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Chapter B

Statistical Analysis of Compositional Data 

from Desmoinesian Sandstones in Oklahoma

By THADDEUS S. DYMAN

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

Denver, CO 80225

Library of Congress Cataloging-in-Publication Data

Dyman, T. S.

Statistical analysis of compositional data from Desmoinesian sandstones in 

Oklahoma / by Thaddeus S. Dyman.

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

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

"A multidisciplinary approach to research studies of sedimentary rocks and 

their constituents and the evolution of sedimentary basins, both ancient and 

modern." 

Bibliography: p.

Supt. of Docs, no.: I 19.3: 1866-B

1. Sandstone Oklahoma Composition. 2. Petrology Statistical 

methods. I. Title. II. Series. III. Series: U.S. Geological Survey bulletin ; 

1866-B.

QE75.B9 no. 1866-B 

[QE471.15.S25] 

557.3 s-dc20

[5521.5] 89-600158

CIP
CONTENTS

Abstract Bl 

Introduction Bl 

Regional geology B2 

Regional stratigraphy and sedimentology B3 

Method of study B4

Statistical analysis of compositional data B4 

R-mode analysis B5 

Q-mode analysis B6

Petrofacies I B6

Petrofacies II B6

Petrofacies III B7

Petrofacies IV B8 

Factor-score maps B8 

Paleogeographic implications BIO 

Summary Bll 

References cited B12

FIGURES

1. Map showing major structural features of Oklahoma during Pennsylvanian 

time B2

2. Chart showing generalized stratigraphy for Desmoinesian sandstones, 

Arkoma basin and northern Oklahoma platform B3

3. Map showing sample localities for this study B4

4. Weighted pair-group average dendrogram of framework grains for

Desmoinesian sandstones B7 

5-9. Photographs showing:

5. Petrofacies I sandstone, sample 24-1 B8

6. Petrofacies II sandstone, sample 13-2 B8

7. Petrofacies III sandstone, sample 17-1 B8

8. Petrofacies IV sandstone, sample 81-1 B9

9. Petrofacies IV sandstone, sample 91-1 B9 

10-12. Correspondence analysis factor-score maps for:

10. Factors 1 and 2 B9

11. Factors 3 and 4 BIO

12. Factors 2 and 4 BIO

13. Plot showing total quartz-total feldspar-total lithics compositions of 

Desmoinesian sandstones in study Bll

TABLES

1. Absolute variable-factor contribution matrix (first four factors) and cumulative 

percent contribution for ten original framework grain variables B6

2. Petrofacies summary for Desmoinesian sandstones in this study B7

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

Statistical Analysis of Compositional Data from 

Desmoinesian Sandstones in Oklahoma

ByThaddeus S. Dyman

Abstract

Desmoinesian sandstones from the northern Oklahoma 

platform and the Anadarko, Arkoma, and Ardmore basins 

record a complex interaction between mid-Pennsylvanian 

source-area tectonism and cyclic sedimentation patterns 

associated with numerous transgressions and regressions. 

Framework-grain summaries for 50 thin sections from 

sandstones of the Krebs, Cabaniss, and Marmaton Groups 

and their surface and subsurface equivalents were subjected 

to multivariate statistical analyses to establish regional 

compositional trends for provenance analysis.

R-mode cluster and correspondence analyses were 

used to determine the contributing effect (total variance) of 

key framework grains. Fragments of monocrystalline and 

polycrystalline quartz, potassium and plagioclase feldspar, 

chert, and metamorphic, limestone and mudstonesandstone rock fragments contribute most to the variation in 

the grain population. Q-mode cluster and correspondence 

analyses were used to identify four petrofacies and establish 

the range of compositional variation in Desmoinesian 

sandstones. Petrofacies I is rich in monocrystalline quartz 

(78-98 percent); mica and rock fragments are rare. Petrofacies II is also rich in monocrystalline quartz (60-84 percent) 

and averages 12 percent total rock fragments. Petrofacies III 

and IV are compositionally heterogeneous and contain 

variable amounts of monocrystalline and polycrystalline 

quartz, potassium feldspar, mica and chert, and metamorphic and sedimentary rock fragments.

Quantitative analyses indicate that Desmoinesian 

sandstones were derived from sedimentary, igneous, and 

metamorphic source areas. Petrofacies I and II sandstones 

occur predominantly in the lower Desmoinesian and are 

widely distributed, although they are most abundant in 

eastern and central Oklahoma; sandstones from petrofacies 

III and IV are widely distributed and occur primarily in the 

middle and upper Desmoinesian. The range of

Manuscript approved for publication, April 11, 1989.

compositional variation and the distribution of petrofacies are 

related to paleotectonics and basin development, sediment 

recycling, and varying depositional environments.

INTRODUCTION

The present-day geologic framework of Oklahoma 

and the entire southern midcontinent region is related 

directly to Pennsylvanian paleotectonic development (fig. 

1). Source-area variability and multiple marine 

transgressions and regressions have resulted in abrupt 

facies changes and complex depositional cycles. Many 

published studies have reconstructed Pennsylvanian 

paleogeography by using stratigraphic and sedimentologic data within these depositional cycles, but detailed 

petrologic studies are rare. Published compositional data 

for sandstones are generally limited to field or core rock 

descriptions and are not detailed enough for provenance 

studies. Quantitative analysis of existing data is difficult.

Desmoinesian sandstones in Oklahoma record a 

complex interaction between source-area tectonism, 

regional transgression, and sediment recycling. These 

sandstones are readily identifiable in both outcrop and 

core and exhibit much compositional heterogeneity. 

Studies to better understand compositional variations in 

these sandstones may aid in paleogeographic 

reconstruction and stratigraphic correlation, especially 

where nomenclature is confusing. These studies may be 

valuable because of the significant oil and gas potential of 

Desmoinesian strata in Oklahoma.

A quantitative petrographic analysis of Desmoinesian sandstones was conducted in order to: (1) define 

sandstone petrofacies for regional correlation and 

determine which framework grains contribute the most 

to variations in sandstone composition; (2) describe 

lateral and vertical variations in source area in order to 

add to the sedimentary-tectonic framework for the

Statistical Analysis of Compositional Data, Desmoinesian Sandstones, Oklahoma B1
EXPLANATION 

Anticline 

Syncline

Thrust fault teeth on 

upper plate

Figure 1. Major structural features of Oklahoma during Pennsylvanian time. OKC, Oklahoma City; AR, Ardmore; BRT, 

Bartlesville. Data from Jordan (1961), Branson (1961), Johnson (1971), Frezon and Dixon (1975), and Krumme (1981).

Desmoinesian in the region; and (3) determine the 

usefulness of statistical analyses in petrographic studies. 

The most important goal of this study was to simply 

define the range of compositional variation in 

sandstones. The petrographic database exhibits much 

variation, and because variations in the sample 

population were difficult to define subjectively, a 

statistical approach was undertaken.

This study is preliminary and is intended to 

establish a base for future quantitative petrographic 

studies. The compositional range of Desmoinesian 

sandstones may be expanded in the future as more 

sandstones are analyzed. Additional sandstones must be 

compositionally and sedimentologically analyzed before 

a thorough understanding of Pennsylvanian paleogeography is attained. Any final provenance determination 

should be based on stratigraphic, sedimentologic, and 

petrologic data.

Core samples were obtained from the Oklahoma 

Geological Survey Core and Sample Library. This report 

was prepared for the U.S. Geological Survey Evolution of 

Sedimentary Basins Program.

REGIONAL GEOLOGY

The geography of Oklahoma and the surrounding 

region during the Pennsylvanian was strongly affected by 

the Ouachita orogeny, the result of a collision of North 

America with South America and Africa (Kluth and 

Coney, 1981). Regional structural elements active during 

the Pennsylvanian are shown in figure 1. The AmarilloWichita-Criner uplift was a prominent structural feature

throughout most of the Pennsylvanian and extended for 

more than 300 mi from the Texas Panhandle 

southeastward into southern Oklahoma. The Muenster 

arch is a southern extension of the Wichita-Criner trend 

but is separated from the Criner uplift by the Marietta 

basin (Frezon and Dixon, 1975). The Cimarron uplift 

and Keyes dome form a northward extension of the 

Amarillo uplift in the Oklahoma Panhandle.

The Nemaha uplift is a prominent subsurface 

structural feature that trends from south of Oklahoma 

City northward for more than 400 mi into Nebraska 

(Luza, 1978). The axis of this feature represents the 

highest part of a more extensive Early Pennsylvanian 

positive area often referred to as the Nemaha highlands.

The Anadarko basin is bordered by the Nemaha 

uplift to the northeast, the central Kansas shelf to the 

north, and the Amarillo-Wichita-Criner trend to the 

south. It is one of the deepest cratonic basins in North 

America and contains more than 40,000 ft of Cambrian 

through Permian sedimentary rocks along its southern 

margin. More than 20,000 ft of stratigraphic separation 

exists along the Wichita megashear in southwestern 

Oklahoma (Evans, 1979).

During Desmoinesian time, the southern part of 

the Ouachita geosyncline in southeastern Oklahoma was 

uplifted by thrusting and folding and a prominent positive 

feature known as the Ouachita uplift developed. The 

northern part of the geosyncline and a shelf region to the 

north retained a basinal configuration and are together 

referred to as the Arkoma basin (Branson, 1961). The 

Arbuckle and Paul's Valley uplifts were positive 

elements in south-central Oklahoma during Desmoinesian and Missourian time. The Ardmore basin contains

B2 Evolution of Sedimentary Basins Anadarko Basin
almost 20,000 ft of Upper Mississippian and 

Pennsylvania!! strata and is separated from the Anadarko 

basin by local uplifts (Jacobson, 1959).

The Ozark uplift in northeastern Oklahoma and 

Missouri is an earlier Paleozoic structural feature that 

was rejuvenated during the mid-Pennsylvanian at 

approximately the same time as the Ouachita uplift 

(Branson, 1961; Frezon and Dixon, 1975).

REGIONAL STRATIGRAPHY AND 

SEDIMENTOLOGY

Stratigraphic names for outcrop and core samples 

of sandstones are from published reports and summaries 

prepared by well-site geologists. Stratigraphic 

nomenclature in Oklahoma is confusing in part because 

of facies differences between platform and basin and in 

part by historic differences in surface and subsurface 

nomenclature (Krumme, 1981). Figure 2 illustrates 

Desmoinesian sandstone nomenclature for the State 

compiled from Jordan (1957), Tomlinson and McBee 

(1959), Branson (1961), Frezon and Dixon (1975), 

Ebanks (1979), Krumme (1981), and Sutherland (1982). 

Limestone and shale units not addressed in this report 

have been omitted from the figure. Informal subsurface 

Stratigraphic names have also been omitted from figure 2 

because of the uncertainty of precisely correlating them 

with surface units.

Desmoinesian formations are divided into three 

groups, from oldest to youngest, the Krebs, Cabaniss, 

and Marmaton (Krumme, 1981). These groups and their 

Stratigraphic equivalents are bounded by unconformities 

and are found throughout Oklahoma. In the Ardmore 

and eastern Anadarko basins, equivalent strata are 

included in the Deese Formation. In western Oklahoma, 

the Krebs and Cabaniss Groups are informally referred 

to as the Cherokee Group or are left as undivided 

Desmoinesian strata (Frezon and Dixon, 1975). The 

term Cherokee Group is generally not accepted in 

Oklahoma (Ebanks, 1979).

The oldest Desmoinesian formation in central and 

eastern Oklahoma, the Hartshorne Sandstone, rests 

unconformably on older Atokan or pre-Pennsylvanian 

strata. The overlying McAlester Formation is 

predominantly shale but contains one regionally 

persistent sandstone referred to as the Warner Sandstone 

Member and its informal subsurface equivalent the 

Booch sandstone. The Savanna Formation unconformably overlies the McAlester Formation in the 

Arkoma basin and contains many discontinuous 

sandstone and coal beds. The base of the overlying Boggy 

Formation is drawn at the base of the Bluejacket 

Sandstone Member and its informal subsurface 

equivalent, the Bartlesville sandstone (Branson, 1961). 

Informal subsurface sandstone equivalents of the upper

LLJ

DC 

LLJ

FORMATION AND MEMBER

Upper Marmaton Group sandstones 

Labette Shale 

Calvin Sandstone

Senora Formation

Chelsea Sandstone Member

Thurman Sandstone

Boggy Formation

Taft Sandstone Member 

Bluejacket Sandstone Member

Savanna Formation sandstones 

McAlester Formation

Warner Sandstone Member

Hartshorne Sandstone

Figure 2. Generalized stratigraphy for Desmoinesian 

sandstones, Arkoma basin and northern Oklahoma platform. 

Informal subsurface names have been omitted from the chart 

because of the discontinuous nature of Pennsylvanian 

sandstones and the difficulty of correlating surface with 

subsurface units. Chart is incomplete because only stratigraphic names addressed in this report are included. Deese 

Formation of south-central Oklahoma includes strata 

equivalent to the three groups identified here. Data from 

Jordan (1957), Tomlinson and McBee (1959), Branson 

(1961), Frezon and Dixon (1975), Ebanks (1979), Krumme 

(1981), and Sutherland (1982).

part of the Boggy (Taft Sandstone Member) include the 

Red Fork and Burbank sandstones.

The Thurman Sandstone unconformably overlies 

shales in the upper Boggy in southern Oklahoma but is 

absent on the northern Oklahoma platform. The 

overlying Senora Formation is laterally persistent but 

lithologically variable. The Chelsea Sandstone Member 

is locally present in eastern Oklahoma. The Skinner 

sandstone is an informal subsurface equivalent of the 

Senora Formation (Krumme, 1981).

The upper Desmoinesian Marmaton Group is 

composed primarily of shale, sandstone, and limestone. 

In the Arkoma basin, the Calvin Sandstone forms the 

base of the group but is replaced by the Fort Scott 

Limestone on the northern Oklahoma platform. The 

informal Prue sandstone may represent a lateral shelf 

equivalent of the Calvin. The overlying Peru sandstone is 

part of the Labette Shale (Krumme, 1981). Sandstones in 

the upper Marmaton Group, such as the informal 

Cleveland sandstone, are interbedded with shale and are 

often discontinuous.

Statistical Analysis of Compositional Data, Desmoinesian Sandstones, Oklahoma B3
Sedimentologically, Desmoinesian sandstones 

were deposited in fluvial, deltaic, and marine 

depositional environments associated with the Early 

Pennsylvanian northward transgression. During the early 

Desmoinesian, fluvial, deltaic, and shallow-marine 

depositional environments dominated the northern 

Oklahoma shelf, whereas deeper water marine 

environments dominated the southern Anadarko and 

Ardmore basins. With a presumed southward shift in 

provenance (Krumme, 1981), marine carbonate shelf 

sedimentation dominated northern Oklahoma during the 

late Desmoinesian. Coarse-grained alluvial sediments 

were deposited along the margins of uplifts. Paleoenvironments may vary from these regional trends because of 

local source-area influence and sea level changes. Most 

of the sandstones analyzed in this report were deposited 

in deltaic and shallow-marine environments. 

Compositional variations are considered to be due 

primarily to different source areas; however, 

compositional modification due to changing depositional 

environments cannot be totally discounted until a 

thorough provenance study has been completed.

METHOD OF STUDY

The study includes core and outcrop samples on 

the northern Oklahoma platform, both east and west of 

the Nemaha uplift, and in the Anadarko, Arkoma, and 

Ardmore basins in both western and southeastern 

Oklahoma (figs. 1, 3). Fifty medium-grained sandstone 

samples were cut, thin sectioned, stained for potassium 

feldspar, and point counted. More than 300 grains were

counted per slide. Quartz grains were examined for 

extinction patterns, inclusions, and overgrowths (Folk, 

1968). Accessory minerals such as micas, hornblende, 

garnet, and zircon were identified as either present or 

absent. Compositional variations due to differential 

weathering of surface versus subsurface samples were 

not addressed in the statistical analysis. These variations 

are considered minor in this population of sandstones.

Sample location and composition data for all 

samples in this study are given in Dyman (1987). Data 

were aggregated according to methods presented in 

Dickinson and Suczek (1979).

STATISTICAL ANALYSIS OF 

COMPOSITIONAL DATA

The following statistical procedure was used in this 

study. (1) R-mode correspondence analysis was used to 

determine the contributing effect (percentage of total 

variance) of each framework grain type (variable). Based 

on their contributing effect, variables were then 

aggregated into genetic groups. (2) Q-mode cluster 

analysis and correspondence analysis were then used to 

determine sample relationships and the range of 

compositional variation. Samples were aggregated into 

petrofacies groups to analyze stratigraphic and 

geographic variations in sandstone composition.

Correspondence analysis is a form of factor 

analysis that combines the results of both Q- and R-mode 

studies and reduces variable scaling problems. It reduces 

the problem of N-dimensional space (many variables) by 

projecting combinations of original variables on a new set

37 .103

95°

1 

1 13-2

20-2 "'&

^06-2 V'2

42-2

®

33 

TO

H46-t 

40

1

A30 '

35 MILES

EXPLANATION 

Outer symbols

A Petrofacies I 

D Petrofacies II 

O Petrofacies III 

O Petrofacies IV

Inner symbols

X Lower Krebs Group (basal Desmoinesian) 

 Upper Krebs and Cabaniss Groups (mid Desmoinesian) 

O Marmaton Group (upper Desmoinesian)

Figure 3. Sample localities for this study. Detailed geographic and compositional data for all samples given in Dyman 

(1987).

B4 Evolution of Sedimentary Basins Anadarko Basin
of axes (eigenvectors) that define new hypothetical 

variables called factors (David and others, 1977). 

Variable contribution on the new set of axes is based on 

variance. Data standardization to reduce problems 

induced by varying magnitude is not required. Data are 

transformed into conditional probabilities by dividing 

each data element by the sum of all elements.

Output from correspondence analysis includes: (1) 

relative and absolute factor-variable contribution 

matrices that define the relative or absolute contribution 

of each original variable (as a percent) to each new factor 

(that is, which variables are important in distinguishing 

all samples together); (2) a factor-score data matrix that 

contains factor-score loadings (that is, which variables 

are important in distinguishing each sample from other 

samples); and (3) factor-score maps (plots) created from 

the factor-score matrix that graphically display sample 

similarity in factor space. Lines are drawn on each plot to 

illustrate how each numbered variable contributes to 

differences among samples. The lines pass through a 

portion of factor space defined by their R-mode loadings. 

The lines represent the strength and direction according 

to which the different variables affect the sample 

population (David and others, 1974). The lines intersect 

at a point representing the average composition of the 

sandstones. The proximity of a group of sample points 

near a variable line (or lines) illustrates the similarity of 

samples and the variable (or variables) responsible for 

the similarity. Closely spaced sample points on one 

factor-score plot (for example, a plot of factors 1 and 2) 

may not occur together on a plot of different factors (for 

example, factors 3 and 4) because of the difference in 

variable contribution to different factors.

Cluster analysis is a multivariate classification 

method by which relatively homogeneous groups are 

defined by assigning samples to a group based on their 

similarity. A dendrogram defining all of the groups is 

created by the computer program (Davis, 1973,1986). In 

hierarchical clustering, the most similar samples are 

joined in a cluster that then successively joins with other 

clusters until all samples are included in the dendrogram. 

Modal analyses for Desmoinesian sandstones were first 

standardized by using the variable-mean deviation to 

insure that each variable was weighted equally.

The weighted pair-group clustering program of 

Davis was used with the r-correlation coefficient in this 

study. Cluster dendrograms produced with distance 

coefficients may include well-defined cluster groups even 

if some samples are very dissimilar from other samples. 

In this study, cluster dendrograms were generated 

separately with distance and r-correlation coefficients 

and provided similar results.

In the weighted pair-group cluster method, 

correlation matrices of samples are calculated and 

samples having high correlations are extracted. In

subsequent steps, similarity matrices are recomputed; 

clustered elements are treated as a single element. Each 

new cluster member is given equal weight with the 

existing cluster. Thus, late cluster arrivals carry more 

weight than do earlier arrivals.

Several alternative clustering methods are 

available (Davis, 1986), and determining the best 

clustering method may depend on the specific data set. 

Davis (1986) suggested that the weighted pair-group 

method provides the best results but that researchers 

should compare different methods. In this study, the 

results from cluster analysis were corroborated using 

correspondence analysis.

R-Mode Analysis

Table 1 shows the absolute variable-factor 

contribution matrix for the 10 framework grain types 

analyzed in this study. Sandstone, siltstone, and mudstone grains (mudstone-sandstone in table 1) were 

combined for the statistical analysis. Dark-gray to brown, 

siliceous and calcareous mudstone and shale are the 

most abundant of these grain types. In some cases, it was 

difficult to differentiate between weakly foliated metamorphic grains and shale grains. Together, the first four 

factors contribute 85 percent to the variation in the total 

sample of framework grains. The most important 

variables are for factor 1, potassium feldspar (92 

percent); for factor 2, monocrystalline quartz (22 

percent), limestone grains (19 percent), polycrystalline 

quartz (16 percent), metamorphic rock grains (15 

percent), plagioclase (11 percent), and chert (10 

percent); for factor 3, limestone grains (76 percent); and 

for factor 4, metamorphic rock grains (43 percent), 

mudstone-sandstone grains (29 percent), and chert (18 

percent). Volcanic and mica grains contribute less to the 

total variation in the sample population than do the other 

variables.

Factor 1 is controlled primarily by the high loading 

for potassium feldspar due to the two samples from the 

Cherokee Group in the Oklahoma Panhandle (samples 

53-1 and 81-1). The high loading for limestone in factor 

3 is due to limestone-rich samples from northern and 

southern Oklahoma (samples 91-1 and 20-2). Samples 

rich in variables with high loadings for factor 2 are widely 

distributed in Oklahoma in part because of the many 

grain types contributing to factor 2. Factors 3 and 4 are 

controlled primarily by chert and lithic grains from 

middle and upper Desmoinesian samples.

When the correspondence analysis was rerun 

without the potassium feldspar- and limestone-rich 

samples, cumulative variation was distributed 

proportionally according to the relative importance of the 

remaining variables. Monocrystalline and polycrystalline 

quartz, mudstone-sandstone, and metamorphic grains 

contributed more to each factor.

Statistical Analysis of Compositional Data, Desmoinesian Sandstones, Oklahoma B5
Table 1 . Absolute variable-factor contribution matrix (first four factors) and cumulative percent contribution 

for ten original framework grain variables

Grain type

Monocrystalline quartz

Polycrystalline quartz

Chert

Plagioclase

Potassium feldspar

Muds tone-sandstone

Limestone

Volcanic

Metamorphic

Mica

Cumulative percent contribution

1

1.2

.8

.1

2.9

92.0

.2

.7

.1

1.7

.2

41

2

22.4

16.4

10.4

10.8

.3

4.2

19.1

.2

15.0

.9

60

Factor 

3

2.9

2.3

1.5

1.6

.6

7.9

76.1

.1

5.0

1.6

77

4

0.1

2.0

17.6

.1

1.2

28.8

.4

4.9

42.8

2.1

85

Quartz, chert, potassium and plagioclase feldspar, 

and limestone, mudstone-sandstone, and metamorphic 

grains contribute the most to variation in this population 

of Desmoinesian sandstones.

Q-Mode Analysis

Four petrofacies groups were identified for 50 

sandstone samples by using cluster analysis. Figure 4 

illustrates the weighted pair-group dendrogram and 

petrofacies groups using all 10 original framework 

variables. Petrofacies subdivision based on clustering 

procedures is somewhat arbitrary, especially if cluster 

groups join at low levels of similarity. Additional cluster 

groups can be defined depending on the level of 

compositional similarity we wish to establish in the 

sample population. Table 2 summarizes the characteristics of each petrofacies defined in this study. 

Petrofacies differences are based on compositional 

variations in framework grains. Quartz extinction 

patterns and the presence or absence of accessory 

minerals do not significantly vary between samples and 

were not used to differentiate sandstones.

The geographic distribution of petrofacies for 

lower, middle, and upper Desmoinesian sandstones is 

presented in figure 3. For the purpose of this study, lower 

Desmoinesian includes only the lower part of the Krebs 

(Hartshorne Sandstone and the Warner Sandstone 

Member of the McAlester Formation; middle 

Desmoinesian includes the upper part of the Krebs 

(Savanna and Boggy sandstones) and Cabaniss Groups; 

and upper Desmoinesian includes sandstones in the 

Marmaton Group. This subdivision is arbitrary and is 

meant only to address gross compositional variations in 

Desmoinesian strata. The subdivision also alleviates 

some of the correlation problems introduced when 

comparing informal subsurface with surface 

nomenclature. Future studies including more samples 

could define additional or different stratigraphic groups.

Petrofacies I

Petrofacies I is subdivided into two petrofacies 

subgroups and is rich in monocrystalline quartz (mean 84 

percent) (fig. 5). Subgroup A contains an average of 88 

percent monocrystalline quartz, whereas subgroup B 

contains 80 percent. Polycrystalline quartz averages only 

5 percent for petrofacies I. Lithic grains are rare or 

absent in subgroup A and reach a maximum value of 14 

percent for subgroup B (sample 11-2, Red Fork 

sandstone, northern Oklahoma; fig. 3). Metamorphic 

grains are more abundant than sedimentary grains for 

both subgroups but are most abundant in subgroup B. 

Feldspar is rare or absent in both subgroups.

Petrofacies I is widely distributed throughout the 

study area especially along a north-trending belt in part 

coinciding with the axis of the Nemaha uplift. Stratigraphically, all three groups of Desmoinesian age are 

represented in petrofacies I, but most samples are from 

the lower and middle Desmoinesian. No relationship 

appears to exist between stratigraphic group assignment 

and geographic distribution. Both upper Desmoinesian 

petrofacies I samples (sample 5, Senora Formation, and 

sample 41-2, Prue sandstone; fig. 3) are in subgroup A 

and contain an average of more than 90 percent total 

quartz.

Petrofacies II

Petrofacies II contains less monocrystalline quartz 

(mean 75 percent) and more chert (mean 8 percent) and 

polycrystalline quartz (mean, 10 percent) than petrofacies I (fig. 6). It is more compositionally heterogeneous 

than petrofacies I and averages 12 percent total lithic 

grains (including chert) and 2 percent feldspar. Sample 

46-1 (Bartlesville sandstone) is not representative of 

petrofacies II (fig. 4) and contains only 70 percent total 

quartz. Its presence in petrofacies II is probably an 

artifact of the clustering method.

B6 Evolution of Sedimentary Basins Anadarko Basin
CORRELATION COEFFICIENT

0.5 0.6 0.7 0.8 0.9 

I I I I I

Table 2. Petrofacies 

sandstones in this study

summary for Desmoinesian

I-A

HI

IV

Figure 4. Weighted pair-group average dendrogram of 

framework grains for Desmoinesian sandstones. Petrofacies 

I and II are rich in monocrystalline quartz and contain rare 

rock fragments, whereas petrofacies III and IV are compositionally heterogeneous and contain variable amounts of all 

constituents. Sample numbers shown along right-hand 

margin. Detailed petrofacies descriptions are given in table 2; 

sample location and compositional data are given in Dyman 

(1987).

Petrofacies II sandstones are found throughout the 

Desmoinesian in all but the westernmost part of the 

study area. Petrofacies II is intermediate in composition 

between quartz-rich petrofacies I and quartz-poor petrofacies III and IV.

[n, number of samples in each group. Mean and range given for 

framework constituents: Qm, monocrystalline quartz; Qp, polycrystalline quartz; Lt, total lithics; F, total feldspar]

I (n=19) Qm=84 78-98 

Qp=5 1-9

Lt=4 1-14

F=l 0-3

Samples widely distributed throughout Oklahoma; generally in 

lower Demoinesian Krebs Group. Two samples from Cabaniss 

Group (05 and 41-2). Subgroups I-A and I-B defined: I-A 

contains a mean of 88 percent Qm; I-B, 80 percent. Straight to 

slightly undulose quartz extinction. Trace of zircon and 

tourmaline.

H (n=8) 60-84 

3-15 

2-24

Qm=75

Qp=10

Lt=12 

F=2

Distributed throughout the Desmoinesian and absent from only 

western part of study area. Straight to slightly undulose 

extinction. Trace of zircon, tourmaline, and hornblende.

m (n-15) Qm=60 49-74

Qp=13 7-22

Lt=21 11-37 

F=4 0-8

Compositionally heterogeneous group restricted to mid and 

upper Desmoinesian samples. Distributed throughout study 

area. Highest metamorphic rock fragments content in sample 

population (mean 9 percent). Contains sample 36-1 (5 percent 

mica) and sample 17-1 (8 percent plagioclase). Variable quartz 

extinction. Trace of zircon, tourmaline, and hornblende.

IV (n=8) Qm=65 45-85

Qp=7 0-20

Lt=16 7-28

F=12 1-36

Compositionally heterogeneous upper Desmoinesian group, 

widely distributed throughout study area. Group includes two 

feldspar-rich samples (53-1, 81-1) from Oklahoma Panhandle 

and two limestone-rich samples (20-2, 91-1) from north and 

south parts of study area. Variable quartz extinction. Trace of 

zircon, tourmaline, and hornblende._______________

Petrofacies III

Petrofacies III is Compositionally heterogeneous, 

and, although it generally contains less than 70 percent 

monocrystalline quartz (mean 60 percent), values range 

from 49 to 74 percent (fig. 7). Polycrystalline quartz 

ranges from 7 to 22 percent and averages 13 percent. 

Petrofacies III is lithic rich (mean 21 percent) and 

metamorphic grains are the most abundant (mean 9 

percent). Sandstones vary from those with abundant 

metamorphic and polycrystalline quartz grains (sample 

40, Senora Formation, and sample 6-3, Red Fork 

sandstone) to those with abundant chert and metamorphic grains (sample 26-1, Red Fork sandstone, and 

sample 42-2, Bartlesville sandstone). Some samples

Statistical Analysis of Compositional Data, Desmoinesian Sandstones, Oklahoma B7
Figure 5. Petrofacies I sandstone. Red Fork sandstone, 

Gulf Oil Company No. 1 Sheik, sec. 25, T. 28 N., R. 1 E.; 

sample 24-1 taken at 3,605 ft. Quartzarenite (3.0 mm 

across).

Figure 6. Petrofacies II sandstone. Red Fork sandstone, 

Indian Wells No. 4-24 Hajek, sec. 24, T. 28 N., R. 5 W.; 

sample 13-2 taken at 4,681 ft. Litharenite (3.0 mm across).

Figure 7. Petrofacies III sandstone. Red Fork sandstone, 

Davis Oil No. 1 Herbing, sec. 17, T. 14 N., R. 14 W.; sample 

17-1 taken at 10,916 ft. Litharenite (3.0 mm across).

contain abundant plagioclase (sample 17-1, 8 percent, 

Red Fork sandstone) or mica (sample 36-1, 5 percent, 

Prue sandstone). Many compositionally intermediate 

forms exist.

Petrofacies III sandstones are found throughout 

the study area but are restricted to the middle and upper 

Desmoinesian. Sandstones from both petrofacies III and 

IV together form lithic-rich concentrations in eastern and 

western Oklahoma (fig. 3). Metamorphic-rich petrofacies III sandstones are abundant in the northwestcentral and eastern parts of Oklahoma.

Petrofacies IV

Petrofacies IV is also compositionally 

heterogeneous because cluster groups join at low levels 

of similarity. Petrofacies IV includes sandstones 

containing from 45 to 85 percent monocrystalline quartz 

(mean 65 percent). Polycrystalline quartz varies from 0 

to 20 percent and averages 7 percent. Samples vary from 

those containing abundant potassium feldspar, from the 

Oklahoma Panhandle (samples 53-1 and 81-1, 

Cherokee Group; fig. 8), to those containing abundant 

limestone grains, from the northern and southern parts 

of the study area (sample 20-2, Red Fork sandstone, and 

sample 91-1, Deese Formation; fig. 9). Petrofacies IV 

samples are generally feldspar and lithic rich, and 

sedimentary rock grains are more abundant than metamorphic rock grains. Several plagioclase-bearing samples 

(sample 20-2, 5 percent, Red Fork sandstone) are in 

petrofacies IV. Many compositionally intermediate 

forms exist.

Petrofacies IV samples are widely distributed in 

Oklahoma but are restricted to middle and upper 

Desmoinesian strata.

Factor-Score Maps

The relative importance of each grain type in 

differentiating between sandstone samples cannot be 

graphically defined using cluster diagrams. 

Correspondence analysis factor-score maps were 

generated in order to: (1) corroborate the petrofacies 

subdivision identified by cluster analysis (Can the four 

petrofacies be recognized on the factor score maps?); (2) 

observe sample distribution in factor space (How are the 

samples compositionally related, what is the range in 

compositional variation, and what can be said about 

provenance?); and (3) identify variable influence for 

factor score groupings (How does each variable affects 

each sample?). Figures 10-12 are factor-score maps for 

the first four factors and incorporate the 10 framework 

grain types used in the cluster analysis.

Figure 10 is the factor-score map for factors 1 and 

2. Sixty percent of the sample population variance

B8 Evolution of Sedimentary Basins Anadarko Basin
Figure 8. Petrofacies IV sandstone. Red Fork sandstone, 

Texaco No. 1 Hartley, sec. 33, T. 3 N., R. 10 E.; sample 81-1 

taken at 4,535 ft. Subarkose (3.0 mm across).

Figure 9. Petrofacies IV sandstone. Deese Group, BuckLeben No. 1 Harmon, sec. 8, T. 4 N., R. 1 W.; sample 91-1 

taken at 5,467 ft. Litharenite (3.0 mm across).

contributed mostly by potassium feldspar, quartz, plagioclase, chert, and limestone and metamorphic grains is 

represented by the first two factors (table 1). The cluster 

of points in the lower left part of the diagram represents 

monocrystalline quartz-rich (variable 1) sandstones 

predominantly from petrofacies I and II (samples 5, 10, 

and 41-2). Monocrystalline quartz-rich sandstones in the 

lower part of the lower left also tend to contain metamorphic grains (sample 28, Warner Sandstone Member; 

variable 9), whereas sandstones in the upper part of the 

left tend to contain more potassium feldspar grains 

(sample 48-1, Bartlesville sandstone; variable 5).

The scattered array of points at the right center and 

top of the figure represents quartz-poor petrofacies III 

and IV sandstones from the middle and upper 

Desmoinesian. Samples 53-1 and 81-1 at the top of the 

diagram are the potassium feldspar samples from the 

Cherokee Group in the Oklahoma Panhandle. Sample

46-1 (Bartlesville sandstone, lower right; variable 8) is 

the only sample containing volcanic grains. Sample 26-1 

(Red Fork sandstone) represents monocrystalline 

quartz-poor, polycrystalline quartz-rich (variable 2) 

petrofacies III and IV samples. The distribution of most 

points is gradational, and intermediate forms exist 

between clusters of samples.

Figure 11 is the factor-score map for factors 3 and 

4, which together contribute approximately 25 percent to 

the total variation in the sample population. This plot 

emphasizes sample differences resulting from the 

distribution of chert, mudstone-sandstone, monocrystalline and polycrystalline quartz, and limestone, and metamorphic grains. This plot is similar to the plot shown in 

figure 10 because the quartz-rich and quartz-poor petrofacies and the potassium feldspar-, volcanic-, and 

limestone-rich samples can be recognized. Because 

monocrystalline and polycrystalline quartz have lower 

loadings for factors 3 and 4, sample points are more 

centrally located on figure 11 and their lines are short.

The factor-score plot for factors 2 and 4 (fig. 12) 

reveals a greater spread of sample points because these 

two factors are not dominated by a single variable (for 

example, limestone or potassium feldspar) but instead 

contain higher loadings for several variables. Samples 

rich in metamorphic grains (samples 40 and 6-3, variable

1.0

0.5

cc 

O

o -

46-1.

QUARTZ 54 

RICH

0 0.5 1.0

FACTOR 2

Figure 10. Correspondence analysis factor-score map, 

factors 1 and 2. Numbers in squares represent variable 

contributions in factor space where variable 1 is monocrystalline quartz, variable 2 is polycrystalline quartz, variable 3 is 

chert, variable 4 is plagioclase, variable 5 is potassium 

feldspar, variable 6 is mudstone-sandstone, variable 7 is 

limestone, variable 8 is volcanic, variable 9 is metamorphic, 

and variable 10 is mica. Sample location and identification 

shown in figure 3; factor loadings given in table 1.

Statistical Analysis of Compositional Data, Desmoinesian Sandstones, Oklahoma B9
0.4

0.2

cce °

o

-0.2

-0.4

GD

ffl

QUARTZ POOR

.17-1

0.5

-0.5 0.5 1.0

FACTOR 3

Figure 11. Correspondence analysis factor-score map, 

factors 3 and 4. Numbers in squares represent variable 

contributions in factor space where variable 1 is monocrystalline quartz, variable 2 is polycrystalline quartz, variable 3 is 

chert, variable 4 is plagioclase, variable 5 is potassium 

feldspar, variable 6 is mudstone-sandstone, variable 7 is 

limestone, variable 8 is volcanic, variable 9 is metamorphic, 

and variable 10 is mica. Sample location and identification 

shown in figure 3; factor loadings given in table 1.

9) are well identified at the top of the figure because of 

the high loading for variable 9 in factor 4. The greater 

spread in monocrystalline quartz-rich (petrofacies I and 

II) samples is due to minor variations in the contribution 

of chert, lithic, and feldspar grains.

Sample distribution patterns in factor space based 

on other combinations of factors (for example, factors 2 

and 3) provide the same relationships presented here. 

The four petrofacies previously defined by using cluster 

analysis can be recognized using the correspondence 

analysis method. The variation in composition of 

sandstone samples based on the influence of each grain 

type is best illustrated, however, by using the 

correspondence analysis factor-score maps. The 

compositional limits defined for each plot represent the 

known compositional limits for Desmoinesian 

sandstones in this study.

PALEOGEOGRAPHIC IMPLICATIONS

A total quartz (Q)-total feldspar (F)-total lithics 

(L) plot (Dickinson and others, 1983) was prepared 

separately to verify and support the quantitative studies 

(fig. 13). QFL plots do not differentiate sandstones based 

on many variables but do support the quantitative

cc 

O

QUARTZ . 

RICH- /

V .ID-' ^1 

41-2 * . . 81-1

FACTOR 2

Figure 12. Correspondence analysis factor-score map, 

factors 2 and 4. Numbers in squares represent variable 

contributions in factor space where variable 1 is monocrystalline quartz, variable 2 is polycrystalline quartz, variable 3 is 

chert, variable 4 is plagioclase, variable 5 is potassium 

feldspar, variable 6 is mudstone-sandstone, variable 7 is 

limestone, variable 8 is volcanic, variable 9 is metamorphic, 

and variable 10 is mica. Sample location and identification 

shown in figure 3; factor loadings given in table 1.

studies. Early Desmoinesian (petrofacies I) sandstones 

were derived from craton interior (CI) continental block 

(cratonic shields and platforms) and recycled orogen 

(RO) terranes (collision orogens and foreland thrust 

belts), whereas middle and late Desmoinesian 

sandstones were derived from recycled orogen and 

transitional continental (TC) terranes (foreland 

continental blocks). Samples migrate toward the lithic 

pole from petrofacies I to IV.

Quantitative analyses in this study support the 

plate tectonic implications derived from the plot of 

Dickinson and others (1983) and indicate that 

Desmoinesian sandstones were derived from 

sedimentary, metamorphic, and granitic source areas 

(craton, erogenic belt, and batholith). Compositional 

trends from these quantitative analyses include the 

following:

1. Although compositional heterogeneity 

increases slightly upward from early to late Desmoinesian, some exceptions exist. The lower Desmoinesian 

Warner Sandstone Member and Hartshorne Sandstone 

are the most quartz rich but contain slightly less quartz 

westward in eastern Oklahoma. There is a change 

upward stratigraphically in eastern Oklahoma from Atokan, predominantly marine shelf sandstones to

BIO Evolution of Sedimentary Basins Anadarko Basin
PETROFACIES 

I-I

7 PETROFACIES

104-1 II-IV

PETROFACIES IV

Figure 13. Total quartz (Q)-total feldspar (F)-total lithics (L) 

plot of Desmoinesian sandstones used in this study. Cl, 

continental interior; TC, transitional continental; BU, 

basement uplift; RO, recycled orogen; DA, dissected arc; TA, 

transitional arc; UA, undissected arc. Methods and 

provenance boundaries from Dickinson and others (1983).

Desmoinesian, predominantly deltaic sandstones 

(O'Donnell, 1983). The central Oklahoma quartz-rich 

(petrofacies I) belt coincides in part with the Nemaha 

uplift. Adkison (1972) identified a north-trending 

sandstone-rich belt within the Ordovician Simpson 

Group in south-central Kansas. The north-trending 

quartz-rich belt may be related to these quartz-rich 

Simpson Group sandstone source areas; however, a 

thorough basin analysis should be conducted in order to 

fully define this trend.

2. Total lithics content is greatest (petrofacies III 

and IV) in two broadly defined north-trending belts in 

western and eastern Oklahoma. The total average lithic 

content of Desmoinesian sandstones is greatest in 

northern Oklahoma; available lithic detritus from 

southern sources may have been trapped in the deeper 

parts of the Anadarko, Ardmore, and McAlester basins. 

Hare (1970), however, recognized schistose metamorphic and shale fragments in the Thurman Sandstone 

and identified an Ouachita source for the Thurman 

Sandstone in Hughes and Coal Counties (southeast 

Oklahoma). Jacobson (1959) identified sedlitharenites 

rich in shale fragments in the Desmoinesian Deese 

Formation in the Ardmore basin and attributed these to 

unroofing of shales of the Mississippian and 

Pennsylvanian Springer Formation from the Arbuckle 

uplift. No change in the early to late Desmoinesian 

distribution of lithic grains was identified in this study.

3. Sandstones rich in limestone detritus are 

concentrated in two zones, one in northern Oklahoma 

and one in southern Oklahoma. Unroofing of lower 

Paleozoic carbonate terranes may have been greater in 

the Wichita-Criner and Arbuckle regions during the 

middle Desmoinesian (Tomlinson and McBee, 1959). 

Dunham (1955) identified limestone conglomerates and 

cherty, quartzose, and calcareous sandstones in the 

Deese Formation in the northern part of Murray County 

in southern Oklahoma. The northern Oklahoma sample 

maybe related to lower Paleozoic carbonate source areas 

of the Nemaha and central Kansas uplifts. Additional 

samples must be analyzed before the influence of local 

limestone sources can be fully established.

4. Areas rich in polycrystalline quartz coincide in 

part with areas rich in monocrystalline quartz and areas 

rich in total lithic grains, but the relationship to 

provenance is not clear. Problems may exist in assigning 

polycrystalline grains to either sedimentary lithic grains 

or quartz.

5. The two arkosic sandstones from the 

Oklahoma Panhandle are related to western uplifts of the 

ancestral Rocky Mountains. Precambrian granitic 

basement rocks of the Arbuckle and eastern WichitaCriner uplifts were not a sediment source during the 

Desmoinesian. Feldspar-bearing samples in northeastern 

Oklahoma are probably related to cratonic source areas 

to the north and east.

SUMMARY

Correspondence and cluster analysis is very 

useful in understanding compositional variation and 

establishing petrofacies in highly variable sample 

populations such as the one used in this study.

Results from R-mode correspondence analysis 

indicate that the relative proportions of monocrystalline 

and polycrystalline quartz, chert, potassium and plagioclase feldspar, and limestone, metamorphic, and 

mudstone-sandstone grains best characterize Desmoinesian sandstones in the population of samples 

studied here. Mica and volcanic grains, however, are not 

important in differentiating sandstones.

Results from Q-mode cluster and correspondence 

analysis indicate that lower Desmoinesian sandstones 

(Krebs Group) are relatively homogeneous and rich in 

monocrystalline quartz and contain rare rock fragments 

(petrofacies I and II). Basal Desmoinesian quartz-rich 

sandstones are restricted to eastern Oklahoma. Middle 

to upper Desmoinesian sandstones (Cabaniss and Marmaton Groups) are compositionally heterogeneous 

(petrofacies III and IV) and are widely distributed 

throughout the State. Desmoinesian sandstones exhibit a 

slight upward increase in compositional heterogeneity. 

Source areas include the craton, foreland blocks of the

Statistical Analysis of Compositional Data, Desmoinesian Sandstones, Oklahoma B11
Ancestral Rocky Mountains, and the orogenic terranes of 

southern Oklahoma. The broad north-trending quartzrich belt of the Desmoinesian coincides in part with the 

Nemaha trend and may have been derived from 

sandstone-rich beds within the Simpson Group.

REFERENCES CITED

Adkison, W.L., 1972, Stratigraphy and structure of Middle and 

Upper Ordovician rocks in the Sedgewick basin and 

adjacent areas, south and central Oklahoma: U.S. 

Geological Survey Professional Paper 702, 33 p.

Branson, C.C., 1961, Pennsylvanian System of the midcontinent, in Branson, C.C., ed., Pennsylvanian System in 

the United States: American Association of Petroleum 

Geologists, p. 431-460.

David, M., Campiglio, C, and Darling, R., 1974, Progresses in 

R- and Q-mode analysis; correspondence analysis and its 

application to the study of geological processes: 

Canadian Journal of Earth Sciences, v. 11, p. 131-146.

David, M., Dagbert, M., and Beauchamin, Y., 1977, Statistical 

analysis in geology, correspondence analysis method: 

Colorado School of Mines Quarterly, v. 72, no. 1, 60 p.

Davis, J.C., 1973, Statistics and data analysis in geology: New 

York, John Wiley, 550 p.

____ 1986, Statistics and data analysis in geology (2nd ed.): 

New York, John Wiley, 646 p.

Dickinson, W.R., Beard, L.S., Brackenridge, G.B., Erjavec, J.L., 

Ferguson, R.C., Inman, K.G., Knepp, R.A., Lindberg, 

F.A., and Ryberg, P.T., 1983, Provenance of North 

American Phanerozoic sandstones in relation to tectonic 

setting: American Association of Petroleum Geologists 

Bulletin, v. 94, p. 222-235.

Dickinson, W.R., and Suczek, C.A., 1979, Plate tectonics and 

sandstone compositions: American Association of 

Petroleum Geologists Bulletin, v. 63, p. 2164-2182.

Dunham, R.J., 1955, Pennsylvanian conglomerates, structure, 

and orogenic history of the Lake Classen area, Arbuckle 

Mountains, Oklahoma: American Association of 

Petroleum Geologists Bulletin, v. 39, p. 1-30.

Dyman, T.S., 1987, Petrographic data for Atokan through 

Virgilian sandstones in Oklahoma: U.S. Geological 

Survey Open-File Report 87-137, 15 p.

Ebanks, W.J., Jr., 1979, Correlation of Cherokee (Desmoinesian) sandstones of the Missouri-Kansas-Oklahoma tristate area, in Hyne, N.J., ed., Pennsylvanian sandstones 

of the midcontinent: Tulsa Geological Society Special 

Publication 1, p. 295-312.

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

the Anadarko basin, in Hyne, N.J., ed., Pennsylvanian 

sandstones of the midcontinent: Tulsa Geological Society 

Special Publication 1, p. 97-114.

Folk, R.F., 1968, Petrology of sedimentary rocks: Austin, Tex., 

Hemphill's, 170 p.

Frezon, S.E., and Dixon, G.H., 1975, Paleotectonic 

investigations of the Pennsylvanian System in the United 

States, Texas Panhandle and Oklahoma, in McKee, E.D., 

and Crosby, E.J., eds., Paleotectonic investigations of the 

Pennsylvanian System in the United States: U.S. 

Geological Survey Professional Paper 853, p. 177-196.

Hare, B.D., 1970, Petrology of the Thurman Sandstone 

(Desmoinesian), Hughes and Coal Counties, Oklahoma: 

The Compass, v. 48, no. 1, p. 45-55.

Jacobson, L., 1959, Petrology of Pennsylvanian sandstones and 

conglomerates of the Ardmore basin: Oklahoma 

Geological Survey Bulletin 79, 139 p.

Johnson, K.S., 1971, Geologic fieldtrips in Oklahoma, Book 

I Introduction, guidelines, and geologic history: 

Oklahoma Geological Survey Educational Publication 2, 

15 p.

Jordan, L., 1957, Subsurface stratigraphic names of Oklahoma: 

Oklahoma Geological Survey Guidebook 6, 220 p.

Kluth, C.F., and Coney, P.J., 1981, Plate tectonics of the 

ancestral Rocky Mountains: Geology, v. 9, p. 10-15.

Krumme, G.W., 1981, Stratigraphic significance of limestones 

of the Marmaton Group (Pennsylvanian, Desmoinesian) 

in eastern Oklahoma: Oklahoma Geological Survey 

Bulletin 131, 67 p.

Luza, K.V., 1978, Regional seismic and geologic evaluations of 

Nemaha uplift, Oklahoma, Kansas, and Nebraska: 

Oklahoma Geology Notes, v. 30, no. 2, p. 49-60.

O'Donnell, M.R., 1983, Regressive shelf deposits in the 

Pennsylvanian Arkoma basin, Oklahoma and Kansas: 

Shale Shaker, v. 33, p. 23-37.

Sutherland, P.K., 1982, Lower and Middle Pennsylvanian stratigraphy in south-central Oklahoma: Oklahoma 

Geological Survey Field Conference Guidebook 20,44 p.

Tomlinson, C.W., and McBee, W., 1959, Pennsylvanian 

sediments and orogenies of the Ardmore district, 

Oklahoma, in Petroleum geology of southern Oklahoma, 

volume II: American Association of Petroleum 

Geologists, p. 3-52.

* U.S GPO: 1989 773-894

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and Open-File Reports Section, Federal Center, Box 25425, Denver, 

CO 80225. (See latest Price and Availability List)

"Publications of the Geological Survey, 1879-1961" may be purchased by mail and over the counter in paperback book form and as a 

set of microfiche.

"Publications of the Geological Survey, 1962-1970" may be purchased by mail and over the counter in paperback book form and as a 

set of microfiche.

"Publications of the U.S. Geological Survey, 1971-1981" may be 

purchased by mail and over the counter in paperback book form (two 

volumes, publications listing and index) and as a set of microfiche.

Supplements for 1982,1983,1984,1985,1986, and for subsequent 

years since the last permanent catalog may be purchased by mail and 

over the counter in paperback book form.

State catalogs, "List of U.S. Geological Survey Geologic and 

Water-Supply Reports andMaps For(State)," may be purchased by mail 

and over the counter in paperback booklet form only

"Price and Availability List of U.S. Geological Survey Publications," issued annually, is available free of charge in paperback booklet form only.

Selected copies of a monthly catalog "New Publications of the U.S. 

Geological Survey" available free of charge by mail or may be obtained 

over the counter in paperback booklet form only. Those wishing a free 

subscription to the monthly catalog "New Publications of the U.S. 

Geological Survey" should write to the U.S. Geological Survey, 582 

National Center, Reston, VA 22092.

Note.-Prices of Government publications listed in older catalogs, 

announcements, and publications may be incorrect. Therefore, the 

prices charged may differ from the prices in catalogs, announcements, 

and publications.