Volume VI-A
OCCURRENCE AND CHARACTERISTICS OF GROUND
WATER IN THE GREAT DIVIDE AND
WASHAKIE BASINS, WYOMING
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Volume VI-A
OCCURRENCE AND CHARACTERISTICS OF GROUND
WATER IN THE GREAT DIVIDE AND
WASHAKIE BASINS, WYOMING
by
Michael Collentine, Robert Libra, Kenneth R. Feathers,
and Latif Hamden
Project Manager
Craig Eisen
Water Resources Research Institute
University of Wyoming
Laramie, Wyoming
Report to
U.S. Environmental Protection Agency
Contract Number G-008269-79
Project Officer
Paul Osborne
August 1981
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Introduction
This report presents the findings of a ground-water study of the
Great Divide and Washakie basins in south-central Wyoming. The study
was funded by the U.S. Environmental Protection Agency (EPA) for the
Underground Injection Control (UIC) program, which is designed to
protect sources of usable ground water from possible contamination
caused by underground injection of liquid wastes and other fluids. This
ground-water report is one of seven prepared by the Wyoming Water
Resources Research Institute for the EPA. The reports cover all of the
state of Wyoming except for the Yellowstone National Park area in the
northwestern part of the state. The results of the study are primarily
intended for use by the EPA and Wyoming state agencies concerned with
development and preservation of the ground-water resources of the area.
The purpose of this report is to delineate, characterize, and
document ground-water occurrence, flow, quality, and use in the Great
Divide and Washakie basins, using available information; no
site-specific ground-water investigations were conducted during the
course of this study by the Wyoming Water Resources Research Institute
(WRRI). Specific work by WRRI included (a) field geologic
reconnaissance of parts of the study area and adjacent areas; (b)
collection, screening, and analyses of existing water well and oil test
well data; and (c) review of previous reports.
Water well and oil test well data were obtained from well records
at the Wyoming State Engineer's Office, Wyoming Geological Survey,
Wyoming Oil and Gas Conservation Commission, and from tabulated data in
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previous reports. Published reports of previous studies with pertinent
information on the geology and ground-water conditions in the study area
include (a) a detailed U.S. Geological Survey report on ground-water
conditions in a 634-square mile tract located in the vicinity of Rawlins
in the eastern part of the study area (Berry, 1960); (b) a recon-
naissance-level U.S. Geological Survey report on ground-water conditions
in the study area (Welder and McGreevy, 1966); and (c) a reconnaissance-
level ground-water report of the study area prepared for the Wyoming
Natural Resources Board by a private consultant (Dana, 1962). Some of
the information provided in these reports is used herein.
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TABLE OF CONTENTS
Chapter Page
I. SUMMARY OF FINDINGS 1
II. GENERAL DESCRIPTION OF STUDY AREA 7
POPULATION AND LAND USE 8
TOPOGRAPHY AND DRAINAGE 11
III. GEOLOGY AND HYDROSTRATIGRAPHY 15
GEOLOGIC OUTCROPS AND STRATIGRAPHIC SEQUENCE .... 16
STRUCTURAL GEOLOGY 23
HYDROSTRATIGRAPHY 26
IV. WATER USE 29
INDUSTRIAL WATER USE 30
Petroleum Industry 34
Coal Industry 35
Uranium Industry 36
AGRICULTURAL WATER USE 36
Irrigation 36
Stock Watering 38
PUBLIC AND PRIVATE DOMESTIC WATER USE 38
V. GROUND-WATER OCCURRENCE AND FLOW PATTERNS 41
MAJOR WATER-PRODUCING ZONES 42
Quaternary Aquifers 42
Upper Tertiary Aquifers 48
Tertiary Aquifer System 50
Mesaverde Aquifer 58
Frontier Aquifer 60
Cloverly Aquifer 64
Sundance-Nugget Aquifer 66
Paleozoic Aquifer System 68
SUMMARY OF REGIONAL GROUND-WATER CIRCULATION .... 72
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CHAPTER Page
VI. WATER QUALITY 75
GENERAL WATER QUALITY 77
Summary of Regional Water Quality .... .... 77
Quaternary Aquifers 78
Upper Tertiary Aquifers ' 80
Tertiary Aquifer System 82
Mesaverde Aquifer 88
Frontier, Cloverly, and Sundance-Nugget
Aquifers 91
Paleozoic Aquifer System 93
DRINKING WATER STANDARDS 97
Primary Standards 97
Fluoride 99
Lead
Other Primary Standards 102
Secondary Standards 102
Radionuclide Species 102
VII. REFERENCES 107
APPENDIX A: GROUND-WATER USE BY INDUSTRY AND FOR
IRRIGATION AND DRINKING WATER A-l
APPENDIX B: SUMMARY OF HYDROLOGIC PROPERTIES OF
- MAJOR WATER-BEARING ZONES B-l
APPENDIX C: RECORDS OF WELLS AND SPRINGS C-l
APPENDIX D: DETERMINATION OF AQUIFER PROPERTIES .... D-l
APPENDIX E: CHEMICAL ANALYSES OF GROUND WATERS
SAMPLED BY WRRI E-l
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LIST OF FIGURES
Figure Page
II-l Great Divide and Washakie basins study area 9
III-l General surficial geology, Great Divide and
Washakie basins 17
III-2 Generalized geologic column, Great Divide and
Washakie basins 18
III-3 Structural cross-sections, Great Divide and
Washakie basins 21
III-4 Index map for structural and potentiometric
cross-sections 22
III-5 Major structural features of the Great Divide
and Washakie basins 24
III-6 Hydrostratigraphic column, Great Divide and
Washakie basins 28
IV-1 Percent total water use, by economic sector 32
IV-2 Areal distribution of water users 33
V-l Potentiometric surface map, Upper Tertiary
aquifers 51
V-2 Potentiometric surface map, Tertiary aquifer
system 57
V-3 Potentiometric surface map, Mesaverde aquifer. ... 61
V-4 Potentiometric surface map, Frontier aquifer .... 63
V-5 Potentiometric surface map, Cloverly aquifer .... 65
V-6 Potentiometric surface map, Sundance-Nugget
aquifer 67
V-7 Potentiometric surface map, Tensleep aquifer .... 70
V-8 Potentiometric cross-sections, Great Divide and
Washakie basins 73
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Figure
Page
VI-1 Major ion composition of waters from the
Quaternary aquifers 79
VI-2 Major ion composition of waters from the
Upper Tertiary aquifers . . 81
VI-3 Major ion composition of waters from the
Battle Spring aquifer . . 84
VI-4 Major ion composition of waters from the
Laney aquifer 85
VI-5 Major ion composition of waters from the
Lance-Fort Union aquifers 86
VI-6 Major ion composition of waters from the
Wasatch aquifer 87
VI-7 Major ion composition of waters from the
Mesaverde aquifer 90
VI-8 General stratigraphic distribution of total
dissolved solids and major ion compositions
within Mesozoic and Paleozoic aquifers, Rock
Springs uplift area 92
VI-9 Major ion composition of waters from the
Frontier aquifer 94
VI-10 Major ion composition of waters from the
Cloverly aquifer 95
VI-11 Major ion composition of waters from the
Sundance-Nugget aquifer 96
VI-12 Major ion composition of waters from the
Paleozoic aquifer system 98
VI-13 Fluoride concentrations exceeding the primary
drinking water standard in Mesaverde through
Quaternary aquifers 100
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LIST OF TABLES
Table Page
II-l Population of the Great Divide and Washakie
basins 10
IV-1 Estimated water use in the Great Divide and
Washakie basins 31
V-l Generalized stratigraphy, lithology, and water-
bearing characteristics of geologic formations
in the Great Divide and Washakie basins 43
VI-1 Exceedences of primary drinking water standards
for species other than fluoride in ground waters
of the Great Divide and Washakie basins 101
VI-2 Concentration ranges of TDS, chloride, and
sulfate in ground waters of the Great Divide
and Washakie basins 103
VI-3 Concentrations of radionuclide species in
ground waters of the Great Divide and Washakie
basins 105
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LIST OF PLATES*
Plate
1. Structure contour map on top of the Cloverly Formation,
Great Divide and Washakie basins, Wyoming.
2. Wells permitted for domestic use, Great Divide and Washakie
basins, Wyoming.
3. Total dissolved solids map of Quaternary aquifers, Great
Divide and Washakie basins, Wyoming.
4. Total dissolved solids map for Upper Tertiary aquifers, Great
Divide and Washakie basins, Wyoming.
5. Total dissolved solids map for the Tertiary aquifer system,
Great Divide and Washakie basins, Wyoming.
6. Total dissolved solids map for the Mesaverde aquifer, Great
Divide and Washakie basins, Wyoming.
7. Total dissolved solids map for the Frontier aquifer, Great
Divide and Washakie basins, Wyoming.
8. Total dissolved solids map for the Cloverly aquifer, Great
Divide and Washakie basins, Wyoming.
9. Total dissolved solids map for the Sundance-Nugget aquifer,
Great Divide and Washakie basins, Wyoming.
10. Total dissolved solids map for the Paleozoic aquifer system,
Great Divide and Washakie basins, Wyoming.
*Plates contained in Volume VI-B.
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I. SUMMARY OF FINDINGS
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I. SUMMARY OF FINDINGS
1. Eight major water-bearing zones, each consisting of one or
more aquifers, have been identified in the Great Divide and Washakie
basins. They are: (1) Quaternary aquifers, (2) Upper Tertiary
aquifers, (3) the Tertiary aquifer system, (4) Mesaverde aquifer (Upper
Cretaceous), (5) Frontier aquifer (Upper Cretaceous), (6) Cloverly
aquifer (Lower Cretaceous), (7) Sundance-Nugget aquifer (Jurassic), and
(8) the Paleozoic aquifer system. These zones are separated by either
stratigraphic unconformities or thick and extensive geologic units of
very low permeability (primarily shale). Many of the aquifers are
under confined conditions over large area. Yields are generally low,
and water quality is poor, relative to other basins of the state.
2. The following aquifers are considered to be the most important
ground-water sources in the study area based on estimates of well
yield, water quality, and accessibility.
a. The Tertiary aquifer system is the most important and most
extensively distributed and accessible ground-water source in the
study area. Permeable sandstones of the Wasatch Formation are
present throughout most of the Great Divide and Washakie basins.
Sandstones and conglomerates of the Battle Spring Formation are at
the surface in the eastern part of the Great Divide basin. The
upper Laney Member of the Green River Formation is an important
aquifer in the western part of the Washakie basin, where permeable
sand lenses intertongue with silts and shales. Sandstones of the
Fort Union Formation are considered a major aquifer around the
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periphery of the basins. Tertiary aquifer system transmissivities
range from less than 300 in the Laney Member to more than 1,000
gpd/ft in the Wasatch, Battle Spring, and Fort Union formations.
Shallow (<1,500 feet) Tertiary ground waters from all member
aquifers generally contain less than 3,000 mg/1 TDS. The Battle
Spring and Wasatch aquifers in the Great Divide basin typically
yield water with less than 1,000 mg/1 TDS, with sodium, calcium,
sulfate, and bicarbonate predominating.
b. The permeable unconsolidated sand and gravel aquifers of
Quaternary age constitute important water sources in the valleys
of the Little Snake River and its major tributaries in the south-
eastern Washakie basin, and in the area south of the Ferris
Mountains in the northeastern Great Divide basin.
Low TDS (<1,000 mg/1) waters are generally available in these
areas. Calcium, sodium, and bicarbonate are the principal
dissolved constituents. Transmissivity estimates from alluvial
aquifers east of the Rock Springs uplift range from 168 to 560
gpd/ft, though water quality in this area is very poor.
c. The Upper Tertiary aquifers are important sources of water
in the eastern and western parts of the study area. These
aquifers include saturated parts of the Browns Park Formation on
the western side of the Sierra Madre uplift, North Park Formation
in the vicinity of Rawlins, and South Pass Formation and Bishop
Conglomerate in the Rock Springs uplift area. These aquifers are
characterized by good interstitial permeability, particularly in
conglomerate zones. Transmissivities are generally 1,000 gpd/ft
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or less, with specific capacities ranging from less than 1 to 1.5
gpm/ft.
Chemical data for the eastern part of the area indicate TDS
levels generally below 500 mg/1, primarily as calcium bicarbonate.
No data are available for the western part of the area.
d. The Mesaverde aquifer is a major aquifer throughout the
study area, but, due to water quality variability, it is
considered an important water source only near outcrop areas on
the structural uplifts in the eastern and western parts of the
study area. Major producing members within the aquifer include
the Ericson Formation, and to a lesser degree, the Almond and Rock
Springs formations. Transmissivity estimates for the Mesaverde
aquifer are generally less than 3,000 gpd/ft, though much lower in
the uppermost part of the aquifer (Almond Formation).
Mesaverde outcrop waters generally contain less than 1,000 mg/1
TDS, principally as sodium-bicarbonate. Water quality degrades
rapidly away from outcrop, with TDS levels exceeding 10,000 mg/1
in mid-basin areas where the aquifer is deeply buried.
3. All of the water-bearing units below the Baxter Shale
(Frontier, Cloverly, and Sundance-Nugget aquifers and the Paleozoic
aquifer system) are considered important sources of water only in the
vicinity of their outcrops, where drilling depths are shallow, and
these aquifers produce low TDS (<1,000 mg/1) waters. The major ion
composition of near-outcrop waters varies from calcium-magnesium-
bicarbonate to sodium sulfate. Salinity increases rapidly away from
outcrop, generally exceeding 10,000 mg/1 in all pre-Baxter aquifers.
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4. Ground-water movement within the Great Divide and Washakie
basins is generally from topographically high areas along the basin
peripheries toward discharge areas in the basin centers. However,
available data also indicate some discharge across the western basin
boundaries into the Green River basin, and from the Washakie basin into
the Sand Wash basin in Colorado. Interaquifer flow across the Baxter
Shale is highly restricted, as indicated by segregation of ground-water
chemistries.
5. Total estimated water use in the Great Divide and Washakie
basins is 80,000 to 89,000 acre-feet/year. Industry uses about 46,000
acre-feet/year. Half the industrial use (25,000 acre-feet/year) is
surface water diverted from the Green River for power plant cooling.
The remainder (21,000 acre-feet/year) is ground-water use, which is
evenly used by the petroleum, coal and uranium industries. Agriculture
uses 31,000 to 39,000 acre-feet/year, 95 percent of which is surface
water used for irrigation. The remainder (1,800 acre-feet/year) is
ground water used for either irrigation or stock watering. Estimated
public and private domestic water use is 3,000 to 3,600 acre-feet/year,
of which 2,400 acre-feet/year is surface water.
The majority of ground water withdrawn in the Great Divide and
Washakie basins is derived from the Tertiary aquifer system and, where
drilling depths permit, the Mesaverde aquifer. Petroleum industry
ground-water withdrawals are principally oil well by-product water
derived from Paleozoic rocks.
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II. GENERAL DESCRIPTION OF
STUDY AREA
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II. GENERAL DESCRIPTION OF
STUDY AREA
POPULATION AND LAND USE
The study area encompasses approximately 10,500 square miles
located in parts of Sweetwater, Carbon, and Fremont counties in south-
central Wyoming (Figure II-l). It extends from T. 12 N. to T. 26 N.,
inclusive, and from R. 86 W. to R. 103 W., inclusive.
According to the 1980 preliminary census data, the total popula-
tion of the area is 15,000, or about 1.4 people per square mile (Table
II-l). Most of the population is centered about the city of Rawlins
(1980 population: 11,547), which is the county seat for Carbon County.
Practically all of the residents of Sweetwater County live in towns,
oil company camps, or residences near the highways. Vast areas of this
region are uninhabited.
More than 50 percent of the land in the area is public domain,
administered by the Bureau of Land Management. Most of the remaining
land is owned by the Union Pacific Railroad, controlling nearly all
odd-numbered sections for 20 miles north and south of the railroad,
which roughly bisects the area.
The principal mineral resources of the region are natural gas,
oil, coal, oil shale, uranium, and sodium sulfate salts. Gas and oil
development is one of the most important stimulations to the local
economy. There are also large reserves of high-grade coal. Oil shale
occurs in the Green River Formation, especially in the Washakie basin.
Uranium-bearing ores have been found in the Great Divide (Pipiringos,
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Figure II-l. Great Divide and Washakie basins study area.
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Table II-l. Population of the Great Divide and Washakie basins.
1980
County Locality Population
Carbon Baggs 433
Dixon 82
Rawlins 11,547
Rural areas 1,037
Sweetwater South Superior 586
Wamsutter 681
Rural areas 634
TOTAL 15,000
U.S. Department of Commerce, Bureau of the Census, 1980 Census of
Population and Housing Preliminary Reports, Wyoming.
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1961) and Washakie (Vine and Prichard, 1954) basins and on Miller Hill
south of Rawlins (Vine and Prichard, 1959), but the only commercial
production in the area is in the southeastern Washakie basin, west of
the town of Baggs. Sodium sulfate salts were being mined in 1964 from
Bull Lake, 25 miles north of Rawlins in T. 25 N., R. 89 W. (Young,
1951); other commercial deposits may be present in the playa lakes in
the Great Divide basin.
In addition to mining, transportation, tourist trade, and agri-
culture are the basic industries in the region. Agricultural
activities include sheep and cattle raising throughout much of the area
and farming in the Little Snake River valley, where approximately
20,000 acres are cultivated.
With the exception of several species of sagebrush (Artemesia),
more than 90 percent of the region supports little vegetation, although
pine, spruce, and aspen grow at the higher altitudes (Welder and
McGreevy, 1966).
TOPOGRAPHY AND DRAINAGE
The greater part of the study area is occupied by two large,
centrally located basins: the Great Divide basin, also known as the
Red Desert basin in the north, and the Washakie basin in the south. In
general, the topography of both basins is controlled by and coincides
with the major basin and uplift structural features.
The basins are characterized by low-lying plains that grade upward
into relatively rugged uplifts, including the Sierra Madre uplift and
Rawlins uplift in the east; the Wind River Mountains and Granite
Mountains uplift in the north; the Rock Springs uplift in the west; and
the Cherokee Ridge along the Wyoming-Colorado state line in the south
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(Figure II-l). The Wamsutter arch, a broad subsurface structural
feature, structurally separates the basins.
The Great Divide basin is a large structural and topographic basin
having an area of about 3,500 square miles. Altitudes range from 6,467
feet in T. 24 N., R. 94 W., section 32, near the center to more than
8,000 feet in some of the adjacent highlands. The rounded ridge and
valley topography along the margins has a maximum relief of as much as
400 feet, but toward the middle of the basin vast stretches of sand
dunes and playa lakes generally have less than 100 feet of relief.
Some parts of the basin are topographically closed and almost no
precipitation leaves as surface runoff. Precipitation to the basin
seeps into the ground, evaporates, or flows into large playa lakes
where additional evaporation and seepage take place. A few of the
lakes, such as Hansen Lake in T. 23 N., R. 93 W., section 16, are also
fed by springs and contain water during most of the year.
The Washakie basin is about 2,600 square miles in area. Topog-
raphy in the basin is characterized by high rock rims on the north and
southwest, and by isolated, irregularly shaped highlands and lowlands
elsewhere. Altitudes range from 6,100 feet near the Little Snake River
in the southeast to 8,700 feet at Pine Butte on the west margin. Most
of the streams in the basin, except for those such as the Little Snake
River and Bitter Creek, flow only for short periods in response to
precipitation. Drainage is westward to the Green River and southward
to the Little Snake River, and is part of the Colorado River system.
The topography of the Rock Springs uplift, an area of about 1,400
square miles, consists of a central basin and surrounding ridges and
mountains. Altitudes average about 6,400 feet in the Baxter basin and
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over 7,000 feet in the highlands. The lowest point (6,200 feet) is in
Bitter Creek at the west side of the uplift, and the highest point
(8,680 feet) is on Aspen Mountain in the south half of the uplift.
Several igneous extrusive rocks in the north part of the uplift, known
as the Leucite Hills, have altitudes in excess of 7,500 feet. Stream
drainage is toward Bitter Creek, -which flows westward across the middle
of the structure to the Green River. Little Bitter, Salt Wells, and
Killpecker creeks flow intermittently for much of the year in response
to runoff from precipitation and discharge from springs.
The Sierra Madre uplift is topographically higher than other major
structures in the study area; altitudes average more than 7,000 feet
and range from 6,330 feet in the bed of the Little Snake River near
Dixon to 11,007 feet on Bridger Peak.
The Rawlins uplift, an area of about 350 square miles, has rugged
topography and altitudes that range from 6,400 to 7,800 feet. The
Continental Divide, which separates drainages of the Colorado and
Missouri rivers, crosses the uplift 4 miles north of Rawlins, and
encircles the northeastern half of the Great Divide basin.
CLIMATE
The climate of the study area is characterized by low precipita-
tion, rapid evaporation, and a wide temperature range. The summers are
usually dry and mild and the winters are very cold. Summer days are
occasionally hot, but wind and low humidity make the nights rela-
tively cool.
The average annual precipitation at Rawlins in the eastern part of
the study area is 11.3 inches; the highest recorded precipitation is
17.0 inches (1912) and the lowest is 3.8 inches (1907) (Berry, 1960).
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At Wamsutter, near the center of the study area, and Rock Springs, just
west of the study area, precipitation averages 6.3 and 7.0 inches per
year, respectively (Welder and McGreevy, 1966). Welder and McGreevy
(1966) also indicate that some of the highlands surrounding the basins
probably receive 12 to 15 inches of precipitation per year, and part of
the Sierra Madre uplift may receive as much as 35 inches in some years.
Precipitation is greatest in the spring and summer months, particularly
in May and August.
The mean annual temperature is 43.5°F at Rawlins and the length of
the growing season generally is about 4 months. In 1953, however, the
last day in the spring having a temperature below 32°F was June 25, and
the earliest day in the fall having a temperature below 32°F was
September 3 (Berry, 1960). The temperature extremes for 18 years of
record at Wamsutter are -37°F and +104°F, and the average annual
temperature is reportedly 42°F (Welder and McGreevy, 1966).
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III. GEOLOGY AND
HYDROSTRATIGRAPHY
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III. GEOLOGY AND
HYDROSTRATIGRAPHY
GEOLOGIC OUTCROPS AND STRATIGRAPHIC
SEQUENCE
The geologic formations that underlie the study area range in age
from Precambrian to Recent. Figure III-l is a general surficial
geology map for the area. About 75 percent of the rocks exposed at the
surface are post-Cretaceous in age and about 22 percent are of
Cretaceous age; the remaining outcrops are Jurassic through Precambrian
in age.
A generalized geologic column for the area indicating formation
types and stratigraphic sequence is given in Figure III-2. Descrip-
tions of individual formations are provided in Table V-l (Chapter V).
Figure III-3 shows two east-west and one north-south geologic
sections through the study area; locations of the cross-sections are
shown in Figure III-4. The Precambrian basement consists of igneous
and metamorphic rocks with outcrops that are found mostly in the Sierra
Madre uplift in the southeastern part of the area and in some smaller
uplift areas in the north and northeast. In the remaining part of the
area, the Precambrian is overlain by variable but generally large
thicknesses of sedimenary rocks. The greatest thicknesses of
sedimentary formations in the area are found in the eastern part of the
Great Divide basin and the central Washakie basin. Sedimentary rocks
in the Washakie basin may have a thickness in excess of 25,000 feet
(Welder and McGreevy, 1966).
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Figure III-l. General surficial geology, Great Divide and Washakie
basins.
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Figure III-2. Generalized geologic column, Great Divide and
Washakie basins.
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Paleozoic rocks are characterized by an undifferentiated Cambrian
sandstone base overlain by the Mississippian Madison Limestone, and the
Pennsylvanian Amsden Formation and Tensleep Sandstone. The uppermost
Permian Phosphoria Formation is composed of dolomite and shale beds.
There are no rocks of Ordovician, Silurian, or Devonian age within the
report area. The Paleozoic formations in the area are primarily marine
shelf deposits with a maximum reported thickness of about 2,600 feet in
the deepest part of the Great Divide basin, though some units thin out
or are even absent toward the southeast (Keller and Thomaidis, 1971).
The Triassic and Jurassic rocks of the Mesozoic are essentially
shelf or shelf-marginal marine sediments about 3,000 feet thick. Lower
units are composed of siltstone, sandstone, and shale in the Dinwoody
and Chugwater formations. They are overlain by the Nugget Sandstone
and limestones and shales of the Sundance Formation.
Cretaceous deposits consist of alternating and intertonguing sand-
stone and shale formations. Thick sandstones are found in the
Cloverly, Frontier, Mesaverde, and Lance formations. Shales of the
Thermopolis, Mowry, Frontier, Niobrara, Baxter, and Lewis formations
comprise several thousand feet of cumulative thickness.
Tertiary deposits are composed of intertonguing sandstones, silt-
stones, and shales. Sandstones are found in the Wasatch, Battle
Spring, Fort Union, Browns Park, and North Park formations. Conglom-
erate and sandstone comprise the South Pass Formation and Bishop
Conglomerate. The Bridger and Uinta formations are primarily clay-
stones and siltstones. The Green River Formation consists of fine-
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fsj
o
EXPLANATION
O Water Well
® Oil Well
A Spring
© unidentified well
Tma- Moonstone-Arikaree formations
Tnp - North Park Format ion
Tbp - Browns Park Formation
Tgr - Green River Formation
Tgl - Laney Member (Green River Formation)
Tbs - Battle Spring Formation
Tw - Wasatch Formation
Twc - Cathedral Bluffs Member (Wasatch Formation)
Tfu - Fort Union Formation
Tu - Tertiary undivided
Kl - Lance Formation
Kfh - Fox Hills Sandstone
Kle - Lewis Shale
Kal - Almond Formation
Ke - Ericson Formation
Kr - Rock Springs Formation
Kbl - Blair Formation
Kmv- Mesaverde Formation
Kb-Kst-Baxter-Steele Shole
Kc - Cody Shale
Kn - Niobrara Formation
Kf - Frontier Formation
Kmd- Muddy Sandstone
Kcv - Cloverly Formation
Kd - Dakota Sandstone
Kla - Lakota Sandstone
Jm - Morrison Formation
Js — Sundance Formation
Jr - Nugget Sandstone
¦Be - Chugwater Group
Pp - Phosphoria Formation
fff - Tensleep Sandstone
IPo - Amsden Formation
Mm - Madison Limestone
¦Gf - Flathead Sandstone
•€ - Cambrian undivided
p-G - Precambrian
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Figure III-3. Structural cross-sections, Great Divide and Washakie basins (locations shown on
Figure III-4) .
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Figure III-4. Index map for structural and potentiometric cross-
sections .
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grained lacustrine shales with several discontinuous sandstones. The
maximum thickness of the Tertiary deposits is estimated at about 14,000
feet (Welder and McGreevy, 1966).
The Quaternary deposits in the study area include Pleistocene to
Recent sand, silt, and gravel deposits of glacial, lacustrine, aeolian,
and alluvial origin. The maximum thickness of these deposits is
approximately 70 feet (Welder and McGreevy, 1966).
STRUCTURAL GEOLOGY
The general structural setting of the Great Divide and Washakie
basins is depicted in Figure III-5 and Plate 1.
The Great Divide basin is a broad synclinal depression containing
up to 18,000 feet of Paleozoic through Recent sediments which uncon-
forraably overlie the Precambrian basement rocks. The axis of the
syncline generally trends northwest to southeast and is located
northeast of the basin center (Figure II-5). Maximum structural relief
in the basin is on the order of 20,000 feet (Keller and Thomaidis,
1971). North-south trending anticlines, the Rock Springs uplift and
the Rawlins uplift, bound the basin on the west and east, respectively.
Separating the Great Divide basin from the Wind River basin to the
north are a series of major structural features characterized by a
major thrust zone on the west side and complicated thrust and normal
faulting along the South Granite Mountains fault system to the east
(Figure III-5). For a descriptive summary of the structural and
tectonic history of the Granite Mountain uplift area, the reader is
referred to Heisey (1951), Berg (1961), Love (1970), and Sales (1971).
The Great Divide and Washakie basins are structurally separated by
the Wamsutter arch (Figure III-5). The Wamsutter arch is a broad,
23
-------
T3IN
Rock o
Springs
COLORADO
EXPLANATION
Approximate boundary of study area
Area of exposed basement rocks
-J > Anticlinal axis, showing direction of plunge
> Synclinal axis, showing direction of plunge
D
U
Normal fault
Thrust fault (teeth on upthrown side of thrust)
inch=approximately 20 miles
N
Figure III-5. Major structural features of the Great Divide and Washakie
basins (modified from Dana, 1962, and POMCO Geologic
Structure map (Plate 1)).
24
-------
east-west trending anticline with no surface expression (Berry, 1960;
Dana, 1962; and Welder and McGreevy, 1966); however, Precambrian rocks
along the arch are elevated as much as 9,000 feet above basement rocks
of the Washakie basin and 3,000 feet above the Precambrian underlying
the western platform of the Great Divide basin (Love, 1961).
The Washakie basin is a deep structural depression, smaller in
area and more symmetrical than the Great Divide basin. The axis of the
syncline plunges to the southwest and is located close to the center of
the basin (Figure III-5). Paleozoic through Recent sedimentary rocks
may have a thickness exceeding 25,000 feet in the central Washakie
basin (Welder and McGreevy, 1966). On the east and west sides, the
Washakie basin is bounded by anticlinal uplifts. Separating the basin
from the Sand Wash basin south of the Wyoming-Colorado border is a
complex series of east-west trending anticlines and normal faults
(Keller and Thomaidis, 1971). Undeformed Tertiary strata extend across
these structures (McDonald, 1975).
The major structural features between the study area and basins to
the west and east are the Rock Springs uplift, and the Sierra Madre and
Rawlins uplifts, respectively.
The north-south trending Rock Springs uplift (Figure III-5) is cut
by numerous normal faults with throws commonly less than 100 feet and
lengths exceeding 15 miles in some instances (Schultz, 1920). Maximum
structural relief at the crest of the uplift is estimated at about
17,000 feet (Love, 1961).
The Sierra Madre uplift (Figure III-5) is a westward thrust block
of Precambrian through Early Cenozoic rocks which extends southeastward
into the Park Range of Colorado. Anticlinal structures on the west
25
-------
flank of the uplift are genetically related to the westward thrusting
of the Sierra Madre fault block (Ritzma, 1949). Vertical and
horizontal displacements along faults associated with the Sierra Madre
uplift are not known.
The Rawlins uplift (Figure III-5) is a north trending asymmetric
anticline with steeply dipping strata on the west flank. Maximum
structural relief is estimated at 30,000 feet. A large reverse fault
on the west side of the uplift has a reported maximum displacement of
about 5,000 feet (Barlow, 1955).
HYDROSTRATIGRAPHY
Various data sources were utilized to identify water-bearing units
within the Great Divide and Washakie basin. Spring occurrence and flow
is an indicator of saturated, permeable zones within sedimentary
strata. Records of water well pump tests and completion intervals
provide quantitative data on the hydrologic properties and thicknesses
of producing zones. Petroleum test data can provide similar infor-
mation. Qualitative information on water-bearing capabilities is
determined by the lithologic, structural, and secondary features of the
rock units.
The hydrologic divisions to which the rock units within the study
area have been assigned are identified solely by their water-bearing
properties.
The term "aquifer system" is used in this report to identify a
group of water-bearing units with (1) relatively similar hydrologic
properties, and (2) the absence of extensive regional zones of low
vertical permeability that will greatly restrict vertical hydraulic
communication within the system. Therefore, an aquifer system
26
-------
typically contains a thick series of permeable zones with interbedded
low-permeability intervals, none of which are considered to effectively
isolate any specific water-bearing unit.
The term "aquifer" identifies a distinct water-bearing unit that
has regional extent and favorable water-bearing potential for exploita-
tion. Aquifers are positioned either within aquifer systems or
hydrologically isolated by regionally, extensive low-permeability
confining beds (aquitards). Aquifers are categorized herein as "major"
or "minor" based on their relative regional water-bearing potential.
A total of' eight water-producing zones, each consisting of a
single aquifer or a number of aquifers, have been identified using the
above criteria (Figure III-5). These are: (1) Quaternary aquifers,
(2) Upper Tertiary aquifers, (3) the Tertiary aquifer system, (4)
Mesaverde aquifer, (5) Frontier aquifer, (6) Cloverly aquifer, (7)
Sundance-Nugget aquifer, and (8) the Paleozoic aquifer system.
Ground-water occurrence and flow and ground-water quality in each zone
are discussed subsequently.
These aquifers and aquifer systems are separated by a number of
thick regional confining layers (aquitards) (Figure III-6). Although
the aquitards are often capable of transmitting small amounts of water
to wells and over large areas and time periods can provide significant
interformational flow, they serve principally to hydraulically isolate
the more highly permeable zones. The two thickest regionally extensive
aquitards are the Upper Cretaceous Lewis and Baxter shales, both more
than 2,000 feet thick over much of the area.
27
-------
Geologic Age Lithology
Formation
Hydrologic Role | Hydrologic Unit
Quaternary
Alluvlo^dune, lake.
ond glacial deposits
Discontinuous
Major Aquifer
Quaternary Aquifers
Tertiary
Upper
Cretaceous
o . o
North Pork, Browns Pork
ond South Post formations
ond Bishop Conglomorote
Discontinuous
Minor Aquifers
Upper Tertiary
Aquifers
Bridaer and Uinta
formations
Aquitard
Green River
Formation
Confining Unit
with Discontinuous
Aquifers
Wasatch and
Battle Spring
formations
Major
Aquifers
Fort Union
Formation
Major
Aquifer
O • O ¦ O . o o ¦ O ' o .
Lance Formation
Fox Hills Sandstone
Minor
Aquifer
Lewis
Shale
Major
Aquitard
Mesaverde
Formation
Major
Aquifer
Baxter Shale and
equivalents
Major
Aquitard
Frontier Formation
Minor
Aquifer
Tertiary
Aquifer
System
Mesaverde
Aquifer
Frontier
Aquifer
Lower
Cretaceous
Mowry Shale
TherrtiopoUs Shale
Aquitard
Cloverly Formation
Minor Aquifer
Cloverly Aquifer
Jurassic
Triassic
Permian
Pennsylvanian
Mississippian
Cambrian
Precambrian
Morrison Formation
Aquitard
Sundance Formation
Nugget Sandstone
Minor Aquifer
Chuguater Formation
Phosphoric Formation
Aquitard
/ r /'/[ ••
Tensleep Formation
Major Aquifer
1 ¦ 1 11
Amsden Formation
Aquitard
i''' ^ r
Madison Limestone
Major Aquifer
o
• o
O •
Undifferentiated
Combrlan Rocks
Major Aquifer
Preeombrlan Rocks
Minor Aquifer
Sundance-Nugget
Aquifer
Paleozoic
Aquifer
System
Figure III-6. Hydrostratigraphic column, Great Divide and Washakie basins.
28
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IV. WATER USE
-------
IV. WATER USE
Water use within the Great Divide and Washakie basins is estimated
to be 80,000 to 89,000 acre-feet/year (Table IV-1, Figure IV-1).
Industrial water demands, related to energy resource development and
power generation, are met by roughly equal volumes of surface and
ground water, and require about 46,000 acre-feet/year. Agricultural
water use, mainly surface water for irrigation, is estimated to be
31,000 to 39,000 acre-feet/year. Public and private domestic water use
is between 3,000 and 3,600 acre-feet/year, and is met primarily by
surface-water supplies. Estimates of total surface-water use vary from
56,400 to 64,400 acre-feet/year, with 25,000 acre-feet/year imported
from outside the basin. Annual ground-water use is estimated to be
between 23,000 and 24,500 acre-feet.
Appendix A details ground-water use for industry, irrigation, and
public drinking water supply. Figure IV-2 shows the areal distribution
of principal industrial users, all inventoried public drinking water
supplies, and irrigation wells. The areal and stratigraphic
distribution of permitted domestic use wells is shown on Plate 2.
INDUSTRIAL WATER USE
Total industrial water use is about 46,000 acre-feet/year in the
Great Divide and Washakie basins. Over half is surface water, diverted
from the Green River for power plant cooling use, and the remainder is
ground water. Ground-water use is evenly divided between petroleum,
coal, and uranium industry users, and all principal aquifers are
utilized.
30
-------
Table IV-1. Estimated water use in the Great Divide and Washakie basins (see text and Appendix A for
detailed information).
Economic Sector
Ground-Water Use
(acre-feet/yr)
Surface Water Use
(acre-feet/yr)
Total Use
(acre-feet/yr)
Industry
Petroleum
By-product water
Fresh water
Coal mining
Power production
Uranium mining
Agriculture
Irrigation
Stock watering
Public and Private Domestic Use
Community supplies
Non-community supplies
Private domestic supply
TOTAL
<20,562-21,550
7,492-7,550
6,510
982-1,040
<7,344
0
5,726-6,656
1,929
829
VL.100
1,158
767
54
337
<23,649-24,637+
^25 ,000
0
0
0
0
^25,000a
0
29,000-37,000
29,000-37,000
0
2,437
2,409
28
0
56,437-64,437
<45,562-46,550
7,492-7,550
6,510
982-1,040
<7,344
^25,000
5,726-6,656
30,929-38,929
2S,829-37,829
1,100
3,027b~3,595
3,176
82
337
<79,518-89,074
Diverted from the Green River.
Estimate based on total population, undivided by use class or water source.
-------
^GRICULTUffp
Totol Water Use
8.4 X I04 AF/y
Total Ground Water Use
2.4 X I04 AF/y
Livestock
Noncommunity
and Private
DRINKING
WATER
'NDUSTR^
Economic Sector
Percent total
water use
Percent total ground
water use
Percent total surface
water use
INDUSTRY
AGRICULTURE
DRINKING WATER
55
41
4
87
8
5
41
55
4
Figure IV-1. Percent total water use arranged by economic
sector. Shaded areas designate percent ground-
water use, unshaded areas designate surface-
water use.
32
-------
5o
EXPLANATION
© Municipal water supply
• Community
Public drinking
water supply
(non-municipal, inventoried)
o Non-community
Public drinking
water supply
(inventoried)
Oilfield with over 100
) acre feet/yr produced water
ft Oilfield with active
woterflood project
IP Coal mining
fTTl Uronium mining
~ Power plont
a Irrigation well
Number of woler wells
represented by symbol
S Indicates principal
water source is Surface
water
Scale
20
\ ®s
Figure IV-2. Areal distribution of water users.
33
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Petroleum Industry
The petroleum industry uses about 7,500 acre-feet of ground water
annually in the Great Divide and Washakie basin. Although most water
used is a by-product of petroleum production, about 13 percent is fresh
water used to enhance oil recovery through waterflooding.
In 1979, a total of 6,510 acre-feet of water were produced as a
by-product of oil and gas production at 61 active fields through 743
wells (Appendix A, Table A-l). An additional 45 fields with 133 wells
produced no water, according to operator reports. There are another 53
fields in the basins with no reported 1979 production; 20 of these
fields are classed as abandoned. Paleozoic and Lower Cretaceous strata
yield most of the produced water in the basins. The overlying Frontier
and Mesaverde formations produce significant amounts of gas, but little
associated water. Roughly 60 percent of the total produced water is
from Paleozoic strata at the Lost Soldier Field (T. 26 N., R. 90 W.).
A total of 3,676 acre-feet of water was injected during 1979 to
enhance petroleum recovery through waterflooding at 10 units in six
fields (Appendix A, Table A-2). Sixty percent of this water was
injected into the Tensleep Sandstone at the Lost Soldier and Wertz
fields.
Most secondary oil recovery projects in the study area inject
solely produced water. Those projects which use "fresh" (make-up)
water from other ground-water sources withdrew about 1,000 acre-feet in
1979. About 70 percent of the fresh water used for waterflooding in
the basins is derived from the Fox Hills Sandstone of the Tertiary
aquifer system and injected into the Mesaverde Formation at the Patrick
Draw Field (T. 18 N., R. 99 and 100 W.). More detailed information on
34
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water injection projects in Wyoming can be found in Collentine and
others (1981).
Coal Industry
The two active coal mines within the Great Divide and Washakie
basins produced an estimated 6,900,000 tons of coal from the Fort Union
Formation in 1979 (Glass, 1980). Production levels should double in
the next few years as the Black Butte Mine becomes fully developed.
Currently most coal production in the basin is utilized in the Jim
Bridger Power Plant, with expected production increases contracted to
out-of-state users.
The active coal mines in the basin hold 13 water well permits with
permitted yields totaling 4,500 gpm (Appendix A, Table A-3). If fully
utilized, the maximum permitted ground-water use is 7,344 acre-feet/
year, but intermittent production by these wells is expected. Exact
water use data are unavailable. The primary coal mine water use is for
dust control; other uses include equipment washdown and irrigation.
The Bridger Coal Company obtains its water from pit dewatering
wells completed in the Fort Union Formation of the Tertiary aquifer
system, while the Black Butte Coal Company taps the Ericson Formation
of the Mesaverde aquifer.
The Jim Bridger Power Plant is a 4-unit, 2,000-megawatt, coal-
fired steam-generated electric power plant operated by Pacific Power
and Light. Approximately 25,000 acre-feet of cooling water, diverted
from the Green River, are used annually. Most waste water is
discharged to evaporation ponds but up to 750 acre-feet/year are used
for irrigation at the Jim Bridger Mine.
35
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Uranium Industry
The Crooks Gap-Green Mountain uranium district is located in the
northeastern part of the Great Divide basin and produces uranium from
the Tertiary Battle Spring Formation. Annual water use at the two
active mines is about 5,700-6,700 acre-feet (see Appendix A, Table
A-4), and is entirely derived from the Tertiary aquifer system. A
commercial scale in-situ mine, approved by the Wyoming Department of
Environmental Quality, has a planned plant capacity of 1,200 gpm;
little water will be used because fluids are to be recirculated in
closed cycle during both mining and restoration. Numerous uranium test
holes have also been drilled within the basins, but no water is
produced from these wells.
AGRICULTURAL WATER USE
Agriculture uses minimal amounts of water in the Great Divide and
Washakie basins, in comparison to the rest of the state. Total annual
water use is about 31,000 to 39,000 acre-feet, most of which is surface
water used for irrigation.
Irrigation
Little irrigation is conducted within the Great Divide and
Washakie basins, and most irrigated acreage is supplied by
surface-water rights along the Little Snake River. Permitted irri-
gation using ground water represents only one to two percent of total
irrigation.
Inventories of acreage with valid surface-water rights have been
conducted at various times (Smith and Associates, 1965; Worthington and
others, 1965; Wyoming Water Planning Program, 1971). Within the
36
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drainages of the Little Snake and Sweetwater rivers, Bitter Creek, and
the Great Divide basin, there are valid surface-water irrigation rights
for about 53,000 acres of land; over half are in the Little Snake River
drainage area and most of the remainder lie outside the basin
boundaries. Inventories of the amount of land irrigated in the same
area during 1968 and 1969 (Wyoming Water Planning Program, 1970 and
1971) determined that only approximately 22,000 acres of land were
actually irrigated, and almost two-thirds were in the Little Snake
River drainage.
Ground water is permitted as a source of irrigation water for
492.5 acres. It is obtained from 13 wells with a total permitted yield
of 7,766 gpm (Appendix A, Table A-5). The majority of water is derived
from the Mesaverde and Upper Tertiary aquifers.
Trelease and others (1970) determined irrigation water require-
ments of grass at four climate stations in the basins, using the
Blaney-Criddle method. They found water needs were 20.08, 21.90,
18.55, and 12.83 inches per acre per year at Rawlins, Wamsutter, Dixon,
and South Pass City, respectively. The first three stations, located
in more arid central basin areas, average 20.2 inches per year. On the
basis of acreage for which ground water is permitted as a water source
and this average water requirement, irrigation in the basins uses about
800 acre-feet of ground water annually. Assumptions incorporated into
this estimate include: (1) irrigation of 100 percent of permitted
acreage, (2) all irrigated acreage is grass or crops with similar water
needs, (3) 100 percent of calculated water needs are met, and (4) no
excess water is applied and lost as waste. Surface water use for
irrigation totals about 37,000 acre-feet/year using the same estimating
37
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technique. The actual amount of surface water used for irrigation may
be only 16 inches/acre/year (Wyoming Water Planning Program, 1970),
giving a lower water use estimate of 29,000 acre-feet/year.
Little increase in irrigated acreage in the Great Divide and
Washakie basins is anticipated (Wyoming Water Planning Program, 1970
and 1971) with the exception of the Savery-Pot Hook Project, which will
use surface water from the Little Snake River to irrigate an additional
7,000 acres of cropland.
Stock Watering
Sparseness of vegetation limits the numbers of cattle and sheep
within the Great Divide and Washakie basins; estimated populations are
53,800 cattle and 73,900 sheep. These estimates are derived from 1979
county stock population reports (Wyoming Crop and Livestock Reporting
Service, 1979), proportionally divided on the basis of county area
within the study area boundaries.
Total stock use of water is about 1,100 acre-feet/year based on
estimated populations and consumption rates of 15 and 3 gpd per capita
for cattle and sheep, respectively. The proportion of stock water
supplied by surface sources is presumed small due to the scarcity of
dependable surface flow. Because stock water from underground sources
is typically supplied by shallow, low-yield, intermittently producing
wells at the point of use, the major ground-water source for stock
water is the areally extensive Tertiary aquifer system.
PUBLIC AND PRIVATE DOMESTIC WATER USE
Drinking water supplies can be divided into public and private
systems. Public systems include community systems, serving more than
38
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25 permanent residents, and noncommunity systems, serving less than 25
permanent residents but a transient population greater than 25. Within
the Great Divide and Washakie basins there are 12 community systems and
15 noncommunity systems listed in the U.S. Environmental Protection
Agency Public Water System Inventory (1979) (see Appendix A, Tables A-6
and A-7).
The total number of completed wells permitted by the Wyoming State
Engineer for domestic use within the basin boundaries was 202 as of
February, 1980. The locations of these wells are shown on Plate 2,
which also identifies source aquifers.
Estimated total public and private domestic water use in the Great
Divide and Washakie basins is 3,027 acre-feet/year, based on a popula-
tion of 15,000 and per capita use of 180 gpd. Estimated use by
individual supply class (U.S. Environmental Protection Agency, 1979)
totals 3,595 acre-feet/year, which is somewhat higher than the above
estimate. Community systems account for 88 percent of this higher
total (3,176 acre-feet/year) and noncommunity systems account for only
82 acre-feet/year. Private domestic use is estimated at 337 acre-feet/
year, based on a rural population of 1,671 and daily consumption of 180
gallons per capita.
Over two-thirds (2,437 acre-feet/year) of the total estimated
domestic water use is surface water, diverted from the North Platte
drainage basin to supply Rawlins, the Little Snake River to supply
Baggs and Dixon, and the Green River to supply the Jim Bridger Power
Plant. Ground-water sources supply most of the remaining 590 to 1,158
acre-feet/year of water used for domestic purposes, generally through
intermittently pumped, relatively shallow wells at the point of use.
39
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The principal aquifers utilized are the Tertiary aquifer system in much
of the area, Upper Tertiary aquifers (where present in the eastern
uplift areas), the Mesaverde aquifer near outcrops, and the Paleozoic
aquifer system near Rawlins.
40
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V. GROUND-WATER OCCURRENCE
AND FLOW PATTERNS
-------
V. GROUND-WATER OCCURRENCE
AND FLOW PATTERNS
This chapter presents a thorough description of individual water-
bearing zones, and discusses ground-water flow patterns within the
study area.
MAJOR WATER-PRODUCING ZONES
The water-producing zones discussed below range in age from
Quaternary to Precambrian, and will be considered in descending
stratigraphic order. The stratigraphic sequence of these zones and the
confining beds separating them can be seen in Figures III-2 and III-6.
Information on formation type, thickness, and water-bearing character-
istics are summarized in Table V-l. The results of aquifer tests and
yields of all wells and springs on record are tabulated by formation in
Appendix C. Transmissivity data based on estimated calculations from
drill stem tests and specific capacities are, at best, accurate only to
an order of magnitude. The methodology used to determine transmis-
sivity is described in Appendix D.
Quaternary Aquifers
The Quaternary aquifers consist of unconsolidated sand and gravel
formations, mainly of alluvial origin, interbedded with lake and wind-
blown sediments. The Quaternary sediments occur in several localities
throughout the Great Divide basin; in the Washakie basin, they occupy
the flood plains of the Little Snake River and its major tributaries,
Bitter Creek, Shell Creek, Vermillion Creek, and Alkali Creek (see
42
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TnbleV-1. Generalized stratigraphy, lithology and water-bearing characteristics of geologic formations in the Great Divide and Washakie basins/1
Period
Geologic Unit
Thickness (ft.)
Lithologic Description
Hydrologic Properties
Cenozo ic
Quaternary
0-70
Unconsolidated alluvial clay, siJt
sand and gravel along Kittle Snake River
vallev, playa lake deposits of clay,
silt, and sand present in Great Divide
basin, and sand dunes of northern Rock
Springs uplift, west-central Great
Divide basin and north of the Rawlins
uplift. Also glacial clay, silt, sand,
and gravel on the flanks of the Sierra
Madre Mountains.
Sand and gravel deposits capabLe of supplying
stock and domestic water supplies. Utilized
extensively in Little Snake River valley and
area north of Rawlins uplift. Well yields are
generally less than 30 gpm. Springs south of
Ferris Mountains flow up to 20 gpm. Trans-
missivity estimates from area east of Rock
Springs uplift are 168 to 560 gpd/ft.
Calculated permeabilities ^n same areas
range from 21 to 62 gpd/ft • Fine-grained
lake deposits will produce poor yields.
Tert iary
North Park
Format ion
0-800
Fine- to medium-grained sandstone,
tuff and limestone with a basal con-
glomerate member up to 100 feet thick.
Present in the northwest Sierra Madre
uplift.
Minor aquifer that supplies excellent quality
spring water to City of Rawlins. Three wells
yield 4 to 20 gpm. Transmissivity estimates
from two pump tests are 150 and 1,000 gpd/ft.
Specific capacity values from same tests are
.06 and 1.43 gpm/ft.
-F-
OJ
Browns Park
Formation
0-1,200 Sandstone, tuffaceous, sandy clay-
stone, and conglomerate. Present on
the Rock Springs uplift, southern
Washakie basin, western Sierra Madre
uplift and possibly along the northern
edge of the Great Divide basin. Basal
conglomerate up to 100 feet thick with
quartz and quartzite boulders, cobbles,
and pebbles in sandstone and volcanic
ash. Uranium occurrences near Baggs,
Wyoming.
Unit is considered an excellent aquifer with
good interstitial permeability, particularly
in the basal conglomerate zone. Well yields
range from 3 to 30 gpm with specific
capacities generally between 0.03 and 1.0
gpm/ft (10 wells). Transmissivity estimates
are 100 to 10,000 gpd/ft. Numerous springs
maintain base flow of streams soutli of the
Rawlins area. One spring flows 343 gpm.
Possible saturated zone 870 feet thick, based
on water depths in wells.
Bishop
Conglomerate
0-200+
Conglomerate with well rounded
boulders and cobbles of quartzite
limestone and schist. Present in
southern Rock Springs uplift area.
Major aquifer in Rock Springs uplift area,
though absence of thick, saturated zones
limits well yields. One well yields 42 gpm.
Good interstitial permeabiJity.
Ui nta
Formation
Br idger
Forma t ion
(Washakie
Formation
in
Wa shakie
Basin )
0-3,200+ Tuffaceous claystone with tuffaceous,
fine-grained, lenticular sandstone
and minor amounts of shale, lime-
stone, and dolomite. Present mainly
in central Washakie basin.
Tuffaceous clastic sediments present
in NW Great Divide basin.
Relatively impermeable unit with only one
questionably identified well and no spring
data reported. Very low yields are expected.
Green River
Formation
(includes Tipton,
Wilkins Peak, and
Laney members)
0-1,500 Generally, a thick lens of fine-
grained, calcareous lake sediments-
oil shale, mudstone, shale and
sandy mudstone, with few, relatively
thick sandstone lenses, particularly
in the upper part of the unit (Sand
Butte Bed of Laney Member), and some
evaporite deposits in the middle
part (Wilkins Peak Member).
Laney Member of the Green River Formation
includes sandstone lenses which yield up to
200 gpm to wells, particularly in the western
Washakie basin. Other members are relatively
impermeable and would produce very low yields
to wells. Laney transmissivities range from
110 to 300 gpd/ft. Permeability in the Laney
averages around 10 gpd/ft ^ and the storage
coefficient is between 3.4 x 10"-* and 5.9 x
10 .
-------
Table V-l.
(cnnii nued)
Era Per iod Geologic Unit Thickness (ft.
Cenozolc Tertiary Wasatch Formation 0-4,000+
Battle Spring 0-4,700
Formation
-[>
-P-
Fort Union 0-2,700+
Format ion
MesozoLc Upper Lance Formation 0-4,500+
Cretaceous
Fox Hills
Sandstone
0-400
Lithologic Description
Hydrologic Properties
Claystone, siltstone, fine-to medium-
grained, calcareous sandstone,
carbonaceous shale, oil shale, and
coal. Grades eastward into Battle
Spring Formation in eastern Great
Divide basin.
Major aquifer of Tertiary aquifer system.
Numerous water-bearing sandstone lenses yield
5 to 250 gpm (^90 wells) though most yields
are 30 to 50 gpm. Wells tapping the lower
sands are artesian in some areas. Trans-
missivity estimates from 9 pump tests are 150
to 10,000 gpd/ft. Specific capacities for
same wells range from 0.17 to more than 10
gpm/ft. Porosity and permeability from 6 oil
field reports are 16 to 38 percent and 0.04
to 18.2 gpd/ft , respectively. Yield-drawdown
relationships from 5 wells indicate possible
yields of 500 gpm from thick, saturated
sequences.
Arkosic, fine-to coarse-grained
sandstone and claystone with boulder
conglomerate near the Green Mountains.
Intertongues with Wasatch and Green
River formations to the west.
Uranium deposits in Crooks Gap area.
Fine-to coarse-grained sandstone,
carbonaceous shale, and coal with
minor siltstone and claystone in '
the upper part.
Very fine- to fine-grained, clayey,
calcareous sandstone with shale, coal
and lignite. Sandstone lenses up to
20 feet thick at intervals within the
formation near Rawlins.
Fine-to medium-grained, cross-
stratified, calcareous sandstone.
Major aquifer of eastern Great Divide basin.
Well yields range from 1 to 157 gpm. Estimates
of transmissivity are 29 to 3,157 gpd/ft from
26 test wells. Specific capacity is typically
less than 1 gpm/ft. Pay zone porosity at one
oil field is 15 to 25 percent. Estimated
coefficient of storage is 1 x 10
Major aquifer, particularly around the
periphery of the basins. Water-bearing
sandstones are lenticular causing
discontinuous, isolated water-bearing
zones. Well yields range from 3 to 300 gpm
Transmissivity estimates are generally less
than 2,500 gpd/ft. Porosity and permeability
are 15 to 39 percent and less than 1 gpd/ft ,
respectively, based on oil field and coal mine
reports. Specific capacity ranges from less
than 0.001 to 75 gpm/ft (6 pump tests).
Permeability is largely fault-related on east
side of Rock Springs uplift.
Minor aquifer of Tertiary system with
well yields typically less than 25 gpm.
Transmissivity estimates are generally less
than 20 gpd/ft with two estimates of 150 and
200 gpd/ft. Oil field porosity and permeabil-
ity are 12 to 26 percent and 0.007 to 8.2
gpd/ft'
respectively.
Minor aquifer at base of Lance Formation.
Well and spring yields not available. Oil
field reports indicate pay zone porosity,
permeability, and transmissivity of 20 percent,
0.9 gpd/ft , and 10 to 20 gpd/ft,
respec tively.
-------
Table V-l. (continued)
Era Period Geologic Unit Thickness (ft~ )
Mesozoic Upper Lewis Shale 0-2,700+
Cretaceous
Mesaverde 0-2,800
Formation (2,200-5,600
(Mesaverde Group on west
near Rock Spring side of
Uplift includes study area)
Blair, Rock Springs,
Ericson, and Almond
format ions)
.in
Ln
Baxter Shale
(includes Cody
and Steele shales,
and Niobrara
Format ion)
2,000-5,000+
Frontier
Formation
190-900+
Lower Mowry Shale 150-525
Cretaceous
Thermopolis 40-235
Shale (20-155)
(includes Muddy
Sandstone
Member)
Cloverly 45-240
Format ion
Lithologic Description
Hydroloftlc Properties
Calcareous to non-calcareous,
carbonaceous shale, with numerous beds
of siltstone and very fine-grained
sandstone.
Massive, very fine- to medium-grained
sandstone with carbonaceous shale,
lignite and coal.
Aquitard between underlying Mesaverde aquifer
and overlying Tertiary aquifer system.
Mostly impermeable shale, but scattered sand-
stone lenses may be capable of yielding stock
supplies. Porosity ranges from 6 to 24
percen^, permeability from 0.002 to 0.9
gpd/ft
gpd/ft ,
and transmissivity from 0.03 to 50
based on oil field data.
Major aquifer throughout study area. Maximum
well yield is 470 gpm from Rock Springs
Formation. Most reported yields are less than
100 gpm. Transmissivity estimates are
generally less than 3,000 gpd/ft and much
lower in the uppermost part of the aquifer
(Almond Fm). Porosity ranges from 8 to 26
percent. Ericson Formation is best water
source near Rock Springs uplift.
Shale with minor, interbedded sand-
stone, siltstone, and limestone.
Major regional aquitard between Mesaverde and
Frontier aquifers throughout area west of
Rawlins uplift. Thin sandstone beds may yield
small quantities of water; however, high TDS
concentrations are likely.
Sandstone and shale with bentonite
beds and lenses of chert-pebble
conglomerate.
Productive aquifer, particularly in the
eastern part of the study area near outcrop.
Yields range from 1 to more than 100 gpm with
specified capacities between 0.29 and 30 gpm/ft.
Transmissivity estimates from water well pump
tests were 15,000 to 20,000 gpd/ft; however,
drill stem test transmissivities were generally
less than 100 gpd/ft with a maximum of 6,500
gpd/ft. Variability probably due to varying
percentage of bentonite and shale within the
tested interval.
Siliceous shale with siltstone and
bentonite.
Unit is considered a regional aquitard. Well
and spring data are not available.
Fissile shale containing a few thin
beds of sandstone, siltstone, and
bentonite. The Muddy Sandstone
Member consists of fine-grained,
shaly sandstone and interbedded
siltstone and shale.
Unit is considered a leaky confining unit;
however, water is produced from the Muddy
Sandstone Member at oilfields in the north-
east Great Divide basin. Well and spring
data are not available.
Sandstone, shale, conglomerate,
and a lesser amount of siltstone.
Major Mesozoic aquifer which crops out on
Rawlins uplift. Deeply buried over most of the
study area. Water well yields range from 25
to more than 120 gpm with specific capacities
between 0.26 to 1.36 gpm/ft. Water well and
drill stem test transmissivities are 340 to
1,700 and 1 to 177 gpd/ft, respectively.
-------
Table V-l.
(com inucd)
Em
Per iod
Geologic Unit
Thickness (ft.)
Lithologic Description
Hydrologic Properties
Mesozoi c
Upper Jurassic Morrison Formation
170-450+ Variegated claystone, shale, lenticular
sandstone, and minor conglomerate and
limestone.
Confining unit between the Cleverly
and Sundance-Nugget aquifers. Well
spring data unavailable.
and
Sundance Formation
130-450+ Sandstone, shale, siltstone, and
limestone; upper part is glauconitic.
Upper unit of the Sundance-Nugget aquifer.
Artesian flow to several wells in Rawlins area-
Well yields between 27 and 35 gpm (3 wells).
Specific capacity at one well is 0.17 gpd/ft.
Transmissivity ranges from 12 to 3,500 gpd/ft.
Lower
Jur ass ic-
Upper
Triassic
Nugget Sandstone
0-650+
Fine- to medium-grained sandstone with
minor, interbedded shale and siltstone.
Lower unit of the Sundance-Nugget aquifer. Two
well yields reported, 35 and 200 gpm. Maximum
transmissivity from drill stem tests was 2,166
gpd/ft.
Triassic
Chugwater
Forma t ion
900-1,500+
Shale, siltstone and interbedded,
fine-grained sandstone.
Generally considered a confining unit between
Sundance-Nugget aqtiiferand Paleozoic aquifer system.
Hydrologic data not available for Chugwater.
-P>
ON
Mesozoic-
Paleozoic
Lower
Tr iass ic-
Permian
Phosphoria
Formation
(i ncludes
Phosphoria
Formation and
intertonguing
Permian Park City,
Goose Egg and
Lower Triassic
Dinwoody
formations)
170-460
Interbedded shale, siltstone, sand-
stone, and limestone.
Water-bearing capabilities for these formations
are unknown in the study area, but are probably
poor, due to low permeability of the rock units.
Paleozoic
Permian-
Pennsylvanian
Tensleep Formation
0-840+
Fine- to medium-grained, quartzitic
sandstone and lesser amounts of thin,
interbedded limestone and dolomite.
Absent in the southeast part of the
area. Crops out on Rawlins uplift.
Important water-bearing zone of Paleozoic
aquifer system. WeLl yields range from 2'» to
400 gpm. One spring flows 200 gpm in Rawlins
area. Transmissivity is generally low, ranging
from 1 to 374 gpd/ft.
Lower and
Midd1e
PennsyIvan i an
Amsden Formation
0-260+
Sandstone, shale, and siltstone with
cherty limestone. Approximately 60
feet of basal, fine-grained sand-
stone (Darwin Sandstone Member).
Amsden is absent in the southeast
part of the area.
Hydrologic data are not available; unit
probably has poor water-bearing potential
due to predominance of fine-grained sediments.
Mississippian Madison Limestone
5-325+
Limestone, dolomite, and lesser
amounts of thin-bedded sandstone and
chert.
Major aquifer of Paleozoic system. Excellent
secondary permeability development due to
solution channeling, caverns, and fractures.
Well yields up to 400 gprc are reported with
specific capacities of 100 gpm/ft at two wells.
Reported transmissivities are highly variable.
-------
Table V-J.
(cone inued)
Era
Per iod
Geologic Unit
Thickness (f t.)
Lithologic Description
Hydrologic Properties
Pa 1 eo7.o ic
Cnmbrian
Und if ferent ia ted
Cambrian rocks
0-800+
Quartzitic, conglomeratic sandstone in
the lower part; upper part consists
of glauconitic sandstone and inter-
bedded siltstone, shale, and limestone.
Major water-bearing zone, especially near
Rawlins, where 13 wells are completed in
Cambrian units. Wells yield between 4 and 250
gpm. Specific capacities at two wells were
0.67 and 150 gpm/ft. Transmissivity data are
suspect.
Precambr ian
unknown Granite, gneiss, and schist exposed
in Sierra Madre and Rawlins uplifts,
and along northern edge of Great
Divide basin.
Frequently utilized aquifer in the north-
western corner of the Great Divide basin, near
South Pass City. Well yields typically range
from 10 to 20 gpm with specific capacities
between 0.5 and 2 gpm/ft. Most reported
transmissivity values are less than 1,000
gpd/ft. Generally high permeability in
fractured and weathered zone in upper 200 feet
of the unit.
4N
^ Data Sources: Berry, 1960; Black Butte Coal Mine Report; Bradley, 1945; Dana, 1962; Pipiringos, 1955; Randall, 1960; Roehler, personal communication,
1981; Roehler, 1973; Stephens, 1964; Sullivan, 1980; Welder and McGreevy, 1966; Wyoming Geological Association, 1979;
Woodward Clyde Consultants, 1980.
-------
Figure III-l). Maximum total thickness for the Quaternary sediments is
estimated at 70 feet.
Hundreds of water wells are completed in the coarse sand and
gravel of the Little Snake River Valley where yields of 25 to 50
gallons per minute (gpm) are common. One well in that area yields 300
gpm (T. 12 N., R. 91 W., section 5 ad). South of the Ferris and Green
mountains, wind-blown sand is typically 50 to 70 feet thick, and
reported well and spring yields range from 1 to 20 gpm. East of the
Rock Springs uplift, monitoring wells at the Black Butte Coal Mine
produced 5 to 30 gpm from the alluvium of Bitter Creek (Black Butte
Coal Co., 1981), though these waters are of generally poor quality
(Chapter VI).
Transmissivities in the alluvial aquifer near the Jim Bridger Coal
Mine (T. 19 and 20 N., R. 99 W.) are 168 to 500 gallons per day per
foot (gpd/ft) with calculated permeabilities of 21 to 62 gallons per
2
day per square foot (gpd/ft ) (Woodward-Clyde Consultants, 1980).
The Quaternary deposits are not productive everywhere they occur.
In the Rawlins area, Quaternary deposits generally lie above the water
table. The deposits are highly permeable, absorb rainfall and
ephemeral streamflow, and transmit it downward into the underlying
formations (Berry, 1960). The Quaternary lake deposits in the interior
of the Great Divide basin consist of predominantly fine-grained
sediments and are poor aquifers (Welder and McGreevy, 1966).
Upper Tertiary Aquifers
These aquifers consist of conglomerates and sandstones of the
Bishop Conglomerate, Browns Park Formation, South Pass Formation, and
North Park Formation. They vary in thickness depending on location,
48
-------
but generally are several hundred feet thick. These formations do not
overlie one another; they have been identified at different localities
and are considered ay equivalents. Major outcrop areas include the
Bishop Conglomerate in the southern part of the Rock Springs uplift;
the Browns Park Formation along the west side of the Sierra Madre
uplift; and the North Park Formation in the Rawlins area (Berry, 1960;
Welder and McGreevy, 1966).
The Upper Tertiary aquifers are either exposed at the land surface
or blanketed by a thin cover of Quaternary sediments. Locally, Upper
Tertiary deposits are separated from Quaternary deposits by intrusive
and extrusive rocks north of Rock Springs and east of Baggs (Love and
others, 1955).
Quantitative data from 43 water wells were used to evaluate the
hydrologic properties of the Upper Tertiary aquifers. Sources for the
well data are Dana (1962), Welder and McGreevy (1966), U.S. Geological
Survey well records, well permit records from the Wyoming State
Engineer's Office, and one preliminary coal mine report.
Well data indicate that the Browns Park Formation is the most
productive unit of the Upper Tertiary. This formation consists of
about 100 feet of basal conglomerate and up to 1,000 feet of fine- to
medium-grained sandstone. Water well yields of up to 30 gpm are
common. Berry (1960) reports that several Browns Park wells south of
Rawlins have reached water at only 5 to 128 feet, indicating a possible
zone of saturation at least 870 feet thick. One spring in that area
flows 343 gpm (Welder and McGreevy, 1966). It is also reported that
springs issuing along the contact of the basal Browns Park and the
49
-------
underlying less permeable units maintain the base flow of the perennial
streams in the southeastern part of the Washakie basin (Berry, 1960).
The yields of three wells completed in the North Park Formation,
located on the northwest side of the Sierra Madre uplift, range from 4
to 20 gpm. There is only one well on record that is completed in the
Bishop Conglomerate. This well, located in T. 16 N., R. 104 W.,
section 8, has a yield of 42 gpm. There are no wells on record that
are completed in the South Pass Formation.
Based on the results of pumping tests of ten Browns Park wells,
the aquifer transmissivity generally ranges from 100 to 1,500 gpd/ft.
One test result gives an estimate of 10,000 gpd/ft (T. 12 N., R. 91 W.,
section 9 ad). The results of tests of two North Park wells indicate
an aquifer transmissivity between 150 and 1,000 gpd/ft. Well specific
capacities from both formations were found to be on the order of 1
gallon per minute per foot of drawdown (gpm/ft).
The potentiometric gradients in the Upper Tertiary aquifers
generally conform with topography. Ground-water movement is from
topographically high areas along the flanks of the Sierra Madre uplift
toward topographically low areas in the valleys of the Snake River and
its tributaries, where the aquifers are partially or completely
dissected (Figure V-l).
Tertiary Aquifer System
The Tertiary aquifer system includes all formations between the
Laney Member of the Green River Formation and the Fox Hills Sandstone,
inclusive (Figure III-6) . This zone is separated from the overlying
Upper Tertiary aquifers by a large thickness of low-permeability clay-
stone and shale (Uinta and Bridger formations). The Lewis Shale
50
-------
Figure V-l. Potentiometric surface map, Upper Tertiary aquifers.
51
-------
constitutes the basal boundary for the Tertiary aquifer system and
separates it from the underlying Mesaverde aquifer.
Over the greater part of the study area, the formations of the
Tertiary system are exposed at the land surface or underlie Quaternary
and Upper Tertiary deposits. The Tertiary formations are missing in
those areas adjacent to the Rock Springs, Rawlins, and Sierra Madre
uplifts, where older rocks are exposed. The maximum thickness of the
Tertiary aquifer system is estimated between 11,000 and 12,000 feet in
the central Washakie basin (McDonald, 1975).
Hydrologic data for the Tertiary aquifer system are derived from
the records of 193 water wells and springs, and 13 oil field drill stem
tests. Other sources of information include Wyoming Geological
Association (1979). The sources for well and spring data are the State
Engineer's Office, the Wyoming Geological Survey, Welder and McGreevy
(1966), Dana (1962), Berry (1960), and numerous coal mine reports.
Each geologic unit within the Tertiary aquifer system is water-
bearing to some degree. The major aquifers, in order of importance,
are the sandstones and conglomerates in the Battle Spring, Wasatch, and
Fort Union formations, and the Laney Member of the Green River
Formation.
The Battle Spring Formation crops out over most of the eastern
Great Divide basin west of the Rawlins uplift. It is a stream and
deltaic facies of the Wasatch Formation composed of fine- to coarse-
grained, highly permeable, arkosic sandstone and conglomerate. The
Battle Spring is capable of yielding at least 150 gpm to water wells,
though most yields generally range from 30 to AO gpm. Welder and
McGreevy (1966) state that wells tapping the greatest thicknesses of
52
-------
the Battle Spring can have yields of over 1,000 gpm; however, specific
capacities for 23 of 26 tested wells were less than 1 gpm/ft. Data
obtained from pump tests for 26 water wells indicate a transmissivity
range between 29 and 3,157 gpd/ft, though most values are less than 500
gpd/ft. Transmissivity values from 11 aquifer tests in the area of
Minerals Exploration Company's proposed uranium mine (T. 22-26 N.,
R. 90-95 W.) averaged 40,000 gpd/ft, with a calculated average storage
-3 -5
coefficient ranging from 10 to 10 (Minerals Exploration Company,
1978).
The Wasatch Formation is an excellent source of water, par-
ticularly in the western Great Divide basin and along the axis of the
Wamsutter arch. In these areas it crops out or underlies younger,
permeable formations and has its highest percentage of sandstone
(Welder and McGreevy, 1966). In the Washakie basin, the Wasatch
intertongues with or underlies relatively impermeable claystone and
shale beds of the Green River, Bridger, and Uinta formations.
In the Great Divide basin, the discontinuous sandstones of the
Wasatch are generally fine- to medium-grained, coarsening toward the
southern end of the Wind River Mountains, where highly permeable
boulder conglomerates are present. Artesian conditions exist in many
of the sandstone lenses of the lower Wasatch Formation, especially in
the northwestern Great Divide basin (Dana, 1962; Welder and McGreevy,
1966).
Water well yields from the Wasatch Formation are typically between
5 and 50 gpm, though several wells completed in thick saturated
sequences produce between 200 and 325 gpm. Well specific capacities
less than 1 gpm/ft are characteristic of the Wasatch aquifer.
53
-------
Transmissivity estimates from water well and oil field aquifer
tests range from 1 to 100,000 gpd/ft, with the majority between 150 and
6,000 gpd/ft. Porosity and permeability estimates from Wasatch tests
at oil fields across the southern Washakie basin are 16 to 38 percent
2
and <1 to 18.2 gpd/ft , respectively (Wyoming Geological Association,
1979).
The Fort Union Formation underlies the Great Divide and Washakie
basins between outcrop areas on the east flank of the Rock Springs
uplift and the west flank of the Rawlins uplift. The thickness of the
Fort Union varies from less than 1,000 feet in the northern Great
Divide basin to approximately 2,500 feet immediately west of the
Rawlins uplift (Pipiringos, 1955; Berry, 1960; Weimer and Guyton, 1961;
Stephens, 1964; Welder and McGreevy, 1966). According to Woodward-
Clyde Consultants (1980) and Haun (1961), discontinuous lenticular
sandstone and conglomerate beds in the lower 200 to 500 feet of the
formation are integrated into one aquifer through possible fracture
zones.
Fort Union well yields are generally less than 100 gpm, although
yields of up to 300 gpm have been reported. Welder and McGreevy (1966)
suggest that yields as high as 500 gpm could be expected from a well
penetrating the thickest sections of the Fort Union. Oil field data
indicate a porosity range in Fort Union pay zones of 15 to 39 percent,
2
and permeabilities typically less than 1 gpd/ft (Wyoming Geological
Association, 1979). Transmissivities are characteristically less than
2,500 gpd/ft.
The Laney Member of the Green River Formation is present through-
out the Washakie basin. A band of Laney outcrop 3 to 10 miles wide
54
-------
encircles the central basin area. Within the central basin, the Laney
is buried by younger Tertiary age silts and shales. The Laney Member
is composed of fine-grained, calcareous mudstone and shale with several
relatively thick sandstone lenses. The thickness of the Laney Member
ranges from 900 to 1,200 feet in the western part of the basin and from
500 to 900 feet in the east, with a maximum reported thickness of 1,800
feet (T. 14 N., R. 97 W.) in the south-central area (Roehler, 1973a).
Wells completed in the Laney Member in the western Washakie basin
(Kinney Rim area) have reported yields of up to 200 gpm. Transmis-
sivities between 110 and 300 gpd/ft were estimated from Laney aquifer
tests at Ogle Petroleum's Bison Basin uranium mine site in the
northwestern Great Divide basin. Permeability reportedly ranges from
2 -5
7.4 to 13.0 gpd/ft ; the storage coefficient varies from 3.4 x 10 to
5.9 x 10~\
Ground-water producing capabilities from minor water-bearing units
of the Tertiary aquifer system—the Fox Hills, Lance, and Green River
(except the Laney Member)—are adequate for stock and domestic supplies
over most of the Great Divide and Washakie basin.
Oil field pay zone data indicate porosity, permeability, and
2
transmissivity values of approximately 20 percent, 0.9 gpd/ft , and 10
to 20 gpd/ft, respectively, for the Fox Hills Sandstone (Wyoming
Geological Association, 1979). Yields from stock wells in the Lance
Formation near outcrop areas on the west flank of the Rawlins uplift
are estimated between 5 and 30 gpm (Welder and McGreevy, 1966). Twenty
of 22 transmissivity estimates from the Lance Formation pump tests and
drill stem tests were less than 22 gpd/ft.
55
-------
No well data exist for specific members of the Green River
Formation, with the exception of the Laney Member. Welder and McGreevy
(1966) characterize ground-water possibilities from the Tipton and
Wilkins Peak members of the Green River Formation as very poor, due to
the low permeability of the marlstone, oil shale, and infrequent,
thinly bedded, fine-grained sandstones particularly in the central
Washakie basin. Eight water wells, identified as "Green River
Formation Undivided," yield 15 to 250 gpm; however, these wells may be
completed in the Laney Member and may not be indicative of well yields
from other members of the Green River Formation.
Potentiometric data for the Tertiary aquifer system (Figure V-2)
indicate that ground-water flow is from the high peripheral areas of
the Great Divide and Washakie basins toward the basin centers.
Although it has no surface expression, the Warasutter arch is a ground-
water divide for flow within the Washakie and Great Divide basins. The
Tertiary aquifer system is recharged primarily by outcrop-related
infiltration of snowmelt and streamflow, and by downward seepage from
overlying, permeable Miocene, Pliocene, and Quaternary sediments
(Welder and McGreevy, 1966). The areas of ground-water discharge
include the valleys and playas in the central part of the Great Divide
basin, particularly Chain Lakes flat and Battle Spring flat (Minerals
Exploration Company, 1978). Discharge areas in the Washakie basin
include springs along the Little Snake River and its tributary valleys,
and underflow to the Tertiary formations of the Sand Wash basin in
northwestern Colorado (Welder and McGreevy, 1966).
56
-------
EXPLANATION
Contour on poiint©m«tr< wrf«»,
dathad -here inferred (Contour
mtervol 250 (Ml)
Figure V-2. Potentiometric surface map, Tertiary aquifer system.
57
-------
Mesaverde Aquifer
The Mesaverde aquifer consists predominantly of fine- to medium-
grained sandstone interbedded with some shale and coal beds (Welder and
McGreevy, 1966; Hale, 1950). It is situated stratigraphically between
the major confining units of the Lewis Shale above and the Baxter Shale
and equivalents below. On the western side of the study area along the
Rock Springs uplift, this aquifer consists of, in ascending order, the
Blair, Rock Springs, Ericson, and Almond formations of the Mesaverde
Group. In this area, the maximum thickness of the aquifer ranges from
2,200 to 5,600 feet (Welder and McGreevy, 1966). To the east, the
Mesaverde is not subdivided, and has a maximum thickness of about 2,800
feet (Berry, 1960; Welder and McGreevy, 1966). Along the axes of the
Rawlins and Rock Springs uplifts, the Mesaverde has been eroded,
exposing older Mesozoic and Paleozoic geologic units. On the east
flanks of the Rock Springs uplift, the continuity of the Mesaverde is
disrupted by a series of east-west trending faults.
Quantitative data for the Mesaverde aquifer were obtained from a
number of sources, including well and spring permit records from the
Wyoming State Engineer's Office, the Wyoming Geological Survey, and
previous publications (Welder and McGreevy, 1966; Dana, 1962; Berry,
1960; and several coal mine reports).
Records of existing wells completed in the Mesaverde aquifer
indicate that in the western part of the study area, water is obtained
from all units within the Mesaverde Group, including the Blair, Rock
Springs, Ericson, and Almond formations.
The Ericson is the primary water-bearing unit with well yields
between 10 and 200 gpm (Dana, 1962; Welder and McGreevy, 1966). One
58
-------
well (T. 21 N., R. 101 W., section 21 ada) has a reported yield of 250
gpm from two Ericson intervals. Transmissivity values for the Ericson
Formation, estimated from two oil field drill stem tests, were 43 and
2,883 gpd/ft (see Appendix C).
The Rock Springs Formation constitutes a unit of permeable fine-
to medium-grained sandstone with good water-bearing capability (Hale,
1950). The records of nine wells completed in this unit indicate that
well yields vary between 2 and 470 gpm, though most wells produce
between 100 and 250 gpm. Reported porosity of one oil-producing zone
in the Rock Springs Formation is 10 percent (Wyoming Geological
Association, 1979).
The yields of four wells completed in the Blair Formation are 30
to 60 gpm from fine- to medium-grained sandstones in the upper part of
the formation. The lower part of the Blair is composed of relatively
impermeable interbedded shales and siltstones. Blair pay zone
porosities from two oil fields on the east flank of the Rock Springs
uplift are 16 and 19 percent (Wyoming Geological Association, 1979).
There are no available data to compute the permeability or transmis-
sivity for the Rock Springs and Blair formations.
The upper part of the Almond Formation consists of permeable
massive beds of fossiliferous sandstone which overlie low-permeability
carbonaceous shale, siltstone, mudstone, and coal beds of variable
thickness and quality. The upper sandstone has a reported porosity of
2
16 to 23 percent and permeability of <1 gpd/ft (Wyoming Geological
Association, 1979). One water well yield of 250 gpm was reported by
Dana (1962), and is the only available yield data for the Almond
Formation. Transmissivity values determined from two coal mine pump
59
-------
tests and 11 oil field drill stem tests were low, between 0.7 and 15.8
gpd/ft.
On the east side of the study area the Mesaverde Formation
consists mainly of fine- to medium-grained sandstone with localized
lenses of carbonaceous shale, lignite, and coal. Yields from five
wells completed in the Mesaverde in this area are between 15 and 40
gpm. Specific capacities determined from pump tests on these wells
varied from less than 2 to greater than 20 gpm/ft. Transmissivity
values from two of the wells were less than 3,000 gpd/ft. Transmis-
sivities estimated from five Mesaverde drill stem tests range from 4 to
67 gpd/ft. Reported data from 50 oil field test wells, the majority of
which are located in the Washakie basin, indicate a porosity range from
2
8 to 26 percent, and hydraulic conductivity between <1 and 1.8 gpd/ft
(Wyoming Geological Association, 1979).
Based on potentiometric data (Figure V-3), the general direction
of ground-water flow in the Mesaverde aquifer is from the recharge
areas toward the basin centers. Outcrop-related recharge to the
Mesaverde aquifer occurs along the Rock Springs, Rawlins, and Sierra
Madre uplifts. Recharge is mainly from infiltration of snowmelt and
streamflow (Welder and McGreevy, 1966). Little flow contribution is
supplied by the Tertiary aquifers due to the presence of the
intervening Lewis Shale.
Frontier Aquifer
The Frontier aquifer consists of sandstone and shale with a few
bentonite beds and lenses of pebble conglomerate (Welder and McGreevy,
1966). It underlies most of the study area and has a thickness of 190
to 900 feet. It crops out along the Rawlins uplift in the east and the
60
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Figure V-3. Potentiometric surface map, Mesaverde aquifer.
61
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Rock Springs uplift in the west. The formation dips from the east and
west toward the central part of the area; depth to the top of this
formation in the central parts of the Great Divide and Washakie basins
is estimated at over 8,000 feet.
Information on ground-water occurrence and water-bearing
characteristics for the Frontier is available from the records of 24
oil test wells, 21 water wells, and 2 springs. The great majority of
the water wells and all springs are located in the eastern outcrop
areas. The remainder of the wells are located in the western part of
the area in the vicinity of the Rock Springs uplift. About one-third
of the wells are flowing.
Based on the results of two short-term pump tests, the estimated
aquifer transmissivity is between 15,000 and 20,000 gpd/ft. Other
computations from results of drill stem tests indicate values usually
less than 100 gpd/ft, with a maximum of about 6,500 gpd/ft. Aquifer
transmissivity probably varies over a wide range depending on the
percentage of bentonite and shale beds within the sandstone; however,
it is believed that the values computed from the drill stem tests are
underestimates because of inherent test and calculation errors (see
Appendix D).
Frontier well yields for five wells reportedly vary over a wide
range, from 1 gpm to over 100 gpm, and well specific capacities vary
from 0.3 gpm/ft to as much as 30 gpm/ft.
Potentiometric data for the Frontier aquifer are sparse. Avail-
able data indicate that the regional flow in this aquifer is toward the
center of the Great Divide and Washakie basins (Figure V-4). Recharge
occurs in the uplift areas in the east, north, and west parts
62
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Figure V-4. Potentiometric surface map, Frontier aquifer.
63
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of the study area. Discharge from the Frontier aquifer to overlying
formations is assumed to occur in the central basin areas.
Cloverly Aquifer
The Cloverly aquifer consists of two parts: an upper sandstone
unit and a lower unit, known elsewhere as the Dakota Sandstone and the
Lakota Conglomerate, respectively. It is between 45 and 240 feet thick
and is separated from the Frontier aquifer by several hundred feet of
low-permeability sediments in the Mowry and Thermopolis shales. This
aquifer crops out at the Rawlins uplift in the eastern part of the
area. It dips basinward to the west and occurs at a depth of over
13,000 feet in the vicinity of Baggs, near the central part of the
Washakie basin.
Information on ground-water occurrence and hydrologic character-
istics of the Cloverly aquifer is available from 39 oil test wells and
7 water wells. The water wells are located south of Rawlins, and the
majority of the oil wells are located to the south of the Rock Springs
uplift.
Based on available potentiometric data (Figure V-5), recharge to
the aquifer from overlying formations occurs along the Sierra Madre and
Rawlins uplifts in the east, Crooks Mountain in the north, and the Rock
Springs uplift in the west. There are no potentiometric data to
delineate flow in the central part of the Great Divide and Washakie
basins.
The aquifer transmissivity estimates computed from drill stem test
data are generally low, between 1 and 177 gpd/ft. Available
information from other sources (Berry, 1960; Dana, 1962; Welder and
McGreevy, 1966) suggests that aquifer transmissivity is higher than
64
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Figure V-5. Potentiometric surface map, Cloverly aquifer.
65
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that computed from the drill stem tests, ranging between 340 and 1,700
gpd/ft.
Based on reported tests for 13 wells, well yields range from 25
gpm to over 120 gpm, and specific capacities range from about 0.3 to
1.4 gpm/ft.
Sundance-Nugget Aquifer
The Sundance-Nugget aquifer is comprised of permeable sandstone
beds, separated from the Cloverly aquifer by 200 to 300 feet of
Morrison shale. The lower part of the Sundance reportedly contains
some shale, siltstone, and limestone beds, while the Nugget contains
minor interbedded shale and siltstone. Both formations either crop out
or are thinly covered with Tertiary deposits in the uplift areas.
Maximum combined thickness of the Sundance Formation and Nugget
Sandstone is between 170 and 1,100 feet. These formations may be as
deep as 14,000 feet below ground surface near the center of Washakie
basin.
Information about ground-water occurrence and hydrologic charac-
teristics of the Sundance-Nugget aquifer is available from 30 oil test
wells and 7 water wells. One water well and five oil test wells are
reportedly flowing. Most wells are located in the northern and western
parts of the study area.
The available potentiometric data are sporadic and cannot be used
to delineate flow patterns in the Sundance-Nugget aquifer. Potentio-
metric heads are highest in the uplift areas of the east, west, north,
and northeast (Figure V-6).
66
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Figure V-6. Potentiometric surface map, Sundance-Nugget aquifer.
67
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Paleozoic Aquifer System
The Paleozoic aquifer system consists of all the formations below
the shales and other fine-grained sediments of the Chugwater and
Phosphoria formations. It includes three important water-bearing
intervals: the Tensleep Sandstone, the Madison Limestone, and undif-
ferentiated Cambrian and weathered Precambrian rocks. The Amsden
Formation, which is of low permeability, partially separates the
Tensleep and Madison aquifers. There is no apparent confining bed
separating the Madison Limestone and the underlying Cambrian and
Precambrian undifferentiated rocks.
Although the carbonate units of the Paleozoic aquifer system have
very low intergranular permeability, they are highly permeable where
secondary porosity features exist. These features occur where solution
zones and fractures are prominent. Permeabilities in the Tensleep and
Cambrian sandstone aquifers are primarily intergranular.
The Tensleep consists of fine- to medium-grained sandstone,
locally quartzitic, with lesser amount of thin interbedded layers of
limestone and dolomite. It has a maximum thickness of about 800 feet
(Welder and McGreevy, 1966) and, reportedly, it is completely missing in
the southeastern part of the study area (Gudim, 1956; Ritzma, 1951;
Lawson, 1949; Weimer, 1949).
Information about the water-bearing capabilities and ground-water
occurrence in the Tensleep aquifer is available from the records of 28
wells, of which the great majority are oil test wells. At least three
of the wells are flowing. Tensleep well yields are reported at between
24 and 400 gpm. Aquifer transmissivity is low, ranging from less than
1 to 374 gpd/ft.
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Potentiometric data for the Tensleep aquifer are shown in Figure
V-7; the resultant potentiometric contours are considered
representative of the entire aquifer system. Figure V-7 shows recharge
occurring along the northern and eastern flanks of the Great Divide
basin. Additional recharge into the Washakie basin may occur to the
south and east of the Rock Springs uplift. Ground-water flow from the
recharge areas is toward the basin centers.
The Madison aquifer is comprised of predominantly limestone and
dolomite, with thin sandstone and chert beds (Gudim, 1956; Ritzma,
1951; Lawson, 1949; and Weimer, 1949). Aquifer thickness reportedly
ranges from about 5 feet to 325 feet (Welder and McGreevy, 1966).
Information about the water-bearing characteristics and ground-water
occurrence in the Madison Limestone is available from the records of 15
wells and 1 spring. Four water wells are located near the city of
Rawlins. The other wells are oil wells located near the uplifts in the
east, west, and north parts of the study area. The spring is located
to the north of the study area. Based on outcrops outside the study
area, much of the Madison Limestone permeability is secondary due to
development of caverns and solution channels (karst conditions).
Well yields on record range from 4 to 400 gpm. Well specific
capacity for two of the wells is reported at 100 gpm/ft. There are no
other well specific capacity data available.
Madison aquifer transmissivity, based on DST results, is low, on
the order of 10 to 20 gpd/ft; however, the results of pump testing at a
water well (T. 21 N., R. 87 W., section 9 bd) is reportedly 200,000
gpd/ft (see Appendix C). Where Madison transmissivities are high,
secondary permeability is typically well developed.
69
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Figure V-7. Potentiometric surface map, Tensleep aquifer.
70
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The Cambrian rocks consist of sandstones with interbedded silt-
stone, shale, and limestone (Berry, 1960; Gudim, 1956; Lawson, 1949;
Weimer, 1949). Parts of the underlying Precambrian include weathered
granite, gneiss, and schist (Love and others, 1955). Information about
the water-bearing capability and ground-water occurrence in these
formations is available from water wells and springs located at or near
these formation outcrops and from a limited number of deep oil wells.
Well records indicate that 13 water wells and one spring, all
located near the city of Rawlins, derive their supply from the Cambrian
formations at less than 400-foot depth (most wells are less than 250
feet deep). Two oil wells, located in the Bison basin area (T. 27 N.,
R. 97 W.), reportedly encountered water in the Cambrian at about 1,650
feet and 1,300 feet. Water well yields reportedly range from 4 to 250
gpm; specific capacities for two of the water wells are reported at
about 1 and 150 gpm/ft. Aquifer transmissivity is reported at <1 and
27 gpd/ft based on drill stem tests of the oil wells, and 100 and
300,000 gpd/ft (T. 21 N., R. 87 W., section 17 aa) based on testing of
two of the water wells (see Appendix C). This wide range in aquifer
transmissivity may result from increased permeability due to fracture
enhancement in structurally disturbed areas in the north and east Great
Divide basin.
Available records indicate that 11 springs and about 70 water
wells derive their supply from the Precambrian. The springs and wells
are generally located at or near the weathered Precambrian outcrops in
the vicinity of South Pass City in the extreme northwest part of the
study area. One spring is located in the southeast flank of the Sierra
Madre uplift in the eastern Washakie basin.
71
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Well yields in the Precambrian range from 2 to 150 gpm, with the
majority yielding 10 to 20 gpm. Specific capacities range from 0.1 to
150 gpm/ft, with most between 0.5 and 2 gpm/ft. Aquifer
transmissivities range from 6 to 4,000 gpd/ft, but the majority are
less than 1,000 gpd/ft.
SUMMARY OF REGIONAL GROUND-WATER CIRCULATION
Figure V-8 depicts regional ground-water circulation for two east-
west cross-sections and one north-south cross-section through the study
area. Potentiometric data from 50 wells were used in the construction
of Figure V-8; the geographic locations of these data are shown in
Figure III-4 (p. 22)-
The potentiometric contours and flow lines shown in Figure V-8 are
in agreement with individual aquifer potentiometric maps (Figures V-l
through V-7). In general, regional flow patterns are consistent with
topographic features of the area: the recharge regions are located in
the topographically high areas along the periphery of the basins, and
the discharge areas are located in the nearly flat depressions in the
central Great Divide and Washakie basins.
The Rawlins uplift is the location of the regional ground-water
divide along the eastern boundary of the study area. The Wamsutter
arch is also a ground-water divide between the two basins for aquifers
above the Baxter Shale; ground-water flow paths for underlying aquifer
cannot be determined from available data.
Along parts of the western boundary of the study area available
data indicate that ground-water flow is across the Rock Springs uplift
into the Green River basin to the west. In the southwest part of the
study area, potentiometric data for the pre-Baxter aquifers indicate
72
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C*C*T OiviM frtSM)
RAWLINS UPLIFT
Figure V-8.
Potentiometric cross-sections, Great Divide and Washakie basins (locations shown
on Figure III-4).
-------
that the regional ground-water divide is east of the uplift, with a
component of flow toward the Green River basin. Recharge from the
Uinta Mountains to the south may provide the flow for this divide. In
the northwest part of the Great Divide basin, data also indicate a
Tertiary aquifer ground-water divide east of the Rock Springs uplift,
and a western component of flow into the northeastern Green River
basin. Certainly, more potentiometric elevations are needed to
accurately determine ground-water circulation in this area.
74
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VI. WATER QUALITY
-------
VI. WATER QUALITY
Water quality data for about 300 water samples were used to
delineate ground-water quality in the Great Divide and Washakie basins.
These data were obtained from several sources, including the records of
the U.S. Geological Survey WATSTOR data system, the Wyoming Water
Resources Research Institute (WRRI) WRDS data system, compilations of
oil field water quality data by Crawford (1940) and Crawford and Davis
(1962), and the Wyoming Oil and Gas Commission files. Additionally,
water samples were collected by the WRRI staff from 10 wells, and
analyzed by a private laboratory.
Water quality data on record generally include the results of
chemical analyses of water samples, although much of the data obtained
from the Wyoming Oil and Gas Commission files include only TDS esti-
mates based on results of resistivity measurements of formation water
samples. Water resistivity data were used herein to supplement other
data in these areas where chemical analyses are lacking.
As virtually all data are available elsewhere, tabulated analyses
are not produced in this report, except for determinations of samples
collected by WRRI staff specifically for this report (see Appendix E).
It is difficult to assess the quality and accuracy of the avail-
able water quality data used in this report due to the variety of data
sources and the long time period (more than 40 years) over which the
measurements were made. Sampling techniques and analytical methods are
not specified for some of the data sets, and older data and oil test
well data may be suspect. The water samples collected through drill
76
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stem tests in oil test wells may not be representative of the formation
sampled due to possible contamination by the drilling fluids or water
from other formations. The Wyoming Oil and Gas Commission files do not
provide any information with respect to the accuracy of data on record.
The spatial distribution of data is poor for the aquifers lying
below the Baxter Shale, with essentially no data from the central part
of the study area. Most of the available data are for the aquifers
above the Baxter Shale due to larger surficial exposures and shallower
drilling depths.
The following two sections summarize (1) general ground-water
quality, and (2) ground-water quality in terms of U.S. Environmental
Protection Agency standards.
GENERAL WATER QUALITY
This section presents a summary of regional water quality, and
specific discussions of water quality by aquifer in terms of total
dissolved solids (TDS) concentrations and major ion compositions.
Relationships between these constituents are identified and where
possible, geochemical controls on the observed trends are identified.
Where data are sufficient, inferences into ground-water flow paths and
interaquifer communication are suggested.
Summary of Regional Water Quality
Regional analysis of water quality data for the Great Divide and
Washakie basins identifies several areas and aquifers where ground
waters contain less than 1,000 mg/1 total dissolved solids. These
include: (1) Quaternary aquifers in most drainages other than Bitter
Creek, (2) Upper Tertiary aquifers along the Sierra Madre and Rawlins
77
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uplifts, (3) shallow parts of the Battle Spring member aquifer, and,
locally, other members of the Tertiary aquifer system, (4) the
Mesaverde aquifer, in outcrop areas along both the Sierra Madre and
Rock Springs uplifts, and (5) Cretaceous and older aquifers in limited
outcrop exposures along the Sierra Madre and Rawlins uplifts. Major
ion composition of these low-TDS waters is generally dominated by
dissolved calcium, sodium, and bicarbonate and/or sulfate.
Ground-water supplies with less than 3,000 mg/1 TDS may generally
be obtained, in addition to the sources mentioned above, from shallow
(<1,500 feet) wells completed in all members of the Tertiary aquifer
system, with local exceptions. Limited data from the deeper parts of
this system indicate waters with greater than 10,000 mg/1 TDS. Avail-
able data for older aquifers indicate that salinity increases rapidly
away from outcrop, and that ground water containing less than 3,000
mg/1 TDS exists in limited near-outcrop areas only. Dissolved solids
concentrations exceed 10,000 mg/1 in these aquifers over most of their
subsurface extent, with dissolved sodium and chloride ions
predominating.
Quaternary Aquifers
Water quality data for the Quaternary aquifers are available from
water samples from 21 wells. These wells are located in the alluvial
deposits along a number of streams, including the Little Snake River,
Bitter Creek, and Muddy Creek (Plate 3) .
Total dissolved solids concentrations in Quaternary aquifers vary
widely from about 200 to over 60,000 mg/1 (Plate 3). Major ions in
solution are calcium, sodium, and bicarbonate at TDS levels below 1,000
mg/1, while the more highly saline (TDS greater than 10,000 mg/1)
78
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TDS Range, mg/1
Figure VI-1. Major ion composition of waters from the Quaternary
aquifers, Great Divide and Washakie basins.
79
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Quaternary waters contain mainly sodium and chloride (Figure VI-1).
Intermediate salinity corresponds to sodium and sulfate enrichment.
Data are insufficient to identify any spatial distribution of TDS
and major ion composition within individual drainages. However,
Quaternary waters with the highest TDS concentrations and sodium-
chloride enrichment are located in the Bitter Creek drainage (Plate 3)
in the western part of the area. High TDS levels are likely due to
evapotranspiration. Additionally, the presence of faults in the
underlying bedrock and the relatively high chloride enrichment in the
alluvial waters suggests discharge from deeper aquifers into Quaternary
aquifers in this vicinity. Combined with evaporation, these factors
may generate the highly saline alluvial waters.
Upper Tertiary Aquifers
Chemical data from 19 shallow wells and springs in the eastern
Washakie basin are available for the Upper Tertiary aquifers. Most
data are for Browns Park/North Park waters. Total dissolved solids
concentrations in waters from these aquifers vary from 84 to 860 mg/1,
and are generally below 500 mg/1. Available data indicate that some
spatial distribution of dissolved solids exists (Plate 4), with
increased mineralization occurring away from the Sierra Madre uplift.
Dissolved calcium and bicarbonate are the principal constituents of
North Park/Browns Park waters (Figure VI-2), with sulfate enrichment
coinciding with increased salinity.
Many of the existing ground-water analyses are from springs and
seeps, and may represent the hydrochemical conditions of local flow
systems. Therefore, increases in TDS and the accompanying changes in
major ion composition may result from localized variations in
80
-------
TDS Range, mg/1
Figure VI-2. Major ion composition of waters from the Upper Tertiary
aquifers. Great Divide and Washakie basins.
81
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permeability and/or soluble mineral content, as opposed to regional
downgradient geochemical evolution of the ground water.
Tertiary Aquifer System
Member aquifers of the Tertiary aquifer system are the shallowest
present over much of the Great Divide and Washakie basins, and over 100
chemical analyses of ground waters from these units exist. Most
analyses are for Laney Member (Green River Formation), Wasatch, and
Battle Spring waters, and essentially all available data are from
relatively shallow (maximum depth of about 1,500 feet and generally
less than 500 feet) outcrop and near-outcrop wells. Therefore, this
discussion is primarily concerned with the chemical character of
shallow Tertiary waters; a discussion of available data on deep
Tertiary ground waters is at the end of this section.
Total dissolved solids in shallow Tertiary aquifer system waters
vary from 150 to 7,200 mg/1. A geographic distribution of dissolved
solids exists which in part reflects differences in the soluble mineral
content and/or permeability of the member aquifers. TDS levels below
500 mg/1 are limited to Battle Spring and Wasatch aquifer waters along
the northern Great Divide basin flank (Plate 5). The areas of high
salinity (>3,000 mg/1 TDS) are found within the Wasatch and Laney
aquifers along the east rim of the Washakie basin and within the Fort
Union and Lance aquifers along the east flank of the Rock Springs
uplift. Over much of the remainder of the area, dissolved solids range
from 1,000 to 3,000 mg/1.
Available data indicate interformational differences in major ion
composition between Tertiary aquifer system member waters. Analyses of
ground waters from the Battle Spring and Green River aquifers indicate
82
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changes in major ion composition occur with increasing salinity, while
in waters from the other member aquifers the relationship between these
parameters is sporadic and vague.
Low-TDS Battle Spring ground water contains primarily dissolved
sodium-bicarbonate, with increasing calcium-sulfate as TDS levels
approach 1,000 mg/1 (Figure VI-3). Low TDS (<250 mg/1) water
containing sodium enrichment, often exceeding 80 percent of the
dissolved cations on a milliequivalent basis, and the common presence
of calcium-magnesium carbonate soil horizons in arid region soils
suggests that fairly complete reactions between exchangeable sodium and
dissolved calcium and magnesium are taking place. Enrichment of
calcium and sulfate with increased salinity is probably due to
gypsum/anhydrite dissolution.
Analyses of Laney Member aquifer water indicate an increase of
dissolved sodium with higher salinities, though this change is not
always seen (Figure VI-4). Anionic composition varies from roughly
equal amounts of dissolved sulfate and bicarbonate to primarily sulfate
as TDS increases. The variable rate of sodium enrichment with
increased TDS may result from differences in the amounts and types of
ion exchange materials present within individual water-bearing zones.
Major ion composition of shallow waters from the Washakie, Fort
Union, and Lance aquifers is shown in Figures VI-5 and VI-6. Little
correlation between major ions and dissolved solids is apparent within
these ground waters. Available data indicate Lance and Wasatch aquifer
waters are generally sodium-sulfate in character, although exceptions
exist; some Lance water shows chloride enrichment, for example. Fort
83
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TDS Range, mg/1
Figure VI-3. Major ion composition of waters from the Battle Spring
aquifer, Great Divide and Washakie basins.
84
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TDS Range, mg/1
O 0-1000
1000-3000
3000-5000
Figure VI-4. Major ion composition of waters from the Laney aquifer,
Great Divide and Washakie basins.
85
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TDS Range, mg/1
O 0-1000
1000-3000
3000-5000
Subscript L indi-
cates Lance
aquifer; all other
points are for
Fort Union aquifer
Figure VI-5. Major ion composition of waters from the Lance-Fert Union
aquifers, Great Divide and Washakie basins.
86
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TDS Range, mg/1
O 0-500
® 500-1000
~ 1000-3000
3000-5000
Figure VI-6. Major ion composition of waters from the Wasatch aquifer,
Great Divide and Washakie basins.
87
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Union ground water is extremely variable in composition, suggesting
widely differing hydrochemical environments between individual water-
bearing units.
Sparse water quality data are available for Tertiary aquifer
system waters away from outcrop areas. Existing data are largely
derived from formation water resistivities obtained during drill stem
tests. Dissolved solids (as NaCl) exceed 35,000 mg/1 in one Lance
aquifer test (T. 23 N., R. 99 W., section 14). Along the southern edge
of the area (T. 12 N.), IDS (as NaCl) increases westward from less than
2,000 mg/1 near outcrop in R. 92 W., to over 35,000 mg/1 in R. 99 W.
One Fort Union test (T. 13 N., R. 95 W., section 25) indicated
dissolved solids concentrations in excess of 60,000 mg/1. These
extremely saline waters suggest highly restricted ground-water flow at
depth within the Fort Union and Lance, or upward migration of saline
waters from underlying units.
Mesaverde Aquifer
Hydrochemical data for the Mesaverde aquifer are fairly numerous,
and include about 50 analyses and 10 resistivity measurements. Most
data are for waters in the Washakie basin and its bounding uplifts.
Available data indicate a wide, yet systematic, variability in dis-
solved solids concentrations and major ion compositions in Mesaverde
ground water.
Dissolved solids concentrations in Mesaverde aquifer water vary
from less than 500 to over 50,000 mg/1. TDS levels below 1,000 mg/1
are limited to outcrop and near-outcrop zones along the southeast flank
of the Washakie basin and on the northern and southern ends of the Rock
Springs uplift (Plate 6). Increasingly saline water is found toward
88
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the central part of the Washakie basin, where TDS concentrations are
generally in excess of 10,000 mg/1. The rate of increase in TDS away
from outcrop is variable, with the most saline Mesaverde waters found
along the east flank of the Rock Springs uplift at a relatively short
distance from outcrop. Numerous faults cut the Mesaverde and
associated rocks in that area. The high TDS levels that exist
basinward may result from a fault-related restriction of ground-
water circulation, or alternatively, through a fracture-controlled
influx of saline waters from stratigraphically adjacent shales. The
existence of stratigraphic gas traps and the generally low permeability
2
(<1 gpd/ft ) of Mesaverde gas reservoir rocks in this area (Higgins and
Antelope fields, T. 16 N., R. 98-100 W.) indicate that zones of highly
restricted flow also contribute to the high salinity levels (Wyoming
Geological Association, 1979).
Major ion composition of Mesaverde aquifer water varies with
salinity, and therefore with location within the basin. Low-TDS
(<1,000 mg/1) outcrop water contains primarily dissolved sodium and
bicarbonate (Figure VI-7). Water containing 1,000 to 3,000 mg/1 is
enriched in calcium sulfate, probably from gypsum/anhydrite dissolu-
tion. Increasingly saline water is characterized by dissolved sodium,
chloride, and bicarbonate, and is essentially free of sulfate. The
chemical character of this highly mineralized Mesaverde ground water
likely results from (1) exchange of dissolved calcium for sodium; (2)
sulfate reduction and the resulting bicarbonate generation; and/or (3)
intermixing with saline, sodium-chloride rich water, from low perme-
ability zones within either the Mesaverde or adjacent shale units.
89
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TDS Range, mg/1
Figure VI-7. Major ion composition of waters from the Mesaverde aquifer,
Great Divide and Washakie basins.
90
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Frontier, Cloverly,
and Sundance-Nugget Aquifers
Chemical data for the Frontier, Cloverly, and Sundance-Nugget
aquifers are sparse and limited to three general areas: (1) outcrop
and near-outcrop areas adjacent the Sierra Madre uplift, (2) scattered
oil-producing areas in the northeast Great Divide basin, and (3) along
the Rock Springs uplift. Available data indicate both similarities and
differences in the general chemical character of waters from these
aquifers-
Total dissolved solids range from 500 to 60,000 mg/1 in the
Frontier, 200 to 60,000 mg/1 in the Cloverly, and 1,100 to AO,000 mg/1
in the Sundance-Nugget. Low TDS concentrations (less than 1,500 mg/1)
for these aquifers are limited to near-outcrop areas along the Sierra
Madre uplift (Plates 7, 8, and 9), indicating zones of recharge. These
outcrop exposures are small, with much of the area along the Sierra
Madre covered by Upper Tertiary aquifers, suggesting that part of the
recharge to Cretaceous aquifers is through downward leakage from
overlying units.
In the northeast Great Divide basin Sundance-Nugget and Cloverly
aquifer waters generally contain 3,000 to 5,000 mg/1 dissolved solids,
while Frontier waters vary between 1,000 and 15,000 mg/1 TDS.
The most saline water in all these aquifers occurs along the Rock
Springs uplift. Data from this area indicate a distinct stratigraphic
control on ground-water chemistry and circulation (Figure VI-8).
Nugget water characteristically contains less than 10,000 mg/1
dissolved solids, as does most Sundance water, with several waters
having TDS levels below 5,000 mg/1. Waters in overlying and underlying
units are notably more saline in most cases, generally contain
91
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M
8000
6000
4000 -
2000
UJ
UJ
0 -
<
>
UJ
w -2000 -
-4000 -
-6000 7
-8000
TI2N TI3N TI4N
TI5N
TI6N
TI7N
TI8N
TI9N
T20N
T 21N
Figure VI-8. General stratigraphic distribution of total dissolved solids and major ion compositions
within Mesozoic and Paleozoic aquifers, Rock Springs uplift area (for abbreviations,
see p. 20)•
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significantly lower relative bicarbonate concentrations, and are
chloride rich. This hydrochemical zonation indicates a lack of inter-
formational flow through the Sundance-Nugget aquifer. However, one
well (T. 16 N., R. 104 W., section 21), reportedly drilled in a
fracture zone (U.S. Geological Survey Oil and Gas Division, Casper,
information files, 1981), produced waters from the Triassic Chugwater
through Cloverly sequence with less than 10,000 mg/1 TDS and
significantly higher relative bicarbonate concentrations. This
suggests that although there is little interformational flow, vertical
movement may take place in zones of faulting and fracturing.
These aquifer waters show similar trends in major composition as
related to changes in salinity (Figures VI-9, VI-10, and VI-11). All
vary from predominantly sodium-bicarbonate to sodium-chloride waters as
TDS increases, with little calcium, magnesium, or sulfate present at
TDS levels above 1,000 mg/1.
Paleozoic Aquifer System
Development of the Paleozoic aquifer system is currently limited
to outcrop and near-outcrop areas along the eastern edge of the Great
Divide and Washakie basins. Chemical data for these aquifers consist
of water well samples from the east basin outcrop area, as well as oil
field water analyses and resistivity measurements from scattered areas
along the basin margins. Existing data, though sparse, show generally
similar trends in the regional distribution of dissolved solids
concentrations and associated major ion compositions in ground waters
from these aquifers.
TDS concentrations in Paleozoic aquifer system waters vary from
about 200 to over 100,000 mg/1. TDS levels below 1,000 mg/1 (Plate 10)
93
-------
TDS Range, mg/1
Figure VI-9. Major ion composition of waters from the Frontier aquifer,
Great Divide and Washakie basins.
94
-------
TDS Range, mg/1
Figure VI-10. Major ion composition of waters from the Cloverly aquifer,
Great Divide and Washakie basins.
95
-------
TDS Range, mg/1
Figure VI-11. Major ion composition of waters from the Sundance-Nugget
aquifer, Great Divide and Washakie basins.
96
-------
are limited to outcrop and near-outcrop Tensleep and Cambrian aquifer
waters along the eastern edge of the area. Dissolved solids concen-
trations increase downgradient from these areas, exceeding 100,000
mg/1 along the east flank of the Rock Springs uplift. These highly
saline waters are the result of lengthy subsurface residence time,
due to: (1) the long distances from potential outcrop recharge
zones, and (2) highly restricted flow as suggested by the existence
of stratigraphic traps within some Paleozoic oil fields in the area
(Brady South Unit, T. 16 N., R. 101 W.) (Wyoming Geological Associa-
tion, 1979).
Dissolved solids concentrations are related to major ion compo-
sition in ground waters from Paleozoic aquifers (Figure VI-12). Low-
TDS (<1,000 mg/1) near-outcrop waters are predominantly calcium-
bicarbonate. Waters of intermediate salinity (3,000 to 10,000 mg/1
TDS) contain mainly dissolved sodium and sulfate, while more highly
mineralized waters, such as those along the Rock Springs uplift, are
predominantly sodium and chloride.
DRINKING WATER STANDARDS
Primary Standards
Existing data on ground-water concentrations of species for which
primary drinking water standards have been established are sparse in
the Great Divide and Washakie basins. Most existing analyses originate
from (1) U.S. Geological Survey investigations, (2) baseline monitoring
adjacent to coal and uranium mines, and (3) samples collected by WRRI
for this project. There are little data available for Cretaceous and
older aquifers. Identified species with concentrations above primary
97
-------
Member Aquifer
P Phosphoria
T Tensleep
A Amsden
M Madison
C Cambrian
TDS Range, mg/1
o 0-1000
© 1000-3000
~ 3000-5000
5000-10,000
£> +10,000
Figure VI-12. Major ion composition of waters from the Paleozoic aquifer
system, Great Divide and Washakie basins.
98
-------
standards include fluoride, lead, cadmium, selenium, silver, and
chromium.
Fluoride
Existing data indicate 26 fluoride concentrations in excess of 2.0
mg/1 F, all from aquifers lying stratigraphically above the Baxter
Shale. The majority of these exceedences are from Mesaverde, Wasatch,
Laney, and Fort Union waters. Nine analyses indicate fluoride levels
of 5.0 mg/1 F or more, four of which originated from the Mesaverde
aquifer. Stratigraphic and areal distribution of fluoride exceedences
are given in Figure VI-13. Whether this distribution of high fluoride
levels is due to hydrogeologic conditions or a result of the small
number of data points cannot be confidently determined.
Lead
Available data indicate 12 historic exceedences of the primary
standard established for lead, 0.05 mg/1. All but one of these exceed-
ences are from coal development areas (T. 18-20 N., R. 100-101 W., and
T. 21 N., R. 89 W.), where analyses for trace elements are routinely
performed. Therefore, distribution of data is biased toward such
areas. Aquifers showing exceedences in these areas include the
Mesaverde, Lance, Fort Union, and Quaternary alluvium. The single
exceedence noted away from coal mine areas is from a Frontier outcrop
well (T. 13 N., R. 87 W., section 15) with a lead concentration of 0.07
mg/1. Locations and source aquifers of lead exceedences are given in
Table VI-1.
99
-------
04.5
3.4
O
A2.3
5.4^2.8
04.0
5DAa°3.8
° f 4.8
02.7
02.3
24
®
2.6
O
A2.3
~ 3.7
2.3
~
5.5
R379r
4.8 O
~5.0
A Quaternary aquifers
® Laney aquifer
O Wasatch aquifer
© Fort Union aquifer
S Lance aquifer
~ Mesaverde aquifer
0
l_
N
10
_L_
Scq le
20
i
30
40 Miles
_J
50 Kilometers
J
Figure VI-13. Fluoride concentrations exceeding the primary drinking water standard in Mesaverde
through Quaternary aquifers, Great Divide and Washakie basins.
-------
Table VI-1. Exceedences of primary drinking water standards for species other than fluoride in ground
waters of the Great Divide and Washakie basins.
Location
Aquifer NO^-N
As Pb Ag
Ba Cd
Cr Se
Hg
Remarks
18/100-5 da
Alluvium
0.300
18/100-22 ad
Alluvium
0.300
23/96-25 bba
Wasatch
0.01
18/100-29 dd
Ft. Union
0.400
19/105-33 be
Ft. Union
0.130
21/89-11 dl
Ft. Union
0.050
Well
completed
in
coal
21/89-11 d2
Ft. Union
0.110
Well
completed
in
coal
21/89-11 d3
Ft. Union
0.228
0.073
0.091
Well
completed
in
coal
18/100-10 cb
Lance
0.190
0.020
18/100-20 db
Lance
0.300
13/90-27 cca
Almond
0.010
18/101-13 da
Almond
0.400
0.010
20/101-27 ca
Mesaverde
0.160 0.020
0.010
13/87-15 da
Frontier
0.070
0.01
21/87-10 bb
Cambrian
0.01
-------
Other Primary Standards
Five cadmium, three selenium, one silver, and one chromium exceed-
ence were found in existing data. As before, most are from coal mine
areas. Locations and source aquifers are given in Table VI-1.
Secondary Standards
Species for which secondary drinking water standards have been
established, and for which data exist within the Great Divide and
Washakie basins, include sulfate, chloride, and total dissolved solids.
The standards for sulfate and chloride are 250 mg/1; for TDS, 500 mg/1.
Few aquifers within the basins meet these three criteria. As shown on
TDS contour maps (Plates 3 through 10), TDS values below 500 mg/1 are
rare, consistently occurring only in upper Tertiary aquifers, the
Battle Spring aquifer, and in outcrop zones of the Mesaverde aquifer.
Where dissolved solids are greater than 1,000 mg/1, sulfate concen-
trations in most waters approach the 250 mg/1 standard. Chloride,
I
however, is generally below 250 rag/1 in areas where dissolved solids
are below 3,000 mg/1.
Table VI-2 summarizes ranges of concentrations of sulfate,
chloride, and TDS by aquifer and geographic area for the two areas
where data are available.
Radionuclide Species
Existing analyses of radionuclide species in the Great Divide and
Washakie basins ground water generally include determinations for gross
alpha and gross beta radiation, dissolved uranium, and radium-226
(Ra-226), a decay product of uranium-238. Primary drinking water
102
-------
Table VI-2. Concentration ranges of TDS, chloride, and sulfate
in ground waters of
the Great
Divide
and Washakie basins.
Aquifer
Geographic Area
TDS3
a
Chloride
Sulfate
Quaternary
Great Divide basin
200-2,050
4-114
25-914
Washakie basin
200-60,700
9-31,000
15-1,450
Upper Tertiary
Sierra Madre uplift
84-860
1-41
6-175
aquifers
Battle Spring
Great Divide basin
150-750
2-35
10-375
Wasatch
Great Divide basin
165-1,750
6-110
5-630
Washakie basin
450-3,590
5-345
7-1,620
Green River
Great Divide basin
560-1,810
2-105
10-600
Washakie basin
570-7,210
14-1,460
26-3,150
Ft. Union/Lance
Great Divide basin
84-4,950
3-945
10-2,010
Mesaverde
Great Divide-Washakie
250-64,000
15-35,400
12-2,240
basins
Frontier
Northeast Great Divide-
550-13,200
50-5,100
1-300
Sierra Madre
Rock Springs uplift
21,600-57,300
5,150-30,000
40-90
Cloverly
Northeast Great Divide-
200-5,500
2-1,100
30-740
Sierra Madre
Rock Springs uplift
8,200-63,000
4,100-34,500
20-300
Sundance-Nugget
Northeast Great Divide-
165-4,500
1-2,400
25-75
Sierra Madre
Rock Springs uplift
4,400-49,950
1,560-26,970
160-3,407
Paleozoic (all)
Northeast Great Divide-
215-14,960
3-6,140
25-5,225
Sierra Madre
Rock Springs uplift
5,500-100,000
140-52,300
1,800-3,200
All constituents in milligrams per liter.
-------
standards have been established for radium-226 (5.0 pCi/1) and gross
alpha (15.0 pCi/1).
Analyses for radium-226, gross alpha, and gross beta often contain
an error limit that generally indicates the 95 percent confidence
interval of the analysis. Large error limits are usually due to either
(1) a lack of instrument sensitivity at low concentrations, or (2)
particle absorption in samples containing high dissolved solids. Where
the confidence interval is large relative to the given absolute value,
interpretation of results is difficult.
Available data indicate two exceedences of the Ra-226 and gross
alpha standards. These exceedences originated from two Battle Spring
wells (T. 24 N., R. 93 W., section 9 ad, and T. 24 N., R. 94 W.,
section 25 db) (Table VI-3) drilled in uranium mine areas. All other
analyses of Battle Spring water show relatively low levels of
radiation.
There is currently no drinking water standard for uranium. Hem
(1970) states that uranium concentrations in ground waters are
generally less than 10 ug/l. Three analyses of ground waters in the
Great Divide and Washakie basins from the Battle Spring, Mesaverde, and
Madison aquifers indicated uranium levels of 12.2, 34, and 27 yg/1,
respectively. All other tests indicate generally lower uranium
content. Table VI-3 summarizes concentrations of radionuclide species
in area ground waters.
104
-------
Table VI-3. Concentrations of radionuclide species in ground waters of the Great Divide and
Washakie basins.
Ra-226
Gross Alpha
Gross Beta
Uranium
Aquifer
Location
(pci/1)
(pCi/1)
(pCi/1)
(yg/i)
Bishop Conglomerate
12/90-11 ad
0.09±0.12
1±1
5±3
5.0
North Park/Browns
15/89-33 cc
0.3±0 . 2
1±1
6±2
5.0
Park
16/88-22 db
0.1
3.0
3.7
3.4
18/88-22 dd
0.35
4.4
2.9
3.6
88/89-15 cd
0.19
6.2
4.1
5.2
Battle Spring
24/93-9 ad
14.7±17
4. 5±9
21±4
-
24/93-10 dc
1.15±0.1
-
-
12. 2
24/93-14 cd
0.5±0.01
-
-
0.9
24/93-15 ca
1.3±0.1
-
-
7.1
24/93-15 dd
0.07
-
-
6.7
24/93-25 ad
0.65+0.1
-
-
4.6
24/94-22 c
-
0.6
0.4
0.5
24/94-25 db
33.5
156±34
90±9
-
25/90-17 ca
0.06
1.95
6.4
1.8
26/91-11 bba
0.04
2.1
6.2
1.2
Wasatch
23/96-25 ba
1.3±0.3
0±4
5+6
2.0
24/103-32
-
-
-
15
26/97-3 ddc
0.71
4.5
2.1
2.7
Green River
15/99-12 be
0±0.1
3±1
4 + 2
4.0
Ft. Union
20/100-13 bb
4
3.4
11.7
1.0
Mesaverde
12/90-14 ad
0.46±0.2
0 + 2
3±3
0
13/90-22 aa
0.17
<5.0
4.7
-
14/90-3 ad
0.88
2.3
4.9
0.5
14/90-5 da
0.05
3
<1.7
0.07
14/90-10 cb
0.12
8.3
7
0.18
19/101-33 cd
0.86
<6.7
15
<0.01
20/101-27 ca
0.38+0.16
0±16
16±7
34.0
-------
Table VI-3. (continued)
Aquifer
Location
Ra-226
(pCi/1)
Gross Alpha
(pCi/1)
Gross Beta
(pCi/1)
Uranium
(yg/D
Frontier
13/87-15 da
0.23+0.16
0±1
4±3
5.0
23/88-16 db
0.1+0.2
10+4
2±3
6.0
Madison
21/87-10 bb
1.5+0.3
13±5
36±8
27.0
Cambrian
21/87-9 bd
0.32+0.18
11 + 2
14 + 3
9.0
-------
VII. REFERENCES
-------
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112
-------
APPENDIX A
GROUND-WATER USE BY INDUSTRY AND
FOR IRRIGATION AND DRINKING WATER
IN THE GREAT DIVIDE AND
WASHAKIE BASINS, WYOMING
-------
Table A-l. Water produced as a by-product of petroleum production in the Great Divide and Washakie basins, 1979, by field (data from
Wyoming Oil and Gas Conservation Commission Files and Wyoming Oil and Cas Conservation Commission (1980)).
Field
Location
(T/R)
No. of
Wells
1979
Produced Water
(bbJ)
Produc ing
Forma tion(s)
Remarks
>
I
Ai rport
Alkaline Creek
Antelope
Antelope Springs, E.
Arch
Baggs, S.
Baggs, S. Extension
Baggs, W.
Bailey Dome
Barrel Springs
Bartlett
Bastard Butte
Battle Springs
Baxter Basin, Middle
Baxter Basin, N.
Baxter Basin, S.
Bell Springs
Bison Basin
Bitter Creek
Black Butte Creek
Blue Gap
Brady
Browning
Browns Hill
Bunker Hiil
Busli Lake
Camel Rock
Canyon Creek
Cherokee Creek
Cherokee Ridge
Chimney Rock
19/103
16/98
17/99
27/93
19/98
12/92
1 2/92
12/93
26/89
19/93
19/102
25/97
23/96
18/103
19-20/103-106
16/106
23/88
27/95
16/99
19/102
J 5/92
16/101
16/91
16-16/89-91
27/89
26/96
18/102
12-13/100-101
J 5/91
12/96
18/102
2
1
10
0
23
16
2
0
2
12
1
2
1
5
18
17
0
13
1
1
18
19
2
1
1
6
1
35
2
0
0
30
0
0
0
38,758
3,736
0
0
1 ,390,692
0
0
0
0
0
0
2,277
0
182,930
0
0
81,836
1 ,397,682
0
0
0
0
1,861
17, J 28
310
0
0
F ront i er
Lewis
AImond
UNK
Almond
Lewis, Mesaverde
Lewis
UNK
Tensleep
Almond
UNK
Lewis
Lewis
Dakota,
Frontier
Dakota, Nugget,
Morrison, Frontier
Dakota, Frontier
UNK
Front ier
Weber
Dakota, Morrison
Mesaverde
Nugget
Tensleep
UNK
Steele, Frontier
Mesaverde
Dakota
Wasatch, Mesaverde
Frontier, Deep Creek
UNK
UNK
Shut in 9 mos.
No 1979 production; abd. 1966
No 1979 production; shut down
Shut in 7 mos.
No 1979 production; Discov. 1978
Shut in 9 mos.
No 1979 production; nbd.
No 1979 production
No 1979 production; discov. 1976
No 1979 production; shut-in
Production started 6/79
No 1979 production; abd. 1962
No 1979 production; abd. L966
-------
Table A-l. (continued)
1979
Location No. of Produced Water
Field (T/K) Wells (bbl)
Conl Gulch
1 7/91
1
0
Cole Springs Draw
23/88
0
0
Continental Divide
22/93
0
0
Cow Creek
16/92
2
914
Creston
19/92
2
0
Cres ton » S.E.
19/90
1
18
Crooked Canyon
21/103
11
2,931
Crooks Gap
28/92-93
9
3,555,01/.
Deadman Wash
20/10]
3
0
Deep Creek
16/90
2
0
Deep Gulch
16/91
3
15,486
DeLaney Rim
18/97-98
10
24,965
Desert Flats
19/95
2
0
Desert Springs
20-21/97-98
9
2,30 4
Desert Springs, E.
21/97
1
402
Desert Springs, W.
19-20/99
44
5,23 7
Divide
22/87
1
0
Dixon
13/90
1
0
Echo Springs
19/93
15
5,486
Espy
19/89
9
48,215
Ferris, E.
26/86-87
0
0
Ferris, W.
26/87
0
0
Fillmore
20/92
2
239
Fireplace Rock
12/95
1
0
Five Mile Gulch
21/93
2
0
Forbes
25/97
1
0
Gale
23/96
1
138
Girrard
27/95
1
0
Golden Goose
28/92
2
1,576
Go Iden Wn 11
18/101
I
0
GP Dome
25/86
1
0
Producing
Formation(s)
Remarks
Almond
UNK
UNK
Frontier, Dakota
Ericson
A1roond
Dakota
Frontier, Lakota,
Muddy, Nugget
Dakota, Frontier
Deep Creek, Muddy
Frontier, Deep Creek,
Nugget
Almond, Lewis
UNK
Almond , Lewis
Almond, Lewis
Almond
Steele
UNK
Mesaverde, Lewis
Tensleep, Niobrara
UNK
UNK
Mesaverde, Lewis
UNK
Mesaverde
Ericson
Ericson
Dakota
Dakota
Dakota
"Cretaceous"
Production started 10/79
No 1979 production; abd.
No 1979 production; Temp. jbd.
No 1979 production; shut-in
Temp. abd. 4/79
No 1979 production; discov. 1979
Shut-in 5 mos.
No 1979 production; abd. 1945
No 1979 production; abd. 1954
No 1979 production; shut-in
No 1979 production; discov. 1979
Shut-in 2 mos.
No 1979 production; shut-in
Rhut- in 5 mos.
-------
Table A-l. (continued)
Fie Id
Location
(T/R)
No. of
We 1 1 s
J 979
Produced Water
(bbl)
>
I
U>
Great Divide
Hallvil1e
Hansen Draw
Hdppy Springs
Hatfield
Hay Reservoir
Haystack
Hiawatha
Higgins
Horn Canyon Unit
Hugus
Iron Pipe
Jade Ridge
Joyce Creek
Kinney
Kirk
Lamont
Laney Wash
Leucite Hills
Little Snake
Little Worm Creek
Lost Creek
Lost Soldier
Mahony,1S.
Mahony Dome
Mahony Dome, E.
Mahony Draw
Marianne
Masterson
22-23/95-96
19/100
17/96
28/93
19-20/88
24/97
U./96
12/99
17/99
24/100
19/87
16/98
28/93
15/103
J 3/99
28/92
25/89
17/97
22/103
12/94-96
15/104
23/97
26/90
25/88
26/88
26/87-88
21/90
20/103
20/102
0
29
1
18
11
1
0
1
2
9
7
0
0
1
3
0
0
2
52
3
7
0
1
1
2
15
0
0
1,974,954
0
3,986
0
1,611
0
0
0
0
0
34,320
12,805
0
0
0
40
0
0
0
30,385,995
80,475
421,445
0
68
0
0
Producing
Formation(s)
Remarks
Lewis
Almond
Rock Springs
FronLier, Muddy,
Dakota
UNK
Lewis
Mesaverde
Wasatch
Lewis
Frontier
UNK
Mesaverde
Dakota
Frontier, Dakota
Mesaverde, Dakota,
Frontier, Nugget
UNK
UNK
Lance
Dakota
UNK
Lakota
UNK
Frontier, Tensleep,
Madison, Cambrian
UNK
Tensleep
UNK
Mesaverde
Lakota
Dakota, Blair, Muddy
Shut-in 2 mos.
Shut-in 10 mos.
No 1979 production; abd. 1965
No 1979 production; shut-in
No J979 production; shut-in
No 1979 production; abd.
No 1979 production; shut-in
1 mo. data missing
No 1979 production; temp. abd.'72
No 1979 production; shut-in
No 1979 production; shut-in
No 1979 production; abd. 1969
No 1979 production; shut-in
No 1979 production; abd. 1978
No 1979 production; abd. 1953
No 1979 production; discov. 1979
-------
Table A-L. (continued)
1979
Location No. of Produced Water
Field (T/R) Wells (bbl)
McPherson Springs
13/94
1
0
Melton
22/86
0
0
Middle Mountain
12/103
1
0
Mone1 J
J 8-19/99
49
1,657,300
Monument Lake
21/92
1
0
Mud Lake
23/98
0
0
Nef f
18/98
0
0
Nickey
24/96
1
0
Nitchie Gulch
23/103
20
690
O'Brien Springs
25/86
1
0
Osborne Draw
26/93
0
0
Patrick Draw
18/99-100
36
4,270
Picket Lake
26/97
2
0
Pine Canyon
23/103
7
0
Platte River Bend
24/85
0
0
Playa
20-21/98-99
17
3,7 43
Point of Rocks
20/101
1
56
Potter Mountain
14/103
2
0
Powder Springs
12/97
1
93
Pretty Water Creek
15/104
1
4
Red
16/94
1
0
Red Desert
22/97
1
0
Red Hill
19/100
0
0
Red Lakes
18/94
5
4,649
Rim
19/88
1
0
Robbers Gulch
14/91
2
660
Robin
19/97
3
963
Roser
21/101
0
0
Round Table
12/96
0
0
Salazar
16/95
2
232
Salt Wells
14/103
2
140'
Produc in g
Formation(s)
Remarks
UNK
UNK
UNK
Almond
Mesaverde
UNK
UNK
Almond
Frontier, Dakota
Tensleep, Muddy
UNK
Almond
Lewis
Frontier
UNK
Almond, Lewis
Blair
Frontier
UNK
UNK
UNK
Mesaverde, Lewis
UNK
Mesaverde
UNK
Mesaverde
Almond
UNK
UNK
Mesaverde
Front icr, Dakota
No 1979 production; discov. 1979
No J 97 9 production; abd. 1966
No 1979 production; abd. 1977
Production started 11/79
No 197 9 production; abd. 1960
No 1979 production; shut-in
No 1979 production; discov. 1979
No 1979 production
Shut-in 7 mos.
No 1979 production; abd. 1966
Shut-in 7 mos.
No 1979 production; discov. 1979
Shut-in 5 mos.
No 1979 production; shut-in
No 1979 production; temp. abd.
Shut-in 4 mos.
No 1979 production; shut-in
No 1979 production; abd. 1971
-------
Table A-l. (continued)
Fie Id
Loca t ion
(T/R)
No. of
Wei Is
1979
Produced Water
(bbl)
>
I
Ln
Sand Butte
Savery
Sentinel Ridge
Separation Flats
Sheep Camp
Sheep Creek
ShelI Creek
Sherard
Shiprock
Siberia Ridge
Six Mile Springs
Smith Ranch
Smokey
Stage Stop
Standard Draw
State I.me
Stock Pond
Sugar Creek
Table Rock
Table Rock, S.
Tab 1e Rock, S.W.
Ten Mile Draw
Tierney
T ierney, N.
Tipton
Trail
Trail Ridge
Tr i ton
Twin Buttes
Twin Rocks
Vermi11 ion
17/99
13/89
23/94
24/87
22/97
28/92
19/96
25/88
20/101
21/94
18/104
12/93
15/99
18/99
18/93
12/94-95
22/95
19/90
18-19/97-98
18/98
] 8/98
21/98-99
19/94
20/94
19/97
13-14/100
27/95
13/94
26/90
21/103
13/100-101
1
2
2
1
4
4
1
5
2
7
2
4
1
11
3
0
2
1
35
2
1
5
5
0
1
5
0
1
0
0
0
0
0
0
0
281
7,100
0
145,999
0
6,294
0
0
0
5,141
0
0
0
5,219
59,336
906
0
0
0
0
" 53
5,869
0
0
0
0
0
Producing
Formation(s)
Remarks
Almond
Deep Creek
Mesaverde
Muddy
Almond
Phosphoria
Mesaverde
Tensleep, Mowry,
Frontier, Muddy
Frontier
Mesaverde
Front ier
Lewis, Lance
UNK
Lewis, Lance, Almond
Mesaverde
UNK
Mesaverde
Frontier, Tensleep
Almond, Lewis
Almond
Mesaverde
Lewis, Almond
Mesaverde
UNK
A lmond
Mesaverde
UNK
UNK
UNK
UNK
UNK
Shut-in 4 mos.
Production started 5/79
No 1979 production; discov. 1979
Shut-in 3 mos.
No 1979 production; abd. 1970
Shut-in 7 mos.
Shut-in 2 mos.
No 1979 production
No 1979 production; abd. 1966
No 1979 production; discov. 1979
No 1979 production; te^p. abd.
No 1 979 production; temp. .ibd.
No 1979 production; abd. 1963
-------
Table A-l. (continued)
Field
Location
(T/R)
No. of
Wells
1979
Produced Water
(bbl)
Producing
Format-ion (s)
Remarks
Wnmsut ter
Wells Bluff
Wer tz
Westside Canal
Wild Rose
Windmill Draw
TOTALS: 159 fields:
20-21/94-95
18/96
26/89-90
12/91
17-18/94
I 5/94
27,
1
39
28
29
0
901
2,273
0
8,878,418
1,245
14,552
0
50,501,191
Mesaverde
Mesaverde
Tensleep, Mesaverde,
Amsden
Fort Union, Lance, Lewis
Mesaverde
UNK
Shut-in 10 mos.
No 1979 production; discov. 1979
>
I
cr>
-------
Table A-2. Water use for secondary recovery of oil in the Great Divide and Washakie basins, Wyoming, 1979, by field.3
App roxIma Lc
l.ocn t ion
Injected
Formation
No. Injectors
Injected
Water
(1979, bbl)
Produced
Water
(1979, bbl)
CaLcu1 ated
Makeup Water*5
(bbl)
Makeup Water
Source
Arch
Lost Soldier
19N-98W
Bison Basin 27N-95W
Happy Springs 28N-93W
26N-90W
Patrick Draw 18N-99.100W
Wertz 26N-89,90W
Arch
Frontier
Dakota
Frontier
TOTAL
Tenslecp
Cambr ian
Madison
TOTAL
Wertz "D"
West Wertz
A1mond
(Mesaverde)
Frontier
Dakota
Tensleep
Cambr ian
Madison
Almond
(Mesaverde)
Ten6leep
Tensleep
Tensleep
45
1
0
0
0
40
3
4
47
77
1
1?
10?
180
(5)
(6)
(1)
(1)
(2)
(2)
(1)
(0)
(3)
(1)
(1)
(0)
(0)
(1)
(18)
2,245,832
182,930
56,597
0
56,597
9,574,778
1,797,240
1,463,164
12,835,182
5,412,601
6,739,459
412,789
630,202
7,782,450
28,515,592
(3,676 ac-ft)
38,758
1 ,974,954
30,385,995
4,2 70
8,878,418
2,207,074
5,408,331
UNK
None
None
None
Fox Hills
None
Battle Spring
None
"Purchased water.'
Solely produced water
Solely produced water from Dakota
and Tensleep; no injection
July-Dec., I 979.
Shut-in during 1979.
Lost Soldier field uses solely
produced water from Sundance,
Tensleep, Madison, and Cambrian.
Solely produced water from
Paleozoic rocks
Also uses Madison produced water.
Solely Madison produced water
7,615,405
(982 ac-ft)
Data from files of the Wyoming1 Oil and Gas Conservation Commission and Wyoming Oil and Gas Conservation Commission (1980).
Amount of makeup water calculated by subtracting reported amount of produced water from reported amount of injected water.
-------
Table A-3. Water use Tor coal mining in the Great Divide and Washakie basins, Wyoming (data from Wyoming Department of Environmental Quality (DEQ) files, Wyoming State
Engineer's Office (SF.O) files, and Glass, ]980).
DEQ
Permit
Company
Locat luii
(T/R)
1979
Production
(tons)
Water Use
lllack Butte Coal Co.
Black Butte Strip 467 18/100 500,000 4 wells in Ericson Formation (Me-^averde aquifer) supply water for dust abatement, equipment u.-u-.hdown ,
Mine irrigation, fire protection, and domestic use.
Maximum permitted yields total 1,950 gpm (3,148 ac-ft/yr) but actual use may be less because water is
recirculated and reused where possible, and intermittent pumpage is expected.
Permits for up to 4,000 gpm of pit discharge (SE0 permit it's 40333-40335, 54328; Fort Union Formation;
1,000 gpm each) are pending completion. Water is to be used for dust abatement.
>
I
00
SEO
Permit It
Well Name
Yield
Location (gpm)
Total
Dep th
30220 Chandler-
Simpson fl]
45085 Darter #1
51015 Darter 02
luebell #13 19/100-13 3507
18/100-8 500?
19/100-29 500
18/100-20 600
51016 Darter it3
19/100-35 (350)
1,219 Washdown, fire protection,
domestic
4,932 Dust abatement
2,077 Dust abatement
2,000 Washdown, dust abatement,
ir r Iga t ion
(2,310) Dust abatement
SEO permitted yield
is 50? gpm.
SEO permitted yield
is 250 gpm.
SEO permitted yield
is 300 gpm.
SEO permit 056050
enlarged yield to
600 gpm.
Permit pending comple-
tion at SEO.
Bridget Coal Co. Jim Bridger Mine 338 21/100 6,400,000 Water from 8 dewatering wells (maximum yield ?50 gpm each. Fort Union Formation. SEO permits 536895.
^ 56279-5i'i285) ic pumped to storage and evaporation ponds, then used for duct oupprcooion or discharged
to Deadman Draw, a tributary of Bitter Creek.
One additional well permitted for construction, plant, and domestic uses (maximum yield 600 gpm, SEO permiL
06437, see Appendix A-8).
Maximum total ground-water use, based on permitted yield, is 2,600 gpm (4,197 ac-ft/yr) but actual use
may be less, because intermittent or reduced pumpage is expected.
Up to 750 ac-ft/yr of waste water from Jim Bridger power plant is also used for irrigation, source is
diversion from the Green River.
-------
Table A-4. Water use for uranium raining in the Great Divide and Washakie basins, Wyoming (data from Wyoming Department of Environmental Quality (DEQ) and Wyoming State
Engineer's Office (SEO) fiLes).
DEQ
Permit Location Ore
Company Mine 8 (T/R) Production __ Water Use
26 dewatering wells removed J,865.75 x 10^ gal in 1979-80:
130 x 10^ gal used on site
332.3 x 10 gal lost from settling ponds by infiltration and evaporation
1,403.21 x 10^ gal discharged to Battle Spring Draw, a tributary to a playa on Battle Spring flat,
from which it evaporated.
SEO permit numbers for dewatering wells are 41699-41716, 53849, 54883-54894, 54896-54903; several of these
wells are not yet completed (as of 7/81).
Potable water and water for fire, offices, and trailers is supplied by 3 wells:
SEO Tot.t 1 Meld
Permit if Well Name Locat ion Depth (ft) (Rpm)
34388 RDW-l 24/93-10 340 300
43125 P-l 24/93-15 400 60
43126 P-2 24/93-]5 400 60
Western Nuclear Crooks Gap Mines 381 28/92 652,000 T/yr 14 wells with maximum permitted yield 583 gpm, actual water use may be less because plant water is
Inc. (8 facilities) (reported recycled and intermittent or reduced pumpage is expected.
1978-1979) ^35 gpm discharged to Crooks Creek drainage, remaining water used in mill.
SEO
Permit 8
Well Name
Location
Yield
(Rpm)
Total
Depth
(ft)
Use
1490
Golden Goose W.W.tfl
28/92-21
800
5
Domestic, drilling water.
1458
Yellow Sands 01
28/92-20
500
12
Domestic, drilling fluid, dust abatement.
28674
Sheep Mountain ff 1
28/92-21
1,360
10
Shaft dewatering.
28675
Golden Goose 11 W.W.fll
28/92-20
500
18
Drinking, sanitation, equipment cLeanLng.
28676
Green Mountain WW03
28/92-16
447
8
"Domestic, industrial."
32934
Mc Lntosh 8\
28/92-29
500
250
Pit dewatering
33910
Mcintosh 82
28/92-29
250
5
Drinking and sanitation, at maintenance bldg.
41188
Golden Goose 1 8\
28/92-21
810
1 25
Shaf t dewatert ing.
41189
Reserve 01
28/92-2L
462
15
Pit dewatering.
41190
Seismic if I
28/92-21
485
30
Pit dewatering.
43954
Mc lntosh 83
28/92-29
300
25
Sanitation, at pit office.
44469
SD 18-16
28/92-28
1,410
20
Offices, shops, drilling fluid.
44886
PL-21A
28/92-22
1,410
35
Offices, drilling fluid.
56266
Congo pit fll
28/92-16
225
25
Pit dewater ing.
TOTAL
583
Minerals Explora- Sweetwater Uranium 481 23/93 720,000 yd^/yr
tioti Co. Mine (projected
1980-1981)
-------
Table A-5. Permitted irrigation wells in the Great Divide and Washakie basins, Wyoming (data from Wyoming State Engineer files, as of
July (?), 1980).
Acreage Irrigated
County
Location
State Engineer's
Permit Number
Total Depth
(ft)
Aquifer(s)
Reported Yield
(gpm)
Original
Supply
Supplemental
Supply
To Lai
Carbon
13/91-32
8616
31
Alluvium
30
20
0
20
18/88-10
339G
210
Frontier?
50
10
0
10
18/88-11
156
UNK
LINK
20
60
0
60
21/88-24
1116
32
Alluvium
6
2.5
0
2.5
22/88-24
325G
47
Upper Tertiary
3,000
30
0
30
22/88-24
41
70
Upper Tertiary
350
100
0
100
22/88-24
326G
49
Upper Tertiary
3,000
30
0
30
Sweetwater
17/94-13
43626
180
50
40
0
40
18/100-8
6790
1,200
Mesaverde
500
61
39
100
18/101-18
499C
400
Mesaverde
250
16
5
21
18/101-18
500C
400
Mesaverde
250
17
47
64
19/95-1
26024
300
Waaatch (Tertiary
system)
aquifer
10
UNK
0
UNK
20/94-34
695
1,250
Waaatch (Tertiary
system)
aquifer
250
15
0
15
TOTALS:
7,766
401.5
91
492.5
-------
Table A-6. Community water supplies In the Great Divide and Washakie basins. Facilities are those previously identified by the U.S. Environmental Protection Agency.
Facility
EPA PWS
ID 0a
Reported
Produc tion
Population Rate®
Served3 (gpd)
Water Source
SEO Well
Total
Depth^
(ft)
Aquifer
Reported
Yieldb
(gPm)
Completion
Date
CARBON COUNTY
Baggs (municipal)
Dixon (municipal)
Lamont Village
Rawlins (municipal)
Western Hills Trailer
Court, Rawlins
5600058 350 100.000
5600059
5600227
80 21,000
25
3,000
5600045 14,500 2,000,000
5^00066
150
28,000
Little Snake R.
Baggs 01
Baggs 01 Enl.
Baggs 02
Baggs well and
infiltration Pipe 01
Little Snake R.
Dixon #1
Dixon 82
Well
North Platte R.
•Sage Creek Drainage
Old City 01
New City 0lA
City of Rawlins 02
Pine Grove Well
Purchase
Well
12/91-5
12/91-5
12/91-5
12/90-5
21/87-16
21/87-16
18/88-10
UNK
15173
31718
13673
31
40628
13/90-33 40629
UNK UNK
2677
26777
306C
UNK
(50)
18
650?
305?
1,000
UNK
Alluvium
Alluvium
Alluvium
45 Alluvium
50
300
(350)
UNK
20
(500) Upper Tertiary7 UNK
UNK UNK UNK
Madison 300?
Tensleep 400?
Frontier & Morrison 120
UNK
UNK
UNK
N. A.
N. A.
UNK
N. A.
UNK
8/7/1891
5/61
8/27/54
UNK
Surface water; primary
source, obtained by in-
filtration gallery7
Increased permitted yield
of Baggs ii 1 .
Permit #13673 cancelled.
Replaced by Baggs II1 .
Surface water; primary
source.
Long-term yield too small,
pump may be installed
In future.
Permit 40629 cancelled.
EPA data base lists one
well, no identifiable
record at SEO.
Surface water.
Surface water and springs,
primary source.
Well identified by EPA
data base, no record at
SEO.
Purchased water from City
of RawLins.
EPA data base also lists
one well, no identifiable
record at SEO.
SWEETWATER COUNTY
AMOCO Production 5600003
Company, Baroil
(company town)
Colorado Interstate 5600100
Gas, Table Rock Village
(company town)
37,500
9,000
Baroil Well 01
Well
Springs
Village well 01
Village Well 02
26/90-16 1608
UNK
UNK
19/98-11
19/98-11
UNK
UNK
42166
42167
301
UNK
UNK
500
500
Mesaverde
UNK
UNK
Wasatch
Wasatch
10
UNK
UNK
75
100
3/28/66
UNK
UNK
3/13/77
12/1/77
ETA data base also lists
a second well and springs,
no identifiable records
at SEO.
Well 02 is stand-by well.
-------
Table A-6. (continued)
Facility
EPA PWS
ID 8a
Population
Served3
Reported
Production
Rate®
(gPd)
Water Source
SEO Well
Location Permit S*5
Totalb
Depth
(ft)
Aquifer
Reported
Yield
(BP")
Comp Letion
Date
SWEETWATER COUNTY (continued)
Point of Rocks Mercantile, 5600093 120 15.000
Point of Rocks i
(trailer court, etc.)l
South Superior (municipal) 5600092 647 52,000
Stage Stop Texaco, 5600094 90 8,500
Point of Rocks
(trailer court, etc.)
Union Pacific Railroad, 5600368 27 259,200
Point of Rocks
(company town)
Wamsutter (municipal) 5600105 700 300,000
Old Iron #1
Soda 02
Deep Well £3
Superior #14
Superior #15
Well
Well
Well #6
Well #7
20/101-27 12415
20/101-27 12416
20/101-27 12508
21/101-21
21/101-21
UNK
UNK
459C
460C
90
90
340
1,200
1,235
Ericson
Ericson
Almond?
Erlcson
Eric son
UNK UNK
UNK UNK UNK
UNK UNK UNK
II
13
48
250
250
UNK
UNK
-/-/50?
5/68
4/15/72
6/30/43
9/23/43
UNK
UNK
UNK
EPA data base lists one
well, no identifiable
record at SEO.
EPA data base lists one
well, no Identifiable
record at SEO.
EPA data base lists two
wells, no record at
SEO.
Data from U.S. Environmental Protection Agency (EPA) Public Water Supply Inventory (1979).
^Data from Wyoming State Engineer's Office (SEO) well permit files.
-------
Table A-7. Non-community public water supplies in the Great Divide and Washakie basins, Wyoming. Facilities are those previously identified by the U.S. Environmental Protection
Agency.
Reported
Production Total Reported
(EPA PWS Population Rate3 SEO Well Depth Yieldb Completion
Facility ' ID ga Served3 (gpd) Mater Source Location Permit 8 (ft) Aquifer (gpm) Date
CARBON COUNTY
Boyer YL Ranch, 8 ml.
,5600337
25
1 ,250
Well n
UNK
UNK
UNK
UNK
UNK
UNK
EPA data base lists one well,
NE of Savery
1
no identifiable record at SEO
Dick's Service,
5600172
600
12,000
weii n
UNK
UNK
UNK
UNK
UNK
UNK
EPA data base lisis 3 wc]lc,
Lamont
Well n
UNK
UNK
UNK
UNK
UNK
UNK
no identifiable record at SEO
Well 53
UNK
UNK
UNK
UNK
UNK
UNK
Gay Johnsons, W of
5600102
750
7,500
Cay Johnsons
Well
n
21/88-14
1488
100
Upper
Tertiary
(80)
11/19/64
EPA data base lists 5 wells.
Rawlins
Gay Johnsons
Well
02
21/88-14
1489
100
Upper
Tertiary
(80)
11/18/64
only 4 have records at SEO.
Well 03
UNK
UNK
UNK
UNK
UNK
UNK
Gay Johnsons
lnc.
04
21/88-14
26400
200
Upper
Tertiary
15
3/21/75
Gay Johnsons
Inc.
#5
21/88-14
26401
200
Upper
Tertiary
15
4/3/75
Red Hills Service,
5600339
25
500
Spring
UNK
UNK
UNK
UNK
UNK
UNK
EPA data base lists one sprlnj
Raw]ins
no identIf lab 1e record at SEO
Three Forks - Muddy
5600350
35
1,750
Erickson #1
28/89-27
27507
223
Upper
Tertiary
10
9/17/77
Well originally permitted for
Gap Service
domestic use only
1st ENL Erickson
01
28/89-27
50290
223
Upper
Tertiary
12.7
N.A.
Enlarged for expanded yield
and use.
FREMONT COUNTY
Cove Bar & Grocery,
5600712
25
250
Well #1
UNK
UNK
UNK
UNK
UNK
UNK
EPA data base lists one well.
South Pass City
no identifiable record at SEO
SWEETWATER COUNTY
Bitter Creek Rest Area
- 5600470
1,000
5.000
Bitter Creek
01
19/99-10
1642
472
Wasatch
30
10/66
West, 13 ml. E of
Point of Rocks
Bitter Creek Rest Area
- 5600469
1,000
5,000
Bitter Creek
02
19/99-11
1643
720
Wasatch
30
10/66
East, 13 ml. E of
Point of Rocks
Black Butte Coal Co.,
5600638
400
8,000
Bluebell 13
19/100-33
28456
1,219
Mesaverde
50
3/18/75
F1owing wel1
9 mi. SE of Point of
Rocks
Creston Junction
5600331
100
500
Well n
UNK
UNK
UNK
UNK
UNK
UNK
EPA data base lists one well.
Standard Station,
no identifiable record at SEO
Creston Junction
Divide Cafe & Truck
5600327
200
1,500
Well tfl
UNK
UNK
UNK
UNK
UNK
UNK
EPA data base lists one well,
Stop, W of Rawlins
no identifiable record at SEO
Jim Bridger Power
5600639
500
25,000
Green River
—
—
—
—
--
Surface water is only source
Plant, 3 mi. N of
listed by EPA.
Point of Rocks
Jim Bridger !
n
20/101-3
6437
1,451
Mesaverde
600
4/15/71
Well permitted for constructs
plant, and domestic use.
-------
Table A-7. (continued)
Facility
EPA PWS
ID l"
Reported
Production
Population Rate
Served3 (gpd)
Water Source
Total
SEO Well Depth
Location Permit (ft)
Aquifer
Reported
Yield Completion
(gpm) Date^
Remarks
SWEETWATER COUNTY (continued)
5600101
Moyers Service,
Red Desert
Red Desert Standard*
Red Desert
Table Rock Service,
Table Rock
5600542
5600099
100
100
250
1,650
500
3,200
Moyer #1
Well n
Well
19/95-4 14942
UNK UNK
UNK UNK
210 Wasatch
UNK UNK
UNK UNK
10
UNK
UNK
8/30/73 EPA data base also indicates
Wamsutter as a source.
UNK EPA data base lists one well,
no identifiable record at SEO.
UNK EPA data base lists one well,
no identifiable record at SEO.
^Data from U.S. Environmental Protection Agency (EPA) Public Water Supply Inventory (1979).
^Data from Wyoming State Engineer (SEO) well permit files.
>
-------
APPENDIX B
SUMMARY OF HYDROLOGIC PROPERTIES
OF MAJOR WATER-BEARING ZONES
GREAT DIVIDE AND
WASHAKIE BASINS
-------
APPENDIX B
SUMMARY OF HYDROLOGIC PROPERTIES OF MAJOR WATER-BEARING ZONES, GREAT DIVIDE AND WASHAKIE BASINS
Ma j or
Water-bearlng Zones
Data
Type3
Number
of Data
Points
Summarized
Yield
Range
(SPm)
Specific
Capacity
Range c
(gpm/ft)
Porosity
Range
c % )d
Permeability
Range
(apd/ft )
Transralssivity
Range
(gpd/f t)
f
Remarks
Quaternary Aquifers
WW PUB
SEO
49
50
<1-200
<1-300
Upper Tert iary
WW
PT
12
3-25
<1-6.3
-
-
100-10,000
10 specific capacities
Aquifers
<1 gpm/ft.
WW
PUB
1
42
-
-
-
-
WW
PO
5
6, 16,7
-
-
-
-
Only two with yield data
Tertiary Aquifer
WW
PT
52
<1-325 .
85
_
20-150,000
Most yields <100 gpm
Sys tern
17 specific capacities <1 gpm/ft.
Most transmissivities <2,500
gpd/ft.
WW
PUB
54
1-220
-
-
-
-
WW
P0
16
15-250
-
-
-
-
CMTW
45
10.6-30
<1-2.9
-
<1-3,157
OW
DST
14
-
-
-
-
<1-19
2
OF
PUB
25
-
-
12-39
<1-18.2
<1-546
Most permeabilities 20
_
_
25-35,000
Two transmissivities <3,000
gpd/ft.
WW
PUB
8
30-250
-
-
-
-
WW
PO
7
-
-
-
-
-
CMTW
4
60
-
-
-
8, 10
Two wells yield 60 gpm each
OW
DST
18
-
-
-
-
<1-2,883
OF
PUB
56
-
-
8-26
<1-1.8
<1-54
Most transmissivities <5 gpd/ft.
Frontier Aquifer
WW
PT
4
10-106
<1-30
_
-
600-30,000
WW
PUB
17
1-100
<1
-
-
-
WW
PO
3
20
-
-
-
SP
PO
2
-
-
-
-
-
OW
DST
21
-
-
-
-
<1-6,552
OF
PUB
31
-
-
7-25
<]-4.5
<1-164
Most transmissivities <10
gpd/f t.
OW
PO
4
-
-
-
-
CJoverly Aquifer
WW
PUB
10
25-85
<1-1.3
_
340-1,700
OW
DST
29
_
_
-
-
1-175
Most transmissivities <20 gpd/ft.
OF
PUB
34
-
-
8-25
<1-18
<1-260
Sundance-Nugget
Aquifer
WW PUB
WW PO
OW DST
OF PUB
OW PUB
4
2
24
14
6
27, 28
35
<1
3-21
<1-4.8
240
1-3,500
<1-493
Most transmissivities <100
gpd/ft., several estimates from
Entrada Sandstone.
One reported yield.
Paleozoic Aquifer
System
Tensleep Aquifer
WW PUB
OW DST
OF PUB
OW PUB
OW PO
1
17
14
10
1
<1-15
<1-8.2
<1-374
<1-318
24-400
-------
APPENDIX B
(continued)
Ma j or
Water-bearing Zones
Data
Type
Number
of Data
Points
Summar ized
Yield
Range
(RPm)
Specific
Capacity
Range
(gpm/ft)C
Porosity
Range
(%)d
Permeability
Range
(gpd/ft2)e
Transmi ssivity
Range
(gpd/ft)
Remarks
Madison Aquifer
WW PT
1
100
100
_
-
150,000
WW PUB
8
5-400
100
-
-
200,000
SP PUB
1
-
-
-
-
-
OW DST
7
-
-
-
-
9-22
OF PUB
3
-
-
12-13
<1
5-68
OW PUB
2
-
-
-
-
-
Cambrian and
Precambr ian Aqu i fers
WW PT
WW PUB
WW PO
SP PUB
OW DST
OF PUB
13
8
73
1
2
2
2-150
100-150
b-250
<1-150
12, 12.3
<1
6-300,000
<1, 27
33-37
Most transmissivities <1,000
gpd/ft. Only one specific
capacity >10 gpm/ft.
- Water well pump test
- Published water well data
- Water well potentiometric data only
- Spring potentiometric data only
Data Type
WW PT
WW PUB
WW PO
SP PO
^Yield Range
gpm - gallons per minute
cSpecific Capacity Range
gpm/ft - gallons per minute per foot of drawdown
"^Porosity Range
% - percent
^Permeability Range
gpd/ft2 - gallons per day per square foot
^Transmissivity Range
gpd/ft - gallons per day per foot
SP PUB - Published spring data OW PUB
OF PUB - Published oil field data SEO
OW DST - Oil well drill stem test CMTW
OW PO - Oil well potentiometric data only
Published oil well data
State Engineer's Office
Coal mine test well
-------
APPENDIX C
RECORDS OF WELLS AND SPRINGS
IN THE GREAT DIVIDE AND
WASHAKIE BASINS
-------
~op I
_Cl_
[ATI
18
20
20
1 5
25
10
1 2
5
35
80
15
6
30
26
25
10
JO
28
25
18
10
I 5
22
22
1 5
14
20
15
I 5
18
50
14
14
APPENDIX C
RECORDS OF EXISTING WELLS AND SPRINGS IN THE GREAT DIVIDE AND WASHAKIE BASINS
Geologic^ Date
Forma t ion of Test
Wei 1
Description
Reference^
Elevation
Water
Leve 1
(ft bel.
surface)
Potentio-
roetric
Surface
Eleva t ion
(ft abv msl)
Yield
(fipm)
Specif ic
Capacity
(gpm/ft of
drawdown)
Transmis-
sivity^ Data
(gpd/ft) Source^
Qal
1914
n
10
25
SEO
Qal
1958
GD/W
Qal
1912
WS ,0
Flowing
25
SEO
Qa 1
1920
WS,I)
10
15
SEO
Qal
1920
1)
1
25
SEO
Qal
1900
WS, D
20
20
SEO
Qal
1900
WS , D
15
20
SEO
Qal
1959
D
6
33
SEO
Qa 1
1
GD/W
Qal
1927
D
25
3
SEO
Qal
1958
GD/W
Qal
D
3
25
SEO
Qal
1920
WS ,D
2
12. 5
SEO
Qal
1945
WS,D
6
15
SEO
Qal
1973
D
9
25
SEO
Qal
1900
WS ,D
15
25
SEO
Qal
1979
D
5
0?
SEO
Qal
1976
D
15
25
SEO
Qal
1978
D
7
SEO
Qal
1934
D
-0.1'
5
SEO
Qal
1979
M
18
0
SEO
Qal
1979
D
8
20
SEO
Qal
1900
1)
13
15
SEO
Qal
1980
D
SEO
Qal
1980
0
SEO
Qal
D
10
50
SEO
Qal
r
10
300
SEO
Qal
1977
D
3
15
SEO
Qal
1979
SEO
Qa 1
1931
WS,D
10
25
SEO
Qa 1
1965
WS , D
10
2
SEO
Qal
1980
WS.I)
5
0
SEO
Qal
GD/W
Qa I
CD/W
Qal
1958
GD/W
Qal
1960
M
1 3
40
SEO
Qal
1961
M
L3
40
SEO
Qal
1979
SEO
-------
r>
ho
l.ocal ion'1
ToLnl
l)ej>i h
(ft)
Tested or
Per f orated
Lniorvn1
(Ct)
Geologic^
Forma Iion
Da te
of Test
We 11
Description
Re ference^
Eleva tion
ALLUV 1 UM - QUATERNARY (continued)
12-91-5 dd
14.5
Qai
1978
I)
6
12-91-5 dd
Qa 1
1980
1 2-91-7 dc
16
Qal
1910
D
8
I 2-91-9 cn
36
Qal
1975
WS .D
19
12-91-9 cn
1 3
Qal
1977
WS ,D
5
12-91-9 cn
1 3
Qal
1977
D
6
12-91-9 db
30
Qal
1978
0
6
12-91-10 cn
5.5
Qal
1940
WS,D
4
12-91-10 cc
4
Qa 1
1924
WS ,D
12-91-11 n,i
1 2
Qal
1973
WS ,D
4
12-91-II aa
1 2
Qa 1
1958
l2-91-12 ab
25
Qnl
1948
WS ,D
8
I 2-9 I-l2 nb
20
Qal
1900
WS,D
5
I 2-92-I abb
1 36
Qal
I 2-92-I 2 bba
15
Qal
l 2- 100-22 ,ib
Qal
I 2-102-24 ba
Qa 1
1963
S
13-89-22 an
22
Qal
1941
D
13-89-^fi dad
18
Qal
13-91-32 ad
31
Qal
1973
WS.I.D
17
14-90-8 ddn
50
Qal
14-104-31 bd
Qal
15-94-4 d
50
Qa I
15-102-34 cb
22
Qal
15-104-14 c
39
Qnl
16-88-26 dd
Qnl
16-91-27 bbb
Qs
16-92-29 dad
Qal
1958
S
16-93-19 (,c
40
Qa]
17-90-17 bh
Qs
1958
17-90-32 ac
20
Qs
1945
WS , D
5
17-92-12 b
Qal
1958
S
19-93-15 a
Qal
L9-102-6 cd
30
Qal
22-101-22 bab
Qa 1
s
23-88-16 cb
9
Qnl
23-88-24 dab
Qa 1
23-104-26 bdd 32
Qa 1
23-104-33 bdd 30
Qal
24-87-6 ad
21
Qs
APPENDLX C (continued)
Water
Level
(ft bel.
surface)
Potentio-
mctric
Surface
Elevation
(ft abv rosl)
Yield
(spm)
Spec i f ic
Capacity
(gpm/ft of
dravdown)
Transrais-
sivity*-
(gpd/ft)
25
SEO
SEO
25
SEO
10
SEO
2.5
SEO
25
SEO
15
SEO
25
SEO
25
SEO
20
SEO
GD/W
10
SEO
10
SEO
37
GD/W
13
GD/W
GD/W
F-15
GD/W
25
SEO
6
' GD/W
30
SEO
32
GD/W
GD/W
22
CD/W
10
GD/W
5
CD/W
GD/W
CD/W
CD/W
dry
GD/W
200
GD/W
5
SEO
F-10
GD/W
CD/W
22
GD/W
3
GD/W
5
CD/W
CD/W
11
CD/W
8
GD/W
4
GD/W
-------
0
Location
To t a 1
Depth
(fo
Tested or
Perforated
Intervo1
(ft)
Geologic^
Formation
Date
of Test
Wc 11
Description0
Refer
Eleva
ALLUVIUM-QUATERNARY
(continued)
24-87-13 bab
1 5
Qal,Qs
1964
35
24-88-30 bd.i
•2220
26-45
Qal
<1935
24-88-30 h-i.i
2220
43-45
Qal ?
<1935
24-88-31 hi)
2300
45-70
Qal?
<1935
flh,
" 1 ' 1 1 » |
t '»r>n
70-72
Qal ?
(Ml
•H 935
".-Kf.-S 1„
i
10KO
()-()7
o.< I
Qd*
1920
25-86-9 t(c
3790
0-91
Qd?
<1935
25-86- 1 7 .ibb
4920
115-120
Qd?
<1920
25-87-1 7 c.<\
Qs
25-87-22 bed
70
Qs
26-88-32 abb
Qs
1964
S
1
26-88-35 bd(_
5. 5
7-5. 5
Qd?
1922
26-88-36 hdc
Qs
s
26-88-36 da
0-85
Qd?
<1935
26-88-36 db
5.5
Qal
1922
C.D
2
26-89-16 cdb
28
Qal ,Qs
22
26-89-21 b.i
40
20-30
Qa 1
1976
D
15
27-97-32 cda
Qal
29-100-12 ac
10
Qal
1978
D
7
NORTH PARK
15-87-18 lc
60
26-60
Tnp
7610
19-87-30 b.i
160
80-160
Tnp
D ,WS
7600
17-88-33 bda
205
Tnp
8/64
7 700
I 7-88-33 to
36
Tnp
10/51
S(19)
BISHOP CONGLOMERATE
16-104-8 ddtl
I 20
Tbi
8/63
7600
BROWNS PARK
12-90-3 cd
100
80-100
Tbp
I) ,ws
6210
12-90-5 da
45
21-41
Tbp
p
6365
12-90-6 an
160
120-140
Tbp
0
6488
12-90-8 be
1 25
95-125
Tbp
D
6 300
12-90-10 bb
95
70-95
Tbp
0 ,ws
6 390
12-91-9 ad
90
65-90
Tbp
D
6275
12-91-9 ad
60
Tbp
I) ,WS
6275
12-91-10 cb
Tbp
6390
12-92-3 bde
Tbp
6390
APPENDIX C (continued)
Potentio-
Water metric Specific
Level Surface Capacity Transmis-
(£t bel. Elevation Yield (gpm/£t of slvity^ Data
surface) (ft abv msJ ) (gpm) drawdown) (gpd/ft) Source^ Remarks 1
3
.3
art.
100
b
7
34
20
2 5
1
5
2
2 5
5
7 7603 20
80 7520 4
13 7687 6
78 7522 42
20 6190 7.5
.2 6320 20
90 6398 5
8 6292 20
30 6360 15?
75 6200 25
40 6235 25
20 6370
37 6353
CD/W
D
D
D
D
'.n/w
Ui/W
D
D
D
GD/W
GD/W
GD/W
D
GD/W
D
SEO
CD/W
SEO
CD/W
SEO
1.43 1000 SEO
.06 150 SEO
GD/W
GD/W
CD/W
.25 500 SEO
.63 1000 SEO
.08 200 SEO
.33 700 SEO
.75 1500 SEO
.29 600 SEO
6.25 10000 SEO
USGS
uses
-------
Tested or
Total Perforated
Depth Interval
Location* (ft) (ft)
Geol °gick
Formation
Date
of Test
Wei 1
Reference
De sc rlp t ion Eleva t ion
0
1
UROWNS PARK (continued)
12-92-3 cdb
12-92-4 bch
12-92-4 bcc
12-92-4 bcc
12-92-4 cac
12-92-4 dab
12-92-4 db 450
12-92-5 db 210 1 70-
1 2-92-5 deb
12-92-6 licb
12-92-10 cbn
12-93-1 b.-i.n
12-96-14 b
13-88-10 be
13-88-29 ada
13-88-29 nda 15
13-89-20 cn
13-92-31 cc,i
13-92-31 dac
13-92-32 dbc
13-92-33 ccc
14-87-33 ca 55
15-85-1 ca 106
16-87-22 ebb
16—88—4 hcc
16-88-4 bcc
17-85-31 ben
17-104-26 cidd
60
600
39-55
4-18
36-48
100-106
Tbp
Tbp
Tbp
Tbp
Tbp
Tbp
Tbp
Tbp
Tbp
Tbp
Tbp
Tbp
Tbp
Tbp
Tbp
Tbp
Tbp
Tbp
Tbp
Tbp
Tbp
Tbp
Tbp
Tbp
Tbp
Tbp
Tbp
Tbp
10/63
5/60
11/54
6370
6305
6 310
6290
6340
6310
6420
6285
6340
6385
6520
6320
7910
7130
7100
6930
6440
6 340
6422
6365
7914
7400
7950
8000
8040
7220
BATTLE SPRING
22-90-23 da
22-91-8 cbc
23-91-26 aaa
24-90-2 ddd
24-92-J 6
24-93-20 cn
24-93-20 dd
24-93-29
192
504
250
365
424
Tbs
Tbs
Tbs
Tbs
Tbs
Tbs
Tbs
Tbs
5/63
10/63
6/64
10/63
6600
6540
6540
6540
APPENDIX C (continued)
Potentio-
Water metric Specific
Level Surface Capacity Transmis-
(ft bel. Elevation Yield6 (gpm/ft of sivity^ Data
surface) (ft abv msl) (gpm) drawdown) (gpd/ft) Source^ Remark:
107 6263 USGS
56 6249 USGS
38.25 6271 USGS
28.6 6261 USGS
59 6281 USGS
25.7 6284 USGS
25 6395 3 .04 100 SEO
30 6255 2.5 .03 100 SEO
97.2 6242 USGS
94.4 6290 USGS
124 6396 USGS
44.44 6276 USGS
104 USGS
5 7905 USGS
8 7122 USGS
8 7092 CD/W
40 6890 USGS
100.8 6339 USGS
184.6 6155 USGS
137.6 6284 USGS
97.2 6267 USGS
40 7874 5 .63 1000 SEO
6 7394 16.7 D
5 7945 D
128 7872 D
129 7911 USGS
18 7202 USGS
30 CM
24 6576 3 CD/W
2 CD/W
62 6538 5 CD/W
20 GD/W
300 CM
53.5 6487 15 1.15 1880 CM
50.9 6489 30 .33 395 CM
33.5 6507 15 .54 1230 CM
-------
APPENDIX C (continued)
Potentio-
Tested or Water metric Specific
Total Perforated Level Surface Capacity Transmis-
IJepth Interval Geologic Date Well Reference^ (ft bel. Elevation Yield (gpm/ft of sivity Data
Location'1 (ft) (ft) Formation of Test Description0 Elevation surface) (ft abv msl) (gprn) drawdown) (gpd/ft) Source8 Remarks
BATTLE SPRING (continued)
25-96-23 f.bd
Tbs
10/63
S
GD/W
26-90-7 cc
36 7
102-367
Tbs
M
7275
82
7193
85
. 52
1000
SEO
26-94-30 ccd
Tbs
10/63
S
GD/W
27-90-28
Tbs
S
CM
2 7-91-4 ba
3441
1826-3360
Tbs
M
9020
1050
7970
37
.17
300
SEO
27-91-34 ad
36 5
80-365
Tbs
M
7775
110
7665
96
.59
1300
SEO
27-92-1 cc
8 50
440-850
Tbs
M
7 700
210
7490
150
1.5
2500
SEO
27—92— 7 bb
4 20
300-340
360-420
Tbs
M
6843
57
6786
108
.35
900
SEO
27-92-7 cl
154
134-144
Tbs
M
6832
8
6824
17.5
.44
600
SEO
27-92-7 cc
145.6
8-145
Tbs
M
6832
8
6824
20. 1
.29
300
SEO
27-92-7 cc
162.8
8-20
Tbs
M
6835
8
6827
21
.31
300
SEO
27-92-7 cc
152.6
8-25
Tbs
M
6832
8
6824
10
.15
150
SEO
27-92-7 cd
157.1
143-155
Tbs
M
6832
11
6821
15.1
.23
2000
SEO
27-92-7 cd
1 74
11-174
Tbs
M
6830
11
6819
24
.38
250
SEO
^ 27-92-7 cd
163
11-163
Tbs
M
6833
11
6822
24
.38
250
SEO
^ 27-92-7 cd
1 71
7.1-20
Tbs
M
6828
11
6817
19.6
.29
150
SEO
27-92-7 dc
155
138-148
Tbs
M
6848
26.4
6821
5. 1
.12
200
SEO
27-92-7 dc
1 55. 3
27-155
Tbs
M
6848
27
6821
19.2
.26
150
SEO
27-92-7 dc
155
27.4-155
Tbs
M
6848
27.4
6820
19.6
.27
150
SEO
' 7-fP-7 (1.
1 -> 7 .
26.4-157
Tbs
M
6851
26.4
6825
20.6
.60
500
SFO
? "1- I ' .| .
1.''
155-2 15
;5'>-
1 hi
M
(,860
1 1
f>849
1 57
. 79
1 50
sro
760
649-729
Tbs
7220
236
6984
15. 1
.06
29
CM
28-92-29
440
357-437
Tbs
7031
135
6896
20. 2
.26
198
CM
28-92-29
200
118-198
Tbs
6887
101
6786
1 1
2.89
3157
CM
28-92-29
280
194-279
Tbs
6989
1 29
6860
11.8
.14
80
CM
2.>0
133-218
'lbs
6999
168
683 1
10.6
. 33
294
CM
LAN 1 ^
13-96-15 ac
710
Tgl
7/63
1 7
GD/W
14-99-15 b
104
Tgl
8/63
10
CD/W
15-98-18 a
Tgl
7/58
S
GD/W
16-99-2 bd
Tgl
7/58
S
200
GD/W
18-95-9 b
Tgl
7/58
s
1
GD/W
27-96,97W
360-380
Tgl
7127
149
6978
190
CM
360-380
Tgl
7129
150
6979
180
CM
360-380
Tgl
7123
143
6980
300
CM
380-400
Tgl
7075
108
6967
135
CM
389-415
Tgl
7076
107
6969
120
CM
380-400
Tgl
7072
105
6967
165
CM
380-400
Tc 1
7072
105
6967
117
CM
-------
Tested or
Total Perforated
Depth Interval Geologic Date Well Reference^
Location3 (ft) (ft) Formation of Test Descrlptionc Elevation
LANEY (continued)
Tgl
Tgl
Tgl
Tgl
Tgl
Tgl
Tgl
Tgl
Tgl
Tgl
Tgl
Tgl
Tgl
Tgl
n
^ GREEN RIVER (UNDIVIDED)
13-99-16 cc
80
40-80
Tg
60
C
13-99-18 bdc
80
55-80
Tg
60
C
13-99-18 db
690
325-345
575-595
630-690
Tg
43
C
7300
13-99-19 acb
82
72-82
Tg
60
C
13-99-21 bdc
82
45-82
Tg
60
C
13-99-21 dbd
80
55-80
Tg
60
C
13-99-21 dcd
81
45-81
Tg
60
C
13-100-9 caa
377
368-377
Tg
52
D,C
7175
14-99-21 b
12180
200+
Tg
1/61
14-100-36 abc
82
Tg
60
16-99-3 dda
140
90-104
Tg
42
C
7200
16-99-11 b
235
40-150
Tg
42
C
7100
16-99-11 b
308
130-165
Tg
42
C
7100
16-99-11 bba
255
Tg
42
C
7100
16-99-18 cad
80
50-80
Tg
60
C
16-99-22 cbd
309
195-200
230-309
Tg
56
C
7300
24-97-11 dd
255
175-180
Tg
ws
6700
WASATCH
12-91-8 ac
420
390-420
Tw
D ,WS
6300
12-91-8 baa
415
Tw
10/63
12-95-4 ddd
325
120-127
Tw
37
D,C
APPENDIX C (continued)
Potentio-
Water metric Specific
Level Surface Capacity Transmis-
(ft bel. Elevation Yield8 (gpm/ft of sivity Data ^
surface) (ft abv msl) (gpm) drawdown) (gpd/ft) Source^ Remarks
110 CM
130 CM
110 CM
110 CM
120 CM
120 CM
120 CM
120 CM
110 CM
110 CM
120 CM
120 CM
120 CM
120 CM
D
D
125 7175 67 D
D
D
D
D
350 6825 D
D
D
19 7181 100 D
34 7066 200 D
44 7056 250 D
36 7064 200 D
D
160 7140 15 D
40 6660 17
15 .39 700 SEO
2 GD/W
42 D
-------
Tested or
Total Perforated
Depth Interval Geologic Date Well ^ Reference^
Location0 (ft) (ft) Formation of Test Descrlptionc Elevation
WASATCH (continued)
12-100-24 ab
2240
875-890
Tw
6/28
12-101-3 cab
881
860-881
Tw
55
D, C
7050
12-101-10 dca
740
495-505
665-675
Tw
29
D,C
7050
13-94-12 hn
1 10
58-110
Tw
12/41
C,WS
6400
13-94-13 nc
200
180-200
Tw
D.WS
6405
1 3-97-28 d.i
150
90-140
Tw
12/41
c.ws
13-99-22 ccc
82
60-80
Tw
60
C
13-99-27 bbc
80
50-80
Tw
60
C
14-92-12 :ic
1 10
93-110
Tw
L2/61
WS
64 20
14-92-22 ab
145
57-145
Tw
12/41
c.ws
6410
14-93-32 bb
143
90-143
Tw
12/49
C.WS
14-101-30 ba
145
Tw
9/63
71 30
16-92-7 ad
440
80-160
Tw
D.WS
6660
16-92-17 dbb
330
40-65
105-115
Tw
59
C
6600
16-101-8 acc
1 15
Tw
60
C
16-101-10 dac
335
285-320
Tw
51
c
7100
16-102-14 an
115
Tw
60
c
I 7-93-11 bb
600
560-600
Tw
M
6750
18-93-2
265
180-210
230-258
Tw
M
6805
]8-93-16 c,i
300
180-280
Tw
M
6736
18-98-1 bhel
572
354-358
498-517
Tw
45
C
7100
18-98-28 b10 10000 STO
8 GD/W
L 75 6635 28 D
art. 6750+ 20 D
art. 6750+ 15 D
-------
Tested or
To La I Perforated
DepLh Interval Geologic Date Well Reference^
Location3 (fc) (ft) Formation of Test Description Elevation
WASATCH (continued)
20-94-34 abd
1801
Tw
7/58
6800
20-94-34 abc
1801
Tw
21
C
6750
20-94-34 .icn
1 365
Tw
1902
C
6750
20-94-34 bhd
Tw
20-97-3 aa
1910
Tw
8/64
6750
20-97-28 hba
500
Tw
7/58
6850
20-98-3 dh
6460
1040-1300
Tw
5/58
6 700
20-99-10 dt-b
305
60-65
225-265
Tw
WS
6990
21-95-34 bed
93
Tw
10/63
6620
21-97-34 bb.i
74 5 7
Tw
22-93-28 bb
105
Tw
5/63
6850
22-98-22 bb
7642
1612
2000-3000
Tw
4/60
OA
6600
22-99-B dbd
6100
Tw
9/63
22-9'J-28 atm
195
Tw
7/58
23-96-24 cc
2250
Tw
31
6500
23-96-25 hb;i
2250
Tw
10/63
23-102-32 bb
108
Tw
9/63
7200
24-98-2 cd
180
Tw
6/64
6700
24-101-32 ai
1 25
55-84
Tw
60
WS
7500
26-94-I 7 hha
260
65-85
145-245
Tw
C
6850
26-94-17 bbc
285
265-280
Tw
56
C
6850
26-96-27 dn
300
285-300
Tw
48
WS
6900
CATUKDRAl. BLUFFS
I 7-94-12 lc
300
100-120
180-220
240-260
Twc
N
6 700
17-94-13 nd
180
140-180
Twc
d.ws, i
6618
18-94-18 cr
580
415-580
Twc
M
6764
18-94-28 cd
350
220-240
280-320
Twc
M
6764
FORT UNION
12-92-15 abc
4029
1600-3288
Tfu
7/49
6400
12-93-11 bb
5506
3345-3357
3370-3785
Tfu
2/62
OA
14-103-35 bdd
Tfu
7498
16-92-17 dbb
Tfu
17-92-12 bdd
Tfu
6800
APPENDIX C (continued)
Potentio-
Water metric Specific
Level Surface Capacity Transrais-
(ft bel. Elevation Yield0 (gpra/ft of sivity^
surface) (ft abv msl) (gpm) drawdown) (gpd/ft)
24 6776 GD/W
art. 6750+ 67 D
art. 6750+ 10 D
250 CM
51+ 6750+ 32 GD/W
76 6774 GD/W
art. 6700+ D
40 6950 30 D
48 6572 30 CD/W
10 GD/W
68 6782 GD/W
art. 6600+ D
110 GD/W
11 GD/W
art. 6500+ 30 D
50 CD/W
78 7122 3 GD/W
22 6678 30 CD/W
34 7466 25 D
65 6785 34 D
60 6790 50 D
48 6850 17 D
.25 600
30 6588 50 50 100000 SEO
415 6349 125 .63 900 SEO
70 6649 53 -59 800 SEO
art. 6400+ D
art. II D
uses
uses
USGS
-------
Tested or
Total Perforated
Depth Interval
Location0 (ft) (ft)
Geologic Date Well
Formation of Test Description12
Reference .
n
I
VO
FORT UNLON (continued)
17-92-14 bb 250
1 25
1 76
18-91-1 acc
18-91-1 acc
18-91-2 bbd
18-91-29 edd
18-91-29 edd
18-92-24 db 460
18-100-11 neb
18-100-11 at-b
18-100-22
18-100-28
18-100-29
18-100-29 d.uJ
18-100-33 cdn
19-90-5 cci'
19-90-8 cdb
19-90-18 ana
19-91-5 ccd
19-91-8 dc
19-92-1 bd
19-92-2 cm
19-92-25 bca
19-99-2 cbc
( '¦ Wi 1 ' 1
550
11
.on
19-99-/
-------
APPENDIX C (continued)
Tested or
ToLal Perforated
Depth Interval
Location*' (ft) (ft)
Geologic
Wei 1
Water
Level
Reference (ft bel.
Formation of Test Description Elevation surface)
Potentio-
tnetric
Sur face
Elevation
(ft abv msl)
Specific
Capacity Transmis-
Yield6 (gpm/ft of sivity^ Data
(gpm) drawdown) (gpd/ft) Source
g
0
1
I 740
155
70
150
FORT UNION (continued)
20-89-7 ahc
20-89-8 ccc
20-90-5 dab
20-90-7 aa
20-90-12 cba
20-90-18 bed
20-90- 1.9 da
20-90-23 bbc
20-90-23 bbc
20-90-23 ddb
20-90-23 ddb
20-90-31 ebb
20-90-31 ebb
20-90-34 acc
20-91-1 I dec
20-91-15 bbh
20-91-21 db
20-91-33 im,i
20-91-35 lcI,i
20-93-17 cb
20-93-17 cb
20-95-12 d 10478
20-95-14 d 10345
21-89-10 dda
21-89-21 ccc
21-89-22 aa.i
21-89-22 .ian
21-89-22 jd
21-89-2: (Jda
21-89-22 cb
21-90-26 db
21-100-7 cb
21-100-35 dn
21-101-2 db
22-99-8 dbd
132-152
50-69
3318-341 1
3549-3624
340
180
60-180
6100
370-7
573-618
653-710
Tfu
Tfu
Tfu
Tfu
Tfu
Tfu
Tfu
Tfu
Tfu
Tfu
Tfu
Tfu
Tfu
Tfu
Tfu
Tfu
TFu
Tfu
Tfu
Tfu
Tfu
Tfu
Tfu
Tfu
Tfu
Tfu
Tfu
Tfu
Tfu
Tfu
Tfu
Tfu
Tfu
Tfu
Tfu
1900
7/63
6/58
1/59
6 /64
OA
OA
OA
DA
10/58
6862
7024
6750
6860
6750
6860
6830
6855
6855
6980
6980
7000
7026
6930
6866
6990
6914
7031
6822K
6822K
6710
6662
6 700
6750
6705
6705
66 78
6723
66 50
66
168
300
116
150
20
80
70
74
66
86
37
160
130
75
220
71
20
4!
30
37
44
30
44
6796
6856
6450
6744
6710
6810
6775
6785
6906
6914
6914
6770
6860
6839
6811
6818
6804
6639
6642
6659
6720
6668
6661
6648
6679
6800
6785
6870
6650+
20
.07
30
.001
200
3.0 2500
2496
33.9
75
75 150000
uses
uses
D
SEO
uses
USGS
SEO
USGS
USGS
USGS
USGS
GD/V
USGS
USGS
USGS
USGS
USGS
USGS
USGS
DST
DST
D
D
USGS
USGS
USGS
GD/W
SEO
uses
USGS
USGS
CM
CM
CM
D
Transmissiviry may be overestimated
-------
a
Location
Total
Depth
(ft)
Tested or
Perforated
I nterva1
(ft)
Geologic^
Formation
Date WeLl
of Test Description
Rc fcrcn
Elevati'
TERTIARY (UNDIVIDED)
21-87-19 bb
165
140-160
Tu
D,C
6840
21-88-13 bb
140
20-140
Tu
D
6950
21-88-13 cd
215
190-195
Tu
D,WS
6930
21-88-13 db
200
100-200
Tu
D
6930
21-88-14 cc
100
30-LOO
Tu
D
7090
21-88-14 cr
200
20-40,
140-180
Tu
M,C
7090
22-88-24 tic
47
Tu
12/54
7000
27-96-20 bd
350
150-210
240-270
290-350
Tu
M
7000
27-97-25 bd
385
357-373
Tu
M
7126
27-97-25 db
408
388-403
Tu
M
7073
28-92-21 nc
800
600-640
Tu
D,C
7400
28-92-28 t.c
220
L 33-218
Tu
M
6999
28-92-32 nd
440
357-437
Tu
M
6825
28-101-34 db
70
45-70
Tu
D
7230
LANCE
15-100-6 ;ib
6230
6105+
Kl
7400
16-101-11 be
1700-1805
K1
OP
7121K
17-99-8 db
336 5-3658
Kl
OA
7060K
17-100-24 db
4474-4514
K1
OP
7381K
18-91-1 bd
200
155-175
Kl
M
7103
18-99-34 ,i.i
3650-3693
K1
OP
6818K
18-100-10
6 5
54-65
Kl
6668
18-100-20
I 50
Kl
6807
19-92-32 dn
5684-5718
Kl
OA
7277
L9-92-J2 d.i
6184-6233
Kl
OA
7277
19-98-21 db
3931-3957
Kl
OP
6744K
19-100-8
1 98
178-198
Kl
6927
19-100-15
164
144-164
Kl
6898
L9-L00-3I
L50
130-150
KL
6883
21-88-19 ac
305
245-305
Kl
D
6840
21-99-10 cc
3030-3102
Kl
OA
71 50K
22-96-28 ca
6030-6050
Kl
OA
6591 K
23-99-14 ac
5239-5261
Kl
OP
6724K
24-101-31 bd
364 3-3680
Kl
OA
7473
APPENDLX C (continued)
Potentio-
Water metric Specific
Level Surface Capacity Transmis-
(ft bel. Elevation YieLdG (gpm/Et of sivity^ Data
surface) (ft abv msl) (gpm) drawdown) (gpd/ft) Source^ Remark
15 6825 20
29 6921 9.5
25 6905 12
35 6895 5
10 7080 85
15 7075 15
4 6996
150 6850 40
153 6973 10.2
112 6961 8.4
347 7053 5
168 6831 10.6
135 6690 20.2
40 7190 8
art. 7400+
6724
6776
5801
63 7040 .015
6694
48 6620
88 6719
6091
6513
6529
179 6748
144 6758
28 6855
40 6800 7
6336
6341
6718
6653
.67 L000 SEO
.11 100 SEO
.13 200 SEO
2.5 4000 SEO
>85 1000000 SEO
.5 800 SEO
CD/W
>40 70000 SEO
.17 300 SEO
.05 100 SEO
.02 40 SEO
.34 700 SEO
.26 500 SEO
.8 300 SEO
D
DST
. 3 DST
. 7 DST
<.001 20 SEO
U DST
13.24 CM
21.7 CM
1.8 DST
3.5 DST
8.7 DST
9.28 CM
.82 CM
6.36 CM
.13 150 SEO
5,3 DST
1.6 DST
1.5 DST
4 DS'I
-------
Tested or
Total Perforated
Depth Interval Geologic, Date Well ^ Reference
Location'1 (ft) (ft) Formation of Test Description0 Elevation
25-102-17 be
5792-5892
Kfh
OA
7501K
LEWIS
12-98-14 db
11210
98 78-9897
10574-10745
Kle
10/60
OA
16-91-27 deb
71
Kle
10/63
18-97-6 da
6790-6850
Kle
OP
7180K
18-97-6 da
6743-6800
Kle
OP
7180K
18-99-26 ab
5040-5107
Kle
OP
6747K
21-97-6 db
5888-5928
Kle
OA
6693K
21-97-19 ab
5864-5951
Kle
OA
6849K
21-98-1 d
5787-5845
Kle
OS
6680K
21-99-22 aa
3782-3785
Kle
OA
7168K
ALMOND
16-100-J 7 aa
6080
5555-5585
Kal
L7-101-35 bb
2291-2336
Kal
OA
7075K
17-101-35 bb
2372-24 78
Kal
OA
7075K
18-99-1 J bb
5440-5493
Kal
OA
6773
18-99-24 dd
6304-6621
Kal
OA
6954K
18-100-7
137
] 17-137
Kal
6745
18-100-11 db
2650-2700
Kal
OA
6830K
18-100-13
87
Kal
6901
19-100-2 ad
2665-2685
Kal
OA
7030K
19-100-2 ad '
2851-2862
Kal
OA
7030K
21-100-10 cu
3131-3197
Kal
OA
7104K
21-100-10 cc
3132-3142
Kal
OA
7104K
21-101-21 ada
1 200
215-450
789-1200
Kal
P ,D »C
6800
22-104-15 ccd
8/64
23-101-4 cb
4963-5018
Kal
OA
7189
24-101-31 bd
4722-4866
KaJ
OA
7473
ER1CS0N
15-102-4 bb
60
Ke
9/63
16-102-20 bca
1 15
Ke
c
18-100-22 bb
5850
1925-1943
2190-2275
Kc
12/60
19-99-29 bd
3930-3950
Ke
OA
7089K
APPENDIX C (continued)
Potentio-
Water metric Specific
Level Surface Capacity Transmis-
(ft bel. Elevation Yield0 (gpra/ft of sivity^ Data
surface) (ft abv msl) (gptn) drawdown) (gpd/ft) Source^ Remarks
6995
D
CD/W
6350 .5 DST
599L -5 DST
5776 2.9 DST
6073 2.9 DST
6013 1.1 DST
5718 1.2 DST
6606 6.5 DST
D
6836 8.8 DST
6790 5.7 DST
5909 .8 DST
5517 .7 DST
14 6731 9.65 CM
6228 2.2 DST
71 6830 8.3 CM
6560 5.3 DST
6458 15.8 DST
6639 11.5 DST
6583 2.9 DST
120 6680 250 D
CD/W
6435 4.2 DST
6635 4.3 DST
CD/W
60 n
D
2883 DST
-------
APPENDIX C (continued)
Tested or
ToLa I Per forated
Depth InLervnl
Location'1 (ft) (ft)
Geologic Date
Wei 1
Re ference
Formation of Test: Description" Elevation
Potent io-
Water metric
Level Surface
(ft be 1. Elcva t ion
surface) (ft abv msl)
Spec i f ic
Capacity Trarvsrois-
YieldC (gpm/ft of sivity
(gpm) drawdown) (gpd/ft)
Source^
ERICSON (continued)
20-100-22 bbc 6052 2253-2292 Ke
5186-5237
20-100-30 cc 1400? Ke.Kal
20-100-36 cb 2578-2604 Ke
20-101-27 caa 90? Ke,Kr?
20-101-27 cbd 480 Ke
21-101-21 ada 1200 215-450 Ke
789-1200
7/60
C
P , I), C
6977K
6520
6800
17
1 7
120
6532
6503
6680
100
250
43.4
D
GD/W
DST
GD/W
D
D
n
ROCK SPRINGS
15-103-26 ana 120 Kr
18-100-8 cc 1000 Kr
18-101-18 bbb 400 Kr
18-101-18 bda 400 Kr
18-101-18 dc 110 48-110 Kr
20-101-27 caa 90 Kr
I 20-101-27 cbc 1112 Kr
M
LaJ
BLAIR
15-103-22 bud 60 5-60 Kbl
16-104-8 ddd 120 100-120 Kb I
17-104-26 add 250 148-178 Kbl
18-105-14 dc Kbl
20-102-28 db Kbl
60
9/63
16
16
60
7/58
05
60
36
36
D.WS.I
D,WS,I
C
C
D, C
D,C
7000
7000
6520
6520
7620
8200
17
17
78
140
6992
6992
6503
6503
7542
8060
250
250
100
42
30
60
60
D
GD/W
0
D
D
D
D
D
D
D
CM
CM
MESAVERDE (UNDIVIDED)
12-90-12 bb
13-89-15 dd
13-89-32 d
13-103-8 da
14-91-11 dd
! 60
85
100-160
85
4864 1450-3800
10040
14-102-36 abc 4092 1900-2455
16-91-21 aac
16-92-13 ac
16-92-17 db
16-101-11 be
L8-90-3 a
18-90-3 add
19-89-9 aa
2933
4297
10415 9296-9422
9690-978!
2548-2600
250
605
2 50
138-200
Kmv
Kmv
Kmv
Kmv
Kmv
Kmv
Kmv
Kmv
Kmv
Kmv
Kmv
Kmv
Kmv
7/59
10/63
D ,WS
D,WS
S
OP
C
c:
c
6560
6720
6680
7121K
7170
71 70
7600
100
07
art.
art.
art.
6460
6720
6680+
6868
7170+
71 70+
7600+
20
<25
20 35000
-1.67 2500
SEO
SEO
GD/W
D
D
D
GD/W
D
D
DST
D
0
D
Transmissiv1ty may be overestimated
-------
APPENDIX C (continued)
To l a 1
Depth
Location' (ft)
Tested or
i'er forated
IntervaI
(ft)
Geologic^
Formation
Date
of Test
We 11
c
De script ion
Reference^
Elevation
Water
Level
(ft bel.
surface)
Potentio-
metric
Surface
Eleva tion
(ft abv msl)
Specific
Capacity
Yield0 (gpm/ft of
(fcpm) drawdovm)
Transmis-
sivicy^
(fcpd/ft)
Da ta
Source®
Remarks*1
MKSAVERDE (UNIHV IDED) (cont inued)
19-89-9 cc
2681
500-2681
Kmv
C
7600
art.
7600+
D
21-98-35 da
6100-6115
Kmv
OP
6771
6322
2.7
DST
26-89-1 dd
180
50-180
Kmv
D.WS
6540
60
6480
15 3.0
3000
SE0
25-102-26 bd
6410-6546
Kmv
OA
7229
6193
5.1
DST
27-93-35 ca
4257-4330
Kmv
OA
7107K
7078
66. 7
DST
27-93-35 ca
4969-5027
Kmv
OA
7107K
7069
2.4
DST
BAXTER, STEELE* Nl
OBRARA, CODY
14-87-33 ca
1 1 7
97-117
Kn-?
WM
7914
7
7907
3 0.03
10
SEO
Possibly Ks
14-89-1 bdd
Kb-Kst
7310
uses
15-88-30 bb
Kst
S
(7100)
F
7100+
SEO
17-103-8 bbd
Kb
7310
USGS
1 7-104-10 bad
16-
-7 0-76
Kb-?
W,D,C,WS
(7000)
F
7000+
D
Sandstone & shale
18-89-17 bed
Kb-Kst
7380
USGS
19-86-36 baa
Kb-Kst
6 720
26
6694
USGS
19-88-22 dd
Kb-Kst
7083
USGS
I 9-104-23 ad
Kb
6307
180
6127
USGS
21-88-5 dda
335
Kc-?
7155
30,31
7L24
8-7
GD/W
Cretaceous undivided-?
22-89-17 ebb
Kb-Kst
6655
USGS
26-89-17 cb-l
162
Kc
(6700)
F- ?
6 700+
SEO
26-89-17 cb-2
208
Kc-?
(6700)
F-?
6 700 f
SEO
26-89-17 cbd
208-
. ?
Kc-7 ,Qal
(6650)
140
6510
GD/W
Same as well cb-2 (7)
26-89-18 ch
208
1 95-208-7
Kst-7
(6760)
195-?
6565
22
D
Same as well cb-2 (?)
26-89-1 a da
1 26
Kc
(6700)
F-?
6700+
SEO
26-89-18 dnb
1 26
100-126-?
Kst- 7
(6720)
100-?
6620
10
D
Same as we 11 da (?)
26-90-3 ctd
860
770-790
Kc-?
"I lulc"
D
27-89-15 ai.
120
Kc
--
7
6370
WR
Sp. Cond. = 7000
27-89-34 bd
105
Kc
—
42
6525
WR
27-90-33 ml
35
Kc
(7350)
20
7330
SEO
28-90-26 bc-1
100
Kc
(6720)
35
6685
SEO
28-90-26 bc-2
180
Kc
(6720)
60
6660
SEO
28-92-8 ca
730
649-729
Kc-?
WM
(6590)
236
6354
15 0.06
1500
SEO
28-92-18 aa
2.1 5
Kc
10
6550
WR
28-92-L8 be
8
Kc
S-7
(6660)
4
6656
SEO
28-92-28 ab
1 500
500-1500
Kc-7
WM
7516
" 500
7016
40-50 0.10-0.12
80
SEO
28-92-28 ac
I 4 10
530-1410
Kc-?
WM
7449
757
6692
42 0.07
200
sen
28-95-26 db
180
Kc
(fi900)
100
6800
SEO
-------
APPENDIX C (continued)
PotentJo-
Tested or Water metric
Total Perforated Level Surface
Doplh Interval Geologic Date Well Reference^ (ft bel. Elevation
Location'^ (fi) (ft) Formatlonb of Test Description0 Elevation surface) (ft abv msl)
FRONTIER
13-87-15 da
4 5
Kf-
?
WD
(7500)
28
7472
14-103-10 ab
9379
5735-5791
Kf
73
OA
7081
2908
15-102-34 d
901 2
8880-9002
Kf-
Kd
77
OA
7128
5200
16-103-16 bb
4822
3810-3849
Kf
60
OA
7257
5822
17-88-2 cd
1000
Kf
(7390)
F
7390+
17-102-17 dc
8720
4370-4511
Kf
74
OA
6647
6537
18-88-3 dc.i
1026
Kf
Kcv
7242
F
7242+
18-88-3 da
(7225)
18-88-10 ac
Kf
18-88-10 ac
210
Kf
(7380)
80
7300
18-88-10 bda
1000
460-486
Kf
WD,P,C
(7375)
F
7375+
18-88-10 db
210
Kf
7340
15,80-?
7260
18-88-11 bb
165-
?
Kf
7260
F
7260+
o
18-RB-22 bb
90-
?
Kf
7560
+5-?
7565
h-1
Ln
18-88-27 baa
860
Kf
(7420)
10
7410
18-90-11 ba
10330
7525-7575
Kf
71
OA
7551
7492
18-101-28 be
7910
6843-6867
Kf
63
OA
7233
6325
18-103-6 bb
3250
2301-2318
Kf
73
OA
6403
6687
18-103-16 ccc
2654
2590-2625
Kf
Oil
F-?
19-90-36 be
10795
7840-7896
Kf
71
OA
7689
5848
20-88-34 bh
3460
2960-3065
Kf
Ol 1
(74 30)
7430
22-103-20 bd
7585
6482-6532
Kf
75
OP
6866
6399
23-88-3 cb-l
7
Kf-
?
ws
(6790)
6
6784
23-88-3 cb-2
7
Kf-
?
WS
(6790)
F
6790+
23-88-6 cbc
Kf
6533
F
6533+
23-88-6 dbd
2561
1020-1125
Kf
Ol 1
(6790)
F-9
6790+
23-88-8 ccc
2445
1 190-I 225
Kf
oi!
(6650)
K-?
6650+
23-88-16 cb-L
100
24-28-?
Kf
6837
24
6813
23-88-16 cb-2
100
17-22-7
Kf
6837
22
6815
24-88-30 bde
2200-
7
Kf
651 1
F
6511+
25-87-2 dab
2600
1770-1780
Kf
(6900)
F
6900+
25-88-3 cc
4908
1692-1 71 5
Kf
61
OA
6 784
6568
25-88-11 bb
2863
1730-1770
Kf
62
OA
6764
6554
25-88-31 ac
6715
2103-2163
Kf
66
OA
6486
6595
25-89-11 dbb
1845
1840-1845
Kf
(6580)
F
6580+
Specific
Capac ity
Yield6 (gpm/ft of
Transmis-
sivity^
(gpm) drawdown) (gpd/ft) Source
0.83
20
F-l 5
38
50-100?
50
30
F-50-7
F-20-?
F-5-?
50-?
F-l-7
1
20
30
F-1-?
0. 29
20*
30*
90
2
3
1
3
10
18
15000
20000
54
L0
6552
SEO
DST
DST
DST
SEO
DST
GD/W
R
R
D
D
GD/W
GD/W
GD/W
GD/W
DST
DST
DST
D
DST
D
DST
SEO
SEO
GD/W
D
D
SEO
SEO
GD/W
D
DST
DST
DST
D
Probable water cushion in DST recovery
Sp. Cond. = 1150
Dual completion with Kcv (test
in both aquifers) ^
Field coef. of perm. = 17 gpd/ft ;
saturated thickness - 20'
Produces 50 gpm; possibLy could
produce 100 gpm
Triple completion with Kd,Jm
Salt water; probable water cushion in
DST recovery
Salt waLer; poor DST
Sp. Cond. = 4800
Triple completion with Kd»Jsd
"Sa1t water"
Dual completion with Kd
Sp. Cond. - 6000
Salt water
Muddy water
Very poor DST
Water "brackish"
-------
APPENDIX C (continued)
To La I
Depth
Location' (ft)
Tested or
I'c r f orated
Interval
(ft)
Geologic^
Formation
Date
of Test
Wei 1
Description
Re ference^
Elevation
Water
Level
(ft bel.
surface)
Potent io-
metric
Surface
Eleva t ion
(ft abv msl)
Specif ic
Capacity
Yield0 (gpm/ft of
(gpm) drawdown)
Transrois-
sivityf
(Rpd/ft)
Data
Source®
Remarks*1
FRONTIER (continued)
25-89-12 ab
J 541
J 995-2002
Kf
60
OA
6548
6582
24
DST
Gas cut water
25-89-24 ccc
2010
?-2010
Kf
(6550)
F
6550+
D
25-89-26 foea
3439
_?
Kf
6495
F
6495+
F-10-?
GD/W
Sp. Cond. ¦= 3500
26-87-26 bca
4623
1095-1305
Kf
(7000)
1200-?
5800
D
26-87-30 dd
4557
4414-4474
Kf
59
OA
7033
6750
3.5
DST
Sulfur water
26-88-28 ddd
251 1
1595-1605
Kf
(6810)
F
6810+
D
1220-1650
Kf
26-88-30 cc
3264
2045-2087
KF
54
6602
6632
7
DST
26-88-32 hi)
2971
1882-1912
Kf
54
OA
6693
6598
13
DST
Fresh water
26-88-33 ad
5000
1 199-1290
Kf
78
or
6801
5936
6
DST
26-89-25 ac
2373
2300-2360
Kf
59
OA
6600
6539
1
DST
Muddy fresh water
26-90-3 ad
5380
1814-1898
Kf
74
OP
7129
6403
28
DST
Salt water ; poor DST
26-90-9 b.n
6400
5129-5169
Kf
67
OA
6574
6388
3
DST
26-95-6 n
7955
3960-4536
Kf
77
OA
698 7
7010
23
DST
Poor DST
27-89-1 4 ba
220
130-J 40
Kf
WD
6580
35
654 5
106 0.53
900
SEO
MUDDY
25-89-14 dc
6544
2826-2900
Kind
64
OA
6496
6350
8
DST
26-88-30 cc
3264
3089-3106
Kind
54
6602
6604
3
DST
26-90-3 ad
5380
2617-2680
Kind
74
OP
7129
5169
1 7
DST
26-90-14 cb
7010
4779-4796
Kmd
57
OA
6881
4316
3
DST
27-95-5 cb
1852
1005-1050
Kmd & Kmr
74
OA
6959
6676
12
DST
CLOVISRM (LAKOTA-DAKOTA)
I 2-92-i 0 cc
1 6248
13443-13779
Kcv & Kmd
60
OA
6563
950'
1. 1
DST
13-87-33 dc
64 7 5
5585-5600
Kd
75
OA
7760C
7370
36
DST
Probable water cushion in recovery
13-89-15 db
7958
6053-6066
Kd
66
OA
6978
7365
2
DST
14-88-34 cb
7192
5247-5305
Kd
67
OA
7976
7440
1 6
DST
14-103-10 ab
9379
6225-6330
Kd ,Jm
73
OA
7081
4870
4
DST
16-103-16 bb
4822
4216-4252
Kd
60
OA
7257
5818
10
DST
Oil & water cue mud; gas cut
salt water
17-88-1] aa
580
Kcv-?
F
F-85
GD/W
Sp. Cond. = 913
—
Kcv
(7425)
7425+
85 0.86
1600
R
4 other Kcv wells flow 25-65 gpm
580
Kd
Wl'
(7425)
F
7425+
85
D
City of Raw!ins
J 7-88-LI ba
620
Kd
ws
(7500)
F
7500+
25
D
18-88-3 da
—
Kcv.Kf
(7225)
38 0.29
340
R
Field coef. of perm. = 17 gpd/ft^;
saturated thickness = 20'
18-88-10 bda
1000
928-955
Kd,K f,Km
W , P , n, c
(7375)
F
7375+
70
n
Water quality "good"
Triple complelion with Kf.-Im
18-88-10 bda
—
Kc v
(7390)
-
6 5 0.26
4 50
R
18-88-10 bda
1000
Kcv
(7360)
+287
764 7
65
GD/W
Sp. Cond. » 346
-------
APPENDIX C (continued)
Total
DepUi
Location3 (ft)
Tested or
Perforated
IntervaI
(ft)
Geologic^
Formation
Date
of Test
Well
Descr Ip t ion
Reterence
E Leva tion
Water
Level
{It bel.
surface)
Potent io-
metric
Surface
Eleva t ion
(ft abv msl)
Specific
Capacity
Yield6 (gpm/ft of
(gpra) drawdown)
Transmi^-
sivity
(Rpd/ft)
Data
Source®
Remarks*1
C [,() VF.R 1 .Y (LAKOTA-DAKOTA) ( cone inued )
18-88-10 bdd
960
Kd
Kcv
WP
(7390)
F
7390+
42
4 3 1.36
1 700
D
R
Field coef. of perm. = 25 gpd/ft^;
saturated thickness * 69
18-101-28 be
7910
7315-7385
Kd
63
OA
7233
6545
175
DST
Salt water; poor DST
18-101-28 be
7910
7386-7512
Kd & Jm
63
OA
7233
6379
19
DST
Salt water
18-102-6 cd
4420
3740- 3793
Kd
73
OA
6481
6616
45
DST
Gas cut black water; poor DST
18-102-18 ab
4715
4022-4033
Kd
72
OA
6593
6462
14
DST
Probable water cushion in DST recovery
18-103-6 bb
3250
2948-2978
Kd
73
OA
6403
6386
5
Poor DST
18-103-8 db
3133
2594-2623
Kd
71
OA
6558
637-4
48
DST
Salt water; poor DST
18-103-8 db
31 33
2653-2716
Kd
71
OA
6558
6423
47
DST
Gas cut salt water; poor DST
18-104-25 dc
24 78
2368-2388
Kd
oil
D
19-89-34 ab
13356
5702-5820
Kd
74
OP
7554
7318
17
DST
•
19-102-19 a
4857
4281-4345
Kd
60
OA
6477
6557
14
DST
19-102-19 a
4857
4355-4420
Kd
60
OA
6477
6338
5
DST
Gas cut salt water
19-102-30 cc
4216
3812-3850
Kd
65
P
6500
6484
11
DST
Sulfur water
19-103-12 cb
4455
3930-3978
Kd
77
OA
6369
5742
2
DST
Salt water
19-103-25 dd
42J6
3812-3850
Kd
65
P
6499
6481
12
DST
Transmissivity may be overestimated;
salty sulfur water
19-103-36 ca
4100
3886-3910
Kd a Am
70
OA
6527
6497
4
DST
23-88-6 dbd
2561
1928-2031
Kd
oil
(6 790)
F
6790+
D
Triple completion with Jsd and Kf
23-88-8 ccc
2445
2431-2440
Kd
Ol 1
(6650)
F
6650+
D
Dual completion witli Kf
24-88-29 dd
3805
1810-1835
Kd & Jm
80
OP
6516
6823
2
DST
Gas cut water
26-88-30 cc
3264
3202-3221
Kc
54
OA
6602
5891
9
DST
26-89-23 ba
4554
4503-4554
Kd?
73
OA
6670
5816
1
DST
26-90-11 ac
5641
3830-3880
Kd
68
OA
6837
5689
35
DST
Mud and gas cut water; poor DST
26-90-14 cb
7010
5065-5095
Kd
57
OA
6881
5068
DST
26-94-17 bb
9728
9506-9513
Kd
56
OA
6817
6745
1
DST
27-95-8 aa
1600
1441-1500
Kd
62
OA
7092
6631
3
DST
Fresh water
28-93-4 dd
4470
4440-4465
Kd
oil-PB
(7000)
4450-?
2550-?
90
Dissolved solids = 7000 ppm
28-93-21 ab
7034
6900-69L2
Kd
69
OA
8147
3731
7
DST
28-94-36 bb
10720
10615-10637
Kd
74
OA
7500
5712
1
DST
Gas cut salt water; poor DST
30-93-32 bd
6592
4243-^278
Kla
oil
(64 20)
F-?
64 20+
3 DST recovered 2350-5925'
"fresh water"; triple comple-
tion with Jsd, Pt
MORRISON
13-89-17 ad
8055
6444-6457
Im
54
01'
70 30
__
DST
Incomplete data
17-103-33 ba
4665
4225-4296
Jm-J s?
62
OA •
7699
6495
177
OST
Black mid cut svilfur vateci poor DST
with probable water cushion in recove
18-88-10 bd
1000
.Im
(7380)
16
7364
1 20+
SEO
Probably same as 10 bda
18-88-J0 bda
1000
968-983
Urn
W,P,D,C
(7375)
F
7375+
50
D
Water - "soft"
19-102-19 a
4857
4566-4619
Jm
OA
6477
5924
1
DST
G?s cut salt water
-------
Total
Depth
Location (ft)
Tested or
Perf orated
IntcrvaI
(ft)
Geologic Date Well
Forma Lion of Test Description
Water
Level
Reference^ (ft bel
Elevation surface
MORRISON (continued)
19-J03-2 dc
4375
3805-3923
Jm & Kd
77
OP
6375
20-103-18 be
4973
4046-4167
Jm
72
OA
6513
20-103-24 da
5465
5307-5465
Jm & Kd
57
OA
6697
23-103-29 dc
8600
8551-8576
Jm
67
OP
7203
27-95-29 be
4558
4155-4182
Jm
57
OA
7409
SUNDANCE AND
ENTRADA
13-89-17 ad
8055
6655-6700
Je
54
OP
70 30
16-104-16 dd
71 26
3340-3346
le
73
01'
7299
1ft-87-27 ccd
2523
2515-2523
Jsd
oil
18-102-12 cd
6746
6490-6630
Je (, Jca
55
OP
7005
19-88-34 da
Js
(7200)
19-88-34 daa
1890
1750-1770
Js
WS
(7190)
19-88-34 dac
Js
(7155)
J 9-102-35 an
8644
6391-6426
.Is
52
OA
7117
19-103-28 cd
4250
420 3-4211
Je
74
0ft
6772
23-88-6 dbd
2561
2415-2505
Js
oil
(6790)
24-87-13 aad
3300+
3300-?
Js
O I 1
(6620)
25-89-14 bac
34 7 7
34 72-3477
Js
oil
(6570)
?6-rq_7 Mr
5886
4065-4073
Js
o 1 1
(6770)
JO-u t- i ' ].,l
f> V>2
Wi6-4692
is
"11
(64 20)
NUi.U.l
12-92-10 t-c
16248
14 140-14273
Je A In
60
OP
6563
14-88-34 be
7192
5840-5860
Jn
67
OA
7976
14-101-18bb
1 2900
10711-10770
Jn
75
OA
7094
15-91-23 bd
1 1 248
8776-8800
Jn
64
OA
6779K
16-92-12 dc
12533
9686-9726
Jn
78
OA
666J
16-101-J 5aa
14482
I 1820-11845
Jn
72
OP
7090
16-104-16 dd
7126
3550-3571
Jn
73
OP
7299
17-99-14 db
20000
16222-16506
Jm7,Is-Jn
78
OP
70 70
17-102-17 dc
8720
5788-5838
In
74
OA
6647
18-90-11 ba
10330
8755-8785
Jn-Js
71
OP
7551
18-101-32 bd
8121
8057-8071
In
74
OP
7032
18-102-12 dc
6746
6683-6746
Jn
55
OP
7005
F
167
F
F
1800
F- ?
IX C Icont inucd J
Potentio-
metric
Surface
Elevation
(ft abv msl)
Specific
Capacity Transmis-
Yieltle (gptn/ft of sivity Data
(gpm) drawdown) (gpd/ft) SourceS
6397
7103
5818
4940
66 79
3
44
2
1
6
DST
DST
DST
DST
DST
Sal t water ; poor DST
Gas cut sulfur water
Muddy water
Gas cut water
6535
7190+
6988
6723
6
-------
Tested or
Total Perforated
^ Depth Interval Geologic Date Well ^ Reference^
Location (ft) (ft) Formation of Test Description Elevation
NUGCblT (continued)
18-102-12 dc
6746
6701-6714
Jn?
55
op
7005
19-87-29 ad
581 1
3740-4107
Jn & Trc
71
OA
6993
19-102-35 n;i
8644
6588-6631
Jn
52
OA
7117
19-103-18 cc
41 20-
7
Jn
19-104-18 ccb
Jn
24-87-1 cb
64 54
4 776-48 L6
Jn
59
OA
6 7 76
25-89-12 bn
3541
34 73-3481
Jn
60
OA
6548
26-90-3 bb
78 78
4100-4175
Jn
64
OS
7145
26-95-6 a
7955
5942-5954
Jn
77
OA
6987
27-95-18 bdd
4 78 7
1690-1740
In
(7150)
27-95-18 bd
Jn
7140
28-93-2 ad
5340
5092-5135
Jn
76
OP
6759
CHUGWATER
13-89-15 db
7958
6548-6574
Trc
66
OA
6978
16-104-16 dd
71 26
4 532-45 70
Trc
73
P
7299
18-90-11 bn
10330
8755-8785
Trc 9
71
OA
7551
19-87-29 da
581 1
4090-4200
Trc
71
OA
6993
28-89-33 be
60
Trc
__
PHOSPHORIA -
PARK CITY
16-104-16 dd
71 26
5459-5489
Pp
73
OP
7299
16-104-16 dd
71 26
5511-5672
PP
71
op
7I>Qq
17-102-17 cd
8720
7580-7607
Pp?
74
n\
664 7
27-95-9 be
3990
3535-3580
Pp
57
OP
7154
27-97-25 ad
3700
2800-2878
PP
59
OA
7040
28-91-20 an
81 30
7665-7780
Pp & Trd
73
OA
7178
28-93-4 ba
6292
6158-6190
6210-6224
6234-6284
Pp
Oil-PB
28-94-2 bd
3095
2184-2226
Pp
54
OA
6726
29-96-20 ab
2578
1531-L561
Pp
(6675)
30-96-7 beb
269
229-269
Pp
(5890)
30-97-U b
408
Pp
APPUNDJX C (continued)
Potentio-
metric
Specific
Level
(ft be].
surface)
Surface
El evation
(ft abv tnsl)
Capac ity
Yield6 (gpm/ft of
(ftpm) drawdown)
Transmis-
sivity
(gpd/ft)
Da ta
Source^
Rema rks'1
6532
663
DST
Poor DST
7481
370
DST
Poor DST
6641
2166
DST
Sulfur waLer ; poor DST
F
( )
F-200?
GD/W
Spec. Cond. = 13000-?
6319
uses
6059
1
DST
6235
30
DST
5400
114
DST
Gas & mud cut water ; poor DST
6327
8
DST
200-500
6800
35
D
Total dissolved solids = 10436
200
6940
uses
5717
10
DST
2 DST
6388 .5 DST
74 78 14 DST
7456 2 DST
6620 WR
6522 12
6318 7
6600 7
6871 1
6855 3
6848 20
30
F 66754-
F-? 5890+ 700-?
'>() r)HK)
DST Transmissivity may be under-
estimated
Bl.uk water
nsr Hr.ii k ish I I w »l rr
DST Black sn I L w.ner; p DSl
recovery
DST
DST
DST
D Dissolved solids - 4600 mg/L
Yield applies to 3 intervals
combined
DST
D Dual completion with Mm
DST record 320* sulfurous water
D Located north of study aren
Sn fond. = 1800
WR S|». Com! = 1400
-------
Tested or
Total Perforated
Depth Interval
Location" (ft) (ft)
Geologic^ Date
Formation of Tea
Well
Reference^
Elevation
TENSLEEP AND
WEBER
13-88-8 d
8163
8010-8089
t
Oil
14-101-18
12900
L27 71-12800
Pw 75
OA
7094
15-91-11 ba
10329
t
OA
6665C
16-91-8 dd
10913
10865-10913
l 75
OA
6608C
16-104-16 dd
7126
5700-5756
w 73
OP
7299
17-89-2 bba
1607
1050-1392
t or Mm
W-?
17-102-17 dc
87 20
7810-7850
l 74
OA
6647
1 '0 .i.i .
I'.t) I
24 32-
(
ls-101- 12 .Hi
DIDII
10048-10066
W 75
OA
71 29
19-88-10 cb
6305
6167-6220
t 74
OA
7224
i 1o j¦> .i.i
Hf»4
8587-K617
l 5y
71 17
21-8 7-2 li.ui
980
600-800-?
1- f
(6900)
21-87-16 ccc
650
Ira, ft
1m, ft
( )
21-87-16 cc
305
t
(6700)
21-88-4 ac
1 520
1481-1520
t 58
OA
7915
22-88-28 bdd
2255
2161-2217
t
23-88-20 aaa
(7400)
23-89-1 <_bb
4818
4770-4811
t
oil
(6650)
24-87-27 dc
6313
6157-6175
t 70
OA
6580
25-87-11 ba
6442
6360-6400
t 75
OA
6860
25-88-3 cc
4908
4805-4871
t 61
OA
6784
25-89-14 dc
6544
5260-5310
t 64
OA
6496
26-87-32 bb
46 75
4420-
t-TrPc 58
OA
6998
26-89-6 cd
7818
6340-6402
t 78
OP
6978
26-9 5-6 a
7955
7791-7859
i 77
OA
6987
28-98-18 bb
8380
8340-8 380
I 51
OA
5662
29-93-9 aa
6552
6301-6 34 3
I
oil
30-93-32 bd
6592
6525-6582
Pt
oil
AMSDEN
16-104-16 dd
7126
6150-6173
r-' 73
OP
7299
18-97-30 dc
22290
21686-22293
Pm 74
OP
7547
O
I
hO
o
APPENDIX C (continued)
Potentio-
Water metric Specific
Level Surface Capacity Transmis-
(ft bel. Elevation Yield (gpm/ft of sivity Data
surface) (ft abv msl) (gpm) drawdown) (gpd/ft) Source8 Remarks
6900
6638 .1
7142 .5
64 56 .7
6610 23
71*3
6372 5
600 6300
F 400
L95
F 6 700+
7725 374
F 7400+ 200-?
F-? 6650+ 24
6164 1
654] 5
6823 156
67J9 8
6979 .4
4
6994 4 5
5856 60
F- ?
D Rec. 1893' "fresh" water
Dissolved solids e 1363 ppm
DST
DST
DST
DST
U
D
I) DST roc . 440' si. mnddv water
DST Gas nil -.ulfur wilcr
T Mud-In. ->m I l in w.ili'i ; " i . h \ h I i- u.i I rr
i u^li 11 -u w i ' .i 11 • I r. \. i \
DSI Su1fur wa ler
D
D Dual completion with Mm
R Water "rather" highLy mineralized
SE0
DST
D DST rec. 350' water
GD/W Sp. Cond. = 58)
D Water quality "good"
DST
DST Brackish water
DST Black sulfur water; poor DST
DST
DST
DST
DST Poor DST
DST Sulfur water; poor DST
D DST records 5610 feet of "fresh"
water
D 3 DST rec. 2350-5925' "fresh"
water; triple completion with
Kla, Jsd
6358
6370
DST
DST
Cas and mud cut water
-------
APPENDIX C (continued)
To t a 1
Dcpi >>
(i L )
Tested or
Perforated
InLorv.t I
(ft)
Ceolufci
Korm.ii 10
Date We 1 I
of Test Description
16-92-12 cd 1 2533 1 2!50-1 2310 Mm
78
OA
Reference,
6661
Wa ter
Level
( f L be 1.
s»rf nee)
Pote-ntio-
me t r ic
Sur face
Elev.it ion
(ft abv msl)
7 260
16-101-11 ba 1049 7 15013-15035 Mm
72
7135
6317
16-104-L0 dd 7126 7074-7130 Mm
17-89-2 bba 1607 1050-1392 Pt or Mm
17-100-4 db 15211 15145-15211 Mm
18-97-30 dc 22290 21686-22290 Pa & Mm
73
74
74
OP
W-?
OP
OP
7299
6884
7547
6496
6917
6838
l »•
• vw
I
-------
Tested or
Total Perforated
lk-i'i
b hitcrva 1
Ceo 1 ok it ,
Date
' . ! '
Kl III! IH'I
I.I» If inn"' (1 I )
....(J. O
!• *•» riii,11 i on
of Test
Dcsi i 11'( i • •'
l.lt vii un
( AM 1 IA;.1 (I'NM 1 ) Mi ))) (< out ituji-il )
Zl-oz-JJ cc
2Ub
(6990)
>1-88-11 cd
s
6
S
(7300)
7- V 7- : * h« I
580 | 280-1 \2 1
H
60
OA
70 26
I'KLl.AMIJK IAN (L'N!)J V UJEI)).
1 7_ I |)(|
pG
s
14-87-1 c, i—l
S
pG-?
S
14-8 7-1 c;i- 2
s
Pe-?
S
15-87-8 be
8
pG
15-8 7-12 dn
1 Ul
pG
W-M
(8380)
15-87-32 cd
S
pG
S
29-87-28 na
70
p6- ?
'-1 . (1
iO
pG
i- G
s
—
' 0O-I 1 < «
hO
pb
__
29-100-11 da
60
pG
29-100-1 2(1 )
39
pG
29-100-12(2)
61
pG
29-100-12(3)
56
PG
W-D
29-100-1 2 aa
80
PG
29-100-12 nb
34
pG
W-D
7665
29-100-12 en-1
(S3 46-61
p6
w-n
29-100-12 ca-2
68
pG
w-n
7710
29-100-12 ca-3
39
P6
29-100-12 cn-4
65
P6
29-100-12 r.n-5
41
PG
W-l)
29-100-12 cn-6
60
PG
29-100-12 ca-7
31
Pe
W-D
29-100-12 ca-8
60
pG
29-100-12 ca-9
37
pG
W-l)
29-100-12 ca-10
60
pG
29-100-12 ca-11
5
pG
S
29-100-12-cb-l
56
29-100-12-cb-2
77
PG
29-100-12-cb-3
40
pG
29-100-12-cb-4
50
pG
29-100-12-cc-1
50
pG
29-100-12 cc-2
60
pG
W-D
29-100-12 cc-3
40
Pe
29-100-12 cc-4
3!
pG
APPENDIX c (continued)
Potentio-
Water metric Specific
Level Surface Capacity Transmis-
(ft bel. Elev.itLun ld° (gpm/fL of sivily Data ^
surface) (ft abv msl) (m>m) drawdown) (upd/ft) Source^ Remarks '
75
100-'
6915
7300+
6945
SEO
CD/W
nsT
Sp. Cond. =353
Rracki^h salt witer
F
F
F
F
10
F
20
U
F
20
15
9
30
I 7
50
16
40
45
25
25
10
60
19
30
28
F-?
F
23
32
10
20
12
36
7.5
15
83 70
7i6n
7649
7665
10
2
7-10
5
20
3.3
1 50-?
0.03
0.09
0. 56
1.67
0.83
10-12 1.7-2.0
20
10
50
400
300
50
300
500
150* 120000
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
WR
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
Gran ito
Sp. (\>nd. = 130; out of study area
Water-bearinft faul t
-------
APPCNDTX C (continued)
Tot a 1
!'. |.l li
Ml)
Tested or
Perforated
1 n Lerv.i I
(fL)
Ceoli-Kiu
forma t ion
Da te Wo I 1
of TesL Hesti IpL ion
Re f erence ,
Water
Leve 1
(ft i.el .
surf .ii e)
['KIT I'l i <\\ (I'NU I V I MED) (hhil Limed)
29-10"- 11 . < - >
2Q- i nn-11 , , -r>
m,_ |on_ | _> , , _ 7
Z'l-i no- ! > 1-, -h
29-100-12 cc-9
29-100- 1 2 cc-10
29-100-]2 cr- 1 ]
29-100-12 cc-12
29-100-12 cc-13
29-100-12 cc-l.\
29-100-12 cd-1
29-100-12 cd-2
29-100-12 cd-3
29-100-12 cd-4
29-100-12 cd-5
O 29-100-12 cd-6
I
N3 29-100-12 cd-7
29-100-I 2 cd-8
29-100-12 cd-9
29-100-12 cd-10
29-100-12 cd-l3
29-100-12 cd-14
29 — J00— J 2 cd-I 5
29-100-12 cd-1 6
29-100-12 cd-17
29-100-12 dd
29-100-13 nn
29-100-1 3 a 1) -1
29-100-13 ab-2
29-100-13 ad
29-100-13 ba
29-100-20 da-1
29-100-20 da-2
29-100-20 da-3
29-100-20 db-1
29-100-20 db-2
29-100-20 db-3
29-100-20 db-4
<50
p6
1 I
PG
40
Ph
tU3
pfc
50
PG
100
PG
90
PG
60
PG
4b
Pe
92
PG
62
PG
42
PG
1 3
7-1 3
PG
47
p6
100
PG
50
PG
40
pG
1 3
pG
55
PG
100
Pe
146
83-146
PG
60
PG
80
pG
60
pG
38
PG
90
PG
40
PG
38
PG
88
27-88
pG
60
PG
90
pG
140
pG
25
PG
30
pG
60
PG
120
PG
80
pe
60
pG
75
PG
(7000)
(7000)
(7175)
(7175)
(7175)
(7800)
(7900)
5
15
5
1 2
34
39
45
30
15
10
62
40
8
8
42
55
48
27
6
45
12
35
20
56
30
9
50
23
10
59
15
85
96
12
18
1 5
75
1 2
45
22
Potentlo-
metric
Surface
i I i >n
',11 ¦ I»\ nis 1)
Yield
(gpm)
Specific
Capacity
(ftpm/ft of
drawdown)
Transmip-
siv Liy
(Kpd/f t.)
6966
6970
4000
7120
7163
7140
14
2.3
1000
3.5
7704
7825
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
Open hole
Open hole
-------
APPENDIX C (continued)
Locationa
Total
Depth
(ft)
Tested or
Perforated
Interval
(ft)
Geol
Formation
Date Well
of Test Description
Re ference^
Elevation
Water
Level
(ft bel.
surface)
Potentlo-
roetric
Surface
Elevation
(ft abv rosl)
Yield®
(spm)
Specific
Capacity
(gpra/ft of
drawdown)
Transtnis-
sivity^
(Rpd/ft)
Data
Source8
Remarks*1
PRECAMBRIAN
(UNDIVIDED) (continued)
29-100-24 db
6-S
P6
s- -
2
SEO
29-101-13 ac
40
PG
15
SEO
30-87-29 db
S
pG
—
F
6400
R
Out
Sp.
of study area
cap. = 100
30-88-34 bb
s
P6
—
F
6480
R
Out
Sp.
of study area
cap- = 90
30-89-3L be
S
pG
—
F
6495
R
Out
of study area
30-90-15 be
S
PG
—
F
6330
R
Out
Sp.
of study area
cap. e 750
Location (T-R-Sec,1/4,1/16,1/64)
O
I
ro
For abbreviations, see Figure «-1 11-4.
cData type and status or use: OA - abandoned oil test
OP - producing oil well (generally producing
from a different formation)
OS - suspended oil well
S - spring
W - water well
WS - stock well
D - domestic
U - unused
M - miscellaneous
P - public supply
C - commerical, industrial
I - irrigation
PB - plugged back well
( ) - number of wells or springs
K - Kelly Bushing elevation
8,
Feet above mean sea level; elevations in parentheses from 1:250,000 AMS topographic maps.
BWell yield or flow; spring flow
^See Appendix C for tnethology. Number in parentheses indicates value calculated for specific capacity. Assumed one foot of drawdown.
GO/W - USGS Hydrologic Atlas 219 (Welder and KcGreevy, 1966)
USGS - Unpublished data from U.S. Geological Survey
SEO - Wyoming State Engineer's Office file of permitted domestic wells
D - Dana, 1962
R - USGS Water Supply Paper 1458 (Berry, 1960)
DST - Petroleum Information card drill stem test synopsis
WR - USGS Hydrologic AtLas 270 (Whitcomb and Lowry, 1968)
CM - Coal mine tests
^Sp. Cond. - Specific conductivity
Field Coef. of Perm. - Field coefficient of permeability
DST - Drill stem test
Miscellancous abbreviations
S - Spring
F - Flowing well
* - zero drawdown reported
art. - artesian well
? - questionable data
-------
A P P E N
DETERMINATIO
P R 0 P E
D I X D
N OF AQUIFER
R T I E S
-------
APPENDIX D
DETERMINATION OF AQUIFER PROPERTIES
Determination of Transmissivity
from Specific Capacity
For many water wells in Wyoming the only pump test information
available is yield-drawdown-duration data from constant yield well
performance tests. Specific capacity (the yield per unit drawdown)
and an estimation of transmissivity can be determined from these
data.
Walton (1962) rearranged the Cooper-Jacob simplification of
the Theis equation to express the theoretical relationship between
specific capacity and aquifer properties as
4 = 1 (1)
5 [264 log ( - 65.5]
2693 r S
where: ^ = specific capacity (gpm/ft),
Q = discharge (gpm),
s = drawdown (ft),
T = transmissivity (gpd/ft),
S = coefficient of storage,
r = nominal well radius (ft), and
t = time after pumping started (min).
Walton assumes an infinite, homogeneous, isotropic, non-leaky, artesian
aquifer and a fully penetrating well with no well losses. He also
assumes that the effective radius of the well is equal to the nominal
D-l
-------
radius. If drawdown is small compared to saturated thickness, the
same equation can be applied to unconfined aquifers (Brouwer, 1978,
p. 76).
Equation (1) cannot be rearranged to easily express transmissivity
as a function of specific capacity; Walton (1962) constructed a series
of graphs relating transmissivity and specific capacity. The indivi-
dual graphs are each for a specific pumping time, assume a well radius
of 6 inches, and require an estimate of the aquifer's coefficient
of storage. According to Walton (1962, p. 12) "Because specific
capacity varies with the logarithm of 1/S, large errors in estimated
coefficients of storage result in comparatively small errors in coeffi-
cients of transmissibility estimated with specific capacity data."
The transmissivity estimate is insensitive to variations in well
radius for the same reason.
For the transmissivity estimates In this report all wells were
presumed to have effective radius of six inches, in order to use
Walton's (1962) graphs. Confined conditions (artesian, S = 0.0001)
were assumed for wells over 200 feet deep and shallower wells were
assumed to be unconfined (water table, S = 0.2).
Walton (1962) recognizes that partial penetration, well losses,
and geohydrologic boundaries often adversely affect specific capacity,
resulting in underestimation of transmissivity. Delayed drainage
and vertical flow near wells affect specific capacity of water table
(unconfined) wells and also violate some assumptions incorporated
in equation (1). As a result transmissivity estimates based on
specific capacity must be considered as indicative only of the general
order of magnitude of true aquifer transmissivity.
D-2
-------
Quantitative Determination of Aquifer
Properties from Drill Stem Tests
If detailed drill stem test data are available, determination of
aquifer hydraulic properties is relatively simple using the methods
described in Bredehoeft (1965) and Miller (1976) (summarized below).
The concepts involved resemble the recovery analysis of Theis (see
Brouwer, 1978, p. 96) and are based on the non-steady state pressure
buildup following a flow period. Basic assumptions include Darcian
flow, a single fluid phase, a homogeneous and isotrophic reservoir,
and uniform flow rates.
Horner (1951, in Miller, 1976) described the pressure buildup
in the transient state as
m <3 t + At
2.3qp , o
pw" po - mSt 108 — <2>
where t = preceding period of flow,
At = time elapsed since flow period,
q = production rate during test,
y = viscosity of fluid,
k = intrinsic permeability,
h = thickness of producing zone,
Pw = pressure in the well at time At, and
p = undisturbed formation pressure,
o
Bredehoeft (1965) simplified this to
^ 2-30(l
kh _ a
U AirAp
(3)
D-3
-------
where qa = the average production rate during the test, and
t At
Ap = the pressure change per one log cycle of time (In ° )
as axis).
Miller (1976) noted that Todd (1959) says
W
where K = hydraulic conductivity, and
Y = specific weight of water
and then simplified equation (3) to
T " 114 If• (5)
where q = average production rate (gal/min),
3l
Ap = pressure change (psi/log cycle of time), and
T = transmissivity (gal/day/ft).
Miller's (1976) simplification requires water with temperatures
less than A5°C and dissolved solids concentrations below 10,000 mg/1 in
order to limit errors to 1 percent because it assumes unity for the
specific weight of water. Bredehoeft (1965) did not further simplify
his equation because, where it was applied in the Bighorn basin, water
temperatures exceeded 300°F and viscosity and specific weight were there-
fore important variables to consider.
The transient state solution procedure is to plot pressure versus
the logarithm of (t + At)/At, with Ap determined from a straight line
fitted to later time data. Undisturbed formation pressure is determined
by linear extrapolation to the point where log (Ct + At)/At) = 0.
For many drill stem tests the time versus pressure data required
for the rigorous solution presented above are not available in the
public sector. A less rigorous solution which can utilize the publicly
D-4
-------
available data is desirable. Presumption of steady state flow is a
gross simplification which eliminates the need for time data.
Gatlin (1960) presents a steady-state equation for radial Darcian
flow to a well of an incompressible fluid, which is essentially the
Theis equation (seeBrouwer, 1978, p. 67). This equation, simplified
somewhat and rearranged, is
2rrkh(P - p )
(6)
^ y ln(r /r )
e w
where Q = productivity,
k = effective permeability,
h = net producing thickness,
y = fluid viscosity at reservoir conditions,
r ,r = drainage and well bore radii, and
e w °
p^,pw = undisturbed formation and well bore pressures.
The effective permeability (k) incorporates formation damage due to
drilling fluids, which results in reduced permeability of the near-
well altered zone. The transient method avoids this complication
through its biased use of late time data, which better reflect undisturbed
formation permeability. The quantity (p^ - p^) can be viewed as the
steady-state pressure difference which induces the observed flow.
Gatlin (1960) notes that it is commonly assumed that ln(rg/rw) = 2tt
for drill stem tests. Equation (6) thus simplifies to
Q - ^ (pe" "V> • <7)
By rearranging, substituting equation (4), and following Miller's
(1976) assumptions about the fluid, equation (7) is changed to
D-5
-------
(8)
where
AP = effective driving pressure differential (psi),
Q = productivity (gpm), and
T = effective transmissivity (gal/day/ft).
The term Q/AP in equation (8) is essentially the productivity index
of the oil well (Gatlin, 1960, p. 246) and is comparable to the specific
capacity of water wells (yield per unit drawdown). Estimation of trans-
missivity from this value incurs limitations equivalent to those for the
water well case (see previous section).
The effective transmissivity (T) determined using equation (8)
is an underestimate of the formation transmissivity because it incor-
porates the reduced transmissivity of the damage zone near the well.
Formation damage results from both interaction of formation clay with
drilling fluid and invasion of drilling mud solids into the formation.
The Damage Ratio (D.R.) expresses the relationships between true and
effective transmissivity:
Damage ratios of clay-poor formations such as clean sandstones and
fractured carbonates are typically low, ranging from 2 to 3 according to
John Evers, Associate Professor of Petroleum Engineering, University of
Wyoming (personal communication, February, 1981), while damage ratios of
clay-rich formations can exceed 30. Thus the effective transmissivity
estimates true aquifer properties fairly closely for some formations but
may be more than one order of magnitude too low for clay-rich formations.
T = D.R.(T)
(9)
D-6
-------
Methodology and Limitations in Interpretation
Both Bredehoeft (1965) and Miller (1976) discuss the limitations
of the drill stem test. By simplyifing the analysis to the steady-
state the method described above introduces additional error if steady-
state flow was not obtained. Uncertainty is also introduced by the
necessity of estimating average productivity and driving pressure from
drill stem test synopses, often the only data available.
The average productivity rate is determined by dividing total
volume of fluid recovered by total flow duration. Typically fluid
recovery data are reported as feet of drill pipe filled, but drill pipe
diameter is not reported. Evers (personal communication) suggests
assuming kh inch drill pipe (about 0.6 gal/ft) for "shallow" wells
(<15,000 ft total depth) and 5h inch drill pipe (about 0.9 gal/ft) for
"deep" wells (>15,000 ft). If smaller drill pipe were actually used the
flow rate and transmissivity would be overestimated, by a maximum one
order of magnitude for the smallest (1.9 inch) pipe. Conversely, if
larger drill pipe were used, the maximum underestimate would be by a
factor of 3 (with 8-5/8 inch pipe) .
Average driving pressure can be estimated as
tpp + FFP
AP = FSIP - , (10)
where FSIP = final shut-in pressure,
IFP = initial flow pressure, and
FFP = final flow pressure.
Due to short shut-in durations the final shut-in pressure may not be
identical to undisturbed formation pressure, resulting in underestimation
of the average driving pressure and overestimation of transmissivity.
D-7
-------
Reported flow pressures and recovery often do not agree. ' In many
instances the discrepency can be attributed to an unreported "water
cushion" within the drill pipe, used to reduce pressure differentials
between the drill pipe and both the hole and formation. As a result
the reported recovery, calculated flow rate, and transmissivity are too
high. For wells with large reported recoveries, verifiable by flow
pressures, the error due to unreported water cushions is estimated as
less than a one-half order of magnitude.
Madison Group (carbonate) transmissivities determined using
equations (8) and (10), and reported flow rates were within one-half
order of magnitude of transmissivities determined by Miller (1976),
using equation (5), for 80 percent of the 16 tested data sets. The
remaining 3 data sets underestimated transmissivity by one order of
magnitude when steady state equations were used, as did a data set for
the Tensleep Sandstone (from Bredehoeft, 1965). This demonstrates
steady-state techniques will provide adequate estimates of transmissivity
in the absence of better data.
'It should be noted that transmissivities estimated using equations
(5) or (8) are for water at formation temperatures and pressures,
thus incorporating the decrease of viscosity associated with temperature
increases.
Drill stem tests often are conducted only on selected, thin, porous
and permeable intervals within a formation. Derived estimates of
hydraulic conductivity thus represent a maximum for the formation but
transmissivities underestimate total formation transmissivity due to the
thickness differences.
D-8
-------
Potentiometric Surface Elevation from Drill Stem Tests
The elevation of the potentiometric surface is determined from the
following equation, modified from Miller (1976):
h = (Po x C) - PRD + RP, (11)
where h = potentiometric elevation (feet above msl),
Po = undisturbed formation pressure (psi) ,
C = conversion factor from psi to feet of water,
PRD = pressure recorder depth (ft below reference point), and
RP = altitude of reference point (feet above msl).
The reference point utilized for most drill stem test data is the Kelly
bushing.
If complete drill stem test data are available the undisturbed
formation pressure can be determined by extrapolating pressure buildup
during shut-in periods (see p. C-4), and the pressure recorder depth is
also known.
If only drill stem test synopses are available the pressure
recorder depth is unknown and reported shut-in pressure must be utilized
as an estimate of undisturbed formation pressure. Initial shut-in
pressures are often higher than undisturbed formation pressure due to
"supercharging" (Murphy, 1965), which is formation overpressurization
due to high drilling mud pressures. The reported final shut-in pressure
may be less than undisturbed formation pressure due to incomplete
recovery following the flow period. For this report the final shut-in
pressure was used as an estimate of undisturbed formation pressure,
resulting in possible underestimate of potentiometric elevation. The
pressure recorder was presumed to be located at the top of the tested
interval, following a suggestion by Evers (personal communication).
D-9
-------
The conversion factor used in this report is 2.3067 feet of water
3
per psi. It assumes water with a density of 1.0 gm/cm (i.e., if pure,
a temperature of 39.2°F or 4°C). Miller (1976) discusses temperature
and dissolved solids corrections which may be made if data are avail-
able. Higher temperatures increase the conversion factor by up to five
percent, because the density of water is less at elevated temperatures.
Dissolved solids increase the density of water, resulting in a decrease
in the conversion factor of up to ten percent for water with
mg/1 TDS.
D-10
-------
APPENDIX E
CHEMICAL ANALYSIS OF GROUND WATERS
SAMPLED BY WRRI IN THE
GREAT DIVIDE AND
WASHAKIE BASINS
-------
APPENDIX E
CHEMICAL ANALYSES OF WATER SAMPLES COLLECTED BY WRRI STAFF,
GREAT DIVIDE AND WASHAKIE BASINS, WYOMING
Location
Aquifer
Ca"*^ Mg"^
Na
.+
K
SO,
HCO,
CO,
CI
pH
As
Ba
Cd
15/89-33 cc
23/96-25 bba
15/99-12 be
12/90-11 ad
20/101-27 ca
13/87-15 da
21/87-9 bd
21/87-10 bb
North Park
Wasatch (?)
Laney
Mesaverde
Mesaverde
Frontier
Madison
Cambrian
54
3
42
97
46
74
17
1
19
32
726 542
126 17
18
35
8
463
103
48
293
47
78
375
2
3
1
6
25
2
4
24
9
0
174
108
4000
157
161
655
241
989
273
371
449
293
150
329
0
84
0
19
0
48
0
0
72
55
8
26
180
10
50
86
8.1 ND
8.6 ND
8.0 ND
8.3 ND
8.2 ND
8.6 ND
8.0 ND
8.1 ND
0.09
0.64
ND
ND
ND
0.10
ND
ND
ND
ND
ND
ND
0.01
ND
ND
ND
-------
APPENDIX E
(continued)
Location
Aquifer
Cr
F
Pb
Hg
no3-n
Se
Ag
U
Ra-226d
Gross
Alpha
Gross
Beta^
TDS
15/89-33 cc
North Park
ND
0.18
ND
ND
0.09
ND
ND
0.005
0.32+0.16
1+1
6+2
246
23/96-25 bba
Wasatch(?)
ND
5.2
ND
ND
ND
0.01
ND
0.002
1.33+0.3
0+4
5+6
1088
15/99-12 be
Laney
ND
0.15
ND
ND
0.14
ND
ND
0.004
0+0.1
3+1
4+2
496
12/90-11 ad
Mesaverde
ND
0.68
ND
ND
0.09
ND
ND
0.005
0.09+0.12
1+1
5+3
602
20/101-27 ca
Mesaverde
ND
0.54
0.16
ND
.1.97
0.01
0.02
0.034
0.38^.16
0+16
16+7
6378
13/87-15 da
Frontier
ND
0.16
0.07
ND
ND
ND
ND
0.005
0.23+0.16
0+1
4+3
534
21/87-9 bd
Madison
ND
0.34
ND
ND
0. 79
ND
ND
0.009
0.32+0.18
11+2
14+3
514
21/87-10 bb
Cambrian
ND
0.73
ND
ND
ND
0.01
ND
0.027
1.5+0.3
13+5
36+8
1522
All constituents in milligrams per liter, except as noted.
kpH given in standard units.
CND indicates not detected. Pertinent detection limits are: As, 0.01; Ba, 0.05; Cd, 0.01; Cr, 0.05;
Pb, 0.05; Hg, 0.001; N03-N, 0.01; Se, 0.01.
^Analyses of radioactive species in picocuries per liter.
-------
|