Petrology and Depositional Facies of Siliciclastic 

Rocks of the Middle Ordovician Simpson Group, 

Mazur Well, Southeastern Anadarko Basin, Oklahoma

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Chapter E

Petrology and Depositional Facies of Siliciclastic 

Rocks of the Middle Ordovician Simpson Group, 

Mazur Well, Southeastern Anadarko Basin, Oklahoma

By ROMEO M. FLORES and C WILLIAM KEIGHIN

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

Flores, Romeo M.

Petrology and depositional facies of siliciclastic rocks of the Middle 

Ordovician Simpson group, Mazur Well, southeastern Anadarko Basin, 

Oklahoma.

(Evolution of sedimentary basins Anadarko Basin ; ch. E) (U.S. 

Geological Survey bulletin ; 1866-E)

"A multidisciplinary approach to researach studies of sedimentary rocks 

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

and modem."

Bibliography: p.

Supt.ofDocs.no.: 19.3:1866-E

1. Sandstone Anadarko Basin. 2. Geology, Stratigraphic Ordovician. 

3. Geology Anadarko Basin.

I. Keighin, C. William. II. Title. III. Title: Simpson group, Mazur Well, 

southeastern Anadarko Basin, Oklahoma. IV. Series. V. Series: U.S. 

Geological Survey bulletin ; 1866-E.

QE75.B9 no. 1866-E 557.3 s [552'.5] 89-600196 

[QE471.15.S25]
CONTENTS

Abstract El 

Introduction El 

Stratigraphy E2

Geophysical logs E2 

Core lithofacies E2

Sandstone lithofacies E2 

Siltstone lithofacies E3 

Mudstone lithofacies E4 

Limestone lithofacies E5 

Vertical lithofacies associations E5

Interpretation E6 

Sandstone petrography E7 

Textural analysis E7 

Mineralogical analysis E9

Detrital framework composition E9 

Cement Ell 

Paragenetic sequence Ell 

Porosity E12 

Interpretation E12 

Summary E14 

References cited E14 

Appendix 1 Photographs of core recovered from the Middle Ordovician Simpson

Group E18 

Appendix 2 Photographs of selected sedimentologic and (or) lithologic features in

core from the Middle Ordovician Simpson Group E32

Appendix 3 Photomicrographs showing features typical of core samples from the 

Middle Ordovician Simpson Group E39

FIGURES

1. Map showing location of Mazur well and Knox oil field in southeastern Anadarko basin of Oklahoma in relation to major tectonic features El

2. Generalized stratigraphic column for Middle Ordovician Simpson Group, 

Arbuckle Mountains E2

3. Logs for Mazur well showing response of various logging tools, cored 

intervals, and formation tops E3

4. Geophysical logs showing response of various logging tools for Simpson

Group interval in Mazur well E4 

5-8. Gamma-ray and lithologic logs for Mazur well:

5. McLish, Tulip Creek, and Bromide Formations E6

6. Cycle 1, Tulip Creek Formation E8

7. Cycle 2, lower member of Bromide Formation E9

8. Cycle 3, upper member of Bromide Formation E10 

9. Map and cross sections showing location of Mazur well in relation to aulacogen that existed in southern Oklahoma from Late Cambrian to Early Devonian time Ell

Contents II!
10. Frequency histograms of quartz grains in sandstones of cycles 1, 2, and 3, 

Mazur well E13

11. Quartz-feldspar-total rock fragments ternary diagram showing major mineral 

composition and classification of sandstones from the Mazur well E13

12. Diagram showing postdepositional and burial diagenetic history of sandstones 

from the Mazur well E13

TABLES

1. Grain-size properties of sandstones of the Simpson Group, Mazur well Ell

2. Mineral composition of sandstones of the Simpson Group, Mazur well E12

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

Petrology and Depositional Facies of Siliciclastic 

Rocks of the Middle Ordovician Simpson Group, 

Mazur Well, Southeastern Anadarko Basin, Oklahoma

By Romeo M. Flores andC. William Keighin

Abstract

The Mazur well in the southeastern Anadarko basin of 

Oklahoma penetrates the McLish (oldest), Tulip Creek, and 

Bromide Formations of the upper part of Middle Ordovician 

Simpson Group. Lithofacies and petrographic analysis of 650 

ft of core indicates deposition in a rapidly subsiding aulacogen. Lithofacies associations suggest that the deposits 

accumulated in cycles that consist of mudstone-siltstonelimestone in the lower part of the lithofacies sequence and 

quartzarenite in the upper part. The lithofacies sequence in 

the lower part of the cycles is interpreted as deposits of 

subtidal to intertidal environments. The lithofacies sequences 

in the upper part of the cycles are deposits of tidal channels.

The sandstones are made up of generally rounded and 

well-sorted to moderately sorted quartz grains and exhibit 

highly quartzose characteristics. They consist of framework 

grains and cement and lack detrital matrix. The framework 

grains are composed of monocrystalline and polycrystalline 

quartz (as much as 99 percent); feldspar (as much as 4 

percent) including orthoclase, microcline, and perthite; and 

rock fragments (as much as 12 percent) consisting of chert, 

micaceous rock fragments, siltstone, shale, limestone, glauconite, cellophane, and skeletal fossil fragments. Cements 

include silica, carbonate, and clay. The silica cement consists 

of quartz overgrowths, and the carbonate cement comprises 

calcite, ferroan calcite, ferroan dolomite, and ankerite. The 

mineralogical and textural maturity of the sandstones 

suggests deposition in tidal-influenced environments in 

which winnowing by waxing and waning tidal currents 

promoted clean, mature sediments.

INTRODUCTION

Extensive drilling in the Anadarko basin, a major 

hydrocarbon-producing basin in Oklahoma, has yielded a

Manuscript approved for publication, May 26, 1989.

100 KILOMETERS

WICHITA UPLIFT

ARBUCKLE UPLIFT

OUACHITA UPLIFT

Figure 1. Location of the Mazur well and Knox oil field in 

the southeastern Anadarko basin of Oklahoma in relation to 

major tectonic features.

large collection of Paleozoic cores. The core described in 

this report is from the Sunray Parker DX No. 1 Mazur 

well and consists of rocks from the middle part of the 

Upper Cambrian and Lower Ordovician Arbuckle 

Group and the upper part of the Middle Ordovician 

Simpson Group. The well is in southeastern Grady 

County (sec. 1, T. 3 N., R. 5 W.), in the southeastern part 

of the Anadarko basin (fig. 1). It is in the Knox oil field, 

from which gas is produced from the McLish and 

Bromide Formations of the upper part of the Simpson 

Group below depths of 15,000 ft (Kennedy, 1982).

The purpose of this report is to describe the 

lithofacies and petrography of 650 ft of core from the 

upper part of the Simpson Group in the Mazur well and 

to interpret the environments of deposition. Lithology, 

sedimentary structures, trace and body fossil content, and 

contact relationships are described for each rock unit. 

Textures and mineralogical compositions of the 

sandstones were estimated from 29 thin sections. In 

addition, geophysical log responses, including gammaPetrology and Depositional Facies, Simpson Group, Oklahoma E1
ray, sonic, neutron, resistivity, conductivity, and density, 

are related to lithology and depositional facies.

Acknowledgments. We acknowledge the assistance of the Oklahoma Geological Survey, Charles J. 

Mankin, Director, in providing access to the core, and to 

Eldon Cox and Walter Esry, Oklahoma Geological 

Survey Core and Sample Library, for their generous help.

STRATIGRAPHY

The interval of the Simpson Group studied in the 

Mazur core includes parts of the McLish, Tulip Creek, 

and Bromide Formations. A generalized stratigraphic 

column for the Simpson Group in the Arbuckle 

Mountains is shown in figure 2 (Ham, 1969; Johnson and 

others, 1984). The Arbuckle section has been used by 

Schramm (1964) and Borras (1979) as reference to the 

Simpson rock units in the Anadarko basin. Although 

lithologies in the Mazur core are similar to those of the 

Arbuckle section, the Mazur core contains less limestone 

and the thicknesses of units are different.

The upper 220 ft, or upper third, of the McLish 

Formation was cored in the Mazur well (fig. 3). The 

McLish is composed of interbedded sandstone, 

conglomeratic sandstone, siltstone, mudstone, and 

limestone; about 60 percent of the formation is 

composed of sandstone and conglomeratic sandstone. 

The McLish grades upward into the Tulip Creek 

Formation, which is 235 ft thick; the uppermost 55 ft of 

the cored interval is missing (fig. 3). The Tulip Creek 

consists of sandstone, conglomeratic sandstone, siltstone, 

mudstone, and limestone; about 90 percent of the

INTERVAL OF

MAZUR CORE

STUDIED

FEET METERS 

500 -i

0

 0

EXPLANATION

Sandstone 

HEI Shale

Calcareous shale 

Limestone

Figure 2. Generalized stratigraphic column for the 

Middle Ordovician Simpson Group in the Arbuckle 

Mountains. Modified from Ham (1969) and Johnson and 

others (1984).

formation is composed of sandstone and conglomeratic 

sandstone. The Bromide Formation, 295 ft thick, overlies 

the Tulip Creek (fig. 3). The contact between the two 

formations was not observed because 50 ft of core is 

missing. The Bromide Formation includes a lower 

member, 125 ft thick, and an upper member, 170 ft thick. 

It consists mainly of interbedded sandstone, siltstone, 

mudstone, and limestone; however, the lower part 

contains thick sandstone units. The formation as a whole 

contains about 35 percent sandstone; the sandstone is 

concentrated in the lower part and vertically dispersed in 

the upper part.

The cored interval of the Simpson Group contains 

about 60 percent sandstone and conglomeratic 

sandstone. The McLish interval in the well is more sandy 

than in other areas in the Anadarko basin, where it 

contains only as much as 25 percent sandstone. In the 

cored interval, the Tulip Creek Formation includes as 

much as 100 percent sandstone and the Bromide 

Formation as much as 35 percent sandstone (Borras, 

1979).

Geophysical Logs

Gamma-ray, sonic, neutron, resistivity, conductivity, and density logs are available for portions of the 

Mazur well. Available logs of suitable quality in the 

interval of principal interest were digitized so that the log 

curves could be compared with the lithologies observed 

in the cores. Gamma-ray, sonic, and neutron logs display 

the most graphic response to changes in lithology (fig. 4); 

log responses (figs. 3-8) may be compared with the 

lithologies illustrated and with the photographs of cores 

included in appendix 1.

Sandstones, or sandy intervals, and dark, waxy 

mudstones are clearly visible on the gamma-ray logs. The 

only log available through the cored interval to the total 

depth of the hole is the gamma-ray log (fig. 3); it 

indicates that, except for the Oil Creek Formation, few 

sandstones are found below the McLish Formation.

CORE LITHOFACIES

Sandstone Lithofacies

The white to gray sandstones vary from very fine to 

medium grained to conglomeratic. The conglomeratic 

sandstones consist of granule- to pebble-size clasts of 

quartz, mudstone, siltstone, limestone, and fossil (brachiopods and crinoids) fragments that occur either as 

basal lag deposits in the sandstone or distributed 

throughout the sandstone. Basal contacts are sharp to 

erosional; multiple erosional contacts (appendix 2-1)

E2 Evolution of Sedimentary Basins Anadarko Basin
E * B-12

B-6 

B-7

B-3 

B-9 

B-5

B-13

Upper member of 

Bromide Formation

Lower member of 

Bromide Formation

Tulip Creek 

Formation

McLish 

Formation

Oil Creek 

Formation

Joins 

Formation

Arbuckle 

Group

occur in the sandstones. The white sandstones are wellsorted, locally calcareous or calcite-cemented quartzFigure 3 (facing column). Gamma-ray log for Mazur well 

showing cored intervals (heavy lines), formation tops (picked 

from logs), and locations (asterisks) and numbers of 

photographs of core shown in appendix 2 (referred to by 

prefix B). Log to total depth of well; depth below surface (in 

feet) shown.

arenites. The gray sandstones are litharenites and contain 

a higher proportion of rock fragments than the quartzarenites. Quartzarenites are more common than litharenites.

The sandstones contain cross-laminated, ripplelaminated, parallel-laminated, and convoluted bedding 

(fig. 5; appendix 2-2, 2-3, 2-4). These sedimentary 

structures show the following combinations of vertical 

sequences: (1) cross laminations in the lower part of the 

sequence and ripple laminations in the upper part; (2) 

parallel laminations in the lower part of the sequence and 

ripple laminations in the upper part; and (3) multiple 

successions or series of cross laminations and ripple 

laminations as well as parallel laminations and some 

convolutions. Inclinations of cross laminations show 

bimodal orientation and range from 5° to 20°. The cross 

laminations are from 2 to 11 in. thick and are commonly 

defined by layers of finely divided plant fragments. The 

sandstones also contain many bioturbated beds 

(appendix 2-5) that are interbedded with crosslaminated, ripple-laminated, and parallel-laminated 

beds. The burrows are nondescript, horizontal and 

vertical, tubelike structures; vertical burrows are more 

common.

Siltstone Lithofacies

The siltstones are dark gray to light gray to white, 

depending on quartz content (appendix 2-6). A few of 

the sandy siltstones are arkosic, comprising 20-25 

percent feldspar (mainly orthoclase) (appendix 3-1). The 

siltstones show gradational upper and lower contacts 

where they are interbedded with mudstones and 

erosional contacts where they are overlain by sandstones. 

The siltstones are commonly ripple laminated 

(asymmetrical ripple laminations; appendix 2-7). Flaser 

bedding is developed where siltstones are intercalated 

with mudstones; pinstripe burrows are formed in the 

mudstones that bind the flasered units (appendix 2-8). 

Horizontal and vertical burrows of unknown origin are 

common in the siltstones, and horizontal bioturbation is 

more common than in the sandstones. Fragments of 

crinoid columnals and brachiopod shells commonly 

occur as lenses.

Petrology and Depositional Facies, Simpson Group, Oklahoma E3
Gamma-ray Sonic Neutron Resistivity Conductivity

50 1000 0 232

Density

Figure 4. Response of various logging tools for the Simpson 

shown in greater detail in figures 5-8; location of cycles shown 

shown.

Group interval in the Mazur well. Selected intervals are 

in figures 6-8 is marked. Depth below surface (in feet)

Mudstone Lithofacies

The mudstones are waxy and dark gray to black; 

black mudstones contain abundant finely divided plant 

fragments (appendix 2-9). Most mudstones are 

calcareous. Contacts with most adjoining rock types are 

gradational, but where overlain by sandstone the contact 

is erosional. The mudstones are locally fissile and 

splintery and may correctly be classified as muddy shales. 

X-ray diffraction analysis (Weber, 1987) indicates that 

the clay fraction in the shale of the McLish is mainly 

composed of illite and some chlorite. Sedimentary

structures include laminations that are apparent when 

the core is freshly cut. Some of the mudstones are 

interlaminated with thin, white, quartzose silty units that 

form parallel and ripple laminations, but most of the 

primary structures of the mudstones have been 

obliterated by bioturbation (appendix 2-10). Trace fossils (Planolites, Trichophyens, and Dictyodord) are 

common burrows in shales and mudstones of the 

Bromide Formation (Longman, 1981). Most of these 

animal burrows are interpreted as feeding traces. Body 

fossils of transported and abraded crinoid and brachiopod fragments also were found.

E4 Evolution of Sedimentary Basins Anadarko Basin
Limestone Lithofacies

The limestones are light to dark gray, and contacts 

with adjoining rock types are generally gradational to 

sharp. The limestones (appendix 2-11) vary from micrite 

to biomicrite (Folk, 1959). Most of the limestones are 

nodular or lumpy bedded (appendix 2-12). The nodules 

are as thick as 2 in. and as long as 3 in. Longman (1981) 

suggested that nodular-bedded limestones in the 

Bromide Formation are caused by concentrations of shell 

fragments. The nodules comprise white biosparite 

bounded by dark-gray micrite. Massive limestones 

consisting of sparse biomicrite are also common.

Limestones of the McLish Formation have been 

classified as wackestones to grainstones by Weber 

(1987). They consist of fossil fragments of echinoderms, 

bryozoans, trilobites, brachiopods, and ostracods. 

Limestones of the Tulip Creek and Bromide Formations 

commonly contain well-rounded crinoid, brachiopod, 

and bryozoa bioclasts (as much as 40 percent) (appendix 

3-2). Subordinate allochemical fragments of limestone 

include micritic pelletoids and ooids. Minor amounts of 

quartz, feldspar, and cellophane (as pyritized brachiopod 

fragments) grains make up the remaining constituents of 

the limestones. The allochemical and detrital grains are 

bounded by micritic calcite and cemented by sparry 

calcite, ferroan calcite, dolomite, and ankerite (appendix 

3-3). Fine-grained dolomites are associated with fossiliferous biomicrite.

Most of the sedimentary structures of the 

limestones are spar- and micrite-filled, tubular, vertical 

and horizontal burrows and burrow-mottles. V-shaped 

dessication mud cracks (appendix 2-13) are 

perpendicular to bedding planes and filled by micrite or 

sparite (appendix 2-13). Some clasts in the limestones 

appear to have been derived from the mud cracks. Shell 

fragments of brachiopods and crinoids (appendix 2-14) 

are the most important bioclasts and are concentrated in 

lenses or scattered throughout. Stylolites, which 

represent a diagenetic feature due to compaction, are 

common. A few small-scale cross laminations were 

observed.

VERTICAL LITHOFACIES ASSOCIATIONS

An inspection of the vertical lithofacies sequence 

shows cyclic repetition of rock types. The lithofacies 

associations consist of a lower mudstone unconformably 

overlain by quartzarenite. In other parts of the study 

interval, mudstone interbedded with limestone is overlain by siltstone. Thus, where quartzarenite unconformably overlies mudstone, it is assumed that the 

associated siltstone and limestone have been eroded.

The lithofacies association of quartzarenite and 

mudstone occurs in the McLish, Tulip Creek, and 

Bromide Formations. In the McLish, it is as thick as 85 ft; 

in the Tulip Creek, it is more than 200 ft thick and makes 

up almost the entire formation; in the Bromide 

Formation, the sequence is as thick as 75 ft. In addition, 

the Bromide Formation contains numerous thin intervals 

(10^40 ft thick) of the quartzarenite-mudstone lithofacies association. These vertical lithofacies associations 

occur throughout the upper part of the Simpson Group 

and are typified by the three cycles as shown in figures 

5-8.

Cycle 1 (fig. 6), in the Tulip Creek Formation, 

consists of mudstone, 10 ft thick, unconformably overlain 

by quartzarenite, 160 ft thick. The quartzarenite consists 

of multiple erosional-based sandstones that contain 

granule- to pebble-size particles or conglomeratic 

sandstones. The cycle contains a few thin limestones. The 

sandstone units are 2-40 ft thick and each unit contains a 

succession of cross, parallel, and ripple laminations 

commonly interrupted by burrowed units.

The basal mudstone of cycle 1 is represented by a 

distinctive peak on the gamma-ray log (figs. 5, 6). 

Although core is missing from this interval (fig. 3), the 

top of the cycle, on the basis of log response, is probably 

approximately 16,160 ft below the surface.

Cycle 2 (figs. 5, 7), 75 ft thick, is developed in the 

lower member of the Bromide Formation. It includes a 

mudstone, 30 ft thick, that is burrowed, silty, and fossiliferous in the lower part and grades upward into a 

burrowed, rippled, quartzose siltstone, 5 ft thick, interbedded with mudstone. The siltstone is, in turn, unconformably overlain by a quartzarenite 35 ft thick; the 

uppermost 5 ft of the quartzarenite is a scour-based 

sandstone. Internal structures are a succession of cross 

laminations and ripple laminations separated by bioturbated zones. The uppermost scour-based quartzarenite contains lag deposit of shells of crinoid and brachiopod fossils. Cycle 2 (fig. 7) is not as clearly defined by 

gamma-ray response as cycle 1; individual units and (or) 

beds are thinner, and it is difficult to place precise cycle 

boundaries on the basis of log response.

Cycle 3 (fig. 8), about 30 ft thick, is in the upper 

member of the Bromide Formation. It consists of a 

burrowed mudstone, 8 ft thick, that grades upward into a 

rippled, quartzose siltstone, 1 ft thick. The siltstone is 

unconformably overlain by 15 ft of quartzarenite that 

displays internal scouring. The quartzarenite is, in turn, 

conformably overlain by flaser-bedded quartzose siltstone (2 ft thick) and calcareous quartzarenite (4 ft 

thick). The scale of bedding in cycle 3 (fig. 8) is small 

enough that logs are of very limited utility in defining 

cycles.

Petrology and Depositional Facies, Simpson Group, Oklahoma E5
GAMMA

SEDIMENTARY 

LITHOLOGY STRUCTURES

DESCRIPTION 

LITHOLOGIC

16,000

16,200

16,400

16,600

o g "J*

F -"* 

F o >-i

g u. 0"

C fl\ ^

i ?^vV;

V ^iiffiS

 * i f 

<r v \r

Sandstone, fine-grained, white, low-angle cross laminations

Sandstone, siltstone, mudstone, limestone; locally fpssiliferous 

with brachiopod shells; quartzose sandstone

Sandstone, fine-grained, white, calcareous, silty and muddy 

units

Sandstone, siltstone, and mudstone; quartzose, fine-grained 

sandstone; waxy black mudstone

Sandstone, fine-grained, white, low-angle cross laminations 

local scours

Siltstone, gray, quartzose 

(Missing interval)

Mudstone, black, waxy, silty; with quartzose sandstone and 

limestone interbeds

(Missing interval)

Sandstone, fine-grained, with local fining-upward units 

(medium to fine grained) and conglomerate units, internal 

local scours, high- to low-angle cross laminations

Mudstone, black, waxy

Sandstone, fine-grained, white to light-gray, muddy to silty, 

with limestone units, fossiliferous with crinoid and 

brachiopod shells

Sandstone, fine-grained, white, quartzose 

Limestone, gray, muddy with waxy shale

Sandstone, fine-grained, white, quartzose, high- to low-angle 

cross laminations

Mudstone, black, waxy 

Sandstone, fine-grained, white

Interpretation

The precursor of the Anadarko basin was an 

aulacogen (Hoffman and others, 1974). The aulacogen in 

southern Oklahoma began with a graben stage of block 

faulting followed by volcanism and graben filling (late 

Proterozoic to Middle Cambrian time). The area evolved 

into a subsiding basin by Late Cambrian to Early Devonian time (fig. 9). Longman (1981) proposed that the 

Simpson Group was deposited in this subsiding basin and 

that the McLish, Tulip Creek, and Bromide Formations 

were deposited during pulses of subsidence. Between

these pulses, the aulacogen filled with sediments that 

passed into a gently dipping, terrigenous mud-dominated 

subtidal ramp merging with adjacent borderlands. 

During deposition of the Bromide Formation on this 

subtidal ramp along the northeast side of the basin, a 

basin-forebuildup-buildup-lagoon carbonate platform 

developed (Longman, 1981). Shale was deposited in the 

basin, micrite in the forebuildup, biosparite in the 

buildup, and micrite and shale in the lagoon. The 

lagoonal environment of this carbonate platform 

probably served as the primary depositional setting for 

the Simpson Group at the Mazur core site.

E6 Evolution of Sedimentary Basins Anadarko Basin
EXPLANATION

LITHOLOGY 

Conglomerate 

Sandstone 

Siltstone 

Mudstone

Limestone 

Calcareous rocks

SEDIMENTARY 

STRUCTURES

Cross laminations 

^"^ Ripple laminations 

 \XVX\X Flaserbeds

"" Parallel laminations

^ C Convolute laminations

VVV Burrows 

VOW Desiccation cracks

^X/IT" Fossil shells

GRAIN SIZE

Indicated by extent of lithologic column. CGL, conglomerate; 

SS, sandstone; SLTST, siltstone; MDST/LS, mudstone or 

limestone

Figure 5 (above and facing page). Gamma-ray and 

lithologic logs for McLish, Tulip Creek, and Bromide 

Formations, Mazur well. Depth below surface (in feet) 

shown.

The cyclic deposits of mudstone-siltstonequartzarenite probably represent seaward outbuilding or 

progradation of quartzarenites into the lagoonal 

environment. The mudstone-siltstone-limestone lithofacies association is interpreted as mainly subtidal 

lagoonal deposits. Flaser bedding in the siltstones 

suggests deposition in a lagoonal tidal-flat environment 

(Reineck and Singh, 1980), where tidal fluctuations 

provided sedimentation of silt during waxing stage and 

mud during waning stage. Reworking of sediments by 

feeding animals was prevalent during the waning stage 

and caused bioturbation. Desication mud cracks in 

limestones suggest deposition in an intertidal 

environment, where subaerial exposure contributed to 

drying of carbonate muds.

The quartzarenites contain erosional bases, 

multiple internal scours, and conglomeratic units and 

probably were deposited in channels. The types and 

succession of sedimentary structures of the quartzarenites are similar to those observed by Kumar and Sanders 

(1976), Hayes and Kana (1977), and de Mowbray and 

Visser (1984) in subtidal channel deposits. The lagconglomeratic sandstones consist of reworked clasts and 

fossil fragments and cross laminations (dunes and 

megaripples) and represent channel-bottom deposits. 

Associated ripple laminations and bioturbations reflect 

structures developed in channel-bar deposits, and the 

parallel laminations formed in shallow channel deposits. 

Tidal-flat deposition is probably represented by

bioturbation in the uppermost parts of the quartzarenite 

units. Multiple scours in the quartzarenites probably 

represent incised ebb and (or) flood-tidal channels.

The abundance of subtidal channel arenites 

suggests that the well location was either in close 

proximity to the source area or in a locus of terrigenous 

deposition. Schramm (1964) suggested that the point 

source of these sands was to the northeast, probably the 

Canadian Shield. Proximity to a locus of terrigenous 

deposition in a rapidly subsiding basin, however, is 

probably the more appropriate hypothesis. Deposition in 

a subtidal lagoon-intertidal setting in a subsiding basin is 

indicated by the location of the well southwest of the 

northwest-southeast hingeline of the aulacogen (fig. 9).

SANDSTONE PETROGRAPHY

The petrography of the sandstones of the Simpson 

Group was analyzed to determine textural and 

mineralogical variations of cycles 1, 2, and 3 (tables 1, 2). 

Textural analysis included measurements of mean grain 

size, sorting, skewness, and kurtosis, and mineralogical 

analysis comprised identification of framework, matrix, 

and cement composition, as well as recognition of paragenetic sequence and porosity. The petrography of the 

sandstones was determined by examining 29 epoxyimpregnated and stained (sodium cobaltinitrite, alizarinred-S, and potassium ferricyanide) thin sections.

Textural Analysis

Quartz grains are fine to medium grained, with 

mean grain size of 2.22 0. Sandstones of cycles 1 and 2 

are generally fine grained, with a mean grain size of 

2.32-2.35 0, and sandstones of cycle 3 are medium 

grained, with a mean grain size of 1.87 0. Most quartz 

grains are well rounded; minor quantities of grains are 

sub rounded (appendix 3-4). No apparent difference in 

roundness of quartz grains was observed between the 

fine-grained and medium-grained sandstones.

In general, the sandstones are moderately sorted 

(0.96 0); however, sorting varies from moderate (0.82 0) 

to poor (1.07 0). Sorting of the sandstones of cycles 1, 2, 

and 3 is best demonstrated by the frequency distributions 

of quartz grains shown in figure 10. Frequency 

distributions in cycles 1 and 2 are unimodal, skewed 

toward fine grained (0.77-0.91 0), and near symmetrical 

(0.05 0). The frequency distribution of cycle 3 is bimodal 

and skewed strongly toward fine grained (0.72 <£). Thus, 

the sandstones of cycle 3 are poorly sorted compared to 

those of cycles 1 and 2, which are moderately sorted.

The measure of peakedness of the frequency 

distribution curves of quartz grain size is indicated by 

kurtosis. In general, the frequency distribution curves are

Petrology and Depositional Facies, Simpson Group, Oklahoma E7
GAMMA

SEDIMENTARY 

LITHOLOGY STRUCTURES LITHOLOGIC DESCRIPTION

fc H

oco co 5 

1 1 1 1

160

16,250

16,350

s/ss/s/s 

S//SJ// 

S//7J7/ \r v *

Sandstone, fine-grained, locally gray, quartzose, low-angle 

cross laminations, local clasts

Conglomerate, sedimentary rock clasts; fining-upward, 

medium- to fine-grained sandstone units

Sandstone, fine-grained, white, quartzose, locally contains very 

thin conglomerate units, high- to low-angle cross 

laminations

Limestone, gray, no visible sedimentary structures

55-»»» 

rv vr'f

Sandstone, fine-grained, white, quartzose, contains numerous 

very thin conglomerate units, some silty-muddy laminations, high- to low-angle cross laminations

Mudstone, black, waxy

Sandstone, fine-grained, white, quartzose, silty to muddy

EXPLANATION

SEDIMENTARY 

STRUCTURES

Cross laminations 

^"VT* Ripple laminations 

 \X\\XX Flaserbeds

 Parallel laminations

\ C. Convolute laminations

Calcareous rocks

Burrows 

WVW Desiccation cracks

fXx^?N Fossil shells

GRAIN SIZE

Indicated by extent of lithologic column. CGL, conglomerate; 

SS, sandstone; SLTST, siltstone; MDST/LS, mudstone or 

limestone

Figure 6. Gamma-ray and lithologic logs for cycle 1, Tulip Creek Formation, Mazur well. Depth below surface (in feet) shown.

E8 Evolution of Sedimentary Basins Anadarko Basin
SEDIMENTARY 

LITHOLOGY STRUCTURES LITHOLOGIC DESCRIPTION

GAMMA

II II

16,050

16,100

V 

If

V V 'V

» r * w v

Iff xXxXX^x

Mudstonc, black, waxy, silty

Sandstone, fine-grained, white, quartzose 

Mudstone, black, waxy, silty

Sandstone, fine-grained, white, quartzose

Siltstone, gray, locally quartzose 

Mudstone, dark-gray, waxy, silty

(Missing interval)

Mudstone, black, silty

Sandstone, fine-grained, white, quartzose

Limestone, light-gray, fossiliferous with crinoid and brachiopod 

shells

EXPLANATION

Calcareous rocks

SEDIMENTARY 

STRUCTURES

Cross laminations 

^fXC" R'Pplc laminatio'ns 

"XXVXXX Flaserbeds 

- "= Parallel laminations 

£(. Convolute laminations

VV Burrows

VWW Desiccation cracks

'V1T* Fossil shells

GRAIN SIZE

Indicated by extent of lithologic column. CGL, conglomerate; 

SS, sandstone; SLTST, siltstone; MDST/LS, mudstone or 

limestone

Figure 7. Gamma-ray and lithologic logs for cycle 2, lower member of Bromide Formation, Mazur well. Depth below surface 

(in feet) shown.

platykurtic (0.78 0); however, the frequency distribution 

curves of the quartz grains of cycles 1 and 3 exhibit more 

peaks (mesokurtic and leptokurtic) than those of cycle 2 

(platykurtic).

Mineralogical Analysis

The sandstones of the Simpson Group are 

classified as arenites (Folk, 1968) and consist mainly of 

detrital framework grains and cement. Detrital clay

matrix is rare; authigenic clays sometimes occur as 

pore-filling cements. Quartzarenite (82 percent) is the 

most abundant sandstone type, and sublitharenite (14 

percent) and subarkose (4 percent) are the least common 

(fig. 11).

Detrital Framework Composition

The average detrital framework composition of the 

sandstones is 97.2 percent quartz, 1.5 percent feldspar,

Petrology and Depositional Facies, Simpson Group, Oklahoma E9
SEDIMENTARY 

LITHOLOGY STRUCTURES LITHOLOGIC DESCRIPTION

GAMMA II II

160

15,950

16,000

v «r v 

VVV

V * V

r w

.WV 

V

V V

V V

Limestone, gray, burrowed, fossiliferous

Limestone, gray, with locally waxy mudstone, burrowed

Sandstone, fine-grained, white, quartzose, locally silty to muddy; burrowed zones, local rip-up clasts; low-angle cross 

laminations

Mudstone, light-gray, waxy, silty, calcareous; limestone, gray

Sandstone, gray, fine-grained, locally quartzose, calcareous 

Siltstone, gray, muddy, locally quartzose, calcareous 

Sandstone, fine-grained, white, locally gray, quartzose, lowangle cross laminations 

Mudstone, black, waxy

Sandstone, fine-grained, white, quartzose

Mudstone, black, waxy

Sandstone, fine-grained, white, quartzose

EXPLANATION

LITHOLOGY 

Conglomerate

Sandstone

Siltstone

Mudstone

Limestone 

Calcareous rocks

SEDIMENTARY 

STRUCTURES

Cross laminations 

^J~~^* Ripple laminations 

 \X\\XX Flaserbeds

~ Parallel laminations 

Q Convolute laminations

W Burrows 

"VWW Desiccation cracks

^J^^ Fossil shells

GRAIN SIZE

Indicated by extent of lithologic column. CGL, conglomerate; 

SS, sandstone; SLTST, siltstone; MDST/LS, mudstone or 

limestone

Figure 8. Gamma-ray and lithologic logs for cycle 3, upper member of Bromide Formation, Mazur well. Depth below surface 

(in feet) shown.

and 1.3 percent rock fragments. Quartz includes monocrystalline and polycrystalline grains (appendix 3-5). 

Monocrystalline quartz, which exhibits straight to undulose extinction, is the most dominant constituent, ranging 

from 79 to 99 percent. Polycrystalline quartz is a minor 

constituent, ranging from 0 to 16 percent.

Feldspar rarely exceeds 4 volume percent and is 

composed of potassium feldspar (as much as 8 volume 

percent) consisting of orthoclase, microcline, and perthite. Orthoclase is the most common potassium feldspar;

some grains have been altered to kaolinite. Plagioclase is 

rare and does not exceed 1 volume percent.

Rock fragments rarely exceed 12 volume percent 

and consist of chert, micaceous rock fragments, siltstone, 

shale, limestone, glauconite, cellophane, and skeletal 

fossil fragments (crinoids, brachiopods, echinoderms, 

and bryozoans). Chert is the most common rock 

fragment (as much as 12 volume percent) (appendix 3-6, 

3-7). Siltstone and shale fragments rarely occur in 

amounts greater than 1 percent.

E10 Evolution of Sedimentary Basins Anadarko Basin
100 MILES

100 KILOMETERS

NE SW 

Late Proterozoic-Middle Cambrian

Late Cambrian-Early Devonian

EXPLANATION

I Rhyolite, basalt, hypa - 

byssal sills, tuffs, and 

sedimentary rocks

Marine carbonate rocks

Marine shale with sandstone and conglomerate

Figure 9. Location of Mazur well in relation to aulacogen 

(patterned area) that existed in southern Oklahoma from 

Late Cambrian to Early Devonian time. Schematic cross 

sections for two periods of time drawn through area of well 

are also shown.

Accessory minerals occur in amounts less than 0.5 

percent and include brown tourmaline, zircon, and hornblende. Opaque minerals include magnetite-ilmenite and 

leucoxene.

Visual comparison of the detrital framework 

composition of the sandstones (table 2) suggests some 

differences between sandstones of cycles 1, 2, and 3. The 

sandstones of cycle 1 contain the least quartz (95.6 

percent average) as compared to sandstones of cycles 2 

and 3, which may average as much as 99.8 percent. The 

sandstones of cycle 1 contain more feldspar (2.6 percent 

average) and rock fragments (1.8 percent average) than 

sandstones of cycles 2 and 3, which on average contain 

only 0.2-0.3 percent feldspar and no rock fragments.

Cement

Several types of cement are in the sandstones: silica 

(18 volume percent), carbonate (15 volume percent), and 

clay (3 volume percent). Authigenic silica cement in the 

form of syntaxial quartz overgrowths (appendix 3-8) is 

very common (as much as 37 volume percent). Many of 

the overgrowths are separated from their host grains by 

thin dust rims. Some overgrowths lack dust rims but can 

be identified by their euhedral outlines.

Authigenic carbonate cements include calcite, ferroan calcite, ferroan dolomite, and ankerite and may 

account for as much as 40 volume percent (individual 

sample) of the sandstone. Calcite (appendix 3-9) occurs

Table 1 . Grain-size properties of sandstones of the Simpson 

Group, Mazur well

[Properties in (j>; 50 measurements per thin section. Cycles shown in 

figureS. Measurements from Folk (1968)]

Mean grain 

size Sorting

Cycle 1 

Cycle 2 

Cycle 3 

Others

2.32 

2.35 

1.87 

2.22

0.82 

.82 

1.07 

.96

Skewness

0.05 

.05 

.72 

.04

Number of 

Kurtosis thin sections

0.91 

.77 

1.16 

.78

14 

5 

3 

7

both as poikilotopic and equant, mosaic crystals. Bluestained ferroan dolomite/ankerite commonly occurs as 

zoned euhedral rhombs (appendix 3-10), which clearly 

indicate variations in the ferrous iron content of pore 

fluids. The dolomite/ankerite commonly occurs as a 

pore-filling cement. Many detrital quartz grains and 

chert rock fragments display corroded boundaries and 

partial replacement by carbonate cements (appendix 

3-6).

Authigenic clay (appendix 3-11) is the least 

important cement and is in only about 25 percent of the 

samples. Where present, however, it accounts for as 

much as 23 volume percent of the sample. The clay is 

brown (in plane-polarized light) and appears to act as a 

pastelike, pore-filling cement (a pseudomatrix). The 

association of this clay with micaceous rock and clay-rich 

siltstone fragments indicates that the clays are alteration 

products of the rock fragments.

Cements in the sandstones of cycles 1,2, and 3 can 

be differentiated by the amounts of the quartz overgrowths, authigenic clays, and carbonate constituents. 

Quartz overgrowths are common (19.8-22 volume 

percent) in cycles 1 and 2; authigenic clay is most 

common (average 4.8 volume percent) in cycle 2; and 

carbonate cement is abundant (average 31.7 percent) in 

cycle 3.

Paragenetic Sequence

The postdepositional and burial diagenetic history 

of the sandstones (fig. 12) may be summarized as: (1) 

introduction of detrital clay coatings, (2) precipitation of 

quartz overgrowths, and (3) precipitation of carbonate 

cements. Formation of primary clay (appendix 3-12) and 

(or) some hematite coatings on the detrital quartz grains 

is the earliest diagenetic event and may have occurred 

either during deposition of the sediments or during a very 

early stage of diagenesis. It was followed by early burial 

diagenesis, during which quartz overgrowths formed. 

Dust rims between the primary detrital quartz grains and 

quartz overgrowths suggest that the cement may have 

been derived from pressure solution (Heald, 1965) and 

probably from alteration of shales (Hower and others, 

1976).

Petrology and Depositional Facies, Simpson Group, Oklahoma E11
Table 2. Mineral composition of sandstones of the Simpson Group, Mazur well

[In percent; 100 points each per thin section for detrital framework grain constituents and for total rock constituents.

Cycles shown in figure 5]

Total rock constituents

Detrital framework erains

Cycle 1 sandstones 

Cycle 2 sandstones 

Cycle 3 sandstones 

Other sandstones 

All sandstones

Quartz

95.6 

99.8 

99.7 

97.8 

97.2

Feldspar

2.6 

.2 

.3 

.5 

1.5

Rock 

fragments

1.8 

0 

0 

1.7 

1.3

Cement

Framework 

grains

65.6 

61.4 

59.3 

65.5 

64.0

Quartz 

overgrowths

22.0 

19.8 

9.0 

5.5 

18.0

Carbonate

12.0 

14.0 

31.7 

23.8 

15.0

Clay

0.4 

4.8 

0 

5.2 

3.0

Number 

of thin 

sections

14 

5 

3 

7 

29

Authigenic clay is an early diagenetic constituent 

that predates carbonate precipitation. It formed as porefilling cement binding detrital quartz grains, and its 

ductile appearance reflects early compaction during 

burial. It may have formed as the result of dissolution 

and recrystallization of clay-rich rock fragments and 

perhaps as the result of alteration of glauconite (AlShaieb and Walker, 1986).

Carbonate cementation occurred in three stages. 

The first stage consists of precipitation of mosaic and 

poikilotopic calcite, which replaced quartz overgrowths 

and grains and filled pores. The second stage is the 

replacement of early calcite cement by iron-bearing 

calcite and dolomite. The third stage includes 

precipitation of ferroan dolomite and ankerite as porefilling euhedral rhombs and replacement of early calcite 

cement. The source of carbonate is probably from 

pressure solution of skeletal fragments; however, where 

the sandstone is cemented by as much as 40 percent 

carbonate, the source of the carbonate remains an 

enigma.

Diagenetic events in the paragenetic sequence are 

not observed in all the sandstones. The most commonly 

recognized paragenetic sequences in sandstones of the 

cycles include the following.

Porosity

Much of the primary intergranular porosity of the 

sandstones has been destroyed by precipitation of quartz 

overgrowths, formation of authigenic clay, and carbonate 

cements. These cements occlude substantial amounts of 

primary porosity. Secondary porosity, formed by intergranular dissolution of quartz overgrowths and grains 

and dissolution of carbonate cement, ranges from a trace 

to slightly less than 10 percent. Where porosity is high, 75 

average percent of the porosity is due to intergranular 

dissolution and the resulting pore space is interconnected. Dissolution is marked by jagged quartz 

boundaries (appendix 3-13). The highest porosity is in 

the uppermost 20 ft of cycle 1, where total porosity

averages 4-5 percent. Total porosity of sandstones of 

cycles 2 and 3 varies from a trace to less than 1 percent 

(appendix 3-6).

The mechanisms of development of secondary 

porosity in the sandstones have been discussed by 

Schmidt and McDonald (1979), Larese and others 

(1984), and Loucks and others (1984), who emphasized 

the importance of CO2 in leaching detrital and authigenic 

constituents of the sandstones. The CO2 is produced by 

decarboxylation of organic acids during thermal 

maturation of shales. Surdam and others (1984) 

proposed that secondary porosity may have been 

developed by organic acids produced during maturation 

of kerogen. We propose that development of secondary 

porosity in sandstones of the Simpson Group may be 

related to leaching fluids.

Interpretation

The lithofacies interpretation of the Simpson 

Group sandstones as tidal deposits is suggested by their 

petrography. Their mineralogical and textural maturity, 

as indicated by quartz contents of more than 95 percent 

and by well-developed sorting and roundness, reflects 

vigorous winnowing and (or) a mineralogically mature 

source. The environment in tidal-influenced coasts is 

characterized by intensive physical and chemical 

breakdown of immature mineral grains.

Minor differences in the quartz, feldspar, and rock 

fragments contents of sandstones of cycles 1, 2, and 3 

may represent either derivation of the sediments from 

the same source area and (or) rocks or the distance of 

transport. The high quartz content may indicate 

sedimentary source rocks in which the quartz detritus 

was recycled; it may also be a function of the distance of 

transport of the sediments in which immature minerals 

are reworked and selectively removed from the sediment 

load by physical and chemical weathering. Early workers

El 2 Evolution of Sedimentary Basins Anadarko Basin
CYCLE 1 SANDSTONES

0.2

3 2

CYCLE 2 SANDSTONES

0 0.2 0.4 MILLIMETERS 

32 10

30 ,-

CYCLE 3 

SANDSTONES

02

3 2

0.4 0.6 MILLIMETERS

GRAIN SIZE

Figure 10. Frequency histograms of quartz grains 

in sandstones of cycles 1, 2, and 3, Mazur well.

(Drake, 1921; Dapples, 1955; Schramm, 1964) 

postulated that the Simpson Group sediments were 

derived from the Canadian Shield, a distance of

QUARTZARENITE

F RF 

O 14 SAMPLES 

O 4 SAMPLES 

0 2 SAMPLES 

3 1 SAMPLES

Figure 11. Quartz (Q)-feldspar (F)-total rock fragments 

(RF) ternary diagram showing major mineral composition 

and classification of sandstones from the Mazur well.

CARBONATE

Leaching 

(creates secondary porosity)

Fe dolomite and ankerite 

Fe calcite and dolomite 

Calcite

Authigenic clay

Quartz overgrowths

Detrital clay 

coatings

EARLY TIME LATE

Figure 12. Postdepositional and burial diagenetic history 

of sandstones from the Mazur well.

900-1,000 mi from the site of deposition, and they 

proposed long-distance transport by eolian processes and 

(or) longshore currents. These hypotheses cannot be 

confirmed or denied by this study. The concept of 

recycled sedimentary rocks as possible provenance 

cannot be voided by the rare occurrence of secondary 

dust rims on detrital quartz grains. A tidal origin for the 

maturity of the sandstones is here suggested as another 

working hypothesis.

Regardless of the problems of provenance and 

mode and distance of transport of the sediments, 

evidence of vigorous energy at the site of deposition is 

provided by removal of substantial quantities of labile 

minerals, extensive abrasion, and concentration of 

uniform grain sizes. The lack of detrital matrix also 

represents the effect of lag concentrates, in which fine 

detritus is selectively eroded, leaving only coarser grains. 

This process of selective sorting is probably produced by 

repeated application of shearing forces such as those

Petrology and Depositional Facies, Simpson Group, Oklahoma £13
inherent to waxing and waning tidal currents. The 

bimodality of quartz grains of cycle 3 perhaps mimics 

differential size sorting during high- and low-tide 

oscillations. Distribution of lag concentrates toward the 

fine grains, as characterized by poorer sorting than beach 

environments (from well to moderate sorting) and by 

skewness of less than 1 0, indicates a tidal-influenced, 

shallow-marine environment (Fuchtbauer, 1974, p. 60). 

Flushing out of the fine-grained matrix permits grainto-grain contacts and creates pore spaces that promote 

cementation during burial diagenesis.

Summary

Lithofacies and petrographic data compiled from a 

650-ft-thick core of the Middle Ordovician Simpson 

Group in the Mazur well show that the southeastern part 

of the Anadarko basin in Oklahoma was a tidalinfluenced coast. Sediments of the McLish, Tulip Creek, 

and Bromide Formations were deposited in a subsiding 

basin as cyclical lithofacies sequences containing a lower 

subtidal-intertidal mudstone, siltstone, and limestone 

lithofacies and an upper tidal-channel sandstone lithofacies.

The sandstone lithofacies consists mainly of quartzarenites that contain as much as 99 percent quartz, 4 

percent feldspar, and 12 percent rock fragments. The 

quartzarenites are fine to medium grained, exhibit well to 

moderate sorting, and have skewness of less than 1 <j>, all 

of which typify sediments formed in tidal-influenced 

shallow-marine environment.

The sandstones are composed of silica, carbonate, 

and clay cements and have a paragenetic history 

characterized by initial development of detrital clay 

coatings on the quartz grains, succeeded by precipitation 

of quartz overgrowths, and then formation of carbonates. 

The carbonate cement, a late diagenetic constituent, 

formed in three stages: precipitation of calcite that 

replaced quartz overgrowths and grains and filled pore 

spaces, replacement of early calcite by ferroan calcite and 

dolomite, and precipitation of ferroan dolomite and 

ankerite as pore fillings and replacement of early calcite. 

Although these cements destroyed primary porosity of 

the sandstones, secondary porosity developed by 

dissolution of the cements and grains.

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E14 Evolution of Sedimentary Basins Anadarko Basin
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chemistry of secondary porosity: American Association 

of Petroleum Geologists Memoir 37, p. 127-149.

Weber, S.J., 1987, Petrography and diagenesis of the McLish 

Formation, Simpson Group (Middle Ordovician), 

southeastern Anadarko Basin, Oklahoma: Stillwater, 

Oklahoma State University, M.S. thesis, 97 p.

Petrology and Depositional Facies, Simpson Group, Oklahoma E15

Appendixes 1-3
Appendix 1. Photographs of core recovered from the McLish, Tulip Creek, and Bromide Formations 

of the Middle Ordovician Simpson Group in the Mazur well, 15,913-16,413 ft. See figure 5 for lithologic 

descriptions and appendix 2 for photographs of selected core intervals and (or) sedimentary features.

El8 Evolution of Sedimentary Basins Anadarko Basin
Petrology and Depositional Facies, Simpson Group, Oklahoma E19
E20 Evolution of Sedimentary Basins Anadarko Basin
Petrology and Depositional Facies, Simpson Group, Oklahoma E21
E22 Evolution of Sedimentary Basins Anadarko Basin
Petrology and Depositional Facies, Simpson Group, Oklahoma E23
E24 Evolution of Sedimentary Basins Anadarko Basin
Petrology and Depositional Fades, Simpson Group, Oklahoma E25
E26 Evolution of Sedimentary Basins Anadarko Basin
Petrology and Depositional Facies, Simpson Group, Oklahoma E27
E28 Evolution of Sedimentary Basins Anadarko Basin
Petrology and Depositional Facies, Simpson Group, Oklahoma E29
E30 Evolution of Sedimentary Basins Anadarko Basin
Petrology and Depositional Facies, Simpson Group, Oklahoma E31
Appendix 2. Photographs of selected sedimentologic and (or) lithologic features in core from the Mazur well, McLish, Tulip 

Creek, and Bromide Formations of the Middle Ordovician Simpson Group. Centimeter scale shown.

2-1. Erosional contact (siltstone clast?) in litharenite. Depth 2-2. High-angle cross lamination in litharenite. Depth 16,382ft. 

16,306.5ft.

E32 Evolution of Sedimentary Basins Anadarko Basin
2-3. Low-angle cross laminations and ripple laminations in 2-4. Ripple laminations in litharenite. Depth 16,321 ft. 

litharenite. Depth 16,337.8 ft.

Petrology and Depositional Fades, Simpson Group, Oklahoma E33
2-5. Intense bioturbation in sandstone. Depth 16,404 ft.

2-6. Interbedded white quartzose siltstone and gray siltstone. 

Depth 16, 097 ft.

E34 Evolution of Sedimentary Basins Anadarko Basin
2-7. Ripple laminations in siltstone. Depth 16,098 ft. 2-8. Combination of vertical and horizontal burrows in flaser unit 

in siltstone. Depth 16,425.5 ft.

Petrology and Depositional Facies, Simpson Group, Oklahoma E35
2-9. Dark-gray, waxy mudstone. Depth 16,386 ft. 2-10. Vertical and horizontal burrows in mudstone. Depth 

16,396.8ft.

E36 Evolution of Sedimentary Basins Anadarko Basin
2-11. Light-gray dolomitic limestone (biosparite) interbedded 2-12. Nodular bedding of limestone; local concentrations of 

with light-gray micrite. Depth 16,457 ft. brachiopod fossils. Depth 15,919 ft.

Petrology and Depositional Facies, Simpson Group, Oklahoma E37
2-13. Dessication mudcracks in limestone. Depth 16,575.3 ft. 2-14. Brachiopod and crinoid fossil fragments in limestone. 

Depth 16,316.5ft.

E38 Evolution of Sedimentary Basins Anadarko Basin
Appendix 3. Photomicrographs showing features typical of core samples from 

the Middle Ordovician Simpson Group, Mazur well. Depths below surface.

3-1. Sandy siltstone containing potassium feldspar (K). Scale bar 0.5 mm; plane-polarized 

light. McLish Formation, 16,422 ft.

3-2. Fragments of brachiopods and crinoids (red-stained calcite) surrounded by (slightly) 

iron-bearing dolomite(?). Scale bar 0.1 mm; plane-polarized light. Tulip Creek Formation, 

16,832.9ft

Petrology and Depositional Facies, Simpson Group, Oklahoma E39
3-3. Rhombohedral crystals of dolomite(?) surrounded by poikilotopic calcite. Scale bar 1 

mm; plane-polarized light. McLish Formation, 16,555.3ft.

3-4. Sandstone, very tightly cemented by calcite (C); some quartz grains embedded in 

clay clast (Cy). Scale bar 1 mm; crossed nicols. Bromide Formation, 15,928.9 ft.

E40 Evolution of Sedimentary Basins Anadarko Basin
3-5. Intergranular quartz overgrowths (arrows) on rounded quartz grains and polycrystalline quartz grains. Scale bar 0.1 mm; crossed nicols. Tulip Creek Formation, 16,338 ft.

3-6. Low-porosity sandstone containing angular to subangular grains of quartz, partially 

leached chert (Re), and calcite (C), which has replaced some earlier detrital minerals. Scale 

bar 0.2 mm; crossed nicols. Tulip Creek Formation, 16,354 ft.

Petrology and Depositions! Facies, Simpson Group, Oklahoma E41
3-7. Low-porosity sandstone; porosity essentially limited to partially leached chert grains 

(arrow). Scale bar 1 mm; plane-polarized light. Tulip Creek Formation, 16,354 ft.

3-8. Sandstone cemented by quartz overgrowths and intergranular poikilotopic calcite (C). 

Scale bar 0.5 mm; crossed nicols. Tulip Creek Formation, 16,338 ft.

E42 Evolution of Sedimentary Basins Anadarko Basin
3-9. Rhombohedral grains of iron-bearing dolomite (D) intergrown in poikilotopic calcite 

(C), and detrital quartz grains and rock fragments (R). Scale bar 1 mm; plane-polarized light. 

Tulip Creek Formation, 16,302 ft.

3-10. Rhombohedral grains of iron-bearing carbonate (ankerite?) in intergranular matrixpseudomatrix of clay between subrounded detrital quartz grains. Scale bar 0.5 mm; 

crossed nicols. Bromide Formation, 15,966ft.

Petrology and Depositional Facies, Simpson Group, Oklahoma E43
3-11. Same as photograph 10; plane-polarized light.

3-12. Remnant of feldspar(?) (F) in intergranular, pore-filling calcite; thin layer of clay 

(arrow) partially coats one quartz grain. Scale bar 0.5 mm; crossed nicols. Tulip Creek 

Formation, 16,251 ft.

E44 Evolution of Sedimentary Basins Anadarko Basin
3-13. Intergranular porosity and slight dissolution of quartz grain surfaces. Scale bar 0.2 

mm; crossed nicols. Tulip Creek Formation, 16,230 ft.

Petrology and Depositional Facies, Simpson Group, Oklahoma E45

* U.S. GOVERNMENT PRINTING OFFICE: 1990-774-047



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