeromagnetic map of north half of Du Noir Addition and vicinity .. 15

6. Map showing location of mining claims and U.S. Bureau of Mines

sample localities ............................................. 18

7. Map showing U.S. Geological Survey sample localities ............ 19

8. Map showing location of oil and gas leases ....................... 33
VI

TABLES

Page

TABLE 1. Paleozoic rocks exposed in the Du Noir Addition.................. 8

2. Estimated crustal abundance and minimum values used for computer

retrieval of 15 elements ....................................... 21

3. Selected analyses of the U.S. Geological Survey samples from the

Du Noir Addition and vicinity................................. 22

4. Analyses of U.S. Bureau of Mines samples from the Du Noir Addition and vicinity ............................................. 26

5. 'Summary of analyses for selected elements in Eocene carbonaceous

shales near the Du Noir Addition .............................. 29

6. Selected analyses of bedrock samples from the Phosphoria Formation, Du Noir region, Wyoming................................ 31

7. Chemical analyses of limestone from the Madison Limestone ...... 32
STUDIES RELATED TO WILDERNESS

MINERAL RESOURCES OF THE DU NOIR

ADDITION, WASHAKIE WILDERNESS,

FREMONT COUNTY, WYOMING

By H. J. PROSTKA and J. C. ANTWEILER, U.S. Geological Survey 

and C. L. BlENIEWSKI, U.S. Bureau of Mines

SUMMARY

The Du Noir Addition to the Washakie Wilderness consists of 34,200 acres (13,840 

hectares) of scenic mountainous terrain that adjoins the Teton Wilderness and 

Washakie Wilderness. The area was studied in 1973 by the U.S. Geological Survey 

and U.S. Bureau of Mines to evaluate its mineral, fuel, and geothermal energy potential. This evaluation is based on a search of the geologic literature, claim and production records, and fieldwork including mapping, inspection of claims and prospects, interpretation of aeromagnetic maps, and analyses of bedrock and stream-sediment 

samples.

Flat-lying Eocene volcaniclastic rocks of the Absaroka volcanic field are exposed in 

about two-thirds of the Du Noir Addition. These volcanics unconformably overlie the 

deeply eroded, northwest-trending Du Noir anticline in which Paleozoic marine strata 

of Devonian through Permian age are exposed. Of lesser importance areally are small 

deposits of Eocene nonvolcanic conglomerate, and basaltic intrusive and extrusive 

rocks of late Pliocene and possibly younger age.

The results of this study indicate that the mineral, fuel, and geothermal potential of 

the Du Noir Addition are minimal. Low-grade copper-molybdenum mineralization occurs outside the addition, associated with intrusive rocks, but no indications of alteration or mineralization were found within the study area. Anomalous, but not 

economically important, concentrations of molybdenum and uranium were found in 

Permian and Eocene carbonaceous shales. Phosphate rock in the Phosphoria Formation occurs in beds too thin to constitute a resource. Large amounts of very pure 

limestone are present in the Madison Limestone, but equally pure limestone, much 

closer to transportation facilities, is found throughout this part of Wyoming. That 

part of the Du Noir anticline in the addition is too deeply eroded to be a likely reservoir of oil and gas. Present data indicate a low potential for geothermal energy in or 

near the addition.

INTRODUCTION

The Du Noir Addition is an area of scenic mountainous terrain and 

broad forested valleys located along the precipitous southern margin 

of the Absaroka Range in Shoshone National Forest, Fremont County, northwestern Wyoming (fig. 1). Adjoining it on the north and
DU NOIR ADDITION, WASHAKIE WILDERNESS, WYOMING

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FIGURE 1. Location of the Du Noir Addition, Washakie Wilderness, Wyoming.

northeast are the Teton and Washakie Wilderness areas. To the 

south, the Du Noir Addition faces the northwestern end of the Wind 

River Basin, and beyond it, on the distant skyline, the Wind River 

Range. It encompasses an area of 34,200 acres (13,840 hectares) that 

includes the upper drainage basin of Du Noir Creek and the encircling 

spectacular high divides and plateau remnants. Pinnacle Buttes (fig. 

2) on the west, Du Noir Butte and Crescent Mountain to the north, 

and The Ramshorn (fig. 3) on the east are the principal high mountains. Elevations range from more than 11,300 feet (3,400 m) along 

the divide to less than 7,600 feet (2,300 m) in the valley of Du Noir 

Creek. 1 A small glacier, the Du Noir glacier, is on the east side of Coffin Butte. The rugged outlines of the mountains contrast markedly 

with the broad rolling forested valleys and their clear sparkling 

streams, charming meadows, and numerous small lakes.

Foot and horse trails follow the major valleys and connect with the 

well-used trail systems in the adjacent wilderness areas, but the

'Until recently this has been called Du Noir River and is so indicated on U.S. Geological Survey base maps 

through 1963 and on W. R. Reefer's 1955 and 1957 maps.
INTRODUCTION

FIGURE 2. Pinnacle Buttes and Kisinger Lakes seen from the southeast. Rugged 

Pinnacle Buttes are carved from flat-lying volcanic sediments of Wiggins Formation; forested ridge in foreground is underlain by Tepee Trail Formation; Kisinger 

Lakes are in depressions of extensive landslide deposits.

FIGURE 3. The Ramshorn and Frozen Lake Creek seen from the southwest. Cliffs are 

flat-lying beds of Wiggins Formation; Tepee Trail Formation is hidden in trees near 

base of cliffs, and glacial-scoured rocks in foreground are Paleozoic strata in the 

northeast limb of the Du Noir anticline.
4 DU NOIR ADDITION, WASHAKIE WILDERNESS, WYOMING

higher parts of the area are accessible only by mountain-climbing 

techniques. There are about 10 miles (16 km) of roads in the southcentral part of the addition, but most of them are closed to motorized 

vehicles. The nearest town is Dubois, Wyo., about 15 miles (24 km) to 

the southeast; many guest ranches and hotels are nearby. U.S. 

Highway 26-287 is just to the southwest, and from it one can see 

many spectacular views of the study area.

Fieldwork for this study was done by the U.S. Geological Survey 

and U.S. Bureau of Mines during June, July, and August of 1973.

PREVIOUS STUDIES

A comprehensive study of the geology of the Du Noir area was 

done by Keefer (1955, 1957); it contains a summary of the earlier 

geologic work in the region, presents detailed descriptions and interpretations of nearly all rock units present in the Du Noir Addition, 

and includes a geologic map that covers the eastern half of the study 

area. The descriptions of the prevolcanic rocks in the present report 

are taken from Keefer. A report on the stratigraphy and mineral 

resources of Permian rocks in western Wyoming (Sheldon, 1963) includes Permian rocks in the Du Noir area. A study of the mineral 

potential of the Stratified Primitive Area, now part of the Washakie 

Wilderness (Ketner and others, 1966), gives additional information, 

especially on the volcanics, as does a paper on the regional 

stratigraphy of the Absaroka volcanic field (Smedes and Prostka, 

1972). A paper by Blackstone (1966) describes the Pliocene basaltic 

volcano on Crescent Mountain. A map by Rohrer (1966) shows the 

geology of the southwestern part of the Du Noir Addition, and a 

paper by Rohrer and Obradovich (1969) deals with the Eocene 

volcanic rocks and their ages.

PRESENT INVESTIGATIONS

The purpose of the present study was to map the geology and to 

evaluate the mineral and geothermal-energy potential of the Du Noir 

Addition. These objectives were met through geologic studies that 

included preparation of a reconnaissance geologic map, through a 

geochemical sampling program, through interpretation of 

aeromagnetic data, and by searching for records of mineral production or mining claims. This report of our evaluation is the combined 

effort of the U.S. Geological Survey and U.S. Bureau of Mines. 

Harold J. Prostka and John C. Antweiler, U.S. Geological Survey, 

assisted by Gregory Lee and David Phelps, collected bedrock and 

stream-sediment samples and pan concentrates for the geochemical
INTRODUCTION 5

analyses. Prostka did most of the bedrock sampling and geologic 

mapping. The U.S. Geological Survey fieldwork was done mostly in 

July and August 1973, using a helicopter almost daily to facilitate 

access.

The published map of Keefer (1955) and that of Rohrer (1966) were 

incorporated in our map (fig. 4) with a minimum of remapping; 

however, these areas were thoroughly sampled by us. A U.S. 

Geological Survey mobile field laboratory, located nearby, performed 

the chemical and spectrographic analyses and returned the analytical 

results to us in a matter of days.

Fieldwork by Carl L. Bieniewski of the U.S. Bureau of Mines, conducted during June and July 1973, consisted of reconnaissance in and 

around the addition and sampling of bedrock units and stream 

sediments. Companies known to have been interested in minerals 

near the addition were contacted.

A search of the records of Fremont, Park, and Teton Counties was 

made to determine whether any mining claims had been located in the 

Du Noir Addition. Land-status records of the Bureau of Land 

Management in Cheyenne, Wyo., were examined for mineral leases 

and for patented mining claims. Forest Service personnel and Dan 

Miller, Wyoming State Geologist, were contacted for knowledge of 

any mineralization or prospecting activities in and near the addition.

ACKNOWLEDGMENTS

Appreciation is expressed to Forest Service and Bureau of Land 

Management personnel for their cooperation, and special thanks are 

extended to John Butruille, Dubois District Ranger for the Shoshone 

National Forest. Percy Yarborough permitted us to use private roads 

through Retlaw Enterprises ranchlands to the National Forest 

boundary, and Barry Horn allowed us to use the Brooks Lake Lodge 

as a base of operations.

U.S. Geological Survey field analyses were provided by John Viets, 

G. W. Day, and R. T. Hopkins. Other Geological Survey analyses 

were made in Denver. Computer programming and retrieval of data 

were handled by L. R. Wilch and Ricke Smith. Geologic field help was 

provided for the Geological Survey investigation by Gregory Lee, 

David Phelps, and John Antweiler III, and for the Bureau of Mines 

by John M. Hoppe.

We are particularly grateful to J. D. Love, who spent several days 

in the field with us and contributed to the work through his vast 

geological knowledge of the area, and to W. R. Keefer, who prepared a 

geologic map of the southern part of the area in 1955 and spent two 

days in the field with us at the beginning of the Geological Survey 

investigation.
DU NOIR ADDITION, WASHAKIE WILDERNESS, WYOMING

I09°82'30"

01234 KILOMETERS 

CONTOUR INTERVAL 200 FEET

FIGURE 4. Geologic map of the Du Noir Addition. Base from AMS 1:250,000 Thermopolis (1955).

State and county officials, local residents, and company officials of 

Gulf Minerals Company and Timberline Minerals cooperated with us 

and furnished information of value.

GEOLOGY

The Du Noir Addition (fig. 4) lies along the south margin of the Absaroka Range, a highly dissected volcanic plateau made up primarily 

of nearly flat-lying andesitic volcanic rocks of Eocene age. Partly exposed along the abrupt erosional edge of this plateau is the westnorthwest-trending Washakie Range, consisting of Precambrian, 

Paleozoic, and Mesozoic rocks that were highly deformed during the 

Laramide orogeny and were later buried by the volcanics. Within the 

Du Noir Addition, middle and upper Paleozoic marine sedimentary 

rocks are exposed in about one-third of the area, occurring mainly in 

the deeply eroded northwest-trending Du Noir anticline. A small area 

of Devonian rocks is present on the axial part of the fold, and a larger
Qa 01

Tb

GEOLOGY

CORRELATION OF MAP UNITS

\ Holocene and ~\ QUATER(V|ARY 

J Pleistocene J

Unconformity

Pilocenel?) and 

Pliocene

Eocene

Unconformity

Pp

Pt

PMa

Mm

Dd

> TERTIARY

PERMIAN 

PENNSYLVANIAN

MISSISSIPPIAN 

DEVONIAN

DESCRIPTION OF MAP UNITS 

Qa ALLUVIUM (HOLOCENE AND PLEISTOCENE) Unconsolidated

deposits of sand, gravel, and silt along present streams 

LANDSLIDE AND GLACIAL DEPOSITS (HOLOCENE AND 

Ql PLEISTOCENE) Unconsolidated poorly sorted deposits of 

blocks and boulders, generally with hummocky surfaces; includes talus and small lacustrine deposits

Tb BASALT (PLIOCENE)?) AND PLIOCENE) Lava flows, dikes, and 

a scoria-spatter cone of dark- to medium-gray aphanitic basalt 

and basaltic andesite

Twi WIGGINS FORMATION (EOCENE) Light- to medium-gray and 

brown andesitic well-bedded coarse volcanic mudflow and 

fluvial breccia and conglomerate, mudstone, and airfall tuff 

Tt TEPEE TRAIL FORMATION (EOCENE) Medium-brown, green, 

and buff andesitic well-bedded medium- to fine-grained volcanic sandstone, siltstone, breccia, conglomerate, and tuff 

Tim INDIAN MEADOWS FORMATION (EOCENE) Red massive conglomerate consisting of clasts of Paleozoic rock in a sandy 

matrix

Pp PHOSPHORIA FORMATION (PERMIAN) Tan, gray, and buff interbedded dolomite, chert, limestone, siltstone, and 

sandstone, and minor shale and phosphate rock 

Pt TENSLEEP SANDSTONE (PENNSYLVANIAN) Buff and white 

fine-grained crossbedded to massive sandstone; weathers 

dark brown or black

PMa AMSDEN FORMATION (PENNSYLVANIAN AND MISSISSIPPIAN) Red, gray, buff, and purple shale, sandstone, 

and dolomite 

Mm MADISON LIMESTONE (MISSISSIPPIAN) Gray massive and

thin-bedded limestone, and minor chert and red shale 

Dd DARBY FORMATION (DEVONIAN) Gray, brown, and buff fetid 

dolomite, and greenish-gray and red siltstone and shale

Contact

Fault Bar and ball on downthrown side

Fold axis Showing plunge. Dotted where concealed

Strike and dip of beds

Boundary of Du Noir addition
8 DU NOIR ADDITION, WASHAKIE WILDERNESS, WYOMING

area of gently northwest-dipping Devonian strata is near the headwaters of West Du Noir Creek. Mississippian strata are extensively 

exposed in the broad, complexly folded core of the anticline, and 

Pennsylvanian and Permian rocks compose the limbs and the 

southeast-plunging nose. The lithology and thickness of these strata 

are briefly summarized in table 1; more detailed descriptions are 

given in Keefer (1957). The Phosphoria Formation is the only exposed 

Paleozoic unit of economic interest. It is the stratigraphically lowest 

horizon producing oil and gas in the Dubois field, 8 miles (13 km) 

southeast of the addition. Regionally, the phosphatic beds contain as 

much as 0.10 percent uranium and are a major source of phosphate 

rock in western Wyoming (Sheldon, 1963). For these reasons the 

lithology and stratigraphy of the Phosphoria Formation will be 

described in more detail than those of the other Paleozoic formations. 

The remaining two-thirds of the area is underlain mainly by Eocene 

volcaniclastic rocks, consisting of breccias, tuffs, and epiclastic 

volcanic conglomerates and sandstones derived from andesitic vent 

complexes that lie outside the study area. A variety of surficial 

deposits are present mainly glacial deposits of several ages, talus, 

alluvium, and extensive landslide deposits which thickly cover the 

bedrock in about one-half of the study area.

TABLE 1. Paleozoic rocks exposed in the Du Noir Addition

[Modified from Keefer (1957) and Mallory (1967)]

Age

Permian

'ennsyl van 1 an

lisslsslppian

Devonian

Formation

Phosphoria

Tensleep Sandstone

Amsden

Madison Limestone

Darby

Approximate 

thickness

260 feet

(80 m)

210-21(5 feet

(62-73 m)

290-310 feet

(90-98 m)

7<tO feet

(225 m)

190-210 feet 

(58-61. m)

Description

Dolomite, chert, limestone, siltstone, and

sandstone, interbedded, tan, gray, and buff; 

a few thin beds of phosphate rock; a minor

amount of shale.

Sandstone, buff and white, fine grained, thinly

crossbedded to massive, cliff-forming; weatherec

surfaces generally dark brown to black.

Shale, sandstone, and dolomite, Interbedded, red,

gray, buff, white, and purple; sandstone fine 

to medium grained, crossbedded.

Limestone, gray, massive to thin bedded; some

thin beds of chert; in places contains red

shale near top.

Dolomite, buff, gray, and brown, fetid; greenish- 1 

gray and red siltstone and shale.
GEOLOGY 9 

PERMIAN PHOSPHORIA FORMATION

The Phosphoria Formation crops out along the flanks of the Du 

Noir anticline (fig. 4) and consists of interbedded dolomite, chert, 

limestone, siltstone, and sandstone and minor conglomerate, shale, 

and phosphatic beds. The predominant colors are light brown and 

gray, although the phosphatic beds are dark gray and dark brown. 

The dolomite and limestone occur as massive and thin bedded units. 

Many of the carbonate beds are cherty and contain nodules and irregular masses of chert. Fossils are common, especially brachiopods 

and bryozoans. The sandstones and siltstones are tan, gray, pink, and 

white, containing both massive and thin-bedded units; most of them 

are limy or cherty. The sandstones are mostly fine grained. Minor 

gray shale is present, as well as thin beds of dark-gray and darkbrown oolitic phosphate rock. The section described by Reefer (1957, 

p. 174-175), beginning just southeast of the Du Noir area, contains 

only a single 1-foot (0.3-m)-thick bed of phosphate rock. In the wellexposed section just east of Du Noir Creek (NEVi sec. 9, T. 43 N., R. 

108 W.), there is only an 8-inch (20-cm)-thick bed of phosphate rock 

and a 2-foot (0.6-m)-thick bed of phosphatic sandstone and siltstone 

interbedded with carbonate rocks. On the north flank of the Du Noir 

anticline there are local beds of dark phosphatic sandstone, siltstone, 

and limestone a few inches thick, but no beds of oolitic phosphate 

rock were found. Regional studies of the Phosphoria Formation indicate that the phosphatic members are thickest along the WyomingIdaho border, and that they thin and become less pure eastward and 

northeastward (Sheldon, 1963). Because the Du Noir Addition is near 

the distal edges of these phosphatic tongues, the presence of beds of 

phosphate rock of minable thickness beneath the volcanics is extremely unlikely.

The Phosphoria Formation was deposited on an erosion surface 

having a few feet of relief incised in the Tensleep Sandstone; the basal 

bed of the Phosphoria Formation is a conglomerate 5-15 feet(2-5 m) 

thick (Keefer, 1957). A complete section of the Phosphoria Formation 

is about 260 feet (80 m) thick in this part of Wyoming, and it is conformably overlain by the Dinwoody Formation of Triassic age. In the 

Du Noir Addition, however, the top of the Phosphoria Formation and 

the overlying Mesozoic strata are covered by volcanic rocks.

CENOZOIC ROCKS

Cenozoic rocks in the Du Noir Addition include the coarse nonvolcanic conglomerates of the Indian Meadows Formation, the extensive andesitic volcaniclastic sediments assigned to the Tepee Trail
10 DU NOIR ADDITION, WASHAKIE WILDERNESS, WYOMING

and Wiggins Formations, and two small areas of Pliocene basalt. The 

Cenozoic rocks rest unconformably on the deeply eroded Washakie 

Range, whose surface has several hundred feet of relief. The Cenozoic 

strata are flat-lying or dip gently north to northeastward. Because of 

extensive glacial and landslide deposits in the broad valley bottoms, 

the extent of the Indian Meadows and Tepee Trail Formations is 

poorly known.

INDIAN MEADOWS FORMATION

The Indian Meadows Formation was named by Love (1939) for a sequence of coarse- to fine-grained clastic sediments along the East 

Fork of the Wind River about 20 miles (32 km) southeast of the Du 

Noir Addition. Coarse massive conglomerates along West Du Noir 

Creek were assigned to the Indian Meadows Formation by Keefer 

(1957). These conglomerates consist of subrounded cobbles, boulders, 

and pebbles of Paleozoic sandstone, limestone, dolomite, and chert in 

a red and gray matrix of coarse-grained calcareous sandstone; 

however, they contain no Precambrian or volcanic rock fragments. 

The deposit is as much as 200 feet (60 m) thick. The Indian 

Meadows Formation is believed to have been deposited during a 

period of rapid erosion following folding and faulting of the Washakie 

Range (Keefer, 1957). These coarse conglomerates, found lapping 

against the south flank of the Washakie Range, grade southward into 

finer grained strata in the Wind River Basin. Vertebrate fossils in the 

type locality date the Indian Meadows Formation as early Eocene.

ABSAROKA VOLCANIC SUPERGROUP

The Absaroka Volcanic Supergroup was defined by Smedes and 

Prostka (1972) to include all the Eocene volcanic rocks, associated intrusives, and volcanic sediments that compose the Absaroka volcanic 

field. The supergroup consists of, in ascending order, the Washburn 

Group, the Sunlight Group, and the Thorofare Creek Group all of 

middle to late Eocene age. Only rocks belonging to the Thorofare 

Creek Group are present in the Du Noir Addition (fig. 4) those 

assigned to the Tepee Trail and Wiggins Formations. Both of these 

formations were first defined and described by Love (1939) in an area 

about 15 miles (24 km) southeast of the Du Noir Addition, but 

because of stratigraphic complications the type Tepee Trail may not 

be equivalent to the rocks called Tepee Trail in the Du Noir area.

The source vents for these volcanic sediments were andesitic 

stratovolcanoes located northwest, north, and northeast of the Du 

Noir Addition. At the time these volcanoes were being formed they
GEOLOGY 11

were also being eroded, and the epiclastic and pyroclastic materials 

were redeposited as thick widespread alluvial aprons outward from 

the vent complexes (Smedes and Prostka, 1972). In the Du Noir area, 

the Tepee Trail and Wiggins Formations consist almost entirely of 

reworked volcanic material mudflow breccias, fluvial breccias and 

conglomerates, volcanic sandstones, siltstones, and air-fall tuffs.

TEPEE TRAIL FORMATION

The Tepee Trail Formation is a sequence of well-bedded brown, 

green, and buff volcanic sediments and tuffs present along much of 

the south margin of the Absaroka volcanic field (Love, 1939; Keefer, 

1957; Ketner and others, 1966; Rohrer, 1966; Rohrer and Obradovich, 

1969). In the Du Noir area, the strata mapped as Tepee Trail contain 

a higher proportion of fine-grained beds than do those in the type section. They mostly consist of interbedded tuffaceous sandstone, 

mudstone, and claystone, with lesser amounts of breccia and conglomerate. The upper part of the formation is coarser grained than 

the lower part. A distinctive conglomerate consisting of quartzite 

pebbles in a green sandy matrix occurs at the base of the formation 

southwest of the Du Noir area, but this unit was not found exposed 

within the study area itself. The upper part of the formation contains 

several flinty beds of tuff, with abundant fossil leaves, and a few thin 

beds of carbonaceous shale. Northward, the formation thins and 

becomes coarser grained, and the carbonaceous shales pinch out. The 

Tepee Trail Formation unconformably overlies the Indian Meadows 

Formation and the Paleozoic rocks of the Du Noir anticline. Because 

of considerable relief beneath the Tepee Trail, the formation varies in 

thickness from a maximum of about 1,800 feet (550 m) near Pinnacle 

Buttes to less than 300 feet (90 m) west of The Ramshorn. The top of 

the formation is approximately located where predominantly brown 

and light green flintstones and claystones of the Tepee Trail are 

overlain by the predominantly light gray mudflow breccias and conglomerates of the Wiggins Formation. This lithologic break has been 

interpreted to be time-transgressive and to migrate stratigraphically 

upward toward the southeast, and so the top of the Tepee Trail would 

be somewhat younger at the eastern end of the Du Noir Addition 

than at the western end (Ketner and others, 1966; Rohrer and 

Obradovich, 1969). On the basis of recent paleontological work, 

however, J. D. Love (written commun., 1974) believes that the Tepee 

Trail of the Du Noir area is older than the type Tepee Trail and is correlative with the Aycross Formation instead. Detailed stratigraphic 

work, which is beyond the scope of the present study, is needed to 

determine lithologic continuity of the formations and their relation to 

time lines determined by paleontologic studies.
12 DU NOIR ADDITION, WASHAKIE WILDERNESS, WYOMING

WIGGINS FORMATION

The Wiggins Formation is a thick sequence of dominantly light to 

medium gray and brownish-gray coarse volcanic mudflow and fluvial 

breccias and conglomerates that are spectacularly exposed in prominent cliffs throughout the southern Absaroka Range. The mudflow 

deposits are massively bedded units several feet to tens of feet thick. 

They consist of dark-gray angular to subangular clasts, as much as 6 

feet (2 m) across, of hornblende- and pyroxene-bearing andesite in a 

light-gray to pinkish-gray tuffaceous mudstone matrix. The volcanic 

conglomerates and well-sorted breccias contain much less matrix 

than the mudflow deposits and stand out as much darker layers in 

the cliffs. The volcanic sandstones and mudstones are massively bedded light-gray to buff units. Several beds of biotitic air-fall tuff and 

pumice, each less than 6 feet (2 m) thick, are interbedded in the sequence and form prominent thin white bands. A lava flow and 

associated flow breccia occur in the middle part of the formation near 

the top of Pinnacle Buttes. Because the epiclastic volcanic sediments 

must have originally been deposited in beds that dipped gently away 

from the vent complexes north of the study area (Smedes and Prostka, 1972), the present gentle northward to northeastward dip of 

these beds must be tectonic. The Wiggins is 1,000 feet (300 m) to 

more than 2,000 feet (600 m) thick in the Du Noir area, with the 

thickest sections being on The Ramshorn. In the Du Noir Addition, 

the top of the Wiggins is an erosional surface, and so the uppermost 

part of the formation is not present.

PLIOCENE BASALT

Remnants of Pliocene and younger basalt are found scattered 

throughout the southern Absaroka Range (Ketner and others, 1966; 

Rohrer, 1966). Two such remnants occur in the Du Noir area (fig. 

4) a dissected volcano with associated lava flows on Crescent Mountain (Blackstone, 1966) and a patch of lava flows, possibly the remains of a small shield volcano, north of The Ramshorn. The Crescent Mountain volcano is an arcuate ridge of massive dark-gray lava 

flows of platy basalt about 300 feet (100 m) thick. It includes part of a 

red to reddish-brown scoria-spatter cone intruded by a northeasttrending dike, probably a feeder for the volcano. These basalts or 

basaltic andesites contain sparse small phenocrysts of plagioclase 

and augite. A whole rock K-Ar determination on one of the flows gave 

an age of 3.6 m.y. (million years) (Blackstone, 1966).
GEOLOGY 13 

PLIOCENE(?) INTRUSIVE ROCKS

Intrusive rocks in the Absaroka volcanic field are closely 

associated with vent complexes and are generally not present in 

alluvial facies deposits. No intrusives related to Absaroka volcanism 

were found in the Du Noir Addition, but there are dikes of vesicular 

basalt on the west side of Coffin Butte that are of probable Pliocene 

age. These dikes are less than 5 feet (2 m) thick, dip about 10 ° northwest, and contain sparse small plagioclase phenocrysts. They have 

somewhat irregular trends, but they strike in a general way toward 

the Pliocene volcano on Crescent Mountain.

Rohrer (1966) mapped a thick basalt dike of similar trend on the 

west side of Pinnacle Buttes, but it was not found to extend northeast of there. These dikes are all believed to be part of the late 

Cenozoic episode of basaltic volcanism.

SURFICIAL DEPOSITS

A variety of surficial deposits are present in the Du Noir Addition, 

but they were not studied or mapped in detail. Alluvial and fan 

deposits of sand and gravel rich in volcanic clasts are discontinuously 

present along modern streams; these are the only surficial deposits 

that were sampled for geochemical analysis.

Colluvium and talus mantle the lower parts of cliffs and steep 

slopes; these have been included with units shown as landslide 

deposits on our map (fig. 4).

Glacial deposits are present mainly in high cirques and at much 

lower elevations along the southern border of the Du Noir Addition. 

Rohrer (1966) distinguished three ages of glacial till in the 

southwestern part of the area. None of these glacial deposits was important enough in terms of this study to be shown separately.

Landslide deposits are by far the thickest and most extensive of 

the surficial deposits, covering nearly one-half of the study area. 

Most of the landslides were a result of failure of glacially steepened 

slopes in the Wiggins and Tepee Trail Formations. The sliding seems 

to have occurred along structurally weak beds of claystone and shale 

that occur in the basal part of the Wiggins Formation and 

throughout the Tepee Trail Formation. Practically all of the steep 

cliffs in the Wiggins Formation are giant landslide scars modified by 

later rockfalls. In the valleys in the north half of the addition, thick 

deposits of Wiggins debris cover large areas of Tepee Trail and 

Paleozoic rocks. In the south half of the area, most of the landslides
14 DU NOIR ADDITION, WASHAKIE WILDERNESS, WYOMING

are in Tepee Trail Formation; some of the landslides have moved only 

a small amount and are only slightly out of place.

STRUCTURE

The Paleozoic rocks of the Du Noir Addition (fig. 4) have been folded into a broad northwest-trending anticline that plunges gently to 

the southeast; the limbs dip about 20 °. A section across this fold as 

well as structure contours on the top of the Precambrian surface, is 

given by Reefer (1957).

The Cenozoic rocks lie unconformably on the Du Noir anticline and 

dip gently, less than 5 °, to the north and northeast. This dip is consistent with that observed in the Stratified Primitive Area (now part of 

the Washakie Wilderness) just to the east (Fisher and Ketner, 1968). 

The Cenozoic rocks are cut by steep faults that trend predominantly 

northwest and northeast and have displacements of only a few tens ef 

feet. The age of these faults is unknown, but they are presumed to 

have formed in late Cenozoic time when the south margin of the 

volcanic field was tilted northward, as was shown by Fisher and 

Ketner (1968).

The basalt on Crescent Mountain and the dikes on Coffin and Du 

Noir Buttes and Pinnacle Buttes all lie along a zone that extends 

southwest to Lava Mountain, a Pleistocene basaltic volcano about 6 

miles (10 km) southwest of the addition. The alinement of these 

young basaltic vents and intrusive rocks suggests that there is a 

northeast-trending line of deep crustal fracturing beneath the northwestern part of the addition that provided channelways for ascending 

magma.

AEROMAGNETIC SURVEY

By M. DEAN KLEINKOPF, U.S. GEOLOGICAL SURVEY

The aeromagnetic map (fig. 5) covers the northern half of the area 

and shows no evidence of buried intrusives that might be indicative 

of mineralization. In general, the trend of the magnetic contours is 

parallel to the geologic contacts. Near the center of the Du Noir area, 

the northwesterly trending magnetic high correlates with the thick 

volcanic pile that extends through the area and beyond to the northwest.
MINERAL RESOURCES 15

R. 108 W. 

4 MILES

 2000-

EXPLANATION

Magnetic contours Showing total intensity magnetic field 

of the Earth in gammas relative to arbitrary datum. Contour interval 20 gammas

Location of measured maximum or minimum intensity 

within closed high or closed low

Flight path Showing location and spacing of data

Boundary of Du Noir addition

FIGURE 5. Aeromagnetic map of the north half of the Du Noir Addition and vicinity. 

Base from AMS 1:250,000 Thermopolis (1955).

MINERAL RESOURCES

SETTING

Northwestern Wyoming contains a wide variety of earth resources 

of present or future potential commercial value. These resources may 

be grouped into five categories as follows: (1) metallic mineral 

deposits some bedded and others related to igneous rocks, (2) coal, 

phosphate, and limestone, (3) oil and gas, (4) geothermal, and (5) surficial deposits of building stone, gravel, and sand.
16 DU NOIR ADDITION, WASHAKIE WILDERNESS, WYOMING

Nearby areas of known metallic mineralization associated with igneous activity are Kirwin, 28 miles (45 km) northeast of the study 

area (Hewett, 1914; Wilson, 1964), and the Stinkingwater region, 23 

miles (37 km) north (Fisher, 1972). Neither area has had significant 

past production, but they have future potential for low-grade 

disseminated deposits of copper and for molybdenum deposits.

Gold occurs in gravels along the Wind River and several of its 

tributaries. According to Schrader (1915), at the time of his reconnaissance in 1913, these deposits had been worked intermittently for 

50 years with generally poor results.

Sedimentary rocks in the vicinity of the Du Noir Addition range in 

age from Cambrian to Quaternary. Regionally some of these rocks 

are hosts for oil and gas, and some contain bedded deposits of coal, 

phosphorite, gypsum, bentonite, and limestone. Many mining claims 

for uranium have been filed since 1950, particularly in areas having 

exposures of the Phosphoria Formation or the Wind River Forma* 

tion. /

Geothermal energy is present in the region south of the addition, 

where warm and hot springs occur, and in the well-known thermal 

areas of Yellowstone National Park.

MINING CLAIMS AND MINERAL PRODUCTION HISTORY

A search of the records of Fremont, Park, and Teton Counties was 

made to determine whether any unpatented mining claims had been 

located in the Du Noir Addition. None was found in the addition. 

Land-status records of the Bureau of Land Management in 

Cheyenne, Wyo., were examined for mineral leases and for the existence of patented mining claims. These records show no patented 

claims. Forest Service personnel and Dan Miller, Wyoming State 

Geologist, were contacted for knowledge of any mineral activity in 

and around the addition. They were not aware of any such activity. 

Companies that were known to have been interested in minerals near 

the addition were contacted, and they furnished the information 

discussed below.

No mineral production is reported from the Du Noir Addition, and 

the area has no record of mineral production activity. During the field 

investigation, no mine or prospect workings were found. However, 

groups of unpatented lode mining claims, presumably for uranium, 

called No Name, Ram, 6 M, and Skylark, were located in 1967, adjacent to and near the south boundary of the addition. A part of Ram 

claim No. 206, and a part of one of the 6 M claims may extend within 

the study area. An unidentified claim stake was found about 100 feet 

(30 m) inside the addition, near the jeep road between Esmond Creek
MINERAL RESOURCES 17

and East Du Noir Creek. In 1967 and 1968, Gulf Mineral Resource 

Co., which acquired most of these claims, conducted an exploration 

program on their holdings, but none of the holes drilled by the company was on any of the claims shown in figure 6. The target for the 

drilling was the Wind River Formation, but no uranium mineralization was found.

The Wind River Formation probably underlies some of these 

claims, as it is extensively exposed farther south. This formation is 

the host rock for uranium ores being mined in the Gas Hills district, 

about 110 miles (177 km) southeast of the Du Noir Addition.

The mineral resource appraisal was made by using geochemical 

sampling methods in conjunction with geological mapping and field 

observations. Stream-sediment samples and bedrock samples were 

collected (fig. 7) and analyzed. Two kinds of stream-sediment samples 

were collected: (1) pan concentrates for metals, such as gold, 

platinum, mercury, tin, tungsten, chromium, niobium, titanium, rare 

earths, and zirconium, that are most likely to occur in heavy detrital 

minerals; and (2) silt-sized stream-sediment fractions for metals, such 

as silver, copper, lead, zinc, molybdenum, and vanadium, that are 

preferentially adsorbed or precipitated on organic-rich mud, clay, or 

manganese oxides. A major part of the sampling program was 

directed toward the collection of both kinds of samples from all of the 

streams in the area, as well as from streams that head in the drainage 

divides but do not flow into the Du Noir drainage, such as tributaries 

of Brooks Lake Creek and Cub Creek and the South Fork of the 

Shoshone River.

Pan concentrates were collected at sites most likely to favor the accumulation of heavy detrital minerals from the insides of meanders, 

at places protected from swift currents (beside or under boulders, 

below willow bushes, at the edges of gravel bars), or between the 

roots of streamside vegetation, particularly moss. One large pan (16 

inch (40.6 cm) in diameter) of material (dry weight about 8,000 g) was 

taken from small streams and two such pans of material from large 

streams; these were panned down to a heavy mineral fraction, which 

ranged in weight from only 1 or 2 g to as much as 92 g. The heavy 

mineral concentrate thus represents as much as 92/8,000 or as little 

as 1/8,000 of the material sampled. In discussions of analytical 

results, weighting factors are considered. The concentrate was 

carefully examined in the pan, particularly for gold, and then was 

scanned for radioactivity using a scintillation counter. Splits were
£|_^

FIGURE 6. Location of mining claims and U.S. Bureau of Mines sample localities in an
MINERAL RESOURCES 19

6 KILOMETERS

EXPLANATION

Bedrock sample ° 

Stream-sediment sample

e Pan-concentrate sample

Stream-sediment and panconcentrate samples

FIGURE 7. U.S. Geological Survey sample localities. Base from AMS 1:250,000 Thermopolis (1955).

removed for six-step semiquantitative spectrographic analysis, mercury analysis, and cold-extractable heavy metals analysis. All the remaining material was analyzed for gold.

Silt-sized stream-sediment samples were usually collected from 

mud or silt at the edges of streams, below rocks and logs, in streams, 

or in the roots of vegetation. One to four pounds (0.5-2 kg) of material 

was collected at each locality. In the field laboratory the sample was 

dried, scanned for radioactivity, sieved to pass 80 mesh, and then
20 DU NOIR ADDITION, WASHAKIE WILDERNESS, WYOMING

analyzed for gold, mercury, and cold-extractable heavy metals and by 

six-step semiquantitative spectrographic analysis.

Rock samples also were collected as part of the geochemical sampling program (fig. 7). Most of the rocks of the addition are Eocene 

volcaniclastic rocks or Paleozoic sedimentary formations, but small 

Pliocene basaltic intrusives cut the volcaniclastic rocks on The Ramshorn, Coffin and Du Noir Buttes, and Crescent Mountain.

Formations consisting almost wholly of volcaniclastic material 

(Wiggins and Tepee Trail Formations) and the large areas of landslide 

debris constitute more than three-fourths of the surface area of the 

addition. Representative samples were collected from these rocks, 

with a special effort made to collect some samples that might be 

enriched in some metal or element of interest. Such samples came 

from altered areas, carbonaceous shales, lenses of well-sorted conglomerates and sandstones, or areas stained by celadonite.

The Indian Meadows Formation and the Paleozoic rocks (table 1) 

were examined for possible resource potential economic concentrations of metals, and bedded deposits of coal, phosphate rock, bentonite, and building stone.

Analytical data were obtained by several methods: six-step semiquantitative spectrographic analyses for 30 elements; chemicalatomic absorption analyses for gold, mercury, and cold-extractable 

heavy metals; instrumental-atomic absorption analyses for mercury; 

the citrate-soluble heavy metals test (CxHM) for copper, lead, and 

zinc; and routine scanning of samples for radioactivity with a scintillation counter. Some rock samples were analyzed by gamma-ray 

spectrometer for equivalent uranium (eU).

The chemical and spectrographic data were stored on magnetic 

tape and are available from the National Technical Information Service (Prostka and Antweiler, 1974).

Analytical data indicate that the amount of each element in nearly 

all the samples is commonplace. Some elements (arsenic, boron, 

beryllium, bismuth, cadmium, lanthanum, antimony, scandium, tin, 

strontium, tungsten, yttrium, and zirconium) were either not 

detected in the analyses or were too infrequently detected to be useful 

in geochemical or resource studies. A list of selected analyses of 

samples with higher-than-ordinary values for 1 or more of 15 

elements, plus the CxHM test, was retrieved via computer from the 

complete data stored on magnetic tape. Values of samples chosen for 

computer retrieval were IVz to 14 times greater than estimates of 

crustal abundance. To provide perspective, crustal-abundance 

estimates are given in table 2 along with the values used for computer retrieval.

Listed in table 3 are the samples retrieved using the cutoff values 

shown in the center column of table 2.
MINERAL RESOURCES 21

TABLE 2. Estimated crustal abundance and minimum values

used for computer retrieval of 15 elements 

[Titanium is given in percent; other elements in parts per million]

Ag -- -

Co- -

Mo 

Hg... .......... ...

CxHHl/ ............

......... .075

.... .. 390

25

......... 1.3

 - 19

 89

. - .0035

 

Minimum value

125 

17

70

.05

.17

7

 Estimates were taken from Lee and Yao (1970).

 Cold extractable heavy metals.

As a supplement to the geochemical sampling done by the U.S. 

Geological Survey, the U.S. Bureau of Mines collected and analyzed 

23 samples, consisting of 12 pan concentrates, 2 stream-sediment 

samples, and 9 bedrock samples. The bedrock samples included two 

samples of tuff from the Wiggins Formation, 2 samples of conglomerate from the Indian Meadows Formation, 3 samples of highpurity limestone from the Madison Limestone (discussed below), 1 

sample from the Phosphoria Formation, and 1 sample from the Darby Formation, which looked as though it could have been hydrothermally altered. Analyses of these samples are shown in table 4. All 

samples were checked for radioactivity, with negative results.

ANALYTICAL RESULTS AND RESOURCE POTENTIAL

METALLIC MINERALS

Many of the metallic mineral deposits in the Rocky Mountains are 

related to igneous intrusive activity. Except for minor upper Tertiary 

basaltic intrusives, igneous intrusive rocks are not present in the ad-
TABLE 3. Selected analyses of the U.S. Geological Survey samples from the Du N

[Values shown are in parts per million, except titanium, which is in percent, symbols used are: G, greater than the sensitivity 

and L, an undetermined amount present below the lower limit of detection. Gold and mercury analyses were made by at

heavy-metals test (CxHM) by colorimetric comparison; other elements by 6-step semiquantitative spectrographic analy

number in the series 1, 0.7, 0.5, 0.3, 0.2, 0.15, 0.1, which represent approximate midpoints of group data on a geometr

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?o

20

?0

20

20

20

20

20

20

SO

20

20

20

20

70

20

20

20

20

20

20

20

20

20

,N

,N

,N

 ''

.N

.N

, <

,N

.N

,N

.N

,N

, N

,N

,N

«N

.N

.N

.N,

 N

. N

,N

, N

.N

. N

§

.N

. M

. N

, L

t

, M

. M

. <

>N

 N

«N

>N

.N

. «

200.

150.

150.

100.

200.

too.

100.

200.

100.

ISO.

150.

200.

150.

150.

200.

200.

150.

300.

150.

5.

50.

50.

15.

20.

ISO.

100.

so.

10.

ISO.

7.

50.

7.

ISO.

20.

50.

10.

5.L

b.L

200.

rfOO.

70.

10. N

15.

15.

to.

10.

15.

15.

15.

15.

10.

15.

10. N

10.

10. N

15.

15.

70.

to.

50.

15.

150.

150.

50.

10.

70.

70.

70.

tO."i

1U.

15.

50.

to.

?0.

100.

150.

50.

15.

to.

?0.

SO.

20.

300.

ISO.

300.

200.

300.

300.

500.

SCO.

300.

200.

300.

500.

300.

300.

200.

200.

200.

300.

300.

SO.

200.

too.

too.

100.

ISO.

200.

too.

500.

300.

206.

ISO.

500.

100.

SO.

50.

so.

100.

300.

200.

200.

too.

200

200

200

200

200

200

200

200

200

200

200

200

200

200

200

200

200

200

200

200

IbOO

1500

200

200

200

200

200

200

200

200

200

200

200

500

500

200

200

200

200

200

200

4/

 Darby Formation.

 Tepee Trail Formation. 

y Tertiary igneous iotrus
TABLE 4. Analyses of U.S. Bureau of Mines samples from the Du Noir A

[Sample localities are given below by T. (township), R. (range), and S. (section) north and west of the 6th Principal Meridia

44-108-22. Samples were analyzed by semiquantitative spectrographic and fire assay methods at the U.S. Bureau of M

analyses were made using a 3.4-m Wadsworth spectrograph with 30-inch (76 cm) plateholder. Estimates of concentrat

in sample spectra with intensity of lines in spectra of a graded series of standards. The numbers in parentheses benea

lower limit of detection for that element. An error of plus 100 percent, minus 50 percent of the reported concentration 

percent; >, more than the amount shown; <, less than the amount shown; NA, no analyses; Tr, trace; -, looked for but 

below the lower detection limit. The following elements were looked for spectrographically but were not detected: As

Sb, Ta, Te, Tl, W, and Zn. The following elements were detected in some samples and the results reported at the botto

and Y. Ca, Na, and Si were detected in most samples but were found in amounts normal for the rocks samples]

Assay

Sample

,

2 2

3

4

3 5

"6

5 7 

6 8

10 

11

12

13

14

15

16

17

18

19

20

21

22

'Sample

^Sample

Location

T. R. S.

43-108- 2

44-108-33

44-108-27

44-108-26

44-108-26

44-108-22 

44-108-21

44-108- 4 

44-108- 4

44-108- 8

44-108- 6

44-109-10

44-109-15

44-109-22

44-109-25

44-109-25

44-109-25

44-108-31

44-108-31

44-108-31

1 contains

2 contains

(oz

Au

__

NA

NA

NA

Tr

_

NA

NA

50

80

/ton)

Ag

.1

.4

NA

NA

NA

Tr

.1

.1

.1

.1

.2

NA

Tr

.1

.2

NA

ppm Ag

ppm Sn

Ba

(1,000)

40,000

2,000

2,000

<1,000

1,000

_

1,000

^Sample

''Sample

Co

(40)

40

40

40

40

50

50

50

50

100

40

Cr

(30)

4,000

500

1,000

1,000

1,000 

300

60

500

500

500

500

1,000

1,000

200

200

5 contains

6 contains

Cu

(20)

40

40

<20

60

60

40 

80

40 

40

40

40

40

40

40

30

<20

30

40

40

20

1,000

2,000

Semiquantitative

Mn

(30)

4,000

2,000

10

2,000

2,000

2,000 

.200

1,000 

1,000

4,000

1,000

100

1,000

2,000

2,000

60

2,000

300

300

100

ppm Sr

ppm Sr

Ni Pb

(20) (100)

300 100

200

 <100

200 200

200 200

200

200

200 100

200 100

 <100

300 100

300 200

600

300 <100

 

^Sample

6 Sample

spectrographic

(ppu

Sc

(50)

__

__

<50

<50

<50

<50

_

50

<50

7 coi

0

V Zr

(60) (70)

400 300

100 300

60

100 100

100 300

200

 100

60 <70

500 <70

100 <70

100 <70

500 <70

100 100

<60 200

<60 200

italns 20

8 contains 20,

analyses

Al

(0.003)

3.0

3.0

.04

M

M

4.0 

.7

5.0 

1.0

M

M

1.0

3.0

2.0

M

.01

4.0

2.0

1.0

.02

ppm Ag

000 ppm P,

(pe

Fe

(0.004)

M

4.0

.05

4.0

4.0

7.0 

2.0

1.0 

1.0

6.0

M

.4

6.0

M

M

.05

M

.4

.4

.1

and 30

rcent

M

(0.

>

ppm 
MINERAL RESOURCES 27

dition. Geologic mapping and field examination do not suggest the 

presence of mineralization associated with these upper Tertiary 

basaltic intrusive rocks. Bedrock samples D1501R-D1510R, D558R, 

D559R, and D544R-D546R were collected on and near Crescent 

Mountain from the intrusive and the intruded rocks. Only samples 

D559R, D1503R, and D1504R were sufficiently anomalous to be included in table 2; the "anomalous" element was chromium 700 

ppm which is only slightly enriched (if enriched at all) in comparison 

to other mafic rocks in the Earth's crust. The basalt on The Ramshorn is outside the addition and was not sampled, but it showed no 

evidence of mineralization. Stream-sediment samples from Frozen 

Lake Creek (D57P and D58S), which drains that area, show no enriched metal values except for titanium and chromium, and these are too 

small to be of value.

The possibility of any economic mineral resources in the addition is 

slight. Gold was observed in a few pan concentrates and one rock 

sample (D508R). The most likely source of gold in pan concentrates is 

quartzite gravel lenses that occur near the base of the Tepee Trail 

Formation. These lenses were apparently derived from the Pinyon 

Conglomerate and Harebell Formation of Paleocene and latest 

Cretaceous age, which occur extensively to the west and northwest 

(Antweiler and Love, 1967). The small amount of gold found, plus the 

very small volume of quartzite gravels in the addition, precludes the 

possibility of a gold resource. The one bedrock sample in which gold 

was detected (D508R) was sandstone from the Tensleep Sandstone. 

Other analyses from this sandstone failed to show any gold.

Silver, copper, lead, and zinc, although found in amounts exceeding 

normal background values in a few samples, are not present in sufficient quantity to be of any resource interest. The cold extractable 

heavy metals test is particularly useful in detecting zinc; the four 

samples that showed high values for the CxHM test had enough zinc 

to be detected by spectrographic analysis as well.

Many of the samples in table 3 appear to be high in titanium and 

chromium. However, most of the high values are in pan concentrates 

and result from concentration of ilmenite and chromite by panning. If 

the values shown are divided by the concentration factor (which is 

usually about 100) to obtain the actual concentrations present in 

alluvium prior to panning, it is doubtful that either element is present in an amount great enough to be of importance. The amounts of 

chromium and titanium found in bedrock samples are within the 

ranges expected for the kinds of rock analyzed. There are no naturally 

concentrated ilmenite or chromite deposits in the stream gravels 

large enough to be of any economic importance.
28 DU NOIR ADDITION, WASHAKIE WILDERNESS, WYOMING

Carbonaceous shale is present along the southern margin of the 

outcrop belt of the Tepee Trail Formation. It contains abundant 

leaves and freshwater invertebrates indicative of swamplike conditions. Organic-rich muds in these areas evidently provided favorable 

conditions for precipitation or sorption of several metals including 

molybdenum (samples D617R, D2617R, D623R, and D2623R). 

Volumetrically, the carbonaceous shales constitute only a small fraction of the formation, but in the aggregate they could amount to a 

substantial tonnage. However, because of their thin lenslike 

character they would be extremely expensive and difficult to mine, 

even if they were rich in metals. To further evaluate their resource 

potential, 45 additional samples of similar shales were obtained from 

the region, and a summary of pertinent analytical results is presented 

in table 5.

Table 5 shows a greater enrichment in molybdenum than in any 

other element, but even its concentration is considerably below that 

required for molybdenum to be a potential resource. Of geochemical, 

but not economic, interest is the fact that two of the samples had sufficient tungsten to be detected spectrographically.

The geology of the area virtually precludes the possibility of exposed primary uranium deposits. The best possibilities for uranium concentrations are the black shales of the Tepee Trail and Phosphoria 

Formations. Radiometric eU determinations were made on all carbonaceous shale samples, and fluorimetric determinations for 

uranium were made on those that registered 90 ppm eU or more.

Of the samples collected within the addition, only one had sufficient uranium to justify a chemical-fluorimetric determination; that 

sample, which came from the Phosphoria, contained 80 ppm uranium. 

The samples of Eocene shale referred to in table 3 all contain less 

than 50 ppm eU and, therefore, do not appear to constitute a 

resource.

The uranium content of the Phosphoria Formation has been 

studied regionally by Sheldon (1963), who stated (p. 157), "The rocks 

in the western part of the report area [that is, western Wyoming-eastern Idaho] are more uraniferous than in the eastern part. 

In fact, in the Wind River Range in the eastern part of the area, no 

minable phosphorites contain as much as 0.005 percent uranium [50 

ppm] * * *. Thus, most phosphate rock mined in westernmost Wyoming and adjacent parts of Idaho will contain maximum quantitites 

of uranium; whereas, rock mined in most of western Wyoming will 

contribute smaller quantities of uranium as a byproduct." The Du 

Noir Addition is in the eastern part of the region studied by Sheldon, 

and therefore is a less likely area for high uranium concentrations in 

the Phosphoria Formation than are areas farther west.
MINERAL RESOURCES 29

-2 «> 43 *

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lit

Q) g

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30 DU NOIR ADDITION, WASHAKIE WILDERNESS, WYOMING

As a further check, J. D. Love collected samples, using a scintillation counter to find material with maximum radioactivity, from the 

Phosphoria at Stony Point (not on map, but located at 43 °32 '30" N., 

109 °43 7" W.; 14 miles (22.5 km) south of the addition). The analytical 

results are listed in table 6, together with those from the Phosphoria 

collected in the addition.

These analyses indicate that the Phosphoria in this vicinity is a 

possible low-grade source of several metals, as it is elsewhere (Service 

and Popoff, 1964, p. 7). However, none of the trace elements (ineluding vanadium, fluorine, and molybdenum) that occurs in the 

Phosphoria is being recovered at the large phosphate-mining and 

-processing plants in southeastern Idaho. Even though it is 

technologically feasible to recover uranium from this source, it is not 

now profitable or competitive with uranium from other sources. Even 

though individual values are high enough to indicate potential 

resources, the beds are so thin that there is little possibility of a 

minable resource of any of these elements in the Du Noir Addition.

COAL, PHOSPHATE, AND LIMESTONE

Mineral leasing records of the Bureau of Land Management show 

Federal coal withdrawals in 1910 for all of T. 43 N., R. 108 W., and T. 

43 N., R. 109 W., and phosphate withdrawals in 1912 for parts of the 

area included within the addition. In 1914, the coal withdrawal was 

revoked for most of T. 43 N., R. 108 W., including those parts of the 

township in the addition. At the same time, the land was opened to 

mineral entry for phosphate in all the withdrawn lands. No phosphate 

or coal leases have been issued in the Du Noir Addition since the 

Mineral Leasing Act of 1920, which established phosphate and coal 

as leasable minerals. In 1966, the U.S. Geological Survey classified T. 

43 N., R. 109 W., as coal land, meaning that it may have potential for 

coal. Thin coal seams occur in the Wind River Formation about 6 

miles (10 km) south of the addition. If any of this formation exists in 

the addition, it would be beneath the Wiggins and Tepee Trail Formations. Consequently, exploration costs would be expensive and the 

possibility of finding coal seams is slight.

Thin beds of phosphate rock occur in the Phosphoria Formation, as 

mentioned in the uranium discussion. Thicker, more accessible beds 

with a higher phosphate content occur throughout western Wyoming 

and southeastern Idaho (Sheldon, 1963). The phosphate beds in the 

addition are not of resource value at the present time.

The Madison Limestone was sampled at three localities (fig. 6) to 

determine the chemical composition of the limestone (table 7). The 

results suggest that high-quality lime from this area could be a
MINERAL RESOURCES 31

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32 DU NOIR ADDITION, WASHAKIE WILDERNESS, WYOMING

TABLE 1. Chemical analyses of limestone from the Madison Limestone

[Figures are in weight percent; <, less than]

Sample Sample 18 Sample 22

Major constituents:

Lime (CaO) 

Volatile matter --------

Calculated calcium carbonate '

Other constituents:

57(±l) 56(±1) «9(±D

- 10l(±D 100(±1)

 - -ju

 .057

- .062

- .0^5

.057 

.01(2 

<.025 

.055

.03ft 

.062 

<.025 

.020

 Calculated by adding lime and volatile matter, which is here considered 

as carbon dioxide (CO,).

resource; however, the Madison Limestone is exposed and readily accessible over large areas of western Wyoming and adjacent parts of 

Montana and Idaho, and the demand for lime in this region is small. 

High-calcium lime has many industrial and agricultural uses (Hubbard and Ericksen, 1973), but high shipping costs limit mining to 

areas near its market.

OIL AND GAS

The area southeast of the Du Noir Addition has a history of oil and 

gas leasing that began in 1946 (fig. 8). The first lease issued for land 

actually within the addition was in 1955, but by 1972 all of these 

leases were terminated. No drilling for oil and gas has been done in 

the addition; the nearest test is a dry hole drilled in 1965 in about the 

SWV* sec. 21 (unsurveyed), T. 43 N., R. 107 W. The Dubois oil field in 

sec. 11, T. 42 N., R. 108 W., is the nearest oil field; it is about 8 miles 

(13 km) southeast of the addition. This oil field was discovered in 

1946, and through 1972 it had produced approximately 98,000 barrels of oil from the Phosphoria Formation.

The Du Noir anticline (fig. 4) is on strike with the Dubois anticlinal 

complex in which the Dubois oil field is located. However, it is not a 

good target for oil and gas exploration because it has been deeply 

eroded into the Devonian rocks and largely stripped of favorable pro-
MINERAL RESOURCES 33

3123 KILOMETERS

EXPLANATION 

ill Land that has been leased for oil and gas

FIGURE 8. Location of oil and gas leases in and near the Du Noir Addition. Section 

lines shown are only approximately located. Except for T. 43 N., R. 108 W., which 

has been surveyed, the townships have not been surveyed or have been only partially 

surveyed.

ducing horizons. Because the axis of the Du Noir anticline plunges to 

the southeast, the possibilities for finding oil and gas beneath the 

volcanics in the addition are considered to be negligible.

BUILDING STONE, GRAVEL, AND SAND

Quantities of good building stone, gravel, and sand are very limited 

within the addition. The Madison Limestone would be a satisfactory 

source of building stone; however, stone of equal or better quality can 

be obtained much more easily near established transportation routes. 

Deposits of sand and gravel tend to be poorly sorted and of limited 

extent within the addition; they contain a high proportion of soft 

volcanic fragments generally unsuitable for concrete aggregate and 

road metal.
34 DU NOIR ADDITION, WASHAKIE WILDERNESS, WYOMING 

GEOTHERMAL RESOURCE POTENTIAL

The geothermal resource potential within the Du Noir Addition is 

small. The closest warm or hot spring is an inactive geyser between 

Geyser Creek and Warm Spring Creek, in the northeast quarter of 

sec. 32, T. 42 N., R. 107 W., about 11 miles (18 km) south of the Du 

Noir Addition.

The basaltic rocks on Crescent Mountain, Du Noir Butte, Pinnacle 

Buttes, and Lava Mountain are late Pliocene and younger and occur 

along a northeast-trending line, suggesting the presence of a deepfracture zone along which the magmas rose. A radiometric date 

(K-Ar, whole rock) that W. L. Rohrer and J. D. Obradovich determined on the basalt at Lava Mountain, which is outside of the study area, 

gave an age of only 500,000 years (U.S. Geological Survey, 1968, p. 

27). Although there are no recognized geothermal anomalies along 

this zone, it may be a possible target for geothermal energy investigations.

CONCLUSIONS

The results of the present investigation of the Du Noir Addition by 

the U.S. Geological Survey and U.S. Bureau of Mines show no 

evidence of significant mineral, fuel, or geothermal potential within 

the area. Neither the geochemical study nor the geologic mapping 

revealed any areas of alteration or mineralization, although minor 

anomalous concentrations of molybdenum and uranium were found 

in some Permian and Eocene carbonaceous shales. Phosphate rock in 

the Phosphoria Formation occurs in beds too thin to constitute an 

economic resource either at present or in the foreseeable future. There 

are large amounts of very pure limestone in the Madison Limestone 

within the addition, but equally pure limestone, much closer to 

transportation facilities, is found throughout this part of Wyoming. 

Coal was not found in any of the exposed formations. Sand and gravel 

deposits are all of low quality. The part of the Du Noir anticline 

within the addition is too deeply eroded to be a likely reservoir of oil 

and gas, and the absence of warm or hot springs in or near the addition does not favor its geothermal energy potential.

REFERENCES CITED

Antweiler, J. C., and Love, J. D., 1967, Gold-bearing sedimentary rocks in northwest 

Wyoming A preliminary report: U.S. Geol. Survey Circ. 541,12 p.

Blackstone, D. L., Jr., 1966, Pliocene volcanism, southern Absaroka Mountains, Wyoming: Wyoming Univ. Contr. Geology, v. 5, no. 1, p. 21-30.
REFERENCES CITED 35

Fisher, F. S., 1972, Tertiary mineralization and hydrothermal alteration in the Stinkingwater mining region, Park County, Wyoming: U.S. Geol. Survey Bull. 1332-C, 

33 p.

Fisher, F. S., and Ketner, K. B., 1968, Late Tertiary syncline in the southern Absaroka 

Mountains, Wyoming in Geological Survey research 1968: U.S. Geol. Survey 

Prof. Paper 600-B, p. B144-B147.

Hewett, D. F., 1914, The ore deposits of Kirwin, Wyoming: U.S. Geol. Survey Bull. 

540-C, p. 121-132.

Hubbard, H. A., and Ericksen, G. E., 1973, Limestone and dolomite, in Brobst, D. A., 

and Pratt, W. P., eds., United States Mineral Resources: U.S. Geol. Survey Prof. 

Paper 820, p. 357-364.

Keefer, W. R., 1955, Geologic map of the Du Noir area, Fremont County, Wyoming: 

U.S. Geol. Survey Oil and Gas Inv. Map OM-166 [1956].

___1957, Geology of the Du Noir area, Fremont County, Wyoming: U.S. Geol. Survey Prof. Paper 294-E, p. 155-221.

Ketner, K. B., Keefer, W. R., Fisher, F. S., Smith, D. L., and Raabe, R. G., 1966, Mineral resources of the Stratified Primitive Area, Wyoming: U.S. Geol. Survey Bull. 

1230-E, 56 p.

Lee, Tan, and Yao, Chi-lung, 1970, Abundance of chemical elements in the earth's 

crust and its major tectonic units: Internat. Geology Rev., v. 12, no. 7, p. 778-786.

Love, J. D., 1939, Geology along the southern margin of the Absaroka Range, Wyoming: Geol. Soc. America Spec. Paper 20,134 p.

Mallory, W. W., 1967, Pennsylvanian and associated rocks in Wyoming: U.S. Geol. 

Survey Prof. Paper 554-G, 31 p.

Prostka, H. J., and Antweiler, J. C., 1974, Magnetic tape containing semiquantitative spectrographic analyses, and some selected chemical analyses of rocks, 

stream sediments, and panned concentrates form the proposed Du Noir Headwaters Addition to the Washakie Wilderness, Wyoming: U.S. Geol. Survey Rept. 

USGS-GD-74-023, available only from U.S. Dept. Commerce Natl. Tech. Inf. Service, Springfield, Va., 22161, as Rept. PB-235001/AS.

Rohrer, W. L., 1966, Geologic map of the Kisinger Lakes quadrangle, Fremont County, Wyoming: U.S. Geol. Survey Geol. Quad. Map GQ-527.

___1969, Age and stratigraphic relations of the Tepee Trail and Wiggins Formations, northwestern Wyoming, in Geological Survey research 1969: U.S. Geol. 

Survey Prof. Paper 650-B, p. B57-B62.

Schrader, F. C., 1915, Gold placers on Wind and Bighorn Rivers, Wyoming: U.S. Geol. 

Survey Bull. 580-G, p. 127-145.

Service, A. L., and Popoff, C. C., 1964, An evaluation of the western phosphate industry and its resources: U.S. Bur. Mines Rept. Inv. 6485, 86 p.

Sheldon, R. P., 1963, Physical stratigraphy and mineral resources of Permian rocks 

in western Wyoming: U.S. Geol. Survey Prof. Paper 313-B, p. 49-273.

Smedes, H. W., and Prostka, H. J., 1972, Stratigraphic framework of the Absaroka 

Volcanic Supergroup in the Yellowstone National Park region: U.S. Geol. Survey 

Prof. Paper 729-C, 33 p.

U.S. Geological Survey, 1968, Geological Survey research 1968: U.S. Geol. Survey 

Prof. Paper 600-A, 371 p.

Wilson, W. H., 1964, The Wood River-Greybull River area, in Geologic reconnaissance 

of the southern Absaroka Mountains, northwest Wyoming: Wyoming Univ. Contr. Geology, v. 3, no. 2, pt. 1, p. 60-77.

ftU.S. GOVERNMENT PRINTING OFFICE: 1979-677-129/14
^ V , ^' *"? " 4 9 ^ » ' * '"*" f 

Prost.*^, Antweiler, and Bieniewski DU NOIR ADDITION, WASHAKIE WILDERNESS,