Volume V-A
OCCURRENCE AND CHARACTERISTICS OF GROUND
WATER IN THE GREEN RIVER BASIN AND
OVERTHRUST BELT, WYOMING
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Volume V-A
OCCURRENCE AND CHARACTERISTICS OF GROUND
WATER IN THE GREEN RIVER BASIN AND
OVERTHRUST BELT, WYOMING
by
John Ahern, Michael Collentine, Steve Cooke
Project Manager
Craig Eisen
Water Resources Research Institute
University of Wyoming
Report to
U.S. Environmental Protection Agency
Contract Number G-008269-79
Project Officer
Paul Osborne
July 1981
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INTRODUCTION
This report is one of a series on the hydrogeology and water
quality in the ten structural basins of Wyoming. The report summarizes
and interprets the available geologic, hydrologic, and water quality
data in the Green River basin-Overthrust belt. It includes a discussion
of ground-water movement, identification of aquifers with yields and
water quality suitable for drinking water supplies, and estimates of
current ground-water use by source aquifer and economic sector.
This study was funded by the U.S. Environmental Protection Agency
under Contract No. G-008269-79 to provide hydrologic and water quality
information for the Underground Injection Control Program (UIC). The
UIC program, authorized by the Safe Drinking Water Act (P.L. 93-523), is
designed to protect current and potential underground drinking water
sources from contamination by injection of brines, sewage, and other
waste materials. One of the Wyoming Water Resources Research
Institute's contributions to this program is the development of
background information included in this report and the other reports of
the series.
While much hydrologic and water quality information has been
gathered since the last basinwide report on the Green River basin-
Overthrust belt (Dana, 1962), data on yield and quality for most
aquifers are concentrated in the relatively few areas covered by
federally funded studies and oil and gas drilling. Thus, the importance
of this report is not only to define the current extent of knowledge on
hydrogeology and water quality in the Green River basin-Overthrust belt,
i
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but also to identify those areas where future research on water
development potential and water quality need to be conducted.
ii
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TABLE OF CONTENTS
Chapter Page
I. SUMMARY OF FINDINGS 1
II. GEOGRAPHIC AND GEOLOGIC SETTING 7
GEOGRAPHIC SETTING 8
Topography 10
Climate and Surface Drainage 10
Population 11
Land Ownership and Use 13
GEOLOGIC SETTING 13
Stratigraphy 13
Structure 22
Green River Basin 22
Overthrust Belt 26
Hydrostratigraphy 27
III. GROUND-WATER USE 31
MAJOR GROUND-WATER USERS 34
Agricultural Industry 34
Irrigation 34
Livestock 35
Underground Drinking Water Supplies 36
Private Domestic Use 36
Public Drinking Water Supplies 38
SURFACE WATER USE 41
IV. HYDROLOGIC PROPERTIES OF THE MAJOR WATER-BEARING
UNITS 43
METHODOLOGY 44
PRECAMBRIAN AQUIFER 45
FLATHEAD AQUIFER 45
iii
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Chapter Page
(IV) PALEOZOIC AQUIFER SYSTEM 51
Bighorn Dolomite 52
Darby Formation 53
Madison Limestone 53
Tensleep Sandstone 54
Phosphoria Formation 55
NUGGET AQUIFER SYSTEM 55
Thaynes Limestone 56
Ankareh Formation 56
Nugget Sandstone 57
Twin Creek Limestone 58
UPPER JURASSIC-LOWER CRETACEOUS AQUIFERS 58
Gannett Group 59
Bear River Formation 60
Aspen Shale 61
FRONTIER AQUIFER 61
MESAVERDE-ADAVILLE AQUIFER 62
TERTIARY AQUIFER SYSTEM 64
Lance Formation 65
Evanston Formation 65
Fort Union Formation 66
Wasatch Formation 66
Green River Formation 68
Bridger Formation 69
QUATERNARY AQUIFERS 70
V. GROUND-WATER CIRCULATION 73
OVERTHRUST BELT 74
Pre-Hilliard-Baxter Aquifers 75
Post-Hilliard-Baxter Cretaceous and
Tertiary Aquifers 77
Quaternary Aquifers 78
GREEN RIVER BASIN 78
Pre-Hilliard-Baxter Aquifers 82
Post-Hilliard-Baxter Aquifers 83
iv
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Chapter Page
(V) Mesaverde Aquifer 84
Tertiary Aquifer System 84
Quaternary Aquifers 87
VI. WATER QUALITY 89
GENERAL WATER QUALITY 90
Precambrian through Upper Cretaceous Units. . . 91
Tertiary Aquifer System 93
Quaternary Aquifers 96
PRIMARY STANDARDS 98
Fluoride 101
Nitrate 103
Other Constituents with Primary Standards . . . 104
SECONDARY STANDARDS 106
Total Dissolved Solids 107
Sulfate 109
PH Ill
Chloride
Iron 113
Other Constituents with Secondary Standards . . 114
VII. REFERENCES 117
APPENDIX A: SUMMARY OF HYDROLOGIC PROPERTIES
BY FORMATION A-1
APPENDIX B: HYDR0GE0L0GIC DATA BY WELL b-1
APPENDIX C: DETERMINATION OF AQUIFER PROPERTIES .... c-1
APPENDIX D: CHEMICAL ANALYSES OF GREEN RIVER
BASIN-OVERTHRUST BELT GROUND WATERS
SAMPLED BY WRRI D-l
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LIST OF FIGURES
Figure Page
II-l Green River basin-Overthrust belt study area 9
I
J
II-2 Population projections for the five major
counties within the Green River basin-Overthrust
belt 14
II-3 Population centers of the Green River basin-
Overthrust belt 16
II-4 (a) Diagrammatic stratigraphy, pre-Hilliard-
Baxter shales, Overthrust belt-Green River
basin 18
(b) Diagrammatic stratigraphy, post-Hilliard-
Baxter shales, Overthrust belt-Green River
basin 19
II-5 Tectonic sketch map of the Green River basin 23
II-6 (a) East-west structural section, Green River basin . . 24
(b) Representative structural section, Overthrust
belt 25
II-7 Hydrostratigraphic column, Green River basin-
Overthrust belt 29
III-l Ground-water withdrawals by user type 33
III-2 Consumptive use of drinking water summarized by
source and user type 37
V—1 Location map of pre-Quaternary springs, Green River
basin-Overthrust belt 76
V-2 Potentiometric surface map of the Tertiary Wasatch
aquifer, Green River basin-Overthrust belt. . 79
V-3 Potentiometric surface map of the Tertiary Laney
aquifer, Green River basin 80
V-4 Potentiometric surface map of the Tertiary Bridger
aquifer, Green River basin-Overthrust belt 81
V-5 Idealized diagram of ground-water flow within the
Tertiary aquifer system, Green River basin 85
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VI-1 Major ion composition of waters from the Precambrian
through Upper Cretaceous aquifers, Overthrust belt. . . 92
VI-2 Major ion composition of waters from the Wasatch
aquifer, Green River basin 95
VI-3 Major ion composition of waters from the Bridger,
Laney, and Wilkins Peak aquifers, Green River basin . . 97
VI-4 Nitrate and fluoride concentrations exceeding the
primary drinking water standards in the Tertiary
aquifer system 102
VI-5 Sulfate concentrations exceeding the secondary
drinking water standard in the Tertiary aquifer
system 110
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LIST OF TABLES
Table Page
II-l Surface drainage in the Green River basin-Overthrust
belt 12
II-2 Populations of the major counties and population
centers in the Green River basin-Overthrust belt. ... 15
III-l Number of public drinking water supplies in the
Green River basin-Overthrust belt by service
category 39
III-2 Municipal ground-water supplies in the Green River
basin-Overthrust belt 40
IV-1 Generalized stratigraphy, lithology, and water-bearing
characteristics of geologic formations in the Green
River basin-Overthrust belt 46
VI-1 Drinking water quality standards 99
viii
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LIST OF PLATES*
Plate
1. Structure contour map on top of the Lower Cretaceous
Dakota Formation, Green River basin and Overthrust belt,
Wyoming.
2. Wells permitted for domestic or municipal use, Green River
basin and Overthrust belt, Wyoming.
3. Potentiometric surface map of pre-Hilliard-Baxter formations,
Green River basin and Overthrust belt.
A. Total dissolved solids concentrations in the Precambrian
to Upper Cretaceous aquifers, Green River basin and Overthrust
belt, Wyoming.
5. Total dissolved solids concentrations in the Tertiary aquifer
system, Green River basin and Overthrust belt, Wyoming.
6. Total dissolved solids concentrations in Quaternary deposits,
Green River basin and Overthrust belt, Wyoming.
*Plates contained in Volume V-B.
ix
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I. SUMMARY OF FINDINGS
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I. SUMMARY OF FINDINGS
1. Nine major water-bearing zones, each consisting of one or more
aquifers, have been identified in the Green River basin-Overthrust belt:
(a) the Precambrian aquifer, (b) the Flathead aquifer, (c) the Paleozoic
aquifer system, (d) the Nugget aquifer system, (e) the Upper Jurassic-
Lower Cretaceous aquifers, (f) the Frontier aquifer, (g) the Mesaverde-
Adaville aquifers, (h) the Tertiary aquifer system, and (i) the
Quaternary aquifers. These aquifers and aquifer systems are separated
by either thick, areally extensive low-permeability zones (shales) or
stratigraphic unconformities. The most prominent regional
low-permeability zone is the Cretaceous Hilliard-Baxter aquitard, which
contains up to 5,000 feet of shale and siltstone.
2. The Green River basin and the Overthrust belt comprise two
largely different hydrogeologic regions because of their different
structural settings. In the Green River basin, which constitutes the
eastern two-thirds of the study area, the stratigraphic discontinuity of
pre-Hilliard-Baxter formations between recharge zones and the basin
produces highly restricted ground-water circulation. This poor
circulation results in flat potentiometric gradients, no well-defined
discharge zones, and poor water quality. In post-Hilliard-Baxter
formations, recharge is along flanks of the uplifts and ground-water
flow is directed toward the Green River. However, impermeable zones
within the Tertiary Green River Formation greatly restrict inter-
formational flow. Available potentiometric data do not delineate a
major discharge zone for these units.
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In the Overthrust belt, major fault zones and resultant
stratigraphic displacements have produced areas with highly disrupted
regional ground-water circulation. This results in enhanced local
ground-water circulation through high-discharge springs with good water
quality. The ground-water development potential is greater in the
Overthrust belt than in the Green River basin because of high fracture
permeability, greater recharge, and shallower drilling depths to the
more productive aquifers.
3. The Paleozoic and Nugget aquifer systems are the two major
bedrock water-bearing zones in the Overthrust belt. Aquifers of the
Paleozoic aquifer system are primarily carbonate and are most productive
where secondary permeability (solution openings and fractures) is well
developed. The Nugget aquifer system consists of a carbonate-
sandstone-carbonate sequence. Secondary permeability of this aquifer
system is well developed in some tectonically disturbed areas, as
evidenced by spring flows up to 2,000 gpm from the Nugget Sandstone.
4. The most important water-bearing zones within the Green River
basin are the Tertiary aquifer system and the Quaternary aquifers.
These units are heavily utilized and easily accessible due to shallow
depths. In some areas they are capable of producing sufficient
quantities of water for irrigation.
The major aquifers of the Tertiary system are comprised of fine- to
coarse-grained sandstones in the Wasatch Formation, particularly along
the basin flanks in the north and central basin; discontinuous sand
lenses in the Laney Member of the Green River Formation in the
Eden-Farson area; and fine-grained sandstones of the Bridger Formation,
most productive in the south-central basin. Transmissivity estimates
3
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for these aquifers generally range from 500 to 5,000 gpd/ft. Perme-
abilities are primarily intergranular. Well yields of 50 to 100 gpm are
common from aquifers of the Tertiary system.
5. The Quaternary aquifers consist of unconsolidated sand, gravel,
silt, and clay deposits present along the western flank of the Wind
River Mountains, in the valleys of the Green River and its major
tributaries, and in the down-faulted valleys of the Bear, Salt and Snake
rivers of the Overthrust belt. Transmissivity estimates vary from less
than 500 gpd/ft in fine-grained alluvial and terrace deposits along the
Green River drainage, to 370,000 gpd/ft in the alluvium of the Star
Valley, though most estimates generally range from 5,000 to 30,000
gpd/ft. Where thick, saturated sections of alluvium (up to 400 feet
thick in Bear River Valley) are penetrated, well yields may exceed 500
gpm; however, yields less than 100 gpm are more common.
6. Water quality in the Precambrian to Upper Cretaceous aquifers
is generally suitable for drinking water throughout the Overthrust belt,
and generally unsuitable for drinking water where sampled in the Green
River basin. The total dissolved solids concentrations are typically
less than 500 mg/1 in the northern Overthrust belt, but frequently
increase to 500-1,000 mg/1 in the southern Overthrust belt where
regional flow dominates. Violations of primary drinking water standards
are rare in the Overthrust belt. Total dissolved solids concentrations
frequently exceed 3,000 mg/1 (and even 10,000 mg/1) in the Green River
basin. Calcium and bicarbonate are the dominant ions in these waters
within the Overthrust belt, while dissolved sodium, sulfate, and
chloride dominate in most Precambrian to Upper Cretaceous aquifers in
the Green River basin.
4
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Water quality in the Tertiary aquifer system is generally unsuit-
able for drinking water in the Green River basin, except in the Wasatch
aquifer in the northern and far southern parts of the basin. Total
dissolved solids concentrations frequently fall in the 500 to 3,000 mg/1
range in most Tertiary aquifers in the central part of the basin, and
exceed 10,000 mg/1 in the Wilkins Peak aquifer of the Green River
Formation. Sulfate is typically above the secondary drinking water
standard in those areas where total dissolved solids also exceed the
standard, except in the Wilkins Peak aquifer. Fluoride concentrations
frequently exceed the primary drinking water standard, particularly in
the Laney aquifer of the Green River Formation, but also in the Wasatch
aquifer where it intertongues with the Laney aquifer.
Water quality in the Quaternary aquifers is generally suitable for
drinking water in the Overthrust belt and where sampled in the Green
River basin. The total dissolved solids concentrations are typically
less than 500 mg/1. Violations of primary drinking water standards are
rare.
7. Ground water supplies approximately 2.5 percent of the total
water consumed in the Green River basin-Overthrust belt. It is a more
important contributor to private domestic drinking water supplies, and
provides water to 19 municipalities in the study area. Fourteen of
these are in the Overthrust belt. The alluvium is the most frequently
used aquifer in the Overthrust belt, although municipal supplies are
also obtained from the Madison Limestone and Bighorn Dolomite of the
Paleozoic aquifer system, and the Thaynes Limestone and Twin Creek
Limestone of the Nugget aquifer system. The Wasatch Formation and the
alluvium are the principal ground-water sources of drinking water in the
5
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Green River basin, although one municipality near Rock Springs derives
its supplies from the Mesaverde aquifer.
6
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II. GEOGRAPHIC AND GEOLOGIC
SETTING
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II. GEOGRAPHIC AND GEOLOGIC
SETTING
The Green River basin-Overthrust belt occupies the sparsely
populated and semi-arid southwestern part of the state. The economic
importance of this region lies in its vast reserves of coal, oil and
gas, trona, and oil shale. All of the resources are currently being
exploited. Expanding mineral development and resultant population
growth will place an increasing stress on the area's water resources.
Surface-water supplies derived from the mountainous regions surrounding
the basin currently meet the majority of the area's water demand.
However, because Wyoming's use of this region's surface water is limited
by interstate compacts, growing water needs may result in greater
exploitation of ground-water sources.
GEOGRAPHIC SETTING
The Green River basin-Overthrust belt is defined by structural
boundaries on the east (the Rock Springs uplift and Wind River
Mountains), by the 11th Standard Parallel on the north, and by state
lines on the west and south (Figure II-l). The area encompasses roughly
18,600 square miles and includes all of Lincoln, Uinta, and Sublette
counties, the portion of Sweetwater County generally west of Rock
Springs, the portion of Teton County south of Jackson Lake, and a very
small portion of Fremont County west of the Continental Divide in the
Wind River Range. The maximum east-west extent is 120 miles; the
maximum north-south extent is 195 miles.
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Figure II-l. Green River Basin - Overthrust Belt study area.
9
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Topography
The Green River basin-Overthrust belt is a mixture of arid high
plains, mountain valleys, and high mountains. The structural basin is
flanked by mountains in Wyoming on the northeast and north and by
mountains in Idaho and Utah on the west and south. The eastern boundary
is defined by low-lying hills which mark a subsurface but not surface
water divide.
The east and central parts of the area comprise the Green River
basin. The region is characterized by high treeless plains, badlands,
mesas, bluffs, and deep canyons. Elevation in the central interior is
generally from 6,000 to 7,000 feet above sea level. To the northeast,
north and northwest are wooded, upland slopes flanked with grass-covered
mountain meadows, rising steeply to bounding high mountains. Elevations
in these mountains commonly exceed 10,000 feet, and reach a maximum of
13,785 feet above sea level at Gannett Peak on the Continental Divide in
the Wind River Mountains.
The Overthrust belt lies along the western edge of the state. The
topography changes to a series of north-south trending mountain ranges
and valleys, ranging in elevation from 7,500 to 10,500 feet. The
Overthrust belt occupies roughly one-fourth of the study area.
Climate and Surface Drainage
Climate in the area varies primarily with altitude. Most of the
central interior receives less than eight inches of precipitation per
year, while the surrounding mountains can expect up to 50 inches per
year. The mountains regions receive the greatest part of their
precipitation during the winter as snowfall, while the central interior
receives the greatest precipitation from convective spring and summer
10
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thunderstorms. The areawide mean monthly temperature is about 38.5°
with a range from 34.8°F at Big Piney to 42.5°F at Rock Springs. Daily
temperatures range from highs of about 95°F in summer to lows of -40°F
in winter.
Most streamflow from perennial streams within the basin is the
result of snowmelt in the high mountains. Ephemeral streams in the
central and southern parts of the basin flow principally in response to
thunderstorms and contribute an insignificant amount to the area's
overall streamflow in most years. Major streams within the area are
listed in Table II-l and are shown in Figure II-l. All streams listed
in the table are perennial except for Bitter Creek.
The surface water divides do not always conform to the structural
boundaries of the study area. Bitter Creek, a tributary of the Green
River, flows across the Rock Springs uplift, which forms the eastern
structural boundary of the study area. The headwaters of this ephemeral
creek are in the Great Divide-Washakie basins approximately 50 miles
east of the uplift. To the west, the Hams Fork, Muddy Creek, and
several other smaller tributaries of the Green River originate in the
Overthrust belt and flow into the Green River basin. These streams flow
north or south in the Overthrust belt and veer sharply eastward when
they enter the Green River basin.
Population
The population of the five counties which comprise almost all of
the Green River basin-Overthrust belt was about 43,000 in 1970, having
increased by 1,500 during the 1960's. The preliminary 1980 census shows
a population increase of 90 percent over the decade to 80,000. This
corresponds to a population density of 4.3 persons per square mile in
11
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Table II-l. Surface drainage in the Green River basin-Overthrust belt.
(Colorado River Basin)
Green River
Henrys Fork
Blacks Fork
Hams Fork
Muddy Creek
Smiths Creek
Bitter Creek
Big Sandy River
Pacific Creek
Little Sandy River
Fontenelle Creek
La Barge Creek
Piney Creek
New Fork River
Cottonwood Creek
(Columbia River Basin)
Snake River
Salt River
Grey1s River
Little Grey's River
Hoback River
Gros Ventre River
(Bear River Basin)
Bear River
Smiths Fork
Twin Creek
12
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the five-county area. Growth is expected to continue beyond the end of
the century (Wyoming Water Planning Program, 1970), mostly due to the
widespread and abundant mineral resources found in this region of the
state (Figure II-2).
One trend apparent in the area, as in much of Wyoming, is the
movement of the population from the rural areas into the towns and
cities. Currently, approximately 70 percent of the area's population
lives in incorporated areas. Populations for towns and counties in the
Green River basin-Overthrust belt are presented in Table II-2 and
population centers are located in Figure II-3. Rock Springs is the
basin's largest city with a population of 19,400. Other major cities or
towns in the study area are Green River, Evanston, Jackson, and
Kemmerer.
Land Ownership and Use
Over 70 percent of the land within the Green River basin-Overthrust
belt is under federal jurisdiction. The Bureau of Land Management has
control over most of the central interior, while the Forest Service
manages most of the higher mountain areas. About 25 percent of the land
area is privately owned and is concentrated along rivers, streams, and
railroads. State and local government ownership accounts for about 5
percent of the land area.
GEOLOGIC SETTING
Stratigraphy
Sedimentary rocks in the area range in age from Cambrian to Recent.
They overlie a Precambrian igneous-metamorphic basement, which is
exposed only in a very small part of the study area. The stratigraphic
13
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FIGURE II-2
Population Projections for the Five Major Counties
within the Green River Basin-Overthrust Belt
"U.S. Department of Commerce
Bureau of Census, 19 70 Census
of Population, Number of In-
habitants, Wyoming.
125 —
'U.S. Department of Commerce
Bureau of Census, 1980 Census
of Population and Housing Pre-
liminary Reports, Wyoming.
100 —
75 -(-
Wyoming Department of Admini-
stration and Fiscal Control,
Division of Research and
Statistics, Wyoming Population
and Employment Forecast.Report,
June 1980.
25 --
1960
1970
1980
(preliminary)'
1990
(proj ected)
YEAR
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Table II-2. Populations of the major counties and population centers
in the Green River basin-Overthrust belt.
County
1970a
1980b
Lincoln
8,640
12,177
Sublette
3,755
4,545
Sweetwater
18,391
41,662
Teton
4,823
9,354
Uinta
7,100
13,021
TOTAL
42,709
80,759
Af ton
1,290
1,473
Big Piney
570
530
Cokeville
440
513
Diamondville
485
1,008
Evanston
4,462
6,420
Granger
137
176
Green River
4,196
12,785
Jackson
2,101
4,504
Kemmerer
2,292
3,271
Lyman
643
2,293
Marbleton
223
539
Pinedale
948
1,061
Rock Springs
11,657
19,411
Thayne
195
253
TOTAL
29,639
54,237
U.S. Department of Commerce Bureau of Census, 1970 Census of Population,
Number of Inhabitants, Wyoming.
^U.S. Department of Commerce Bureau of Census, 1980 Census of Population
and Housing Preliminary Reports, Wyoming.
15
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Figure II-3. Population centers of the Green River basin -
Overthrust belt.
16
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column is shown in Figures II-4a and II-4b and described in Table IV-1
(Chapter IV). In general, correlation of the various rock units
increases in complexity with decreasing age, due to complex
intertonguing of most Cretaceous and Tertiary sediments. Stratigraphic
nomenclature used in this report generally follows that by Lines and
Glass (1975), with a few modifications as indicated. For additional
stratigraphic information the reader is referred to Welder (1968),
Welder and McGreevy (1966), and Love and Christiansen (1980) .
Precambrian basement rocks underlie all of the study area. These
rocks include granite-gneiss and lesser amounts of schist, granite, and
pegmatite.
Paleozoic rocks consist mainly of calcareous miogeosynclinal
sediments, aggregating a maximum of 9,800 feet and averaging 5,000 feet
in thickness. The calcareous formations are composed of both
crystalline limestone and dolomite. With the exception of the Missis-
sippian Madison Limestone these formations generally lack solution
zones. Thus, in absence of fractures, they have relatively poor
permeability. Quartzite, sandstone, and conglomerates, as well as
mudstone, siltstone, and shale, occur as interbedded zones or formations
within the Paleozoic.
Mesozoic sediments are essentially clastic, deposited in
shelf-continental environments. The Triassic through pre-Mesaverde
Cretaceous formations are predominantly shale, mudstone, and siltstone,
although significant limestone, dolomite, and sandstone also occur.
They have a maximum thickness of 29,000 feet, with a combined average of
12,000 feet.
17
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Overthrust Belt
Lithotomy
ThiUntw Gttoqlc Formation
(It) Symbol
HYDROCARBON
OCCURRENCE
¦ Qoi production
a oil production
• oil or got production
<>«•! ICIH
• •ooo
'-j'n'q '-t lT'-
3000-6WXX?)Kh Hdliord Shol*
(Kbb Ghnd Bull Formation in
E 0»»rihfu»t Sail)
1100-3000 Kf Frontier Formation
400-2200 Ko Aip«n Shot*
000-1500 Kfcr Boar Riw Fofmotion
Kmd Muddy Sandtton*
Ki TtwmopflIU Utnftti
M "Ookote' Mtmfitf
800-5000(?Xg Gonaott Group
Kio Lokoio Congtomoroto
90-120 .Jt Slumo Sandtton*
160-340 Jp Pr«w»» Rtdb«di
000-3800 jtc Tam Cr«*h Umaiton*
750—1300 Jn Nugget 9and*tgn<
200-600 "V« AM«r«h Formation
1100-2600 Ht Thayn«» Limation*
350-600 Wo«d«id« Formation
230-700 T»d Om*oody Fo««ouoft
--- ^ Phoiphono Formonon (N)
200-400 Pp Pork Clr» FofmotKw (S)
450-1600 Wtlli Fo'molio
400-700 PMa Ajfliatfi formohon
600-2000 Mm MoOnon Lim«»lor>«
(PUb Brortf limttlont 0«
Uppti M*mfe»r tocotly)
«0Q- 1000 MC*4 Oo»fcy Formotton
400-1000 Ob BtgHotn Ooiomn*
(Ol) ( l«igh Oolomit* M«mb«r)
125-1000 €g Gollal»n UmMlon*
500-2300 *6 Sartdlton*
Anfconh Formation Ho
Tboyntt L'mMtoit* "St
Woodtitf* formation "fcw
Oimoody Formolion Id
Photphorlo Forwiotlon (NBW) p.
Phaapnona or Pofk City (SAW) **
Ansa** Formation (Nawl PMa
(Osrwln Sandtlorv* (PUd«
Momftor ot Mm)
ModitoK L*mMtDn« Mm
Oarby Formottoa U04
Bighorn DoJemii* Ob
(t_«igh Oolomit* M«mb«<) (01)
Gollotm LlrwjUjo# €g
Gift* Formotlon €qv
Flothoad Sonditon* €t
Pfocombrion pCt
130-500
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J I
J:. i 1.
Thickness Geologic Formation
(ft) Sy mbol
50-410 Qal Quaternary Alluvium
(includes floodpla'in, alluvial, terrace, and glacial deposits
ond londstide, slopewosh ond talus tnatenot)
0-1000 Tsi Sail take Formation
500-2600 Tt Fowkes Formolion
(includes Sillem, Bulldog Hollow, and Gooseberry members)
400-470 Tgr Green River Formotion
(includes Fossil Butte ond Angelo members)
2,500-3600 Tw Wosatch Formation
(includes basa conglomerate, lower member, main body
Wosotch Formotion, sandstone ond mudstone tongues,
Bullpen Member, and Tunp Member , oKo includes
Knight Member of Eocene cge)
1350-2900 TKe Evonston Formotion
(includes Hams Fork Conglomerate Member and tower
member of Evanston Formotion also includes Almy
Formation of Poleocene age)
1400-5000 Kov Adaville Formation
(includes Lazeort Sandstone Member)
3000-6800 Kh Milliard Shale
Figure II-4b. Diagrammatic stratigraphy, post-Hilliard-Baxter
shales, Overthrust belt.
19
-------
Western
„lo Green River Basil
D o u
£ S*
v u- £SS Lithoioat
-?-
o O c o a o o a 4
a a o e # o o e
o o 0 O O O 0 o c
e © o o o o 0 o o
o o o o o o a o o
o 0 O O O 0 O OO
CO o 0 O O o o 0
OOOOOOOOO
OOOaOoo©
o© 0 0 O O d O O
a a Oooooo
_o_o 0 o o o O O O
i T 4~ a~ a- «¦ u •« •
e o o o o o
OOOO O o O O o
P Q p ¦ OOqQOQ
TMckmn Gtolpgte Fof/nolion
(M Symbol
0-200 Qol Quaternary AHunum
(inefcd«i fioodptom, olluviol, tar roe*, oa4 glacial dtponti I
2££Q-320Q Tee Comp Go*n Foimotlon
( mctudti T»»»moi Fortnonon of fiorlft««»l Wyoming )
4200 Tbp 0/c«frt Part formation
200 Tbi Bttiiop Co»gi9i«*fan
1700-2300 TP ftridgar FormOKon
32S-6O0 Tgc G'Mri R>*«r Formation
(inctwdti lo««r Fonwn«ll« Tonguo, miMIt longtit, one
upper uwigui)
<100-3230 !¦ Waiotch Formatton
(mclyd«» Choppe Mi*, Lo8org« WtmCir, N««Fofk
Tongue, upp•/ Ioaqm, and congto««rof* mtint«r , clip
includt* Poi» Paok Conglotnarola in ngrihwaii)
8000-16,000Th Hobock Formalin (Noririvtti) (lad)
0-2300 rtg Fori Unron Formoiion (SoulH««»il (right)
Km» M««o»ardt Fornotun
Eastern
,.1": Green River Basin
° £3
J u; *q« LlthoiooT
*553"
0 E O o o «
-<=sCS>_-:
:--<^sr=; - °1
i'ro'jj'o '¦>' o o'Att'J _
TMctwu G*o*oqic Formation
(H) Symbol
0-100 Qcl OuoUiaqt? Ailuviuw ttooqptan,
aHuvtal.1Itrrsct, onfl ctacifll dapoMti'
0-200 Tip South Poll Fwmolion
? Tbe Browni Pork Formoiion
0-200 Tb> Bishop Canglomtrata
300-2500 Tb 8(tdq«( Formation
IOO-2BOO Tgr Gr**n R««000 SOO Q i OOP 2O00H
Figure II-4b (continued). Diagrammatic stratigraphy, post-Hilliard Baxter shales,
Green River basin.
20
-------
Formations of Upper Cretaceous (post-Hilliard-Baxter) and Paleocene
age generally consist of sandstone, siltstone, and shale with
interbedded coal and conglomerate units. The combined maximum thickness
of these sediments ranges from 7,900 feet in the Overthrust belt to more
than 16,000 feet in the Hoback basin (Figure IJ.-4b).
Late Paleocene and Eocene deposits in the Green River basin are
comprised of complex intertonguing fluvial and lacustrine sediments
within the Wasatch, Green River, and Bridger formations. This inter-
tonguing was caused by areal expansions and contractions of ancient Lake
Gosiute and regional tectonic activity around the basin periphery
(Surdam and Stanley, 1976). The predominant lithologies of the Wasatch
Formation are mudstone and sandstone while laminated marlstone and oil
shale comprise much of the Green River Formation. The Bridger Formation
and its equivalent in the Overthrust belt, the Fowkes Formation, are
dominated by tuffaceous mudstones and sandstones. The aggregate
thickness of these sediments is more than 12,000 feet in the
south-central Green River basin, but probably averages between 5,000 and
8,000 feet over most of the study area.
Sediments of Miocene and Pliocene age are primarily conglomerate,
claystone, and sandstone. The maximum thickness of Miocene-Pliocene
rocks ranges from about 4,000 feet in the southeast to more than 6,000
feet in the Jackson Hole area where the Camp Davis Formation has a
thickness of up to 5,200 feet.
Quaternary sediments generally consist of unconsolidated silt,
sand, clay, and gravel, rarely exceeding 100 feet thick in the Green
River basin, but up to 410 feet thick in the down-faulted valleys of the
Overthrust belt. Quaternary deposits include flood plain, alluvial
21
-------
terrace, and glacial deposits, as well as minor talus, slope-wash, and
landslide material.
Structure
The Green River basin-Overthrust belt can be divided into two major
and two minor structural and physiographic provinces. These are shown,
along with major internal structures, in Figure II-5. Structural
cross-sections of the Green River basin and Overthrust belt, located on
Figure II-5, are shown in Figures II-6a and II-6b. Plate 1 is a
structural contour map of the top of the Dakota Sandstone, which depicts
the regional structural setting of the area.
Green River Basin
The Green River basin is a north-south elongated intermontane
basin, formed during the Laramide Orogeny, with deposition of at least
8,000 feet and possibly 10,000 feet of Tertiary sediments (Keller and
Thomaidis, 1971). Tectonic activity has resulted in at least 27,000
feet of structural relief on the Precambrian basement (Keller and
Thomaidis, 1971).
At its northern end, the basin has been depressed and overridden by
thrusting, which has brought Paleozoic and Mesozoic strata from the west
and Precambrian rocks from the northeast over late Cretaceous and early
Tertiary sediments. Further to the south, the basin rises gradually to
the Rock Springs uplift on the east and the Overthrust belt on the west,
where it is again overthrust by pre-Cenozoic rocks (Krueger, 1960).
Along the eastern part of the Overthrust belt, the pre-Cenozoic
sediments are folded into a north-trending, long, broad, relatively low
anticline of 2,000 feet structural relief, the Moxa arch, which is the
22
-------
SNAKE RIVER
VALLEY
(JACKSON HOLE)
STAR VALLEY
BEAR RIVER
VALLEY
LEGEND
THRUST FAULT SHOWING
— UPPER PLATE
NORMAL OR REVERSE fault,
SHOWINC RELATIVE DISPLACEMENT
FOLD AXIS
BASEMENT
A' CROSS SECTION
geographic sub-areas
TOWNS
A
AF70N
BP
BIG PINEY
E
EVANSTON
F
FARSON
GR
GREEN RIVER
J
JACKSON
K
kemmerer
LB
la barge
P
pinedalE
RS
ROCK SPRINGS
APPROXIMATE SCALE
12 6 O 6 12 18 MILES
Figure II-5. Tectonic sketch map of the Green River Basin
(modified from Krueger, 1960, Fig. 3, and Lines
and Glass, 1975, map sheet 2).
-------
A
A'
-ASPEN
-BEAR RIVER
rBECKWiTH
-TWIN CREEK
PALtOZOlC
SEOIMENTS-.(?)
— to.ooo
ts>
->
PALE0Z0IC6
ROCK SPRINGS UPLIFT-
B'
IO.OOO 1
C'
-MOXA ARCH
ROCK SPRINGS UPLIFT^
— - a,000
- -«o,ooo
Figure II-6a. East-west structural section, Green River basin (after Krueger, 1960, Fig. 3).
-------
D
WESTERN HALF OF SECTION
EASTERN HALF OF SECTION
O I I S 4 UILCS
Figure II-6b. Representative structural section, Overthrust belt.
-------
locus of numerous gas fields (Vietti, 1974). At its southern end in
Utah and Colorado, the basin abuts the Uinta uplift (Keller and
Thomaidis, 1971).
The Hoback basin is a sub-basin of the Green River basin, located
at its northern end. It represents a physiographic continuation of the
Green River basin, although its surficial drainage is to the north.
This relatively small area has been overridden on the southwest and the
northeast by thrusting from the Overthrust belt and the Gros Ventre
Range, respectively. The Hoback basin contains at least 15,000, and
possibly 30,000, feet of Lower Tertiary clastic sediments (Wiese, 1955;
Keller and Thomaidis, 1971).
Overthrust Belt
The Overthrust belt is a major structural feature which extends
from British Columbia southeast to the Uinta Mountains of Utah. The
thrust region within the study area is an arcuate belt of strike valleys
and ridges, approximately 60 x 25 miles, with as much as 3,000 feet of
topographic relief per mile. In general, Paleozoic and Mesozoic rocks
have been thrust eastward by a series of low-angle, westward-dipping,
imbricated thrust faults, with stratigraphic displacements on the order
of 20,000 to 40,000 feet each. Data indicate 15 to 45 miles of lateral
movement on the five major and numerous imbricate second-order thrusts.
Within each thrust plate, especially in the northern thrust belt, the
sediments have been folded intensely, and in some cases overturned (see
cross section D-D1, Figure II-6b). However, there are no major breccia
or gouge zones, and the rocks are not metamorphosed. Rocks above and
below thrust-fault surfaces generally remain in the same stratigraphic
position for many miles along outcrop, suggesting that the fault
26
-------
surfaces are essentially parallel to bedding for some distance downdip
under cover (Suydam, 1963; Lines and Glass, 1975).
Most of the subparallel mountain ranges are bounded on the east by
thrust faults, and on the west by younger high-angle normal or reverse
faults that are downdropped on the west. These younger high-angle
faults dip from 70° to 90°, have up to 5,000 feet of stratigraphic
displacement, and delineate many of the mountains and valleys of the
thrust belt. Transverse faults also occur locally (Lines and Glass,
1975).
Hydrostratigraphy
The water-bearing potential of the various rock units has been
determined from a number of sources. Spring flow is indicative of
saturated and permeable zones within the sedimentary rocks of the study
area. Records of water well tests and completion intervals provide
quantitative data on thicknesses of producing intervals, well specific
capacity, and aquifer transmissivity. Petroleum test data can provide
similar information. The lithology and special features of the rock
units, such as fracturing, solution zones, jointing, and the nature of
bedding, provide qualitative data on water-bearing capabilities.
The hydrologic divisions assigned to the rock units within the
study area have been identified solely by the relative water-bearing
properties. Except for a few cases, there is not sufficient information
to adequately determine interformational flow.
The term "aquifer system" is used in this report to identify a
group of geologic units with (1) relatively similar hydrologic
properties, and (2) an absence of extensive regional zones of low
27
-------
vertical permeability that will greatly restrict vertical hydraulic
communication within the system.
The term "aquifer" identifies a distinct hydrologic unit that has
regional extent and favorable water-bearing potential for exploitation.
Such units are either positioned within aquifer systems or
hydrologically isolated by very low-permeability confining beds
(aquitards).
"Minor aquifers" are stratigraphically isolated and regionally
discontinuous water-bearing zones that are capable of yielding only
small quantities of water to wells.
Nine aquifer systems and aquifers have been identified in the study
area. These are shown in Figure II-7. These aquifers and aquifer
systems are separated by a number of thick regional confining layers, or
aquitards (Figure II-7). Although they are often capable of
transmitting small amounts of water to wells and over large areas can
provide significant interformational flow, the aquitards serve
principally to hydraulically isolate the more highly permeable zones.
28
-------
W E
Geologic Age
Litho logy
Format ion
Hydrologic Role
Hydrologic Unit
Quaternary
O ' . ' o .
¦ o •
Alluvial, terrace, and
qlacial deposits
Major
Aquifer
Quaternary
Aquifers
• o ¦ o . ¦ 0 ¦¦ o
p.o ¦ o ' o
Browns Pork, South Pan,
Comp Ocxii, Salt Laht, ar»(J
Teeainot tor mat Ions, and
Bishop Conglomerate
Major
Aquifer
Tertiary
Aquifer
System
o '¦ ¦ o o ¦ ¦ o ¦ o ¦
Fowkes and Bridger
formations
Major
Aquifer
— — •
Green R iver
Formation
Confining Unit
with Discontinuous
Aquifers
Tertiary
ZErZ-iIHI.—:'
o " o , • O o .
Wasatch
Formation
Major
Aquifer
o.
. o ¦ • • •
. o
Fort Union and
Hoback formations
Minor
Aquifer
—: — '— i— — —a
Evanston ^
Formation^-^Lance
Formation
Minor
Aquifer
Upper
Cretaceous
Lewis
^\Shale
Mesaverde —
and Adavilie
formations
Aquitord
Major N.
Aquifer
Mesaverde -
Adaville
Aquifer
——————————
Baxter and
Hilliard Shales
Major
Aquitard
—
Frontier
Formation
Minor
Aquifer
Frontier
Aquifer
Lower
Cretaceous
— —
Aspen Shale
Discontinuous Aqui-
fers with local con-
fining beds
Upper Jurassic-
Lower Cretaceous
Aquifers
Bear River
Formation
• o • "o " • o • o • ' o
Gannett Group
Jurassic
. —± T_. . I mi- ,,, , -J
Stump-Preuss Fms.
Aquitard
1 1—1 —J—1—1 —(—1 1 1
Twin Creek Limestone
Minor
Aquifer
Nugget
Aquifer
System
I 1 1 1—1 -1—1 1 1
1 1 1 II 1 1 II 1
Nugget Sandstone
Major
Aquifer
Triasslc
/_!• I * J * ' ; ' ;
Ankoreh Formation
Minor Aquifer
1 T ! I I 1 I 1
Thaynes Limestone
Major Aquifer
l l l l l l l l l
Woodside Formation
Aquitord
— — -
Dinwoody Formation
Permian
-r1 1 ! 1 - 1 - 1 ¦ 1 I ~ L •
Phosphoria Formation
Minor Aquifer-
Paleozoic
Aquifer
System
Pennsylvanian
Tensleep Sandstone
Major Aquifer
Amsden Formation
Minor Aquifer-
Locally Confining
Mississippian
_ . _ . — . — . —_ . — —
III 1111(1
Madison Limestone
Major
Aquifer
1 1 ! 1 1 1 [ 1
1; ,1 , 1, J
Devonian
) i n'vi,
Darby Formation
Cambrian
r./.r.t-r//[ 'rL\ l-J-L, I.J.L,
Gallatin Limestone
Minor Aquifer
. • ; - • • — • ¦ • — • •
Gros Ventre Formation
Aquitard
• ' o • • • o : -.a..-
Flathead Sandstone
Minor Aquifer
/lathead Aquifer
Precambrian
^ \ 1 / / —
Procambrion rocks
Minor Aqulfsr
Precombrian Aquifer
Figure II-7. Hydrostratigraphic column, Green River basin and Overthrust
belt.
29
-------
III. GROUND-WATER USE
-------
III. GROUND-WATER USE
Ground-water use within the Green River basin-Over thrust belt is
difficult to quantify due to the lack of current consumption data for
all economic sectors. The numbers presented in this section are the
best estimates of water use, based on numerous assumptions, and are
useful in showing the relative demands on ground water by each user
type. Estimates are given for total quantities of ground water with-
drawn and for consumptive use, which is the fraction of ground water not
returned underground or to streams.
Ground-water withdrawals in the study area currently total about
18,800 acre-feet per year, whereas ground-water consumption is approxi-
mately 10,800 acre-feet per year. Ground-water consumptive use is 2.5
percent of the area's estimated annual water consumptive use of 441,400
acre-feet per year.
The Quaternary and Tertiary aquifers supply the majority of the
ground water consumed within the area, although other water-bearing
strata are exploited locally. Major ground-water users include
agriculture, the petroleum industry, municipalities and private .
residences, and, to a lesser extent, the coal industry and wildlife.
Ground-water withdrawals by user type are summarized in Figure III-l.
Agricultural activities withdraw approximately 8,500 acre-feet of ground
water annually, comprising about 55 percent of the total ground-water
withdrawals. An estimated 82 percent of the agricultural ground-water
withdrawal is for irrigation, with the remainder for stock watering.
32
-------
Figure III-l. Ground-water withdrawals by user type.
33
-------
Drinking water supplies withdrawn from underground sources are
roughly 7,150 acre-feet per year, or 42 percent of the total annual
ground-water withdrawal. Nineteen municipal water systems, AO non-
municipal community water systems, and virtually all private water
supplies utilize ground water.
Ground water produced through oil and gas production averages about
1,570 acre-feet per year. An estimated 94 percent, or 1,470 acre-feet,
is returned underground for secondary oil recovery, while an estimated 6
percent or about 100 acre-feet is either discharged to surface waters or
evaporated.
The coal industry utilizes about 430 acre-feet per year of ground
water. These waters are used principally for coal-dust control.
Wildlife consumes approximately 100 acre-feet of ground water
annually. Wild horses, which drink mostly from flowing springs in the
arid high plains, are the largest wildlife user group (Jim Dunder,
personal communication, Rock Springs District Office, Bureau of Land
Management, 1980).
MAJOR GROUND-WATER USERS
Agricultural Industry
Agriculture is the largest ground-water user in the Green River
basin-Overthrust belt. Ground water is used principally for cropland
irrigation, and secondarily for stock watering.
Irrigation
The study area contains approximately 5,700 acres of land irrigable
by ground water (U.S. Soil Conservation Service, personal communication,
December, 1980). An estimated 4,675 acres were actually irrigated with
34
-------
ground water in 1980 (Wyoming State Engineer, personal communication,
December, 1980). The highest concentration of these irrigated lands,
about 75 percent, are in the Star Valley along the western border of
Wyoming. Other concentrated areas of ground-water irrigation occur in
the Bridger Valley and the Eden-Farson area.
A net consumptive use of 1.25 acre-feet per acre is the areawide
estimate for irrigated crops (Trelease and others, 1970). Based on this
assumption, consumptive use of ground water for the 4,675 acres
irrigated in 1980 is 5,850 acre-feet. Sprinkler irrigation, which is
the primary irrigation system using ground water, is assumed to have an
efficiency of 75 percent. Based on this assumption, and assuming that
all irrigation projects using ground water use sprinkler systems, total
ground-water withdrawal is an estimated 7,800 acre-feet per year. The
primary aquifer developed for irrigation is the Quaternary alluvium,
although other shallow aquifers, such as Tertiary-age Wasatch in the
Eden-Farson area, are used where possible.
The amount of irrigable land in the Green River basin-Overthrust
belt is roughly 20 percent higher than that presently irrigated, and
projections by the Wyoming Water Planning Program are that much of this
land will be put into production in the future. It is expected that
most other increases in irrigated land will be due to surface-water
development, with ground water playing a less critical role (Wyoming
Water Planning Program, 1970).
Livestock
Ground-water consumptive use for stock watering is estimated at
1,665 acre-feet per year. Based on cattle and sheep populations
reported for 1979 (Wyoming Crop and Livestock Reporting Service, 1979)
35
-------
and an average daily water consumption of 15 gallons for cattle and 3
gallons for sheep (Wyoming Water Planning Program, 1972), a total of
3,330 acre-feet per year is required. Approximately half of this
requirement is supplied by ground water (U.S. Soil Conservation Service,
personal communication, 1980). Most of the stock-watering ground-water
supplies are produced from the Quaternary alluvial aquifers, although
other aquifers such as the Wasatch are used heavily near Pinedale and
Big Piney.
Underground Drinking Water Supplies
Although most people in the study area obtain their drinking water
supplies from surface waters, ground water is an important contributor,
particularly to rural water users. Consumptive use of drinking water is
summarized by source and user type in Figure III-2. More detail on each
ground-water user type is provided below.
Private Domestic Use
Of the total 1980 population of the Green River basin-Overthrust
area, about 10 percent, or 8,100 persons, are not living within
communities. These people are served almost entirely by ground water
from private wells. Assuming a consumption of 180 gallons per capita
per day, private domestic use is estimated at roughly 1,640 acre-feet
per year. The majority of the domestic wells are in Sublette County and
are producing from the Wasatch aquifer (Tertiary aquifer system), but
Quaternary aquifers are exploited heavily in areas adjacent to the major
surface drainages.
Records of the Wyoming State Engineer indicate that there were
about 880 permitted domestic wells completed in the study area through
36
-------
Community / Municipal
57.2
Community/ Non-Municipal
0.7
0^ -b
A
G° -b.
Private
Oomest»c
9.6
Community/Municipal
25.5
Figure III-2. Consumptive use of drinking water summarized
and user type.
37
-------
1979. The number of wells completed in each aquifer system reflect both
settlement patterns and areal extent of the various aquifers within the
area (Plate 2). Fifty-two percent of the domestic wells are completed
in the Tertiary aquifer system. The next largest group of wells (44
percent) are completed in Quaternary aquifers. The remaining wells (4
percent) are completed in Precambrian to Upper Cretaceous formations and
are concentrated in the Overthrust belt.
Public Drinking Water Supplies
Public drinking water supplies within the area have been divided
into community and non-community supplies. Community supplies include
19 municipal systems that serve incorporated areas and 40 non-municipal
supplies that support individual subdivisions or mobile home courts.
There are 114 non-community public water supplies (motels, service
stations, restaurants, dude ranches, campgrounds, etc.) served by ground
water within the area. Table III-l lists the types and numbers of
public water supplies in the Green River basin-Overthrust belt.
Municipal Systems. Municipal use is the largest component of
drinking water use of ground water. Municipal withdrawal of ground
water exceeded 4,300 acre-feet per year in 1977 (U.S. Environmental
Protection Agency, 1978), and had increased to more than 6,800 acre-feet
per year in 1980.
Eighteen municipalities are served entirely by ground water, while
Evanston utilizes mainly surface water, augmenting its supply with
ground water during the summer irrigation season. The municipal systems
are listed in Table III-2. Most are publicly owned; several in Lincoln
County are owned by private pipeline companies. Approximately 63,000
people were served by municipal water systems in 1977, about 15,000
38
-------
Table III-l. Number of public drinking water supplies in the Green
River basin-Overthrust belt by service category (serviced
by ground water).
Community 59
Q
Municipal 19
Non-municipal 40
Residence'3 21
Mobile Homes 19
c
Non-Community 114
Motel 27
Restaurant 23
Ski Resort 0
Service Station 13
Campground 13
School 5
Lodge 6
Recreation 2
Other'* 25
TOTAL 173
alncludes the City of Evanston which uses ground water to supplement
municipal supplies during the irrigation season.
^Includes the Wyoming State Hospital in Evanston.
c
Some public water supplies provide more than one service type.
System have been categorized according to principal use.
^"Dude" ranches, drive-in movies, country clubs, etc.
39
-------
Table 111-2. Municipal ground-water supplies in the Crcen River basin-Overthrust belt.
Municipality
EPA FWS
ID lla
Location
(T-R-S)
Popula t ion
Served
Source
Depth
(feet)
Aquifer
Average Production
MGD AK/yr
¦>
O
Town of l.yman
TeLon Vil1 age
Town of Jackson
City of Evanston
Town of Big Piney
Town of Marbleton
Afton Board of Public
Utilities
Alpine Water and Sewer
District
Bedford Community
Pipe]ine Corp.
Town of Cokeville
ETNA Pipeline Co.
Fairview Pipeline Co.
Freedom Pipeline Co.
Grover Domestic Water
Works
Town of La Barge
Alta Community Pipeline
Co.
Smoot Farmers Pipeline
Town of Thayne
Reliance Public Water
System
5600033
5600218
5600213
5600150
5600007
5600049
5600223
5600002
5600156
5600006
5600015
5600157
5600166
5600158
5600160
5600222
5600275
5600165
5600159
5600046
16-114-32 dd
15-115-16
15-115-21
15-115-20
15-114-31
42-117-24
41-116-27 bb
15-120-
15-120-
15-120-
30-111-
30-112-
21 bb
21 bd
21 cb
31 db
36 ac
30-111-30
32-118-25 b
37-118-
34-118-
-29
-26
24-119
35-119
31-118-
35-119-
32-118-
-2 bd
-7 cb
¦28
6 aa
26-112-6
44-118-??
31-118-?
34-119-24 dd
20-105-
19-105-
19-105-
36 cc
2 be
2 be
2,000
250
4,800
6,000
650
100
400
(600)
1,500
275
300
600
200
130
110
150
250
130
50
315
1,200
we 11
4 springs
wel 1
3 springs
4 uelIs
3 wells
2 wells
3 wells
2 wells
spring
wel 1
spring
spring
spring
spring
spring
well
spring
infiltration
ga]1ery
spring
spring
spring
3 we11s
1 ,200
158
0
%200
65
76
185
115,428
138,152,510
•x-580
0
375
0
60
0
26
93
865
880
Wasatch
Forma t i on
A11uvi um
A11uvium
Alluvium
A] 1uvium
Wasatch
Formation
Wasatch
Format ion
Mad ison
Limestone
Alluvium
Bighorn
Dolomite
Alluvium
Bighorn
Dolomite
Thaynes
Limestone
A11uvium
Twin Creek
Limestone
A1 luvium
Madison
Limestone
Twin Creek
Limestone
Salt Lake
Formation
Mesaverde
Formation
0.160
0.060
(0.166)
1 .430
3.000b
0.130
0.020
0.060
(0.180)
0.300
0.080
(0.190)
0.04 5
0.135
0.030
0.019
0.014
0.022
0.032
0.005
0.007
0.063
0.1 75
179
67 I
(186)
1 .569
0
(3.361)1
168
68
(202)
336
90
(213)
50
151
34
21
16
25
36
6
8
71
196
information from Water Supply Division, U.S. Environmental Protection Agency (1978), unless noted.
^1980 estimates made by officials in telephone interviews with Wyoming Water Resources Research Institute (WRRI).
-------
exclusively by ground water, 6,000 by—both-surface and ground water, and
42,000 by surface water.
Most municipal users of ground water derive their supplies from
Quaternary alluvial aquifers (Table III-2). However, the Wasatch
aquifer (Tertiary aquifer system) provides water for three small towns
in the central part of the Green River basin, the Mesaverde aquifer
supplies the town of Reliance, and five other Cretaceous aquifers,
identified in Table III-2, serve eight small communities in the
Overthrust belt.
Non-Municipal Systems. Forty non-municipal community drinking
water supply systems utilizing ground water support a population of
roughly 4,200 persons (U.S. Environmental Protection Agency, 1978).
These systems include 19 mobile home courts and 21 residential
subdivisions. Total non-municipal community withdrawal of ground water
is about 640 acre-feet per year. The Quaternary alluvial aquifers are
the primary ground-water source.
Non-Community Systems. There are 114 non-community public drinking
water supply systems in the Green River basin. These systems provide
water to a variety of businesses, schools and other facilities serving
transient populations. Withdrawal from non-community wells is estimated
at 570 acre-feet annually (U.S. Environmental Protection Agency, 1978).
Several aquifers are exploited, but most common are the Quaternary and
shallow Tertiary aquifers.
SURFACE WATER USE
Estimated surface water consumptive use within the study area is
430,600 acre-feet per year, with over 83 percent of the total amount
used for irrigation activities. Approximately 285,000 acres were
41
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irrigated with surface water in 1977 and 1978 (Wyoming Crop and
Livestock Reporting Service, 1979) . Other major surface water users
include electric power generation, 48,200 acre-feet per year; trona
mining and processing, 15,400 acre-feet per year (Southwestern Wyoming
Water Quality Planning Association, 1978); drinking water supplies,
9,800 acre-feet per year (U.S. Environmental Protection Agency, 1978);
stock watering, 1,700 acre-feet per year (Wyoming Crop and Livestock
Reporting Service, 1979); and wildlife consumption, 400 acre-feet per
year (Wyoming Game and Fish Commission, personal communication, 1981).
Additional surface water supplies are available in the study area.
Under the terms of the Upper Colorado River Compact, about 800,000 to
1,000,000 acre-feet per year are available to Wyoming from the Green
River watershed. The best estimate is that 40 to 50 percent of this
allocation is presently being used consumptively. Under the Snake River
Compact, Wyoming is allotted about 162,000 acre-feet per year, and a
conservative estimate is that about 30,000 acre-feet are presently used
on an annual basis (Wyoming State Engineer, 1965). Under the Bear River
Compact, Wyoming has fully appropriated its share of 17,750 acre-feet
per year (Wyoming State Engineer, 1965).
Approximately 500,000 acre-feet per year of surface water are
available for future development. Potential problems involved in
developing these allocations include: (1) the need for greater storage
reservoir capacity; (2) the need for possible trans-basin diversions to
areas of intense energy or industrial development; and (3) possible
effects of salt loading or concentration on downstream water users.
42
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IV. HYDROLOGIC PROPERTIES OF THE
MAJOR WATER-BEARING UNITS
-------
IV. HYDROLOGIC PROPERTIES OF THE
MAJOR WATER-BEARING UNITS
METHODOLOGY
The hydrologic properties of the major water-bearing units
evaluated in this section include well and spring yields, permeability,
specific capacity, and transmissivity. These properties, with
additional information, are summarized by formation in Appendix A and by
well in Appendix B. For a description of the well numbering system
utilized in this study, see Appendix B.
Porosity and permeability values have been obtained from the
literature, mainly from Wyoming Geological Association, 1979. Specific
capacity has been obtained largely from pump test data for permitted
domestic wells on file at the Wyoming State Engineer's Office.
Transmissivity has been determined in three ways: (1) by conver-
sion of published oil field permeability data (Wyoming Geological
Association, 1979); (2) by calculations based on specific capacity; and
(3) by calculations based on drill stem test (DST) data obtained from PI
(Petroleum Information) card data (Wyoming Geological Survey, various).
The second and third methods have been adapted from published sources,
and are described in Appendix C. The methods make numerous assumptions
and are, at best, accurate only to an order of magnitude. In general,
it is assumed that most factors which would bias the final values in one
direction or the other cancel each other out. However, transmissivity
values calculated from drill stem tests are up to an order of magnitude
low in comparison to those from permeability tests or from aquifer pump
44
-------
tests, due to the limited stratigraphic interval enclosed by drill stem
packers and/or the lack of well development.
There is a lack of data for many formations, especially those older
than the Upper Cretaceous Hilliard and Baxter shales. This is because
these units are not highly utilized due to their depth in the Green
River basin and to the availability of alluvial and surface water
sources in the Overthrust belt. Therefore, in some cases, their
water-bearing properties are inferred from lithologic properties in
outcrop, and from hydrologic data obtained from other basins within the
state.
Table IV-1 summarizes the hydrologic properties of all geologic
units within the study area; the more permeable units are discussed in
the following sections.
PRECAMBRIAN AQUIFER
The Precambrian is highly fractured and weathered in outcrop or
near the surface in the Teton, Gros Ventre, and Wind River ranges.
Zones of high permeability exist in these areas. In the rest of the
study area, it is buried beneath thick sedimentary cover. As the size
and number of fractures decrease with depth, the optimum productive
zones are the shallowest saturated parts (Lines and Glass, 1975). Most
of the permitted wells completed in Precambrian rocks are located along
the west flank of the Wind River Range. No data are available to
quantify the hydrologic properties of the aquifer.
FLATHEAD AQUIFER
The Cambrian Flathead aquifer is comprised solely of the Flathead
Sandstone. It overlies the Precambrian, which forms an essentially
45
-------
Table LV-1. Generalized stmt igraphy, lithology, and water-bear
Era
Period
Geologic Unit
Thickness (ft.)
Cenozo i c
Qua tier nn ry
Alluvium
<100 thick
in Green
River basin;
up to 410
feet thick ir
Bear River
Valley of
Overthrust
Belt.
Ter tia ry
Miocene and
Pliocene sod iments
including Bishop
Conglomerate,
Browns Park, South
Pass, Camp Davis,
Salt Lake, and
Teewinot
forma t ions.
0-6,000
¦O
Fowkes Formation
0-2,600
Bridger Formation
0-2,300
Green River
Formation
100-2,800
Wasatch Formation 2,500 to
7,200
characteristics of geologic formations in the Green River basin-Overthrust belt.
LitholoRic Description Hydrologic Properties
Unconsolidated sand, gravel, silt, and Highly permeable, productive water-bearing
clay. deposits. Well yields commonly 50 to 500 gpm.
Transmissivity generally 5,000 to 30,000
gpd/ft. Total dissolved solids are generally
less than 500 mg/1.
Conglomerate, limestone, sandstone Poorly consolidated conglomerates are well
and tuffaceous mudstone. drained. Yields generally range from 10 to
120 gpm. Maximum reported spring discharge
from Salt Lake Formation is 8,000 gpm. Three
transmissivity calculations range from 1000 to
>100,000 gpd/ft. Total dissolved solids
generally less than 500 mg/l.
Basal conglomerate overlain by
tuffaceous mudstone, tuffaceous,
calcareous sandstone and rhyolitic
ash.
Locally yields water to wells and springs in
Overthrust belt. One Fowkes spring discharges
125 gpm.
Tuffaceous lacustrine and flood
plain deposits, becoming locally
conglomeratic near the Uinta
Mountains.
A major aquifer in the southern Green Rivor
basin-Overthrust area. Yields from wells and
springs commonly range from 2 to 100 gpm.
Transmissivities are commonly between 500 and
3,000 gpd/ft.
Lacustrine claystone, marlstone, oil
shale and saline deposits with
discontinuous lenses of fine-grained
sandstone in the Laney and Tipton
shale members of the upper and lower
Green River Formation, respectively.
Trona deposits occur in the Uilkins
Peak Member of the middle Green
River Formation.
Silty to sandy claystone, lenticular
beds of fine— to medium-grained
sandstone becoming conglomeratic to
the south and west.
A major aquifer in eastern Green River basin.
Sandstone lenses in Laney Shale and Tipton
Shale members generally yield 3 to 100 gpm to
wells and springs. Transmissivities range
from 1,000 to 6,500 gpd/ft. Vertical
permeability is very low due to great thickness
of tight marlstone and shale above and below
sands. Total dissolved solids concentrations
in Laney Shale usually exceed 1,500 mg/1.
Wilkins Peak TDS levels are typically 10,000
to 100 ,000 nig/ 1 .
Major aquifer of Green River basin. Well
yields range from 1 to 1,300 gpm, though
commonly less than 50 gpm. Transmissivity
generally ranges from 200 to 1,000 gpd/ft.
Oil field pay zone porosity and permeability
range fijom 20 to 25 percent and 0.02 to 18
gpd/ft. , respectively. Total dissolved solids
concentrations between 300 and 1,000 mg/1 may
be expected.
-------
Table IV-1. (continued)
Em
Period
Geologic Unit
Thickness (ft~)
Hoback Formation
0-16,000
Fort Union
Format ion
0-6,000
Cenozoi c-
Mesozoic
Tcrt iary-
Upper
Cretaceous
Evanston
Format ion
1,350-
2,900
Mesozoic
Upper
Cretaceous
Lance
Format ion
0-50?
Lewis Shale
200-2,000
Mesaverde Group
(includes Blair,
Rock Springs,
Ericson, and
Almond formations
near Rock Springs
uplift)
1,300-
5,200
Adav i 1 le
Formal ion
1,400-
5,000
HilJ iard Sha 1 e
Baxter Shale
3,000-
6,800?
Lithologi c Description
Hydrologic Properties
Interbedded sandstone and calcareous
shaje with thick Lenses of conglomerate.
Present in Moback and Snake River
bas i ns.
Fine- to medium-grained, silty sand-
stone and lignitic mudstone with
coal; becomes coarser grained near
mountainous areas. Major coal seams
occur in the lower Fort Union.
Lower member of mudstone, siltstone,
claystone, and carbonaceous sandstone;
middle member of conglomerate in a
matrix of fine to coarse sand; upper
member consists of carbonaceous sandy
to cLayey siltstone interbedded with
sandstone and conglomerate.
Very fine- to fine-grained, lenticular,
clayey, calcareous dark shale, coal
and lignite.
Calcareous to non-carbonaceous shale
with beds of siltstone and very fine-
grained sandstone.
Tightly cemented, very fine- to fine-
grained sandstone and siltstone
interbedded with gray shale and a
few thin coal seams in the western
Green River basin. Near the Rock
Springs uplift the Mesaverde Group
consists of interbedded fine-grained
to conglomeratic sandstone, siltstone,
sha1e, and coa1.
Fine- to medium-grained calcareous
sandstone and carbonaceous mudstone
with numerous coal beds. Present in
Overthrust belt.
Sandy shale with interbedded mudstone
and shaley sandstone.
Hydrologic data arc scarce; however thick
sandstone and conglomerate lenses provide an
excellent potential water source. One well
yields 20 gpm with estimated transmissivity of
2,300 gpd/f L.
Locally utilized aquifer of Green River basin
and southern Overthrust belt. Oil and gas
field data indicate pay zone porosities of 9
to 23 percent and sandstone permeability of
<.01 to 0.5 gpd/ft. .
Conglomerates and conglomeratic sandstones
present in the Overthrust belt are capable of
yielding moderate to large quantities of water
to wells. Yields to two Evanston wells aro 3
and 200 gpm. An estimated 1,000 gpm flows
from one Evanston spring.
No water well data for Lance Formation. The
unit is probably capable of yielding small
quantities of water from fine-grained sands
and conglomeratic sandstone at base (Fox
Hills Sandstone). Oil field pay zone porosity
is 12 to 18 percent.
Unit is an aquitard where present in the east-
ern Green River basin and Rock Springs uplift.
Well data are not available.
Unit is utilized locally, particularly near
Rock Springs uplift, for stock and domestic
supplies. Sandstones of Ericson Formation
(middle to upper Mesaverde Group) arc highly
permeable and capable of large yields to wells
and springs. Reported oil field pay zone
porosities range from 9.5 to 24 percent. ^
Permeability estimates are <.01 to l.L gpd/ft. .
Reported yields from Mesaverde wells east of
the basin boundary, on the Rock Springs uplift,
are 100 to 200 gpm.
Generally considered a minor aquifer of the
Overthrust belt area, though no well data or
spring yield records exist for the unit.
Major regional confining unit of Green Kiver
basin and Overthrust belt. Locally yields
small quantities to wells from sand lenses.
Oil field pay zone porosity is 10 to 21 percent.
-------
Table LV-1. (continued)
Era
Peri od
Geologic Unit
Thickness (ft,'
Frontier Formation
1,100-
3,000?
Lower
Cretaceous
Aspen Shale
400-2,200
Bear River
Format ion
800-1,500
00
Gannett Group
(Overthrust
belt)
800-5,000
Upper
Jurassic
Stump Sandstone-
Preuss Redbeds
(Overthrust belt
and NW Green
River basin)
Curtis Formation-
Entrada Sandstone
(SE Green River
bas i n)
27 0-460
Middlo
Jurass1c
Twin Creek
Limestone
800-3,800
Lower
Jurassic
Nugget Sandstone
750-1,300
LithoJogic Description
Hydrologic Properties
Lenticular sandstone, fine to medium-
grained; interbedded mudstone, clay-
stone, siltstone, minor coal;
prolific gas and occasional oil
producer.
Aquifer yields 5 to 50 gpm to springs.
Porosity of oil field pay zones is 8 to 25%;
TransmLssiviti-es from drill stem tests generally
less than 10 gpd/ft. Variable cementation
and lenticu1arity of beds causes irregular
occurrence of high transmissivity zones.
Shale; interbedded fine-grained
sandstone and siltstone.
Locally utilized aquifer, maximum spring and well
yields 25 to 30 gpm. Oil field pay zone porosity
of 15 percent in "fractures." Water yields are
mainly from stray sands and fracture zones.
Fissile shale with sandstone interbeds
in Overthrust belt, fine shaley sand-
stone with shale and siltstone inter-
beds ("Muddy" sandstone upper) and
shale with sandstone, siltstone and
bentonite interbeds (Therroopolis Shale
-middle, and "Dakota" sandstone-lower)
in Great Divide and Washakie basins
just east of Rock Springs uplift.
Interbedded siltstone, calcareous
siltstone, calystone, mudstone,
sandstone, conglomerate, limestone.
Lower conglomerate unit (Lakota).
Minor aquifer with spring yields generally
4 to 15 gpm and similar well yields. Oil
field pay zone porosity is 8 to 21 percent.
Pump test transmissivities are 300, 2300,
9500 gpd/ft. (specific capacities 0.3, 2.3,
and 7.8 gpm/ft.), calculated drill stem test
transmissivity generally less than 45
gpd/ft. Porosity and permeability are highest
in the "Muddy" and "Dakota" members.
Water-bearing units restricted to sandstones
and conglomerate in lower part. Lakota
porosity ranges from 18 to 21 percent with one
transmissivity estimate of 160 gpd/ft. for the
Bechler Member. Springs in Lakota and
Bechler conglomerate members flow 5 to 75 gpm.
Interbedded sandstone, siltstone,
mudstone and limestone.
Unit is considered a poor aquifer with one
well yield of 5 gput and spring flows of 20
and 50 gpm. Transmissivities estimated from
3 drill stem tests are less than 12 gpd/ft.
Upper- limestone and shale
Lower- limestone, mainly brecciated,
but partly honeycombed, and claystone.
Sandstone, fine to medium-grained,
welJ-sorted, quartzitic, cross-bedded
minor clay and silt in upper part,
significant clay and silt In lower
part; locally highly calcareous;
prolific oil and gas producer.
Minor aquifer in Overthrust belt. Spring
flows range from 20 to 300 gpm. Transmissivity
estimates range from less than 1 to 16 gpd/ft.
Permeability is generally less than 0.002
gpd/ft and porosity from one oil field pay
zone is 1.7 percent.
Major aquifer of Mesozoic system. Springs flow
3 to 300 gpm with four flows of 1,400 to 2,000
gpm. Well yields not available. Transmissivity
estimates range from 9 to 37 gpd/ft in the
Green River basin and 1.9 to 186 gpd/ft in the
Overthrust belt. Oil and gas field pay zone
porosities range from 10 to 20 percent. Perme-
ability is 0.2 to 3 gpd/ft^, highest in the upper
part of the aquifer.
-------
Table 1V-1. (continued)
Era
Per iod
Geologic Unit
Thlckness (ft.)
Lithoiogic Description
llydrologic Properties
Tr iass J c
Anknreh
Forma t ion
200-800
Shale, interbedded siltstone, fine-
grained sandstone, and, locally, lime-
stone in the middle part.
MLnor regional aquifer, locally confining,
spring flows 200 gpm. No current well
production. Transmissivity from one drill
stem test is 0.5 gpd/ft.
One
Thaynes
Limestone
,100-
,600
Silty limestone, with siltstone and
shale in the upper part.
Generally considered a regional aquifer with
spring flows of 5 to 1,800 gpm (4 less than 100
gpm) and one well flowing 150 gpm. Oil field
pay zone porosity at one field is less than 5
percent. Transmissivity estimates from 3 oil
field drill stem tesLs are 0.3 to 38 gpd/ft.
The unit is most productive where solution
openings, bedding plane partings, and fractures
exist.
Woodside
Format ion
350-600
Anhydritic siltstone and mudstone with
some fine-grained sandstone.
Unit acts as regional aquitard.
spring data not available.
WeL1 and
Dinwoody
Forma t ion
250-700
Siltstone and shale, dolomite and
interbedded anhydrite in upper part.
Regional aquitard with local productive zones.
One spring flows 150 gpm. Transmisslviiy
estimate from one drill stem test is 8.8 gpd/ft
gpd/ft.
Pa 1 eozo i c
Permian
Phosphoria
Format ion
200-400
Phosphatic carbonate, cherty shale and
sandstone in N. Overthrust belt and
in NVJ Green River basin. Non-phosphat ic
carbonate with subordinate sandstone
in S. Overthrust belt and SK Green
River basin.
Unit is minor aquifer, locally confining. One
well and one spring yield 200 and 300 gpm,
respectively. Transmissivity estimates
typically less than 13 gpd/ft. Most productive
from fracture zones and interbedded sandstones
in the upper part of the formation.
PennsyI vanLan Tensleep
Sandstone
450-1,000
Mississippian-
PennsyI van i an
Amsden Formation
(Overthrust belt
and NW Green
River basin)
Darwin Sandstone
Member (Green
River basin)
400-700
Quartzite, thick-bedded, calcareous
sandstone, and limestone (mainly in
upper part) (Overthrust belt). Sand-
stone, fine-grained and well-sorted
with quartzite and thinly layered
siliceous dolomitic limestone (Green
River basin and E. Overthrust belt).
Mudstone, siltstone and sandstone,
with cherty limestone.
Major aquifer of Paleozoic System. Well yields
range from 210 to 700 gpm. Spring flows arc-
commonly less than 210 gpm. Transmissivity
estimates from 11 drill stem tests are 0.14 to
38 gpd/ft. Good interstitial permeability and
excellent secondary permeability where
f ractured.
Minor aquifer in Green River basin, but loc.nl ly
confining in Overthrust belt and NW Green River
basin. One Amsden well yields 8 gpm. Oil
field pay zone porosity at 3 fields is 7 to 12
percent. Transmissivity estimates from 4 drill
stem tests are less than 1 to 4.8 gpd/Jjt.
Permeability is less than 0.02 gpd/ft. (one
estimate).
Mississipplan Mad ison Limestone
800-2,000 Limestone, thin-bedded to massive,
brecciated and partly cherty, and
dolomite, thick-bedded to massive.
Excellent karst and fracture develop-
ment throughout the area.
Major regional aquifer in study area and entire
state of Wyoming. Excellent solution and
fracture permeability. Maximum well yield of
720 gpm, though most yields are less than 100
gpm. Four springs flow less than 350 gpm, two
others flow 4,000 and 40,000 gpm. Trans-
missivity is typically less than 15,000 gpd/ft.
Specific capacity generally 0.1 to 10 gpm/ft.
-------
Table IV-J. (continued)
Period
Geologic Unit
Thickness (ft.)
Lithologic Description
Devonian- Darby Formation
Mj ssissippian
400-1,000 Limestone and dolomite, thin-bedded
to massive, and siltstone; shale and
sandstone predominate in northern
Overthrust belt.
Hydrologic Properties
Major aquifer with permeability dependent upon
degree of fracturing and secondary solution,
best developed in Overthrust belt. Four
Darby springs flow 5 to 1,100 gptn. One well
yields more than 5 gptn.
Ordovic ian
Bighorn Dolomite
400-1,000
Fine- to medium-grained massive dolomLte
and dolomitic limestone.
Highly productive aquifer where fracture,
secondary solution and bedding plane perme-
ability are well developed. Three Bighorn
springs flow 250 to 450 gpm, one flows 3,200
gpm. Porosity from one oil field is 2 percent.
Well data are not available.
Cambr ian
Ga11alin Limestone
125-1,000 Limestone, thin-bedded and dolomitic
limestone with minor interbedded
conglomerate and thin shale partings.
Well and spring data not available; however,
lithology as well as fracture and secondary
solution permeability development are
indicative of a potentially productive aquifer.
O
Gros Ventre
Format ion
Flathead
Sandstone
500-2,500 Shale and interbedded conglomerate in
the upper part, underlain by lime-
stone and a lower hematitic shale
unit.
175-200 Quartzite, fine-grained, with coarse-
grained sandstone lenses. Minor
silty shale beds occur in upper part
with some conglomerate in the lower
part.
Unit is generally considered a regional
aquitnrd with low vertical permeability due to
upper and lower shales. Well data are not
available. One spring flows 900 gpm (?).
Well and spring data are not available for the
unit. Lithology is similar to basal Cambrian
in other basins of western Wyoming where
Flathead equivalents are highly permeable,
product ive aquifers.
Precambrian
Precambrian
und i v ided
Gneissic granite with schist, granite
and pegmatite.
Locally utilized aquifer near outcrop areas on
west side of Wind River and Gros Ventre ranges
and east side of Teton Range, where highly
weathered permeable zones overlie well
fractured bedrock. Optimum productive zones
are probably less than 200 feet deep. Well
and spring data not available.
See Appendix A, "Summary of Hydrologic Properties, by Formation" for details.
-------
impermeable boundary. Overlying the Flathead is the Gros Ventre
aquitard, which isolates the Flathead from overlying aquifers. The
Flathead has been thrust to the surface at several locales in the
Overthrust belt, specifically along the east side of Star Valley, in the
Snake River Valley, and near the La Barge platform. In the northern
Overthrust belt is is 175 to 200 feet thick (Schroeder, 1969); its
thickness in the eastern Green River basin (T. 19 N., R. 104 W., Sec. 11
ac) is 361 feet.
No springs or water wells have been attributed to this formation.
Three petroleum wells penetrating the Flathead have been identified,
although no usable DSTs were conducted.
Because of lack of data on the Flathead, little is known of its
aquifer properties or of water movement. It is known to contain lenses
of permeable sandstone interbedded with virtually impermeable quartzite,
with conglomerate at its base (Schroeder, 1969). Secondary permeability
is well developed along bedding plane partings in outcrop and where the
rocks are highly fractured. Because of the permeable sandstone,
conglomerate, and secondary permeability occurrence, it is "probably a
potential source" of water (Lines and Glass, 1975) in the Overthrust
belt or wherever it is within economic reach of drilling.
PALEOZOIC AQUIFER SYSTEM
The Paleozoic aquifer system crops out as a series of four linear
north-south belts west of and parallel to the major thrust fronts of the
Overthrust belt (see Figure II-5) . Aquifers within this system include
the Bighorn Dolomite, Darby Formation, Madison Limestone, Tensleep
Sandstone, and Phosphoria Formation.
51
-------
Because the major aquifers are primarily carbonate, the most
permeable parts are where solution openings and fractures occur. The
Madison is the most productive aquifer in the system due to its
well-developed paleokarst.
Numerous springs and wells have been attributed to the Paleozoic
aquifer system, with flows or yields ranging from hundreds to several
thousands of gallons per minute. The individual aquifers are discussed
below in stratigraphic order. Units not discussed below are primarily
of low permeability, and are seldom sources of water supplies.
Bighorn Dolomite
The Bighorn is a massive bedded crystalline dolomite in the upper
part of the formation, but is thin-bedded dolomite and sandstone in the
lower part. Permeability in the upper dolomite is essentially nil,
except where fractured. In the lower part of the formation, the sand-
stones exhibit good intergranular permeability and secondary
permeability along bedding plane partings. The Bighorn is 200 to 450
feet thick in the Green River basin (Randall, 1960), 400 to 450 feet
thick in the northern Overthrust belt, and more than 1,000 feet thick in
the west-central Overthrust belt (Schroeder, 1969; Oriel, 1969).
Six Bighorn springs, two of which are the source of water for small
communities and four with yields of 250 to 3,200 gpm, have been
identified between T. 31 N. and T. 37 N. in the Overthrust belt.
However, no known water wells penetrate the Bighorn, and no usable DSTs
have been found. The Wyoming Geological Association (1979) reports the
Bighorn, at one producing field, to have two percent porosity due to
fractures.
52
-------
Darby Formation
The Darby consists of thin-bedded to massive dolomite and limestone
in much of the area (Schroeder, 1969), but is predominantly shale and
siltstone along the Teton Range (Randall, 1960). The formation
thickness varies from 1,000 feet in the southwest Overthrust belt to 330
feet in the Green River basin (see Figure II-4a).
The Darby is penetrated by at least one water well (T. 28 N., R.
113 W., Sec. 19), which yields more than 5 gpm. Four springs, located
near T. 28 N. and T. 38 N. within the Overthrust belt, yield from 5 to
1,100 gpm.
Madison Limestone
The Madison consists of thin to massive bedded dolomite and
limestone which exhibits excellent secondary permeability throughout its
entire thickness in the study area. This permeability is produced by
solution zones along bedding plane partings and joints. Madison
thickness varies from 1,300 to 2,100 feet in the Overthrust belt
(Schroeder, 1969) to less than 10 feet thick in the Washakie basin
(Welder and McGreevy, 1966), east of the Green River basin.
The Madison is the most productive aquifer within the Paleozoic
aquifer system, based on data from the Overthrust area. Seven Madison
/
springs occur within the Overthrust belt (T. 26-39 N.), five yielding 15
to 350 gpm, and a sixth, 40,000 gpm. Ten water wells within the
northern Overthrust belt, Teton Range, and along the edge of the Snake
River Valley yield from 6 to 720 gpm. Specific capacities of from <1 to
7 gpm/ft (6 wells), 46 gpm/ft, and 140 gpm/ft were used to compute
estimated transmissivity values from 100 to 15,000, 50,000, and 100,000
53
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gpd/ft, respectively. Transmissivities of 2 to 20 gpd/ft from four DSTs
were also determined. High transmissivity zones are located principally
along the north-south trending faults in the southeast Overthrust belt.
Very little hydrologic data exist for the Madison within the Green
River basin, as it does not crop out and is too deeply buried for
current exploitation. However, throughout much of Wyoming (in the
Overthrust belt and the Wind River, Bighorn, and Powder River basins;
Richter, 1981; Libra and others, 1981; Feathers and others, 1981), the
Madison is one of the most productive aquifers, especially where
fracture and solution zones occur. Therefore, it is expected that
similar hydrologic properties exist within the Green River basin.
Tensleep Sandstone
The Tensleep Sandstone consists of well-sorted quartz sandstone,
with an upper limestone member. Sandstones have good intergranular
permeability and excellent secondary permeability where fractured.
Although there is a reported decrease of Tensleep porosity and perme-
ability with increased burial depth (high lithostatic pressure)
(Bredehoeft, 1964), at shallow depths the Tensleep is a consistently
good producing aquifer. In the Overthrust belt, the Tensleep (Wells
Formation) is 450 to 1,000 feet thick, but is thickest in the southern
part (Richardson, 1941; Oriel, 1969). In the Green River basin it is
thickest (up to 850 feet) along the Rock Springs uplift (Welder and
McGreevy, 1966), but thins to less than 370 feet in the northwest basin
(see Figure II-4a).
Discharges from eight Tensleep springs in the Overthrust belt range
from 5 gpm to more than 2,200 gpm. Three Overthrust belt water wells
produce between 200 and 700 gpm. One pump test had a reported specific
54
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capacity of 6 gpm/ft, resulting in an estimated transmissivity of 10,000
gpd/ft. Though transmissivities calculated from 11 DSTs are much lower
(<1 to 38 gpd/ft), the high well and spring yields indicate
substantially better transmissivities for the entire saturated thickness
of the formation.
Phosphoria Formation
Within the Green River basin and Overthrust belt the Phosphoria
consists mainly of low-permeability shale and dolomite with a permeable
sandstone unit restricted to the top of the formation (Lane, 1973). The
Phosphoria produces locally where fractured; elsewhere the formation
yields very little water and is a confining bed for the underlying
Tensleep. It varies from 200 to 400 feet thick in the Overthrust belt
(McKelvey and others, 1959) and is about 290 feet thick in the Green
River basin (see Figure II-4a).
Only three springs issue from the Phosphoria in the Overthrust
belt, and none in the Green River basin. Flow from one spring is 300
gpm; the one known water well completed in the Phosphoria has a reported
yield of 200 gpm (see Appendix B).
NUGGET AQUIFER SYSTEM
Outcrops of the Nugget aquifer system are limited to a north-south
series of high ridges and valleys throughout the Overthrust belt area.
Aquifers within the system include the Thaynes Limestone, Nugget
Sandstone, and Twin Creek Limestone. The Nugget is the primary aquifer.
The Ankareh Formation is locally a confining bed which partially
isolates the underlying Thaynes aquifer from the overlying Nugget.
55
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The aquifer system is isolated from the Paleozoic aquifer system by
the Dinwoody-Woodside aquitard, and from overlying aquifers by three
formations (Preuss, Stump, and Morrison) which, though capable of
locally transmitting and yielding small amounts of water, are relatively
impermeable regionally.
Thaynes Limestone
The Thaynes consists of silty limestone with abundant shale and
siltstone in the upper part. In the central Overthrust belt it varies
from 1,100 to 2,600 feet thick (Veatch, 1907; Ross and St. John, 1960),
but is only about 430 feet thick in the Green River basin (see Figure
II-4a).
Eight artesian springs have been identified in the Thaynes
throughout the Overthrust belt. Four flow from 5 to 100 gpm, with
others at 140, 350, 900, and 1,800 gpm. One well flows at 150 gpm.
Thaynes pay zone porosity of less than 5 percent in "matrix
fractures" occurs in one oil/gas field (T. 17 N., R. 119 W.) (Wyoming
Geological Association, 1979). Transmissivity values of <1, 8, and 38
gpd/ft were computed from DSTs at this field.
Secondary permeability features in Thaynes Limestone include good
bedding plane partings and solution openings in the middle part. Where
secondary permeability exists, the Thaynes is a productive aquifer.
Ankareh Formation
The Ankareh is composed primarily of 200 to 1,000 feet of
low-permeability shale, siltstone, and fine-grained sandstone interbeds,
and some limestone in the middle part (Veatch, 1907; Ross and St. John,
1960; Randall, 1960). The confining properties of the Ankareh are
56
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evident from the occurrence of artesian springs and wells in the
underlying Thaynes (see above) where the Ankareh is near the surface.
One spring, flowing at 200 gpm, is located at T. 29 N., R. 115 W.
There are no water wells attributed to the Ankareh. A transmissivity
value of <1 gpd/ft was obtained from one DST.
Nugget Sandstone
Ten springs originate from the Nugget: two have unknown flows; two
flow at less than 100 gpm; four at 75 to 200 gpm; one at 1,400 gpm; and
one at 2,000 gpm. These springs are located mainly west of La Barge,
although the Nugget also crops out elsewhere in the Overthrust belt.
There are no known water wells completed in the Nugget.
Pay zone porosity and transmissivity values from published data and
from DSTs vary within the study area. These parameters are generally
greater in the Overthrust belt than in the Green River basin, as shown
by the following table.
Green River Basin Overthrust Belt
Published Data
Number of fields
Transmissivity (gpd/ft)
Porosity (%)
Drill Stem Tests
Number of tests
Transmissivity (gpd/ft)
2
9-25
10-14
9
2.8-37
(most <15)
146-186
10-20
10
1.9-66
(most >25)
The sands of the Nugget are well-sorted, and often poorly cemented
in outcrop. Porosity and permeability are good, especially in the
cross-bedded upper part of the aquifer, where clay and silt are almost
absent (Picard, 1975). The decrease in transmissivity in the Green
57
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River basin may be due to increased lithostatic pressure (deeper burial)
and decreased fracture occurrence, as no pronounced stratigraphic
differences are known. Much of the Nugget is considered aeolian due to
its high degree of sorting (Picard, 1975).
The thickness of the Nugget varies from about 500-600 feet in the
Green River basin to a maximum of 1,300 feet in the southern Overthrust
belt (Lines and Glass, 1975; Wyoming Geological Survey, various).
Twin Creek Limestone
The upper Twin Creek is composed of interbedded limestone and
shale. It is relatively impermeable in comparison to the lower part,
which is predominantly brecciated and honeycombed limestone, with
interbedded claystone (Lines and Glass, 1975). The total formation
thickness varies from 800-3,800 feet in the Overthrust belt (Veatch,
1907; Imlay, 1950), to about 360 feet in the southeastern Green River
basin (see Figure II-Aa).
Five springs flow from the Twin Creek; three flow at 20 to 75 gpm;
a fourth at 300 gpm. No known water wells are completed in this
formation.
Porosity of 1.7 percent occurs at one oil field with transmis-
sivities <1 gpd/ft. Two "wildcat" well DSTs produced calculated
transmissivities of 1 and 16 gpd/ft.
UPPER JURASSIC-LOWER CRETACEOUS AQUIFERS
The sequence of sediments from the basal Upper Jurassic Lakota
Conglomerate to the Cretaceous Aspen (Mowry) Shale provides a series of
vertically and areally discontinuous aquifers. The presence of mostly
58
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shales, siltstones, and mudstones, and the general absence of springs,
indicate that these rocks are characteristically of low permeability.
The three principal aquifers (but relatively minor compared to
others in the area) of this rock sequence are the Lakota-Bechler
conglomerates of the Gannett Group and the "Muddy" and "Dakota" sand-
stones of the Bear River Formation; the occurrence of other water-
bearing units such as the Aspen Shale is restricted to stray sands and
fracture zones. As with other pre-Hilliard-Baxter aquifers, there are
little available pump test data. In general, spring and well yields are
less than 100 gpm, with transmissivities less than 100 gpd/ft.
Gannett Group
Permeability characteristics of the Gannett Group are difficult to
determine due to lithologic variability and poor well completion
records. Most of the group consists of up to 5,000 feet of siltstone,
claystone, and limestone, which will have poor permeabilities, except
where carbonate fracture or solution zones are present. Within the
middle part of the Gannett Group, the Lakota (Green River basin) and
Bechler (Overthrust belt) conglomerates are the only formations which
have regionally good permeabilities; they are the known sources for two
water supplies. These well-sorted conglomerates are less than 75 feet
thick (see Figure II-4a).
Eleven springs issue from the Gannett Group (Bechler?) in the
Overthrust belt, with flows ranging from 5 to 75 gpm. Four water wells,
two flowing at 30 gpm and two pumped at 20 and 100 gpm, are completed in
the Gannett.
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Transmissivity estimates for the Bechler vary from <1 to 160
gpm/ft. Reported Lakota porosities vary from 18 to 21 percent at two
locations in the Green River basin (Appendix B).
Bear River Formation
Permeable parts of the Bear River in the Overthrust belt include
fissile shale with discontinuous sandstone interbeds; in the Green River
basin silty sandstones are present in the upper "Muddy" and lower
"Dakota" members, which are separated by the Thermopolis Shale. Zones
of highest permeabilities and potential well production are in the
"Muddy" and "Dakota." However, most spring flow, well yield, and
transmissivity values indicate only moderate water-bearing capabilities
for this formation.
In the Overthrust belt the Bear River is 800 to 1,500 feet thick
(Lines and Glass, 1975). In the Green River basin the "Muddy" and
"Dakota" are always less than 100 feet thick, and may be absent in the
southeastern part. The bentonitic Thermopolis Shale varies from 40 to
235 feet thick (Welder and McGreevy, 1966).
The Bear River Formation has nine known springs with flows of 4 to
15 gpm, and a tenth flowing at 100 gpm. All springs are in the
Overthrust belt, in T. 25 N. and T. 26 N. Pumping yields to wells (5)
vary from 1 to 250 gpm, with specific capacities of <1 to 8 gpm/ft.
Transmissivities of 300, 2,300, and 9,500 gpd/ft have been estimated
from available water well data (Appendix B); values over 1,000 gpd/ft
are in areas with intense fracturing.
Transmissivities from DSTs are significantly lower. The "Muddy"
sandstone transmissivities are about 5 gpm/ft; the "Dakota" sandstone
transmissivities range from <1 to 400 gpm/ft, with most between 2 and 7
60
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gpm/ft. Porosities of the "Muddy" and "Dakota" range from 18 to 20
percent and 8 to 21 percent, respectively.
Aspen Shale
The Aspen in the Overthrust belt is predominantly 1,200 to 2,200
feet (Veatch, 1907; Schultz, 1914) of low-permeability shale, with
exploitable water yields mainly from stray sands and fracture zones.
Four known springs, with flows of 8 to 25 gpm, issue from the Aspen
Shale; all are in the northern Overthrust belt. Six wells are also
completed in the Aspen with yields from 1 to 30 gpm. Pay zone porosity
from one oil field has been reported at 15 percent, in "fractures." Two
DSTs measured transmissivity values of less than 1 gpd/ft.
FRONTIER AQUIFER
The Cretaceous Frontier aquifer is composed solely of the Frontier
Formation, which is bounded below by the Aspen Shale and above by the
3,000 to 5,000 foot thick Hilliard-Baxter aquitard. The permeability of
the aquifer is intergranular, except where fractured, and produces only
moderate amounts of water. The major outcrop of the Frontier aquifer
occurs in the southeastern Overthrust belt between T. 13 N. and T. 28
N., just west of the Darby fault (see Figure II-5).
The Frontier is composed of lenticular sands, variably cemented,
with interbedded mudstone, claystone, and siltstone. It varies from 400
feet thick in the Green River basin to 3,000 feet thick in the south-
central Overthrust belt (Armstrong and Oriel, 1965). Permeability is
highly dependent on the degree of sandstone cementation. The greatest
water-bearing potential is in the Overthrust belt (except in the north-
east part where the Frontier is absent), and in the western Green River
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basin, where two deltaic sandstone complexes were deposited (Chadenas,
1975) .
Petroleum geologists have divided the Frontier into marker
"benches," or prominent sand beds. Three major markers, the Frontier 1
(highest) to 3 (lowest), typically range from 360 to 575, 220 to 500,
and 150 to 325 feet thick, respectively. They are the principal gas and
oil producers, and where flushed, are probably the principal water-
bearing zones within the formation.
Eleven springs, ten with flow data, have been identified in the
Frontier, all occurring within the Overthrust belt. Flows range from 5
to 100 gpm. One water well, flowing at 1 gpm, is also completed in the
Frontier Formation.
Pay zone porosity values from numerous producing fields range from
8 to 25 percent. Most transmissivity values from the literature are
less than 3 gpd/ft. Transmissivities of up to 30 gpd/ft, but usually
less than 10 gpd/ft, were also calculated from other DST data.
MESAVERDE-ADAVILLE AQUIFER
The Upper Cretaceous Mesaverde Group and Adaville Formation are
time-stratigraphic equivalents in the Green River basin and Overthrust
belt, respectively. The water-bearing zones within this aquifer are
bounded below by the Hilliard-Baxter aquitard and above the the Lewis
Shale aquitard, where present in the southeastern Green River basin.
The major outcrop areas of the aquifer is along the west flank of the
Rock Springs uplift; a much smaller exposure exists south of Evanston.
These rocks may be up to 5,000 feet thick in the Overthrust belt, but
average only about 1,300 feet thick in the Green River basin. The
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variability is due to an erosional unconformity on the top of the
formation.
Water production from the aquifer is mainly from well-cemented,
fine-grained sandstone. The siltstones, mudstones, and shales have
significantly lower permeabilities and act as local confining beds. The
most permeable part of the aquifer is within the middle of the Mesaverde
Group (Rock. Springs and Ericson formations), which contains
predominantly sandstone. The basal unit of the Adaville is the Lazeart
Sandstone, which contains permeable sandstone, shale, and some coal
(Anderson and Kelly and others, 1981).
Little quantitative water well and spring data exist for the
Mesaverde-Adaville aquifer within the study area. Seven wells are
completed in the Ericson Formation (middle Mesaverde Group) north of
Rock Springs, with yields varying from 15 gpm (2 wells) to 200 gpm (3
wells). Several other wells also exist in the Rock Springs area but no
yield data are reported.
East of the Rock Springs uplift are several wells and springs that
obtain water from permeable zones throughout the Mesaverde. Reported
well yields and spring discharges range from 100 to 200 gpm (Collentine
and others, 1981).
Porosity, permeability, and calculated transmissivity data for the
Mesaverde Group, derived from Wyoming Geological Association (1979),
indicate a pay zone sand porosity from 9.5 to 24 percent. Permeability
2
for the same zones is not greater than 1 gpd/ft , corresponding to
calculated transmissivities of less than 2 gpd/ft. Two additional
reported transmissivity values are 35 and 165 gpd/ft.
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TERTIARY AQUIFER SYSTEM
The Tertiary aquifer system includes some of the most productive
sandstone aquifers of the Green River basin-Overthrust belt area. Over
the southeastern quarter of the Green River basin, the Tertiary system
is underlain by a major aquitard, the Lewis Shale. Elsewhere in the
study area, the base of the Tertiary aquifer system is marked by an
erosional unconformity—and the Lewis Shale is absent. Quaternary
alluvial deposits overlie the Tertiary sediments in the valley of the
Green River and along the southwestern flank of the Wind River
Mountains, where thick morainal, glacial outwash, and till deposits have
buried Tertiary and older rocks. Included within the Tertiary aquifer
system are up to 15,000 feet of sediments, including the late Upper
Cretaceous Lance up to the Pliocene Browns Park formations (see Figures
II-4b and II-7).
The major aquifers of the Tertiary system are the Wasatch
Formation, the Laney Member of the Green River Formation, and the
Bridger Formation. The Wasatch Formation is most productive along the
basin flanks in the north and central Green River basin, and in the
southwest corner of the basin. Thick tongues of fine- to coarse-grained
sandstone extend basinward from the Wind River and Overthrust belt
ranges in the north and from the Uinta Mountains in the south. Inter-
tonguing with the Wasatch Formation are impermeable marlstone, shale,
and lacustrine limestone of the lower and middle Green River Formation
in the center of the basin. Water-bearing sandstone lenses, present in
the Tipton (lowest) and Laney (uppermost) members of the upper Green
River Formation, are utilized mainly along the east side of the Green
River basin, especially in the Eden-Farson area. Permeable,
fine-grained sandstones of the Bridger Formation, which overlies the
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Wasatch and Green River formations, are present in the south-central
Green River basin, particularly in the Bridger Valley.
Yields from water wells completed in the Tertiary aquifer system
generally range from 10 to 200 gpm, although higher yields may be
expected where thick sandstone sections are penetrated. Permeabilities
are primarily intergranular.
Lance Formation
Documented water well and spring data are unavailable for the Lance
Formation in the Green River basin. The Lance is mainly very fine- to
fine-grained shaley sandstone with moderate porosity, although the basal
unit is much coarser. The average pay zone porosities at two oil and
gas fields in the Lance Formation are 12 and 18 percent (Wyoming
Geological Association, 1979). One oil field DST produced a transmis-
sivity value of more than 20 gpd/ft in these basal sandstones. Though
the Lance Formation remains undeveloped in the Green River basin, its
potential as a moderately productive aquifer is high, particularly near
the west flank of the Rock Springs uplift where it is exposed or near
the surface. Scattered oil well information provided a maximum Lance
thickness in the study area of 2,457 feet.
Evanston Formation
Two water wells are completed in the Evanston Formation and two
springs issue from Evanston outcrops in the southern part of the
Overthrust. The Evanston Formation includes 1,300 to 2,900 feet of
well-sorted conglomerates and conglomeratic sandstones that are capable
of moderate to large well yields, indicated by an estimated 1,000 gpm
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spring (T. 22 N. , R. 116 W., Sec. 6 ab) in the Evanston area (Oriel and
Tracey, 1970) and two water wells yielding 3 and 200 gpm.
Fort Union Formation
Only one water well and one spring in the southeastern Green River
basin are identified as discharging from the fine- to medium-grained
sandstone and mudstone of the Fort Union Formation, and oil and gas test
holes provide the only documented hydrologic data. However, the basal
Fort Union contains a thick conglomerate along the north flank of the
Uinta Mountains, and permeabilities in this unit should be good
(Bradley, 1964). The total thickness of the Fort Union generally ranges
from 0 to 2,500 feet, but may be as much as 6,000 feet thick in a
synclinal trough trending northwest through T. 30 N., R. 108 W. (Welder,
1968) .
The average pay zone porosities from 10 oil fields range from 9 to
23 percent. Permeability estimates from the same fields are all less
2
than 1 gpd/ft , corresponding to calculated transmissivities ranging
from <1 to about 20 gpd/ft (Wyoming Geological Association, 1979).
Transmissivities from five other oil field DSTs range from <1 to 180
gpd/ft.
Wasatch Formation
Hydrologic data for the Wasatch Formation is derived from the
records of hundreds of water wells, 16 springs, and several oil wells,
as well as numerous publications by the U.S. Geological Survey and the
Wyoming Geological Association.
In the Overthrust belt, the thickness of the Wasatch Formation
ranges from 2,500 to 3,600 feet, including 1,500 to 2,000 feet of
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sandstone and siltstone in the main body of the Wasatch (Eardley and
others, 1944). The Wasatch of the western Green River basin is 4,100 to
5,250 feet thick. The combined thickness of the basal Chappo and over-
lying La Barge conglomeratic members is 2,700 to 3,500 feet in this
area. In the eastern Green River basin the Wasatch ranges from 0 to
7,200 feet in thickness with up to 7,000 feet of main body member (Lines
and Glass, 1975; Welder, 1968).
Well yields from permeable sandstones, conglomeratic sandstones,
and conglomerates of the Wasatch Formation are generally moderate to
large. Published data on 104 wells indicate a yield range from <1 to
1,300 gpm, though most wells yield less than 500 gpm. In the north half
of the Green River basin, Wasatch wells are less than 1,000 feet deep,
while wells in the southern basin penetrate the Wasatch Formation at
approximately 4,000 feet. Yields of more than 500 gpm may be expected
from wells 2,000 to 5,000 feet deep penetrating thick Wasatch sandstone
sections (Welder, 1968). In the central Green River basin, the Wasatch
grades from predominantly sandstone into a thick intertonguing unit of
low-permeability mudstone and lacustrine limestone of the Green River
Formation.
Data from 62 Wasatch Formation pump tests were collected from the
State Engineer's permit files (Appendix B). Based on these tests,
specific capacities for the Wasatch range from <1 to 14 gpm/ft. Trans-
missivities determined from specific capacities range from 100 to 30,000
gpd/ft; however, most transmissivities greater than 10,000 gpd/ft are •
estimates for wells with negligible drawdown, and therefore are suspect.
The majority are between 200 and 1,000 gpd/ft. Four oil and gas fields
with wells tested in the Wasatch Formation indicate porosities of 20 to
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2
25 percent and permeabilities of <1 to 18 gpd/ft (Wyoming Geological
Association, 1979), corresponding to transmissivity values of <1 to
about 300 gpd/ft.
Green River Formation
The Eocene Green River Formation is not areally extensive in the
Overthrust belt. In the Green River basin, the Green River Formation
consists of three generally recognized members—the Laney Member, the
Wilkins Peak Member, and the Tipton Member.
Of these, the uppermost Laney is the most prolific aquifer,
particularly in the east-central basin, where permeable discontinuous
sandy units interbed with shale and marlstone. In the western and
southern parts of the basin, the Laney is principally low-permeability
marlstone and oil shale.
Hydrologic data were compiled from more than 60 water wells
completed in the Laney Member in the east-central basin (Appendix B).
Yields from the Laney commonly range from 1 to 75 gpm. Specific
capacities from four pump tests on the Laney range from 4 to 150 gpm/ft
with resulting transmissivity estimates commonly less than 1,000 gpd/ft.
One estimate was more than 100,000 gpd/ft.
The Wilkins Peak Member, which directly underlies the Laney
throughout the basin, consists of low-permeability marlstone, shale, and
trona deposits, and commonly yields less than 30 gpm of very poor
quality, sodium-bicarbonate type water. In the south-central basin the
Wilkins Peak deposits are completely impermeable, as evidenced by
unsaturated trona deposits located directly below the Green River.
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In the east-central part of the basin, sandstones in the lowermost
Tipton Member yield between 10 and 170 gpm to nine water wells. One
Tipton sandstone bed is recognizable on electric logs over approximately
4,000 square miles of the basin, but the permeability distribution
within the sandstone is unknown (Welder, 1968). The member is primarily
composed of low-permeability intertonguing oil shale and marlstone.
Based on available data, these Tertiary sediments are most
permeable in the east-central basin, where sandstone occurrence is most
prevalent. The Green River Formation of the south-central Green River
basin is a 2,000 to 2,500 foot thick sequence of nearly impermeable
shale and marlstone. In the western Green River basin, the Green River
Formation has very few thick sandstone beds and yields only small
quantities of water (Lines and Glass, 1975).
Bridger Formation
Along the northern flank of the Uinta Mountains in the southern
Overthrust belt and Green River basin, significant quantities of water
are available from conglomerates in the Bridger. The Bridger Formation
generally crops out in topographically high areas north of the Uintas,
and numerous springs discharging from Bridger outcrops indicate the
formation is well drained (Lines and Glass, 1975). The formation varies
from 500 to 9,600 feet thick (Welder, 1968; Lines and Glass, 1975;
Bradley, 1964) .
Data from 44 Bridger Formation (Green River basin) wells and 9
springs provide all hydrologic and potentiometric surface information.
The only available data for the equivalent Fowkes Formation (Overthrust
belt) are from one spring (T. 19 N., R. 121 W., Sec. 25 aad). Water
well yields are between 2 and 100 gpm from 33 Bridger wells. Specific
69
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capacities from pump tests run on 30 wells have ranged from less than
0.1 to 5.0 gpm/ft. Transmissivities estimated from measured specific
capacities range from 30 to 6,000 gpd/ft, though the majority are
between 500 and 3,000 gpd/ft. Springs issuing from the Bridger and
Fowk.es formations yield 20 to 50 gpm and 125 gpm, respectively.
The availability of water in the sandstones and conglomerates of
the Bridger Formation depends upon "the sorting, saturated thicknesses,
bedding continuity, and degree of fracturing in the thicker shales and
mudstones" (Lines and Glass, 1975). Based on well logs and Lines and
Glass (1975), the lower Bridger is predominantly conglomerate. As the
Uinta Mountains are the source area for these sediments, conglomerate
occurrence and permeability will be greatest in the southwesternmost
part of the Green River basin.
QUATERNARY AQUIFERS
In the Green River basin, Quaternary alluvial and morainal
sediments are present along the southwest flank of the Wind River
Mountains and in the valleys of the Green River and its major
tributaries. The most productive Quaternary aquifers are the alluvium
and gravel outwash deposits, more than 100 feet thick, near Pinedale and
Boulder, along the New Fork River drainage. Here, reported well yields
exceed 500 gpm (Welder, 1968). Yields of less than 50 gpm are common
from finer-grained, less permeable, alluvial and terrace deposits of the
Green River drainage, in the lower Bridger Valley (Robinove and
Cummings, 1963). In the Eden-Farson area, yields to irrigation supply
wells are at least several hundred gpm. Available specific capacity
data from seven wells indicate a range of <1 to 31 gpm/ft, with five of
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the wells less than 2.9 gpm/ft. Transmissivity estimates for the same
five wells range from 320 to 2,000 gpd/ft.
The most productive Quaternary aquifers of the Overthrust belt are
found in the down-faulted valleys of the Bear, Salt (Star Valley), and
Snake rivers, where alluvium and gravel deposits are commonly more than
100 feet thick, and exceed 400 feet near the town of Border in the Bear
River Valley (Robinove and Berry, 1963; Lines and Glass, 1975).
Alluvium in the Bear River Valley is capable of yielding large
quantities of water to wells (more than 400 gpm), particularly where the
full saturated section of valley fill is penetrated. Specific
capacities from pump tests on wells in the Bear Valley alluvium range
from 17 to 56 gpm/ft (Robinove and Berry, 1963). Estimated
transmissivities for these wells range from 1,000 to 65,000 gpd/ft.
Depth to water in alluvium near the center of the Star Valley
rarely exceeds 25 feet; however, along the east side of the valley,
between the towns of Grover and Smoot, water levels may exceed 100 feet
below the ground surface. Perched water zones nearer the surface have
been frequently tapped in that area for unreliable domestic wells (Lines
and Glass, 1975; Welder, 1968). Pump test data from two wells in
alluvium on opposite sides of the Star Valley (T. 31 N., R. 119 W., Sec.
1 dd and T. 31 N., R. 119 W., Sec. 10 ab) provide transmissivity values
of 82,500 and 370,000 gpd/ft, respectively (Walker, 1965).
The average depth to water in the unconfined alluvial aquifer of
the Snake River Valley is usually less than 25 feet and rarely exceeds
50 feet (Lines and Glass, 1975). Well yields from the alluvium and
glacial outwash commonly range between 20 and 100 gpm. Several wells
completed in less permeable morainal sand, silt,' and gravel deposits
71
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near Jackson Lake yield a few to 118 gpra (Cox, 1976). Specific
capacities reported from pump tests on wells in the alluvium range from
<1 to 500 gpm/ft, with most wells between 1 and 50 gpm/ft (Cox, 1976).
Estimated transmissivity values commonly range from 600 to 20,000
gpd/ft.
72
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V. GROUND-WATER CIRCULATION
-------
V. GROUND - WATER CIRCULATION
No previously published regional potentiometric maps are available
for any of the hydrologic units within the Green River basin-Overthrust
belt area. The interpretations and maps presented here are, therefore,
initial attempts in defining ground-water circulation.
The Green River basin and the Overthrust belt are situated in two
separate hydrogeologic environments, due to differing structural frame-
works: complex folding, faulting, and exposure of Paleozoic and
Mesozoic strata in the Overthrust belt; and deeply buried, relatively
undisturbed pre-Tertiary rocks in the Green River basin. The hydraulic
communication between these two areas is severely restricted because of
the large stratigraphic displacement of pre-Tertiary rocks at the
eastern boundary of the Overthrust belt; and because the resultant
displacement has interposed the Baxter-Hilliard aquitard between
Mesozoic-Paleozoic sequences, as shown in Figure II-6b. Thus, the
following discussion will consider ground-water circulation in the
Overthrust belt and in the Green River basin separately.
OVERTHRUST BELT
Due to the development of complex regional structure and intense
fracture zones, ground-water flow within the Overthrust belt is not
definable by the aquifer and aquifer system boundaries previously
established. This is because major faults and fracture zones act as
hydraulic barriers or conduits, which greatly restrict or enhance
horizontal and vertical ground-water flow. The interpretations of
ground-water circulation in the Overthrust belt are therefore organized
74
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into three subsections: (1) highly fractured pre-Hilliard-Baxter
aquifers, (2) post-Hilliard-Baxter Cretaceous and Tertiary aquifers, and
(3) Quaternary aquifers.
Pre-Hilliard-Baxter Aquifers
The shallow (local) ground-water flow direction in the
pre-Hilliard-Baxter aquifers of the Overthrust belt is similar to the
local topographic gradients, whereas the regional flow direction is to
the west-southwest (Plate 3). Both thrust and normal faults impede
regional ground-water flow due to juxtaposition of permeable and
relatively impermeable strata. Although structure commonly hinders
horizontal flow, normal faults often permit vertical flow along
permeable fractures through otherwise relatively impermeable beds. Many
of the larger artesian springs within the Overthrust belt occur along
such faults (Figure V-l; Lines and Glass, 1975).
Although regional ground-water flow patterns are not well known,
the chemical composition of many springs occurring along normal faults
suggests relatively deep circulation. For example, according to Lines
and Glass (1975), the water of near-outcrop Paleozoic limestones is
usually a calcium bicarbonate type, with 100 to 250 mg/1 (milligrams per
liter) dissolved solids. However, along major normal faults within the
sub-basins of the Overthrust area, Paleozoic spring waters are often
rich in calcium sulfate or calcium-sodium sulfate with greater than
1,000 mg/1 dissolved solids, suggesting longer residence times and flow
paths (Plate 4). In addition, there are three thermal spring discharges
in these areas of the Overthrust belt.
The generally southwestern regional flow is also indicated by
specific conductance values in the Frontier aquifer, which increase from
75
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EXPLANATION
SpfinQt ttiylng from
T«rliory Aqviftr
M*u*ard«- Adavilla AquH«f
frontlar Aqutftr
Upptr Juratalc-Lo««r CrtlOCMut Aqgiltrt
MILES
LOMETCftS
l0®* COLORADO
Figure V-l. Location map of pre-Quaternary springs, Green River
basin-Overthrust belt.
76
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a three-well average of 640 ymhos/cm (micromhos per centimeter at 25°C)
at T. 23 N., R. 116 W., to a four-well average of 1,615 ymhos/cm near T.
18 N., R. 117 W.
The large discharges from several low TDS springs in the northern
Overthrust area indicate that most ground-water circulation is local
intrabasin flow. Local ground-water movement, especially in the
northern part of the Overthrust belt, is influenced by near-surface
structure and steep topography, and is often in the opposite direction
from that of regional flow. In the southern part, where there is
relatively little relief, local flow is to the southwest and west,
following the general pattern of regional ground-water movement.
Recharge to the pre-Hilliard-Baxter aquifers is supplied mainly by
snowmelt or rainfall directly onto the outcrop in the northern
mountainous area. In the south, these formations are only locally
exposed, so direct recharge is limited, and where the Hilliard-Baxter
aquitard is present the possibility for interformational flow into the
lower aquifers is low. Discharge is westward from the Overthrust belt,
with possible localized discharge to the Green River basin to the east
(Plate 3).
Post-Hilliard-Baxter Cretaceous
and Tertiary Aquifers
The Evanston, Wasatch, Green River, and Bridger aquifers are highly
utilized sources of ground water within the southern part of the
Overthrust belt, but available potentiometric data are inadequate to
competently define ground-water movement. In the Fossil syncline area
(Figure II-5), the general movement of ground water in the Tertiary
aquifer system is from south to north. This is based on Wasatch and
77
-------
Bridger potentiometric data (Figures V-2 and V-4) and on total dissolved
solids concentration changes (Plate 5). Ground-water movement is
predominantly topographically controlled; artesian conditions are common
only along stream drainage systems (i.e., discharge zones).
Recharge to the post-Hilliard-Baxter formations occurs mainly by
infiltration of rainfall, snowmelt, and ephemeral stream seepage into
surficial outcrops. Much of the discharge is to wells and through
gravity springs and seeps (Lines and Glass, 1975); however, some
discharge flows directly from these strata into alluvial sediments.
Quaternary Aquifers
Quaternary alluvial deposits occur within the Overthrust belt along
the Bear River, Star Valley, and Salt River drainage systems. Ground-
water flow within these areas generally conforms to the topography.
Recharge to these aquifers is supplied by direct infiltration of
precipitation, discharge from Tertiary and older aquifers, and stream
losses in headwater areas. Aquifer discharge occurs via evapotranspira-
tion, ground-water movement into river channels, and discharge to wells.
GREEN RIVER BASIN
Ground-water circulation within the Green River basin is generally
toward the south-center of the basin (Figures V-2, V-3, V-4, and Plate
3). Potentiometric data are inadequate, however, to fully define inter-
formational ground-water movement, especially in the Paleozoic and
Hesozoic aquifers.
The following discussion of ground-water circulation is divided
into two sections. The first section includes all aquifers below the
78
-------
I
Figure V-2. Potentiometric surface map.of the Tertiary Wasatch aquifer,
Green River basin - Overthrust belt.
79
-------
Figure V-3. Potentiometric surface map of the Tertiary Laney aquifer,
Green River basin.
80
-------
I
Potentiomewic Surface Contour q( the
Ter hory Bridqer Aquifer - Dai^ec * nire
mtarrcd, contou' iniiivol 2b0 f«si, dotum
is mton »*c r• wer
Figure V-4. Potentiometric surface map of the Tertiary Bridger aquifer,
Green River basin - Overthrust belt.
81
-------
Hilliard-Baxter aquitard; the second, aquifers above the Hilliard-
Baxter.
Pre-Hilliard-Baxter Aquifers
The availability of potentiometric data for these units is limited
mainly to drill stem test results along the periphery of the basin
(Plate 3). These test results produce computed potentiometric
elevations that are accurate only to about ±400 feet, which provide only
the most general information on ground-water flow. However, because of
the relatively undisturbed structural setting of the basin, these
sedimentary rocks maintain stratigraphic continuity over large areas.
Additionally, large water quality differences occur between some
aquifers (Chapter VI). Ground-water circulation within the basin is
therefore believed to be controlled principally by the relative
permeability characteristics of the rocks.
Based on available potentiometric data, ground-water flow within
these aquifers is from outcrop areas along the La Barge platform and
possibly from the Salt River and Gros Ventre ranges, to the southeast
towards the southern extent of the basin. Additional flow into the
basin may come from the Great Divide-Washakie basins to the east, based
on available potentiometric data for that area (Collentine and others,
1981). Water quality data along the Rock Springs uplift indicate local
upward movement from the Nugget through fractures (?) to overlying
units, eliminating the possibility for deep aquifer recharge along the
structural high. Here the Nugget water quality (4,000 to 10,000 mg/1
TDS, bicarbonate rich) is present in overlying units which regionally
produce high chloride water with 20,000 to 60,000 mg/1 TDS (Collentine
and others, 1981).
82
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Because most outcrop areas are west of the thrust margin, ground-
water flow into the basin is structurally impeded by the resultant
offsetting of beds (see Figures II-5, II-6a, and II-6b). Any flow
contributions into the basin from outcrop areas must therefore be
transferred down through the Upper Cretaceous shales. A similar
hydraulic problem exists within the basin for downward movement from
Tertiary aquifers. The very flat potentiometric gradients and highly
saline waters (Chapter VI) within the basin further indicate that the
amount of flow in these aquifers is small, and that circulation is very
restricted.
A discharge mechanism or area for these aquifers cannot be
identified from available data. This is because the Tertiary aquifer
-system potentiometric elevations are consistently higher than in
underlying aquifers, in areas where data exist. It is possible that the
principal discharge area is in the southern part of the basin, where no
potentiometric data are currently available.
Post-Hilliard-Baxter Aquifers
Ground-water movement within the Upper Cretaceous, Tertiary, and
Recent aquifers in the Green River basin is better understood because of
a greater availability of data, little structural disturbance of sedi-
ments, and reasonably good stratigraphic control. Discussion of
ground-water circulation in the post-Hilliard-Baxter aquifers is divided
into three sections: the Mesaverde aquifer, the Tertiary aquifer
system, and the Quaternary aquifers.
83
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Mesaverde Aquifer
Ground-water movement in the Mesaverde aquifer is from north to
south along the west side of the Rock Springs uplift, and from the axis
of the uplift westward, based on sparse water well and spring potentio-
metric elevation data. On the west side of the Green River basin
potentiometric elevations and water quality data for the Mesaverde are
not available.
The Mesaverde aquifer is in hydraulic connection with the overlying
Tertiary aquifer system in the southwestern Green River basin due to the
absence of the Lewis Shale aquitard in that area; however, the absence
of potentiometric and water quality data precludes any delineation of
vertical ground-water movement.
Recharge to the Mesaverde aquifer occurs primarily along the west
flank of the Rock Springs uplift by direct infiltration of precipitation
on outcrop areas and by seepage losses from streams. Discharge in the
form of springs, seeps, and water supply wells occurs at lower
elevations on the west side of the uplift. Central basin flow is not
known.
Tertiary Aquifer System
Potentiometric maps (Figures V-2, V-3, and V-4) produced for the
Wasatch Formation, the Laney Member of the Green River Formation, and
the Bridger Formation, respectively, indicate ground-water circulation
is primarily from outcrop-related recharge areas along the foothills of
the Wind River and Gros Ventre ranges, toward the center of the Green
River basin and southward (Figure V-5). This movement is in agreement
with Wasatch ground-water quality patterns which show increases in TDS
from outcrop areas, basinward and to the south (see Chapter VI).
84
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Northern Green River Basin
Southern Green River Basin
explanation
— Represent* ground-woitr
Ho* polh
• Represents southerly horuoniol
Mo» through the Green River
Bonn
""**) Zones of very low permeoblhty
Figure V-5. Idealized diagram of ground-water flow within the Tertiary
quifer system, Green River basin (after Roehler, 1974 and
Sullivan, 1980).
85
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Additional movement in the southwestern part of the Green River basin is
south to north from recharge areas along the north flank of the Uinta
Mountains.
In general, Tertiary potentiometric contours converge along the
Green River drainage, indicating a major discharge area for the system.
However, available data indicate no upward gradient in the Tertiary
aquifers near the Green River, as would be expected in a discharge zone.
Vertical movement of ground water along the drainage in the south-
central basin is virtually impossible because of the impermeable
marlstone and shale beds in the Wilkins Peak Member of the Green River
Formation.
Areas where interformational communication is possible are along
the basin fringes where the Laney Member directly overlies the Wasatch,
and the Wilkins Peak and Tipton members are thinnest. Communication
probably also exists between the basal Lance and overlying Wasatch,
because of the lack of thick regional intervening shales.
Ground-water movement in the Miocene-Pliocene formations of the
Tertiary aquifer system is difficult to decipher from the sparse
potentiometric data. The conglomeratic units are well-drained, as
evidenced by seven Bishop Conglomerate springs along the west flank of
the Rock Springs uplift and in T. 13 N., R. 112 W. The direction of
ground-water movement is most likely controlled by the topography of the
drainage basin in these unconfined aquifers.
Tertiary aquifer system recharge occurs via outcrop-related infil-
tration of precipitation, snowmelt runoff from the mountains, and in
some areas seepage from tributary streams of the Green River. Minimal
86
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recharge occurs to outcrop areas in the Green River basin away from the
uplifts because of high evaporation and low precipitation (Welder,
1968).
In areas of heavy irrigation, particularly the Eden-Farson area,
some recharge may occur through alluvial deposits into the underlying
Tertiary aquifers (Welder, 1968).
Minor discharge from the Tertiary aquifer system occurs through
numerous small saline springs issuing from the Wilkins Peak and Tipton
members of the Green River Formation, from the Bishop Conglomerate in
the southeastern corner of the basin near the Rock Springs uplift, and
from the Laney member in the Eden-Farson area. Some local discharge
also occurs in the north-central basin, where the potentiometric surface
of the Tertiary system reflects the local topography and is several
hundred feet above the level of the Green River (Gordon and others,
1960). It is expected that regional discharge occurs mainly to the
south of the area covered by well and spring data where the Wilkins Peak
Member is partially absent (Figure V-5).
Quaternary Aquifers
Ground-water movement in alluvial deposits along the major
perennial streams of the Green River basin is generally downgradient and
toward the stream channel, based on water quality degradation in these
directions (Chapter VI). Water quality data also indicate ground-water
movement south from the foothills of the Wind River Mountains within
thick morainal and gravel deposits.
Recharge to the alluvial and glacial aquifers is by direct seepage
of precipitation and stream water, and local discharge from bedrock
87
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aquifers. Discharge occurs via seeps and springs into perennial
streams, and by downward drainage into underlying conglomerates of the
Tertiary aquifer system in stream headwater areas.
88
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VI. WATER QUALITY
-------
VI. WATER QUALITY
Water quality data from approximately 800 wells and springs in the
Green River basin and Overthrust belt were used in the preparation of
this report. Most data are for constituents without primary or
secondary drinking water standards (sodium, potassium, calcium,
magnesium, bicarbonate, carbonate). In contrast, many constituents with
standards, including the heavy metals, organic chemicals, and
radionuclear species, have little or no water quality data. Only total
dissolved solids (TDS), sulfate, fluoride, and nitrate have associated
drinking water standards and enough water quality data to delineate
areas of high concentrations.
Approximately two-thirds of the water quality data within the study
area were collected and published by the U.S. Geological Survey.
Another large data base was provided by the Wyoming Department of
Agriculture laboratory in Laramie. Crawford (1940) and Crawford and
Davis (1962) reported on water quality in oil field waters. Additional
water quality data were supplied by the U.S. Environmental Protection
Agency, the Bureau of Land Management, the Department of Energy, and the
Water Resources Research Institute (WRRI). All water quality data used
in this report have been stored on WRRl's computerized Water Resources
Data System (WRDS). Data collected by WRRI during this project are
included in Appendix D.
GENERAL WATER QUALITY
This section describes the changes in general water quality
character within the aquifers of the area. This general water quality
90
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is defined by the relative concentrations of the major species in
solution.
Precambrian through Upper Cretaceous Units
Approximately 150 wells or springs in the Precambrian through Upper
Cretaceous units provide water quality data. TDS data for these units
are plotted on Plate 4. The data fall principally into three groups.
One group of data is from wells scattered through the Overthrust belt.
These wells generally produce water of a quality suitable for drinking,
according to the National Interim Primary Drinking Water Regulations
(U.S. Environmental Protection Agency, 1976). The second group of data
is from oil- and gas-bearing strata in the central part of the Green
River basin, and generally describe extremely poor quality water. The
third group of data is from oil- and gas-bearing strata along the Rock
Springs uplift, and describe poor to extremely poor quality water.
The data along the Overthrust belt are distributed among at least
12 formations. Waters from most wells have a low salinity and a
calcium-bicarbonate composition. This high quality water is a result of
relatively low solubility salts in the rocks and faulting and fracturing
which greatly enhance local circulation.
The few cases of poor quality water in the Overthrust belt include
several Madison springs south of Jackson, two Preuss springs in the Star
Valley, a Phosphoria spring, a Hilliard spring, and several Frontier
wells in the southern part of the Overthrust belt. The quality of these
waters is identified on the trilinear diagram in Figure VI-1. These
cases probably reflect poor ground-water circulation in the Phosphoria
and Hilliard formations and regional ground-water movement in the
Madison, Preuss, and Frontier formations.
91
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AQUIFER
Total Dissolved Solids(mg/l)
O < 500
~ 500-3000
© 3000-10,000
Kh
Kf
Jp
Pp
Hil liard
Frontier
Preuss
Phosphoria
Figure VI-1.
Mm Madison
Typical water composition, all aquifers.
I I
\
Major ion composition of waters frorp the Precambrian through Upper
Cretaceous aquifers, Overthrust belt (numbers plotted are percentages
of total milliequivalents per liter).
92
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The data from the central part of the Green River basin provide
water quality information on the "Muddy" Sandstone and the "Dakota"
Sandstone within the Bear River Formation. The water is highly saline,
with TDS concentrations varying from 10,000 to 55,000 mg/1. The general
water quality character is sodium chloride.
Data from the Rock Springs uplift indicate considerable differences
in water quality between the Nugget and four other formations. Twelve
Nugget samples have TDS concentrations between 4,000 and 10,000 mg/1 and
a sodium chloride-bicarbonate character. Thirteen samples from the
younger Frontier and Dakota aquifers indicate TDS concentrations between
30,000 and 60,000 mg/1 and a sodium chloride enrichment. Thirteen
samples from the older Phosphoria and Weber-Tensleep aquifers have TDS
concentrations between 12,000 and 40,000 mg/1 with a sodium
sulfate-chloride character at lower concentrations and sodium chloride
character at higher concentrations. The lower TDS and different water
quality character in the Nugget suggest that no regional interforma-
tional flow across the Nugget occurs in the Rock Springs uplift.
A few water quality data are also available on the Mesaverde
aquifer along the Rock Springs uplift. TDS concentrations increase
southward from approximately 300 mg/1 to more than 7,000 mg/1, and the
chemistry suggests a southerly flow in the aquifer. The water is
predominantly calcium-magnesium sulfate.
Tertiary Aquifer System
Approximately 500 sites have water quality data available to
describe water quality patterns within the Tertiary aquifer system. TDS
data are plotted on Plate 5. Most of the data are from the Fort Union
aquifer, the Wasatch aquifer, the Wilkins Peak and Laney aquifers within
93
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the Green River Formation, and the Bridger aquifer. The data show wide
interformational and intraformational variations in both TDS and the
composition of the waters.
Most of the water quality sampling of the Fort Union aquifer has
occurred in the Evanston area in the southwestern corner of the basin.
The Fort Union waters range from 200 to 1,500 mg/1 in TDS and tend to be
sodium-magnesium bicarbonate rich. The more saline waters are enriched
in sulfate.
Water quality data on the Wasatch aquifer are concentrated in the
northeastern part of the Green River basin and in the Evanston area.
The TDS concentrations vary from 100 to 6,600 mg/1 in the northeastern
portion of the basin and from 200 to 800 mg/1 in the Evanston area.
Dissolved solids increase downgradient (south and west) in the
northeastern part of the basin. A 500 mg/1 contour is drawn on Plate 5
to delineate where Wasatch waters begin to exceed the secondary drinking
water standard for TDS. The major ion composition changes from calcium
bicarbonate to sodium bicarbonate to sodium sulfate in a downgradient
direction, as illustrated on the trilinear diagram in Figure VI-2. The
most dramatic changes in TDS and major ion composition occur where the
Wasatch intertongues with the Laney, and may reflect movement of Laney
waters into the Wasatch.
The waters within the Wasatch near Evanston show the same pattern
described above. The water tends to have TDS concentrations below 500
mg/1 and a calcium bicarbonate composition near the recharge area. The
salinity increases and the major ion composition changes to sodium
bicarbonate and then sodium sulfate downgradient (north and east) from
94
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Total Dissolved Solids (mg/l)
O 0-500
~ 500-3000
© 3000-10,000
Figure VI-2. Major ion composition of waters from the Wasatch aquifer Green
River basin (numbers plotted are percentages of total
millequivalents per liter).
95
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the recharge area. The same trends also occur with depth in this
region.
Water quality varies greatly in the Green River Formation because
of the discontinuous lenticular nature of the water-bearing zones.
Typical water quality is illustrated on Figure VI-3. TDS concentrations
in the Wilkins Peak aquifer range from 7,000 to more than 100,000 mg/1,
with most concentrations exceeding 30,000 mg/1. The composition of the
waters is sodium bicarbonate or sodium carbonate. Water in the Laney
aquifer of the Green River Formation has been monitored principally in
the Big Sandy region. TDS concentrations in the Laney aquifer range
from 2,000 to 7,000 mg/1. The major ion composition is typically sodium
sulfate, although calcium is frequently present in significant
percentages. The highly saline waters in the Green River Formation are
attributable principally to evaporite deposits laid down during the
existence of ancient Lake Gosiute.
Water quality data on the Bridger aquifer are concentrated in the
Bridger Valley, although a few samples from the Bridger have been taken
in the Big Sandy area. Typical water quality is shown on Figure VI-3.
TDS concentrations vary from 400 to 5,000 mg/1 and exhibit no clear
trend with gradient or depth. The figure illustrates the wide variation
in major ion composition within the Bridger aquifer.
Quaternary Aquifers
The Quaternary wells are principally concentrated in the alluvium
along the major perennial streams. Approximately 200 sites with water
quality data are available on Quaternary aquifers. TDS data are plotted
on Plate 6. These data describe waters which degrade in a downstream or
downgradient direction but which generally remain chemically suitable
96
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AQUIFER
Total Dissolved Solids(mg/l)
O < 500
~ 500-3000
® 3000-10,000
® >10,000
Figure VI-3. Major ion composition of waters from the Bridger, Laney, and
Wilkins Peak aquifers, Green River basin (numbers plotted are
percentages of total milliequivalents per liter).
97
Tb Bridger
Tgw Wilkins Peak
Tg I Laney
-------
for drinking, according to the U.S. Environmental Protection Agency
(1976).
The IDS concentrations in the alluvium of the Overthrust belt vary
from approximately 200 mg/1 in the headwaters of the perennial streams
to 300-500 mg/1 downstream at the border of the study area. Calcium and
bicarbonate are the dominant ions in most of the alluvial waters.
TDS concentrations in the alluvium of the Green River basin exhibit
the same patterns as those in the alluvium of the Overthrust belt.
Concentrations increase from 100-200 mg/1 in the headwaters to 700 mg/1
along the Green River and almost 1,000 mg/1 along the Blacks Fork.
Composition is calcium bicarbonate in the headwaters, and becomes
enriched in sodium and sulfate downstream.
PRIMARY STANDARDS
The U.S. Environmental Protection Agency has assigned primary
drinking water standards to ten inorganic constituents, six organic
constituents, and four radionuclear species in order to protect users
from toxic chemical concentrations in their drinking water supplies.
These standards are listed on Table VI-1. Laboratories require special
equipment to analyze the organic constituents and radionuclear species
and their environmental importance has only recently become known;
therefore, no data are available on the organic constituents and only a
few samples have included the analysis of radionuclear species.
Fluoride and nitrate, two of the inorganic constituents with primary
standards, have been widely monitored and areas of excessively high
fluoride concentrations have been noted in the Tertiary aquifer system.
The remaining eight inorganic constituents with standards have received
98
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Table VI-1. Drinking water quality standards.
Constituent
Primary Drinking
Water Standard
Secondary Drinking
Water Standard
Arsenic
Barium
Cadmium
Chloride
Chromium
Coliform Bacteria
Color
Copper
Corrosivity
Fluoride
0.05
1.
0.01
0.05
1 colony/100 ml^
2.0
250
15 color units
1.
Noncorrosive
Foaming Agents
Iron
Lead 0.05
Manganese
Mercury 0.002
Nitrate (as N) 10.
Odor
Organic Chemicals-Herbicides
2.4-D 0.1
2,4,5-TP 0.01
Organic Chemicals-Pesticides
Endrin 0.0002
Lindane 0.004
Methoxychlor 0.1
Toxaphene 0.005
PH
0.5
0.3
0.05
3 threshold odor units
6.5-8.5 units
Radioactivity
Ra-226 + Ra-228
Gross Alpha Activity
Tritium
Sr-90
Selenium
Silver
Sodium
Sulfate
Total Dissolved Solids
5 pCi/1
15 pCi/16
20,000 pCi/1
8 pCi/1
0.01
0.05
f
250
500
99
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Table VI-1. (continued)
Primary Drinking Secondary Drinking
Constituent
Water Standard Water Standard
Turbidity
1 turbidity unit®
Zinc
5.
All concentrations in mg/1 unless otherwise noted.
The standard is a monthly arithmetic mean. A concentration of 4 colonies/
100 ml is allowed in one sample per month if less than 20 samples are
analyzed or in 20 percent of the samples per month if more than 20 samples
are analyzed.
The corrosion index is to be chosen by the State.
^The fluoride standard is temperature-dependent. This standard applies to
locations where the annual average of the maximum daily air temperature
is 58.4°F to 63.8°F.
The standard includes radiation from Ra-226 but not radon or uranium.
^No standard has been set, but monitoring of sodium is recommended.
£
Up to five turbidity units may be allowed if the supplier of water can
demonstrate to the State that higher turbidities do not interfere with
disinfection.
SOURCE: U.S. Environmental Protection Agency, 1976.
100
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little attention in the area and very little data are available to
define areas of high and low concentrations.
Fluoride
The fluoride standard is based upon the annual average of the
maximum daily area temperature. The standard is set at 2.2 mg/1 in most
of the Green River basin-Overthrust belt, but increases to 2.4 mg/1 in
the northeastern and extreme southwestern parts.
Fluoride has been measured in over 400 wells, usually by a single
sampling. Approximately one-fourth of all wells sampled for fluoride
have exceeded the standard. Fluoride concentrations are generally 0.5
mg/1 or less in the remaining wells sampled for fluoride. Most fluoride
data are from the shallow bedrock and alluvial aquifers.
Fluoride has been measured at 90 sites in the Precambrian to Upper
Cretaceous aquifers, most frequently in the Overthrust belt. Fluoride
concentrations exceeding the standard appear to be associated with oil
field brines in these aquifers. Samples from the oil and gas fields
along the Rock Springs uplift frequently contain fluoride in excess of
the standards. No fluoride data are available on the highly saline oil
and gas field waters toward the center of the basin; but high
concentrations of chloride, another halide, suggest the likelihood of
high fluoride concentrations in these waters. Only one fluoride
concentration exceeding the standard has been detected in samples from
the Overthrust belt.
The Tertiary aquifer system has been sampled at 215 sites for
fluoride, and approximately 34 percent of the Tertiary wells have
fluoride concentrations exceeding the standard. Locations of the wells
are shown in Figure VI-4. Most excessively high fluoride concentrations
101
-------
43°-
TETON
. Jackson
FLUORIDEi mg/l) HI TP ATE {mg/l) AQUIFER
A BRIDGER
0 O LANEY
I 7-270
SUBLETTE
WILKINS PEAK
WASATCH
Range of concentration (mg/l) at
wel Is
Number of wells at location where
Primary Drinking Water Stand-
ard i s exceeded.
30 miles
—I
48km.
1
42°
LINCOLN
e Pinedole
3.2^7 ?
3
^.0T-
y 4.0
^7 33
O
07.4
— q2.3_
26 7.7 5.8 4 1
8 8% $5^15
- jO 8896.!o°8^}|,63
7-2TOD8.6Q|5 2l?2nQ>^:14
8.2-310
w8.6 ^ID 12/-sO
o^s5i2
3e^^894,?\?» o\.9
47 "=47
1.7-450
SWEETWATER
l
I ! 8 I 041
I I ^018
ROCK SPRINGS BI9C
0.4-160(6)
31-157(7)
BS (4) 13-28
~ (13)0-280
724
.30
Evonston UINTA
2Ia ^7 3.8
A 32
4,.-L£
I
III"
27
110°
109°
Figure VI-4.
Nitrate and fluoride concentrations exceeding the primary
drinking water standards in the Tertiary aquifer system.
102
-------
have been detected in the Laney shales within the Big Sandy drainage and
at the Department of Energy's (DOE) oil shale wells. Other high
concentrations have been detected in the Wasatch aquifer, principally
where it intertongues with the Laney aquifer, and in the Wilkins Peak
aquifer toward the center of the Green River basin. These fluoride
data, along with information on major ion composition and potentiometric
levels, indicate that water may be moving from the Laney into the
Wasatch and Wilkins Peak aquifers in certain parts of the Green River
basin.
Maximum concentrations are 450 mg/1 in the Big Sandy drainage, 280
mg/1 at the DOE wells, and 15 mg/1 at the Wasatch wells. Most Tertiary
wells have been sampled once for fluoride. However, the DOE wells west
of Rock Springs and three wells in the Big Sandy drainage have been
sampled more often, and fluoride concentrations at most of these wells
have varied by more than two orders of magnitude over time. The
dramatic changes in fluoride concentrations are not paralleled by
changes in other constituents, however. Therefore, the fluoride
variations may be due to imprecise analyses in the laboratories.
Three of 120 fluoride measurements in the Quaternary aquifers
exceed the standard. One of these, in the Overthrust belt south of
Jackson, is marginally above the standard. The other two excessively
high concentrations are between Pinedale and Farson, and are correlated
with similarly high concentrations in the underlying Tertiary aquifers.
Nitrate
Nitrate has been monitored nearly 700 times in the Green River
basin-Overthrust belt, and approximately 4 percent of the nitrate values
exceed the water quality standard of 10 mg/1 as nitrogen. Twenty-six of
103
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the 30 nitrate concentrations exceeding the standard are recorded in the
Tertiary aquifers. The rest occur in the alluvium near Evanston.
Locations of high nitrate concentrations in the Tertiary aquifers are
identified on Figure VI-4.
The high nitrate concentrations are confined to areas that are
heavily irrigated and contain septic tanks. Failing septic tanks due to
high ground-water levels are a possible source for the nitrate.
Occasionally high nitrate concentrations are also recorded at the DOE
oil shale wells west of Rock Springs. However, the high values probably
reflect analytical problems with standard methods of laboratory analysis
for nitrate (Fox and others, 1978) . It is unlikely that any nitrate
exists in the highly reducing environments monitored by the DOE wells.
Other Constituents with Primary Standards
The other constituents with primary water quality standards have
been monitored infrequently or not at all. Approximately 50 to 60
analyses are available for each of the eight inorganic constituents
besides fluoride and nitrate, and two-thirds of these have been
collected by DOE at their oil shale wells west of Rock Springs and in
the Big Sandy drainage. No ground-water data exist for the organic
constituents with primary drinking water standards, while 20 analyses of
radionuclear species have been done.
Each of the inorganic constituents has been analyzed four to six
times in the Precambrian to Upper Cretaceous aquifers, and no standards
are exceeded. Fewer than ten analyses of each inorganic constituent
have been made in the Quaternary aquifers. One arsenic analysis and one
selenium analysis, both in the upper part of the Big Sandy drainage,
exceed the standards. Another Quaternary analysis of selenium less than
104
-------
one mile away shows no selenium present. No other Quaternary analyses
of arsenic were taken in the area of the high value.
Most analyses of inorganic constituents with primary standards
besides fluoride and nitrate have been conducted on the Tertiary ground
waters, and over half of these have been at DOE oil shale wells east of
Rock Springs and in the lower Big Sandy drainage.* These wells
penetrate the Laney and Wilkins Peak aquifers of the Green River
Formation as well as the Wasatch aquifer. In most cases, more than one
sample was taken at each well and concentrations vary from below
detection limits to values exceeding the standard. The frequency of
concentrations exceeding the standard at the DOE wells is: selenium, 26
of 36; cadmium, 18 of 33; mercury, 13 of 31; arsenic, 11 of 28; lead, 8
of 27; barium, 3 of 31; silver, 1 of 22; and chromium, 1 of 26. Recent
work (Fox and others, 1978) on oil shale process waters indicates
apparently high concentrations of these eight inorganic constituents,
although it documents considerable inaccuracy and imprecision in the
analysis of oil shale waters for these constituents.
Fifteen samples were collected from the Tertiary aquifer system
during the course of this project and analyzed for the constituents with
primary standards and other important water quality parameters. One
sample from the Wasatch aquifer had a lead concentration (0.06 mg/1)
exceeding the standard, and another sample also from the Wasatch aquifer
had a selenium concentration (0.02 mg/1) exceeding the standard. Both
of these were marginally above the standards and isolated instances in
unusually saline Wasatch waters.
*The DOE data must be used with discretion, because the water
quality described by the data reflect specialized conditions which exist
in oil shales during and after retorting.
105
-------
The radionuclear species with water quality standards were
monitored in 20 samples principally from the Tertiary aquifer system.
Radionuclides were detected in all samples except one, but only one
Frontier sample from the extreme southwestern part of the project area
had concentrations exceeding the standard. In that sample, the gross
alpha concentration of 23 pCi/1 exceeded the standard of 15 pCi/1.
Uranium was widely monitored by DOE in the Green River basin—
Overthrust belt, and 21 analyses were above the background
concentrations of 10 yg/1. Five of these analyses were in the
Quaternary aquifers, and the remaining 16 high uranium concentrations
were in the Tertiary aquifer system. More than half of the high
concentrations occurred at DOE's oil shale wells into the Tertiary
aquifer system west of Rock Springs and in the Big Sandy drainage. The
remainder of the high uranium concentrations are marginally above the
background concentrations and are scattered across the lower Green River
basin.
SECONDARY STANDARDS
Several chemical constituents such as sulfate and total dissolved
solids are assigned secondary standards by EPA because they cause
aesthetic problems with drinking water. Secondary drinking water
standards are listed on Table VI-1. Many Wyoming localities have
adjusted to drinking waters which exceed one or more of these secondary
standards because no better drinking water is economically available.
This section delineates those regions in the Green River basin—
Overthrust belt where concentrations exceeding a secondary standard have
been reported. Most of the high concentrations occur in the Tertiary
aquifer system.
106
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Total Dissolved Solids
Total dissolved solids were monitored at over 850 wells and springs
in the Green River basin-Overthrust belt, and concentrations have been
found to vary from less than 100 mg/1 at some sites on the western
border to more than 100,000 mg/1 in the Tertiary aquifer system of the
eastern Green River basin. Concentrations exceeding the secondary
standard of 500 mg/1 are principally confined to oil field waters and
the Tertiary aquifer system.
Total dissolved solids were measured in almost 200 Precambrian to
Upper Cretaceous wells, primarily in the Overthrust belt and at several
oil fields in the central Green River basin. TDS data in these aquifers
are plotted on Plate 4. All measured TDS concentrations in the
Overthrust belt are less than 3,000 mg/1, and most are less than the
secondary standard of 500 mg/1. The few exceptions were identified in
an earlier section on major ion composition (p. 91) and represent water
samples from the Madison, Preuss, and Frontier aquifers.
In contrast to the nonsaline waters in the Overthrust belt, the
salinity exceeds 3,000 mg/1 in three oil and gas areas in the central
and eastern Green River basin, and frequently exceeds 10,000 mg/1.
Fourteen of 28 samples taken from the Bear River aquifer in the region
of the La Barge platform exceed 10,000 mg/1 TDS. Five samples from the
Bear River aquifer east of Bridger Valley exceed 10,000 mg/1 TDS. Data
along the Rock Springs uplift show TDS concentrations exceeding 10,000
mg/1 in the Dakota, Phosphoria, Tensleep-Weber, and Madison aquifers.
In contrast, concentrations in the Nugget aquifer system range between
4,000 and 10,000 mg/1.
107
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Total dissolved solids have been analyzed at nearly 500 locations
in the Tertiary aquifer system. Concentrations exceeding 500 mg/1 are
widespread, as shown on Plate 5. The Tertiary waters with salinities
less than 500 mg/1 are confined to the Overthrust belt and the northern
part of the Green River basin, and are principally associated with the
Wasatch aquifer. The waters in the Wasatch aquifer in the northern part
of the basin become increasingly saline downgradient, and a 500 mg/1
contour on Plate 5 defines where the Wasatch waters tend to exceed the
secondary standard for salinity.
Tertiary waters in the Wilkins Peak and Laney aquifers of the Green
River Formation and the Bridger aquifer typically exceed the secondary
standard for total dissolved solids. Wilkins Peak aquifer was monitored
for salinity in the Big Sandy drainage and at the DOE oil shale wells
west of Rock Springs, and salinity is greater than 3,000 mg/1 and
frequently greater than 10,000 mg/1 in these regions. The Laney aquifer
was monitored principally in the Big Sandy drainage; the salinity tends
to range from 500 to 3,000 mg/1 in the upper drainage, and increases to
between 3,000 and 10,000 mg/1 in the lower drainage. The Bridger
aquifer was monitored principally in the Bridger Valley, and total
dissolved solids typically are less than 500 mg/1 near the Utah border
but increase to 500 to 3,000 mg/1 downgradient.
Total dissolved solids were monitored at over 200 locations in the
Quaternary, and salinity concentrations rarely exceed the secondary
standard of 500 mg/1. Two regions where salinity typically ranges from
500 to 1,000 mg/1 are along the Green River between Fontenelle Reservoir
and the confluence with the Big Sandy River and along the lower part of
108
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the Blacks Fork. Both regions of relatively high salinity are probably
caused by discharge of saline Tertiary waters to the alluvium.
Sulfate
Sulfate was monitored at approximately 850 locations in the Green
River basin, and exceeds the secondary standard of 250 mg/1 in about 30
percent of these locations. Many of these excessively high
concentrations occur in the Tertiary aquifer system, although some high
concentrations of sulfate have also been found in both the Quaternary
and Precambrian to Upper Cretaceous aquifers.
Sulfate was monitored at about 120 locations in the Precambrian to
Upper Cretaceous aquifers, and exceeds the standard at approximately 5
percent of the locations. The high sulfate waters are scattered in six
different formations in the Overthrust belt and the Tensleep-Weber,
Dakota, Phosphoria, and Mesaverde aquifers along the Rock Springs
uplift.
Almost half of the 500 Tertiary wells showed sulfate concentrations
which exceeded the standard. Regions of high sulfate are delineated on
Figure VI-5. The Wasatch aquifer had the lowest percentage
(approximately 20 percent) of excessively high sulfate concentrations.
However, sulfate concentrations tend to increase downgradient in the
Wasatch aquifer in the northern part of the Green River basin, and
generally exceed the secondary standard where the total dissolved
concentrations also exceed the standard. Another region of high
sulfates within the Wasatch aquifer was reported at the DOE wells near
Rock Springs.
Approximately 70 percent of the wells in the Wilkins Peak and Laney
aquifers of the Green River Formation and 60 percent of the wells in the
109
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43°-
42® —
EXPLANATION
A Bridger Aquifer
O Loney Aquifer
Wilkins Peak Aquifer
~ Wasatch Aquifer
T Tertiary Aquifer System undivided
A ^^ Sulfate concentration in mg/1
(28) Number of welts m outlined area
exceeding the standard.
30miles
H
48km
4l°—1
110°
109®
Figure VI-5. Sulfate concentrations exceeding the secondary drinking
water standard in the Tertiary aquifer system.
110
-------
Bridger aquifer have waters where sulfates exceed the standard. The
data on the Green River Formation waters come from the Big Sandy
drainage and the DOE oil shale wells west of Rock Springs, while most of
the Bridger data come from the Bridger Valley. Sulfate concentrations
tend to increase downgradient in both the Big Sandy drainage and the
Bridger Valley. Most sulfate concentrations in the Big Sandy drainage
exceed 1,000 mg/1, while the high sulfate concentrations in the Bridger
Valley are about equally divided between the 250-1,000 mg/1 range and
the greater-than-1,000 mg/1 range.
Approximately 7 percent of the Quaternary wells have sulfate
concentrations in the water which exceed the sulfate standard. Most of
the excessively high concentrations occur in the alluvium along the Big
Sandy River and the perennial streams in the Bridger Valley, where
saline Tertiary ground waters or saline surface waters may recharge the
alluvium. The remaining high sulfate concentrations are isolated cases
scattered through the rest of the basin, where relatively saline waters
in underlying bedrock, formations discharge to the alluvium along
perennial streams.
pH
The pH has been monitored frequently in the Green River basin, and
while no pH values below the secondary standard of 6.5 have been
measured, pH values above the secondary standard of 8.5 are widespread
and tend to be associated with high concentrations of sodium bicarbonate
or sulfate salts in the Tertiary aquifer system. The pH has been
monitored about 20 times in the Quaternary aquifers, about 800 times at
100 locations in the Tertiary aquifer system, and about 35 times in the
Precambrian to Upper Cretaceous aquifers.
Ill
-------
No excessively high pH values are reported in the non-Tertiary
aquifers. However, more than half of the Tertiary wells sampled for pH
have exceeded the secondary standard. One region of pH 9.0 occurs in
the Wasatch aquifer near Big Piney. This region corresponds to an area
of total dissolved solids exceeding 500 mg/1 and principally sodium
bicarbonate and sulfate waters. A second concentration of high pH
values occurs in the DOE oil shale wells in the lower Big Sandy drainage
and west of Rock Springs. The excessively high values have been
detected in the Wasatch aquifer and the Laney and Wilkins Peak aquifers
of the Green River Formation. Approximately half of these high values
in the Wasatch aquifer and nearly all high values in the Wilkins Peak
aquifer in the Big Sandy drainage have exceeded a pH of 10.0, and these
samples are typified by saline sodium-carbonate water. Thirteen DOE
wells west of Rock Springs into the Laney and Wilkins Peak aquifers have
shown pH values fluctuating from well below the standard to 12.8. A
large number of recorded pH values exceed 10.0. These waters are also
principally sodium carbonate and highly saline.
Chloride
Chloride has been monitored at about 180 sites in the Green River
basin, and several chloride concentrations exceeding the secondary
standard (250 mg/1) were recorded. Most of the chloride monitoring has
taken place in the Tertiary aquifers, where chloride is reported in
approximately 350 samples at approximately 70 locations. Chloride has
also been measured approximately 100 times in the Quaternary aquifers
and approximately 180 times in the Precambrian to Upper Cretaceous
aquifers.
112
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Chloride concentrations exceeding the secondary standard occur
frequently in the Precambrian to Upper Cretaceous aquifers within oil-
and gas-bearing areas. Chloride concentrations reach 10,000 mg/1 and
greater in these brines. In contrast, chloride concentrations in
nonpetroleum areas do not exceed the standard and are typically less
than 20 mg/1.
Chloride concentrations exceeding the secondary standard are
reported at almost half the Tertiary wells monitored for chloride. A
Wasatch well and a Bridger well near the confluence of the Blacks Fork
and Smiths Fork have waters with approximately 300 mg/1 chloride;
however, Wasatch and Bridger waters from other wells in the same area
have chloride concentrations between 50 and 100 mg/1. Widely varying
but infrequently high chloride concentrations are reported at DOE wells
in the lower Big Sandy drainage and west of Rock Springs. Wasatch
waters in the Big Sandy drainage have chloride concentrations less than
500 mg/1, while Wilkins Peak and Laney waters in both regions are
usually greater than 500 mg/1 and exceed 8,000 mg/1 in several wells
west of Rock Springs.
Iron
Iron has been monitored at approximately 110 sites in the Green
River basin. As with the other constituents, the Tertiary aquifer
system has been monitored most frequently for iron, where 120 iron data
exist from approximately 50 locations. Iron has also been measured
about 80 times in the Quaternary aquifers and about 80 times in the
Precambrian to Upper Cretaceous aquifers.
Eight iron concentrations exceeding the standard (0.3 mg/1) are
reported in the Quaternary aquifers at locations in the Bridger Valley,
113
-------
near Evanston, and near Jackson. The three values in the Bridger Valley
are not supported by other iron data in the same vicinity, and so the
high values may be caused by contamination from well casings, pipes, or
other sources. The five high concentrations in the Overthrust belt vary
from 0.7 to 7.5 mg/1, and may be caused by upwelling from the Madison
aquifer near Jackson and possibly from the Wasatch aquifer near
Evanston. The only iron data from the Precambrian to Upper Cretaceous
aquifers which exceed the secondary standard are three results of 0.4 to
0.7 mg/1 from Madison wells near Jackson and one of 0.6 mg/1 from a
Hilliard well near Evanston.
Iron concentrations exceed the secondary standard at approximately
one-quarter of the Tertiary wells. Excessively high concentrations have
been most frequently measured at DOE oil shale wells in the lower Big
Sandy drainage and west of Rock Springs and at other wells in the lower
Big Sandy drainage. Most of these wells tap the Wilkins Peak aquifer.
A few high concentrations have also been found in the Laney aquifer in
the lower Big Sandy drainage and in the Wasatch aquifer near Evanston.
Concentrations at most DOE wells vary by several orders of magnitude,
and reflect differing pH and oxidation conditions during oil shale
retorting.
Other Constituents with Secondary Standards
Manganese, zinc, and copper have been monitored approximately 50
times in the Tertiary aquifers and fewer than five times in the
Quaternary and Precambrian to Upper Cretaceous aquifers. Concentrations
of these constituents in excess of the standards are reported at the DOE
114
-------
wells west of Rock Springs.* Excessively high manganese concentrations
occur at 6 of 12 DOE wells with a maximum concentration of 0.6 mg/1.
Excessively high zinc and copper concentrations were measured at 2 of 12
DOE wells with maximum concentrations of 26 and 1.6 mg/1, respectively.
As in the case of iron, all wells sampled more than once indicate
concentrations of these three constituents varying from far below the
standard to far above the standard.
*The DOE data must be used with discretion because the water
quality described by these data reflect specialized conditions which
exist in oil shales during and after retorting.
115
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VII. REFERENCES
-------
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U.S. Geol. Surv. Water-Supply Paper 1669-E.
Roehler, Henry W., 1974. Depositional environment of Eocene rocks in
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121
-------
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122
-------
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123
-------
A P P E
SUMMARY OF HYDR
BY F 0
N D I X A
OLOGIC PROPERTIES
R M A T I 0 N
-------
APPENDJ X A
SUmiARY OF IIYDROLOGtC PROPERTIES, BY FORMATION
Geologic Formation
Data Type1
Number of
Data Points
Summarized
Q
Y i eld
Range
(gpra)
Q/s
Speci fic
Capacity
Range
(spm/ft)
~
Porosity
Range
(X)
K2
Hydrauli c
Conduct Lvity
Range
(gpd/ft2)
¦|.3
Transmissivity
Range
(Rpd/fI)
Remarks
Quaternary1 deposits
AlJ uviurn
WW
WW
PUB
PT
6
47
11-1120
5-400
7-56
0. 3-150
5,000 -65 ,000?
230-200,000
most Y over 500 gpm
most Y <50 gpm; most Q/s <20
gpm/ft, fourty-one T <30,000
gpd/f t
Crave 1
WW
PT
5
15-25
1.1-25?
900-30,000
higher values have "zero
drawdown" (assumed one foot),
for other wells: Q/s <5.0
gpm/ft; T <2,000 gpd/ft
Quaternary and Tertiary Intrusives
WW
PUB
2
10, 50
Teewinot Format 1 on
WW
WW
PUB
PUB
3
1
15-120
1.5
1,000
Two wells have zero drawdown
reported, when assumed 1 ft
the calculated T are 70,000
and >100,000 gpd/ft
Salt Lake - Camp Davis Formations
SP
WW
WW
PUB
PUB
PO
4
1
2
15-8000
10
three flow 15-20 gpm
Browns Park Formation
SP
WW
PO
PO
3
1
Bishop Conglometete
SP
WW
PO
PO
5
1
Fowkes Format ion
SP
WW
PUB
PO
1
2
125
Bridger Formation
SP
SP
WW
WW
WW
PUB
PO
PUB
PT
PO
3
9
3
30
27
20-50
3-8
2-100
<0.1-5
30-6,000
most Y <25 gpm; most Q/s
>1.0 gpm/ft; most T 500-
3,000 gpd/ft
-------
APPENDIX A
(con tin ued)
Q / s
Q
Spec i f i c
Hydraulic T3
Number of
Yield
Capac i ty
Poros Ity
Conductivity Transmissivi ty
Data Points
Range
Range
Range
Range Range
Geologi c Format i on
Data Type
Summarized
(RP"i)
(gpm/ft)
(ft)
(Kpd/ft ) (Rpd/ftl
Remarks
Green River Formation
SP
PO
17
WW
PUB
L6
3-170
most <30 gpm
WW
PT
3
25-30
1.3-1.7
1 ,000-1,200
WW
PO
5
Lnney Member
SP
PO
i
WW
PUB
14
1-68
WW
PT
4
10-300
0.1-150
40->100,000
one well has reported "zero
drawdown11, assumed I ft.
WW
PO
34
Green River and Wasatch
equivalents WW
PUB
23
3-86?
WW
PO
7
Wasatch Formation
SP
PUB
16
<1-80
SP
PO
9
WW
PUB
104
0-1,300
most yields <50 gpm
WW
PUB
1
14
30,000
WW
PT
62
3-100
C
1
00
1007-30,000?
most Y <50 gpm, most T 200-
1,000 gpd/ft, most over
10,000 gpd/ft are estimates
for wells with "zero draw-
down," assumed 1 ft.
WW
PO
69
OF
PUB
4
20-25
0.02-18 0.7-27;550
ow
DST
4
18-26
Hoback Formation
SP
PO
1
WW
PUB
1
20
2.9
2 ,300
Fort Union Formation
SP
PO
1
WW
PO
1
OF
PUB
10
9-23
OF
PUB
5
0.0003-0.5 <0.J-18
OYJ
DST
5
0.3-182
Aimy Sand
OF
PUB
9
14—29
OF
PUB
6
0.2-8.
OF
PUB
4
36-123:^1,000
Evanston Formation
SP
PUB
2
10,1000
WW
PUB
2
3,200
Lance Formation
OF
PUB
2
12, 18
Fox Hills Sandstone
OF
DST
1
2 3+
-------
APPENDIX A
(cont inued
Geologi c Forma t i on
Data Type1
Number of
Data Points
Summarized
Q
Y i e Id
Range.
(gp"0
Q/s
Spec Lf ic
Capaci ty
Range
(spm/f t)
Mcsaverde Formal ton
WW PO
OF PUB
2
9
7
Aimond Formation
i
SP PO
OF PUB
OW DST
Ericson Formation
SP PO
WW PO
WW PUB
OF PUB
15-200
>
U>
Rock. Springs Formatic
Blair Formation
SP PO
WW PO
WW PUB
OF PUB
OF PUB
SP PO
WW PO
60?
Adaviile Formation
Milliard (Baxter) Shale
SP PO
SP PO
WW PUB
WW PO
OF PUB
OF PUB
OW DST
Frontier Formation
SP PUB
SP PO
WW PUB
WW PO
OF PUB
10
2
1
1
23
5-100
1
"First" Frontier Ss.
OW DST
OF PUB
OF PUB
OW DST
"Second" Frontier Ss.
OF PUB
OF PUB
OW DST
24
20
4
K
Hydraulic
Porosity Conductivity
Range Range
(ft)
(fipd/ft )
Transml ss 1 v i t.y
Range
(gpd/f L)
Remark s
12-24
0.009-].1
0.2-22; 165
12, 15
0.002, 0.009
<0.1, 0.15
36
10, ]3 0.002, 0.005 0.1, 0.3
9.5, 16
0.002
0.2
10-21
0.00024
<0.1
0.5-5.0
8-19
0.0015-1.
<0.1-45.
eight flow <50 gpm
f lowj ng
2
most K <0.1 gpd/ft ; most
T <3.0 gpd/ft
8-19
<0.J, 0.7
0.4-0.9;40 high T of 40 gpd/ft is
suspect.
2
8-25
0.004-9. <0.1-1.5 most K <0.1 gpd/ft*
1.2-2.5;32 high T of 32 gpd/ft Is
suspec t.
-------
APPENDIX A
(continued)
GeologLc Formation
Data Type^
Number of
Data Points
Summarized
Q
Yield
Range
(RPm)
Q/s
Specific
Capaci ty
Range
(fipm/Ct)
4>
Porosity
Range
(ft)
Hydrau]i c
Conduct lv Lty
Range
(gpd/ft )
T3
Transmi ssivlty
Range
(spd/ft)
Remarks
Blind Bill L Formation
SP
PO
1
Aspen (Mowry) Shale
SP
PUB
4
8-25
WW
PUB
4
J -30
3 wells flowing
ww
PT
1
17
8.5
6,000
WW
PO
1
OF
PUB'
1
15
"fractures"
ow
DST
2
0.5, 0.9
Bear RLver Formation
SP
PUB
10
4-100
9 flow 4-15 gpm
WW
PUB
2
5,7
WW
PT
3
1-250.
0.3-7.8
300-9,500
WW
PO
1
OF
PUB
6
10-19
OF
PUB
4
<0.002-0.02
<0.1-1.6
ow
DST
2
1.0, 1.8
Muddy Ss. Mbr.
OF
PUB
1
18
< .09
<1.9
OW
DST
1
4.5
"Dakota" Mbr.
OF
PUB
11
8-21
0.004-1.8
<0.1-45
OW
DST
12
<0.1-415?
most T between 2.0 and 7.0
gpd/ft
Gannett Group
SP
PUB
11
5-75
WW
PUB
4
20-100
ow
DST
1
0.6
l.akota Cong.
OF
PUB
2
18, 21
PUB
1
5.1
160
Morrison Formation
OF
PUB
4
8-17
OF
PUB
1
1.8
11
OW
DST
1
0.5
Stump (Curtis) Formation
SP
PUB
1
5
WW
PO
3
OW
DST
1
2.7
Preuss Redbeds ('Entrada Sandstone)
SP
PUB
2
20, 50
WW
PO
2
ow
DST
2
4, 12
Twin Creek Limestone (Carmei Fm.)
SP
PUB
4
20-300
three flow <75 gpm
SP
PO
1
OF
PUB
1
1.7
0.0002-0.002
<0.1-0.3
OW
DST
2
1.2, 16
-------
APPENDIX A
(continued)
Q/s
Q
Specific
~
Hydraulic
T3
Number of
Yield
Capaci ty
Porosity
Conduct ivi ty
Tran.smissivity
Data Points
Range
Range
Range
Range
Range
Goologi c Formation
Data Type
Summarized
(spm)
(gpm/ft)
.(ft)
(ftpm/ft )
(Rpd/fc)
Remarks
Nugget Sands tone
SP
PUB
8
3-2,000
six flow <300 gpm
(Green River Basin)
OF
PUB
2
10, 14
0.2
9, 25
most T <15 gpd/ft
ow
DST
9
2.8-37
(Overtlirust Beit)
SP
PO
2
I
ww?-
1
depth 11,550 ft; no addi-
tional data
0F
PUB
4
10-20
0.6-3
146-186
ow
DST
10
1.9-66
most T >25 gpd/ft
Ankareh Formation
SP
PUB
1
200
ow
DST
1
0.5
Thaynes Limestone
SP
PUB
5-1,800
four flow <100 gpm
WW
PUB
1
150
flowing
WW
PO
1
OF
PUB
1
<5
matrix fracture
OW
DST
0.3-38
two T values <10 gpd/ft
Dinwoody Formation
SP
PUB
1
150
ow
DST
1
8.8
Phosphoria (Park City) Formation
SP
PUB
1
300
SP
PO
WW
PUB
1
200
ow
DST
0.8-34
seven T values <13 gpd/ft
Tensieep Sandstone (WeiJs-Weber
SP
PUB
10
5-2,200
eight flow <210 gpm
formations)
SP
PO
1
WW
PUB
3
210-700
WW
PUB
1
6
10,000?
WW
PO
1
ow
DST
11
0.1-38
eight T values <10 gpd/ft
Amsden (Morgan) Formation
WW
PUB
1
8
OF
PUB
7-12
Morgan Formation
OF
PUB
1
<0.02
<0.4
Morgan Formation
ow
DST
4
0.3-4.8
Mad ison Limestone ¦
SP
PUB
6
15-40,000
four springs flow <350 gpm,
other two: 4,000 gpm, 40,000
gpm
SP
PO
1
WW
PUB
6
6-720
four wells <100 gpm
WW
PUB
5
0.2-140
400->100,000
most Q/s <10 gpm/ft; T
<15,000 gpd/ft
WW
PT
3
0.1-46
<100-50,000
WW
PO
1
ow
DST
4
1.9-20
-------
APPENDIX A
(continued)
Q/s
Kz
Q
Specific
Hydraulic
T3
Number of
Yield
Capacity
Poros ity
Conductivity
Transmissi vi ty
Data Points
Range
Range
Range
Range
Range
Geologic Formation Data Type* Summarized
(gpm)
(gpm/ft)
(ft)
(gpm/ft )
(gpd/ft)
Remarks
Darby Formation
Bighorn Dolomite
Gros Ventre Formation
SP PUB+
WW PUB
SP PUB
SP PO
OF PUB
SP PUB
5-1,1 00
5
250-3,200
900
three springs flow 250-450
gpm
fractures
>
I
!SP = spring
WW = water well
OF = oil field
OW = oil well
PUB = published data - for springs, water wells, see Appendix B for references; for oil fields, data summarized from Wyoming Geological
Association, 1979
Pi = reported pump tests on file at State Engineer's Office
+ = indicates some included data is from USGS data base
DST = drill stem test
PO = potentiometric data only - data from USGS data base
2Assumes water at 60°F where originally reported as permeability in millidarcies.
3For published oil field data T was taken as the product of hydraulic conductivity and pay thickness. Otherwise T calculated from specific capacity or
drill stem test data, see Appendix C for methods.
-------
APPENDIX B
HYDROGEOLOGIC DATA
BY WELL
-------
RII2W RIIIW RIIOW
Well or Spring No.
15-111-9 bed
WELL NUMBERING SYSTEM
Well and test hole numbers in this report describe the location of wells
and test holes according to the Bureau of Land Management's system of
land subdivision as follows: first number, township; second number,
range; third number, section; first letter, 160-acre tract (quarter section)
within that section; second letter, 40-acre tract (quarter-quarter section)
within that quarter section; third letter, 10-acre tract (quarter-quarter-
quarter section) within that quarter-quarter section. The 160-acre, 40-
acre, and 10-acre tracts are designated a, b, c, and d in a counterclock-
wise direction beginning in the northeast corner. For example, well
15-111-9 bed is in the SEJs SWJj NW^ Sec. 9, T. 15 N. , R. Ill W. When two
or more wells are located in the same 10-acre tract, the wells are numbered
serially in the order they were inventoried.
-------
APPENDIX B
HYDROGEOLOCLC DATA, BY WELL
Locat ion 1
-------
APPENDIX B
(continued)
To t a 1
Depth 2
Data
Reference
Potentlometrie
or
Type
Point
Surface
Tested
and
Elevation5
ElevatIon 6
Wei 1
Specific
Test
Location1
Interval
Geologic
Status
(ft above
(ft above
Yield
Capacity7
DuratIon
Transmissivity 6
Data
DST
(T-R-See-1/4-1/16)
(ft)
Format ion3
Date
or Use1*
msl)
msl)
( RPtn)
(Rpttt/ft)
" (hrs)
(Rpd/ft)
Source 9
Validity10
Remarks
39-115-32
be
35 i
Qal
1969
WD
(-9)
25
19.2
1
20.000
SEO
40-116-6 aa
46
Qal
1968
WD
(-L1)
20
*
1
(20,000)
SEO
40-LI 6-17
ddl
90
Qal
1946
WS/D
(-30)
20
0.8
UNK
600?
SEO
40-116-17
dd 2
86
Qal
1965
WD
(-50)
20
5.
0.25
3,000
SEO
40-116-19
cd
105
Qal
1968
WD
(-5)
8.3
10
2
9,000
SEO
40-116-20
ad 1
123?
Qal
1966
WD
(-60)
18
*
1
(20,000)
SEO
40-1J 6-20
ad2
90
Qal
1965
WD
(-60)
24
*
1
(20,000)
SEO
40-116-20
cb
35
Qal
1967
WD
(-15)
22
2.2
1
1.400
SEO
41-116-9 db
39
Qal
1927
WD
(-15)
10
*
1
(9,000)
SEO
41-116-22
b
-------
APPENDIX B
(cont inued)
Total
Depth7
Data
Re ference
PotentiometrIc
or
Type
Po in t
Surface
Tested
and
Elevat ion 5
Elevation6 .
Well Specific Test
LocntI on 1
Interval
Geologic
Status
(ft above
(ft above
Yield Capacity7 Duration Transraissivity8
Dat;
a
DST
(T-R-Sec-1/4-1/16)
(ft)
Formation3
Date
or Useu
msl)
msl)
(Rpm) (Rpm/ft) (hrs) (gpd/ft)
Source
Validity10 Remarks
i
SALT
LAKE/CAMP DAVIS
FORMATIONS - TERTIARY
31-119-15 cc
75
Tsl
U
6,380
6,400
USGS
OTB
34-119-24 ddc
0
Tsl
S
8,000
USGS
OTB
36-119-3 dbe
0
Tsl
s
20
USGS
OTB
36-119-23 abc
126
Tsl
w
5,980
5,946
uses
OTB
37-118-33 bab
0
Tsl
s
20
USGS
OTB
39-115-32 bdb
199
Ted
w
6,190
6,059
10
USGS
OTB
39-L16-2 dec
0
Ted
s
15
USGS
OTB
BROWNS PARK FORMATION - TERTIARY
13-114-7 cac
0
s
7,955
7,955
USGS
13-115-25 dbd
0
s
8,730
8,730
USGS
15-116-7 ccc
0
s
7,497
7,497
USGS
1 7-104-26 add
222
w
8,176
8,030
USGS
BISHOP CONGLOMERATE - TERTIARY
13-105-4 dda
0
s
7,935
7,935
USGS
13-112-17 ddb
0
s
8,340
8,340
USGS
13-116-29 cbc
0
s
8,633
8,633
USGS
14-104-7 dba
0
s
8,023
8,023
USGS
15-104-5 bcc
0
s
7,455
7,455
USGS
16-104-18 ddd
120
w
(-78)
USGS
FOWKES FORMATION - TERTIARY
14-121-14 ccc
150
w
7,000
6,961
USGS
OTB
17-120-32 db
32
w
6,520
6,493
USGS
OTB
19-121-25 nad
0
s
125
USGS
OTB
BRIDGER FORMATION - TERTIARY
12-111-15 cab
0
s
7,315
7,315
USGS
12-111-20 daa
0
s
7,390
7,390
USGS
12-111-24 add
0
s
7,380
7 ,380
USGS
L2-118-1 daa
0
s
8,438
7,438
USGS
12-118-1 dba
0
s
20
uses
OTB
13-115-16 aba
0
s
7,995
7,995
USGS
13-116-24 cb
50
1968
WD
8,000
7,988
15 1.2 0.5 -WOO
SEO
13-116-24 cc
60
1963
WD
8,015
8,000
20 2.0 0.5 1,000
SEO
13-117-35 dbc
0
s
35
USGS
OTB
14-115-9 da
65
w
7,206
7,186
USGS
14-115-16 ddd
30
WD
7,325
7,299
3
USGS
OTB
-------
APPENDIX B
(continued)
Total
Depth2
Data
Reference
Potentiometric
or
Type
Point
Surface
Tested
and
E1eva t ion 5
Elevation6
Wei 1
Location1
Interval
Geologic
Status
(ft above
(ft above
Yield
(T-R-Scc-1/4-1/16)
(ft)
Format ion 3
Date
or Use*4
msl)
msl)
(gpm)
14-115-33 be
5i
W
7,628
7,624
14-116-13 dd
94
W
7,295
7 ,287
14-117-12 dac
0
S
50
15-110-27 ede
0
S
6,455
6,455
15-114-3 cb
67
(47)
1946
ws/n
6,593
6,576
5
15-114-19 be
55
(19)
1945
WS/D
6,775
6,767
25
15-114-21 dd
49
U
6,595
6,580
15-114-30 bb
50
(20)
1950
WD
6,760
6,755
25
15-114-31 hb
45
(15)
1942
WS/D
6,780
6,778
20
15-114-31 bb
50
(20)
1 942
WS/D
6,780
6,778
20
15-115-1 be
43
W
6,7 70
6,745
15-115-12 cc
65
(20)
1976
WS/D
6,800
6,785
5
15-115-19 da
68
W
6,939
6,919
15-115-19 dd
38
(28)
1955
WS/D
6,975
6,960
25
15-115-23
67
(19)
1960
WD
6.850
6,840
20
15-115-23 aal
80
(49)
1942
WD
6,820
6.812
25
15-115-23 aa2
65
(17)
1963
WD
6,820
6,816
20
15-115-23 aa3
11
1963
WD
6,820
6,815
20
15-115-23 aa4
65
(15)
1962
WD
6,820
6.812
20
15-115-23 aa5
60
(24)
1953
WD
6,820
6.815
20
15-115-23 aa6
75
(27)
1964
WD
6,820
6,815
25
15-115-23 aa7
70
(34)
1967
WD
6,820
6,815
22
15-115-23 abl
70
(30)
1966
WD
6,835
6,829
18
15-115-23 ab2
55
(25)
1950
WD
6,835
6,827
20
15-115-23 ab3
65
(25)
1963
WD
6,835
6,831
40
15-115-23 ab4
73
(33)
1953
WD
6,835
6,829
10
15-115-23 acl
60
(30 y
1949
WD
6,840
6,835
100
15-115-23 ac2
55
(5)
1943
WD
6,840
6,835
5
15-115-23 ac3
55
(15)
1953
WD
6,840
6,834
10
15-115-23 ad
65
(27)
1963
WD
6,830
6,820
2
15-115-23 be
70
(25)
1957
WD
6,860
6,857
25
15-115-24 ba
65
(25)
1964
ws/n
6,800
6,794
20
15-115-23 bad
95
win
8
15-115-33 da
35
(3)
1960
WS/D
6,990
6.983
25
15-115-36 dd
46
(U)
1942
WS/D
6,800
6,785
2
16-110-5 edd
109
wu
6,385
6,367
16-111-19 ded
0
S
6.745
6 ,745
16-112-33 cca
0
s
6,835
6,835
16-114-16 abc
38
wu
6,550
6,521
16-114-29 da
40
1900
WS/D
6,610
6,598
15
16-114-32 aba
100
WID
6,630
6,622
3
Specific Test
Capacity7 Duration Transmissivity0 Data DST
(gpm/ft) (hrs) (gpd/ft) Source9 ValidiLy1
<0.1
2.1
0.8
1.0
1 .0
1 .0
5.0
4.0
2.5
1 .0
4. 0
1.3
2.0
5.0
2.2
] .1
1 .0
2.0
0.3
2.5
1.0
0.3
<-0.1
1 .3
1 .0
5.0
0.1
0.5
10
6
8
8
1 .3
4
5
10
6
6
2
1
24
.25
2
24
.5
1
309
1 ,800
500
800
800
800
6,000
3,500
2,300
900
3.000
1,200
1,300
6,000
2,000
900
800
1,200
300
1 ,000
607
300
30?
900
700
5.000
509
350
USGS
uses
USGS 0TB
USGS
SEO
SEO
USGS
SEO
SEO
SEO
USGS
SEO
USGS
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SEO
SKO
SEO
SEO
USGS GRB
SEO
SEO
USGS GRB
USGS
USGS
USGS CRM
SEO
USGS GRB
Elevations 40 fi lower
per USGS
12 inch diameter
-------
APPEND tX B
(continued)
CG
I
Ln
Total
Depth2
Data
Re ference
Potentiometrie
or
Type
Point
Sur face
Tested
and
Elevation
5 Elevation6 Well Specific
Test
Locat ion 1
Interva1
Geologic
Status
(ft above
(ft above YieLd Capacity7
Duration Transmissivity8
Data
(T-R-Sec-1/4-1
/16) (ft)
Format ion 3
Date
or Use
msl)
msl) (gpm) (gpm/ft)
(hrs) (Rpd/ft)
Source 9
16-1 14-32 bad
20^
WPS
6,615
6,605
uses
GRB
16-115-33 cd
66
W
6,665
6,617
uses
18-109-2 bd
200
u
6,175
6,100
uses
18-109-26 bob
47
Tb?
WD
6,128
6,119
USGS
GRB
18-110-27 acc
58
W
6.264
6,256
USGS
18-111-4 bbb
54
wu
6,303
6,267
USGS
GRB
18-113-26 ddc
36
WU
6,840
6,805
USGS
CRB
19-110-17 cd
157
W
6,250
6,225
USGS
19-111-30 ad
200
W
6,300
6,277
uses
19-118-23 aa
65
W
6,342
6,312
USGS
20-110-4 aa
60
w
6.485
6,445
uses
20-110-26 bb
70
w
6,352
6,319
USGS
20-111-23 aad
108
wu
6,450
6,403
USGS
GRB
21-112-32 c
160
w
6,580
6,566
USGS
22-106-16 bd
115
ws
6,770
6,715
USGS
GRB
22-106-17 ba
104
w
6,685
6,615
USGS
22-112-31 cna
200
wu
6,740
6,684
uses
GRB
23-106-30 d
49
ws
6,680
6,663
USGS
GRB
23-107-5 ccc
0
s
6,353
6,353
USGS
26-107-32 abb
200
w
6,775
6,640
USGS
BR1DGER-WASATCH FORMATIONS - TERTIARY
15-113-6 bcb
2,800?
ws
F 3
uses
GRB
GREEN RIVER FORMATION - TERTIARY
12-101-18 bdd
0
Tgt
s
7,140
7,140
USGS
12-102-11 be c
0
Tgt
s
7,680
7,680
USGS
12-103-11 dca
0
Tgw
s
8,380
8,380
USGS
12-109-20 dd
150 (144)
Tgl
1967
WS/D
6,590
6,555 30 7.5
2 6,500
SEO
12-109-20 dd
150
Tgl
w
6,640
6,605
USGS
12-110-2 ca
56
Tgl?
wu
6,370
6,360
USGS
GRB
1 2-110-6 ad
150
Tgl
WD
6,560
F6,560+ 5
USGS
GRB
12-110-22 abb
0
Tgl
s
6,720
6,720
USGS
13-101-28 aad
0
Tgt
s
6,060
7,060
uses
13-102-34 dca
0
Tgw
s
7 , 730
7,730
USGS
13-103-19 ddc
0
Tgt
s
7,760
7,760
USGS
13-105-16 ddd
0
Tgw
s
7,870
7,870
uses
13-105-21 dca
0
Tgt
s
7,495
7,495
uses
13-106-12 bed
0
Tgw
s
7,910
7,910
uses
13-106-16 bdd
0
Tgw
s
7,578
7.578
uses
13-107-3 dab
0
Tgw
s
6,475
6,475
uses
DST
Validity1
-------
APPENDIX B
(continued)
Total
Depth2
Data
Re ference
Potentiometric
or
Type
Point
Surface
Tested
and
Elevation5
E levat ion6
Well
LocaLion 1
Interval
Geologic
Status
(ft above
(ft above
Yield
(T-R-Sec-L/6-1/16)
(ft)
Formation3
Date
or Use1*
msl)
rasl)
(BPm)
1 6-106-27 dbc
a
Tgw
S
7,760
7,760
16-117-11 cd
250
Tgr
W
7,220
7 ,203
25
15-106-30 bbd
0
Tgw
S
6,575
6,575
15-111-20 cd
1 ,995
Tgr
W
6,676
F6.791
15-115-19 aa
60 (20)
Tgr
1958
WS/D
6,820
6,808
30
16-115-33 cc
60 (30)
Tgr
1962
WD
6,690
6,686
30
16-115-33 dc
62 (26)
Tgr
1952
WD
6,680
6,676
25
17-106-32 ccb
0
Tgw
S
6,180
6,180
17-109-2 aba
70
Tgl
WD
6,090
6,072
18-110-17 bac
2,165
Tgt
Wll
6,627
F6.427+
30'
19-110-21 ddb
\ ,908?
Tgt
WID
6,650
6,690'
21-105-32 ddb
0
Tgw
SC
3
21-!16-26 bdb
180
Tgl
W
6,980
6,952
21-116-27 dbc
160
Tgl
W
6,700
6,690
21-117-33 ab
0
Tgr
S
35
22-105-6 dc
99
Tgl
WS
7,050
6,197
2
22-106-16 bd
115
Tgl?
w
6,800
6,765
22-111-11 abe
606
Tgl
w
6,563
6,508
22-113-U. dc
181
Tgl
w
6,620
6,615
22-117-6 nb
0
Tgr
S
2
23-105-12 cac
0
Tgt
S
6,890
6,890
23-106-6 acd
950
Tgt
WD
6,615
6,765
150
23-106-8 abb
1,065
Tgt
WS
6,580
6,562
-
23-107-7 aab
196
Tgl
w
6,582
6,665
23-107-13 acc
1.029
Tgt
WS
6,700
F6.700+
15
23-107-36 cac
998
Tgt, Tgw
WS
6,580
F6,580+
5
23-112-21 ddc
63
Tgl
w
6,537
6,520
23-113-8 bed
76
Tgl
w
6,790
6,736
23-116-2 cac
165
Tgl
w
6,780
6,686
26-103-1-3 aaa
0
Tgt
s
7,597
7,597
26-106-29 aa
166 (78)
Tgl
1966
WS/D
6,610
6,570
10
26-106-30 ac
79
Tgl
wu
68
26-107-1 cc
200?
Tgl
WS
6,580
6,506
26-10 7-29 ddd
120
Tgl
w
6,526
6,687
26-107-35 abc
80
Tgl
w
6,530
6 ,51 7
26-108-20 dd
725
Tgw'
WS
6,600
6,666
5'
26-110-1 ca
72
Tgl
w
6,500
6,676
26-110-8 dc
116
Tgl
w
6,560
6,523
26-111-15 cc
288
Tgl
w
6,600
6,525
26-1 12-7 b
265
Tgr
w
6,590
6,578
25-106-27 aaa
166
Tgl
WS
6,910
6,867
25-105-3 cc
200
Tgl
w
6,803
6,753
Specific
Capacity
(Kpm/ft)
Test
Duration
(hrs)
Transmissivity8 Data DST
(gpd/f t) Source9 Validity 1 0 Remarks
1.7 2 1,200
1.3 6 1,100
1.3 6 1,000
0.1
USGS
USGS 0TB
USGS
USGS
SEO
SEO
SEO
USGS
USGS GRB
USGS GRB
USGS GRB
USGS GRB
USGS
USGS
USGS 0TB
USGS GRB
USGS
USGS
USGS
USGS 0TB
USGS
USGS GRB
USGS GRB
USGS
USGS GRB
USCS GRB
USGS
USGS
USGS
USCS
SEO
USGS GRB
USGS GRB
USGS
USGS
USGS GRB
USGS
USGS
USGS
USGS
USGS GRB
USGS
-------
APPENDIX B
(continued)
Total
Depth2 Dnta Reference Fotentiometric
or Type Point Surface
Tested and Elevation5 Elevation6 Well
Location1 Interval Geologic Status (ft above (ft above Yield
(T-R-Sec-1/4-1 /16) (ft) Formation3 Date or Use*4 msl) msl) (gpm)
25-105-6 cdc
9001
Tgt
U
6,665
F6.806
2 5 105-18 ab
59?
Tgl
WD
6,625
6,615
25-105-18 nd
20
Tgl?
WS
6,620
6,615
5?
25-105-29 cb
200 (150)
Tgl
1962
WS/D
6,660
6,652
30
25-105-31 adc
265
Tgl
WS
6,665
6,642
3?
25-106-4 cd
65 (35)
Tgl
1964
WD
6,650
6,632
300
25-106-12 aab
1 ,069
Tgt:
WS
6,640
F6.765
73
25-106-21 ac
1,262
Tgt
WS
6,595
F6.715
28
25-106-23 aad
70?
Tgl
WU
6,605
F6.605+
25-106-27 cb
1,030
Tgt
wc
6,575
F6.755
170
25-106-28 aac
265
Tgl
WD
107
25-106-28 dd
60
Tgl
WIR
6,570
6,536
25-108-10 ca
882
Tgt, Tgl
WS
6,900
6,883
20?
25-108-34 ab
853
Tgt 9
WS
6,810
6,710
25?
25-109-4 ad
205
TgL
W
6,720
6,714
25-109-11 dd
583
Tgt
WS
6,900
F7.004
20 7
25-110-15 aa
500
TgJ
W
6,800
6,750
26-104-16 dec
113
Tgl
w
6,860
6,807
26—J 05-18 bb
22
Tgl
WU
6,700
6,695
26-106-35 aa
75
Tgl
WD
6,800
6,779
10?
26-107-10 a
22
Tgl
WS
6,650
6,637
75
26-108-30 aa
618
Tgt-Tgl
WS
6,860
6,719
40?
26-109-10 ccd
312
Tgl
w
6,802
6, 74]
26-110-22 bba
316
Tgl
w
6,950
6,879
26-111-28 cca
710
Tgl
w
7,140
6, 707
27-105-8 cc
700
Tgl
w
6,903
6, 753
27-107-36 b
150
Tgl
WS
6,680
6,655
27-109-18 bd
349
Tgl
w
6,970
6,827
27-110-21 bb
493
Tgw, Tgl
w
7,150
6,980
12?
28-108-33 bb
150?
Tgl
WS
6,950
6,924
25?
28-109-23 be
218
Tgl?
WS
7,090
7,021
1
28-109-32 cc
268
Tgl 7
WS
7,150
7,053
2
28-109-36 dc
68
Tgl7
WS
(-31)
1
28-110-9 ad
300
Tgl?
WS
7,150
7, 145
29-105-3 cd
560
Tgl 7, Tii
WS
7,300
F 7,300+
3
Specific Test
Capacity7 Duration Transraissivity0 Data DST
(gpm/f t) (hrs) (gpd/f t) Source9 Validity1
0.16 (20,000)
2 >100,000?
uses
uses
GRB
USGS
GRB
SEO
USGS
GRB
SEO
uses
GRB
USGS
GRB
USGS
GRB
USGS
GRB
USGS
GRB
USGS
GRB
USGS
GRB
USGS
GRB
USGS
USGS
GRB
USGS
USGS
USGS
GRB
USGS
GRB
USGS
GRB
USGS
GRB
USGS
USGS
USGS
USGS
USGS
GRB
USGS
USGS
GRB
USGS
GRB
USGS
GRB
USGS
GRB
USGS
GRB
USGS
GRB
USGS
GRB
-------
APPENDIX B
(continued)
Total
Depth2
Data
Reference
Potentiomctric
or
Type
Point
Surface
Tested
and
Elevat ion15
Elevation6
Well
Specif ic
Test
Location1 Interval
Geologic
Status
(ft above
(ft above
Yield
Capacity 7
Duration
Transraissivity 0
Data DST
(T-R-Sec-1/4-1/16) (ft)
Format Ion3
Date or Use1*
rasl)
msl)
(Rpro)
(KPm/ft)
(hrs)
(gpd/ft)
Source9 Validity10
Remarks
GREEN RIVER AND WASATCH FORMATIONS - TERTIARY
CO
I
00
16-J15-13
630
Tgwe
W
(-10)
30
USGS
CRB
17-114-24 bdd
1 ,056
Tgwe
W1D
F
45
USGS
CRB
2 L — 114-26 bdb
180
Tgwe
WPS
(-28)
USGS
CRB
22-110-5 aba
973
Tgwe?
WD
(+290)
44
USGS
CRB
22-112-9 ddb
570
Tgwe?
WS
F
3?
USGS
GRB
22-112-20 dac
616
Tgwe?
WS
3?
uses
GRB
22-113-1 cdb
560
Tgwe
WS
F
7
uses
GRB
22-113-17 dc
181
Tgwe
WS
(-4)
40 7
USGS
GRB
23-106-35 bd
1,900'
Tgt, Tw
WS
5?
USGS
GRB
23-107-34 cac
998
Tgt, Tgwe
WS
F
5
USGS
GRB
23-112-21 d dc
637
Tgwe
wu
(-17)
USGS
GRB
23-113-8 bed
76
Tgwe
WS
(-56)
USGS
CRB
23-U4-2 cac
143
Tgwe
WS
(-96)
USGS
GRB
24-109-9 adb
1 ,500
Tw, Tgt
WS
F
85
USGS
GRB
24-110-1 ca
72?
Tgwe
WS
(-23)
85
USGS
CRB
24-110-8 dc
118
Tgwe
WS
(-15)
25?
USGS
GRB
24-111-15 cc
288
Tgwe
ws
(-74)
35?
USGS
GRB
24-112-7 b
265
Tgwe
wu
(-9)
USGS
GRB
24-112-8 ccb
1507
Tgwe
WPS
(-64)
17
uses
CRB
25-109-4 ad
205
Tgwe
ws
(-6)
40?
USGS
GRB
25-109-17 d
193
Tgwe
ws
(-59)
USGS
GRB
25-110-21 bd
190
Tgwe
ws
(-40)
40?
USGS
GRB
25-112-31 c
2 70 7
Tgwe
WD
(-30?)
USGS
CRB
26-106-3 aca
1,825
Tw, Tgt
WIR
F(+l20)
86?
USGS
GRB
26-109-6 ad
210
Tgwe
ws
(-337)
60
uses
GRB
26-109-15 cc
312
Tgwe
ws
(-58)
20?
USGS
GRB
26-110-22 a
316
Tgwe
ws
(-71)
24?
USGS
GRB
26-110-34 dc
285
Tgwe
ws
(-60)
40?
USGS
GRB
27-109-18 bbd
349
Tgwe
W
(-143)
45^
USGS
GRB
28-107-16 cb
900?
Tgt?, Tw7
ws
F
5
uses
GRB
12-109-22 cad
13-103-1 ban
13-105-24 ccd
13-111-26 bd
13-119-11 ada
13-119-34 ab
13-120-25 bbb
13-120-31 ccd
13-120-35 add
16
0
0
,014-4,055
100
280 (10)
152
0
39
Tw?
1952
1939
WD
S
S
OA
W
WS/P
W
S
W
6,200
8,100
6,845
6,964
7,300
7,360
7.440
WASATCH FORMATION - TERTIARY
6,191 1
8,100
6,845
5.718
7,280
7,357
7,431
45
20
22
200
USGS GRB
USGS
USGS
DST
USGS OTB
SEO
USGS OTB
USGS OTB
USGS OTB
-------
APPENDIX B
(continued)
Total
Depth7
Data
Re ferenee
Po ten tiomf? trie
or
Type
Point
Surface
Tested
and
E Leva t ion
Elevation6
Well
Location 1
Lntervn1
Geo logic
Status
(ft above
(ft above
Yield
(T-R-Sec-1/4-1/16)
(ft)
Format ion 3
Date
or Use"*
rasl)
msl)
(RPm)
14-115-9 da
65 ,
,(35)
1963
WS/D
7 ,220
7 .200
25
14-118-14 cbn
0
S
7,175
7,175
14-120-12 cbc I
,197
W
7,005
F7 ,005+
15
15-108-28 ebb 2.
,218
WA
6,155
F6.155+
42
15-109-L0 acc 2
>4 20
Tw?
WID
6,210
F6 ,210+
30?
15-]13-6 beb
0
S
6,640
6,640
15-1]5-5 dd
75
w
6,767
6,732
15-117-5 dbb
0
s
6,730
6,7 30
15-117-L9 ba
0
s
<1
15-117-24 cbd
0
s
7,340
7,340
15-118-24 be1
80
Tv7
WD
7,150
7,091
15-118-24 be2
261
W
7,000
6,939
15-118-18 add
W
15
15-119-22 ebb
W
5
15-120-1 ddd
0
S
30
15-120-11 ddc
0
s
2
15-120-20 ab
620
w
6,800
6,710
1 ,300
15-120-34 dc
65
1965
WS/D
7,000
6,951
8
15-120-35 cc
135
Tv7
1950
WD
6,900
F6,900+
^35
15-121-27 da
190
w
6,740
F6.740+
16-107-22 ddd
990
WPS
6,140
F6,429
7
16-114-31 add 1,
,200
Wll
6,630
F6.630+
3?
16-119-27 dbc
0
Tw?
s
40
16-121-2 ab
60
(10)
1919
WS/D
6,500
6,480
20
16-121-2 ac
65
(35)
1955
WS/D
6,505
6,485
25
16-121-2 ad
100
(70)
1952
WS/D
6,505
6,485
25
16-J21-2 ba
110
(10)
1952
WS/D
6,590
6,500
10
16-121-11 ac
34
W
6,580
6,558
17-118-17 cac
0
Tw?
S
5
17-119-13 daa
503
W
7,490
7,010
17-120-8 db
26
Tw?
W
6,460
6,438
17-120-19 db
80
W
6,590
6,560
18-105-6 ad
220
W
6,245
6,200
18-105-7 dab
1587
WD
50?
18-106-11 cb
890
W
6,380
6,1 30
18-106-15 be
900
W
6,331
6,181
18-L07-22 aca
764
Tw?
wu
6,110
F6.1 10+
5?
18-119-12 aad
0
Tw?
S
75
19-105-4 cc
240
W
6,495
6.325
19-105-8 aa
195
W
6,540
6,435
19-105-32 dab
152
WU
6,300
6,257
19-105-32 da
165
w
6,300
6,275
Specific Test
Capacity7 Duration Transmissivity0 Data DST
(gpm/ft) (hrs) (ftpd/ft.) Source9 ValidiLy1
2.5
500
SEO
USGS
USGS
OTB
USGS
GRB
USGS
GRB
USGS
USGS
USGS
USGS
OTB
USGS
USGS
OTB & GRB
USGS
OTB
USGS
OTB
USGS
OTB
USGS
OTB
USGS
OTB
,000?
USGS
OTB
600
SEO
200
SEO
USGS
OTB
USGS
GRB
USGS
GRB
USGS
OTB
600
SEO
600
SEO
500
SEO
000)
SEO
USGS
OTB
USGS
OTB
USGS
USGS
OTB
USGS
OTB
USGS
USGS
GRB
USGS
USGS
USGS
GRB
USGS
OTB
USGS
USGS
USGS
GRB
USGS
14 UNK
1.0 1
l.o J 600 SEO 3 inch diameter
1.0 1
0.8 1
* 2
-------
APPENDIX B
(cont inued)
Total
Depth? Data Reference Potentiometric
or
Type
Point
Surface
Tested
and
Elevation5
Elevat ion6
Well
Locat ion1
Interval
Geologic
Status
(ft above
(ft above
Yield
(T-R-Scc-1/4-
1/16)
(ft)
Formation3
Date
or Use1*
tnsl)
tnsl)
(RPm)
19-105-32 dac
1901
WD
6,300
6,267
19-118-26 can
200
W
6,795
6,685
19-119-17 aac
0
Tv7
S
60
19-119-32 dad
0
s
80
20-105-20 cd
190
u
6,612
6,462
20-105-28 bec
125
ws
6,550
6,456
21-105-33 ddc
60
WD
6,690
6,657
21-117-L8 ac
0
S
15
21-118-2 ccl
500
w
6,590
F6.590+
10?
21-118-2 cc2
350
w
6,590
F6.590+
3?
23-110-13 dca
1
,725
ws
6,420?
F6.590+
420?
23-110-13 dca
I
~ 725
w
6,396
6,046
23-110-13 dd
2
,130-2,420
1958
OA
6,409
7,370
23-110-13 dd
2.
,470-2,510
1958
OA
6,409
6,684
23-110-13 dd
2
,860-3,180
1958
OA
6,409
6,594
23-114-28 daa
WS
8
Cd
1
23-115-13 b
0
Tv?
S
l7
23-118-3 acb
0
S
5
M
23-118-26 dd
0
s
5
O
24-111-15 deb
24-117-25 ab
288
0
Tvn
Tw7
W
s
6,543
6,343
15
25-110-15 aa
500
Twn
wu
6,820
6,770
25?
25-111-2 bd
480
Tvn
ws
6,850
6,752
25-111-22 be
760
Tvn
WS
6,880
6,730
40?
25-112-31 c
2 70
Tvn
u
6,700
6 ,670
25—1 1 3— 29 da
120
Tvn ?
ws
6,800
6,737
40 7
25-117-23 ede
0
Tw?
s
5
26-103-30 edd
10,
,000
W
6,880
5,880
26-104-4 cda
427
ws
6,880
F6,880+
15
26-109-5 cbc
349
Tvn
w
6,828
6,704
26-110-3 cc
405
Twn
ws
7,020
6,942
40?
26-110-30 adb
504?
Tvn
WID
20?
26-111-10 be
461
Tvn
ws
7,210
6,961
20?
26-112-6 ca
123
w
6,600
6,591
26-112-6 da
1 357
WD
6,585
F6,585+
3
26-112-6 db
85 (25)
1966
WD
F
30
26-1J 3-11 ac
145
WPS
6,700
6,680
26-114-3 da
175
W
7,300
7,276
26-117-16 bbd
0
s
3
27-102-24 dda
0
s
7,210
7 ,210
27-105-3 cc
500
wu
6,940
6,926
25?
27-110-6 edd
725
Twn
w
7,280
6,800
Specific Test
Capacity7 Duration Transmissivity0 Data DST
(Rpm/ft) (hrs) (spd/ft) Source9 Validity1
18 DST P
26 DST P Fresh water
22 DST P
4,000
uses
GRB
USGS
uses
OTB
USGS
OTB
USGS
USGS
GRB
USGS
GRB
USGS
OTB
USGS
OTB
USGS
OTB
USGS
GRB
USGS
DST
DST
DST
USGS
GRB
USGS
GRB
USGS
OTB
USGS
OTB
USGS
USGS
OTB
USGS
GRB
uses
GRB
USGS
CRB
USGS
USGS
GRB
USGS
OTB
USGS
USGS
GRB
USGS
USGS
GRB
USGS
GRB
USGS
GRB
USGS
USGS
GRB
SEO
USGS
GRB
USGS
USGS
OTB
USGS
USGS
GRB
USGS
-------
APPENDIX B
(cone inued)
Total
Depth2
Data
Re ference
Potent iomc tr ic
or
Type
Point
Surface
TesLed
and
ElevatIon 5
EievatIon 6
Well
l,ocat ion1
Interval
Geologic
Status
(ft above
(ft above
Yield
(T-R-Sec-1/4-1/16)
(ft)
Formation3
Date
or Use1*
msl)
rasl)
(Rpm)
27-111-25 abb
732'
Twn
W
7,290
6,805
27-112-29
102
W1D
688
27-112-30 a
48*
WD
6,710
6,688
27-113-5 ab
281?
W1D
7,380
7,374
27-113-6 cbc
327
WA
(-11)
4
27-113-15 dbb
908
WID
16
27-113-22 ab 2
,339
W
(-1,250)
15
27-113-25 cca
284
WID
6,860
6,746
23
27-113-25 ccd
930
WID
117
27-113-27 beb
805
WID
25
27-113-28 dac 1
,037
W
53
27-113-36 bdb
760
WID
6,800
6,700
120
27-114-1 ccc
81
WID
7,730
7,674
13
27-114-6 cbc
18?
W
(-56)
13
28-104-34 b
143
ws
7,025
6,976
28-105-25 be
93
wu
7,150
7,096
23-110—1 cb
180 7
ws
6,950
6,907
2
28-110-33 ac
420
Twn?
ws
(-230)
2
28-111-15 ac
217
Twn ?
ws
7,000
6,905
3
28-112-11 can
750
ws
F
28-112-19 ac
153
wu
6,975
6,894
28-112-30 db
170
ws
(-116)
6
28-113-3 cc
60?
ws
F
20
28-113-4 ddb
125
WID
7,325
7,318
200
28-113-15 aa
217
w
(-95)
30
28-1 1 3-20. daa
175
WID
(-20)
28-113-23'd
31
Tw?
w
(-15)
28-114-2 dbb
0
s
8,040
8,040
29-107-5 db
200
ws
(-50)
7
29-107-10 bb
120
wu
7,170
7, 155
38
29-107-10 da
102
ws
7,175
7,151
I
29-107-17 dc
78?
ws
(-37)
3
29-107-20 cb
] 94
WA
dry
dry
29-108-8 bd
1 70
ws
7,210
7,116
29-108-24 ca
349
ws
(-120?)
29-108-31 cc
95
ws
(-69)
29-108-33 dd
215
ws
(-111)
16
29-109-6 bb
174
ws
7,020
6.903
40'
29-109-22 cb
360
ws
(-266?)
10
29-110-11 cd
90
ws
(-42)
72'
29-111-5 ccc
260
ws
6,790
F6,790+
5
29-111-7 add
475
60
Spec if ic Test
Capacity7 Duration Transmissivlty9 Data DST
(gpm/f t) (hrs) (gpd / f t) Source9 Validity10 Remarks
uses
uses
CRB
USGS
CRB
uses
CRB
USGS
CRB
USGS
GRB
uses
0TB
USGS
CRB
uses
CRB
USGS
GRB
uses
0TB
USGS
CRB
uses
CRB
uses
0TB
USGS
CRB
USGS
CRB
USGS
CRB
USGS
CRB
uses
CRB
uses
CRB
uses
CRB
USGS
CRB
uses
GRB
& 0TB
uses
GRB
& 0TB
USGS
0TB
USGS
CRB
uses
GRB
uses
uses
CRB
uses
CRB
uses
CRB
uses
GRB
uses
CRB
USGS
GRB
USGS
GRB
USGS
CRB
USGS
CRB
uses
GRB
uses
GRB
uses
GRB
uses
CRB
uses
GRB
-------
APPENDIX B
(cont inued)
Total
Depth2
Data
Re Terence
Potentiometric
or
Type
Po int
Surface
Tested
and
Elevation5
E levat ion6
Wei 1
Specific Test
Location1
Interval
Geologic
Status
(ft above
(ft
above
Yield
Capacity7 Duration
Transmissivity0
Data
DST
(T-R-Sec-1
L/4-1/16)
(ft)
Formation3
Date
or Use1*
msl)
msl)
(Rpn)
(Rpm/ft) (hrs)
(Epd/ft)
Source9
Validity10 Remarks
29-111-18
ddc
307
ws
6,815
30?
uses
ORB
29-11 1-29
da
iool
u
6,770
6,
715
USGS
29-1 J 1-33
abb
350
WD
F
50?
USGS
GRB
29-111-35
aa
105
WS
(
-56)
36?
USGS
GRB
29-112-25
aa
389
WS
6,950
6,
758
1
USGS
GRB
29-112-34
cdc
554
W1D
(-
110?)
82
USGS
GRB
29-113-3 cac
41
W1D
7,310
7,
298
uses
GRB
29-113-33
da
128
WS
8,000
7,
951
1
USGS
GRB
29-L13-36
be
434
1959
WID
(-
300)
9.
* 24
(20,000)
SEO
Static water level (-9)
ft per USGS
29-11^-28
cb
0
S
8,560
8.
560
USGS
30-106-12
ad
102
W
7,220
7,
199
2
USGS
GRB
30-106-17
cd
96
WS
7,230
7,
188
13?
USGS
GRB
30-106-22
bd
101
WS
(
-20)
2
USGS
GRB
30-107-2 ad
65?
WS
(
-18)
USGS
GRB
30-107-4 da
150
ws
7,290
7,
205
12
USGS
GRB
30-107-6 dd
153
ws
7,250
7,
183
20?
uses
GRB
30-107-13
cb
150'
ws
(
-65?)
3
USGS
GRB
30-107-32
ad
230
ws
(-
135?)
48?
USGS
GRB
30-108-5 <
Sbb
355
wu
7,100
7,
003
USGS
GRB
30-108-20
ba
600
w
7,380
7,
069
uses
30-108-23
dc
375?
ws
(-
167)
2
USGS
GRB
30-109-5 aa
450?
ws
6,850
F6,
850+
5
USGS
GRB
30-109-5 i
ab
55 (15)
Tw?
1967
WD
(-7)
65
6.5 1
5,000
SEO
30-109-19
cd
555
w
7,280
6,
980
USGS
30-110-17
ca
400?
WD
USGS
GRB
30-110-20
ca
106
ws
6,900
F6,
900+
20
USGS
GRB
30-110-30
ab
86 (16)
1962
WD
(
-50)
30
* 8
(30,000)
SEO
30-111-11
dc
100
W
6,910
6,
845
USGS
30-111-17
aca
435?
WPS
6,900
6,
879
uses
GRB
30-111-17
dbb
195
ws
(
-44)
5
USGS
GRB
30-111-30
ac
63
WD
(
-20?)
USGS
GRB
30-i11-30
ac
155 (65)
1954
WD
(
-17)
20
1.0 3
800
SEO
30-111-31
bdd
460
WD
F
USGS
GRB
30-111-31
dbc
L30
1959
WPS
(-5?)
100
1.5 29
1,700
SEO
10 inch diameter
30-112-12
dc
70 (30)
1965
WS/D
(
-40)
30
* 0.5
(30,000)
SEO
30-112-33
cbd
790?
WS
6,980
F6,
980+
2
uses
GRB
30-112-36
accl
500?
WPS
F
5
USGS
GRB
30-112-36
acc2
120
1959
WPS
(-3)
70
.1.0 2
700
SEO
10 inch diameter
30-112-36
bca
172
WPS
F
200?
USGS
GRB
30-113-15
cc
196
ws
7,270
7,
130
20
USGS
GRB
30-113-35
cb
120
ws
7,175
7,
161
50?
USGS
GRB
-------
APPENDIX B
(continued)
Total
Depth2 Data Reference Potentlometric
or
Type
Point
Surf ace
Tested
and
Elevation5
Elevation6
Well
Location1
Interval
Geo logic
Status
(ft above
(ft above
Yield
(T-R-Sec-l/4-1/16)
(ft)
Formation3
Date
or Use1*
msl)
msl)
(BPm)
11-106-32 aha
50 i
W
7,154
7,150
.11-107-1 aa
68 (19)
1935
WS/D
7,134
7,117
14
31-107-1 aa
65 (17)
1950
WS/D
7,134
7,117
18
31-107-G ac
172
WS
7 ,300
7,205
16?
31-107-20 be
238
ws
(-117)
14?
31-10 7-23 dc
133
WS
7.200
7,149
7
31-107-31 dc
224
WS
(-63)
34
31-108-2 bd
34 7
WS
(-40)
10?
3L-I08-9 bd
200
WS
7,010
6,953
32?
31-108-13 ad
251
WS
(-88)
27?
31-109-4 b
325
ws
7,120
6,980
10?
31-110-26 cd
400
WS
7 ,100
7,035'
20 7
31-111-31 cd
235
WS
7,050
6,868
2
31-112-23 cc
327
ws
7,250
7,019
2
32-106-32 dca
75
w
7,208
7,188
32-107-25 aad
85
Tw?
WS
7,180
7,154
32-108-9 dc
123
W
7,000
6,930
32-108-14 cc
135
1964
WS/D
(-15)
25 ¦
32 — 108— L7 aad
76
Tw'
ws
F
1
32-108-30 d
150?
WD
(-10?)
32-109-5 db
34 3
ws
(-177)
107
32-109-13 ca
161
ws
(-247)
40?
32-109-17 aaa
150
ws
6,970
6,930?
70?
32-110-13 ab
409
ws
7,490
7,417
5
32-111-24 ac
no?
WD
6,990
F6.990+
12
32-112-13 ab
71
wu
7,250
7,223
32-113-33 cb
21 1
ws
7,830
7 ,665
2
32-114-11 ad
150?
ws
(-20?)
33-107-28 cc
200
ws
7,400
7,303
1
33-108-10 db
141
1965
WD
7 ,146
40
33-109-2 cb
80
1959
WD
7,180
20
33-109-3
140
1962
WD
(-128)
30
33-109-3 aa
105
1961
WD
(-2)
25
33-109-3 ab
107
1961
WS/D
(-20)
20
33-109-3 be
209
196 7
WD
(-37)
50
33-109-3 cc
75
1974
WD
(-7)
30
33-109-3 dbl
106
W
7 ,200
7 .165
33-109-3 db2
123
1967
WD
(-47)
12-15
33-109-5 bb
160
1964
WS/D
(-8)
100
33-109-6
100
1965
WD
(-7.5)
25
33-109-6
95
1967
WD
(-12)
30
33-109-6 aa
90
1968
WD
7,158
30
Specific Test
Capacity7 Duration Transmissivity8 Data DST
(gpm/ft) (hrs) (fipd/ ft) Source' Validity1
uses
*
1
(I>300)
SE0
*
1
(1.500)
SEO
USGS
CRB
uses
GRB
uses
GRB
USGS
CKB
uses
GRB
USGS
GRB
USGS
CRB
USGS
GRB
USGS
GRB
USGS
GRB
USGS
CRB
USGS
USGS
GRB
USGS
0.5
i
300 7
SEO
USGS
GRB
USGS
GRB
USGS
CRB
USGS
GRB
USGS
CRB
USGS
CRB
USGS
GRB
USGS
GRB
USGS
CRB
USGS
GRB
USGS
CRB
0. 3
UNK
200'
SEO
0.8
UNK
500?
SEO
1 .5
UNK
1 ,000'
SEO
1.4
UNK
1 ,000?
SEO
0.7
UNK
400?
SEO
0.4
4
230
SEO
! .0
0.5
500
SEO
USGS
1.2-0.3
UNK
2007
SEO
2.9
0.5
1 ,300
SEO
1 .0
4
800
SEO
1.0
2
700
SEO
1 .0
2
700
SEO
-------
APPENDIX B
(continued)
Total
Depth 7
Data
Re fe rence
Potent iometric
or
Type
Point
Surface
Tested
and
Elevation 5
E1evat ion 6
Well
Specifie
Test
Location 1
Interval
Geo 1 ogle
Status
(ft above
(ft above
Yield
Capacity 7
Durat ion
Transmissivity 8
Data
DST
(T-R-Sec-L/4-1/16)
(ft)
Formation 3
Date
or Use
msl)
msl)
(RPm)
(Rpm/ft)
(hrs)
(Rpd/ft)
Source 9
Validity10 Remarks
33-109-6 nh
1201?
WD
(-18)
USGS GRB
33-109-10 ad
153
1968
WD
7, ] 75
7.145
20
0.6
UNK
400?
SEO
33-109-22 ab
110'
WD
(-20)
USGS GRB
33-109-22 ab
134 (102)
1956
WS/D
(-15)
15
1 .0
UNK
600?
SEO
33-109-22 dc
95
1962
WD
(-16)
30
1.0
UNK
600?
SEO
33-109-22 dc
65
1914
WD
(-16)
30
1.0
UNK
600?
SEO
33-109-24 ad
165
1959
WS/D
(-75)
15
*
96
(20,000)
SEO
33-109-24 he
96
1964
WS/D
(-117)
21
*
5
(20.000)
SEO
\ inch drawdown
33-110—1J cd
400
WA
dry
dry
USGS GRB
33-111-2 hh
50?
1962
WD
(-16)
25
0/5
UNK
300?
SEO
33-111-2 bb
276
Tw?
1962
WS/D
7,192
7,183
7.5
0.9
12
900
SEO
33-111-15 ca
20 7
W
7.360
7,283
USGS
33-111-19 edd
295
WU
32
10?
USGS GRB
33-112-21 dd
100?
ws
F
20
USGS GRB
33-112-24 cc
390
w
7,520
7,365
USGS
33-113-12 cd
60?
WD
F
2
USGS GRB
33-113-22 dc
170?
WD
(-112)
USGS GRB
34-109-6 db
87
1961
WS/D
7,330
25
*
2
(30.000)
SEO
34-109-20 cc
150
1967
WD
(-70)
30
0.3
2
200
SEO
34-109-20 cc
140
1968
WD
(-65)
20
0.2
4
150?
SEO
34-109-27 dd
200
W
7,370
7,227
USGS
34-109-29 d
62?
WD
(-11?)
USGS GRB
34-109-33 ac
107
1958
WD
(-22)
3.3
*
UNK
(2,300)
SEO
34-109-33 ac
1J0
1968
WD
(-20)
30
0.8
UNK
500?
SEO
34-109-33 ad
115
1963
WD
7,900
7,890
20
0.7
2
400
SEO
34-109-33 dc
125
1952
WD
(-6)
20
0.8
UNK
500?
SEO
34-109-34 db
120
1951
WS/D
(-20)
20
*
6
(20,000)
SEO
34-110-3 cd
85 (5)
1967
WD
(-32)
20
*
UNK
(20,000)
SEO
34-110-10 ba
50
1959
WD
(-20)
30
*
0.5
(20,000)
SEO
34-1 10-11 bd
60?
WD
(-10?)
USGS GRB
34-110-27 cd
115 (5)
1968
WD
(-45)
25
1 . 3
2
1 ,000
SEO
34-110-30 be
58
WD
(-38)
USGS GRB
34-110-31 cbcl
60?
WD
F
100?
USGS GRB
34-110-34 aa
240
1968
WD
7,240
7,160
30
*
0.67
(20,000)
SEO
34-110-34 ba
100
1964
WS/D
(-30)
75
3.8
1.5
3,000
SEO
34-110-34 ba
98
1965
WD
(-24)
60
1 . 7
0.083
400?
SEO
34-110-34 ba
UO (5)
1968
WD
(-35)
25
*
0.17
(15,000)
SEO
34-110-34 be
230 (5)
1962
WD
(-51)
25
0.2
2
200
SEO
34-111-4 bd
114
1963
WD
(-6)
25
1.3
UNK
1,000?
SEO
34-111-19 dc
94
1959
WD
7,000?
7,000?
50
8.3
UNK
700?
SEO
34-111-26 bbd
130?
WC
(-80?)
USGS GRB
34-111-28 aa
225
1972
WS/D
(-110)
12
0.2
I
100?
SEO
-------
APPENDIX 3
(con tinuod)
Total
Depth2
Data
Re ference
Potentlomet ric
or
Type
Point
Surf ace
Tested
and
E ievat ion5
ElevatIon6
Wei 1
Spec if ic
Test
Local Ion 1
Interval
Geologic
Status
(ft above
(ft above
Yield
Capac ity 7
Duration
TransmissivIty 8
Data
(T-R-Sec-L/4-1/16)
(ft)
Formation3
Date
or Use
msl)
msl)
(Rpm)
(Rpm/ft)
(his)
(Rpd/ft)
Source9
34-111-35 cb
llV
WPS
(-4)
USGS CRB
34-112-14 aa
155
WD
(-57)
USGS CRB
34-113-9 ac
212
J 966
WD
7,650
7,615
20
A
0.5
(15,000)
SEO
35-110-8 ac
65
1968
WD
7,506
1 3
0.3
2
200
SEO
35-110-19 bd
150
WD
(-457)
1 5 7
USGS GRB
35-110-20 ca
163
ws
287
USGS CRB
35-110-23 db
186
1962
WD
(-40)
30
0.46
2
300
SF.O
35-111-1 ddb
2 70
Tw?
WS
(-87)
257
USCS CRB
35-111-23 dd
75
Tw7
WU
(-23)
5
USGS CRB
HOBACK FORMATION - TERTIARY
37-112-13 c 0 S 7,400 7,600 USCS 558
38-113-31 a 106 WD 20 2.9 1 . 5 2,300 USCS 558
td
14-101-30 ba
14-103-35 bdd
19-112-22 cc
23-110-13 dd
23-110-13 dd
23-110-13 dd
29-113-25 cc
U5
0
5 ,407-5 ,456
4,587-4,633
6,327-6,364
7,177-7,314
1,801-1,845
1973
1958
1958
1958
1957
W
S
OP
OA
OA
OA
OP
FORT UNION FORMATION - TERTIARY
7,100 7,065
7,498 7,498
6,389 6,809
6,409 6,770
6,409 4,142
6,409 -620
7,526 6,924
31
0.26
2.5
42
182
USGS
uses
DST
DST
DST
DST
DST
I' rod ne I i <
SI r! v
f t om Pm
11 I v vaii-
Fresh writer, oil
Kinv
15-120-16 dc
17-118-13 ede
19-120-15 aba
22-116-6 ab
57
EVANST0N FORMATION - TERTIARY AND CRETACEOUS
6,780
6,760
200
3
10
,000
USGS OTB
USGS OTB
USGS OTB
USCS OTB
UNDIFFERENTIATED - PRE-TERT1ARY
18-116-6 dda
19-I16-32 ca
26-114-1 bac
27-113-28 daa
28-113-19 bbd
28-114-12 aab
32-107-8 ddd
33-115-4 a
38-1J0-2 bd
38-110-11 ba
39-111-22 ba
1 ,005
7
0
1 ,037
64
586
?
0
0
0
664
WS
WS
SIR
WID
WID
WU
WC
SU
SU
SU
WU
(-44)
I
1
4,0007
53?
5?
20 7
5?
2,000?
1007
USGS CUB
USGS CRB
USGS CRB
USGS CRB
USGS CRB
USGS GRB
USGS CRB
USCS CRB
USGS GKB
USCS CRB
USGS GRB
-------
APPENDIX B
(continued)
W
I
Total
DepLli 7
Data
Re Terence
PotcnL LomeLnc
or
Type
Po int
Surface
Tested
and
Elevat ion
5 Elevation6
Well Specific
Test
LocaLIon *
Interva1
Geologic
Status
(ft above
(ft above
Yield Capacity7
Duration
Transmlssivity*
Data DST
(T-R-Sec-1/4-1/16) (ft)
Format ion3
Date
or Use1*
msl)
msl)
(Rpm) (fipm/ft)
(hrs)
(ftpd/ft)
Source9 Validity10
i
FOX HILLS SANDSTONE - CRETACEOUS
27-112-29 dc
2,336-2,358
1963
OA
6,588
6,872
22. 7+
DST
F
MESAVERDE CROUP
- CRETACEOUS
]2-105-22 aca
0
Kg
S
6,425
6,425
uses
12-105-22 aca
0
Ke
S
6,335
6,335
USGS
14-102-10 bbd
0
Kal
S
7,183
7,183
uses
14-103-7 abe
0
Kr
s
7 ,070
7,070
USGS
14-103-18 nbc
0
Ke
s
7,137
7,137
USGS
18-104-28 cc
245
Kbl
w
6,761
6,751
uses
18-104-33 cca
0
Kb I
s
6,800
6,800
USGS
18-105-14 acc
L ,420
Kr
w
6,398
6,300
60?
USGS:
, GD/W
19-105-2 bcc
865?
Kal,Ke
w
(-17)
200?
uses,
, GD/W
19-105-2 beb
880
Ke
w
6,34 7
6,317
200?
USGS,
, GD/W
19-105-10 ab
I ,350
Kmv
w
6, 363
6,313
USGS
19-105-14 ca
180
Kmv
w
6,370
6,210
USGS
19-105-23 beb
550
Ke
w
6,285
6,260
157
USGS,
, GD/W
20-105-1 aca
338
Ke
w
6,700
6,501
200
USGS,
, GD/W
20-105-36 cca
93
Ke
w
6,420
6,388
200
USGS ,
, GD/W
21-104-33-cdb
510
Ke
w
6,700
6,420
USGS
21-104-33 ede
485?
Ke
w
(-235)
40?
USGS ,
, GD/W
22-104-5 cd
2,426-2,539
Kal
1962
OA
6,677
7,342
36
DST
F
22-104-15 ccd
1
Kal (7) , Ke (?)
w
F
75
USGS ,
, GD/W
23-103-19 ca
135?
Kal, Ke(7)
w
F
25?
USGS,
, GD/W
24-115-32 cbd
0
Kav
s
7,540
7,540
USGS
H1LLIARD (BAXTER) SHALE - CRETACEOUS
12-107-3 cd
13,270-13,450
o
7,026
13,797
0.79
DST
P
16-L04-23 baa
0
s
7,095
7,095
uses
17-104-15 abe
0
s
7,357
7,357
uses
17-113-33 da
12,180-12,269
1977
OA
6,428
902
5.3
DST
P
19-104-23 ad
340
w
6,307
6.127
USGS
19-116-18 bd
100
w
6,750
6,670
6
USGS
OTB
21-116-1 bb
21
w
7 ,000
6,686
USGS
22-116-5 aad
0
s
7 ,420
7,420
USGS
26-112-4 dd
6,307-6,400
1957
OA
7,312
3,046
2.6
DST
P
27-L11-27 bb
8,310-8,371
1975
0
7,266
-901
0.49
DST
P
Remarks
fresh water
Sp. Cond. = 380
Sp• Cond. = J,510
-------
APPENDLX B
(cont inued)
Tot a J
Depth ?
Data
Re fercnce
Po tent iometric
or
Type
Po int
Surface
Tested
and
Elevation 5
Elevat ion6
We 11
Spec 1f ic
Test
Locat ion 1
Interval
Ceo logic
Status
(ft above
(ft above
Yield
Capacity 7
Durat ion
Transmissivity0
Data
DST
(T-R-Sec-1/4-
1/16) (ft)
Format ion3
Date
or Use11
msl)
msL)
(ftpm)
(Rpm/ft)
(hrs)
(Rpd/ft)
Source9
Validity10
Remarks
1
FRONTIER FORMATION - CRETACEOUS
14-118-7 cd
665
W
7,540
7,378
uses
14-119-23 ca
4,350-4,435
1977
OA
7,204
7,308
20
DST
F
16-118-25 cac
0
S
6,880
6,880
uses
17-1 17-1 cbd
0
S
7,000
7,000
10
uses
OTB
18-104-26 ca
2,805-2,820
1969
OA
6,631
6,384
12
DST
e
18-116-6 dda
1 ,005
W
6,620
F6.620+
1
uses
0 TB
18-117-13 dc
0
s
6,900
6,900
5
uses
OTB
18-117-20 cda
0
s
7,000
7,000
100
uses
OTB
21-112-10 cb
1 1,100-11,400
Kf 2
1979
OP
6,724
8,592
32
DST
1'
Cns
f rnm K f 2
23-104-1aa
7 ,944-7,984
1955
OA
6,936
-604
2.5
DST
P
23-104-1 d
7,972-8,050
Kf I
1979
OP
6,911
-542
40
DST
P
Cas
from Kf2, Kf3
23-104-1 d
8,379-8,427
Kf 3
1979
OP
6,911
2,338
7.2
DST
P
Cas
f rom K f 2, K f 3
23-115-6 cc
0
S
7,600
7,600
5
uses
OTB
23-116-28 be
0
S
7,400
7,400
30
uses
OTB
23-116-32 ca
0
5
7,575
7,575
75
uses
OTB
24-113-11 bd
10,116-10,180
1954
OA
6,863
-139
0.07
DST
P
26-111-19 ac
8,298-8,478
Kf2
1978
OS
6,970
7,375
1 .2
DST
F
27-114-4 da
7 ,455-7,512
Kf 2
1971
OP
8,862
3,199
2.5
DST
F
Oil
from Jti
28-112-7 cd
7,442-7,513
Kf 1
1958
OP
7,113
1 ,170
0.41
DST
P
Cas
from Kf
28-112-7 cd
7,811-7,893
Kf 2
1958
OP
7,113
1,124
1 .3
DST
P
G.ts
from Kf
28-115-22 bd
8, 172-8,302
1954
OA
10,057
7,732
10
DST
P
29-115-16 dda
0
S
8,000
8,000
50
uses
OTB
30-1 15-2 .ib
7,555-7,660
Kf 1
1973
OA
8,299
1,957
0.90
DS1
P
34-116-1 I c
0
Kf 7
S
7,500
7,500
20
uses
(MB
35-116-36 b
0
S
7 ,700C)
7,700(9)
25
uses
(MB
40-110-26 ad
3,410-3,417
1964
OA
8,718
6,731
0.21
DS'l
41-112-5 d
0
s
8,375
8,375
Uses
558
BLIND BULL FORMATION - CRETACEOUS
33-U5-4 a
0
s
9,000
9,000+
-
uses
ASPEN (MOWRY)
SHALE - CRETACEOUS
18-117-36 dc
625
u
7,250
F7 ,410
26
uses
OTB
19-116-32 ca
?
Ka?
w
6,575
6,575+
1
uses
OTB
22-115-8 bba
?
Ka?
u
7,350
7,350+
30
uses
OTB
24-113-11 bd
10,236-10,262
Ka
1954
OA
6,863
-1,066
0.94
DST
P
26-112-26 db
8,516-8,700
1957
OA
6,819
3,217
0.53
DST
C
36-117-18 dc
0
S
6,380
6,380
20
uses
OTB
37-117-28 d
0
S
-
-
15
uses
OTB
-------
APPENDIX B
(continued)
Locntion 1
(T-R-Sec-1/4-
Depth*
or
Tested
Interval
1/16) (ft)
GeologLc
Format Ion3
Date
Data
Type
and
Status
or Use
Reference
Point
Elevation5
(ft above
msl)
Potentiometric
Surf ace
Elevat ion6
(ft above
msl)
Well
Yield
)
Spec i f ic
Capacity 7
(Rpm/ft)
Test
Durat ion
(hrs)
Transmissivity 8
(Rpd/ft)
Data
Source9
DST
Validity10
Rema rks
38-116-31
b
0 i
S
^6,200
6,200
8
uses
OTB
38-117-36
b
0
S
6,600
6,600
25
USGS
OTB
39-1 16-14
dbc
111
w
6,000
5,965
3
USGS
OTB
39-116-34
86 (44)
1966
WD
^6 ,000
5,935
17
8.5
1
6,000
SEO
39-i17-10
cd
300
U
6,600
6,482
USGS
OTB
Sp.
Cond. = 600
BEAR RIVER FORMATION - CRETACEOUS
12-110-22
ab
18,369-18,407
Kd
1969
OA
6,787
8,551
2.9
DST
c;
Flowed 5 BPH, f1ot
used
to calculate
14-103-12
be
7,226-7,276
Kd
1952
OA
7,851
7,084
0.08
DST
V
15-104-15
cc
4,533-4,572
Kd
1961
OA
7 ,753
6.530
415?
dst
F
Sail
ualov
15-112-29
ac
12,932-12,978
Kd
1972
OP
6,742
9,643
6.8
DST
n
Pmo
product ion
18-104-26
c a
3,389-3,425
Kd
1969
OA
6,631
6,372
2.2
DST
G
21-115-21
add
Kbr7
W
6,960
F6.960+
5
uses
OTB
23-111-29
aa
1L.487-11,708
Kd
1975
OP
6,535
6,425
4.4
DST
p
Gas
from Kf
24-113-11
bd
11,298-11,348
Kd
1954
OA
6,863
9,059
3.2
DST
G
25-115-14
bac
0
Kbr
S
7,725
7,725
15
USGS
OTB
25-119-25
beb
0
Kbr
s
6,600
6,600
100
uses
OTB
26-113-21
ca
8,397-8,425
Kbr-Kmd
1975
OP
6,862
7,546
1 .8
DST
P
Gas
from Kfl
26-118-4 i
da
0
Kbr7
s
7,000
7,000
10
USGS
OTB
27-111-30
be
9,425-9,5 L 5
Kbr
1978
OP
7,269
9,783
1 .0
DST
C
Gas
fmm Kfl, Kbr
27-113-30
cc
8,875-8,892
Kd
1969
OP
8,366
776
2.9
DST
F
Gas
from Kf
27-113-30
cc
8,885-8,932
Kd
1969
OP
8,366
2,171
2.0
DST
C
C.ns
f rom Kf
27-114-10
cb
8,884-8,965
Kd
1970
OP
8,843
261
5.7
DST
C
Oil
f rom !n
27-115-6 .
d
0
Kbr
s
^8,000
8,000
10
USGS
OTB
28-113-25
cb
8,566-8,605
Kmd
1961
OP
7,650
-139
4.5
DST
C
Gas
from Kf2, Kf3
31-114-4 i
cb
12,486-12,583
Kd
1975
OP
8,422
14,401
5.5
DST
r
Gas
from Kf
33-119-34
cc
0
Kbr
s
6,200
6,200
10
USGS
OTB
34-116-18
d
0
Kbr
s
7,850
7,850
h
USGS
OTB
34-116-19
d
0
Kbr
s
7,400
7,400
15
USGS
OTB
35-117-35
a
0
Kbr
s
6,400
6,400
8
USGS
OTB
36-117-30
dbb
0
Kbr
s
6,950?
6,950
5
USGS
OTB
36-117-31
be
0
Kbr
s
6,500?
6,500
5
USGS
OTB
38-113-9 <
cb
13,006-13,156'
Kd
1971
OA
7,127
7,938
0.64
DST
c
39-116-23
c
80
Kbr
w
6,000
5,956
USGS
OTB
39-116-26
72
Kbr
1964
WD
6,000
5,969
14
2.3
24
2,300
SEO
39-116-26
84
Kbr
1961
WD
6,000
5,969
250
7.8
9
9,500
SEO
39-116-26
100 (53)
Kbr
1968
Wd
5,900
5,896
1
0.3
24
300
SEO
39-116-34
bdd
134
Kbr
W
6,000
5,907
7
USGS
OTB
-------
APPENDIX B
(continued)
W
I
Depth7
Data
Reference
Potent iometrlc
or
Type
Po in t
Surf ace
Tested
and
Elevat ions
E 1 cvat ion 6
Well Specific Test
Locat ion 1
Interval
Geologic
Status
(ft above
(ft above
Yield Capacity7 Duration
Transmissivity8
Da ta
(T-R-Spc-1 nf-
1/16) (ft)
Formation3
Date
or Use1*
nisi)
msl)
(fiptn) (Rpra/fc) (hrs)
(RPti/fc) _ __
Source*3
i
GANNETT GROUP
- CRETACEOUS
J 2-118-15 bb
5,165-5,225
Kg7
1978
OA
9,058
6,836
0.63
DST
14-121-14 dec
665
U
6,910
F6.910+
30
USCS OTB
16-117-2 ca
1 ,390
W
6,620
F6.620+
30
USCS OTB
I 7-119-19 cbe
0
Kg?
S
7 ,070
7,070
40
USCS OTB
17-119-20 ede
0
Kg?
S
7,320
7.320
50
USCS OTB
18-119-31 c be
0
S
6,675
6.675
75
USCS OTB
27-119-10 dab
0
S
7 ,370
7,370
20
USCS OTB
28-116-24 daa
0
S
8,000
8,000
5
USCS OTB
29-1]9-24 abc
0
S
7,000
7,000
35
USCS OTB
30-118-29 bb
?
W
7,075
7,055 7
100
USCS OTB
30-118-35 ac
0
S
7,900
7.900
50
USCS OTB
30-119-12 ac
140
W
7,000
6.960
20
USCS OTB
31-116-18 a
0
S
7,600
7,600
25
USCS OTB
38-115-5 baa
0
S
6,100
6,100
75
USCS OTB
38-116-32 b
0
S
6.000
6,000
10
USCS OTB
41-118-5 d
0
S
6,800
6,800
30
uses OTB
"DAKOTA"
-MORRISON UNDIVIDED - CRETACEOUS/JURASSIC
26-110-33 ac
11 ,432-11 ,555
1978
OP
7,037
-822
8.8
DST
MORRISON FORMATION - JURASSIC
15-111-20 cd
14,695-14,840
1975
OP
6.703
6,741
0.46
DST
STUMP (CURTIS)
FORMATION - JURASSIC
19-112-22 cc
13,845-13,892,
1973
OP
6,389
5,411
2 7
DS1
21-115-32 ad
110
w
6,930
6,890
USCS
21-115-34 ada
110
w
6.800
6,760
uses OTB
22-119-26 cbc
s
7.300
7,300
5
uses OTB
32-119-28 ac
320
w
6,175
6.130
USCS OTB
STUMP OR PREUSS
FORMATIONS - JURASSIC
30-118-32 ab
0
s
7,200
7,200
30
uses OTB
PREUSS
REDBEDS (ENTRADA
SANDSTONE) - JURASSIC
12-103-11 ab
14,285-14,332
1968
OA
9,224
6,249
4.0
DST
16-104-16 dd
3,340-3,346
1973
OP
7,299
6,416
12
DST
17-120-6 ac
100
w
6,450
6,435
USCS OTB
28-119-27 bad
0
s
6,420
6,420
20
USCS OTB
29-119-26 bbc
0
s
7,000
7,000
50
USCS OTB
31-119-8 dd
85
w
6,600
6,5607
USCS OTB
DST
VaI id 1ly1
Pumped ;il 200 «pm
Well also Laps l'w
Gas fI'om Kf
Product ion f rom Kb
Product ion f rom I'm
Black water
Cas from Kd
Also includes (}d
Elevation nppioximatc
-------
APPENDIX B
(continued)
Location
(T-R-Sec-1/4-1/16)
Total
Depth?
or
Tested
Interva1
(ft)
Geologic
Formation3 Date
Data Reference Potentiometric
Type Point Surface
and Elevation5 Elevation6 Well Specific Test
Status (ft above (ft above Yield Capacity7 Duration
or Use*4 msl) msl) (Rpm) (Rpm/ft) (hrs)
Transmiss ivity
(ftpd/ft)
Data DST
Source9 Validity1
13-120-16 ac
26-115-28 da
27-115-16 be
32-]18-6 aa
38-116-20 b
39-117-8 da
i
30,877-10,940
0
0
0
0
8,340-8.440
TWIN CREEK LIMESTONE (CARMEL FORMATION) - JURASSIC
J t c ' 1977
1979
OA
S
S
S
s
OS
7.262
8,550
7,475
6,400
6,000?
7,893
7,245
8,550+
7,475
6,400
6,0007
4,930
75
300
20
60
1 .2
DST
USCS OTB
USCS OTB
USCS OTB
USCS OTB
DST
12-101-3 ac
L3,790-14,253
1964
7 ,06 7
PREUSS (ENTRADA)-NUGGET - JURASSIC
6,783
Has from Kmv
Cd
I
ro
o
14-101-
14-121-
14-121-
15-112-
15-118-
16-104-
17-119-
18-1 16-
19-120-
19-120-
21-119-
22-105-
23-119-
26-115-
26-115-
26-115-
27-113-
27-114-
27-114-
28-113-
18 bb
2 cc
11 ac
29 ac
35 cd
16 dd
18 dc
9 dd
4 cc
4 cc
28 ac
11 be
26 ab
15 cdb
26 aa
26 adc
14 ba
9 ad
10 da
19 bb
10,711-
7,125-
6,655-
14 ,597-
3,413-
3,550-
6,300-
2,410-
5,119-
5,125-
2,816-
14,595-
0
0
0
0
10,128-10,176
11,550
11,371-
10,079-
10,7 70
7,160
6,775
14,643
3,525
3,571
6,672
2,458
5,167
5,450
2,834
14,741
11,472
10,101
28-115-19 abd
29-114-16 cd
29-116-28 beb
30-116-4 c
30-116-9 bb
31-116-22 a
32-115-15 ca
36-116-8 be
37-109-5 ca
37-109-7 db
11,321-13,460
0
0
0
0
4,666-4,706
0
2,542-2,592
3,265-3,346
1975
1976
1976
1972
1977
1973
1977
1977
1978
1978
1977
1975
1957
1959
1962
1979
1958
1955
OA
OP
OA
OP
OA
OP
OP
OA
OA
OA
OA
OA
S
S
S
S
OP
?
OP
OP
S
OA
S
S
S
S
OA
S
OA
OA
7,094
7,113
6,836
6,742
7,260
7,299
7 ,244
6,595
7,069
7,069
7,290
7,693
6,800
8,150
7,750
8,450
7,030
8,389
7,546
8.350
8,529
9,190
8,000
8,600
8,800
8,392
7,000
8,379
8,120
NUGGET SANDSTONE - JURASSIC
6,452
6,431
6,398
3,803
7,169
6,466
6,452
7.297
6,614
6,927
6,576
6.541
6,800 300
8,150
7,750 20
8,450
6,971
6,374
4,046
8,350
6,744
9,190
8,000
8,600
8.800
7,809
7,000
7,848
7,946
75
100
1,400
2.000
200
9.1
10.6
32
3.0
33
15
33
42
1.9
59
66
2.8
25
13
10
2.0
10
37
DST
DST
DST
DST
DST
DST
DST
DST
DST
DST
DST
DST
USGS OTB
USGS
USCS OTB
USCS
DST
USCS OTB
DST
DST
USCS OTB
DST
USCS OTB
USGS OTB
USGS OTB
USCS OTB
DST
USCS OTB
DST
DST
Salt water; gns from Jlc
Salt water
Production from I'm
Salt water
Gas from Kd
Gas from Trt
Salt water
Gas from Kbr
Salt water; g.is from Kf2
Salt water with sulfur
odor and gas from Km, Kf
Fresh water
-------
APPENDIX B
(continued)
Total
Depth7
Data
Reference
Potent lotnetr 1c
or
Type
Point
Sur face
Tested
and
Elevat ion5
Elevation6
Well
Spec i f ic
Test
Locat ion
Interva1
Geologic
Status
(ft above
(ft above
Yield
Capacity 7
Durat ion
Transmissivity0
Data
DST
(T-R-Sec-
1/4-
1/16) (ft)
Formation3
Date
or Use*4
rasl)
msl)
(gpm)
(ftpm/ft)
(hrs)
(f>pd/ft)
Source0
Validity 10
Remarks
1
UNDIFFERENTIATED - TRIASSIC
42-113-19
a
45 (5)
WD
7,125
7,125
] 2
*
2
(10,000)
uses
558
Water estimated at
ground level
ANKAREH FORMATION -
TRIASSIC
16-104-16
dd
4,532-4,570
1973
OP
7,299
6,389
0.47
DST
F
Gas from Kd
29-115-12
cb
0
S
7,820
7,820
200
uses
0TB
THAYNES LIMESTONE - TRLASSIC
20-116-27
dc
4.590-4,662
1973
OA
6,982
7,310
38
DST
F
Salt water
22-118-20
baa
600
Trt?
W
6,700
F6.700+
150
uses
OTB
23-115-27
ac
3,034-3,123
1979
OA
7,183
7,212
0.31
DST
G
24-118-9 i
3CC
0
S
7,075
7,075
10
uses
0TB
27-115-22
b
0
Trt ?
S
8,600?
8,600
900
uses
OTB
30-117-26
a
0
S
8,600?
8,600
50
uses
OTB
31-116-21
a
0
S
8,000?
8,000
350
uses
OTB
32-116-28
c
0
S
-
-
140
USGS
OTB
33-119-23
ab
195
Trt?
u
6,075
6,035
uses
OTB
33-119-23
ac
0
Trt?
s
6,075
6,075
38
uses
OTB
33-119-26
ad
0
Trt?
s
6,050
6,050
5
uses
OTB
38-117-16
d
0
Trt?
s
-
-
1,800
USGS
OTB
44-112-31
a a
7,358-7,445
Trt?
1962
OA
8,193
1,100
8.3
DST
P
May be Trw
DINWOODY FORMATION -
TRIASSIC
15-117-15
cb
3,490-3,495
1964
OA
6,872
7,301
8.8
DST
G
Brackish water wiLh
sulfur odor
30-117-11
dc
0
S
^9,000
^9,000
150
USGS
OTB
D1NW00DY
AND PHOSPHOR1A FORMATIONS - TRIASSIC/PERM1AN
20-116-27
dc
5,534-5,596
1973
OA
6,982
7,381
2.0
DST
G
Blnck sulfur waLur,
test included 20 fI of 1
42-113-24
ba
3,516-3,590
1979
OA
7,225
7,335
3.8
DST
G
Includes 20 fl.o of Pp
PHOSPHORIA (PARK CITY)
FORMATION - PERMIAN
13-118-25
bb
2,560-2,572
1977
OA
7,992
7,275
31
DST
F
Sulphur water
15-104-10
cb
7,038-7,058
1978
OA
7,615
6,247
1.4
DST
P
16-104-16
dd
5,511-5,672
1973
OP
7,299
6,318
6.7
DST
G
Black salt water; gas
from Kd
16-104-16
dd
5,459-5,489
1973
OP
7,299
6,523
12
DST
G
Brackish water; gas
-------
APPENDIX B
(continued)
Depth2
Data
Re ference
Potent iometrIc
or
Type
Po int
Surf ace
Tested
and
Elevat ion 5
Elevation6
Well
Specific
Test
Location
Interval
Geologic
Sta tus
(ft above
(ft above
Yield
Capac ity7
Dura L ion
Transmissivity
Data
DST
(T-R-Sec-
1/4-
1/16) (ft)
Formation3
Date
or Use*4
msl)
IDS 1)
(ftpm)
(Rpm/ft)
(hrs)
(Rpd/ft)
Source 9
Validity10
Remarks
2L-115-21
cc
6,353-16,
420
1977
OA
7,058
7,558
4.6
DST
G
22-117-30
cc
2,285-2,
355
1958
OA
6,903
6,982
1 . 3
DST
G
22-118-20
ad
0
S
6,900
6,900
300
USGS
OTB
22-118-29
aab
530
W
6,700
F6,700+
200
USGS
OTB
22-120-3 i
cd
6,604-6,
877
1979
OA
6,366
6,359
3.4
DST
G
28-113-19
bb
12,653-12
,718
1962
OP
7,546
4,475
0.8
DST
G
Gas from Km, Kf2
38-110-2 :
bd
0
S
7,760
7,760
USGS
38-110-11
ba
0
S
7,750
7,750
USGS
42-113-24
ba
3,600-3,
625
1979
OA
7,225
7,316
34
DST
F
TENSLEEP SANDSTONE (WELLS OR
WEBER FORMATIONS -
PENNSYLVANIAN
12-104-1 7
ca
14,214-14
,295
1976
OA
8.190
6,506
7.0
DST
F
13-118-19
cc
7,670-7,
720
1973
OA
7,592
7,377
23
DST
G
Black salt water
14-301-18
bb
12,771-12
,800
1975
OA
7,094
6,638
0.65
DST
G
15-117-15
cb
3,994-4,
085
1964
OA
6,872
7,208
1-3
DST
G
Brackish water
16-104-16
dd
5,700-5,
756
1973
OP
7,299
6,457
7.2
DST
G
Gas from Kd
21-120-10
da
191
u
6,390
6,348
300
6
10,000?
USGS
OTB
21-120-10
db
299
u
6,380
6,348
700
USGS
OTB
22-105-1 1
be
16,760-16
,901
1975
OA
7,693
-3,6557
14
DST
F
Brackish water
22-117-30
cc
6,580-6,
640
1958
OA
6,903
5,801
0.14
DST
G
26-117-13
bad
0
S
8,030
8,030
USGS
26-118-13
bad
0
S
8,190
8,190
1 ,600
USGS
OTB
29-114-19
bd
14,520-14
,669
1951
OA
9,050
3,757
8.3
DST
F
Brackish to sa1ly
water wiLh gas
29-116-7 1
bb
0
Pw>
S
8,900
8.900
35
USGS
OTB
29-117-1 <
ad
0
S
8,750
8,750
200
USGS
OTB
30-115-8 1
bbd
47
W
9,000
8,973
uses
OTB
30-117-35
c
0
S
8,400
8,400
2,200
USGS
OTB
33-116-11
c
0
s
7,700
7,700
5
USGS
OTB
33-116-12
b
0
s
8,500
8,500
30
USGS
OTB
34-116-10
c
0
s
6,950
6,950
25
USGS
OTB
37-115-31
cb
0
s
8,000
8,000
175
USGS
OTB
37-116-25
a
0
s
7,750
7,750
50
USGS
OTB
37-118-12
b
0
s
6,400
6,400
200
USGS
OTB
41-117-25
ddb
217
w
6,175
6,158
210
uses
OTB
44-112-31
aa
9,425-9,
500
1962
OA
8,193
6,528
38
DST
F
Brackish and fresh
44-113-13
bb
9,685-9,
807
1958
OA
7,710
7,309
9.5
DST
F
44-1J 3-13
bb
9,684-9,
720
1958
OA
7,710
6,434
3.2
DST
F
-------
APPENDIX B
(cont inued)
Total
Depth2
Data
Reference
Potentlometric
or
Type
Po in t
Surface
Tested
and
Elevation5
Elevat ion6
Well
Specific
Test
Location
Interval
Geologic
Status
(ft above
(ft above
Yield
Capacity
Duration
Transmissivity8
Data
DST
(T-R-Sec-
1/4-
1/16) (ft)
Formation3
Date
or Use'1
rasl)
msl)
(«pm)
(gprn/ft)
(hrs)
(Rpd/ft)
Source 9
Validity10
Remarks
1
TENSLEEP AND AMSDEN FORMATIONS
- PENNSYLVANIAN AND
MISS1SS1PPIAN
41-115-1 ¦
c
0
S
7,000
7,000
USGS
558
41-116-12
a
217 (21)
WP
6, 300
6,250?
210
1.5
24
3,000
uses
558
41-117-13
dd
180 (75)
WD
6,200
6,150?
40
336
USGS
558
41-117-25
d
246 (24)
WM
6,175
6,125'
250
1.9
6.5
3,500
USGS
558
AMSDEN
(MORGAN AND
DARWIN) F0R.4AT10N - PENNSYLVAN1AN AND Ml SS1SS1PPI AN
16-104-16
dd
6,150-6,173
1973
OP
7,299
6,385
4.8
DST
G
Gas from Kd
22-117-30
cc
7,500-7,582
3 958
OA
6,903
3,659
0.35
DST
F
23-115-27
ac
6,715-6,808
1979
OA
7,183
7,707
1.3
DST
F
40-110—31
aa
3,121-3,140
1971
OA
9,510
8,077
0.27
DST
F
Includes Darwin SS
41-116-32
acc
80
W
6,175
6,140
8
USGS
0TB
MADISON LIMESTONE - MISSISSIPP1AN
12-104-17
ca
15,840-16,097
1976
OA
8,190
5,851
9.6
DST
P
Sulfur water
19-112-22
cc
18,004-18,128
1973
OP
6,389
13,729
8.7
DST
F
Gas from Pm
22-105-11
be
17,998-18,150
1975
OA
7,693
6,702
20
DST
C
Salty sulfur water
26-114-1 1
bac
0
S
8,000
8,000
4,000
USGS
0TB
26-114-1 .
Jcc
0
s
7,440
7,440
USGS
30-1J 7-24
a
0
s
9,100
9,100
100
USGS
0TB
32-118-25
b
0
s
9,200
9,200
40,000
USGS
0TB
33-118-13
acc
0
s
7,200
7,200
150
USGS
0TB
37-118-34
ded
0
s
-
-
15
USGS
0TB
39—J11-22
b
664
w
8,600
-
-
USGS
39-116-32
daa
0
s
5,175
5,175
350
USGS
0TB
39-116-32
dbd
115
w
5,175
-
100
USGS
0TB
40-116-17
db
212 (20) 1
1965
WD
7,197
7,121
20
5.0
8
4,000?
SEO
Reported as 8-hr test
l-hr pumping with 2-hr
test
41-115-19
d
112
WD
720
140
3
>100,000
USGS
558
41-117-15
aa
104
WD
27
46.3
1
50,000
SEO
4 scp. 1-hr tests
41-117-34
be
75 (8)
1976
WD
6,200
6,165
2.5
0.1
3
<100?
SEO
42-1]3-24
ba
4,647-4,665
1979
OA
7,225
7,226
1.9
DST
G
42-115-12
c
197 (8)
WD
6
0.2
10
400?
USGS
558
44-118-18
bl
670 (582)
WC
30
0.3
15.5
600
USGS
558
44-118-18
b2
676
WC
60
1.5
0.5
2,000
USGS
558
44-118-21
c
307 (40)
WP
466
6.7
8
15,000
USGS
558
Includes Qal, 16" well
44-118-?
0
S?
EPA
Water source for com-
munity of Altn (same
as 44-118-21 c)
-------
APPENDIX B
(continued)
Total
Depth2
Data
Reference
Potentiomctric
or
Type
Po int
Sur face
Tested
and
Elevation5
Elevation*
Well
Specific
Test
Location1 Interval
Geologic
Status
(ft above
(ft above
Yield
Capacity7
Duration
Transmissivlty8
Data
DST
(T-R-Sec-1/4-1/16) (ft)
Format ion3
Date or Use
rasl)
msl)
(Rpm)
(Rpm/ft)
(hrs)
(Rpd/ft)
Source9
Validity10
Remarks
DARBY FORMATION - M ISSISS LPPIAN AND DEVONIAN
28-113-19 bbd
28-J15-20 dca
33-117-24 b
38-115-3 bca
38-115-3 bcb
64
0
0
0
0
7,540
8,350
9,100
6,175
6,175
7, A 96
8,350
9,100
6,175
6,175
5
5
40
900
1,100
USCS OTB
uses
USGS OTB
USGS OTB
USCS OTB
BIGHORN DOLOMITE - ORDOVICIAN
26-1 J 3-7 c
31-117-11 c
34-118-26 aad
35-118-7 cba
Od 35-119-7 cb(7)
J
ro
.e-
37-118-18 aab
7,250
8,200
6,860
6,200
5,780
6,000
7,2 50
8,200
6,860
6,200
5,780
6,000
330
.200
450
250
USGS
USGS OTB
USGS OTB
USGS OTB
EPA
USGS OTB
Water source tor com-
munity of Bedford:
50 ac-ft/yr, or 0.45 rogd
(million gallons/day)
Water source, ETNA
PipelIne Company,
utilizing 0.030 mgd
(million Ra 1lons/day)
Incorrect seciion number?
39-113-7 a 0
41-117-36 caa 0
26-113-7 db
42-117-24 d
^7,400+
6,175
7,400
6,390+
CAMBRIAN - UNDIVIDED
^7,400+
6,175 90
GROS VENTRE FORMATION - CAMBRIAN
7,400 900
PRECAMBRIAN - UNDIVIDED
6,390+
USGS 558
USGS OTB
USGS OTB
-------
APPENDIX B
(continued)
NOTES:
1
For n compLelo description of the well numbering system utilized in this study, see Appendix E.
7
Number in parentheses Indicates perforated interval, where known.
3
Tgwe - Tertiary stratigraphic equivalents of Green River (upper and middle tongues) and Wasatch (Upper and New Fork tongues) formations,
for other abbreviations, refer to Figure 11-4.
''OA = abandoned oil test D = domestic
OP = producing oil well (usually producing from different U = unused
OS « suspended oil well formation) M = miscellaneous
S = spring P = public supply
W - water well C = commercial
WS = stock
5Some elevations estimated from 1:250,000 topographic maps.
6F indicates flowing well; number in parentheses is relation of static water level to reference points.
7* indicates zero drawdown reported.
£0 0See Appendix D for explanation of methodology.
fsj Number in parentheses indicates value calculated from specific capacity with assumed 1 foot of drawdown.
Ln
^Refers to data source, transmissivity and specific capacity for most wells calculated for this report:
USGS = U.S. Geological Survey Data Base
USGS CRB = Welder, 1968
USGS 0TB = Lines and Glass, 1975
USCS 558 = Cox, 1968
SE0 = State Engineer's Office file of permitted domestic wells
DST = Drill Stem Test synopsis (PI cards)
R&B = Robinove and Berry, 1963
EPA = Water Supply Division, U.S. Environmental Protection Agency, 1978
USGS GD/W = Welder and McGrcevy, 1966
I0G = good (i.e., transmissivity probably within ±50%)
F = fair
P - poor t
Question mark indicates questionable data.
-------
APPENDIX
DETERMINATION OF AQUIFER
PROPERTIES
-------
APPENDIX C
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
(1)
= t
S [264 log ( ^-5-) - 65.5]
2693 r S
where: j = 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
C-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.
C-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
2. 3qu , 'o + At
p„ ¦ Po " MS" 1oS ~t (2)
where t = preceding period of flow,
At = time elapsed since flow period,
q = production rate during test,
1J = viscosity of fluid,
k = intrinsic permeability,
h = thickness of producing zone,
p = pressure in the well at time At, and
w
p = undisturbed formation pressure,
o
Bredehoeft (1965) simplified this to
i,v, 2-30(l
kh = a
p 47TAp
(3)
C-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
k = f. m
where K = hydraulic conductivity, and
y = specific weight of water
and then simplified equation (3) to
T = 114 if' <5)
where = average production rate (gal/min),
Ap = pressure change (psi/log cycle of time), and
T = transmissivity (gal/day/ft).
Miller's (1976) simplification requires water with temperatures
less than 45°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 ((t + 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
C-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
2irkh(p - p )
Q = y In (r /r ) '
e w
where Q = productivity,
k = effective permeability,
h = net producing thickness,
p = fluid viscosity at reservoir conditions,
r ,r = drainage and well bore radii, and
e w
Pe»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 (pg - 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(re/rw) = 2tt
for drill stem tests. Equation (6) thus simplifies to
Q ' % <»e -
By rearranging, substituting equation (4), and following Miller's
(1976) assumptions about the fluid, equation (7) is changed to
C-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)
C-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 4^ 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
IFP + FFP
AP = FSIP - ^
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.
C-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.
C-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).
C-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.
C-10
-------
APPENDIX D
CHEMICAL ANALYSES OF GREEN RIVER
BASIN-OVERTHRUST BELT
GROUND WATERS SAMPLED
BY W R R I
-------
Location
Formation
Depth
40-116-25 ca Madison or Quaternary 60'
30-119-12 ac Gannet Group
140'
30-111-31 db
Wasatch
a
i
31-109-10 bd Wasatch
25-106-28 aa Laney
105
WL 30'
260'
23-106-4 acd Tipton
23-107-13 acc Tipton
16-107-22 ddd Wasatch
800-950'
(flowing)
1029'
WL 1005
(was flowing)
990'
WL +289
15-109-10 acc Wasatch
2420'
(flowing)
17-109-2 aba
Wasatch
70'
Owner
Temperature (°C)
Bill Resor 12°
Star Route, Box 391
Wilson, Wyoming 83014
Ken Nebeker 9°
Box 66
Smoot, Wyoming 83126
Town of Big Piney (#2) 9°
Attn. J. W. Wilson
Box 126
Big Piney, Wyoming 83113
Herb Skinner 11°
Box 97
Boulder, Wyoming 8292 3
Wyoming Highway Department 9°
Farson #2
Blair and Hay Land 14°
LS Company
Bureau of Land Management 15°
11°
Northwestern Pipeline 25°
Star Rt. 1
Green River, Wyoming 82935
Uinta Development 8°
c/o Don Lindsley
P. 0. Box 3
Granger, Wyoming 82934
-------
Location
Formation
Depth
Owner
Temperature (°C)
16-114-30 abc Wasatch
0
1
hO
16-114-27 ad
14-116-24 ab
13-119-25 bb
13-119-2 bb
18-116-6 dda
19-105
18-105-7 bab
Bridger
Bridger
Wasatch
Frontier
Frontier
Wasatch
Wasatch
1856
(flowing)
96
WL 70'
90'
38
1005
175'
250'
WL 35
Porter Rollins
Box 335
Lyman, Wyoming 82937
Delmar Gross
Box 368
Lyman, Wyoming 82937
Box 715
Robertson, Wyoming 82944
J. R. Broadbent
Verl G. Lester
P. 0. Box 260
Evanston, Wyoming 82930
Bureau of Land Management
Clear View Acres
James C. Martin
Box 1540
Rock Springs, Wyoming 82901
William Volsik
W Bar K Trailer Court
Star Route, 2 West
Rock Springs, Wyoming 82901
18°
llc
12'
10c
llc
10c
-------
CLI-IO
Chemical a Geological Laboratories
P. O. Box 2794
Caiper, Wyoming
ANALYTICAL REPORT
From Wyoming Water Resources Research Inst. Product Water
Address Laramie, Wyoming Date 5-29-81
Other Pertinent Data
Analyzed by MM,BW,RJ
Date
6-22-81 Lab No.
37649-18
WATER ANALYSIS
40-116-2SCA
Sample taken May 25, 1981
mg/1
Total suspended solids 4.4
Total dissolved solids (calc.) 199
Total dissolved solids (obs.) 110
Conductivity @ 68°F., micromhos 310
Total alkalinity as CaCO^ 179
Total hardness as CaCO. 158
Sodium (Na) (calc.) — 17
Sodium (Na) (obs.) 10
Potassium (K) 2
Calcium. (Ca) 50
Magnesium (Mg) 8
Sulfate (SO,) 7
Chloride (CI) 7
Carbonate (CO.) 38
Bicarbonate (HCO.) —— 141
pH, units 8.5
Aluminum (Al) *
Ammonia (as N) *
Arsenic (As) ND(0.01)
Boron (B) *
Barium (Ba) 0.08
Beryllium (Be) *
Bromide (Br) *
Cation-Anion Balance *
Cadmium (Cd) ND(0.01)
Cyanide (CN) *
mg/1
Chromium (Cr) ND(0,05)
Copper (Cu) *
Fluoride (F) 0.44
Iron (Fe)(total) *
Iron (Fe)(dissolved) *
Lead (Pb) ND(0.05)
Manganese (Mn) *
Mercury (Hg) ND(0.001)
Molybdenum (Mo) *
Nickel (Ni) *
Nitrate (as N) ^(0.01)
Nitrite (as N) *
Phenol3 *
Phosphorus (PO.) *
Selenium (Se) N'D(O.Ol)
Silica (Si02) *
Silver (Ag) ND(0.02)
Sulfide (S) *
Zinc (Zn) *
Vanadium O^Oc) *
Uranium (II 0 j ND(0.001)
Eh, millivolts *
Turbidity (JTU's) *
Oil and grease (Freon Method) - *
Chemical Oxygen Demand (COD) — *
Gross Alpha, pCi/1 4 ± 13
Gross Beta, pCi/1 1 ± 13
Lead-210, pCi/1 *
Polonium-210, pCi/1 *
ND = Not detected at level given in parentheses. Radiochemical tests by Chem. Lab.
* = Test not requested.
Above tests were made in accordance with Standard Mei-hods, 14th Edition, 1975, ASTM, WQO
and AEC methods.
CHEMICAL & GEOLOGICAL LABORATORIES
D-3
-------
CU-IO
Chemical & Geological Laboratories
P. 0. Box 2794
Caspar, Wyoming
ANALYTICAL REPORT
From Wyoming Water Resources Research Inst. produc, Water
Address Laramie, Wyoming Qate 5-29-81
Other Pertinent Data
Analyzed by MM,BW,RJ Date 6-22-81 Lab No. 37649-16
WATER ANALYSIS
30-119-12AC
Sample taken May 25, 1981
mg/I
Total suspended solids 1.2
Total dissolved solids (calc.) 282
Total dissolved solids (obs.) 318
Conductivity @ 68°F., micromhos 390
Total alkalinity as CaCO, 248
Total hardness as CaCO, 264
Sodium (Na) (calc.) 7
Sodium (Na) (obs.) 8
Potassium (K) 1
Calcium (Ca) 86
Magnesium (Mg) 12
Sulfate (SO,) 16
Chloride (CI) 11
Carbonate (CO.) 48
Bicarbonate (HCO,) 205
pH, units' 8. 6
Aluminum (Al) *
Ammonia (as N) *
Arsenic (As) ND(O.Ol)
Boron (B) *
Barium (Ba) 0.22
Beryllium (Be) *
t Bromide (Br) *
Cation-Anion Balance *
Cadmium (Cd) ND(0.01)
Cyanide (CN) *
Chromium (Cr) ND(O.OS)
Copper (Cu) *
Fluoride (F) 0.26
Iron (Fe)(total) *
Iron (Fe)(dissolved) *
Lead (Pb) ND(0.05)
Manganese (Mn) *
Mercury (Hg) ND(0.001)
Molybdenum (Mo) *
Nickel (Ni) *
Nitrate (as N) 4.92
Nitrite (as N) *
Phenols *
Phosphorus (PO,) *
Selenium (Se) ND(0.01)
Silica (SiO.) *
Silver (Ag) ND(0.02)
Sulfide (S) *
Zinc (Zn) *
Vanadium *
Uranium (V.6.) ND(0.001)
Eh, millivolts *
Turbidity (JTU's) *
Oil and grease (Freon Method) - *
Chemical Oxygen Demand (COD) — *
Radium-226, pCi/1 0.0 ± 0.1
Gross Alpha, pCi/1 0 ± 3
Thorium-230,PpCi/l *
Lead-210, pCi/1 *
Polonium-210, pCi/1 *
ND = Not detected at level given in parentheses. Radiochemical tests by Chem. Lab.
* = Test not requested.
Above tests were made in accordance with Standard Methods. 14th Edition, 1975, ASTM, WQO
and AEC methods.
CHEMICAL & GEOLOGICAL LABORATORIES
ijvfi. Monsik
D-4
-------
CU-IO
Chemical & Geological Laboratories
P. O. Box 2794
Caiper, Wyoming
ANALYTICAL REPORT
From Wyoming Water Resources Research Inst. produc, Water
Address Laramie, Wyoming Date 5-29-81
Other Pertinent Data
Analyzed by MM,BW,RJ
Date
6-22-81 Lab No.
37649-15
WATER ANALYSIS
30-111-31DB
Sample taken May 26, 1981
mg/l
Total suspended solids 3.2
Total dissolved solids (calc.) 582
Total dissolved solids (obs.) 490
Conductivity @ 68°F., micromhos 780
Total alkalinity as CaCO, 329
Total hardness as CaCO. 24
Sodium (Na) (calc.) 217
Sodium (Na) (obs.) 217
Potassium (K) 1
Calcium (Ca) 8
Magnesium (Mg) 1
Sulfate (SO.) 142
Chloride (CI) 16
Carbonate (CO..) 41
Bicarbonate (HCO.) 317
pH, units 9.0
Aluminum (Al) *
Ammonia (as N) *
Arsenic (As) 0.01
Boron (B) *
Barium (Ba) ND(0.05)
Beryllium (Be) *
Bromide (Br) *
Cation-Anion Balance *
Cadmium (Cd) ND(0.01)
Cyanide (CN) *
mg/1
Chromium (Cr) ND(0.05)
Copper (Cu) »
Fluoride (F) 0.73
Iron (Fe)(total) *
Iron (Fe)(dissolved) *
Lead (Pb) ND(0.05)
Manganese (Mn) *
Mercury (Hg) ND(0.001)
Molybdenum (Mo) *
Nickel (Ni) *
Nitrate (as N) ND(0.01)
Nitrite (as N) *
Phenols *
Phosphorus (PO^) *
Selenium (Se) ND(0.01)
Silica (Si02) *
Silver (Ag) ND(0.02)
Sulfide (S) .
Zinc (Zn) *
Vanadium (V_0 ) *
Uranium (I) 0j ND(0.001)
Eh, millivolts *
Turbidity (JTU's) *
Oil and grease (Freon Method) - *
Chemical Oxygen Demand (COD) — *
Radium-226, pCi/1 0.3 ± 0.2
Gross Alpha, pCi/1 10 ± 4
Thorium-230, pCi/1 *
Polonium-210, pCi/1 *
ND = Not detected at level given in parentheses. Radiochemical tests by Chem. Lab.
* = Test not requested.
Above tests were made in accordance with Standard Methods, 14th Edition, 1975, ASTM, WQO
and AEC methods.
CHEMICAL & GEOLOGICAL LABORATORIES
D-5
-------
CI-l-IO
Chemical & Geological Laboratories
P. O. Box 2794
Ctiper, Wyoming
ANALYTICAL REPORT
From Wyoming Water Resources Research Inst. product Water
Address Laramie, Wyoming, Date 5-29-81
Other Pertinent Data
Analyzed by MM,BW,RJ Date ..6722,78! _ Lab No.. , 376^9-17
WATER ANALYSIS
31-109-10BD
Sample taken May 26, 1981
mR/1
Total suspended solids 0.8
Total dissolved solids (calc.) 149
Total dissolved solids (obs.) 118
Conductivity @ 68°F., micromhos 200
Total alkalinity as CaCO. 128
Total hardness as CaCO. 104
Sodium (Na) (calc.) 18
Sodium (Na) (obs.) 17
Potassium (K) 2
Calcium (Ca) — 30
Magnesium (Mg) 7
Sulfate (SO,) 10
Chloride (CI) 5
Carbonate (CO.) 0
Bicarbonate (HCO.) 156
pH, units 8.2
Aluminum (Al) — *
Ammonia (as N) *
Arsenic (As) ND(0.01)
Boron (B) *
Barium (Ba) 0.08
Beryllium (Be) *
Bromide (Br) *
Cation-Anion Balance *
Cadmium (Cd) — ND(0.01)
Cyanide (CN) *
Chromium (Cr) —r ND(0.05)
Copper (Cu) *
Fluoride (F) 0.26
Iron (Fe)(total) *
Iron (Fe)(dissolved) *
Lead (Pb) — ND(0.05)
Manganese (Mn) *
Mercury (Hg) ND(0.001)
Molybdenum (Mo) *
Nickel (Ni) *
Nitrate (as N) 0.24
Nitrite (as N) *
Phenols *
Phosphorus (PO.) *
Selenium (Se) ND(0.01)
Silica (SiO.) *
Silver (Ag) ND(0.02)
Sulfide (S) *
Zinc (Zn) *
Vanadium (V O ) —— *
Uranium (U..0.J 0.005
Eh, millivolts *
Turbidity (JTU's) *
Oil and grease (Freon Method) - *
Chemical Oxygen Demand (COD) — *
Radium-226, pCi/1 ¦: 0.0 ± 0.1
Gross Alpha, pCi/1 2 + 1
Gross Beta, pCi/1 1 + 3
Thorium-230, pCi/1 *
Lead-210, pCi/1 *
Polonium-210, pCi/1 *
ND = Not detected at level given in parentheses. Radiochemical tests by Chem. Lab.
* = Test not requested.
Above tests were made in accordance with Standard Methods, 14th Edition, 1975, ASTM, WQO
and AEC methods.
CHEMICAL £. GEOLOGICAL LABORATORIES
D-6
-------
CLI-IO
Chemical a Geological Laboratories
P. 0. Box 2794
Ctiper, Wyoming
ANALYTICAL REPORT
From Wyoming Water Resources Research InstProduct Water
Address Laramie, Wyoming Date 5-29-81
Other Pertinent Data
Analyzed by MM,BW,RJ .Date 6-22-81 Lab No. 37649-14
WATER ANALYSIS
25-106-28AA
Sample taken May 27, 1981
"»r/1
mg/1
Total suspended solids 0.4
Total dissolved solids (calc.) 663
Total dissolved solids (obs.) 606
Conductivity @ 68°F., micromhos 850
Total alkalinity as CaCO, 225
Total hardness as CaCO, 245
Sodium (Na) (calc.) — 138
Sodium (Na) (obs.) 133
Potassium (K) 2
Calcium (Ca) 75
Magnesium (Mg) 14
Sulfate (SO.) 267
Chloride (CI) 32
Carbonate (CO.) 34
Bicarbonate (HCO.,) 205
pH, units 9.0
Aluminum (Al) *
Ammonia (as N) *
Arsenic (As) ND(0.01)
Boron (B) *
Barium (Ba) ND(0.05)
Beryllium (Be) *
Bromide (Br) *
Cation-Anion Balance *
Cadmium (Cd) ND(0.01)
Cyanide (CN) *
Chromium (Cr)
Copper (Cu)
Fluoride (F)
Iron (Fe)(total)
Iron (Fe)(dissolved)
Lead (Pb)
Manganese (Mn)
Mercury (Hg)
Molybdenum (Mo)
Nickel (Ni)
Nitrate (as N)
Nitrite (as N)
Phenols
ND(0.05)
0.54
ND(0,05)
*
ND(0.001)
.26
Phosphorus (PO^)
Selenium (Se) ND(0.01)
Silica (Si02)
Silver (Ag) ND(0.02)
Sulfide (S)
Zinc (Zn)
Vanadium (V O5)
Uranium (U.O J o.Oll
Eh, millivolEs
Turbidity (JTU's)
Oil and grease (Freon Method) -
Chemical Oxygen Demand (COD) —
Radium-226, pCi/1 0.0 + 0.1
Gross Alpha, pCi/1 8 + 3
Lead-210, pCi/1 *
Polonium-210, pCi/1 *
ND = Not detected at level given in parentheses. Radiochemical tests by Chem. Lab.
* = Test not requested.
Above tests were made in accordance with Standard Methods. 14th Edition, 1975, ASTM, WQO
and AEC methods.
CHEMICAL 4 GEOLOGICAL LABORATORIES
D-7
-------
CLMO
Chemical & Geological Laboratories
P. O. Box 2794
Cliper, Wyoming
ANALYTICAL REPORT
From Wyoming Water Resources Research Inst. Product Water
Address Laramie, Wyoming Date 5-29r81
Other Pertinent Data
Analyzed by .MM.BWJU Date 6-22-81 |.ab No. 37649-12
WATER ANALYSIS
23-106-4ACD
Sample taken May 27, 1981
mg/1
Total suspended solids 0.4
Total dissolved solids (calc.) 797
Total dissolved solids (obs.) 740
Conductivity 0 68°F., micromhos 1075
Total alkalinity as CaCO^ 414
Total hardness as CaCO.. 7
Sodium (Na) (calc.) 30S
Sodium (Na) (obs.) 298
Potassium (K) 1
Calcium (Ca) 1
Magnesium (Mg) 1
Sulfate (SO.) 222
Chloride (CI) 19
Carbonate (CO.) 84
Bicarbonate (HCO,) 334
pH, units 9.2
Aluminum (Al) *
Ammonia (as N) *
Arsenic (As) ND(0.01)
Boron (B) *
Barium (Ba) ND(0.05)
Beryllium (Be) ——— *
Bromide (Br) *
Cation-Anion Balance *
Cadmium (Cd) ND(0.01)
Cyanide (CN) *
Chromium (Cr) ND(0.05]
Copper (Cu) *
Fluoride (F) 6.25
Iron (Fe)(total) *
Iron (Fe)(dissolved) *
Lead (Pb) ND(0.05)
Manganese (Mn) *
Mercury (Hg) ND(O.OOl)
Molybdenum (Mo) *
Nickel (Ni) *
Nitrate (as N) 0.03
Nitrite (as N) *
Phenols *
Phosphorus (P0.) *
Selenium (Se) ND(0.01)
Silica (SiO.) *
Silver (Ag) ND(0.02j
Sulfide (S) *
Zinc (Zn) *
Vanadium (V 05) *
Uranium (U,0R) ND(0.001)
Eh, millivolts *
Turbidity (JTU's) *
Oil and grease (Freon Method) - *
Chemical Oxygen Demand (COD) — *
Radium-226, pCi/1 0.2 ± 0.1
Gross Alpha, pCi/1 4 ± 3
Gross Beta, pCi/1 2 ± 5
Lead-210, pCi/1 *
Polonium-210, pCi/1 *
ND = Not detected at level given in parentheses. Radiochemical tests by Chem. Lab.
* " Test not requested.
Above tests were made in accordance with Standard Methods. 14th Edition, 1975, ASTM, WQO
and AEC methods.
CHEMICAL & GEOLOGICAL LABORATORIES
-------
CLI-IO
chemical a Geological laboratories
P. O. Box 2794
Cuper, Wyoming
ANALYTICAL REPORT
From Wyoming Water Resources Research Inst. procjuct Water
Address Laramie, Wyoming , Date S-29-81
Other Pertinent Data
AntJyzecf- by .MM,BW,RJ Date 6-22-81 Lab No. 37649-13
WATER ANALYSIS
23-107-13ACC
Sample taken May 27, 1981
Total¦suspended splids ND(0.4)
Total dissolved solids'(calc.) 1320
Total dissolved solids (obs.) 1248
Conductivity @ 68°F., micromhos 1825
Total alkalinity as CaCO^ 890
Total hardness as CaCO. 7
Sodium (Na) (calc.) 532
Sodium (Na) (obs.) —• 526
Potassium (K) 1
Calcium. (Ca) 1
Magnesium (Mg) — 1
Sulfate (SO.) 211
Chloride (CI) 40
Carbonate (CO.) 308
Bicarbonate (HCO^) < ¦— 4SS
Aluminum (Al) *
Ammonia (as N) *
Arsenic (As) ND(0.01)
Boron (B) *
Barium (Ba) ND(0.05)
Beryllium (Be) *
Bromide (Br) *
Cation-Anion Balance *
Cadmium (Cd) ND(0.01)
Cyanide (CN) *
Mg/1
Chromium (Cr)' ND(0.05)
Copper (Cu) - *
Fluoride (F) 8.50
Iron (Fe)(total) *
Iron (Fe)(dissolved) *
Lead (Pb) ND(0.05)
Manganese (Mn) *
Mercury (Hg) ND(0.001)
Molybdenum (Mo) *
Nickel (Nl) *
Nitrate (as N) ND(0.01)
Nitrite (as N) *
Phenols — — *
Phosphorus (PO^) *
Selenium (Se) ND(0.01)
SUica (Si02) —— .*
Silver (Ag) = ND(0.02)
Sulfide (S) *
Zinc (Zn) *
Vanadium (VjOc) *
Uranium (111) ND(0.001)
Eh, millivolts *
Turbidity (JTU's) *
Oil and grease (Freon Method) - *
Chemical Oxygen Demand (COD) — *
Gross Alpha, pCi/1 4 ± 8
Gross Beta, pCi/1 13 ± 10
Thorium-230, pCi/1 *
Lead-210, pCi/1 *
Polonium-210, pCi/1 *
ND = Not detected at level given in parentheses. Radiochemical tests by Chem. Lab.
* = Test not requested.
Above tests were made in accordance with Standard Methods. 14th Edition, 1975, ASTM, WQO
and AEC methods.
CHEMICAL & GEOLOGICAL LABORATORIES
-------
CLI-IO
Chemical & Geological Laboratories
P. O. Box 2794
Cuper, Wyoming
ANALYTICAL REPORT
From Wyoming Water Resources Research Inst. product Water
Address Laramie, Wyoming Date 5-29-81
Other Pertinent Data
Analyzed by MM,BW,RJ 6-22-81 |_a^ fvj0_ 37649-5
WATER ANALYSIS
16-107-22DDD
Sample taken May 19, 1981
mg/1
Total suspended solids 2.0
Total dissolved solids (calc.) 1102
Total dissolved solJ.ds (obs.) 1Q16
Conductivity @ 68°F., micromhos 1525
Total alkalinity as CaCO. 815
Total hardness as CaCO. 22
Sodium (Na) (calc.) 446
Sodium (Na) (obs.) 436
Potassium (K) 2
Calcium (Ca) 7
Magnesium (Mg) 1
Sulfate (SO.) 115
Chloride (CI) 42
Carbonate (CO.) 144
Bicarbonate (HCO..) 701
pH, units 8.8
Aluminum (AX) *
Ammonia (as N) —¦ *
Arsenic (As) ND(0.01)
Boron (B) *
Barium (Ba) ND(0.05)
Beryllium (Be) *
Bromide (Br) *
Cation-Anion Balance *
Cadmium (Cd) ND(0.01)
Cyanide (CN) *
mg/1
Chromium (Cr) ND(0.05).
Copper (Cu> *
Fluoride (F) 2,15
Iron (Fe)(total) *
Iron (Fe)(dissolved) *
Lead (Pb) ND(0.05)
Manganese (Mn) *
Mercury (Hg) ND(O.OOl)
Molybdenum (Mo) *
Nickel (Ni) *
Nitrate (as N) 0.12
Nitrite (as N) *
Phenols *
Phosphorus (PO,) *
Selenium (Se) ND(0.01)
Silica (SiO,) *
Silver CAg) ND(0.02)
Sulfide (S) *
Zinc (Zn) *
Vanadium (f OJ *
Uranium (U 0 J ND(O.OOl)
Eh, millivolts *
Turbidity (JTU's) *
Oil and grease (Freon Method) - *
Chemical Oxygen Demand (COD) — *
Radium-226, pCi/1
Gross Alpha, pCi/1
Gross Beta, pCi/1
Thorlum-230, pCi/1
Lead-210, pCi/1
Polonium-210, pCi/1
ND = Not detected at level given in parentheses. Radiochemical tests by Chem. Lab.
* = Test not requested.
Above tests were made in accordance with Standard Methods, 14th Edition, 1975, ASTM, WQO
and AEC methods.
0 ± 0
CHEMICAL & GEOLOGICAL LABORATORIES
C-10
-------
CLI-10
Chemical a Geological Laboratories
P. O. Box 2794
Coper, Wyoming
ANALYTICAL REPORT
From Wyoming Water Resources Research Inst. procjuct Water
Address Laramie, Wyoming Date 5-29-81
Other Pertinent Data
Analyzed by MM.BW.RJ Date 6-22-81 Lab No. 37649-4
MATER ANALYSIS
15-109-10ACC
Sample taken May 20, 1981
Total suspended solids
Total-dissolved solids (calc.)
Total dissolved colid^ (obs.)
Conductivity @ 68°F. , micromhos
Total alkalinity as CaCO^
Total hardness as CaCO.
Sodium (Na) (calc.)
Sodium (Na) (obs.)
Potassium (K)
Calciuir (Ca)
Magnesium (Mg)
Sulfate (SO.) —
Chloride (CI)
Carbonate (CO.)
Bicarbonate (HCO.,)
pH, units- ¦ ¦¦ ¦
Aluminum (Al)
Ammonia (as N)
Arsenic (As)
Boron (B)
Barium (Ba)
0.02
0.05
Beryllium (Be) *
Bromide (Br) *
Cation-Anion Balance *
Cadmium (Cd) ND(0.01)
Cyanide (CN) *
Chromium (Cr)
Cppper (Cu) —
riuoridfe (r) ——--
Iron (Fe)(total)
Iron (Fe)(dissolved)
Lead (Pb)
Manganese (Mn)
Mercury (Hg)
Molybdenum (Mo) —
Nickel (Ni)
Nitrate (as N)
Nitrite (as N)
Phenols
Phosphorus (PO,)
Selenium (Se)
3il*«a (-SiO.)
Silver (Ag)
Sulfide (S)
Zinc (Zn)
Vanadium (V.O,.)
Uranium (U.O.;
Eh, millivolts
Turbidity (JTU's)
Oil and, grease (Freon Method) -
Chemical Oxygen Demand (COD) —
mg/1
ND(0,05)
*
.26
ND(0.0S)
*
ND (0.001)
*
*
ND(0.01)
.02
.02
ND(0.001)
Radium-226, pCi/1 4.0 ± 0.5
Gross Alpha, pCi/1 0 ± 0
Gross Beta, pCi/1 15 ± 47
Thorium-230, pCi/1
Lead-210, pCi/1
Polonium-210, pCi/1
ND = Not detected at level given in parentheses. Radiochemical tests by Chem. Lab.
* = Test not requested.
Above tests were made in accordance with Standard Methods, 14th Edition, 1975, ASTM, WQO
and AEC methods.
CHEMICAL & GEOLOGICAL LABORATORIES
\.[j. Mcnsik
D-ll
-------
CLI-IO
Chemical & Geological Laboratories
P. O. Box 2794
Coper, Wyoming
ANALYTICAL REPORT
From Wyoming Water Resources Research Inst. product Water
Address Laramie, Wyoming pate 5-29-81
Other Pertinent Data
Analyzed by MM,BW,RJ pate 6-22-81 Lab nd 37649-8
WATER ANALYSIS
17-109-2ABA
Sample ta-ken May 21, 1981
mg/1
Total. suspended solids 0.8
Total dissolved solids (calc.) 1861
Total dissolved solids (obs.) 1902
Conductivity @ 68°F., micromhos 2225
Total alkalinity as CaCO^ 255
Total hardness as CaCO^ 807
Sodium (Na) (calc.) 312
Sodium (Na) (obs.) 311
Potassium (K) 4
Calcium (Ca) 213
Magnesium (Mg) 67
Sulfate (SO,) 900
Chloride (CI) 212
Carbonate (CO.) 60
Bicarbonate (HCO^) 189
pH, units — 8.5
Aluminum (Al) *
Ammonia (as N) *
Arsenic (As) ND(0.01)
Boron (B) *
Barium (Ba) ND(O.OS)
Beryllium (Be) *
Bromide (Br) *
Cation-Anion Balance *
Cadmium (Cd) ND(O.Ol)
Cyanide (CN) *
mg/1
Chromium (Cr) ND(O.OS)
Copper (Cu) *
Fluoride (F) 0.31
Iron (Fe)(total) *
Iron (Fe)(dissolved) *
Lead (Pb) 0.06
Manganese (Mn) *
Mercury (Hg) ND(0.001)
Molybdenum (Mo) *
Nickel (Ni) *
Nitrate (as N) 0.06
Nitrite (as N) *
Phosphorus (PO.) *
Selenium (Se) ND(0.01)
Silica (SiO,) *
Silver (Ag) ND(0.02)
Sulfide (S) r *
Zinc (Zn) *
Vanadium (V O,) *
Uranium (U-O.) 0.007
Eh, millivolts *
Turbidity (JTU's) *
Oil and grease (Freon Method) -
Chemical Oxygen Demand (COD) —
Radium-226, pCi/1 0.2 ± 0.1
Gross Alpha, pCi/1 5 ± 10
Gross Beta, pCi/1 10 ± 12
Thorium-230, pCi/1 *
Lead-210, pCi/1 *
Polonium-210, pCi/1 *
ND = Mot detected at level given in parentheses. Radiochemical tests by Chem. Lab.
* = Test not requested.
Above tests were made in accordance with Standard Methods. 14th Edition, 1975, ASTM, WQO
and AEC methods.
CHEMICAL & GEOLOGICAL LABORATORIES
D-12
-------
CLI-tO
Chemical & Geological Laboratories
P. O. Box 2794
Catper, Wyoming
ANALYTICAL REPORT
From Wyoming Water Resources Research Inst. Product Water
Address Laramie, Wyoming . Date 5-29-81
Other Pertinent Data
Analyzed by MMjBW,RJ Date 6-22-81 Lab 37649-7
MATER ANALYSIS
16-114-30ABC
Sample taken May 20, 1981
pr/1
Total suspended solids 2.0
Total dissolved solids (calc.) 1618
Totcl dissolved sciids (obs.) 1512
Conductivity @ 68°F., micromhos 2225
Total alkalinity as CaCO, 355
Total hardness as CaCO, 41
Sodium (Na) (calc.) 581
Sodium (Na) (obs.) 552
Potassium (K) 1
Calcium (Ca) 13
Magnesium (Mg) 2
Sulfate (SO.) 512
Chloride (CI) 296
Carbonate (CO,) 78
Bicarbonate (ECO.) 274
pH, units —*»•* " . — ¦ ¦ 8.7
Aluminum (Al) *
Ammonia (as N) *
Arsenic (As) ND(0.01)
Boron (B) *
Barium (Ba) 0.08
Beryllium (Be) *
Bromide (Br) *
Cation-Anion Balance *
Cadmium (Cd) ND(0.01)
Cyanide (CN) *
mg/1
Chromium (Cr) ND(0.05)
Copper (Cu) *
Fluoride (F) 1.22
Iron (Fe)(total) *
Iron (Fe)(dissolved) *
Lead (Pb) ND(0.05)
Manganese (Mn) *
Mercury (Hg) ND(0.001)
Molybdenum (Mo'* *
Nickel (Ni) *
Nitrate (as N) 0.07
Nitrite (as N) *
Phenols *
Phosphorus (PO.) *
Selenium (Se) ND(0.01)
SMica (S102> *
Silver (Ag) ND(0.02)
Sulfide (S) *
Zinc (Zn) *
Vanadium (V?0,) *
Uranium (U 6.) ND(0.001)
Eh, millivolts *
Turbidity (JTU's) *
Oil anc grease (Freon Method) - *
Chemical Oxygen Demand (COD) — *
Radium-226, pCi/1 0.5 ± 0.2
Gross Alpha, pCi/1 8 + 11
Gross Beta, pCi/1 21 ± 13
Thorium-230, pCi/1 : *
Lead-210, pCi/1 *
Polonium-210, pCi/J. *
ND = Not detected at level given in parentheses. Radiochemical tests by Chem. Lab.
* = Test not requested.
Above tests were made in accordance with Standard Methods. 14th Edition, 1975, ASTM, WQO
and AEC methods.
CHEMICAL & GEOLOGICAL LABORATORIES
D-13
-------
CUI-IO
Chemical & Geological Laboratories
P. O. Box 2794
Caspar, Wyoming
ANALYTICAL REPORT
From Wyoming Water Respurces Research Inst. product
Address. Laramie, Wyoming Date
Other Pertinent Data
Water
5-29-81
Analyzed by MM,BW,RJ
Date
6-22-81' Lab No. 37649-6
WATER ANALYSIS
16-114-27AD
Sample taken May 20, 1981
as/i-
Total suspended solids 1.2
Total dissolvpd solids (calc.) 2051
Total dissolved solids (obs.) 1910
Conductivity @ 68°F., micromhos 257S
Total alkalinity as CaCO^ 64
Total hardness as CaCO, 135
Sodium (Na) (calc.) 636
Sodium (Na) (obs.) 583
Potassium (K) 1
Calcium (Ca) 49
Magnesium (Mg) 3
Sulfate (SO.) 1110
Chloride (Cl) 214
Carbonate (CO,*) 0
Bicarbonate (HCO.) 78
pH, units 8.0
Aluminum (Al) *
Ammonia (as N) *
Arsenic (As) ND(0.01)
Boron (B) *
Barium (Ba) ND(0.05)
Beryllium (Be) *
Bromide (Br) *
Cation-Anion Balance *
Cadmium (Cd) ND(O.Ol)
Cyanide (CN) *
ng/J-
Chromium (Cr) ND(0.05) ,
Copper (Cu) *
.Fluoride (F) 4.41
Iron (Fe)(total) *
Iron (Fe)(dissolved) *
Lead (Pb) ND(O.OS)
Manganese (Mn) *
Mercury (Hg) ¦ ND(O.OOl)
Molybdenum (Mo) —— *
Nickel (Ni) *
Nitrate (as N) 1.52
Nitrite (as N) *
Phenols *
Phosphorus ¦¦ »
Selenium (Se) o.oi
Silica (Si02) *
Silver (Ag) ND(0.02)
Sulfide (S) *
Zinc (Zn) «
Vanadium (v2°5^ *
Uranium (U,6J ND(O.OOl)
Eh, millivolts *
Turbidity (JTU's)
Oil and grease (Freon Method) -
Chemical Oxygen Demand (COD) —
Radium-226, pCi/1 0.1 ± 0.2
Gross Alpha, pCi/1 0 + 0
Gross Beta, pCi/1 2 ± 4
Thori-um-239i pCi/1 — — *
Lead-210, pCi/1 *
Polonium-210, pCi/1 *
ND = Not detected at level given in parentheses. Radiochemical tests by Chem. Lab.
* = Test not requested.
Above tests were made in accordance with Standard Methods. 14th Edition, 1975, ASTM, WQ0
and AEC methods.
CHEMICAL & GEOLOGICAL LABORATORIES
D-14
-------
CLl-IO
Chemical & Geological Laboratories
P. O. Box 2794
Caspar, Wyoming
ANALYTICAL REPORT
From Wyoming Water Resources Research Inst. Product .Water
Address Laramie, Wyoming Date 5-29-81
Other Pertinent Data
Analyzed by
Date:
_6r22-81 i_a5 n0. 37649-3
WATER ANALYSIS
14-116-24AB
Sample taken May 22, 1981
mR/1
Total suspended solids 0.4
Total dissolved solids (calc.) 269
Total dissolved solids (obs.) 248
Conductivity <3 68°F., micromhos 400
Total alkalinity as CaCO. 129
Total hardness as CaCO- 19
Sodium (Na) (calc.) 96
Sodium (Na) (obs.) 101
Potassium (K) 1
Calcium (Ca) 6
Magnesium (Mg) 1
Sulfate (SO.) 61
Chloride (CI) 27
Carbonate (COO 22
Bicarbonate (HCO.) 112
pH, units 8.7
Aluminum (Al) *
Ammonia (as N) *
Arsenic (As) ND(0.01)
Boron (B) *
Barium (Ba) ND(O.OS)
Beryllium (Be) *
Bromide (Br) *
Cation-Anion Balance *
Cadmium (Cd) NO(0.01)
Cyanide (CN) *
Chromium (Cr) . ND(0.0S)
Copper (Cu) *
Fluoride (F) 0.82
Iron (Fe)(total) *
Iron (Fe)(dissolved) *
Lead (Pb) ND(0.05)
Manganese (Mn) *
Mercury (Hg) ND(0.001)
Molybdenum (Mo) *
Nickel (Ni) *
Nitrate (as N) ND(0.01)
Nitrite (as N) *
Phosphorus (PO^) *
Selenium (Se) ; ND(O.Ol)
Silica (Si02) *
Silver (Ag) ND(0.02)
Sulfide (S) *
Zinc (Zn) *
Vanadium (V 0^) *
Uranium (U.O.J ND (0.001)
Eh, millivolts *
Turbidity (JTU's)
Oil and grease (Freon Method) -
Chemical Oxygen Demand (COD) —
Radium-226, pCi/1 0.1 ± 0.1
Gross Beta, pCi/1 0 ± 4
Thorium-230, pCi/1 *
Lead-210, pCi/1 *
Polonium-210, pCi/1 *
ND = Not detected at level given in parentheses. Radiochemical tests by Chera. Lab.
* = Test not requested.
Above tests were made in accordance with Standard Methods, 14th Edition, 1975, ASTM, WQ0
and AEC methods.
CHEMICAL & GEOLOGICAL LABORATORIES
. Mensik
D-15
-------
CLI.tO
Chemical .& Geological Laboratories
P. O. Box 2794
Ceipor, Wyoming
ANALYTICAL REPORT
From Wyoming Water Resources Research Inst. product.
Address . Laramie, Wyoming patB
Other Pertinent Data
Water
5-29-81
Analyzed by MM,BW,RJ
Date
6-22-81
Lab No.
37649-2
WATER ANALYSIS
13-119-25BB
Sample taken May 22, 1981
mg/1
Total suspended solids 0.8
Total dissolved solids (calc.) 331
local disboiveu soi±us (obs.) l^o
Conductivity @ f^F., micromhos 500
Total alkalinity as CaCO. 297
301
18
Total hardness as CaCO^ —
Sodium (Na) (calc.)
Sodium (Na) (obs.)
Potassium (K)
Calcium (Ca) —
Magnesium (Mg)
Sulfate (SO.)
Chloride (CI)
Carbonate (CO,j
10
2
58
38
17
20
46
268
8.6
Bicarbonata, <-pco.3)
pH, units
Aluminum (Al) *
Ammonia (as N) *
Arsenic (As) ND(0.01)
Boron (B) *
Barium (Ba) 0.20
Beryllium (Be)
Bromide (Br) *
Cation-Anion Balance *
Cadmium (Cd) ND(0.01)
Cyanide (CN) *
Chromium (Cr)
Copper (Cu)
Fluoride IF)
Iron (Fe) (total)
Iron (Fe)(dissolved)
Lead (Pb)
Manganese (Mn)
Mercury (Hg)
Molybdenum (Mo)
Nickel (Ni)
Nitrate (as N)
Nitrite (as N)
Phenols : .
Phosphorus (PO.)
Selenium (Se)
Silica (SiO.)
Silver (Ag)
Sulfide (S) r
Zinc (Zn)
Vanadium (V,0_)
Uranium (U,60)
Eh, milliv3l?s
Turbidity (JTU's)
Oil and grease (Freon Method)
Chemical Oxygen Demand (COD) -
ND(0.0S)
ND (0.001)
.77
D(0.01)
D(0.02)
.004
Radium-226, pCi/1
Gross Alpha, pCi/1
Gross Beta, pCi/1
Thorium-230, pCi/1
Lead-210, pCi/1
Folonium-210, pCi/1
2.9 ± 0.4
9 ± 3
ND = Not detected at level given in parentheses. Radiochemical tests by Chem. Lab.
* = Test not requested.
Above tests were made in accordance with Standard Methods, 14th Edition, 1975, ASTM, WQO
and AEC methods.
CHEMICAL & GEOLOGICAL LABORATORIES
JAa aa Mi
Mensik
D-16
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CLl-IO
Chemical a Geological Laboratories
P. O. Box 2794
Caiper, Wyoming
ANALYTICAL REPORT
From Wyoming Water Resources Research Inst. Product Water
Address Laramie, Wyoming Date 5-29-81
Other Pertinent Data
Analyzed-by . Date . 6-22-81 Lab No. 37649-1
WATER ANALYSIS
13-119-2BB
Sample taken May 21, 1981
mg/1
Total suspended solids 0.4
Total dissolved solids (calc.) 712
Total dissolved solids (obs.) 608
Conductivity @ 68°F., micromhos 910
Total alkalinity as CaCO^ 334
Total hardness as CaCO, 384
Sodium (Na) (calc.) 106
Sodium (Na) (obs.) 102
Potassium (K) 14
Calcium (Ca) 50
Magnesium (Mg) 63
Sulfate (SO.) 256
Chloride (CI) — 23
Carbonate (CO,) 0
Bicarbonate (HCOj) 407
pH, units 8.1
Aluminum (Al) *
Ammonia (as N) *
Arsenic (As) ND(0.01)
Boron (B) *
Barium (Ba) ND(0.05)
Beryllium (Be) *
Bromide (Br) *
Cation-Anion Balance *
Cadmium (Cd) ND(O.Ol)
Cyanide (CN) *
mfi/1
Chromium (Cr) ND(0.05)
Copper (Cu) *
Fluoride (F) 0.74
Iron (Fe)(total) *
Iron (Fe)(dissolved) *
Lead (Pb) ND(0.05)
Manganese (Mn) *
Mercury (Hg) ND (0.001)
Molybdenum (Mo) *
Nickel (Ni) *
Nitrate (as N) 0.22
Nitrite (as N) *
Phenols *
Phosphorus (PO.) *
Selenium (Se) ND(O.Ol)
Silica (S10.) *
Silver (Ag) ND(0.02)
Sulfide (S) *
Vanadium *
Uranium (U.0„; 0^02 !
Eh, millivolts *
Turbidity (JTU's)
Oil and grease (Freon Method) -
Chemical Oxygen Demand (COD) —
Radium-226, pCi/1 0.6 ± 0.30
Gross Beta, pCi/1 20 ± 4
Thorium-230, pCi/1 *
Polonium-210, pCi/1 *
ND = Not detected at level given in parentheses. Radiochemical tests by Chem. Lab.
* = Test not requested.
Above tests were made in accordance with Standard Methods, lAth Edition, 1975, ASTM, WQO
and AEC methods.
CHEMICAL & GEOLOGICAL LABORATORIES
-------
CLI-10
Chemical a Geological Laboratories
P. O. Box 2794
Caspar, Wyoming
ANALYTICAL REPORT
From Wyoming, Water Resources Research Inst. product. Water
Address Laramie, Wyoming Date S-29-81
Other Pertinent Data
Analyzed by MM,BW»RJ .Date. 6-22-81 Lab No. 37649-10
WATER ANALYSIS
18-116-6DDA
Sample taken May 26, 1981
ma/1
Total suspended solids 0.8
Total dissolved solids (calc.) 1430
Total dissolved solids (obs.) 147S
Conductivity @ 68°F., micromhos 2000
Total alkalinity as CaCO, 916
Total hardness as CaCO- 19
Sodium (Na) (calc.) 593
Sodium (Na) (obs.) 578
Potassium (K) 1
Calcium (Ca) —: 6
Magnesium (Mg) 1
Sulfate (SO.) 0
Chloride (CI) — . 280
Carbonate (CO..) 168
Bicarbonate (Hdff.) —- - 776
pH, units 8.9
Aluminum (Al) *
Ammonia (as N) *
Arsenic (As) ND(0.01)
Boron (B) *
Barium (Ba) 0.11
Beryllium (Be) *
Bromide (Br) *
Cation-Anion Balance *
Cadmium (Cd) ND(0.01)
Cyanide (CN) *
unromirim (Cr) ND(0.0S)
Copper (Cu) *
Fluoride (F) 11.20
Iron (Fe)(total)
Iron (Fe)(dissolved)
Lead (Pb) ND(0.05)
Manganese (Mn)
Mercury (Hg)
Molybdenum (Mo)
Nickel (Ni)
Nitrate (as N)
Nitrite (as N)
Phenols ¦ —
Phosphorus (PO,)
Sfeletilum' (Sa)"*-1———
— ND(0.001)
Silica (SiO.)
Silver (Ag)
Sulfide (S)
Zinc (Zn)
Vanadium (V,0,)
Uranium (U,0„j
Eh, millivolts
Turbidity (JTU's)
Oil and grease (Freon Method) -
Chemical Oxygen Demand (COD) —
Radium-226, pCi/1 — 0.1 ± 0.1
Gross Alpha, pCi/1 4 i 5
Gross Beta, pCi/1 0 ± 9
Thorium-230, pCi/1 — *
J.ead.-210pCi/1 — . , *
Polonium-210, pCi/1 *
ND = Not detected at level given in parentheses. Radiochemical tests by Chem. Lab.
* = Test not requested.
Above tests were made in accordance with Standard Methods, 14th Edition, 1975, ASTM, WQO
and AEC methods.
CHEMICAL & GEOLOGICAL LABORATORIES
D-18
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CLI-IO
Chemical & geological laboratories
P. O. Box 2794
Casper, Wyoming
ANALYTICAL REPORT
From Wyoming Water Resources Research Inst. product Water
Address Laramie, Wyoming Date 5-29-81
Other Pertinent Data
Artalyzed- by N5M", BWDate 6-22-91 Lab Mo. 37649-20
WATER ANALYSIS
T19N-R105W
Cle&rv-iew
Sample taken May 28, 1981
mg/1
Total suspended solids 0.4
Total dissolved¦solids (caic.) 1559
Total dissolved soxids (ods.) 1520
Conductivity @ 68° F_, micromhos -— 2000
Total alkalinity as CaCO, 319
Total hardness as CaCO, 71
Sodium (Na) (calc.) 519
Sodium (Na) (obs.) 502
Potassium (K) 3
Calcium (Ca) 15
Magnesium (Mg) 8
Sulfate (SO.) 742
Chloride (CI) 80
Carbonate (CO.) 62
Bicarbonate'(HCO,) 263
pH,. units . 8.8
Aluminum (Al) *
Ammonia (as N) *
Arsenic (As) ND(0.01)
Boron (B) *
Barium (Ba) ND(0.05)
Beryllium (Be) *
Bromide (Br) *
Cation-Anion Balance *
Cadmium (Cd) ND(0.01)
Cyanide (CN) *
mg/1
Chromium (Cr) ND(0.05)
Copper (Cu) *
fluoride (F) 1.21
Iron (Fe)(total) *
Iron (Fe)(dissolved) *
Lead (Pb) ND(0.05)
Manganese (Mn) *
Mercury (Hg) ND(O.OOl)
Molybdenum (Mo) *
Nickel (Ni) *
Nitrate (as -N) 0.29
Nitrite (as N) *
Phosphorus (PO.) *
Selenium (Se)' ND(0.01)
Silica (SiO„) *
Silver (Ag) ND(0.02)
Sulfide (S) *
Zinc (Zn) *
Vanadium ^2^5^ *
Uraniur (vj>j ND (0.001)
Eh, millivolts *
Turbidity (JTU's) *
Oil anc grease (Freon Method) - *
Chemical Oxygen Demand (COD) — *
Radium-226, pCi/1 0.4 ± 0.2
Gross Alpha, pCi/1 0 + 16
Gross Beta, pCi/1 0 ± 14
Thorium-230, pCi/1 *
Lead-210, pCi/1 *
Polonium-210, pCi/1 *
ND = Not detected at level given in parentheses. Radiochemical tests by Chem. Lab.
* = Test not requested.
Above tests were made in accordance with Standard Methods, 14th Edition, 1975, ASTM, WQ0
and AEC methods.
CHEMICAL & GEOLOGICAL LABORATORIES
D-19
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CL1-10
Chemical Be Geological Laboratories
P. O. Box 2794
Cotper, Wyoming
ANALYTICAL REPORT
From Wyoming Water Resources Research Inst. procjuct Water
Address Laramie, Wyoming Date 5-29-81
Other Pertinent Data
Analyzed by. MM,BW,RJ 3&re 6-22-81 [_ab ^jp. 37649-9
WATER ANALYSIS
18-105-7BAB
Sample taken May 28, 1981
mg/1
°°e/i
Total suspended solids 0.4
Total dissolved solids (calc.) 1940
Total dissolved cclilds ' (obs. ) — 2214
Conductivity @ 68°F., micromhos 2075
Total alkalinity as CaCO, 426
Total hardness as CaCO, 212
Sodium (Na) (calc.) 591
Sodium (Na) (obs.) 561
Potassium (K) 4
Calciuz1. (Ca) 42
Magnesium (Mg) 26
Sulfate (SO,) 980
Chloride (CI) — 41
Carbonate (CO.) 54
Bicarbonate (HCO.) 410
pH, units 8.4
Aluminum (Al) *
Ammonia (as N) *
Arsenic (As) ND(0.01)
Boron (B) *
Barium (Ba) ND(0.05)
Beryllium (Be) *
Bromide (Br) *
Cation-Anion Balance *
Cadmium (Cd) ND(0.01)
Cyanide (CN) *
Chromium (Cr) ND(0.05)
Copper (Cu) *
riuoride (r) '— 1.55
Iron (Fe)(total) *
Iron (Fe)(dissolved) — *
Lead (Pb) ND(0.0S)
Manganese (Mn) *
Mercury (Hg) ND(0.001)
Molybdenum (Mo) *
Nickel (Ni) *
Nitrate (as N) 0.02
Nitrite (as N) *
Phenols *
Phosphorus (PO.) *
Selenium (Se) ND(0.01)
Silica (SiO.) *
Silver (Ag) ND(0.02)
Sulfide (S) *
Zinc (Zn) *
Vanadium (V.0_) *
Uranium (U 0 J ND(0.001)
Eh, millivolts *
Turbidity (JTU's) *
Oil and grease (Freon Method) - *
Chemical Oxygen Demand (COD) — *
Radium-226, pCi/1 0.3 ± 0.1
Gross Alpha, pCi/1 1 ± 6
Gross Beta, pCi/1 0 ± 13
Laad-210, pCi/1 *
Polonium-210, pCi/1 *
ND = Not detected at level given in parentheses. Radiochemical tests by Chem. Lab.
* = Test not requested.
Above tests were made in accordance with Standard Methods, 14th Edition, 1975, ASTM, WQO
and AEC methods.
CHEMICAL & GEOLOGICAL LABORATORIES
D-20
-------
CL1-IO
CHEMICAL & GEOLOGICAL LABORATORIES
P. O. Box 2794
Caiper, Wyoming
ANALYTICAL REPORT
From Wyoming^)V?t;er Resources Research Inst. p/0du<;»
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