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III! III III III III IIIIII III IIII |I|I IIII IIII II III III III mm A R y '

Michigan State
University

 

This is to certify that the

thesis entitled

DOLOMITIZATION PATTERNS
IN THE WALKER OIL FIELD,
KENT AND OTTAWA COUNTIES, MICHIGAN

presented by

Richard J. Hamrick

has been accepted towards fulfillment
of the requirements for

Mo So degree in GeOlogY

 

 

W

Major professor

Date 7724/0/00. /77c9
/ J

0-7639

 

W
o - as C!
JAN 0 9 2005

x" '

 

DOLOMITIZATION PATTERNS
IN THE WALKER OIL FIELD,
KENT AND OTTAWA COUNTIES, MICHIGAN

By

Richard J: Hamrick

A THESIS

Submitted to
Michigan State University
in partial fulfillment of the requirements
for the degree of

MASTER OF SCIENCE
Department of Geology

1978

ABSTRACT
DOLOMITIZATION PATTERNS

IN THE WALKER OIL FIELD,
KENT AND OTTAWA COUNTIES, MICHIGAN

By

Richard J. Hamrick

A study of the Walker Oil Field was undertaken to
achieve better understanding about the origin of dolomite
in Devonian reservoir rocks and its relationship to struc-
tural configuration.

Carbonate samples from producing and nonproducing
Traverse Limestone wells were analyzed by the powdered
x-ray diffraction method to determine dolomite percentages
from various depth intervals. It was found that the highest
degree of dolomitization from the upper Traverse Limestone
occurred at or near the top of the formation. The degree of
epigenetic dolomitization shows a general correlation with
the structural contour map developed on the top of the
Traverse Limestone.

The geometry of folds and distribution of dolomite
percentages suggest relationship to faulting. Folding,
faulting, and solution activity are the major causes for
secondary porosity in the Traverse Limestone pay zone(s).

Carbonate and evaporite facies of the Traverse

Limestone appears to be related to the hypothesized West

Michigan Barrier (early diagenetic dolomite).

ACKNOWLEDGMENTS

The writer wishes to express his sincere thanks to
Dr. C. E. Prouty, Chairmanof the Guidance Committee, for
his devotion of time and interest in this problem and for
his helpful suggestions and constructive criticism in re-
viewing this manuscript. Thanks are also extended to Dr.
James W. Trow and Dr. John T. Wilband for their helpful
advice and review of the thesis text and illustrations.

Foremost appreciation must go to my wife Paulette
for her love and friendship throughout this time of trials
and tribulation. Her patience, understanding, and encour-

agement made completion of this work possible.

ii

TABLE OF CONTENTS

LIST OF TABLES . . . . . . . . . . . . . . . .
LIST OF FIGURES . . . . . . . . . . . . . . . .
INTRODUCTION . . . . . . . . . . . . . . . . .

General Statement . . . . . . . . . . . . .

Purpose and Scope
Previous Work . . . . . . . . . . . . . . .

O
O
O
O
O
O
O
‘
C
O
O
O
O
.

STRATIGRAPHIC FRAMEWORK . . . . . . . . . . . .
STRUCTURAL FRAMEWORK . . . . . . . . . . . . .
THE WAIKER 0 IL FIELD O I O O O O O O O O C O 0

Location and Extent .
History of Development

Production . . . . . .
Lithology . . . . . . .
Structure . . . . . . .

LIMESTONE AND DOLOMITE ANALYSES . . . . . . . .
Experimental Procedures . . . . . . . . . .

Source of Samples . . . . .
Sample Study . . . . . . .
Well Sample Preparation . .
X-Ray Diffraction Procedure

The Method . . . . . . . . . . .
Standardization Sample Preparation
Procedure . . . . . . . . . . . . .

Calibration Curve . . . . . . . . . . .
Data Calculation . . . . . . . . . . .

Data Interpretation . . . . . . . . . . . .

Vertical Dolomite Variation . . . . . .
Lateral Dolomite Variation . . . . . .

iii

Page

vi

H

\OKRUNH

16

16
18

19
20

25
25
25

27
27

28
29
30

31
32

34

3h
37

Walker Field Dolomitization Models
CONCLUSIONS . . . . . . . . . . . . .
BIBLIOGRAPHY . . . . . . . . . . . .
APPENDICES . . . . . . . . . . . . .

Appendix I. Sample Well Descriptions

Appendix II. List of Wells Used in Study

Appendix III. Dolomite Percent from

Traverse Limestone

iv

Page
47
57
59
65
65
67

83

LIST OF TABLES
Table Page

1. Different Components Used for Standardization . . 30

LIST OF FIGURES

Figure

10.

11.

12.

13.

14.

150

16.

Stratigraphic Succession in Michigan . .

Regional Structure Map of Michigan and
EnVironS I I I I I I I I I I I I I I I

Regional Structure Map of Michigan with
Important Linear Structures . . . . . .

Major Structural Trends in the Michigan
BaSin I I I I I I I I I I I I I I I I I

Southwestern Michigan Oil and Gas Fields
Location of Walker Oil Field in Michigan
Well Location Map . . . . . . . . . . . .

Structure Map on the Top of the Traverse
Limestone . . . . . . . . . . . . . . .

Calibration Curve of Dolomite Percent . .

Typical Vertical Dolomitization Patterns
in the Traverse Limestone . . . . . . .

Average Vertical Dolomitization Patterns
in the Traverse Limestone . . . . . . .

Dolomite Ratio Map - 0-5 Feet Below the
Top of the Traverse Limestone . . . . .

Dolomite Ratio Map - 5-10 Feet Below the
Top of the Traverse Limestone . . . . .

Dolomite Ratio Map - 10-20 Feet Below the
Top of the Traverse Limestone . . . . .

Dolomite Ratio Map - 20-30 Feet Below the
Top of the Traverse Limestone . . . . .

West Michigan Barrier Axes . . . . . . .

vi

Page

10

13

14
15
17
21

23
33

35

36

39

41

43

45
54

INTRODUCTION

General Statement

Petroleum production has been actively developed in
the southwestern portion of the Michigan Basin, a substan-
tial amount of which has been developed from the dolomitized
Traverse Limestone of Middle Devonian age. Porosity in this
dolomitic limestone has developed because of either strati-
graphically controlled, early diagenetic dolomitization or
epigenetic (post consolidation) dolomite formed by fluids
introduced along faults and fractures.

Many geologists contend that dolomitic limestone has
a tendency to develop along bedding planes, joints, frac-
tures, and faults within limestone formations (Landes, 1946;
Powell, 1950; Jodry, 1954; Goodrich, 1957; Egleston, 1958;
Jackson, 1958; Paris, 1977; Dastanpour, 1977).

A number of geologists have demonstrated that wide-
spread dolomitic facies have developed along shallow epi-
continental shelves and carbonate platform areas (Prouty,
1948; Cohee and Landes, 1958; Adams and Rhodes, 1960;
Deffeyes et al., 1965; Illing et al., 1965; Bathurst, 1971).
And others have proposed the development of dolomitization

related to persistently emergent areas or structural highs

2

(Hanshaw, et al., 1971; Badiozamani, 1973; Land, 1973).

Purpose and Scope

The Walker Oil Field of Kent and Ottawa Counties,
Michigan has been a prolific Traverse Limestone oil reser-
voir, producing over 17 million barrels of oil. This field
was chosen as the area of study because the region has a
well defined structure with accessible well samples.

It is the purpose of this study to; (1) establish
the occurrence of dolomitization in the Traverse Limestone
petroleum producing zone (implies porosity and permeabil—
ity), and (2) examine the distribution of dolomite relative
to the field structure. Also of importance will be a valid
attempt to put forth mechanism(s) which could have produced
dolomitization within the Traverse Limestone of the Walker
Field.

Structural interpretations will be made from maps
based on contacts established through microscopic examina-
tion of well samples. Dolomite percentages will be deter-
mined by comparative quantitative x-ray diffraction analysis
of various well samples and will be vertically represented
via bar graphs and laterally displayed by dolomite/lime-
stone ratio maps representing different depth horizons below
the top of the Traverse Limestone. The dolomite percentage
bar graphs and maps will be compared with the structural map
on the top of the Traverse Limestone to delineate relation-

ships.

3

It is the hope and purpose of this writer that the
results of this study will provide helpful information re-
garding the nature and characteristics of linear-producing
fields and aid future oil and gas exploration and produc-

tion programs in Michigan.

Previous Work

There have been a number of studies related to this
area of research. Chemical analyses demonstrating CaC03/
MgCa(CO3)2 ratios, following suggestions by Landes (1946) in
regard to local dolomitization, was first done in the Mich—
igan Basin by Powell (1950) from the Rogers City-Dundee
formations. Jodry (1954) utilized the titration method for
determining the Mg/Ca ratios of well samples, comparing the
data with several producing oil fields in Mecosta County.

In the studies of Tinklepaugh (1957), Jackson (1958), and
Dastanpour (1977), a definite relationship was observed be—
tween the degree of dolomitization and structural form.
Young (1955) and Egleston (1958) compared their Mg/Ca ratios
with structural maps in Stony Lake and Winfield Fields, res-
pectively, but were not impressed with such correlations in
their studies.

Recent dolomitization studies from semiquantitative
analyses in Michigan were made by Newhart (1976) on the
Middle Ordovician, Runyon (1976) on the Traverse Group, and

Syrjamaki (1977) on the Lower Ordovician. These studies,

4

along with that of Dastanpour (1977), have established the
existence of two types of dolomite: stratigraphic (diage-
netic) and secondary (epigenetic).

A number of studies have been made related to the
Traverse Group in Michigan. Isopach maps of the Traverse
Group were first published by Newcombe (1933). Later, Cohee
(1947) provided a more accurate estimate of Devonian thick-
ness along with a structure contour map based on the avail-
able well records to 1947 which penetrated the entire Tra-
verse Group section.

Henry (1949) studied the Traverse Group in the Pent-
water Oil Field and believed the Traverse pay to be part of
a Devonian reef structure. An investigation of the Traverse
Group in the Lansing area was made by Gustafson (1960), who
generated structural and isopach maps of this area. Fisher
(1969) examined the Traverse Formation, the top unit of the
Traverse Group, and developed a structure contour map on the
top of the Traverse Formation. Gardener (1974) suggests the
Traverse Group represents interfingering of proximal bio-
stromal and biohermal shelf carbonates on the west with dis-

tal fossiliferous gray muds to the east.

STRATIGRAPHIC FRAMEWORK

The stratigraphic sequence of rock lithologies im-
portant to this study is Middle Devonian age. Rock units
representing this geologic time span on the southwestern
side of the Michigan Basin are the Traverse Group and the
Rogers City and Dundee formations (Figure 1).

The Traverse Group with the Bell Shale formation at
the base lies conformably on the top of the Rogers City for-
mation (Cohee and Underwood, 1945). The Traverse Group is
divided into three major units by Cohee (1944): the upper
Traverse Formation, the middle Traverse Limestone, and the
lower Bell Shale.

Fisher (1969) considered the Traverse Formation to
be a legitimate stratigraphic formational unit and recom-
mended its inclusion as part of the Michigan stratigraphic
column. He described the Traverse Formation as a calcar-
eous, medium gray shale and shaley limestone which is a
transition zone between the Traverse Limestone of Middle
Devonian age and the Antrim Shale of probable Upper Devon-
ian age.

Cohee (1947) described the lithology of the Traverse
Group in the Michigan Basin as argillaceous limestone,

shales, and some pure limestone in eastern Michigan grading

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7

to the west into calcareous shales with the limestone becom-
ing more pure until the whole group becomes relatively pure
limestones in western Michigan with some dolomite and dolo-
mitic and argillaceous limestone. Jodry (1957) recognized

a lagoonal dolomitic facies in Western Michigan and open sea
facies east of a line at about the position of the Walker
Field today. The ”barrier" bringing about this facies
change was believed to reflect a high in the Precambrian
basement. Runyon (1976) recognized a similar facies distri-
bution in his semiquantitative study of the dolomite and
limestone of the Traverse Group. More will be said in this
regard later.

The lower Bell Shale formation of the Traverse Group
thins and disappears in much of the western and southwestern
portions of Michigan, so that the middle Traverse Limestones
rest directly on top of the Rogers City-Dundee limestones.
When present in the subsurface, the Bell Shale is typically
a soft, fossiliferous, gray shale (Jodry, 1957).

Cohee and Underwood (1945) stated that the Rogers
City and Dundee formations in the central part of the Michi-
gan Basin were composed of dolomite and limestone, whereas
in the far westcentral and southwestern area it is predomin-
antly dolomite. They also went on to state that although
easily recognizable on the eastern side of the Michigan
Basin, the Rogers City and Dundee formations in the west-
central and western side of the Basin are relatively indis-

tinquishable in subsurface due to similar lithology.

8

The Traverse Limestone, for purposes of this study,
is that interval between the top of the Bell Shale (if pre-

sent) and the base of the Traverse Formation.

STRUCTURAL FRAMEWORK

The Michigan Basin is a roughly circular and symme-
trical structural and sedimentary basin in the Central In-
terior platform of the United States. It encompasses the
Southern Peninsula and the eastern part of the Northern Pen-
insula of Michigan, Eastern Wisconsin, the northeast corner
of Illinois, Northern Indiana, Northwest Ohio and portions
of Ontario bordering Lake Huron, Lake St. Clair, and the
western end of Lake Erie (Cohee and Landes, 1958). Border-
ing the Basin is the Algonquin Arch to the east (Ontario),
the Findlay Arch to the southeast (NW Ohio), the Kankakee
Arch to the southwest (N. Indiana), the Wisconsin Arch to
the west (C. Wisconsin) and the Canadian Shield to the north
and northeast (Figure 2).

A number of theories have been postulated concerning
the origin of the Michigan Basin. Pirtle (1932) thought the
Basin probably originated in Precambrian time. He believed
the Wisconsin and Kankakee Arches were the cores of Precam—
brian mountains that stretched from central Wisconsin to NW
Indiana and that principle folds that now exist in later
sedimentary rocks were controlled by trends of folding or
lines of structural weakness that existed in basement rocks.

Folding by compression was most intense in Mississippian

10

   
  

 

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Figure 2

Regional Structure Map of Michigan and Environs

11

time. Newcombe (1933) also believed that the inherent
structure of the Michigan Basin was of Keweenawan (Precam-
brian) origin. He maintains that the present anticlinal
trend (NW-SE) in the Basin was the result of reactions of
zones of weakness developed in the basement during late Pre-
cambrian disturbances to the northeast. Lockett (19A?) be-
lieved downwarping of the Basin was caused by differential
sedimentary loading, causing block faulting in the basement
complex. He states that the parallel pattern of structural
trends in the Basin conform along basic lines of weakness in
the basement rock. Cohee and Landes (1958) claim that the
incipient folding (NW-SE) occurred intermittently in the
Paleozoic, with the main diastrophic activity during the
Lower Mississippian—pre-Pennsylvanian emergence. Green
(1957) stated that the Michigan and immediately surrounding
basins sank while the present bordering structures remained
stable, with the age of the Michigan Basin being Niagran.
Utilizing both geophysical and geological data, Hinze and
Merritt (1969) believe that a major rift zone (Mid-Michigan
Gravity and Magnetic High) had a dominant role in the devel-
opment of the Basin. The Basin may have originated from
isostatic sinking in response to the added mass of Keweena-
wan mafic rocks in the basement complex. Subsequent defor-
mation within the Basin has been associated with movements
along lines of basement weakness, apparently related to the
rift zone.

Prouty (1970) concludes that the basic structural

12

patterns of the Basin, including basement lineations and
bordering structures, was inherited from the Upper Precam-
brian. Structures within the Michigan Basin (Howell Anti-
cline, Lucas-Monroe Monocline, Albion-Scipio trend, etc.)
are generally thought to be fault controlled with the fault-
ing developing along lines of weakness in the Precambrian
basement rocks, Figure 3 (Ells, 1969; Fisher, 1969; Harding,
1974). Prouty (1976) believes that lineaments gleaned from
LANDSAT imagery are faults which fit a wrenching deformation
model and that the folded structures of the Michigan Basin
are generally related to the faults of this wrench system
(Figure A). From these lineaments, Prouty has demonstrated
that many of the oil and gas fields of Michigan produce
where fractures intersect (Figure 5). He indicates that it
is in these cross-structures that dolomitization is apt to
be most marked. Runyon (1976) states that the coincidence
of the suggested faults in Ottawa and Kent Counties and
Allegan County in crossing present day major structural
trends and tending to fall on isolated oil fields, such as
the giant Walker Field, suggest that these might also be
cross-structures occurring after Traverse deposition and
related to the origin of the major structural trends (Fig-

ures h and 5).

13

 

 
      

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Major Structural Trends in the Michigan Basin
(compiled by C. E. Prouty, 1971)

15

 

Figure 5. Southwestern Michigan Oil and Gas Fields

THE WALKER OIL FIELD

Location and Extent

The Walker Field is located in the western portion
of the present greater Grand Rapids, Michigan area. It in-
cludes sections 19, 20, and 27-35 of Walker Towship (T7N-
R12W), Kent County; sections 2-9 of Wyoming Township (T6N-
R12W), Kent County; Sections 13-15, 22-28, and 33-36 of
Tallmadge Township (T7N-R13W), Ottawa County; and sections
1, 2, and 12 of Georgetown Township (T6N-R13W), Ottawa
County (Figure 6).

The Walker Field extends in a northwest-southeas-
terly direction for a length of nearly eight miles, and is

approximately four miles in width at its widest point.

History of Development

The way to the discovery and development of the
Walker Field was pointed when the Salem Field in Allegan
County showed a northeast trend in the direction of Grand
Rapids. The area which ultimately became the field (Figure
5) was approximately at the intersection of the two trends
determined by extending the main axes of the Salem and Mus-
kegon Fields (Newcombe, 1939). The Grand River takes a

broad southward meander around the area in which doming was

16

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Figure 6.

Location of Walker Oil Field in Michigan

 

18

thought to exist, and shallow bedrock of the Michigan for-
mation quarried and mined near Grandville suggested compara-
tively strong off-structure dip and reversal. The shallow
bedrock was thought to be under a region of abnormal dip
because this condition had been characteristic of several
Michigan producing structures (Newcombe, 1939). A structure
contour map, based on data from 35 water wells and core
holes and the subsurface topography of three gypsum mines,
was developed on the Marshall sandstone to delineate the
structure. The discovery well in the Walker Field was loca-
ted in an area encircled by the highest closing Marshall
contour.

The Walker Oil Field came into being with the dis-
covery of oil on September 24. 1938, by MacCallum and Herr's
L. M. Story No. 1 located in section 32 of Walker Township
(T7N-R12W), Kent County. Field development started slowly
until Spring, 1939, when larger producing wells were brought
in approximately one-half mile east of the discovery well.
Then a drilling boom began which took on major proportions
by June, 1939. Because of this frenzied activity, the
Walker Field was known as the "field of the year" in Mich-

igan in 1939.

Production
The Walker Field produces from the Traverse Lime—
stone at approximately 1,140-1,205 feet depth below sea

level. The limestone section in which porosity has

19
developed is 30-50 feet thick, but the actual pay section is
much less than this. It may total 3-12 feet in thickness.

In 1940, the Walker Field was the most active field
in the state with 170 producing wells completed. With dril-
ling based on a ten acre spacing pattern, production in the
field reached its peak in January, 19h0, with 566,665 bar-
rels of oil and steadily declined to 162,940 barrels of oil
in December, 1940 (Grant, 19fi1). At the end of that year,
recovery had been approximately 1,500 barrels of oil per
acre.

The Walker Field is still an active field with 342
Traverse Limestone wells producing. As of the end of 1976,
784 Traverse wells had been drilled in the Walker Field,
covering and area of 8,560 acres (Mich. Geol. Survey, 1977).
Total production in 1976 was 112,081 barrels of oil, and the
cumulative oil production for the field through 1976 was

17,042,228 barrels of oil (Mich. Geol. Survey, 1977).

Lithology

The lower twenty feet of the Traverse Formation in
the Walker Field is typically a light gray to gray, shaley,
slightly pyritic, fine crystalline limestone. In numerous
wells throughout the field's extent and at various depth
horizons in the lower twenty feet of the Traverse Formation
are thin units of gypsum. These evaporite units are massive‘
and earthy to fibrous, with some random speckling of insol-

uble residue materials.

20

The Traverse Limestone interval from the Walker
Field, as examined under the binocular microscope (Appendix
I), ranges from limestone to dolomite, with dolomitic lime-
stone and calcic dolomite most prevalent. Color is gray to
buff to tan brown. This fine to medium crystalline carbon—
ate rock has associated beds of gypsum, which are typically
white to buff color, massive-earthy, randomly speckled with
very fine grain insoluble residues, and often slightly
pyritic.

In the majority of well sample suites examined, a
5-6 feet thick bed of gypsum occurs approximately 10-15 feet
below the top of the Traverse Limestone interval. This
evaporite unit is usually overlain by fine to medium crys-
talline dolomitic limestone or calcic dolomite. More well
data from the area of study is necessary to attempt success-
fully the generation of cross-sections through the field
depicting possible facies relationships between dolomites,

limestones, and evaporites.

Structure

Structural interpretation of the Walker Field was
based upon a cuttings study from 133 wells and selected
driller's logs. Well locations are shown in Figure 7 and
well locations and depths are recorded in Appendix II.

A general structural contour map of the field on the
top of the Traverse Limestone is shown in Figure 8. This

map reveals a large regional anticlinal structure with a

 

 

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FIGURE 7.

 

 

22

Figure 8

Structure Map on the Top of the Traverse Limestone

 

 

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WELL LOCATION MAP

FIGURE 7.

 

 

22

Figure 8

Structure Map on the Top of the Traverse Limestone

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WALKER OIL FIELD
Kent I: Ottawa Counties, Michigan
Structure Contour Map on the
13 1. 11 1‘ Top of the Traverse Limestone
Contour Int.= 5 Feet Sea Level Datum
Axes-principle Iolds
Axes-cross folds Inferred fault
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24

smaller doubly-plunging anticlinal structure to the south—
west and trending parallel to it. A small synclinal struc-
ture separates these two anticlinal structures. The major
axes of these larger structural trends is in a northwest-
southeast direction. This structural alignment is in agree-
ment with the general structural trends of the Traverse
Group in the southwestern portion of the Michigan Basin as
described by Runyon (1976).

Cross-structure trends within the Traverse Limestone
appear to be oriented in a general southwest-northeast di-
rection. These trends are especially discernable on the
northeast flank of the field where drag folding is observed
between the -1150 to -1175 feet contour intervals. Also, a
number of structural highs are oriented in a northeast-
southwest direction. In a summary of structural trends
within the Basin, Prouty (1970) states that there is promin-
ent NW-SE and NE-SW folding with evident lateral faults
(Figure #). The geometry of the Traverse Limestone struc—
ture highly suggests fault-related folding in the Walker
Field. 0n the basis of LANDSAT imagery studies, Prouty
(1976) has concluded that lineaments gleaned from these
studies are shear faults, that most basin folds are fault
related, that the principal faulting and folding was in pre-
Marshall-Mississippian time, and that the causative shearing
stresses are related to structural activity in the east

(Appalachian Orogeny).

LIMESTONE AND DOLOMITE ANALYSES

Experimental Procedures

Source of Samples

In subsurface geological research, the best type of
sample materials for analysis are well core samples, because
of known depth and lack of contamination. Rotary drill sam-
ples usually are unsatisfactory to work with because of dif-
ficultly in locating sample depth (due to down-hole contami-
nation), whereas cable tool samples are comparatively pure
and are satisfactory for depth location (Krumbein and $1058,
1963).

The well samples utilized in this study were from
cable tool sample suites from the Walker Oil Field which,
among other samples, the Gulf Refining Company donated to
the Department of Geology, Michigan State University.

Sample Study

Because of the lack of electric and mechanical logs
from the Walker Oil Field, the top of the Traverse Limestone
was picked from cuttings from 133 cable tool sample suites
and selected driller's logs. The sample suites represent
both producing and nonproducing wells and display a good

geographical spacing throughout the field.

25

26

To check the validity of certain driller's logs for
their designation of the top of the Traverse Limestone, the
writer contacted two drillers who heavily participated in
the field's development (John Mackey of Marne, Michigan and
Orville Palmer of Allegan, Michigan). It was established
that the Traverse Limestone top is an important drilling
marker throughout much of the Michigan Basin and this parti-
cular top is very distinctive and is an easy call to make.
Two-thirds of the sample suites examined microscopically
were from wells drilled by one or the other of these two
drillers. Comparison of the Traverse Limestone tops as
picked by these drillers and my own interpretation varied
no more than two feet in each well, with one exception.

The Traverse Limestone interval lies between the top
of the Bell Shale and the base of the Traverse Formation.
The top of this limestone interval was placed at the 90-100
percent level of carbonate concentration, as suggested by
Runyon in his study of the Traverse Group of Michigan (1976).
All well cuttings were examined under an Olympus Binocular
Microscope under a 10X combination of lenses, with a maximum
magnification of up to 40X. A fluorescent lamp was used as
the light source. For identifying and differentiating car-
bonates, a mixture of 7 parts water to 1 part concentrated
hydrochloric acid was utilized. Differentiation of carbon-

ate samples followed the procedure discussed by Low (1951).

27

Well Sample Preparation

The well samples to be used for x-ray diffraction
analyses were throughly washed with distilled water and
dried. Samples representing each five foot interval below
the top of the Traverse Limestone were selected and weighed
to approximately 2.0 grams. Most of the well sample suites
used penetrated only up to 30 feet into the Traverse Lime-

stone upon reaching the pay zone.

X-Ray Diffraction Procedure

Conventional chemical methods utilized in the deter-
mination of limestone and dolomite percentages in particular
rock specimens usually are very tedious and time consuming.
The x-ray diffraction method is a newer technique that of-
fers speed without sacrificing the accuracy and precision
found in wet chemical procedures (Kutsykovich, 1971;
Gunatilaka and Till, 1971). In the x-ray method, which is
based on the crystal phases of dolomite and calcite, the
ratio of calcite-to-dolomite is determined independently of
other Mg, Ca, and other carbonate-bearing materials (Tennant
and Berger, 1956). The x-ray diffraction technique is being
applied by workers in various areas of geological research
(Tennant and Berger, 1956; Weber, 1967; Otalora and Hess,
1969; Gunatilaka and Till, 1971; Badiozamani, 1973; Folk and
Land, 1975; Supko, 1977).

28

The Method

The determination of the relative quantities of a
multicomponent mixture by x-ray diffraction is based on the
relationship between the absorptive properties of minerals
and their peak intensities (Jenkins and DeVries, 1968).

The method utilized in this study consists of the
measurement of the relative peak intensities of the stron-
gest powder x-ray diffraction line for calcite and for dolo-
mite in a series of mixtures of known proportions. A cali-
bration curve is then constructed from these standards of
known quantities or proportions, and samples of unknown com-
position are then compared with the calcite/dolomite stand-
ardization curve (Tennant and Berger, 1956). This procedure
is primarily reliable for the determination of a quantita-
tive ratio for the minerals present in a rock specimen.

When an accurate and precise quantitative measurement of a
single mineral is required, a spiking system (use of an in-
ternal standard) becomes necessary (Gunatilaka and Till,
1971).

Diffraction peak intensities are influenced by grain
size, sample packing, and mineral orientation (Jenkins and
DeVries, 1968). To minimize peak intensity variability, all
samples x-rayed (calibration standard samples and well sam-
ples) were crushed and placed in a tungsten carbide grinding
vial and ground for approximately ten minutes in a Spex 8000
Ball Mill Grinder to achieve grain size uniformity. All

powdered samples were packed tightly with consistency into

29
specially crafted sample holders of Bakelite. Sample sur-
faces were then smoothed off and covered with a thin Mylar

strip.

Standardization Sample Preparation

In this study, previously prepared dolomite calibra-
tion standards were used. These standards were prepared by
M. Dastanpour for a recently completed investigation (1977).
The following two paragraphs and Table 1 are a summation
describing the procedure Dastanpour followed in preparing
the calibration standards.

The dolomite and calcium carbonate used in preparing
the calibration standards were purchased specimens of analy-
tical quality. The dolomite grains were soaked in 5 percent
hydrochloric acid for several hours to dissolve any fine
calcite crystals that might have grown between the dolomite
crystals. The dolomite grains were then throughly washed
with distilled water and dried.

Different proportions of dolomite and calcite were
weighed to an accuracy of one tenth of one milligram. Each
component was then completely mixed with another weighed
component to produce the desired dolomite mixture. Table 1
illustrates the different mixtures which were prepared for

use as calibration standards.

30

Table 1. Different Components Used for Standardization.

 

 

 

Grams Grams
Weiggiogiigent Mass dolomite Mass calcite
15 0.3000 1.7000
25 0.5000 1.5000
30 0.6000 1.h000
50 1.0000 1.0000
60 1.2000 0.8000
75 1.5000 0.5000
90 1.8000 0.2000
100 2.0000 0.0000
Procedure

Once packed into sample holders, the powdered car-
bonate samples were placed into the x-ray diffraction gonio-
meter and irradiated using Iron Km radiation with Manganese
filtration at 50 kilovolts and 10 milliamperes. A General
Electric X-Ray Diffraction Goniometer (Model XRD-6) was util-
ized for the irradiation of the carbonate samples. The
x-ray diffraction peaks were recorded by a strip-chart re-
corder (type HF, DC millivolt) with an event marker pen and
multispeed chart-drive unit. A range of 200 counts per sec-
ond and a time constant of 1 were used with a scan rate of
0.50 Ze/minute and a chart speed of 75 inches per hour. All

scans of 029 were made using a 1°, 0.1o slit system.

31

Each calibration standard sample and each well sam-
ple was scanned twice (sample was rotated 1800 in goniometer
holder before second scan) and the average intensity for
both calcite and dolomite was determined.

The following x-ray diffraction data was utilized in
the x—ray procedure (Berry, 1974; Fang and Bloss, 1974).
The interplanar spacing (d) corresponds to 029 for various

wavelengths where 026<90°:

 

Dolomite Calcite
MgCa(C03)2 Caco3
O 0
d spacing 2.88 A 3.03 A
°2e 39.14° 37.13°
File No. 11-78 5-586
Fiche No. 1-38-D10 1-18-E4

Calibration Curve

The meaning of the percentage of dolomite, as used
in this study, is the percent of the total carbonate, dolo—
mite (MgCa(C03)2) plus calcite (CaCOB), which is present as
dolomite in a rock specimen. Also, the dolomite described
in this study is considered an ideal dolomite. The ideal
mineral dolomite is described by Goldsmith and Graf (1958)
as a rhombohedral carbonate containing equal molar propor-
tions of calcium carbonate and magnesium carbonate.

A calibration curve was constructed by plotting the
dolomite/(dolomite+calcite) x 100 intensity ratio as measur-

ed versus the weight percent dolomite in the mixture

32
(Figure 9). Points plotted on the calibration curve were
obtained by preparing three samples of each weight percent
dolomite concentration and scanning each one twice (sample
rotation of 180°). Each point on the curve represents the
average result of six separate intensity peaks for each

dolomite standard concentration.

Data Calculation

 

The correlation coefficient between the peak inten-
sities and the mass of dolomite percents from the calibra-
tion standard samples is 0.996 (r = 0.996). This value in-
dicates that there is a high correlation or "good fit" be-
tween these two sets of variables. The calibration curve
(Figure 9) demonstrates that the calculated peak intensity
value,-Efia%235 x 100, represents the dolomite percent con-
centrated in that sample. Expressed in another way:
Dolomite_ Dolomite mass x 100 ,_ Dolomite_peak x 100
percent ‘(Dolomite + Calcite) mass-(53lomite + Calcite) peak
Each of the 315 powdered samples from 58 wells in the study
area were scanned twice and the average intensity peaks for
calcite and dolomite were determined. The dolomite percent-
age of each well sample was calculated using the following

expression:

Dolomite average peak x 100

Dolomite percent = (Dolomite + Calcite) average peak

33

100-
90-
80-
70"

60‘

x 100

50'

hD
hD + hC

40‘

30-

20-

10"

 

 

o T T f 1

01020504osow7b§o§i160
% DOLOMITE

O
Height of Dolomite Peak at 2.88 A
0
Height of Dolomite Peak at 3.03 A

hD
hC

Figure 9. Calibration Curve of Dolomite Percent

34

Data Interpretation

The Traverse Limestone in the area of study was
divided into intervals of 0-5, 5-10, 10-20, 20-30, and 30-
40 feet below the top of the Traverse Limestone in each well
that was x-rayed. Some wells do not have the lower depth
intervals because these wells had reached the pay zone.
Dolomite percentage for each of these depth intervals was
calculated from the result of the x-ray diffraction analysis
(Appendix III). Vertical and lateral variation of dolomite

percent is discussed below.

Vertical Dolomite Variation

Dolomite percent values were plotted against their
depth below the top of the Traverse Limestone. Typical
vertical dolomitization patterns within the upper Traverse
Limestone in the area of study is shown in Figure 10. Two
of the wells show the highest dolomite ratios in the 0—5
feet interval, and the other two wells show the highest ra-
tios in the 5-10 feet interval. All these wells display a
distinct decrease in dolomite percentage downward from high-
er dolomite percentages at or near the top of the Traverse
Limestone.

Bar graphs were constructed depicting the field
average of dolomite percent values versus depth interval and
the average percent values versus depth interval from the
northwest portion and the southeast portion of the field's

main structural trend (Figure 11). The bar graphs of the

Depth Below the Top of Traverse Limestone

35

% DOLOMITE

0 1p 20 3‘0 49 so op 79 so 99 190

5-10

 

 

 

10-20

20-30

 

 

Well No. 7

% DOLOMITE

0 1p 29 39 49 so 69 79 8p 99 190

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

__2:§__
5-«> ]
10-20
20-30
30-40
Well No. 89
% DOLOMITE % DOLOMITE
o '3) 29 39 .10 o ‘ua 29 39 10
0-5 0-5
5-10 5-10
10-20 10-20
20-30 20-30
Well No. 121 Well No. 319
Figure 10

Typical Vertical Dolomitization Patterns
in the Traverse Limestone

Depth Below the Top of Traverse Limestone

36

% DOLOMITE

o 53 1o 15 20 25 30 3.5

_°"_5_.
5-10

10-20

 

 

 

20-30

 

30-40

 

 

 

Average values for NW structure
(Tallmadge Township)

% DOLOMITE

o§1o1520253035

A J I l L .1

0-5
5-10 A

10-20

 

20-30

30-40

 

 

Average values for SE structure
(Walker and Wyoming Townships)

% DOLOMITE

0 § ‘NJ 15 20 23 39 35

0-5
5-10 .

10-20

 

 

20-30

 

 

30-40

 

 

 

Average values for Walker Field

Figure 11

Average Vertical Dolomitization Patterns

in the Traverse Limestone

37

field average and that of the NW portion of the structural
trend show the highest dolomite percent values in the 5-10
feet depth interval. The SE portion of the main structural
trend shows the highest dolomite percent value in the 0-5
feet depth interval. As demonstrated in the bar graphs of
individual wells, the bar graphs illustrating average dolo-
mite percent values show a decrease in dolomite percent
downward from higher dolomite percent values at or near the

top of the Traverse Limestone.

Lateral Dolomite Variation

The dolomite analyses provided data for dolomite
ratio maps, which indicate the relative degree of dolomiti-
zation to the Traverse Limestone structure. Dolomite per-
cent values were plotted on the base map of the area for
each of the top four depth intervals (0-5 feet, 5-10 feet,
10-20 feet, and 20-30 feet) and lines of equal dolomite per-
cent (isodolic) were constructed. A similar map of the 30-
40 feet depth interval was not constructed because of the
small lateral variation demonstrated in this section.

The dolomitization patterns of each isodolic map
(Figures 12, 13, 14, and 15) roughly correlate with the
structural alignment of the area. With each of the iso-
dolic maps, high dolomitization values coincide closely with
a structural high located in the most westerly portion of
the field. In the north-northwesterly portion of the field

structure, the highest dolomitization values do not

38

Figure 12

Dolomite Ratio Map
0-5 Feet Below the Top of the Traverse Limestone

 

 
 

OTTAWA CO. KENT CO. I I2W

 

  
 
 
 
 
  
 

WALKER OIL FIELD
Kent In Ottawa Counties, Michigan
Dolomite Ratio Map: 0-5 Feet Below
13 1. " to the Top of the Traverse Limestone
leopleth Interval = 5% Dolomite
Producing Well: . Dry Hole: .

0 miles I
m—

 

_|

 

 

 

 

GEORGETOWN TWP. TALLMADGE TWP.

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

R I3W OTTAWA CO. KENT CO. . R I2 W

q

'dMl ONIWOAM 'clMl IBXIVM

—¢

 

 

40

Figure 13

Dolomite Ratio Map
5-10 Feet Below the Top of the Traverse Limestone

We- «.0 W-v‘w‘.—_H

—--‘-O~"-—.——-.-—c

 

 

R I3 W OTTAWA CO. KENT CO. R I2 W

 

WALKER OIL FIELD
Kent & Ottawa Counties, Michigan
Dolomite Ratio Map? 5-I0 Feet Below
13 1., 16 the Top of the Traverse Limestone
Isopleth Interval = 5% Dolomite
Producing Well: . Dry Hole: 0

0 miles I
m

 

__l__L__.__._______

 

 

2V4

 

‘ ‘4‘—

  

21 22 23
\
\
\
\I:
\
\\
ll 23 \\ 27 26
’l l. \
\33 o \
\\\ 3. \\
\
\
\
T33 34 l 35
__...2o/'i‘ I
. ’0 .2. \

 

GEORGETOWN TWP. TALLMADGE TWP.

.. . ,3... ”A...“ A.) .m,

ZV-I

 

 

l
I
fio
§e
so/ a
l—/
fie
. g.
!e
5 5'
/
I
//
/
‘t L/‘//
,v
fie

 

20"

 

\
i0

 

 

 

 

 

 

 

 

 

 

R I3 W OTTAWA CO. KENT CO. - R I2 W

'dMI. ONIWOAM 'dMl liXIVM

20"

 

 

 

 

 

42

Figure 14

Dolomite Ratio Map
10-20 Feet Below the Top of the Traverse Limestone

 

 

 

 

 

ZV-t

GEORGETOMIN TWP. TALLMADGE TWP.

20-!

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

R I3 W OTTAWA CO. KENT CO. R I2 W
3’ \ WALKER OIL FIELD
Kent & Ottawa Counties, Michigan
Dolomite Ratio Map: IO-20 Feet Below
re 15 ‘1 u the Top of the Traverse Limestone
lsopleth Interval = 5% Dolomite
Producing Well: . Dry Hole: 0
0 miles I
-:-:—:—
21 22 20 21 22 23
\ \
\. *° . \
.. "’ \
\ \
22 21 \0 29 \ 21 26
I
.e ,, ,, \
:/ °/\ \ .
/ , / /.:r1o .:. / .:. .3.
/ \0 ‘U
\ \ 2 \_/ ‘0,
\ \g/ ,o .:.
/
// )3: I“ \\
33 34 35 36 31 32 ° 34 35
.3.
2:. .3.
\ .:. 2 2.
3. ‘°/\ 5'
4 . 3 2 1 o 5 4 3 53' 1
/ if .— ~ — — ~ __—20/ ’z. e
.I. /_/15
//
/
9 1o 11 12 1 e 9 1o 11
. I”
R I3W OTTAWA CO. KENT CO. R I2 W

ZV-e

'dMl ONIWOAM 'dMl IJXIVM

20-!

 

 

44

Figure 15

Dolomite Ratio Map
20-30 Feet Below the Top of the Traverse Limestone

 

OTTAWA CO. KENT CO.

 

 

2‘4"

GEORGETOWN TWP. TALLMADGE TWP.

.4

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

I W R I2W
a /
3’79, / I WALKER OIL FIELD
/ /I ‘0 §// I Kent In Ottawa Counties, Michigan
/ /"’°~g// ,5 I Dolomite Ratio Map: 20-30 Feet Below
16 / 2° \ the Top of the Traverse Limestone
1s / 13 I 10 11 1o
3 \ I lsopleth Interval = 5% Dolomite
I Producing Well: 0 Dry Hole: 0
I 0 miles I
\ I
\ I
\
\\
/ 3 \ \\
21 22 24 \ 21 22 23
\
\\ \\
\ \ 1'
7
\
/\___,_/ \ \\ \ N
.'. I\ \
\\ \
\ \ \
e 21 24 25 \ 29 23 \ 21 26
/ \ 2'" \
‘ -A /
\ a O
.6 ° /” . \
”\ I , /... .3.
‘\ 225 ‘3 \
\ / g
\ 1o
____— /. \
/’ ,2, \
// \ s
33 34 as 34 32 33 34 \ 35 .2
2:4 ‘0 x
5- . \\ S
.2. .1. \ g
___________________________________________ 4:1 m______.______5_ K _____ '
\U ’4 \ 5
.2. 3. .3 \ o
- E
m z
4 3 2 1 5 4 3 .2. 2 ,0
3:9 ' \
I \
l
I T
9 1o . 11 12 I e 9 1o 11 5
I N
I .3.
l I.
R I3W OTTAWA CO. KENT CO. R I2 W

 

46

correlate with the structural high, but increase in value
downdip off structure.

Isodolic maps representing the top three depth in-
tervals (Figures 12, 13, and 14) display a number of NE-SW
trends, which in some instances, closely correlate with
cross-structures observed in the structure contour map. The
isodolic maps of the 0-5 and 5-10 feet intervals display a
N-S trend of certain isodolic contour intervals in the NW
portion of the field.

0f the four isodolic maps constructed depicting lat-
eral dolomite variation in the upper Traverse Limestone, the
isodolic map representing the 0-5 feet depth interval below
the top of the Traverse Limestone most closely correlates
with the field's diverse structure.

Where the degree of dolomitization increases along
the structural trend and the apices of folds, the inference
can be made that channelways along which dolomitization oc-
curred are related in some way to the axes (and origin) of
these folds. This implies faulting and fracturing. Where
dolomitization patterns do not correlate with the structural
trends or folding, the dolomitization patterns might be
identifying the traces of faults and fractures not expressed

by folding.

47

Walker Field Dolomitization.Models

Dolomite percent in the upper portion of the Tra-
verse Limestone throughout the Walker Field displays a wide
variation over a short distance, both vertically and later-
ally. Much of this limestone interval is composed of very
fine to finely crystalline dolomitic limestone and calcic
dolomite with associated evaporite units (gypsum). In only
7 of the 315 well samples x-rayed were the dolomite percent
values over 70 percent. This dolomite was typically fine to
medium crystalline. In the majority of well samples x-ray-
ed, dolomitization values ranging from 10 percent up to 70
percent within limestone and gypsum units indicates the
presence of dolomite, even though dolomite itself was not
observed under the binocular microscope.

Criteria exist which point to two separate dolomiti-
zation processes which developed at different times within
the upper Traverse Limestone of the Walker Field. One dolo-
mitization process is an early diagenetic dolomitization,
where Mg replacement of Ca occurs before cementation of the
calcite matrix, probably penecontemporaneous with sediment
deposition. The second dolomitization process is post-dia-
genetic in nature where a secondary, clearly epigenetic
dolomite replaces calcite after cementation of the original
calcite matrix.

Certain conditions are necessary for dolomitization

to occur (Wilson, 1975): (1) a sufficiently porous and

48

permeable calcareous sediment to act as host for the Mg re-
placement; (2) a fluid of the correct chemical composition
to react, capable of dissolving CaC03 releasing Mg; (3) a
long-enduring supply fo Mg; and (4) a hydrodynamic head to
force great volumes of water through the sediment.

Secondary, post diagenetic dolomite is believed to
exist in a number of wells in the Walker Field based on
crystalline dolomite, high x-ray dolomite percent values,
and a general correlation between dolomite values and the
field's structure. This secondary replacement dolomite is
probably brought about by ground water percolation through
existing fractures in brittle carbonate rocks. Ground wa-
ter in this zone percolating along joints, fractures, seams,
and other post-consolidation channelways could selectively
dissolve the relatively soluble calcite and precipitate
dolomite.

In their study of dolomitization by ground water,
Hanshaw, et al. (1971) state that the Mg/Ca ratio in aquifer
water has low magnitude, where the water is undersaturated
with respect to both calcite and dolomite. With time and
length of travel path in the system, the water increases
systematically in Mg/Ca ratio, then dolomite crystals will
form. Because of the limited amount of magnesium available
from the solution of magnesium calcite and dolomite in the
zone of active fluid circulation, they maintain that only
localized dolomitization can occur.

The source of these dolomitizing fluids necessary to

49

produce secondary, post diagenetic dolomite could be of
artesian origin from outcrops off of the Wisconsin Arch
(Figure 2). The high magnesium concentration in the ground-
water develops by its movement along the bedding planes of
Lower Ordovician (i.e. Pairie du Chien Group) and Upper Cam-
brian dolomitic formations and may have migrated upwards
through fault and fracture systems, dolomitizing the Tra-
verse Limestone, among other susceptible formations.

Hydrocarbon production in stratigraphic sections of
the Middle Ordovician and the Middle Devonian are primarily
located in the south and southwest areas of Michigan (Fig-
ure 5). Newhart (1976) and earlier workers have postulated
for Ordovician fields, and Runyon (1976) for Traverse fields,
that magnesium-rich waters ascended fracture systems and
were dammed by an impervious seal above, the Utica Shale in
the former and the shale-rich Traverse Formation and/or the
Antrim Shale in the latter. The fact that the percent dolo-
mite in the Traverse Limestone of the Walker Field has a
relatively higher at or near the top of the limestone inter-
val beneath the limy shale of the Traverse Formation (Fig-
ures 10 and 11), indicates these shaley beds might have act-
ed as dams to the upward percolating water.

Another possible explanation for the vertical dolo-
mitization patterns observed in the upper portion of the
Traverse Limestone could be an environmental buildup that
allowed increasing dolomitization of the carbonate sediments

to occur. The slow development of a shallow lagoonal or

50

sabkha environment, for example, could be reflected in the
vertical dolomitization patterns, which demonstrate an in-
crease from low dolomite percent values in the lower depth
intervals within the Traverse Limestone to significantly
higher dolomite percent values at or near the top of the
Traverse Limestone. These higher dolomitization values at
or near the top of the Traverse Limestone might indicate the
presence of a carbonate depositional environment that was
more susceptible to early diagenetic dolomite replacement
than earlier environmental conditions represented by dolo-
mite percent values of the lower depth intervals within the
Traverse Limestone.

A high amount of dolomite along the west side of
Michigan in the Traverse Group has been noted by Gardener
(1974). Others, such as Hake and Maebius (1938) indicate
that various counties on the west side of Michigan contain a
higher amount of dolomite than usual. Regional dolomitiza-
tion of carbonate facies in western Michigan is suggested in
the studies by Syrjamaki, 1977, Lower Ordovician; Newhart,
1976, Middle Ordovician: and Runyon, 1976, Middle Devonian.
Some interesting parallels can be drawn between their res—
pective studies. Stratigraphic sections from each of these
studies demonstrate the same high regional dolomite trend in
a north-south orientation, along western Michigan, indica-
ting a possible close relationship to the Wisconsin Arch
during Ordovician and possibly Devonian time. As regional

dolomite content may indicate a shallow, near—shore

 

51
environment (Prouty, 1946), the presence of a high amount of
dolomite in this north-south trend in western Michigan sug-
gests the possibility that the Wisconsin Arch might have
been high and broad enough to cause shallowing of the Tra-
verse seas along it.

Much of the upper Traverse Limestone interval of the
Walker Field is composed of crystalline dolomitized lime-
stones and calcic dolomites with associated evaporites (gyp-
sum). The occurrence of crystalline dolomitized carbonate
rock, the general lack of correlation between dolomite val-
ues of these carbonate rocks and the field structure, the
the significant presence of evaporites in this stratigraphic
interval, and the regional dolomite trends through the area
of study tend to support the idea of early diagenetic dolo—
mitization of some of the Traverse carbonate sediments.

Some of the dolomitization patterns observed from
isodolic maps of the field could possibly be related to an
early diagenetic dolomitization process, probably penecon-
temporaneous with sedimentation.

Adams and Rhodes (1960), Deffeyes, et al. (1965),
and Illing, et al. (1965) have provided a dolomitization
theory to explain early diagenetic replacement based on the
development of Mg-rich brines through evaporation. These
authors have proposed that dense saline brines, whose Mg/Ca
ratios have been raised by the loss of Ca through evapora-
tive precipitation of gypsum and anhydrite in tidal flats,

ponds, and supratidal areas (sabkhas), have migrated

52
regularly down through lime sediment, dolomitizing it (evap-
orative reflux).

Folk and Land (1975) state that an important way to
precipitate dolomite is to dilute sea water or sabkha-evap-
oritic water with fresh water. Dilution allows the Mg/Ca
ratio to remain very high, but slows the crystallization
rate and reduces the concentration of competing ions. There
are two ideal sites where such a mixing mechanism can take
place. One site is floodable sabkhas or inundatable shallow
lagoons where the salinity undergoes rapid fluctuation be-
tween hypersaline and nearly fresh water conditions. Anoth-
er important site is the subsurface zone where sea water or
evaporitic waters come into contact with a wedge or lens of
meteoric water and salinity reduction occurs. In both of
the above cases Mg is supplied by saline waters, but pre-
cipitation is permitted only by dilution with fresh water.
Studies by Land (1973), Badiozamani (1973), and Land, et al.
(1975) indicate that the freshwater phreatic (water table)
zone, in places where some slight mixing with sea water
occurs, may be an important zone of dolomitization.

The Dorag dolomitization model (Ordovician of Wis-
consin) of Badiozamani (1973) illustrates the concept that
saturation with respect to dolomite increases continuously
with increasing sea water added to phreatic water. He cal-
culated that in brackish water ”in the range of 5—30% sea
water, the solution is undersaturated with respect to cal-

cite and many times supersaturated with respect to

53

dolomite." His proposed model necessitates a continuous
supply of Mg derived from sea water and mixing with meteoric
water during constant fluctuations of sea level. During
emergence, the interface where the phreatic lens of fresh
water impinges on underlying marine or saline connate water
would be a dolomitizing zone; this front could pass through
a considerable thickness of sediment as sea level drops.
The same conditions would occur during marine transgression.
In support of the idea of regional dolomitization of
Traverse Group sediments in western Michigan, several wri-
ters have noted the existence of a structural barrier in the
western Michigan area. In postulating the barrier's exis-
tence during Traverse Group time, Jodry (1957) cites as evi-
dence the presence of Traverse structural contour highs,
high dolomite and evaporite content to the west of it, reef
development abreast of it (Paris Oil Field), and a litho-
facies change from a lagoonal environment on the west side
of the barrier to an open sea environment east of the bar-
rier. As additional evidence to delineate this barrier,
Jodry utilized a regional gravity map of Michigan by Logue
(Tulsa Geological Society Digest, volume 18, 1950). The
map shows the major regional gravity anamoly in Michigan to
lie along the axis of the postulated West Michigan "Barrier"
(Figure 16). Jodry further states that by projecting the
barrier from areas of better control, it appears to pass
directly through the Walker-Wyoming Park fields. Gardener
(1974), in his Middle Devonian study of the Michigan Basin,

54

I—ISAOIIID—V‘Ij

_.,-

flit—I" 7
CI_ .

"sfuqsslpu

L!!!
37 (ill.

CAIADA

‘T.JOI!’N III-OI

9 I '2 II."-
I:::==:==

Gardener's Barrier Axis = -— -— ——
Jodry’s Barrier Axis = -—-—-——
Runyon's Barrier Axis =

 

Figure 16. West Michigan Barrier Axes

55

indicates a linear biohermal and biostromal development
along this West Michigan Barrier (Figure 16). Runyon (1976)
suggests that the lack of clastics on the west side of Mich-
igan during Traverse time indicates that the barrier was
probably a physical barrier with respect to currents (Fig-
ure 16).

Gardener (1974), on a common association of dolomite
below anhydrite beds, suggests that the Deffeyes et al.
evaporative reflux model could explain the diagenetic ori-
gin of these sediments in the lagoonal area. Runyon (1976)
believes a evaporative-seepage reflux dolomitization model
helps to explain the relationship of the barrier to the
limestone, dolomite, and evaporite trends observed in the
western part of the Basin during Traverse time.

The Walker Field could possibly be a part of this
hypothetical barrier-backwater lagoonal system. The re-
stricted nature of the waters west of this hypothetical bar-
rier could have developed a highly saline environment favor-
able for the occurrence of early diagenetic dolomitization.
High salinity levels would be enhanced during periods of
slight regression, where the water level in the lagoonal
area would be lowered and possibly favor the deposition of
evaporites. Periodic flushing of these marine saline waters
with fresh water (i.e. tropical rainfall) would lower sali-
nity but maintain a high Mg/Ca ratio that would be conducive
to dolomitization of carbonate sediments. The restricted

nature of this lagoonal area could have been augmented by

56

the presence of the Wisconsin Arch to the west (Figure 2).

Due to the absence of core samples from the upper
Traverse Limestone of the Walker Oil Field, there was no
direct petrographic evidence available with which to postu—
late which dolomitization process (early diagenetic or epi-
genetic) was primarily responsible for the development of
porosity and permeability in the Traverse Limestone pay
zone(s). Petrographic analysis of the total carbonate rock
fabric is necessary to successfully attempt the determina—
tion of the timing of dolomite replacement and its timing
relative to other diagenetic events that could have occur-
red, such as anhydrite replacement, silicification, and
calcite cementation(s).

Utilizing evidence compiled during this study, it
appears that early diagenetic dolomitization occurred pene-
contemporaneously with the deposition of the Traverse Lime-
stone. Secondary, post-diagenetic dolomitization of por-
tions of the Traverse Limestone could possibly have occurred
contemporaneously with or after Basin faulting during post-
Osagean-Mississippian time caused by shearing stresses from

the east.

CONCLUSIONS

From the analytical data obtained from the Middle

Devonian
be drawn:

(1)

(2)

(3)

(4)

(5)

Traverse Limestone rocks, certain conclusions can

The highest values of dolomite percent were found
at or near the top of the Traverse Limestone.

There is a general correlation between the dolomi-
tization patterns and the structural configuration
of the Traverse Limestone interval in the Walker
Field.

A few high dolomite percentage value locations
occur outside of the fold closure area of the
Walker Field and therefore are likely located on
faults or fractures where epigenetic dolomitization
has occurred.

Widespread, crystalline dolomitic limestone is
associated with significant amounts of gypsum.

This type of dolomite is probably the result of
early diagenetic dolomitization and is likely pene-
contemporaneous with sedimentation.

Folding, fracturing, and solution activity are

the major causes for the secondary porosity in the

pay zone(s) of the Traverse Limestone of the Walker

57

I.. .. Let-

IL .rl.‘

l!

 

 

 

(6)

(7)

(8)

58

Field.

Dolomite percentage determinations can be helpful
in detecting fault traces in folded structures in
the Traverse Limestone that may otherwise go unde-
tected.

There appears to be a good correlation between
faults and folds in the Traverse Limestone of the
Walker Oil Field, and the relationship is probably
a "cause and effect" relationship.

The carbonate and evaporitic facies of the upper
Traverse Limestone in the Walker Field appear to
be related in some way to the hypothesized West

Michigan Barrier.

BIBLIOGRAPHY

BIBLIOGRAPHY

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60

Egleston, D. C., 1958, Relationship of the Magnesium/Calcium
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Ells, G. D., 1969, Architecture of the Michigan Basin:
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61

Gustafson, W., 1960, Structure and Stratigraphy of the Tra-
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62

Kutsykovich, M. B., 1971, Roentgen-Diffractometric Method of
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64

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APPENDICES

APPENDIX I

SAMPLE WELL DESCRIPTIONS

APPENDIX I

SAMPLE WELL DESCRIPTIONS

 

Well Name: R. Terpstra No. 1
Location: NW-NE-NE Sec. 15, T7N-R13W
Permit No. 8418

Elevation: 665 feet above sea level

Traverse Formation

fib, pyr I52); tr sh, bl gn: tr bent.
1850-55 LS, shy. 1t gy-gy. Vf Xllt £08 (95%); gypt
gy brn, fib (5%): tr pyr.
1855-62 Ls, shy, gy, vf xll, sl pyr.
1862-67 Ls, dol, gy, vf-f xll, fos (85%): gyp, wh-brn,

rthy-fib, tr cht, wh-lt gy, porcel: tr pyr.

Top of Traverse Limestone

1867-70 Dol, calc, buff-gy, f-m xll (85%); gyp, wh,
rthy-mas, spec: tr pyr; tr cht, wh, porcel.

1870-77 Dol, calc, buff-tan brn, f-m xll (60%); gyp,
wh-buff, mot, rthy-fib: tr sh, gy.

1877-82 Dol, , f-m xll (90%); gyp, wh, rthy-mas,
spec TIO%): tr cht, wh, porcel.

1882-86 Dol, gy-tan brn, f-m xll (50%): gyp, wh,

rthy-mas (50%).

65

66

Appendix I - Continued.

 

Well Name:
Location:

S. Kuiper No. 1
SE-SW-SW Sec. 25, T7N-R13W

Permit No. 6617

Elevation:

686 feet above sea level

Traverse Formation

1838-52

1852-57

1857-64
1864-72

Ls, shy, gy, vf xll (70%); gyp, gy-brn, mas-
fib, sft (30%).

Ls, shy, lt -gy, vf xll (80%): gyp, lt gy,
mas, sft (20% .

Ls, shy, lt gy, vf xll (99%); tr pyr.
Ls, shy, lt gy, vf xll (100%).

Top of Traverse Limestone

1873-79

1879-85

1885-92

Dol, buff, f-m xll (45%): gyp, dol, m-dk gy,
mas. spec (35%): sh. lmy. av (20%). tr pyr-
Gyp, wh-gy, spec (80%): ls, coralline, wh-
buff, f xll: tr pyr: tr cht, wh: tr qtz: clr,
f gr, subang: tr bent, gn gy.

Gyp, lmy, wh-buff, mas-fib, spec (95%): sh,
gn gy-dk gy (5%): tr ls, coralline, wh.

APPENDIX II

LIST OF WELLS USED IN STUDY

APPENDIX II

LIST OF WELLS USED IN STUDY

 

 

 

 

 

 

 

 

Well Permit Section Ground Traverse Traverse
No. No. Location Elev. Ls Top Ls Top
S.L. Datum
Ottawa County, Tallmadge Township, T7N,5R13W
Section 16
1 6801 SE-SE-SE 729 -1996 -1267
Section 15
2 8418 NW-NE-NE 665 -1867 -1202
3 9542 CE/2-SE-NE 677 -1871 -1194
4 9851 NE-SE-SE 683 -1867 -1184
5 7887 SW-SE-SE 667 -1850 -1183
Section 14
6 7699 NE-NE-SW 691 -1877 -1186
7 8287 NW-NW-SE 695 -1875 -1180
8 7695 SE-NW-SW 677 -1861 -1184
9 7318 SW-NE-SW 665 -1848 -1183
10 7825 NE-SE-SW 688 -1863 -1175
11 8424 SW-SE-SW 693 -1870 -1177
12 7768 SE-SE-SW 692 -1865 -1173
13 7995 SE-SW-SE 691 -1861 -1170
Section 13
14 7533 SW-SW-SW 692 -1867 -1175
Section 23
15 8211 NW-NE-NW 695 -1864 -1169
16 7720 NE-NE-NW 691 -1856 -1165
17 7745 NW-NW-NE 694 -1850 -1156
18 7858 NW-NE-NE 684 -1835 -1151
19 7717 SE-NW-NW 695 -1866 -1171

67

68

 

 

 

 

 

Well Permit Section Ground Traverse Traverse

No. No. Location Elev. Ls Top Ls Top
S.L. Datum

Ottawa County,,Tallmadge Township, T7N, R13W

Section 23
20 7605 SW-NE-NW 694 -1858 -1164
21 7637 SE-NE-NW 693 -1855 -1162
22 7681 SW-NW-NE 694 -1846 -1152
23 7578 SE-NW-NE 699 -1854 -1155
24 7263 SW-NE-NE 693 -1856 -1163
25 7378 SE-NE-NE 692 -1854 -1162
26 7600 NE-SW-NW 695 -1853 -1158
27 7570 CN/2-SE-NW 697 -1850 -1153
28 7447 CN/2-SW-NE 695 -1854 -1159
29 7418 NW-SE-NE 694 -1858 -1164
30 7412 NE-SE-SE 699 -1862 -1163
31 7752 CW/2-SE-NW 697 -1853 -1156
32 7411 CE/2-SE-NW 694 -1844 —1150
33 7630 SW-SW-NE 692 -1850 -1158
34 7631 SE—SW-NE 690 -1850 -1160
35 7569 SW-SE-NE 688 -1852 -1164
36 7518 SE-SE-NE 702 -1863 -1161
37 7581 S/2-S/2-SE-NW 695 -1850 -1155
38 7649 NW-NE-SW 688 -1863 -1175
39 7579 NE-NE-SW 694 -1858 -1164
40 7650 NW-NW-SE 694 -1862 -1168
41 7552 NE-NW-SE 691 -1853 -1162
42 7329 NE-NE-SE 709 -1870 -1161
43 8348 SW-NW-SE 693 -1852 -1159
44 7469 SE-NW-SE 691 -1849 -1158
45 7422 SW-NE-SE 697 -1861 -1164
46 7328 SE-NE-SE 711 -1870 -1159
47 8522 NE-SE-SW 689 -1850 -1161
48 7932 NW-SW-SE 693 ~1845 -1153
49 7367 NW-SE-SE 703 -1862 -1159
50 7241 NE-SE-SE 714 -1871 -1157
51 8131 SE-SE-SW 687 -1846 -1159
52 7764 SW-SW-SE 691 -1845 -1154
53 7677 SE-SW-SE 690 -1843 -1153
54 7239 SW-SE-SE 699 -1863 -1164
55 7240 SE-SE-SE 716 -1877 -1161

Section 24
56 7601 SW-NW-NW 714 -1873 -1159
57 7265 SW-NE-NW 746 -1919 -1173
58 7452 NW-SW-NW 719 -1881 -1162
59 7214 NW-SW-NE 752 -1923 -1171
60 7532 SW-SW-NW 717 -1885 -1168

69

 

 

 

 

 

 

Well Permit Section Ground Traverse Traverse

No. No. Location Elev. Ls Top Ls Top
S.L. Datum

Ottawa County, Tallmadge Township, T7N, R13W

Section 24
61 7291 SE-SW-NW 733 -1901 -1168
62 7051 SW-SE-NW 754 -1913 -1159
63 7285 SW-SW-NE 754 -1918 -1164
64 7215 cw/2 757 -1916 -1159
65 7203 SW-NW-SW 717 -1884 -1167
66 7204 SE-NW-SW 720 -1891 -1171
67 7302 SE-NE-SW 720 -1881 -1161
68 8151 SE-NE-SE 739 -1909 -1170
69 7202 NW-SW-SW 712 -1880 -1168
70 7170 NE-SW-SW 705 -1873 -1168
71 7266 NW-SE-SW 705 -1863 -1158
72 7423 NE-SW-SE 754 -1916 -1162
73 7762 NE-SE-SE 740 -1905 -1165
74 7206 SW-SW-SW 710 -1875 -1165
75 7151 SE-SW-SW 698 -1862 -1164
76 7183 SE-SE-SW 711 -1868 -1157
77 7252 SW-SW-SE 726 -1885 -1159
78 7074 SE-SW-SE 748 -1908 -1160
79 7150 SW-SE-SE 748 -1910 -1162
Section 28
80 22008 SE-NE-NE 718 -1910 -1192
81 22020 CE/2-SW-NE 712 -1901 -1189
82 23963 SE-SE-NW 701 -1904 -1203
83 22202 SW-SW-NE 706 -1901 -1195
84 6317 SW-SE-NE 736 -1910 -1174
85 19562 NE-NW-SE 724 -1904 -1180
86 22829 CW/2-NW-SE 710 -1888 -1178
87 23042 SE-NE-SW 671 -1869 -1198
88 22612 NW-SW-SE 715 -1887 -1172
89 7331 NW-SE-SE 686 -1852 -1166
90 22389 CE/2-SE-SE 673 -1836 -1163
91 24122 SE-SE-SW 641 -1842 -1201
92 7730 SW-SW-SE 688 -1866 -1178
93 8581 SW-SE-SE 673 -1833 -1160

Section 27

94 23028 NE-NW-NW 622 -1806 -1184
95 22947 NE-NE-NW _648 -1832 -1184
96 2187 NE-NW-NE 679 -1860 -1181
97 20161 NE-NE-NE 672 -1846 -1174
98 22105 SW-NW-NW 699 -1887 -1188

70

 

 

 

 

 

Well Permit Section Ground Traverse Traverse
No. No. Location Elev. Ls Top Ls Top
S.L. Datum

Ottawa County, Tallmadge Township, T7N, R13W

Section 27

99 6675 SE-NE-NW 612 -1796 -1184
100 22120 SE-NW-NE 663 -1843 -1180
101 20350 SE-NE-NE 677 -1850 -1173
102 22091 NE-SW-NW 670 -1853 -1183
103 20218 NE-SW-NE 677 -1859 -1182
104 20432 NE-SE-NE 666 -1849 -1183
105 22572 SW-SE-NW 617 -1794 -1177
106 22689 SE-SE-NW 639 -1815 -1176
107 19852 SW-SW—NE 612 -1789 -1177
108 22979 SW-SE-NE 669 -1848 -1179
109 23014 SE-SE-NE 655 -1842 -1187
110 19668 NE-NW-SW 682 -1854 -1172
111 19449 NW-NE-SW 628 -1799 -1171
112 19970 NW-NW-SE 610 -1787 -1177
113 23055 NW-NE-SE 624 -1813 -1189
114 19559 SE-NW-SW 619 -1792 -1173
115 19492 SW-NE-SW 605 -1776 -1171
116 21937 SE-NW-SE 679 -1869 -1190
117 21212 NW-SE-SW 649 -1828 -1179
118 21361 NW-SE-SE 672 -1862 -1190
119 8140 SW-SW-SW 606 -1766 -1160
120 8677 SE-SW-SW 636 -1809 -1173
121 6293 SE-SE-SW 661 -1834 -1173
122 7165 SE-SW-SE 717 -1897 -1180
123 21263 SW-SE-SE 682 -1866 -1184
Section 26

124 20280 NW—NW-NW 676 -1849 -1173
125 8409 NE-NE-NW 685 -1842 -1157
126 7535 CN/2-NW-NE 688 -1847 -1 159
127 7171 NE-NE-NE 699 -1857 -1158
128 7292 CN/2-CN/2-NE 689 -1848 -1 159
129 20489 SE-NW-NW 676 -1846 -1170
130 8629 SE-NE-NW 682 -1840 -1158
131 15831 SW-NW-NE 685 -1845 -1160
132 7262 SW-NE-NE 685 -1841 -1156
133 7172 SE-NE-NE 689 -1845 -1156
134 22262 NW-SE-NW 680 -1860 -1180
135 15532 NE-SE-NE 682 -1850 -1168
136 6998 NE-NW-SW 643 -1845 -1202
137 7175 NE-NE-SE 665 -1870 -1205
138 20567 SE-SE-SW 671 -1872 -1201

71

 

 

 

 

 

Well Permit Section Ground Traverse Traverse
No. No. Location Elev. Ls Top Ls Top
S.L. Datum
Ottawa County4 Tallmadge TownshipLMTZNJ R13W
Section 25
139 7142 NW-NW-NW 702 -1867 -1165
140 7235 NE-NW-NW 701 ~1861 -1160
141 7277 NW-NE-NW 697 -1852 -1155
142 7859 NE-NW-NW 702 -1860 -1158
143 7181 NW-NW-NE 710 -1863 -1153
144 7078 SW-NW-NW 688 -1851 -1163
145 7207 SW-NE-NW 680 -1842 -1162
146 7155 SE-NE-NW 697 -1852 —1155
147 7140 SW-NW-NE 682 -1837 -1155
148 6937 SW-NE-NE 734 -1892 -1158
149 6938 SE-NE-NE 735 ~1890 -1155
150 7143 NW-SW-NW 687 -1862 -1175
151 7236 NE-SW-NW 672 -1846 -1174
152 7276 NW-SE-NW 681 -1845 -1164
153 7085 NE-SE-NW 685 -1848 -1163
154 6979 NE-SW-NE 709 -1858 -1149
155 6861 NW-SE-NE 717 -1869 -1152
156 6860 NE-SE-NE 731 -1876 -1145
157 7397 SW—SW-NW 666 —1850 -1184
158 7237 SE-SW-NW 666 -1844 -1178
159 7121 SW-SE-NW 668 -1840 -1172
160 6895 SE-SE-NW 689 -1848 -1159
161 6981 SW-SW-NE 676 -1833 -1157
162 6845 SE—SW-NE 701 -1851 -1150
163 7157 NW-NE-SW 680 -1855 -1175
164 6741 NE-Nw-SE 692 -1849 -1157
165 6953 CW/2-NE-SE 694 -1845 -1151
166 6106 CE/2-NE-SE 711 -1854 -1193
167 6942 SE—NE-SW 682 -1845 -1163
168 6795 SE-NW-SE 688 -1851 -1163
169 6949 NE-SW—SE 686 -1846 -1160
170 6781 NW-SE-SE 680 -1835 —1155
171 6654 NE-SE-SE 699 -1848 -1149
172 6617 SE-sw-sw 686 -1873 -1187
173 7238 SW-SE-SW 670 -1860 -1190
174 6657 SW-SE-SE 680 -1853 -1173
175 6525 SE-SE-SE 674 -1833 -1159
Section 33
176 22063 NE-NW-NE 681 -1854 -1173
177 8232 NE—NE-NE 657 -1820 -1163
178 8360 SW—NE-NE 656 -1828 -1172 .
179 8340 SE-NE-NE 643 -1806 -1163

72

 

 

 

 

 

 

Well Permit Section Ground Traverse Traverse
No. No. Location Elev. Ls Top Ls Top
S.L. Datum
Ottawa County, Tallmadge TownshipJ TZN4 R13W
Section_33
180 8342 NE-SE-NE 635 -1810 -1175
181 22989 W/Z-SE-NE 621 -1802 -1181
182 22827 SE-SW-NE 617 -1820 -1203
183 21891 NE-NE-SE 618 -1815 -1197
Sectiong34
184 8209 NW-NW-NW 602 -1764 -1162
185 8313 NE-NW-NW 632 -1800 -1168
186 8139 NW-NE-NW 638 -1806 -1168
187 21187 NE-NW-NE 678 -1848 -1170
188 22102 NE-NE-NE 663 -1849 -1186
189 8189 SW-NW-NW 597 -1763 -1166
190 8201 SE-NW-NW 630 -1793 —1163
191 8071 SW-NE-NW 663 -1825 -1162
192 8391 SE-NE—NW 679 -1846 -1167
193 8458 SW-NW-NE 672 -1844 -1172
194 20864 SW-NE-NE 696 -1876 -1180
195 20780 SE-NE-NE 679 -1870 -1191
196 8273 NW-SW-NW 622 -1789 -1167
197 8093 NE-SW-NW 625 -1785 -1160
198 8002 NW-SE-NW 647 -1807 -1160
199 7854 NE-SE-NW 675 -1840 -1165
200 7694 NW-SW-NE 686 -1857 -1171
201 21238 NE-SW-NE 713 -1888 -1175
202 8338 SW-SW-NW 604 -1772 -1168
203 8374 SE-SW-NW 635 -1795 -1160
204 8339 SW-SE-NW 650 -1817 -1167
205 7933 SW-SW-NE 710 -1888 -1178
206 21375 SE-SW-NE 689 -1871 -1182
207 8481 NE-NW-SW 639 -1811 -1172
208 8676 NW-NE-SW 676 -1852 -1176
209 23515 NE-NW-SE 674 -1860 -1186
210 21814 SW-NE-SW 617 -1796 -1179
211 21569 SW-NW-SE 609 -1793 -1184
212 8425 SE-NE-SE 610 —1806 -1196
Section<35
213 21314 SE-NE-NW 665 -1870 -1205
214 21152 SE-NW-NE 703 -1910 -1207
215 21399 SE-NE-NE 702 -1905 -1203
216 21084 NW-SW-NE 680 -1867 -1187
217 21335 NW-SE-NE 732 -1927 -1195

73

 

 

 

 

 

Well Permit Section Ground Traverse Traverse
No. No. Location Elev. Ls Top Ls Top
S.L. Datum
Ottawa County; Tallmadge Townshipi T7N, R13W
Section¥35
218 14981 SE-SW-NW 719 -1906 -1187
219 13537 SE-SE-NW 675 -1860 -1185
220 22701 SE-SE-NE 728 -1930 -1202
221 14990 NE-NW-SW 710 -1906 -1196
222 14826 NE-NE-SW 704 -1887 -1183
223 15096 NW-NW-SE 715 -1910 -1195
224 6625 NE-SE-SE 726 -1923 —1197
225 16289 SW-NE-SW 624 -1812 -1188
226 19268 SE-NW-SE 645 -1835 -1190
227 19469 SW-NE-SE 612 -1800 -1188
228 15581 NW-SE-SW 592 -1772 -1180
229 15567 NW-SW-SE 596 -1771 -1175
230 18083 NW-SE-SE 590 -1767 -1177
231 17949 NE-SE-SE 608 -1788 -1180
232 15642 SE-SE-SW 592 -1767 -1175
233 16969 SE-SW-SE 598 -1771 -1173
Section‘36
234 20614 NW-NW-NW 702 -1903 —1201
235 6624 NW-NE-NW 672 -1869 —1197
236 6016 NE-NW-NE 674 -1860 -1186
237 7062 NE-NE-NE 679 -1845 -1166
238 21324 SE-NW-NE 682 -1874 -1192
239 21515 SW-NE—NE 683 -1861 -1178
240 21182 SE-NE-NE 682 -1855 -1173
241 6647 NE-SE-NE 680 -1848 -1168
242 21795 SE-SW-NW 734 -1937 -1203
243 23131 SE-SE-NW 714 -1910 -1196
244 21981 NW-NW-SW 719 -1919 -1200
245 22976 NW-NE-SE 681 -1861 -1180
246 18038 SW-NW-SW 723 -1908 -1185
247 21358 NW-SW-SE 703 -1892 -1189
248 21179 NW-SE-SE 689 -1878 -1189
249 22943 NE-SE-SE 685 -1871 -1186
250 22860 C/SE-SW 720 -1896 -1176
251 18468 SW-SW—SW 619 -1789 -1170
252 21248 SE-SW-SE 703 -1886 -1183
253 21092 SE-SE-SE 687 -1869 —1182

74

 

 

 

 

 

 

 

 

 

Well Permit Section Ground Traverse Traverse
No. No. Location Elev. Ls Top Ls Top
S.L. Datum
Ottawa County, Georgetown TownshipJ T6N._R13W
Section 2
254 7959 NE—NW-NW 603 -1777 -1174
255 7871 NW-NE—NW 596 -1771 -1175
256 8018 NE-NE-NW 606 -1772 -1166
257 8329 NW-NW-NE 595 -1761 -1166
258 8683 SW-NW—NW 600 -1794 -1195
259 8400 SW-NE-NW 607 -1774 -1167
260 8164 SE-NE—NW 597 -1763 -1166
261 8465 SE-NW-NE 607 —1776 -1169
262 8617 NW-SE-NW 595 -1774 -1179
Section 1
263 8639 SW-NE-NW 711 -1884 -1173
264 8369 NE-SE—NW 689 -1861 -1172
265 8430 NE-NE-SW 708 -1881 -1173
266 9901 CE/2-SE 677 -1853 -1176
267 8304 NE-SE-SW 695 -1868 -1173
Section 12
268 8542 NE-NE-NW 671 -1848 -1177
269 8447 NW-NW-NE 663 -1839 -1176
Kent Countyi_Walker Township, T7flJ R12W
Section 19
270 6282 SW-SW-NW 727 -1903 —1176
271 8419 NW-NW-SW 726 -1899 -1173
272 8535 SE-NW-SW 749 -1914 -1165
273 7930 NW-SW-SW 742 ~1905 -1163
274 7327 SW-SW-SW 737 -1894 -1157
275 7662 SE-SW-SW 742 -1900 -1158
276 6549 SE-SE-SE 727 -1908 -1181
Section 20
277 7268 NW-NE-SW 730 -1920 -1190
278 7565 SE-SW-SW 740 -1915 -1175
279 6841 SE-SE-SW 734 -1906 -1172
280 6894 SW-SE-SE 722 -1895 -1173

 

75

 

 

 

 

 

Well Permit Section Ground Traverse Traverse
No. No. Location Elev. Ls Top Ls Top
S.L. Datum
Kent County; Walker TownshipJ T7N57R12W
Section 30
281 6976 NW-NW-NW 739 —1895 —1156
282 6821 NW-NE-NW 739 -1903 -1164
283 6975 SW-NW-NW 736 -1899 -1163
284 7242 SW-NE-NW 741 -1909 -1168
285 7527 SE-NE-NE 722 -1894 -1172
286 6974 NW-SW-NW 737 -1890 -1153
287 6961 CN/2-SE-NW 736 -1898 -1162
288 6674 NW-SE-NE 730 -1895 -1165
289 7257 NE-SE-NE 735 —1901 -1166
290 6604 CW/2-SE-NW 737 -1892 -1155
291 6522 SW-SW-NW 732 -1874 -1142
292 6825 SE-SW-NW 722 -1873 -1151
293 6808 SE-SE-NW 725 —1883 -1158
294 6664 SE-SW-NE 732 -1890 -1158
295 6514 S/2-S/2-SE-NE 736 —1892 -1156
296 6780 NW-NW-SW 717 -1858 -1141
297 6820 NW-NE-SW 732 -1880 -1148
298 6667 NW-NW-SE 728 -1877 -1149
299 6753 NE-NW-SE 736 -1885 -1149
300 6694 NW-NE-SE 733 -1885 -1152
301 6703 NE-NE-SE 707 -1857 -1150
302 6663 SW-NW-SW 703 -1845 -1142
303 6598 SW-NW-SE 740 -1885 -1145
304 6497 SE-NW-SE 728 -1872 -1144
305 6671 SE-NE-SE 726 -1867 —1141
306 6590 NW-SE-SW 702 -1850 -1148
307 6477 NE-SE-SW 704 -1846 -1142
308 6480 W/Z-SW-SE 729 -1872 -1143
309 6917 SW-SW-SW 676 -1829 -1153
310 6698 SW-SE-SW 693 -1846 -1153
311 6593 SE-SE-SW 704 -1852 -1148
312 6496 SE-SE-SE 738 -1883 -1145
Section 29
313 7061 NW—NE-NW 731 -1899 —1168
314 7058 NE-NE-NW 722 -1888 -1166
315 7025 NE-NW-NE 742 -1910 -1168
316 6923 CW/2-NW—NE 727 -1892 -1165
317 8190 SE-NW-NW 739 -1906 -1167
318 7060 SW-NE-NW 716 -1878 -1162
319 6915 SW-NE-NE 726 -1897 -1171
320 7101 NW-SW-NW 727 -1885 —1158
321 7059 NW-SE-NW 707 —1863 -1156

76

 

 

 

 

 

 

Well Permit Section Ground Traverse Traverse
No. No. Location Elev. Ls Top Ls Top
S.L. Datum
Kent County, Walker Township, T7N,_R12W
Section 29
322 7023 NE-SW-NE 748 -1913 -1165
323 6888 SW-SW-NW 710 -1865 —1155
324 6930 SE-SW-NW 732 -1880 -1148
325 6765 SW—SE-NW 708 -1855 -1147
326 7021 SE-SE-NW 712 -1864 -1152
327 7264 SW-SW-NE 715 -1868 —1153
328 6967 SE-SW-NE 743 -1905 -1162
329 6834 NW-NW-SW 705 -1853 -1148
330 7127 NE-NE-SW 713 -1865 -1152
331 6929 NW-NW-SE 724 -1882 -1158
332 6735 SW-NW-SW 689 -1833 -1144
333 7091 SE—NW-SW 728 -1874 -1146
334 6914 SW-NE-SW 733 -1881 -1148
335 7146 SW-NW-SE 741 -1896 -1154
336 8116 SW-NE-SE 746 —1904 -1158
337 6746 NW-SW-SW 687 -1835 -1148
338 6833 NW-SE-SW 730 -1878 -1148
339 6851 NE-SW-SE 747 -1898 -1151
340 7219 NE-SE-SE 753 -1905 -1152
341 6759 SE-SW-SW 691 -1839 -1148
342 7182 SW-SE-SW 729 -1876 —1150
343 7336 SE—SE-SW 707 -1856 -1149
344 6600 SE-SW—SE 742 -1891 -1149
345 6843 SE-SE-SE 759 -1909 -1150
Section 28
346 6971 SW-NW-NE 743 -1923 -1180
347 7445 SE-SE-NW 750 -1920 —1170
348 16114 NE-NW-SE 733 -1902 -1169
349 7330 NW-NE-SE 731 -1902 -1171
350' 6873 SW-NW-SW 747 -1905 -1158
351 7413 NW-SW-SW 746 -1899 -1153
352 7249 CN/Z-SW-SE 749 -1905 -1156
353 7065 SE-SW-SW 739 -1888 -1149
354 7064 CS/2-SE-SW 754 -1905 -1151
355 8162 CS/2-SW-SE 735 -1892 -1157
Section 27
356 7459 SW-NW-NW 702 -1886 -1184
357 7456 SE-NE-NW 758 -1946 -1188
358 7451 SW-SW-NW 699 -1879 -1180
359 5936 SE-SW-SW 704 -1876 —1172

77

 

 

 

 

 

Well Permit Section Ground Traverse Traverse
No. No. Location Elev. Ls Top Ls Top
S.L. Datum
Kent County, Walker Townshig,¥T7N, R12W
Section_31
360 6523 NE-NW-NW 675 -1828 -1153
361 6459 NE-NE-NW 690 -1838 -1148
362 6506 NW—NW-NE 714 -1860 —1146
363 6488 NE-NW-NE 712 -1857 -1145
364 6476 NW-NE-NE 714 -1860 -1146
365 6850 NE-NE-NE 732 —1881 —1149
366 7243 SW-NW-NW 679 -1838 -1159
367 6589 SE-NE-NW 704 -1857 -1153
368 7588 SW-NE-NE 676 -1830 -1154
369 6995 CN/2-SE-NW 681 -1841 -1160
370 6731 NW-SW-NE 679 -1847 -1168
371 6479 NW-SE-NE 675 -1833 -1158
372 6773 S/2-N/2-SE-NW 685 -1857 -1172
373 6513 SE-SW-NE 701 -1873 -1172
374 6137 NE-NE-SW 675 —1863 -1173
375 8459 NE-NE-SE 720 -1887 -1167
376 6788 NW-SW-SE 695 —1870 -1175
377 7352 SE-SE-SE 672 -1837 -1165
Section532
378 6789 NW-NW-NW 730 -1879 -1149
379 6997 NE-NW-NW 711 -1866 -1155
380 6475 NW-NE-NW 713 -1865 -1152
381 6886 NE-NE-NW 727 -1879 -1152
382 7553 NW-NW-NE 721 -1869 -1148
383 7689 NW-NE-NE 735 -1880 -1145
384 6483 SW-NW—NW 700 —1855 ~1155
385 7160 SE-NE-NW 727 -1876 -1149
386 7159 SW-NE-NE 756 -1898 —1142
387 7033 NE-SE—NW 725 -1873 ~1148
388 7037 SE-SW-SW 663 -1821 -1158
389 6056 SW-SE-NW 680 -1835 -1155
390 6478 SE-SW-NE 690 -1838 -1148
391 7426 NW-NE-SW 700 -1855 -1155
392 7295 NE-NE-SW 706 —1860 -1154
393 7057 NW-NW-SE 715 -1868 -1153
394 7810 NE-NE-SE 703 -1853 -1150
395 7145 SE-NE-SW 669 -1817 -1148
396 7820 SE-NW-SE 659 -1804 -1145
397 7763 SE-NE-SE 626 -1769 -1143
398 5937 NE-SW-SW 644 -1794 -1150
399 5858 NE-SW-SE 653 -1796 -1143
400 7316 SW-SW-SW 716 —1874 ~1158

78

 

 

 

 

 

Well Permit Section Ground Traverse Traverse
.No. No. Location Elev. Ls Top Ls Top
S.L. Datum
Kent County, Walker Township, TZN,_312W
Section 32
401 5207 SE-SW-SW 702 -1860 -1158
402 5725 SW-SE-SW 658 -1814 -1156
403 5785 SE—SE-SW 647 -1793 -1146
404 6069 SE-SW-SE 619 -1763 -1144
405 5998 SW-SE-SE 607 -1750 -1143
406 6097 SE-SE-SE 610 -1752 -1142
Section 33
407 7020 NW-NW-NW 738 -1886 -1148
408 7141 NE-NW-NW 702 -1850 -1148
409 7807 CN/2-NE-NW 756 -1906 -1150
410 6940 SW-NW-NW 721 -1870 -1149
411 6987 SW-NE-NW 703 —1855 -1152
412 7003 SE-NE-NW 744 -1902 -1158
413 6166 NE-SW-NW 633 -1782 -1149
414 7144 NW-SE-NW 662 -1815 -1153
415 7004 NE-SE-NW 710 -1868 -1158
416 6495 SW-SW-NW 711 -1860 —1149
417 7335 SW-SE-NW 720 -1866 -1146
418 6842 SE-SE—NW 676 -1820 -1144
419 6386 SW-SW-NE 754 -1910 -1156
420 7558 SE-SW-NE 764 -1920 -1156
421 7218 SW-SE-NE 693 -1856 -1163
422 7290 NW-NW-SW 686 -1829 -1143
423 7153 NE-NW-SW 672 -1819 -1147
424 6554 NE-NE-SW 724 -1868 -1144
425 6760 NW-NW-SE 741 -1886 —1145
426 7571 NW-NE-SE 682 —1833 -1151
427 7480 NE-NE—SE 688 -1842 -1154
428 6292 SE-NW-SW 617 -1764 -1147
429 7317 SE-NW-SE 695 -1840 -1145
430 7960 NW-SW-SE 609 -1753 -1144
431 6177 NE-SW-SW 608 -1750 -1142
432 6190 NE-NE-SW 600 -1738 -1138
433 6052 NW-SW-SE 606 -1744 -1138
434 7479 NE-SE-SE 725 -1874 -1149
435 7323 SW-SE-SW 607 -1748 -1141
436 6468 SW-SE-SE 603 -1743 -1140
437 7478 SE-SE—SE 602 -1752 -1150

79

 

 

 

 

 

 

 

 

Well Permit Section Ground Traverse Traverse
No. No. Location Elev. Ls Top Ls Top
S.L. Datum
Kent County, Walker Township, T7N, R12W
Section 34
438 12899 NE-SE-NW 762 -1924 -1162
439 6973 SW-SW—NW 655 -1813 -1158
440 7072 SW-SE-NW 696 -1856 -1160
441 6807 SE-SE-NW 741 -1904 -1163
442 7269 NW-NE-SE 595 -1771 ~1176
443 7658 SW-NW-SW 622 -1775 -1153
444 7404 NW-SW—SW 603 -1755 -1152
445 6939 NW-SE-SW 598 -1753 -1155
446 7659 SE-SW-SW 605 -1757 -1152
Sectionp35
447 7015 NW-SW-NW 597 -1781 -1152
Kent County, Wyoming Township, T6NJ R12W
Section 6
448 21386 NE-NW-NW 682 -1866 -1184
449 22479 N/2-NE-NW 667 -1849 -1182
450 6339 NE-NE-NE 697 -1863 -1166
451 21741 SE-NW-NE 662 -1837 -1162
452 6053 SW-NE-NE 663 -1825 -1162
453 7580 SE-SE-NE 697 -1865 -1168
454 13042 NW-SW-NE 662 -1842 -1180
455 19890 NE-SW-NE 658 -1834 -1176
456 13040 SE-SW-NW 672 -1850 -1178
457 12560 NW—NW-SE 661 -1840 -1179
458 13157 SE-NE—SW 669 -1845 -1176
459 12805 SE-NW-SE 712 -1889 -1177
460 21658 SE-NE-SE 700 -1884 -1184
461 9611 CW/Z—SW 672 -1831 -1159
462 13231 NW-SE-SW 666 -1831 -1165
463 21542 CSW/4-SE 715 -1899 -1184
464 21584 SW-SW-SW 659 -1820 -1161
465 21538 SW-SE-SE 729- -1914 -1185
Section_5
466 7035 NW-NW-NW 721 -1880 -1159
467 6033 NW-NE-NW 630 -1782 —1152
468 5433 NE-NE-NW 707 -1861 -1154
469 6062 NW—NW-NE 614 -1765 -1151
470 5880 NW-NE-NE 602 -1748 -1146

80

 

 

 

 

 

Well Permit Section Ground Traverse Traverse
No. No. Location Elev. Ls Top Ls Top
S.L. Datum
Kent County, Wyoming Township, T6N, R12W
Section 5
471 6425 NE-NE—NE 603 -1745 —1142
472 6018 SE-NW-NW 665 -1825 -1160
473 6188 SE-NE-NW 612 -1770 -1158
474 6187 SE-NW-NE 605 -1753 -1148
475 6122 SW-NE-NE 605 -1752 -1147
476 22030 NW-SW-NW 702 -1870 -1168
477 6450 NW-SE-NW 626 -1787 -1161
478 6211 NW-SW-NE 605 -1759 -1154
479 5933 E/2-SE-NW 611 -1768 -1157
480 21876 SE-SW-NW 660 -1830 -1170
481 22357 SW-SW-NE 604 ~1758 -1154
482 6315 SW-SE-NE 614 -1768 -1154
483 6316 SE-SE-NE 617 -1767 -1150
484 21819 NW-NE-SW 622 -1799 -1177
485 8593 NE-NE-SW 603 -1777 -1174
486 7178 NW-NW-SE 600 -1771 -1171
487 5923 NE-NW-SE 618 -1788 -117O
488 13698 cw/2-sw-sw 636 -1820 —1184
489 23988 SE-SW-SE 598 —1780 -1182
490 23192 CS/2-SE-SE 597 —1777 -1180
Section 4
491 6170 NE-NE-NW 599 -1741 -1142
492 6530 NW-NW-NE 598 -1738 -1140
493 6920 NW-NE-NE 597 -1735 -1138
494 7247 NE—NE-NE 595 -1744 -1149
495 6309 SW-NW-NW 608 -1754 -1146
496 6341 SE-NW-NW 608 -1752 -1144
497 6696 - SW-NE-NE 596 -1738 -1142
498 7135 SE-NE-NE 595 -1737 -1142
499 6138 NW-SW-NW 611 -1758 -1147
500 6368 NE-SE-NW 615 -1760 -1145
501 6583 NE-SW-NE 600 -1740 —1140
502 6695 NE-SE—NE 598 -1743 -1145
. 503 6449 SW-SW-NW 623 -1772 -1149
504 6376 SE-SW-NW 620 -1770 -1150
505 6702 SW-SW-NE 597 -1741 -1144
506 6562 SW-SE-NE 593 -1738 -1145
507 6673 NW-NW—SW 625 ~1790 -1165
508 6885 NE-NE-SW 594 -1740 -1146
509 6524 NE-NW-SE 601 -1748 -1147
510 6216 NE-NE-SE 595 -1743 -1148
511 6819 SE-NW-SW 596 -1754 ~1158

81

 

 

 

 

 

 

 

Well Permit Section Ground Traverse Traverse
No. No. Location Elev. Ls Top Ls Top
S.L. Datum
Kent County, Wyoming Township, T6N, R12W
Section 4
512 6378 SW-NE-SW 593 -1748 -1155
513 6806 SE—NE—SW 597 -1746 -1149
514 6736 SE-NW-SE 598 -1750 -1152
515 6620 SE-NE-SE 602 -1753 -1151
516 6552 NW—SE-SW 593 -1753 -1160
517 6784 NW-SE-SE 599 -1757 -1158
518 6528 SE-SW-SW 595 -1764 -1169
Section_3
519 7437 NW-NW-NW 595 -1740 -1145
520 7347 SW-NW-NW 594 -1741 -1147
521 6630 SW-NW-NE 598 -1746 -1148
522 7546 SW-NE-NE 605 -1763 -1158
523 6717 NW-SW-NW 595 -1744 -1149
524 6582 NE-SE-NW 594 -1738 -1144
525 7537 NE-SW-NE 598 -1748 -1150
526 6631 SE-SW-NW 603 -1747 -1144
527 6466 SW-SE-NW 598 -1740 -1142
528 7484 SE-SE-NW 599 -1741 -1142
529 7005 SW-SE-NE 607 -1764 -1157
530 6912 NW-NE-SW 594 -1738 -1144
531 7197 NW-NW-SE 606 -1755 -1149
532 6714 SW-NW-SW 595 -1745 -1150
533 5004 SW-NE—SW 607 -1754 -1147
534 6494 SE-NE-SW 603 -1753 -1150
535 7425 SE-NW-SE 619 -1784 -1165
536 6924 NW-SW-SW 602 -1758 -1156
537 8854 NW-SE-SW 613 -1775 -1162
Section 2
538 6536 NE-NW-NE 604 -1786 -1162
539 6670 SW-NW-NW 614 -1780 -1166
540 7087 SE-NW-NW 608 -1784 -1176
541 8261 SW-NW-NE 607 -1788 -1181
Section_Z
542 21425 NW-NW-NW 646 -1821 -1175
543 21237 NE-NE-NW 692 -1869 -1177
544 21407 NE-NW-NE 729 -1912 -1183
545 22502 CNE/4-NE 680 -1867 -1187
546 21781 SE-NW-NW 675 -1863 ~1188

82

 

 

 

 

 

 

 

Well Permit Section Ground Traverse Traverse
No. No. Location Elev. Ls Top Ls Top
S.L. Datum
Kent County, Wyoming Township, T6N, R12W
Section 7
547 22299 CS/2-NE-NW 700 -1879 —1179
548 24170 NW-SW-SW 680 -1875 -1195
549 24870 SE-SW-NW 640 -1840 -1200
550 25364 NE-NE-SW 678 -1876 -1198
551 8675 NW-SW-SW 602 -1885 -1283
Section 8
552 21669 NE-SE-NW 596 -1783 -1187
553 25314 SW-SW-NW 595 -1787 -1192
554 21840 SW-SE-NW 596 -1786 -1190
555 6943 SW-SW-NE 600 -1786 -1186
556 7036 SE-SE-NE 608 -1791 -1183
557 13858 SE-NW-SW 596 -1791 -1195
558 5946 CS/2-NE-SW 601 -1794 -1193
Section_9
559 6653 SW-SE-SE 633 -1810 —1177
Section 11
560 6424 SE-SW-SW 675 -1866 -1191

APPENDIX III

DOLOMITE PERCENT FROM TRAVERSE LIMESTONE

APPENDIX III

DOLOMITE PERCENT FROM TRAVERSE LIMESTONE

 

Well Depth Below Top of Traverse Ls

No. well Name ‘ Operator 0-5 5-10 10-20 20-30 30—40
feet feet feet feet feet

 

2 R. Terpstra No. 1 - 30 70 85 55 X
Perry, Gould, & Cross
3 Cross No. 2 - Oil 25 85 92 X X
Producers
7 R. Bronkema No. 1 - 68 88 14 12 X
Sprenger Brothers
9 A. Lipski No. 1 - Mesel 3O 70 X X X
& Spielberg
16 F. T. White No. 3 - 25 34 14 X X
Turner Petroleum Corp.
19 R. Bronkema No. 2 - 26 50 16 X X
Gulf Refining Company
24 F. Cook No. 1 - George 16 20 6 X X
Kernodle
28 F. T. White - Turner 16 12 11 10 X
Petroleum Corp.
32 C. Den Boer No. 1 - 10 10 6 X X
M. H. Bauman
Refining Company
44 A. E. Raup No. 1 - Gulf 20 22 16 5 X
Refining Company
46 J. Masterson No. 1 - 14 30 8 X X
J. C. Newell, Tr.
47 A. E. Raup No. 3 - 35 14 9 13 X
J. C. Newell, Tr.
63 Daverman No. 1 - 28 35 30 14 6

Columbia Oil & Gas Co.

83

84

 

Well Depth Below Top of Traverse Ls

No. well Name ' Operator 0-5 5-10 10-20 20-30 30-40
feet feet feet feet feet

 

64 J. Zokoe No. 1 - 10 28 7 X X
American Drilling Co.

75 McKay No. B-1 - Twin 22 18 15 X X
Drilling Company

89 Sutter, et al No. 1 — 50 85 38 26 4
Swanson Consol. Oil Co.

99 R. H. Lauer No. 1 - 20 8 20 10 X
Lenoran Petroleum Co.

121 M. Wisniswski No. 1 - 35 20 10 5 X
Smith Petroleum Co.

136 W. H. Clarke No. 1 - 32 20 12 X X
Smith Petroleum Co.

137 W. & A. Bergman No. 1 - 26 8 5 X X
R. W. Atha

144 F. McKay No. 1 - Twin 12 15 9 X X
Drilling Company

149 Park No. 4 - Twin 14 8 4 X X
Drilling Company

171 F. Sund No. 1 - Turner 16 12 8 5 X
Petroleum Corp.

172 S. Kuiper No. 1 - 35 20 11 X X
Welsh Oil Company

235 J. Kuiper No. 1 - North 28 12 10 4 X

American Drilling &
Production Company

267 L. S. Wells No. 1 - 15 X X X X
Fisher-McCall Oil & Gas
Company

269 Doyle No. 1 — Fisher- 22 12 16 14 X
McCall Oil & Gas Co.

277 Lincoln Country Club 16 7 6 6 X
No. 1 - Twin Drilling

Company
297 Handley & O'Sullivan 26 20 22 8 X

No. 4 - Smith Petroleum
Company

305 G. Riddering No. 3 - 14 18 8 X X
Smith Petroleum Co.

85

 

Well Depth Below Top of Traverse Ls

No. well Name ‘ Operator 0-5 5-10 10-20 20-30 30-40
feet feet feet feet feet

 

312 G. Riddering No. 1 - 18 14 12 X X
Smith Petroleum Co.
319 Synder-McGrath No. 1 - 3O 16 11 8 X

Michigan Devonian
Petroleum Company

321 Newhouse No. 3 - 16 18 11 X X
Fisher-McCall Oil &
Gas Company

359 Grand Rapids Plaster Co. 15 18 9 5 X
No. 1 - Smith Petroleum
Company

372 Smith-Burrows No. 1 - 18 25 19 11 5
Cryden Petroleum Corp.

374 Powers No. 1 - Voorhees 18 20 1O 12 9
Drilling Company

384 G. & C. Engelsma No. 1 - 22 15 12 5 X
Smith Petroleum Company

398 Whalen No. 3 - Smith 14 10 13 12 X
Petroleum Company

401 Story No. 1 - MacCallum 18 20 10 10 X
& Herr

404 Laquae-Fletcher No. 1 - 18 12 10 6 8
Swanson Consol. Oil Co.

406 Zeeff No. 1 - Smith 12 15 5 5 X
Petroleum Company

418 Cudahy et al No. 2 - 14 16 10 X X
Smith Petroleum Company

428 Van Euwen No. 1 - Smith 26 18 8 8 4
Petroleum Company

433 Renihan No. 2 - Ide & 28 16 11 9 14
Glavin

452 Sagman No. 1 - R. W. 12 10 19 9 4
Atha

468 Orlik No. 1 - Wolverine 14 8 9 13 X
Natural Gas Company

478 Van Dyke No. 1 - Swanson 12 16 10 7 X
Consolidated Oil Company

489 A. Heald No. 1 - 14 20 14 9 4

R . Wright

86

 

Depth Below Top of Traverse Ls

 

Well
No. Well Name ‘ Operator 0-5 5-10 10-20 20-30 30-40
feet feet feet feet feet

492 Gilbert Estate No. 7 - 11 16 13 8 3
Smith Petroleum Company

496 Johnson No. 6 - 10 12 9 6 3
Wolverine Natural Gas
Company

508 W. Gilbert No. 10 - 18 15 14 7 10
Smith Petroleum Company

518 Grand Rapids Trust Co. 16 X X X X
N00 1 - H. CO Willialns

529 Grand Rapids Gravel No. 20 24 7 8 4
1 - Twin Drilling Co.

533 Grand Rapids Gravel No. 12 10 9 9 5
1 - Cryden Petroleum
Corp.

539 Alabastine Co. No. 1 - 12 8 11 6 4
Hogan Brothers

558 H. A. Chapin No. 1 - 8 12 11 8 10
Charles Harrison

559 Tanglefoot No. 1 - 10 10 10 7 8

R. W. Atha

 

 

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