Thermal Maturation of the 

Eastern Anadarko Basin, Oklahoma

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Chapter C

Thermal Maturation of the 

Eastern Anadarko Basin, Oklahoma

By MARK J. PAWLEWICZ

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 1866

EVOLUTION OF SEDIMENTARY BASINS ANADARKO BASIN
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: 1989

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

Pawlewicz, M. J.

Thermal maturation of the eastern Anadarko Basin, Oklahoma / by Mark J. 

Pawlewicz.

p. cm. (Evolution of sedimentary basins Anadarko Basin ; ch. 

C) (U.S. Geological Survey bulletin ; 1866-C) 

Bibliography: p. 

Supt. of Docs, no.: I 19.3: 1988-C

1. Earth temperature Anadarko Basin Measurement.

2. Geology Anadarko Basin. 3. Petroleum Geology Anadarko 

Basin. 4. Anadarko Basin. I. Title. II. Series. III. Series: U.S. Geological 

Survey bulletin ; 1866-C. 

QE75.B9 no. 1866-C 

[QE509]

557.3 s-dc20 89-600156 

[551.1'4'09766] CIP
CONTENTS

Abstract Cl 

Introduction Cl 

Methods C2 

Regression analysis C3 

Discussion C5 

Burial history C7

Reflectance and temperature C8 

Conclusions C9 

References cited C12

FIGURES

1. Map showing location of Anadarko basin and line of well profile Cl

2. Semilogarithmic plots of vitrinite reflectance versus depth for this and other

studies C3 

3-5. Burial history reconstruction for:

3. No. 1 Atchison well at northern end of well profile C8

4. No. 1 Petree Ranch well near middle of well profile C9

5. No. 51-11 Weller well near southern end of well

profile CIO

6. Cross section along well profile showing isoreflectance lines at 0.6 and 1.3 

percent Rm Cll

TABLES

1. Location of boreholes used in study C2

2. Vitrinite reflectance, depth, reflectance statistics, and temperature for samples 

from wells in this study C4

3. Geothermal gradients for selected wells in study area C6

Contents III
CONVERSION FACTORS FOR SOME SI METRIC AND U.S. UNITS OF MEASURE

To convert from To Multiply by

Feet (ft) Meters (m) 0.3048

Miles (mi) Kilometers (km) 1.609

Pounds (Ib) Kilograms (kg) 0.4536

Degrees Fahrenheit (°F) Degrees Celsius (°C) Temp °C = (temp °F-32)/1.8

IV Contents
EVOLUTION OF SEDIMENTARY BASINS-ANADARKO BASIN

Thermal Maturation of the

Eastern Anadarko Basin, Oklahoma

By Mark J. Pawlewicz

Abstract

Vitrinite reflectance (Rm) measurements on samples 

from wells along a line extending for 125 mi (200 km) from 

the northern shelf area of the Anadarko basin near the 

Kansas State line south to the deep part of the basin show 

that the level of thermal maturity of sedimentary organic 

matter in the samples was set after maximum burial.

Burial history reconstruction curves show the tectonic 

evolution of this area: minimal subsidence occurred in the 

northern part of the basin in the Early Paleozoic, and 

moderate to rapid subsidence occurred throughout most of 

the remaining part of the basin from the Middle Ordovician to 

Permian. Temperatures determined from reflectance values 

are high as compared to those generally accepted for the 

onset of hydrocarbon generation and also to those obtained 

from other similar studies in the basin. Regression analysis 

yields a reflectance gradient of 0.109 percent Rm/1,000 ft 

(300 m) along the profile. Isoreflectance lines show the depth 

to the 0.6- and 1.3-percent Rm levels, the window of oil 

generation. The isoreflectance lines can be used to estimate 

the level of thermal maturity above or below them.

INTRODUCTION

The Anadarko basin (fig. 1) in west-central 

Oklahoma contains the thickest section of Paleozoic 

sedimentary rocks on the North American craton; more 

than 36,000 ft (11 km) of sediments accumulated in the 

deepest parts of the basin (Garner and Turcotte, 1984). 

The basin is bounded on the east by the Nemaha uplift, 

on the north and west by shelf areas, and on the south by 

the Amarillo-Wichita uplift (Evans, 1979).

In the Precambrian, what is now the southern 

Oklahoma region was rifted to form the southern 

Oklahoma aulacogen (Hoffman and others, 1974). In the 

Early Cambrian, the area was faulted and igneous rocks 

emplaced; igneous activity ended in the Middle Cam37e

101 C 99° 97°

36°

35° I

GENERALIZED OUTLINE 

OF ANADARKO BASIN

I_______I_____

0

1

0 50

50 100 MILES 

1 1

1 

100 KILOMETERS

Manuscript approved for publication May 18, 1989.

Figure 1. Location of Anadarko basin and line of well profile 

(A-A 1 ). Well data given in table 1. Modified from Adkison 

(1960).

brian. The Anadarko basin was formed during an orogenic breakup of the aulacogen in the Pennsylvanian 

(Webster, 1980). The Late Mississippian through Early 

Pennsylvanian was marked by a renewed phase of 

accelerated subsidence and by narrowing of the 

depositional trough in the Anadarko basin (Garner and 

Turcotte, 1984). Detailed discussions of the depositional 

history of the basin are presented by Huffman (1959) and 

Adler (1971).

In the present study, I investigated the paleogeothermal history of the eastern part of the Anadarko basin 

by measuring vitrinite reflectance of samples from a 

series of wells (fig. 1, table 1). Two additional data sets

Thermal Maturation of the Eastern Anadarko Basin, Oklahoma C1
Table 1 . Location of boreholes used in study

[Wells in this study are shown by number in figure 1. All wells are in Oklahoma unless noted]

Well

no. Company Well name County

Location

(sec., T., R.)

Adkison (1960)

1 Pure Oil Company 1 William Palmer

2 Harbar Drilling and Atlantic Refining Company 1 Knorp

3 Ohio Oil Company

4 Olson Drilling Company

5 Superior Oil Company

6 Superior Oil Company

7 Superior Oil Company

8 Superior Oil Company

9 Atlantic Refining Company

10 Gait-Brown Company

11 Cameo Oil and Trust

12 Ramsey Petroleum Company

13 Exploration Oil and Gas

14 Cities Service Oil Company

15 Denver Producing and Refining Company

16 Denver Producing and Refining Company

17 Superior Oil Company

1 W.O. Parr

1 Atchison

28-22 Schultz

41-27 Manning

63-30 Fuller

81-17 H.W. Norris

1 Vilhauer

1 Campbell

1 F. Parrington

1 Mansfield

1 E. Hadlock

1 Petree Ranch

1 School Land

ISahCam

51-llWeller

Barber (Kans.)

Barber (Kans.)

Alfalfa

Alfalfa

Major

Major

Major

Blaine

Kingfisher

Kingfisher

Kingfisher

Canadian

Canadian

Canadian

Caddo

Caddo

Caddo

10,338., 10W.

27,348., 10W.

9,28N., 10 W.

12, 24 N., 11 W.

22, 23 N., 10W.

27, 22 N., 10W.

30, 2 IN., 10 W.

17, 19 N., 10 W.

22, 18N..9W.

6, 16 N., 7 W.

14, 15 N., 8 W.

16, 14N..9W.

30, 13 N., 9 W.

18, 11N..8W.

16, ION., 9 W.

33, ION., 10W.

11.8N., 12 W.

This study

1 Olson Drilling Company

2 Sun Set International Petroleum Company

3 Cleary Petroleum

4 Gait-Brown Company

5 Shenandoah Oil

6 Exploration Oil and Gas

7 Cities Service Oil Company

8 Apexco

9 Texas Pacific Oil

10 Jones & Pellow Oil Company

1 1 Superior Oil Company

12 American Petroleum

13 Texaco

14 Sunray

1 Atchison

1 Milacek

1 Phillips

1 Campbell

IVogt

1 E. Hadlock

1 Petree Ranch

1 Buell State

1 Cherry

33-1 Marathon

51-llWeller

1 Sprague

Carr

1 Mazur

Alfalfa

Major

Major

Kingfisher

Kingfisher

Canadian

Canadian

Caddo

Caddo

Caddo

Caddo

Caddo

Caddo

Caddo

12, 24 N., 11 W.

17, 23 N., 9 W.

13, 19 N., 10 W.

6, 16 N., 7 W.

16, 15 N., 8 W.

30, 13 N., 9 W.

18, 11N..8W.

10, 11 N., 12 W.

13, ION., 9 W.

33, ION., 10W

11.8N., 12 W.

11.8N., 12 W.

36, 5 R, 11 W.

1, 3 N., 5 W.

were also evaluated to determine if vitrinite reflectance 

data obtained by different methods, from a diversity of 

lithologies, can be used interchangeably to evaluate 

thermal maturity in the Anadarko basin.

METHODS

The samples for this study are core and cuttings 

samples from the Oklahoma Geological Survey core 

library in Norman, Okla. They range in age from Permian to Silurian and span a depth interval from 3,800 to 

17,200 ft (1,160-5,240 m). Their lithologies include 

sandstone, shale, and carbonate rocks. The samples were 

processed using the rapid concentration technique 

described in Barker and Pawlewicz (1986a), and polished 

slides for reflectance analysis were prepared using the 

procedure described in Baskin (1979).

The quality of each polished slide, in terms of 

abundance of vitrinite, ranges from poor to excellent. 

The number of readings per slide varied from 5 to more

than 100; the targeted number was 50 but was not always 

possible. The amount of kerogen recovered from each 

sample is commonly a function of lithology and typically 

decreases from shale to sandstone to limestone. In 

addition, the material actually measured is a function of 

both the efficiency of the kerogen concentration 

technique and the material exposed to view during the 

microscope examination. Only data from the first 

reflectance analysis were used for this study, and recycled 

and uphole-cavings material was passed over. Problems 

inherent with sampling for and performing vitrinite 

reflectance have been discussed in Barker and Pawlewicz 

(1986b).

Two additional data sets (Cardott and Lambert, 

1985; Schmoker, 1986) were analyzed by using reduced 

major axis regression in order to give a basis for 

comparison between those data and the data from this 

study (fig. 2). These two data sets were used because they 

were compiled by different means and for different 

purposes. One set (Cardott and Lambert) was generated

C2 Evolution of Sedimentary Basins Anadarko Basin
0.1

5,000

10,000

: i5,ooo

20.000

25,000

30,000 LVITRINITE REFLECTANCE, IN PERCENT 

1 10

Q

VITRINITE REFLECTANCE, IN PERCENT 

1 10

30,000 iB

5,000 -

10,000 -

~ 15,000

20,000 -

25,000

30,000 LVITRINITE REFLECTANCE, IN PERCENT

D

0.1

5.000

10,000

: 15,000

20,000

25,000

30.000 L

VITRINITE REFLECTANCE, IN PERCENT

1 10

Figure 2. Semilogarithmic plots of vitrinite reflectance (Rm) versus depth. A, This study; B, Schmoker (1986); C, Cardott and 

Lambert (1985); D, Data sets A, B, and C, combined.

by a single operator from samples from a single lithologic 

unit, the Woodford Shale, and the other set (Schmoker) 

was compiled from the literature and represents the work 

of several individuals. The differences between the data 

form the basis for not only a one-to-one comparison but 

also for an evaluation as to the applicability of the data in 

evaluating thermal maturation in the basin.

REGRESSION ANALYSIS

Regression analysis allows quantification of a 

relationship between a pair of variables such that other 

values can be interpolated or extrapolated. The reduced 

major axis regression technique discussed in Till (1974) 

was used to analyze all three data sets. This technique

Thermal Maturation of the Eastern Anadarko Basin, Oklahoma C3
Table 2. Vitrinite reflectance, depth, reflectance statistics, temperature, and age for samples wells in this study 

[Location of wells shown in figure 1; well data given in table 1. Rm, vitrinite reflectance; n, number of Rm readings; CT, standard deviation. 

Temperature calculated using surface temperature of 60 °F (15 °C) and geothermal gradient of 1.3 °F/100 ft. Time units are generalized because 

most samples are cuttings and knowledge of local stratigraphy is imprecise. Ages from Adkison (I960)]

Depth 

Well number and name (feet)

1. 1 Atchison 5,360

6,748

7,177

2. 1 Milacek 4,995

5,805

6,205

6,710

7,205

3. 1 Phillips 1,905

2,465

3,765

4,225

5,072

5,112

4. 1 Campbell 4,155

4,800

5,445

6,007

6,815

7,483

7,883

5. 1 Vogt 6,385

6,815

7,455

7,755

8,215

8,705

9,115

9,720

6. 1 E. Hadlock 8,837

9,100

9,595

9,862

10,017

7. 1 Petree Ranch 7,675

8,075

8,925

9,565

10,005

10,705

10,995

8. 1 Buell State* 13,831

9. 1 Cherry 9,215

10,205

10,805

11,205

11,705

Rm 

(percent)

1.02

1.02

1.22

.69

.66

.63

.80

.82

1.17

1.43

.93

.89

1.50

1.58

.78

1.29

.83

1.00

.76

.69

.94

.73

.82

.81

.80

.78

.76

.86

.72

.83

.70

.74

.97

1.06

.82

.84

.97

1.17

1.07

1.44

1.65

1.91

.94

.97

.87

1.04

.97

n

21

5

16

36

51

51

37

37

29

57

19

27

38

65

5

21

44

37

81

55

37

25

51

51

51

51

51

51

51

35

45

55

52

51

15

53

39

71

71

61

17

35

45

61

47

75

51

a

0.21

.12

.37

.08

.08

.09

.10

.13

.24

.21

.20

.21

.21

.19

.18

.16

.22

.19

.09

.10

.18

.09

.12

.11

.13

.08

.11

.10

.11

.11

.12

.07

.14

.12

.08

.13

.17

.17

.13

.21

.27

.17

.17

.20

.16

.09

.08

Temperature

op oc

130

148

154

125

135

141

147

154

85

93

109

115

126

127

115

122

130

138

148

158

163

143

148

158

159

167

173

178

186

179

178

185

189

190

160

165

176

185

190

199

203

239

180

193

200

206

212

54

64

68

52

57

61

64

68

29

34

43

46

52

53

46

50

54

59

64

70

73

62

64

70

71

75

78

81

86

79

81

85

87

88

71

74

80

85

88

93

95

115

83

90

93

97

100

Age

Pennsylvanian System; Missourian Series

Mississippian System; Lower Miss. Series

Ordovician System

Pennsylvanian System; Virgilian Series

Pennsylvanian System; Missourian Series

Pennsylvanian System; Des Moinesian Series

Lower Mississippian Series

Ordovician System

Permian System

Permian System

Permian System

Pennsylvanian System

Pennsylvanian System

Pennsylvanian System

Pennsylvanian System; Virgilian Series

Pennsylvanian System; Virgilian Series

Pennsylvanian System; Virgilian Series

Pennsylvanian System; Missourian Series

Pennsylvanian System; Missourian Series

Pennsylvanian System; Des Moinesian Series

Mississippian System; Upper Miss. Series

Pennsylvanian System; Virgilian Series

Pennsylvanian System; Virgilian Series

Pennsylvanian System; Missourian Series

Pennsylvanian System; Missourian Series

Pennsylvanian System; Missourian Series

Pennsylvanian System; Des Moinesian Series

Pennsylvanian System; Des Moinesian Series

Mississippian System; Upper Miss. Series

Pennsylvanian System; Missourian Series

Pennsylvanian System; Missourian Series

PennsylvanianSystem; Des Moinesian Series

Pennsylvanian System; Des Moinesian Series

Mississippian System; Upper Miss. Series

Pennsylvanian System; Virgilian Series

Pennsylvanian System; Missourian Series

Pennsylvanian System; Missourian Series

Pennsylvanian System; Des Moinesian Series

Pennsylvanian System; Des Moinesian Series

Pennsylvania System; Atokan Series

Mississippian System; Upper Miss. Series

Pennsylvanian System; Atokan Series

Pennsylvanian System; Missourian Series

Pennsylvanian System; Missourian Series

Pennsylvanian System; Des Moinesian Series

Pennsylvanian System; Des Moinesian Series

Pennsylvanian System; Des Moinesian Series

C4 Evolution of Sedimentary Basins Anadarko Basin
Table 2. Continued

Depth 

Well number and name (feet)

10. 33-1 Marathon 8,105

9,305

10,105

10,305

11. 51-llWeller 7,705

8,782

10,727

11,477

12,362

14,000

15,817

16,472

17,127

12. 1 Sprague 4,205

5,805

7,065

8,555

9,265

10,125

13. 1 Carr* 10,814

11,469

11,747

12,155

17,002

14. 1 Mazur 15,935

16,099

17,055

17,217

Rm 

(percent)

0.90

.83

.86

.99

.67

.71

.96

.86

1.13

1.63

2.07

2.03

2.20

.93

1.18

.89

.82

.90

.78

.98

1.04

1.06

1.04

1.77

1.71

1.42

1.19

1.73

n

20

37

9

21

61

23

11

45

61

55

55

35

101

17

41

40

55

31

35

35

45

29

45

55

1

11

5

10

a

0.12

.14

.14

.16

.08

.11

.13

.13

.07

.22

.29

.25

.22

.15

.20

.18

.11

.16

.08

.11

.10

.10

.11

.19

None

.14

.25

.31

Temperature

op oC

165

181

191

194

160

174

200

210

221

242

266

275

282

114

135

152

172

181

191

200

210

212

219

281

267

269

282

140

74

83

88

90

71

79

93

99

105

117

130

135

139

46

57

67

78

83

88

93

99

100

104

138

131

132

139

284

Age

PennsylvanianSystem; VirgilianSeries

Pennsylvania!! System; Virgilian Series

Pennsylvanian System; Virgilian Series

Pennsylvanian System; Virgilian Series

Pennsylvanian System; Virgilian Series

Pennsylvanian System; Missourian Series

Pennsylvanian System; Missourian Series

Pennsylvanian System; Des Moinesian Series

Pennsylvanian System; Des Moinesian Series

Pennsylvanian System; Atokan Series

Pennsylvanian System; Morrowan Series

Pennsylvanian System; Morrowan Series

Pennsylvanian System; Morrowan Series

Permian System

Permian System

Pennsylvanian System; Virgilian Series

Pennsylvanian System; Missourian Series

Pennsylvanian System; Missourian Series

Pennsylvanian System; Missourian Series

Pennsylvanian System

Pennsylvanian System

Pennsylvanian System

Pennsylvanian System; Atokan Series

Ordovician System

Silurian System

Silurian System

Silurian System

Silurian System

*Core sample

makes allowances for (1) the lack of precise depth 

control inherent with cuttings samples, and (2) the lack of 

precision in reflectance (Rm) values that results from the 

use of the mean of a set of numbers having a relatively 

wide range. The more common least-squares analysis 

requires that one variable (either depth or Rm) be known 

with certainty.

Semilogarithmic plots of vitrinite reflectance 

versus depth for the three data sets are shown in figure 2. 

Data from the No. 1 Phillips well (table 2) were included 

in the regression curve for data set^l for comparison but 

were excluded from regression calculations because of 

unexplained high Rm values for samples from shallow 

depths. Data from the No. 1 Mazur well were included in 

the regression calculations even though the samples are 

of Ordovician-age rocks that predate the time of higher 

plants, the source of vitrinite. Reflectance values for 

these samples follow the regression trend closely.

Cardott and Lambert (1985) analyzed samples of 

Woodford Shale (Upper Devonian and Lower 

Mississippian) from four wells near those used for this 

study, and their data are plotted in figure 2C. These data

are within the trend of the data from this study and agree 

well with them, particularly in the 7,000- to 15,000-ft 

depth range. The same holds for data from Schmoker 

(1986) (fig. 2B), mostly because Schmoker included the 

data of Cardott and Lambert. For shallowest depths, the 

data of Schmoker differ significantly from those of the 

other two studies, most likely because of sample 

heterogeneity.

DISCUSSION

The data in my study differ in fundamental ways 

from those of Cardott and Lambert (1985) and 

Schmoker (1986), even though we were working toward 

a similar end to use vitrinite reflectance data to predict 

thermal maturation in the Anadarko basin. For instance, 

Cardott and Lambert demonstrated the degree of 

thermal maturation of the Woodford Shale across a wide 

area of the basin, whereas Schmoker used vitrinite 

reflectance to model the evolution of the "oil window" in 

the basin. Schmoker (1986) noted that "***a substantial

Thermal Maturation of the Eastern Anadarko Basin, Oklahoma C5
difference exists between a set of analytical 

measurements and a predictive thermal maturity model 

by which one can project beyond available data***." The 

aim of my study, therefore, was to make some 

generalizations about the use of each of the paleogeothermal models to predict thermal maturation in any part 

of the basin.

The most significant reasons for differences in the 

three data sets are (1) the microscopist, (2) the source of 

the samples, core or cuttings, (3) the lithologies from 

which samples were collected, and (4) the areal 

distribution of the samples. Cardott and Lambert (1985) 

performed their own analyses, whereas Schmoker 

compiled data from several sources. The samples for the 

present study are from profiles of cuttings and core 

samples from wells along a north-south line that extends 

125 mi (200 km) from near the Kansas State line, or the 

shallow shelf area of the Anadarko basin, south to the 

deep part of the basin.

Although shales and other clastic lithologies can 

have a homogeneous organic content, they commonly 

contain several populations of organic material 

representing distinct levels of maturation. This diversity 

results from variations in the source and the material and 

from the recycling of material from previously deposited 

organic matter. It can cause large disparities in the mean 

reflectance value of a sample depending on the level of 

expertise of the microscopist and the calibration of the 

reflectance equipment.

Cardott and Lambert's study has several 

advantages: the samples are from one lithological unit, 

wide-spaced areally, and are from both the shallow and 

the deep part of the basin. These factors insure that the 

samples represent the various heating conditions 

purported to characterize the Anadarko basin. In 

contrast, Schmoker's data, which were collected from 

several studies by different workers (including Cardott 

and Lambert, 1985), are from widespread areas but

Table 3. Geothermal gradients for selected wells in study area

[Gradients were calculated from bottom-hole temperatures and corrected using the method of Harrison and others (1982).

Multiple gradient values are given where incremental bottom-hole measurements were taken during drilling]

Company

Amerada Petroleum Company 

Carter Oil Company and Oklahoma Nat. Gas 

Stanolind Oil and Gas 

Superior Oil Company

Midstates Oil Company

Cities Service Oil Company 

Exploration Oil and Gas

Cameo Oil and Trust

Deardorf Oil Company

Mazda Oil Company 

L.B. Jackson 

Superior Oil Company 

L. J. Horwitz

Olson Drilling Company 

Ashland Oil and Refining 

Ohio Oil Company

The Texas Company 

Sinclair Oil and Gas

Well name

Mack Silverhom No. 1 

L.L.HolsteadNo. 1 

J.W. Chappelear No. 1 

Cogdill33-18

Hennessey No. 1

Petree Ranch No. 1 

Ethel Hadlock No. 1

Parrington No. 1

Gungoll No. 1

Batman No. 1 

Manley No. 1 

Schultz 28-22 

Frech No. 1

W.W. Morris No. 1 

AlbrightNo. 1 

W.O.ParrNo. 1

C.L. Maxwell No. 1 

Hendrixson No. 1

Location 

(sec. T., R.)

24, 6 N., 13 W. 

16.7N., 14 W. 

8, 7 N., 15 W. 

18, 8 N., 11 W.

9,9N., 11 W.

18, UN., 8 W. 

30, 13 N., 9 W.

14, 15 N., 8 W.

11,20N.,8W.

13, 21 N., 11 W. 

36, 22 N., 10W. 

22, 23 N., 10W. 

8.24N., 11 W.

27, 25 N., 9 W. 

31,27N.,7W. 

9, 28 N., 10W.

18, 28 N., 12 W. 

17, 29 N., 8 W.

Gradient (°F)

Calc.

1.23 

1.07 

1.16 

1.05 

.88

1.35

.43 

1.01

1.00

1.02 

1.04 

.99

.95

1.23

1.05

.04 

1.06

.93 

.94

1.06 

1.10 

.95 

.82

1.06 

1.05 

1.18 

1.12

1.49 

1.57

Corrected

1.30 

1.39 

1.48 

1.38 

1.20

1.66

1.51 

1.33

1.32

1.35 

1.10 

1.30

1.29

1.55

1.34

1.37 

1.39

1.24 

1.26

1.37 

1.40 

1.27 

1.14

1.33 

1.31 

1.38 

1.38

1.75 

1.82

C6 Evolution of Sedimentary Basins Anadarko Basin
represent a minimum sampling density. In addition, the 

data were obtained from both core and cuttings samples 

from the deep and shallow parts of the basin.

Problems can occur if data from different tectonic 

provinces are combined to make a model of the heating 

of a basin. In the Anadarko basin, the heating events of 

the deep basin differ considerably from those of the 

shallow basin. The heating of the deep basin is believed 

to have occurred at two different times, during which the 

shelf area was relatively stable, and the basin has been 

cooling since Permian time (Garner and Turcotte, 1984). 

The shelf area was never buried deeply, and because 

high-heat events were confined to the greater depths, the 

thermal histories of the shelf and deep basin are 

completely different. Vitrinite reflectance data from two 

such environments cannot be combined to make a 

representative model for the basin. Geothermal 

gradients, as calculated from bottom-hole temperatures, 

are fairly consistent along the well profile (table 3) 

because of the stabilization through cooling of the 

gradients within the basin since Permian time, after the 

maximum reflectance (maturity) of the organic material 

was set by higher temperatures. Thus, higher 

temperatures from the deep basin modeling will overestimate temperatures predicted for the shallow part of 

the basin.

The vitrinite reflectance data for this study do not 

correlate with the temperatures derived from bottomhole temperature data using the relation of Barker and 

Pawlewicz (1987). The oil window generally is 

considered to fall within the range of from 50-65 °C 

(120-150 °F) to 130-145 °C (265-295 °F), corresponding 

to vitrinite reflectance of between about 0.6 and 1.3 

percent. In the well along the profile that has the largest 

depth range and best individual correlation (No. 51-11 

Weller), the highest reflectance values are significantly 

higher than the oil window. Although temperatures only 

approach the theoretical oil-window limits, the 

reflectance data are well above the limits, in the range of 

2.0 percent (table 2). The deeper part of the well 

probably was subjected to higher temperatures that have 

since decreased. This pattern can also be observed in the 

No. 1 Petree Ranch and No. 1 Carr wells.

The present-day geothermal gradient for the 

region of the well profile is about 1.3 °F/100 ft (24 °C/km) 

(Harrison and Luza, 1986), similar to the gradient of 1.2 

°F/100 ft used by Pusey (1973). Twenty-nine bottom-hole 

temperature data, from eighteen wells parallel with the 

well profile, are in partial agreement with this gradient if 

the temperature correction scheme of Harrison and 

others (1982) is applied to these data (table 3). The 

original calculated gradients are low, generally 1.0-1.2 

°F/100 ft, but if the correction is applied, the gradients 

are close to or exceed 1.3 °F/100 ft. There is no foolproof

way of correcting bottom-hole temperature data, 

however, because there is never the assurance that 

temperatures were collected under equilibrium 

conditions. Thus, the temperatures for table 2 were 

figured using a geothermal gradient of 1.3 °F/100 ft and 

a surface temperature of 60 °F (15 °C).

The data set from this study fared well when its 

correlation coefficient, 0.76, was compared with those for 

the other two data sets, 0.90 (Cardott and Lambert, 

1985) and 0.92 (Schmoker 1986). Although the 

correlation coefficient is not the definitive test of data, it 

conveys the information that internally the analyses are 

consistent and agree well. The correlation coefficient for 

this study of 0.76 is not bad; it indicates that the data have 

scatter but are still consistent and that a strong 

correlation between depth and reflectance is maintained.

BURIAL HISTORY

Burial history provides a useful way to view an 

idealized reconstruction of the depositional and tectonic 

history of an area. Three burial history curves (figs. 3-5) 

were constructed along the well profile (formation tops 

from Adkison, 1960). Figure 3, for the shallow shelf area 

of the basin, shows the relatively shallow subsidence for 

the shelf area during the middle Paleozoic, and figures 4 

and 5 illustrate the rapid subsidence during the late 

Paleozoic for the deeper part of the basin. On all three 

curves, the amount of subsidence from the Pennsylvanian 

to Tertiary and the amount of subsequent uplift are 

estimated.

It is widely held that a regression line drawn 

upward to intercept a vertical line drawn from 0.2 

percent Rm on a semilogarithmic plot will approximate 

the amount of sediment removed by erosion. 

Calculations based on a model of vitrinite reflectance 

from worldwide sources (Waples, 1980) suggest that 

about 3,900 ft (1.2 km) of sediments were removed 

basinwide, whereas calculations based on age spectra 

from microcline-bearing clasts (Harrison and others, 

1987) suggest that about 6,550 ft (2 km) of sediments 

were removed in the southwestern part of the basin. A 

calculation by Schmoker (1986) suggests that about 

2,600 ft (790 m) of erosion occurred, whereas the 

regression line shown in figure 2 indicates 3,200 ft (975 

m) of erosion.

I believe that reflectance data from two areas as 

diverse as a continuously subsiding deep basin and a 

stable shelf cannot be combined to make an average 

value to estimate the amount of erosion. To illustrate, the 

reflectance data from three groups of three wells each 

along the the well profile, representing the shallow, 

intermediate and deep basin, were analyzed using 

reduced major axis regression. The No. 1 Atchison, No. 1

Thermal Maturation of the Eastern Anadarko Basin, Oklahoma C7
0

I,000 

2,000 

3,000 

4,000 

5,000 

6,000 

7,000 

8,000 

9,000 

10,000

II,000

Woodford Shale 

Sylvan Shale 

Viola Limestone'0' 

Simpson -^

Permian

Pennsylvanian

Chesterian

Meramecian

Osagean

Kinderhookian

500 400 300 200 100

TIME, IN Ma

Figure 3. Burial history reconstruction for the No. 1 Atchison well at the northern end of the well profile. The burial 

history from the Pennsylvanian to the present is estimated. Location information for well given in table 1. Formation 

tops from Adkison and Sheldon (1963).

Milacek, and No. 1 Campbell make up the shallow group 

of wells; the No. 1 Hadlock, No. 1 Petree Ranch, and No. 

1 Cherry the intermediate group; and the No. 51-11 

Weller, No. 1 Sprague, and No. 1 Carr the deep group. 

Results of regression analysis of the first two groups were 

poor because of data scatter, and a 0.2-percent 

reflectance intercept line through the two data groups 

was inconclusive. Results of regression analysis of the 

third group were good (r = 0.81) and suggest about 8,000 

ft (2.5 km) of erosion. This amount is hardly applicable to 

the thin shelf area because it is equal to or greater than 

the total sediment thickness in the areas of the first two 

groups. An average value would be similarly useless. 

Data collected in the method of Schmoker that is, from 

a limited sample set from widely spaced locales are also 

not amenable to such calculations. In contrast, the 

equations of Cardott and Lambert would be valid for an 

estimation of thermal maturity, at least for the Woodford 

Shale, because of the internal consistency of both the 

sampling and the analyses. I believe that an estimation of 

the amount of erosion cannot be approached from a 

regional basis without a vast amount of data but, rather, 

must be approached on a local basis, using several (2-10, 

depending on the area size) well profiles from locales 

having a similar tectonic history.

Reflectance and Temperature

Maturation of organic material is widely believed 

to be a function of time and temperature (Lopatin, 1971; 

Waples, 1980). The evaluation of the thermal history of 

the Anadarko basin by Schmoker (1986) used the work 

of Lopatin (1971), which suggests that both time and 

temperature have an affect on the maturation of the 

organic material. If this assumption is true, then almost 

the entire Permian section should be within the oil 

window if the temperature and time since the Paleozoic 

are considered.

In contrast, Barker and Pawlewicz (1986b) showed 

that time has much less of an effect on the rank of organic 

material than indicated by Lopatin (1971). Isoreflectance 

lines and formation boundaries along the line of the well 

profile are shown in figure 6. The isoreflectance lines 

were drawn from points connecting depths calculated for 

several wells (wells 2,5, 7, and 10 of Adkison, table 1) by 

using the reduced major axis regression method. That the 

isoreflectance lines cross formation boundaries at an 

angle is evidence for maturation being a function of 

increased temperatures resulting from burial or renewed 

heating after subsidence stopped. Maturation probably 

was occurring during deformation but at a slower rate.

C8 Evolution of Sedimentary Basins Anadarko Basin
0

I.000 

2,000 

3,000 

4,000 

5,000 

6,000 

H 7,000

LU 

LU

2 8,000

l~

t 9,000

LU

Q

10,000

II,000 

12,000 

13,000 

14,000

15,000

TIME. IN Ma

Atokan

400 300 200 

TIME, IN Ma

100

Figure 4. Burial history reconstruction for the No. 1 Petree Ranch well near the middle of well 

profile. The burial history from the Pennsylvanian to the present is estimated. Location information 

for well given in table 1. Formation tops from Adkison and Sheldon (1963).

CONCLUSIONS

1. Internal consistency in both sample collection 

and analysis and sufficient samples are required to 

adequately represent the area under investigation. A 

single microscopist (for the purpose of vitrinite 

reflectance) and samples from a single lithology will 

usually improve the data and allow more accurate 

prediction of thermal maturity.

2. Rank measurements show that along the 

eastern side of the Anadarko basin on the shelf the 

maturation of sediments resulted primarily from depth of 

burial; however, south of the shelf area in the deeper part 

of the basin, sediments were affected by an early highheat event.

3. Reflectance values computed using the presentday geothermal gradient are at least 50-70 percent 

higher than expected relative to the generally accepted oil 

window values. Temperatures most likely were higher in 

the early Paleozoic and then decreased.

4. Isoreflectance lines show the depth to the limits 

of the oil window and can be used to predict occurrences 

of hydrocarbons.

5. Amounts of erosion cannot be predicted by 

combining data from two tectonic provinces as radically 

different as the shelf and deep basin areas in the Anadarko basin.

Thermal Maturation of the Eastern Anadarko Basin, Oklahoma C9
2.000

4.000

6.000

10.000

12,000

14,000

16,000

18.000

20.000

400 300 200 

TIME. IN Ma

100

Figures. Burial history reconstruction for the No. 51-11 Wellerwell near the southern end of the 

well profile. The burial history from the Pennsylvanian to the present is estimated. Location 

information for well given in table 1. Formation tops from Adkison and Sheldon (1963).

C10 Evolution of Sedimentary Basins Anadarko Basin
SOUTH A'

17 16 15 14 13 12 11 10

NORTH

A

3 2 1

500

1,000

1,500

CO

tr.

LU

2,000

2 2,500

LU

Q

3,000

3,500

4,000

4,500

Permian

10 20 MILES

10 20 KILOMETERS

SEA LEVEL

1,000

2,000

3,000

4,000

5,000

6,000

7,000 tLU 

LL

8,000 

I

0. 

LLJ 9,000 Q

10,000

11,000

12,000

13,000

14,000

15,000

Figure 6. Cross section along well profile showing isoreflectance lines (heavy) at 0.6 and 1.3 percent Rm. 

I so reflectance lines were drawn on points calculated by reduced major axis regression for several wells along 

profile (wells 2,5, 7, and 10of Adkison; table 1). See text for explanation. Numbers along top correspond to wells 

of Adkison listed in table 1. Wavy line indicates unconformity; long-dashed line indicates boundary uncertain.

Thermal Maturation of the Eastern Anadarko Basin, Oklahoma C11
REFERENCES CITED

Adkison, W.L., 1960, Subsurface cross section of Paleozoic 

rocks from Barber County, Kansas, to Caddo County, 

Oklahoma: U.S. Geological Survey Oil and Gas 

Investigations Chart OC-61, 2 sheets.

Adkison, W.L., and Sheldon, M.G., 1963, Sample descriptions 

and correlations for wells on a cross section from Barber 

County, Kansas, to Caddo County, Oklahoma: 

Oklahoma Geological Survey Guide Book 13, 139 p.

Adler, F.J., 1971, Anadarko Basin and central Oklahoma area, 

in Future petroleum provinces of the United States 

Their geology and potential: American Association of 

Petroleum Geologists Memoir 15, p. 1061-1069.

Barker, C.E., and Pawlewicz, M.J., 1986a, Concentration of 

dispersed sedimentary organic matter for vitrinite 

reflectance analysis using a simple crush and float 

method: Society for Organic Petrology Newsletter, v. 3, 

no. 3, p. 3.

____ 1986b, The correlation of vitrinite reflectance with 

maximum temperature in humic organic matter, in Buntebarth, G., and Stegena, L., eds., Paleogeothermics; 

Lecture notes in earth sciences, v. 5: Berlin, SpringerVerlag, p. 79-93.

Baskin, D.K., 1979, A method of preparing phytoclasts for 

vitrinite reflectance analysis: Journal of Sedimentary 

Petrology, v. 49, p. 633-635.

Cardott, B.J., and Lambert, M.W., 1985, Thermal maturation 

by vitrinite reflectance of Woodford Shale, Anadarko 

basin, Oklahoma: American Association of Petroleum 

Geologists Bulletin., v. 69, no. 11, p. 1982-1998.

Evans, J.L., 1979, Major structural and stratigraphic features of 

the Anadarko Basin, in Hyne, NJ., ed., Pennsylvanian 

sandstones of the mid continent: Tulsa Geological 

Society Special Paper 1, p. 97-114.

Garner, D.L., and Turcotte, D.L., 1984, The thermal and 

mechanical evolution of the Anadarko Basin: Tectonophysics, v. 107, p. 1-24.

Harrison, T.M., Heizler, M.T., and Burke, K., 1987, Aspects of 

thermal evolution of Anadarko Basin, Oklahoma:

American Association of Petroleum Geologists Bulletin, 

Abstracts with Program, v. 71, no. 5, p. 565.

Harrison, W.E., and Luza, K.V., 1986, Temperature gradient 

information for several boreholes drilled in Oklahoma: 

Oklahoma Geological Survey Special Publication 86-2, 

42 p.

Harrison, W.E., Luza, K.V., Prater, M.L., and Cheung, P.K., 

1982, Geothermal resource assessment in Oklahoma, in 

Ruscetta, C.A., ed., Geothermal direct heat program 

roundup technical conference proceedings, v. 1: Salt 

Lake City, University of Utah Earth Science Laboratory, 

p. 187-204.

Hoffman, P., Dewey, J.F., and Burke, K., 1974, Aulacogens and 

genetic relation to geosynclines with a Proterozoic 

example from Great Slave Lake, Canada, in Dott, R.H., 

Jr., and Shower, R.H., eds., Modern and ancient geosynclinal sedimentation: Society of Economic 

Paleontologists and Mineralogists Special Publication 19, 

p. 38-55.

Huffman, G.G., 1959, Pre-Desmoinesian isopachous and paleogeologic studies in central and mid-continent region: 

American Association of Petroleum Geologists Bulletin, 

v. 43, no. 11, p. 2541-2575.

Lopatin, N.V., 1971, Temperature and geologic time as factors 

in coalification: Akademiya Nauk SSSR Izvestiya Seriya 

Geologicheskaya, no. 3, p. 95-106.

Pusey, W.C., 1973, The ESR-kerogen method; a new technique 

of estimating maturity of sedimentary rocks: Petroleum 

Times, January 12, 1973, p. 21-25.

Schmoker, J.W., 1986, Oil generation in the Anadarko Basin, 

Oklahoma and Texas; modeling using Lopatin's method: 

Oklahoma Geological Survey Special Publication 86-3, 

40 p.

Till, R., 1974, Statistical methods for earth scientists; an 

introduction: London, Macmillan Press, 154 p.

Waples, D.W., 1980, Time and temperature in petroleum 

formation; application of Lopatin's method in petroleum 

exploration: American Association of Petroleum 

Geologists Bulletin, v. 64, no. 6, p. 916-926.

Webster, R.E., 1980, Evolution of the southern Oklahoma 

aulacogen: Oil and Gas Journal, v. 78, no. 7, p. 150-172.

*U.SGPO:1990 773-047/06032

C12 Evolution of Sedimentary Basins Anadarko Basin
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