Ground-Water Chemistry and Diagenetic 

Reactions in Tertiary Sandstones of the 

Green River and Wasatch Formations, 

Uinta Basin, Utah

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101 Twelfth
Chapter X

Ground-Water Chemistry and Diagenetic 

Reactions in Tertiary Sandstones of the 

Green River and Wasatch Formations, 

Uinta Basin, Utah

By RICHARD B. WANTY, JANET K. PITMAN, and 

THOMAS D. FOUCH

A multidisciplinary approach to research studies of sedimentary 

rocks and their constituents and the evolution of sedimentary 

basins, both ancient and modern

U.S. GEOLOGICAL SURVEY BULLETIN 1 787

EVOLUTION OF SEDIMENTARY BASINS UINTA AND PICEANCE BASINS
U.S. DEPARTMENT OF THE INTERIOR 

MANUEL LUJAN, JR., Secretary

U.S. GEOLOGICAL SURVEY 

Dallas L. Peck, Director

Any use of trade, product, or firm names in this publication is for descriptive 

purposes only and does not imply endorsement by the U.S. Government.

UNITED STATES GOVERNMENT PRINTING OFFICE: 1991

For sale by the

Books and Open-File Reports Section

U.S. Geological Survey

Federal Center

Box 25425

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Library of Congress Cataloging-in-Publication Data

Wanty, Richard B.

Ground-water chemistry and diagenetic reactions in Tertiary sandstones of the 

Green River and Wasatch Formations, Uinta Basin, Utah : a multidisciplinary 

approach to research studies of sedimentary rocks and their constituents and the 

evolution of sedimentary basins, both ancient and modern / by Richard B. Wanty, 

Janet K. Pitman, and Thomas D. Fouch.

p. cm. (U.S. Geological Survey Bulletin ; 1787) (Evolution of 

sedimentary basins Uinta and Piceance basins ; ch.)

Includes bibliographical references.

1. Water, Underground Uinta Basin (Utah and Colo.) 2. Sandstone Uinta 

Basin (Utah and Colo.) 3. Water chemistry. 4. Green River 

Formation. 5. Wasatch Formation. I. Pitman, Janet K. II. Fouch, Thomas 

D. III. Title. IV. Series. V. Series: Evolution of sedimentary basins Uinta 

and Piceance basins ; ch. 

QE75.B9 no. 1787-X 

[GB1027.U38]

557.3 s dc20 91-25812 

[552'.5] CIP
CONTENTS

Abstract XI 

Introduction XI

Geologic setting XI

Well locations, flow paths, and ground-water analyses X3 

Results X3

Petrography and paragenesis X3

Ground-water chemistry X7 

Discussion X7

Chemical evolution of the ground water X8

Silica solubility X9

Flow-path modeling X10

Processes affecting pH and alkaline-earth elements Xll

Processes affecting salinity X13 

Conclusions X14 

References cited X15

Appendix List of unique field identification numbers and sample dates for water 

analyses meeting criteria for completeness and accuracy described in text X19

FIGURES

1. Map showing locations of wells from which samples were taken, flow paths, 

and locations of major oil and gas fields, Uinta basin, Utah X2

2. Southwest-north lithologic cross section through central part of Uinta 

basin X2

3. Plot of potentiometric surface for Wasatch and Green River Formations, Uinta 

basin X4

4. Chart showing generalized paragenetic sequence for sandstones of Green

River Formation in southern half of the Uinta basin X4 

5-7. Piper diagrams of water samples along flow-paths 1, 2, and 3 X7 

8-10. Profiles of changes in some major ground-water chemical parameters along

flow-paths 1, 2, and 3 X10 

11. Histograms of calculated saturation indexes for chalcedony and quartz in

ground-water samples X13 

12-17. Graphs showing:

12. Evolution of ground-water chemistry, flow-path 3, in Na+/H+ versus 

K+/H+ space ^ X14

13. Results of models 1-5, flow-path 3 X15

14. Results of models 3-5, flow-path 3 X16

15. Total dissolved solids along flow-path 3, as compared to predictions 

using PHREEQE X17

16. Predicted variations in pH and ionic strength according to models 11 

and 12 X18

17. Chemical evolution of ground water in Na+/H+ versus K+/H+ space, as 

predicted by models 11 and 12 X18

Contents
TABLES

1. Chemical analyses for samples that fall along flow-paths 1, 2, and 3 X6

2. Features of models used to simulate changes in ground-water chemistry along 

flow-path 3 X13

IV Contents
EVOLUTION OF SEDIMENTARY BASINS UINTA AND PICEANCE BASINS

Ground-Water Chemistry and Diagenetic Reactions in 

Tertiary Sandstones of the Green River and Wasatch 

Formations, Uinta Basin, Utah,

By Richard B. Wanty, Janet K. Pitman, and Thomas D. Fouch

Abstract

An integrated study of ground-water chemistry and 

aquifer petrology reveals close correspondence between the 

chemical evolution of ground water and observed authigenic 

mineral assemblages. In recharge areas, authigenic kaolinite is 

observed in the rocks, and ground-water compositions plot 

within the stability field for kaolinite in a variety of activityactivity diagrams. Feldspar is dissolved from the updip rocks, 

also in accordance with thermodynamic predictions from the 

water chemistry. In down-gradient reaches of the flow system, 

authigenic clay, including smectite and illite-smectite, is 

present and feldspar destruction still prevalent. Near discharge 

areas, feldspar may be stable, although authigenic feldspar is 

not common. Throughout the basin, authigenic calcite and 

dolomite commonly replace detrital feldspar grains. 

Precipitation of carbonate minerals probably is driven by an 

increase in pH and by release of calcium associated with 

feldspar dissolution. Chalcedony, rather than quartz, probably 

is the silicate phase controlling dissolved silica levels. The 

good agreement between the petrographic relationships and 

the present-day ground-water chemistry suggests either that 

the observed authigenic mineral assemblages are still forming 

or that the ground water has had sufficient time to approach 

equilibrium with respect to the assemblage.

INTRODUCTION

Although numerous workers have examined diagenetic changes in sandstones or basinwide changes in 

water chemistry, few of them have integrated water and 

rock data. In a study of Tertiary sandstones in the Kettleman 

North Dome in California, Merino (1975a, b) found that

Manuscript approved for publication May 21, 1991.

diagenetic minerals and water were in chemical 

equilibrium. When plotted on activity-activity diagrams 

showing stability fields for major silicate minerals, the 

water compositions were within stability fields for minerals 

observed to be present as authigenic phases in the 

sandstones. In a similar study, Lee (1985) found that water 

chemistry in Upper Cretaceous aquifers in the Mississippi 

embayment of northern Mississippi and Alabama followed 

a systematic progression that could be related to attainment 

of chemical equilibrium with varied diagenetic mineral 

assemblages along a flow path (Hanor and McManus, 

1988). Further, Lee (1985) used carbon isotopic ratios to 

infer sources and sinks of dissolved inorganic carbon in the 

waters.

The studies described above show the validity of 

using theoretical models to understand natural systems, and 

they serve as appropriate examples for our study of ground 

waters in Tertiary sandstones of the Green River and 

Wasatch Formations in the Uinta basin of northeastern Utah 

(fig. 1). We calculated mineral assemblages that are in 

equilibrium with the observed waters and compared 

calculated and observed assemblages to test how well 

mineral-solution equilibria characterize the processes of 

water-rock interaction in the basin.

Geologic Setting

The Tertiary Green River and Wasatch Formations in 

the Uinta basin are made up of lacustrine and fluvial 

sublitharenite, litharenite, feldspathic litharenite, and lithic 

arkose deposited along the margin of ancient lake Uinta 

during the Paleocene and Eocene. This large lake complex 

developed and reached its greatest areal and volumetric 

extent during the early Eocene to early Oligocene(?). The

Ground-Water Chemistry and Diagenetic Reactions, Uinta Basin, Utah X1
110°W 109°W

20 KILOMETERS

EXPLANATION

Q Oil or gas well with core samples 

HF Oil or gas field 

 Well with water analyses 

 Approximate flow path

Approximate outline of Uinta basin

Figure 1. Map showing the locations of wells from which water or core samples were taken, Uinta basin, Utah. All water 

analyses are from literature sources given in the appendix. Flow-paths 1, 2, and 3 were chosen based on the hydrological model 

of J.D. Bredehoeft (1990, written commun.). The locations of major oil- or gas-producing fields also are shown.

sw

3,000 -

2,000-

1,000 -

Sea level -

-1,000-

-2,000-

-3,000 -

Altamont field N

EXPLANATION 

Alluvial

Marginal lacustrine 

Open lacustrine

METERS 

- 2,000

- 1 ,000

5 10 

I I

"'"c^^

15 20 KILOMETERS 

I I

Paleozoic and Mesozoic' 

rocks

- 3,000

- 2,000

- 1,000 

Sea level

- -1,000

- -2,000

- -3,000

Figure 2. Lithologic cross section through the central part of the Uinta basin from southwest to north. Modified from Fouch 

(1975).

X2 Evolution of Sedimentary Basins Uinta and Piceance Basins
thickest fluvial and lacustrine sequence was deposited near 

the present-day Altamont oil field south of the uplifted flank 

of the Uinta Mountains along the central part of the axis of 

the Uinta basin (fig. 2). In this area, more than 3,000 m of 

Paleocene and Eocene lacustrine rocks are preserved, 

including more than 1,200 m of fine-grained kerogenous 

carbonate and mudstone units, including oil shale, that 

formed during the middle and late Eocene (46-42 Ma).

Mineral composition of rocks in the Uinta basin is 

related to the geographic location of source terrane (Ryder 

and others, 1976; Franczyk and others, 1989). In the 

northern part of the basin, including the areas of the 

Altamont and Red Wash fields, sediments were derived 

from granitic source rocks in the Uinta Mountains to the 

north. In contrast, sediments in the southern half of the 

basin, including the areas of the Natural Buttes and Pariette 

Bench fields, were derived from feldspathic- and lithic-rich 

rocks in Laramide uplifts to the south. The resulting distinct 

petrofacies experienced different diagenetic histories and 

consequently display different authigenic mineral 

assemblages. Our study deals primarily with the 

feldspathic- and lithic-rich rocks in the central and southern 

parts of the basin.

The results of this study may be applied to 

understanding the development or occlusion of porosity in 

oil- and gas-bearing strata of the Uinta basin. Oil-producing 

reservoirs in the Red Wash and Altamont fields include 

marginal-lacustrine fluvial and lacustrine sandstones that 

formed along the lake's northern margin. Open-lacustrine 

turbidites also yield oil at Altamont. Lower deltaic plain 

units and low-permeability sandstones, encased in redbeds, 

on the south flank of the basin in the Natural Buttes field 

and nearby areas produce gas.

Well Locations, Flow Paths, and 

Ground-Water Analyses

Water-chemical analyses were collected from the 

literature (Price and Miller, 1975; Hood and others, 1976; 

Conroy and Fields, 1977) and screened for completeness 

and accuracy. They were all evaluated according to 

following criteria: (1) analyses had to be reasonably 

complete, including measurements for pH, temperature (or 

depth), and major cations and anions; (2) analyses had to be 

charge balanced to within ±10 percent; and (3) the geologic 

formation producing the water had to be identified. 

Approximately 15 percent of the available analyses met 

these criteria, resulting in a total of 201 analyses. The appendix contains the unique field-identification numbers of 

these analyses and the sample collection dates. The full 

analyses can be obtained by consulting the references cited 

above.

Because our study is based on previously reported 

analyses, several limitations are imposed on data

interpretation. For the most part, analytical results are 

limited to the major cations and anions (Ca, Mg, Na, K, 

ECO3 , Cl, and S04) and pH. In some cases, analytical 

results are reported for other elements, including silica and 

iron. The use of analytical results from several literature 

sources introduces additional uncertainty caused by possible 

variations in sampling protocol and technique, equipment 

used, and so forth, the details of which are not adequately 

described in the cited reports. All analyses include measurements of pH, but it is unclear whether the pH reported is at 

the formation-water temperature or surface temperature. All 

modeling in this study was performed assuming the former. 

The uncertainty introduced by this assumption is greatest 

for water samples having temperatures greater than about 

30°C; that is, those collected from depths greater than about 

700 m. In light of these limitations in the data set, 

conclusions based on individual samples are deemphasized; rather, the data are examined with regard to 

describing the general trends of ground-water chemical 

evolution.

The present-day potentiometric surface for the middle 

of the Green River and Wasatch Formations in the basin is 

shown in figure 3 (J.D. Bredehoeft, U.S. Geological Survey, 

1990, written commun.). Potentiometric highs (recharge 

areas) are around the perimeter of the basin, and lows 

(discharge areas) are along the Green River, which cuts 

across the basin from northeast to southwest. The three flow 

paths shown in figure 1 were constructed using the results of 

this hydrologic model. Water-rock reactions are modeled 

along these flow paths, from recharge areas along the basin 

margins to discharge areas.

The map of the Uinta basin (fig. 1) shows the 

locations of major oil fields in the basin as well as the 

locations of oil or gas wells from which core samples were 

collected for the petrographic, mineralogic, and isotopic 

parts of this study.

RESULTS

Petrography and Paragenesis

The feldspathic-lithic petrofacies that characterizes 

Tertiary sandstones in the southern part of the Uinta basin 

has been diagenetically modified by authigenic cements and 

by framework-grain replacement and dissolution. Of these 

processes, cementation and dissolution reactions have had 

the greatest effect on oil- and gas-reservoir quality. The 

extent of alteration within a sandstone sequence is highly 

variable and reflects the diverse compositional varieties of 

feldspar. This variation can account for differences in 

reservoir quality in rocks of the same age and origin at 

different locations. The paragenetic sequence of mineral 

alteration (fig. 4) consists of (1) minor silica cementation,

Ground-Water Chemistry and Diagenetic Reactions, Uinta Basin, Utah X3
Altamont oil field

Green River

Figure 3. Plot of the potentiometric surface for the Wasatch and Green River Formations in the Uinta basin. Modified from J..D. 

Bredehoeft (1990, written commun.).

Secondary quartz

Nonferroan 

calcite

Ferroan 

calcite Dolomite Ankerite

Carbonate 

dissolution

Carbonate 

dissolution

Anhydrite

Illite - smectite

Illite

Chlorite

Hydrocarbon migration

Kaolinite

Early Late

Figure 4. Generalized paragenetic sequence for sandstones of the Green River Formation in the southern half of the Uinta basin.

X4 Evolution of Sedimentary Basins Uinta and Piceance Basins
(2) multiple generations of carbonate precipitation and 

dissolution, (3) local anhydrite and barite cementation, and 

(4) authigenic clay mineral development. A detailed 

description of the various authigenic phases is given in 

Pitman, Fouch, and Goldhaber (1982) and Pitman, Anders, 

and others (1986).

Minor secondary quartz is present in some Tertiary 

sandstones generally as anhedral to euhedral overgrowths. 

Sutured grain contacts or other evidence of pressure 

solution were not observed. Except for the euhedral overgrowths, which are sparse, most secondary quartz overgrowths probably formed along with the detrital grains in 

the sediment source area and were transported to the site of 

sedimentation.

The sandstones have been modified by a complex 

carbonate mineral assemblage composed of ferroan calcite 

and lesser nonferroan calcite, dolomite, and ferroan 

dolomite. Multiple episodes of calcite precipitation can be 

distinguished on the basis of trace-element concentrations. 

For example, early calcite is iron poor (Fe:Ca atomic ratio 

<0.05), but later calcite is iron rich (Fe:Ca atomic ratio as 

high as 0.2). Ferroan calcite is common in sandstones 

throughout the southern part of the basin, whereas ankerite 

is abundant only in the central part of the basin at the 

Pariette Bench field. The amount and distribution of 

authigenic carbonate within and between beds may be 

widespread or localized depending on the depositional 

environment. Iron-free calcite, the earliest carbonate phase 

to precipitate, is present as relict grains and cement 

surrounded by optically continuous ferroan calcite. The 

embayed texture of nonferroan calcite relicts suggests that 

this carbonate phase was affected by dissolution early in the 

diagenetic history. Most calcite is a fine- to coarsecrystalline ferroan variety that formed during later stages of 

diagenesis. Typically, it partly to completely replaces feldspar grains and rock fragments and occludes pores. In 

sandstones that probably had high initial porosity and 

permeability, ferroan calcite is a pervasive cement. 

Framework grains enclosed in the cement typically are 

angular, show little or no alteration, and are not in contact 

with one another. The "rind" of ferroan calcite cement 

probably protected the grains from later alteration by 

chemically active pore fluids. In many sandstones calcite 

and possibly other mineral cements may have been 

widespread. Feldspar grains and lithic fragments having 

embayed margins, calcite relicts in pores, and calcite along 

cleavage planes in feldspar grains suggest that an episode of 

leaching occurred during late-stage diagenesis.

Calcite dissolution features in Tertiary sandstones 

reflect multiple episodes of leaching during different times 

in the burial history. Thermal maturation of coeval, deeply 

buried organic-rich rocks at the Altamont field in the 

northern part of the basin and subsequent oil migration 

southward to the Pariette Bench field may have yielded CO2 

and organic acids to pore fluids. These compounds could

have promoted carbonate dissolution. There is no evidence 

that oil migration affected Tertiary strata at the Natural 

Buttes field, but the presence of thermogenic gas in the 

thermally immature rocks of the field could signal the 

presence of organic acids. More likely, carbonate 

dissolution occurred when meteoric waters infiltrated these 

rocks during a period of erosion.

Similar to calcite, dolomite is present as isolated 

grains and small patches of cement; however, authigenic 

dolomite is difficult to differentiate from detrital dolomite 

because the two phases are complexly intergrown. Where 

authigenic dolomite is abundant, it is as an anhedral pore-fill 

and replacement cement that probably formed relatively 

early in the burial history. Ferroan dolomite is present both 

as optically continuous rims on detrital dolomite grains and 

as discrete rhombs that commonly have coalesced to form a 

cement. There is no evidence of leaching in any of the rocks 

studied. Most ferroan dolomite probably formed in the 

source area and was introduced with other detrital grains, 

although a small fraction clearly precipitated during latestage diagenesis.

The complex carbonate mineral assemblage indicates 

that carbonate- and bicarbonate-charged waters of variable 

chemical composition migrated intermittently through the 

sandstone sequence during burial, resulting in multiple 

cycles of carbonate precipitation and dissolution. A similar 

interpretation is supported by stable isotope analyses of 

end-member carbonate cements in the Natural Buttes field. 

Widely variable calcite 813C values (about -1 to -9 per mil 

relative to PDB) suggest that multiple sources of carbon 

were added to the carbon reservoir through time. Heavy 

carbon values (>-2 per mil relative to PDB) probably result 

from recycled dissolved marine carbonate grains, whereas 

lighter values (<-2 per mil relative to PDB) can be 

attributed to the decomposition of organic material. 

Carbonate 818O values also vary significantly (about -6 to 

-13 per mil relative to PDB). Heavier values in more deeply 

buried Cretaceous rocks suggest that temperature was not 

the dominant controlling factor. Rather, the trend toward 

heavier oxygen isotopic values is interpreted to record 

progressive reaction between meteoric waters and silicate 

minerals along a basinward flow path.

Authigenic anhydrite and barite are present only in 

sandstones at the Natural Buttes field. Both minerals 

preferentially replace carbonate cement and framework 

grains such as feldspar, thus they probably formed relatively 

late in the diagenetic history. Preliminary sulfur isotope data 

for anhydrite cement in Tertiary sandstones at the Natural 

Buttes field show isotopically heavy values averaging about 

+30 per mil relative to CDT. These values are similar to 

those reported for organic and pyrite sulfur in younger 

kerogenous beds of the Green River Formation (Harrison 

and Thode, 1958; Mauger, 1972; Cole and Picard, 1981;

Ground-Water Chemistry and Diagenetic Reactions, Uinta Basin, Utah X5
Table 1 . Chemical analyses for samples that fall along flow-paths 1, 2, and 3

[Depth in meters; temperature in °C; all chemical constituents, including total dissolved solids (TDS), in milligrams per liter. Leader ( ) 

indicates no value reported]

Avg. depth pH Temperature Ca Mg Na K HCO3 C03 SO4 Cl Si02 TDS

Flow-path 1

GR-142

GR-141

GR-140

GR-71

GR-69

GR-67

GR-68

0

360

2,320

2,320

2,140

1,480

1,900

7.6

8.9

8.7

8.7

8.5

8.3

8.4

8.0

17.9

65.3

65.3

61.0

44.8

55.0

56

10

20

20

16

17

22

37

13

16

16

7

20

14

210

3,020

3,020

4,300

23,800

17,300

1.4

24

24

150

170

316

426

3,220

3,220

1,730

4,360

2,090

230

250

280

200

74 3.4

120 12

72 2,560

72 2,560

79 5,300

102 34,000

580 25,000

25 527

- 790

- 8,900

- 9,160

- 11,700

- 62,700

- 45,400

Flow-path 2

GR-226

GR-225

GR-215

GR-111

GR-49

GR-51

GR-52

GR-53

0

0

0

690

1,480

1,350

3,900

1550

7.5

8.4

7.9

8.7

7.9

8.4

8.1

8.1

7

11

11

25.8

44.8

41.7

43.4

46.6

77

48

65

10

2,060

590

990

1,920

26

20

17

7

270

310

270

360

27

33

27

274

23,600

28,700

26,800

21,600

0.8

0.9

0.4

13

303

268

250

380

425

427

878

647

36

100 2.2

44 3.5

52 14

290 32

3,580 38,000

11,900 37,200

2,800 41,300

3,700 34,600

23 559

18 435

14 439

- 1,000

- 68,000

- 79,000

- 73,000

- 62,800

Flow-path 3

GR-229

GR-212

GR-210

GR-211

GR-208

GR-209

GR-196

GR-147

GR-148

GR-144

GR-229

GR-212

GR-210

GR-211

GR-208

GR-209

GR-196

GR-147

GR-148

GR-144

Avg. depth

0

0

10

10

3

3

185

494

508

327

SiO2

17

8.3

19

19

13

12

15

15

15

11

PH

7.2

7.7

7.8

7.4

8

7.6

8.4

8.3

8.5

8.5

S2'

0.1

0.1

180

180

0.1

0.2

120

6.5

6.7

0.5

Temperature

8.5

10

10.5

10.5

9.5

9

14.5

21.5

22

17

Fe

0.02

0.05

0.04

0.06

0.06

0.32

0.1

0.09

0.06

0.05

Ca

53

110

76

64

150

130

2.4

2.1

4

1.1

Mn

0.01

0.03

0.06

0.06

0.02

Mg

27

170

150

150

180

180

3.7

1.2

1

0.5

B

0.02

0.13

7

7.9

4.7

1.8

2

20

21

33

Na

12

1,200

870

890

1,000

970

640

2,400

3,100

3,400

Al

0.01

0.03

0.02

K

0.7

7.7

4

3.1

8.9

6.9

1.8

11

11

11

Sr

0.5

3.4

2.9

2.9

3

3.4

0.46

0.81

0.97

0.34

HCO3 SO4

267 47

556 2,900

540 1,600

545 1,900

530 2,500

564 2,500

880 350

779 140

2,260 100

5,100 58

V U

 

 

Cl F

2.8 0.3

65 0.5

390 6.6

190 6.2

65 1.9

59 2.1

170 2.6

3,200

3,300 25

1,700 120

TDS

427

5,020

0.0031 0.0069 3,850

0.017 0.0002 3,960

0.0005 0.02

0.0021 0.022

4,460

4,430

0.001 0.0008 2,190

 

 

 

6,580

8,850

10,400

Tuttle, 1988). Fluids expelled from tongues of organic-rich 

shale may have contained reduced sulfur that was later 

transported to Wasatch Formation strata where the sulfur 

was oxidized to sulfate.

Authigenic kaolinite, chlorite, illite, and illitesmectite commonly are present together in various amounts 

at the Natural Buttes field, but at the Pariette Bench field,

more central in the basin, kaolinite is absent from this 

assemblage. Corrensite, a regularly interstratified illitechlorite, also was detected in small amounts at the Natural 

Buttes field. Corrensite is present as a network of 

interconnected platelets oriented perpendicular to grain 

surfaces. Kaolinite generally is present as well-crystallized 

booklets in secondary intergranular pores that commonly

X6 Evolution of Sedimentary Basins Uinta and Piceance Basins
Cl 

Anions

Figure 5. Piper diagram of water samples along flow-path 1 in the western half of the Uinta basin. The triangular fields show 

normalized percentages of the equivalents per million of cations or anions.

are lined with fibrous illite or platelets of chlorite. Textural 

relations suggest that the suite of authigenic clay minerals 

formed over a long time span after carbonate dissolution. 

Illite, illite-smectite, and chlorite probably formed when the 

rocks were at or near maximum burial, whereas kaolinite 

precipitation most likely is related to an influx of meteoric 

water associated with late-stage uplift and erosion.

move down gradient. Low-TDS waters are Ca-Mg-HCO3 

dominated, whereas high-TDS waters are Na-Cl dominated. 

Waters in the basin are typically low in sulfate. Groundwater chemical evolution is conveniently summarized in 

Piper diagrams (figs. 5-7). Profile plots in figures 8-10 

demonstrate the increase in TDS, as well as the increase in 

Na:Ca and C1:CO3 ratios along the three flow paths.

Ground-Water Chemistry

The chemistry of ground water evolves along the flow 

paths in a systematic manner. Chemical analyses are given 

in table 1 for samples that plot along the three flow paths 

shown in figure 1. From recharge zones, the waters show 

increasing total dissolved solids (TDS) contents as they

DISCUSSION

The interpretation of ground-water chemical changes 

described here is based on the application of 

thermodynamic models that assume chemical equilibrium. 

Therefore, further limitations are introduced in addition to 

those described earlier that relate to the use of previously

Ground-Water Chemistry and Diagenetic Reactions, Uinta Basin, Utah X7
Cl 

Anions

Figure 6. Piper diagram of water samples along flow-path 2 in the southern part of the Uinta basin. The triangular fields show 

normalized percentages of the equivalents per million of cations or anions.

published chemical analyses. The primary limitation of 

thermodynamic modeling is the availability of reliable and 

complete thermodynamic data for calculation of equilibrium 

constants. In many instances, thermodynamic data may be 

available for 25 °C, but the lack of enthalpy values makes 

temperature corrections or extrapolations uncertain. In 

addition, complexing agents not included in the 

thermodynamic data base may dramatically alter the 

distribution of aqueous species. Kharaka and others (1988) 

have thoroughly discussed these types of limitations.

When modeling ground-water chemical evolution 

along a flow path, the choice of possible chemical reactions 

between water and rock is constrained by petrographic, 

geologic, geochemical, and other observations. Chemical 

evolution pathways based on these preferred reactions may

be realistic but are by no means unique, a factor that must 

be considered when interpreting the results.

Chemical Evolution of the Ground Water

Changes in ground-water chemistry occur in response 

to several factors. Many of the features of the chemical 

evolution of the ground water can be explained in terms of 

mineral dissolution and precipitation reactions, as will be 

seen in more detail in the next section.

Along the flow paths, sample depths range from less 

than 30 to more than 1,500 m, and corresponding water 

temperatures increase from about 9 °C in springs and 

near-surface wells to 40-50 °C in deeper wells. The 

increase in solubilities (and rates of dissolution) for silicate

X8 Evolution of Sedimentary Basins Uinta and Piceance Basins
Cl 

Anions

Figure 7. Piper diagram of water samples along flow-path 3 in the southeastern part of the Uinta basin. The triangular fields show 

normalized percentages of the equivalents per million of cations or anions.

minerals as temperature increases may contribute somewhat 

to the increase in concentrations of various elements with 

depth. Ion exchange reactions also may play a role, 

especially as manifested in the increase in Na:Ca ratios with 

distance along the flow paths. The changes in ground-water 

chemistry in response to these types of reactions are subtle 

in terms of TDS contents. As shown in figures 8-10, TDS 

contents increase slightly along the flow path until the 

deeper parts of the basin are reached, where TDS contents 

increase dramatically. The very high TDS levels must be 

due to other mechanisms such as salt dissolution, mixing 

with connate water, or mixing with migrated brines. These 

possibilities will be discussed at greater length later.

Silica Solubility

The state of saturation of the ground water with 

respect to silica minerals is of interest because it identifies 

which silica phases may be important in controlling 

dissolved silica concentrations. Because water samples 

interpreted in this study range from outcrop (spring) to deep 

drill-hole samples, temperatures from about 8 to more than 

100 °C were encountered. The three flow paths shown in 

figure 1 are limited to the shallower southern part of the 

basin, and the maximum temperature along these flow paths 

is about 45 °C. Using the computer program PHREEQE 

(Parkhurst and others, 1980), saturation indexes (SI) were

Ground-Water Chemistry and Diagenetic Reactions, Uinta Basin, Utah X9
100,000

o

\-

2 80,000-

UL

o

LU

_i

> 60,000- 

o

Q_ 

Q_

\ o 

- \ o X^o

\ "^ \ ^

\ <«

- 40,000 

O

CC

2 

LU 

O

O

o

20,000--

0

DISTANCE ALONG FLOW PATH

Figure 8. Profile of changes in some major ground-water chemical parameters along flow-path 1. Distance along the x-axis is 

proportional to geographic distance between wells sampled. Total length of the flow path is approximately 100 km.

calculated for chalcedony and quartz using the reaction

Si02(s)+2H20«H4Si04(aq),

where SiO2(s) represents either chalcedony or quartz. For 

this reaction, the saturation index is defined as

_ , a (H4SiO4(aq)) 

= 1 °gl° a(H20)2 log 10 KT

Here, a(i) denotes the observed activity of the species 

in parentheses, and KT represents the appropriate 

equilibrium constant corrected for the temperature. Figure 

11 shows histograms of SI values for the 41 samples for 

which silica was reported and for which the temperature 

was less than 45 °C. The mean SI value (±1 standard 

deviation) for quartz is 0.49+0.23 and for chalcedony 

0.04±0.22. As shown in figure 11, chalcedony is 

consistently closer to an equilibrium SI value of zero than is 

quartz, which is generally supersaturated. These 

calculations suggest that the solubility of cryptocrystalline 

chalcedony controls silica concentrations in the shallower 

waters (< 1,500 m) of the Uinta basin, even though

macrocrystalline quartz is the thermodynamically stable 

phase.

Flow-Path Modeling

Chemical changes along the three flow paths shown 

in figure 1 were modeled using the computer programs 

BALANCE (Parkhurst and others, 1982), PHREEQE 

(Parkhurst and others, 1980), SOLMINEQ.88 (Kharaka and 

others, 1988), and SNORM (Bodine and Jones, 1986). 

PHREEQE and SOLMINEQ.88 were used to calculate 

saturation indexes of the ground waters and to model 

reaction paths. BALANCE was used at the front end of the 

reaction-path modeling to create general chemical models 

not constrained by thermodynamics. SNORM was used to 

examine major-salt contents of each of the water samples. 

Mass-transfer reactions such as dissolution or precipitation 

of carbonate minerals, quartz or chalcedony, and feldspar 

minerals were considered in the reaction-path models. 

Initial results provided adequate simulations of the changes 

in pH and alkaline-earth-element concentrations, but 

changes in salinity could not be adequately modeled without 

consideration of NaCl addition.

X10 Evolution of Sedimentary Basins Uinta and Piceance Basins
so.ooo r

tr

u_

2 60,000

D

I

DC 

O

8: 40,000

< tr

z

LU 

O

O

o

20,000

DISTANCE ALONG FLOW PATH

Figure 9. Profile of changes in some major ground-water chemical parameters along flow-path 2. Distance along the x-axis is 

proportional to the geographic distance between the wells sampled. Total length of the flow path is approximately 80 km.

Processes Affecting pH and 

Alkaline-Earth Elements

Flow-path 3 (fig. 1) was modeled in the greatest detail 

because it includes samples having the most complete 

chemical analyses. Several different simulations were run; 

the features of each are described in table 2. The adequacy 

of each model can be judged in several ways. First, the 

reactions included in the model should conform, as closely 

as possible, to observed changes in mineralogy and water 

chemistry throughout the basin. Second, the calculated 

concentrations of the major solutes at each point along the 

flow path should mimic observed concentrations. Third, 

calculated dissolution or precipitation of minerals not 

specifically required to react with the solution should match 

observed petrographic relationships.

Thermodynamic calculations of solution-mineral 

equilibria based on measured water compositions indicate 

that calcite or dolomite should dissolve in recharge areas but 

precipitate deeper in the basin. Carbonate-mineral 

precipitation is driven by the progressive dissolution of 

feldspar and the concomitant rise in pH. Our petrographic 

observations indicate that carbonate precipitation may be 

active in some areas of the basin not extensively affected by 

petroleum migration; however, generation of CO2 during

bacterial metabolism of hydrocarbons may prevent 

precipitation of calcite or dolomite or lead to its dissolution. 

To a limited extent, the increase in temperature along the 

flow paths aids calcite or dolomite precipitation because of 

the retrograde solubilities of these minerals.

Silica concentrations in the waters probably are 

controlled by the solubility of chalcedony or some silicate 

that has a solubility similar to chalcedony. For reaction-path 

calculations that impose a limit on dissolved silica 

concentrations, equilibrium between chalcedony and the 

ground water is assumed.

Chemical reactions occurring along the flow path 

were modeled as a series of mineral precipitation and 

dissolution reactions. The appropriate phases to be 

considered in these reactions were chosen by considering 

the location of sample compositions on activity-activity 

diagrams such as the one shown in figure 12. Ground water 

in the recharge zone is well within the stability field for 

kaolinite, but other ground-water samples along the flow 

path plot along a trend that progresses toward the albite field 

through the muscovite field. Petrographic studies of rock 

samples show that authigenic kaolinite is present in outcrop 

and shallow subsurface samples, whereas illite or illitesmectite is present in deeper subsurface samples. 

Authigenic feldspar was not observed in any samples.

Ground-Water Chemistry and Diagenetic Reactions, Uinta Basin, Utah X11
12,000 r

o

< 10,000 - DC 

LL 

O

HI

Z> _l

>

DC 

O

DC

 z.

LJJ 

O

O

o

8,000

6,000 -

p 4,000

2,000 -

DISTANCE ALONG FLOW PATH

Figure 10. Profile of changes in some major ground-water chemical parameters along flow-path 3. Distance along the x-axis is 

proportional to the geographic distance between the wells sampled. Total length of the flow path is approximately 64 km.

Partial to complete destruction of detrital feldspar was 

observed in many of the samples. Thus, petrographic 

evidence of mineral dissolution and precipitation is 

consistent with predictions based on assumed equilibrium 

between minerals and coexisting ground waters.

The flow-path models had variable success in 

describing ground-water chemical evolution in the Green 

River and Wasatch interval. Models 1 and 2, for which no 

mineralogic control was imposed for silica, predict 

dissolved silica concentrations far in excess of the observed 

values along the flow path (fig. 13). In models 3-5, silica 

concentrations are limited by the solubility of chalcedony, 

in accordance with the earlier discussion. Models 3 and 4 

give the closest fit of the observed changes when plotted on 

a variety of activity-activity diagrams. Silica concentrations 

in model 5 are somewhat higher than in models 3 and 4 

because temperature was increased along the flow path from 

8 to 25 °C during progress of the reaction.

Models 4 and 5 produce closer fits of the data when 

plotted in K+/H+ versus Na+/H+ space (fig. 14). They also

more closely match observed pH values in natural samples; 

model 4 being slightly closer. These two models predict an 

authigenic mineral assemblage of kaolinite, dolomite, and 

chalcedony. Calcite also is predicted as part of the mineral 

assemblage as pH increases due to dissolution of sodium 

feldspar. Because of a lack of iron analyses for the water 

samples, the models are unable to predict the iron content of 

authigenic carbonate minerals. There is petrographic 

evidence that both ferroan and nonferroan carbonate 

minerals replace detrital feldspar grains, consistent with the 

general predictions of the model.

The types of diagenetic reactions that are consistent 

with the chemical evolution of waters along flow-path 3 

apply equally well to flow-paths 1 and 2, although minor 

modifications produced closer fits of the data. The 

important point to be made is that a few simple diagenetic 

reactions can explain the major changes in ground-water 

chemistry throughout the basin and that these same simple 

diagenetic reactions are consistent with textural and 

mineralogical changes in the rocks.

X12 Evolution of Sedimentary Basins Uinta and Piceance Basins
CO

LU

16

12

12

8

0

-1

-

" , 1 I

1 1 :: .:. ::: . ::. 1 I

.0 -0.6 -0.2

:

0 .2 0 6 1

0 SATURATION INDEX

Figure 11. Histograms of calculated saturation indexes for 

chalcedony (A) and quartz (B) in ground-water samples 

interpreted in this study. Vertical dotted lines denote 

equilibrium. Samples having positive values of SI are supersaturated, those having negative values are undersaturated.

Processes Affecting Salinity

Models 1-5 fail to predict the dramatic increase in 

TDS contents in the deepest central parts of the basin (fig. 

15). As seen in the Piper diagrams (figs. 5-7), the high-TDS 

waters contain high concentrations of sodium and chloride. 

One possible source of NaCl is connate water from ancient 

lake Uinta. M.L. Tuttle, C.A. Rice, and P.M. Briggs (U.S. 

Geological Survey, written commun., 1991) suggested that 

Soap Lake, Washington, is a possible modern analogue for 

ancient lake Uinta. Soap Lake has a water composition 

dominated by Na-CO3-SO4 and contains a significant 

amount of chloride, but the lakes that formed the Green 

River sediments probably had much lower sulfate 

concentrations because of almost complete bacterial 

reduction of sulfate in the water column (Tuttle, 1988). 

Thus, brines in ancient lake Uinta probably had a NaCO3-C1 character. Diagenetic evolution of this connate 

brine could have led to a Na-Cl character as feldspar 

minerals dissolved and carbonate minerals precipitated. A 

second source of NaCl could be upward migration of Na-Cl 

brines from the underlying evaporite-bearing Jurassic Arapien Shale.

Other conceptual models also may explain the high 

salinity of ground water in the central parts of the basin, but 

any conceptual model chosen must be able to explain the 

almost complete dominance of sodium and chloride in the 

ionic character of the high-TDS fluids. Therefore, the 

deep-basin system may be adequately modeled using a 

numerical model that adds halite to the solution without 

consideration of its origin.

Table 2. Features of models used to simulate changes in ground-water chemistry along flow-path 3

Model Minerals held at equilibrium Other features

1 Kaolinite

2 Kaolinite, calcite

3 Kaolinite, calcite, chalcedony

4 Kaolinite, dolomite, chalcedony

5 Kaolinite, dolomite, chalcedony

11 Step 1 Kaolinite, dolomite

Step 2 Kaolinite, dolomite, chalcedony

Step 3 Kaolinite, dolomite, chalcedony

12 Step 1 Kaolinite, calcite, dolomite

Step 2 Kaolinite, calcite, dolomite, chalcedony

Step 3 Kaolinite, calcite, dolomite, chalcedony

Temperature increased from 8 to 25 °C.

Dissolve sodium and potassium feldspar, add small amount 

of NaCl. 

Add NaCl.

Dissolve sodium and potassium feldspar, add small amount of

NaCl.

Add NaCl.

Ground-Water Chemistry and Diagenetic Reactions, Uinta Basin, Utah X13
10.0

8.0

6.0

I

O)

o

4.0

2.0

0.0

Microcline

Muscovite

Kaolinite

Albite

2.0 4.0 6.0 8.0 10.0 12.0

Log (Na+/H+)

Figure 12. Evolution of ground-water chemistry along flow-path 3 in Na+/H+ versus K+/H+ space. The arrowhead depicts the 

direction of ground-water flow. The phase boundaries are constructed for a temperature of 25 °C. Water temperatures along 

flow-path 3 ranged from 8.5 to 22 °C.

Models 11 and 12, which give the closest overall fit of 

the data of flow-path 3, utilized three consecutive sets of 

reactions, with subset steps in each set (table 2). As before, 

the initial fluid composition was taken as the most shallow, 

dilute sample. The only difference between models 11 and 

12 is the addition of calcite to the list of minerals 

constrained to be at equilibrium. Figures 16A and B show 

predicted variations in pH and ionic strength as compared to 

observed values. Figure 17 shows the model predictions in 

Na+/H+ versus K+/H+ space. Solution pH increases along 

the flow path due to dissolution of feldspar minerals, and 

salinity increases due to the addition of NaCl.

Models 11 and 12 require only slight modification to 

describe most of the ground-water chemical evolution of 

flow-paths 1 and 2. The major remaining problem is the 

higher total dissolved solids content in downdip reaches of 

flow-paths 1 and 2 (figs. 8-10). More NaCl must be added 

to adequately model flow-paths 1 and 2. In the natural 

system, this might correspond to a greater proportion of 

added brine (from whatever source) or perhaps to addition 

of a more concentrated brine.

CONCLUSIONS

Petrographic observations of rocks and geochemical 

data for coexisting waters indicate the sequence and nature 

of reactions that produced the authigenic phases in the 

Green River and Wasatch Formations in the Uinta basin. In 

the southern half of the basin, diagenesis took place at 

shallow to moderate burial depths at temperatures between 

9 and 45 °C. Carbonate cement, volumetrically the most 

important authigenic carbonate, precipitated from meteoric 

waters that evolved to isotopically heavier oxygen 

compositions through continued reactions with silicate 

phases, especially feldspar. Feldspar dissolution probably 

occurred during maximum burial at high temperatures, and 

analyses of present-day ground water indicate that 

dissolution could still be occurring. Kaolinite is present in 

rocks near the basin margin and probably formed concurrent 

with uplift and erosion of the Colorado Plateau.

The chemistry of ground water evolves along basinward flow paths from Ca-Mg-HCO3 type to Na-Cl type, 

typical for long-range flow paths in sedimentary basins.

X14 Evolution of Sedimentary Basins Uinta and Piceance Basins
8.0

7.0 -

6.0 -

O)

Q 5.0

4.0

3.0

-4.5 -4.0 -3.5 -3.0 -2.5 -2.0

Log[H4 Si04 ]

Figure 13. Results of models 1-5 for flow-path 3. Phase boundaries on the activity-activity diagram are from Drever (1982) and 

are constructed for 25 °C. Squares represent samples along flow-path 3 (see fig. 1).

Updip waters have near-neutral pH and low total dissolved 

solids contents (TDS) (less than 5,000 ppm), whereas 

downdip waters have higher pH, generally between 8 and 9, 

and much higher TDS contents (as much as 75,000 ppm). 

Computer modeling of ground-water chemical evolution 

used published analytical data and a modern 

thermodynamic data base. Preferred (though nonunique) 

solutions are consistent with petrographic and mineralogic 

observations. Thermodynamic calculations indicate that 

ground water in recharge zones is in equilibrium with 

observed authigenic kaolinite and is also capable of 

promoting the observed dissolution of feldspar. Feldspar 

dissolution probably supplies necessary soluble components 

for forming other diagenetic phases, including carbonate 

and clay minerals, observed in deeper rocks. Feldspar 

dissolution drives precipitation of carbonate minerals by 

contributing calcium to the solution and, more importantly, 

by increasing the pH of the water. Calcite precipitation 

buffers the pH and prevents it from rising above about 9. At 

all points along the flow path, silica concentrations most 

likely are controlled by the solubility of chalcedony, even 

though quartz is the thermodynamically stable phase.

Future studies should be directed at determining the 

source of the extreme salinity of the deep-basin waters. 

Trace-element and isotopic data may help to shorten the list

of possible salt sources. The chemical models described 

herein are a useful starting point, but future studies should 

attempt to construct mass-balanced models integrating 

additional data for the hydrologic regime with observed 

changes in water chemistry.

REFERENCES CITED

Bodine, M.W., Jr., and Jones, B.F., 1986, The Salt Norm A 

quantitative chemical-mineralogical characterization of 

natural waters: U.S. Geological Survey Water Resources 

Investigations Report 86-4086, 130 p.

Cole, R.D., and Picard, M.D., 1981, Sulfur isotope variations in 

marginal-lacustrine rocks of the Green River Formation, 

Colorado and Utah: Society of Economic Paleontologists 

and Mineralogists Special Publication, v. 31, p. 261-275.

Conroy, L.S., and Fields, F.K., 1977, Climatologic and hydrologic 

data, southeastern Uinta basin, Utah and Colorado, water 

years 1975 and 1976: Utah Department of Natural 

Resources Basic-Data Release 29, 244 p.

Drever, J.I., 1982, The geochemistry of natural waters: Englewood 

Cliffs, N.J., Prentice-Hall, 388 p.

Fouch, T.D., 1975, Lithofacies and related hydrocarbon 

accumulations in Tertiary strata of the western and central 

Uinta basin, Utah, in Bolyard, D.W., ed., Symposium on

Ground-Water Chemistry and Diagenetic Reactions, Uinta Basin, Utah X15
5.0

4.0

O

3.0

2.0

Muscovite

3.0 4.0 5.0 6.0 7.0 8.0

Log

Na+

Figure 14. Results of models 3-5 for flow-path 3. Phase boundaries on the activity-activity diagram are from Drever (1982) and 

are constructed for 25 °C. Squares represent samples along flow-path 3 (see fig. 1).

Deep Drilling Frontiers in the Central Rocky Mountains: 

Rocky Mountain Association of Geologists, p. 163-173.

Franczyk, K.J., Pitman, J.K., Cashion, W.B., Dyni, J.R., Fouch, 

T.D., Johnson, R.C., Chan, M.A., Donnell, J.R., Lawton, 

T.F., and Remy, R.R., 1989, Evolution of resource-rich 

foreland and intermontane basins in eastern Utah and 

western Colorado: International Geological Congress, 28th, 

Guidebook T324, American Geophysical Union, 53 p.

Hanor, J.S., and McManus, K.M., 1988, Sediment alteration and 

clay mineral diagenesis in a regional ground water flow 

system, Mississippi Gulf Coastal Plain: Transactions, Gulf 

Coast Association of Geological Societies, v. 38, 

p. 495-502.

Harrison, A.G., and Thode, H.G., 1958, Sulphur isotope 

abundances in hydrocarbons and source rocks of the Uinta 

basin, Utah: American Association of Petroleum Geologists 

Bulletin, v. 42, p. 2642-2649.

Hood, J.W., Mundoiff, J.C., and Price, D., 1976, Selected 

hydrologic data, Uinta basin area, Utah and Colorado: Utah 

Department of Natural Resources Basic-Data Release 26, 

321 pp.

Kharaka, Y.K., Gunter, W.D., Aggarwal, P.K., Perkins, E.H., and 

DeBraal, J.D., 1988, SOLMINEQ.88-A computer program 

for geochemical modeling of water-rock interactions: U.S. 

Geological Survey Water-Resources Investigations 

88^227, 420 p.

Lee, R.W., 1985, Geochemistry of groundwater in Cretaceous 

sediments of the southeastern coastal plain of eastern 

Mississippi and western Alabama: Water Resources 

Research, v. 21, p. 1545-1556.

Mauger, R.L., 1972, A sulfur isotope study of bituminous sands 

from the Uinta basin, Utah: International Geology 

Congress, 24th, Proceedings, Comptes Rendus, sec. 5, 

p. 19-27.

Merino, E., 1975a, Diagenesis in Tertiary sandstones from Kettleman North Dome, California, I, Diagenetic mineralogy: 

Journal of Sedimentary Petrology, v. 45, p. 320-336.

____ 1975b, Diagenesis in Tertiary sandstones from Kettleman 

North Dome, California, II, Interstitial solutions Distribution of aqueous species at 100 °C and chemical relation to 

diagenetic mineralogy: Geochimica et Cosmochimica Acta, 

v. 39, p. 1629-1645.

Parkhurst, D.L., Plummer, L.N., and Thorstenson, D.C., 1980, 

PHREEQE A computer program for geochemical 

calculations: U.S. Geological Survey Water-Resources 

Investigations 80-96, 210 p.

____ 1982, BALANCE A computer program for calculating 

mass transfer for geochemical reactions in ground water: 

U.S. Geological Survey Water-Resources Investigations 

82-14, 29 p.

X16 Evolution of Sedimentary Basins Uinta and Piceance Basins
0.16

0.12

<

d

Q 0.08

0.04

0.00

PHREEQE Models

STEP NUMBER

Figure 15. Total dissolved solids (IDS) along flow-path 3, as compared to the predictions using PHREEQE (solid lines). IDS is 

given in total molality of solutes. Squares represent samples along flow-path 3 (see fig. 1).

Pitman, J.K., Anders, D.E., Fouch, T.D., and Nichols, D.J., 1986, 

Hydrocarbon potential of nonmarine Upper Cretaceous and 

Lower Tertiary rocks, eastern Uinta basin, Utah, in Spencer, 

C.W., and Mast, R.F., eds., Geology of tight gas reservoirs: 

American Association of Petroleum Geologists Studies in 

Geology 24, p. 235-252.

Pitman, J.K., Fouch, T.D., and Goldhaber, M.B., 1982, 

Depositional setting and diagenetic evolution of some 

Tertiary unconventional reservoir rocks, Uinta basin, Utah: 

American Association of Petroleum Geologists Bulletin, v. 

66, p. 1581-1596.

Price, D., and Miller, L.L., 1975, Hydrologic reconnaissance of the 

southern Uinta basin, Utah and Colorado: Utah Department 

of Natural Resources Technical Publication 49, 66 p.

Ryder, R.T., Fouch, T.D., and Elison, J.H., 1976, Early Tertiary 

sedimentation in the western Uinta basin: Geological 

Society of America Bulletin v. 87, p. 496-512.

Tuttle, M.L., 1988, Geochemical evolution and depositional 

history of sediment in modern and ancient saline lakes 

Evidence from sulfur geochemistry: Golden, Colorado 

School of Mines, Ph. D. thesis, 312 p.

Ground-Water Chemistry and Diagenetic Reactions, Uinta Basin, Utah X17
0.20

0.15-

0.10-

0.05-

0.00

Models 11 and 12

4 -

5 6 

Log [Na+] / [H+]

Figure 17. Chemical evolution of ground water in Na+/H+ 

versus K+/H+ space, as predicted by models 11 and 12. Data 

points shown are for samples along flow-path 3.

DISTANCE ALONG FLOW PATH

Figure 16. Predicted variations in pH (A) and ionic strength 

(6) according to models 11 and 12. Data points shown are for 

samples along flow-path 3.

X18 Evolution of Sedimentary Basins Uinta and Piceance Basins
Appendix List of unique field-identification numbers and sample dates for water analyses meeting 

criteria for completeness and accuracy described in the text

Using this list of ID numbers, the reader can consult the appropriate source reference to obtain the complete 

analysis. The sample numbers in the format GR-XX are the sample numbers designated in this study. Local ID 

refers to the sample number given in the source reference, which, along with the sample date or depth, uniquely 

identifies the sample. Dates are in the format YY-MM-DD; depths are in meters.

Sample No. Local ID Sample date Sample No. Local ID Sample date

Samples from Hood and others (1976)

GR-01

GR-02

GR-03

GR-04

GR-05

GR-06

GR-07

GR-08

GR-09

GR-10

GR-11

GR-12

GR-13

GR-14

GR-15

GR-16

GR-17

GR-18

GR-19

GR-20

GR-21

GR-22

GR-23

CiR-24

(iR-25

GR-26

GR-27

GR-28

GR-29

GR-30

GR-31

GR-32

GR-33

GR-34

GR-35

GR-36

GR-37

GR-38

GR-39

GR-40

(D-6-21)27cdc-l

(D-6-21)33adc-l

(D-6-21)33adc-l

(D-6-21)34bdc-l

(D-6-21)34bdc-l

(D-6-21)35bbb-l

(D-7-22)14bba-l

(D-7-22)22aac-l

(D-7-22)22acc-lS

(D-7-22)22bab-l

(D-7-22)22cca-l

(D-7-22)25cad-l

(D-7-22)28cca-l

(D-7-22)29abb-l

(D-7-22)29cab-l

(D-7-22)29cab-l

(D-7-22)29cac-l

(D-7-22)34bac-l

(D-7-23)13bab-l

(D-7-23)14cdd-l

(D-7-23)14dad-l

(D-7-23)25aab-l

(D-7-23)27ccc-l

(D-7-23)28cad-l

(D-7-23)29ccc-l

(D-7-23)29ccc-l

(D-7-24)28acd-l

(D-7-24)31acb-l

(D-7-24)36aaa-l

(D-8-21)29bcc-l

(D-8-21)29bcc-l

(D-8-21)29bcc-l

(D-8-22) 4dcd-l

(D-8-23)18dbb-l

(D-10-22)17aadlS

(D-ll-21)31bdd-l

(D-ll-24) 8caa-l

(D-13-23)26acd-l

U(D-l-l)21cbd-l

U(D-l-l)21dbc-l

65-03-08

65-04-20

65-04-20

65-01-16

65-01-16

65-03-04

70-05-01

70-05-01

70-05-01

70-05-01

71-06-15

65-07-07

70-03-27

71-07-16

70-05-29

70-05-29

68-11-01

65-06-16

69-01-31

65-01-15

69-01-31

70-12-30

69-02-03

69-02-03

69-09-18

69-09-18

66-01-06

63-04-17

65-03-02

69-07-16

65-02-12

65-05-27

65-04-08

65-03-04

64-05-11

71-08-31

61-09-06

60-06-00

67-08-24

59-11-05

GR-101

GR-102

GR-103

GR-104

GR-105

GR-106

GR-107

GR-108

GR-109

GR-110

GR-11 1

GR-112

GR-113

GR-114

GR-115

GR-116

GR-117

GR-118

GR-119

GR-120

GR-121

GR-122

GR-123

GR-124

GR-125

GR-126

GR-127

GR-128

GR-129

GR-130

GR-131

GR-132

GR-133

GR-134

GR-135

GR-136

GR-137

GR-138

GR-139

GR-140

GR-141

GR-142

(D-9-20)36ddc-l

(D-9-20)36ddc-l

(D-9-20)36ddc-l

(D-9-20)36ddc-l

(D-10-16)llacd-l

(D-10-16)llacd-l

(D-10-16)lldac-l

(D-10-19)lcbd-l

(D-10-20)4ccb-l

(D-ll-15)2ccc-l

(D-14-20)30bab-l

U(C-l-l)8acd-l

U(C-l-l)8acd-l

U(C-l-l)13ccd-l

U(C-l-2)3bcd-l

U(C-l-2)7cac-l

U(C-l-2)7cac-l

U(C-l-2)7cac-l

U(C-l-2)7cac-l

U(C-l-2)7cac-l

U(C-l-2)7cac-l

U(C-l-2)llbba-l

U(C-l-2)llbba-l

U(C-l-2)llbba-l

U(C-l-2)llbba-l

U(C-l-2)7cac-ls

U(C-l-2)7cac-ls

U(C-3-6)8bba-l

U(C-3-6)18bbd-l

U(C-3-6)18bbd-l

U(C-3-6)18bbd-l

U(C-3-6)18bbd-l

U(C-3-6)18bbd-l

U(C-3-6)20acb-l

U(C-3-7)22acd-l

U(C-3-7)22acd-l

U(C-3-7)22acd-l

U(C-4-l)13dad-l

U(C-4-l)13dad-l

U(C-4-5)10bdd-ls

U(C-4-9)16dba-l

U(C-4-ll)33bda-sl

69-7-29

69-7-30

69-7-31

69-7-31

64-10-1

64-10-18

63-04-00

63-10-15

63-07-00

67-10-3

63-7-22

63-11-7

63-11-30

60-05-04

67-12-04

70-01-23

70-01-24

70-01-25

70-01-26

70-01-27

70-05-06

67-10-02

67-10-03

67-12-04

68-4-26

69-4-18

70-2-26

68-9-16

65-9-30

65-10-1

65-11-1

65-11-19

66-1-7

69-10-22

70-3-26

70-3-27

70-4-9

69-4-10

69-4-10

72-1-4

71-1-25

71-10-21

Ground-Water Chemistry and Diagenetic Reactions, Uinta Basin, Utah X19
Appendix List of unique field-identification numbers and sample dates for water analyses meeting 

criteria for completeness and accuracy described in the text Continued

Sample No. Local ID Sample date Sample No. Local ID Sample date

Samples from Conroy and Fields (1977)

GR-143

GR-144

GR-145

GR-146

GR-147

GR-148

GR-149

GR-150

GR-151

GR-152

GR-153

GR-154

GR-155

GR-156

GR-157

GR-158

GR-159

GR-160

GR-161

GR-162

GR-163

GR-164

GR-165

GR-166

GR-167

GR-168

GR-169

GR-170

GR-171

GR-172

GR-173

GR-174

GR-175

GR-176

GR-177

GR-178

GR-179

GR-180

GR-181

GR-182

GR-183

GR-184

GR-185

GR-186

(D-10-20)35bbc-l

(D-10-21)2aca-l

(D-10-21)16add-l

(D-10-21)16add-l

(D-10-22)17aad-l

(D-10-22)17aad-l

(D-10-24)12bdb-l

(D-10-24)12bdb-l

(D-10-24)12bdb-l

(D-10-24)12cda-l

(D-10-24)12cda-l

(D-10-24)12cda-l

(D-10-24)12cda-l

(D-10-24)12cda-l

(D-10-24)12cda-l

(D-10-24)12cda-l

(D-10-24)13adb-l

(D-10-24)13adb-l

(D-10-24)13adb-l

(D-10-24)13adb-2

(D-10-24)13adb-2

(D-10-24)13adb-2

(D-10-24)13adb-2

(D-10-24)13adb-2

(D-10-24)13adb-2

(D-10-24)13ccc-l

(D-10-24)13ccc-l

(D-10-24)13ccc-l

(D-10-24)13ccc-l

(D-10-24)13ccc-l

(D-10-24)13ccc-l

(D-10-24)13ccc-l

(D-10-24)20aad-l

(D-10-24)20aad-l

(D-10-24)20aad-l

(D-10-24)20aad-l

(D-10-24)20aad-l

(D-10-24)20aad-l

(D-10-24)20aad-l

(D-10-24)20aad-l

(D-10-24)20aad-l

(D-10-24)20aad-l

(D-10-24)20aad-2

(D-10-24)20aad-2

74-8-20

75-6-25

74-8-21

75-6-25

74-8-21

75-6-25

75-11-12

76-6-24

76-9-14

74-11-20

75-3-18

75-5-13

75-6-26

75-8-30

75-11-14

76-6-24

75-11-12

76-6-24

76-9-16

74-11-19

74-11-21

75-3-13

75-11-12

76-6-24

76-9-16

74-11-22

74-12-13

75-3-14

75-11-13

76-3-21

76-6-30

76-9-14

75-3-13

75-5-12

75-6-24

75-7-27

75-8-18

75-8-19

75-11-13

76-3-17

76-6-26

76-9-19

74-11-27

74-12-11

GR-187

GR-188

GR-189

GR-190

GR-191

GR-192

GR-193

GR-194

GR-195

GR-196

GR-197

GR-198

GR-199

GR-200

GR-201

GR-202

GR-203

GR-204

GR-205

GR-206

GR-207

GR-208

GR-209

GR-210

GR-211

GR-212

GR-213

GR-214

GR-215

GR-216

GR-217

GR-218

GR-219

GR-220

GR-221

GR-222

GR-223

GR-224

GR-225

GR-226

GR-227

GR-228

GR-229

(D-10-24)20aad-2

(D-10-24)20aad-2

(D-10-24)20aad-2

(D-10-24)20aad-2

(D-10-24)20aad-2

(D-10-24)25caa-l

(D-10-24)25caa-l

(D-10-24)25caa-l

(D-10-24)25caa-l

(D-10-24)28ddb-l

(D-10-24)36dcd-l

(D-10-24)36dcd-l

(D-10-25)19dda-l

(D-10-25)19dda-l

(D-ll-21)31bdd-l

(D-ll-23)13dcd-l

(D-ll-24)6dbc-l

(D-ll-24)6dbc-l

(D-ll-24)7cac-l

(D-ll-24)7cac-l

(D-ll-24)8caa-l

(D-ll-25)7dac-l

(D-ll-25)7dac-l

(D-ll-25)21cca-l

(D-ll-25)21cca-l

(D-13-25)13add-sl

(D-14-22)25cac-sl

(D-14-24)21ccc-sl

(D-15-20)15bbd-sl

(D-15-23)36ddd-sl

(D-15-25)7bcc-sl

(D-15-25)13bad-sl

(D-15-25)18cda-sl

(D-16-19)18cbc-sl

(D-16-22)23dad-sl

(D-16-23)16bbd-sl

(D-17-19)9acb-sl

(D-17-19)28bab-sl

(D-17-21)10bdd-sl

(D-17-22)19bbd-sl

(D-18-20)7bad-sl

(D-19-19)36caa-sl

S(C-5-104)36cad-sl

75-3-13

75-9-11

75-9-12

75-11-13

76-6-26

74-11-21

74-12-10

75-3-12

75-11-11

75-12-10

74-11-19

75-11-10

75-11-12

76-9-14

74-8-20

75-6-26

74-9-10

75-6-26

74-9-10

75-6-26

74-9-10

75-3-12

75-11-11

75-3-12

75-11-11

74-9-12

74-8-21

74-8-23

75-6-17

75-6-18

74-8-22

74-9-11

76-9-16

74-8-20

74-8-22

74-8-22

75-6-17

74-8-20

75-6-19

74-8-22

74-8-20

75-6-17

74-9-11

X20 Evolution of Sedimentary Basins Uinta and Piceance Basins
Appendix List of unique field-identification numbers and sample dates for water analyses meeting 

criteria for completeness and accuracy described in the text Continued

Sample No. Local ID Sample depth Sample No. Local ID Sample depth

Samples from Price and Miller (1975)

GR-41

GR-42

GR-43

GR-44

GR-45

GR-46

GR-47

GR-48

GR-49

GR-50

GR-51

GR-52

GR-53

GR-54

GR-55

GR-56

(D-9-20)36ddc-l

(D-9-20)36ddc-l

(D-9-20)36ddc-l

(D-9-20)36ddc-l

(D-10-16)llacd-l

(D-10-16)16acd-l

(D-10-17)30bbd-l

(D-10-17)30bbd-l

(D-l(M8)13cdb-l

(D-10-18)14-bbd-l

(D-10-18)14-bbd-l

(D-10-18)14-bbd-l

(D-10-18)14-bbd-l

(D-10-19)lcbd-l

(D-10-20)4ccb-l

(D-10-20)7cdb-l

690-1,028

690-1,079

690-1,179

690-1,179

1,563-1,575

1,318-1,329

1,377-1,381

1,484-1,500

1,475-1,487

788-832

1,342-1,366

1,413-1,427

1,542-1,571

1,039-1,048

1,057-1,094

755-764

GR-57

GR-58

GR-59

GR-60

GR-61

GR-62

GR-63

GR-64

GR-65

GR-66

GR-67

GR-68

GR-69

GR-70

GR-71

GR-72

(D-10-20)7cdb-l

(D-10-20)8cab-l

(D-10-20)8cab-l

(D-10-21)16add-l

(D-10-23)24bba-l

(D-ll-21)14baa-l

(D-ll-16) 3bbc-l

(D-ll-16) 3bbc-l

(D-ll-24) 8caa-l

(D-14-20)30bab-l

U(C-4-l)13dad-l

U(C-4-l)13dad-l

U(C-4-4)13dda-l

U(C-4-4)16aca-l

U(C-4-5)10bdd-l

U(C-6-6)35bdd-l

1,131-1,145

1,207-1,216

1,272-1,281

690-1,283

1,118

231-237

1,502-1,520

1,530-1,538

465

686-696

1,465-1,487

1,874-1,934

2,140-2,164

1,010-1,221

2,309-2,363

1,163-1,188

&U.S. GOVERNMENT PRINTING OFFICE: 1991-573-049/46010

Ground-Water Chemistry and Diagenetic Reactions, Uinta Basin, Utah X21



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