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A MECHANICAL AhD STATISTICAL AHALYSIS OF THE MIDDLE

DEVONIAR ROGERS CITY-—DURDEE FORMATIONS IN MICHIGAN

BY

MILO A. BERNARDON

A THESIS
Submitted to the School of Graduate Studies of Kichigan
State University of Agriculture and Applied Science
in partial fulfillment of the requirements

for the degree of

MASTER OF SCIENCE

Department of Geology

1957

7 " “I. v ,1

ABSTRACT

Lateral variations of rock character suggest differen
sedimentary processes during their formation. In attempting
to reconstruct the tectonic conditions existing during the
deposition of the Rogers City and Dundee formations in the
Michigan Basin, composite samples of twenty-five wells
penetrating the complete system were analyzed with respect
to their lithologic character.

Numerical pictures, in the form of lithofacies maps,
were constructed from ratios relating the data. The clastic
ratio compares the amount of land-derived sediments to the
chemical precipitates and evaporites; the quartz-chart ratio
shows the contrast between primary and secondary sediments;
and the evaporite ratio relates the quantity of evaporite
deposits to the chemically precipitated materials.

Lithofacies maps are relatively new in geologic
literature, and their interpretation poses many problems.

A study of the patterns formed by superimposing these facies
maps on an isopach map of the Rogers City and Dundee forma-
tions was used to determine the possible tectonic conditions

prevailing during the period of deposition.

ACKNOWLEDGEMENTS

The author wishes to express his sincere thanks to
Dr. B. T. Sandefur. It was his constant encouragement,
helpful suggestions, and interest that aided in the
completion of this investigation. Dr. Sandefur was very
generous with his time in helping compile and edit the final
manuscript.

The writer greatly appreciates the assistance given
by the staff members of the Geology Department of Muchigan
State University to problems that arose during the
completion of this investigation.

Dr. W. D. Baten of the Statistics Department was
very considerate in offering suggestions regarding the

statistics used in this study.

11

CONTENTS

INTRODUCTION . . . . . . .

History and Description of the Michigan Basin.

Facies Analysis. .

Purpose. . . . . . . .

WELL SELECTION AND DISTRIBUTION.

Stratigraphy of the Analyzed Section .

Selection of the Top and Bottom of the

Selection of the Wells
LABORATORY PROCEDURE . . .

Method of Sampling . .

Removal of Water-Solubles.

Removal of Acid-Solubles .

Disaggregation . . . .

Sieving. . . . . . . .

Mounting and Analyzing the

Accuracy of the Data .

and Grains

Results of the Quantitative Analysis .

LITHOLOGIC VARIATION . . .

Lithologic Ratios. . .

Construction of the Facies Maps. . . .

iii

Dundee.

Page

m m ...s d .5 .15 _n d ._n .4 .—A '
"‘ “ O) 00 K] K) O\ U1 K)! R) M ‘1 -\] UT U1 4? \JJ

[0
h)

GEOLOGIC INTERPRETATIONS . . . . . . . . . . . .

Methods of Interpretation . . . . . . . . .

Errors in the Analysis . . . . . . . . . .

' Carbonates

Analysis of Variance of "Dundee'
RGSUltS Of the Analy‘SIS o o o o o o o o o 0

Correlation of the Dundee and Upper Detroit
River Group. .

INTERPRETATIONS. . . . . . . . . . . . . . . .

The Clastic-Ratio Map . . . . . . . . . . .
The Evaporite—Ratio Map . . . . . . . . .

The quartZ'Chert Ratio Pia-p. o o o o o o o o

PALEOTECTONICS AND CONCLUSIONS . . . . . . . . .
B IBLIOGRAPHY O O O O O O O O O 0 O O O O O O O 0

iv

32

. 36

36

. 37

39
4O

. 48

ILLUSTRATIONS

FIGURES

1

«Immature

Devonian Column in the Michigan Basin .

Non-Clastic, Clastic Percentages.

Clastic and Quartz-Chert Triangle .

Relations Between the Is0pachs and Facies

Analysis of Variance (Percentage limits).

Analysis of Variance (Numherical Values).

Correlation Data. . . . . . . .

TABLES

I.
II.
III.

MAPS
I.
II.
III.
IV.

VI.
VII.

well Descriptions . . . . . . .

Results of the Quantitative Analysis.

Lithologic Ratios . . . . . . .

Outcrop Pattern of the Dundee Formation

Location of the Wells Used in the Analysis. . .

County Reference Map. . . . . .

Isopach Map . . . . . . . . . .

. Clastic-Ratio Map . . . . . . .

Evaporite-Ratio Lap . . . . . .

Quartz-Chert-Ratio Map. . . . .

Page

. . 8

. 9
Pocket
Pocket
Pocket
Pocket

Pocket

INTRODUCTION

History and Description of the Michigan Basin

Since the turn of this century subsurface exploration
has been greatly intensified in Michigan. Prior to this
time, these explorations had been a subject of great interest.
Earlier subsurface exploration was impractical because parts
of the Michigan Basin were overlain by glacial deposits that
in places reach a thickness of nearly 1300 feet.

Dice (1955) completed a quantitative sedimentary
study of the Devonian deposits in the Michigan Basin. In
his investigation Dice covered a period that probably
encompassed 40 million years. It is quite feasible that
within such a time various geologic events may have occurred
which, although insignificant to the Devonian system as a
whole, may have been highly significant to a group or a
member within the system.

The Devonian system in the Michigan Basin is composed
of the following groups: Traverse, Casenovia, Detroit River,
Onesquethaw and Deer Park.

The Casenovia group consists of two limestone
formations, the Dundee and the Rogers City. The Dundee is
the thicker of the two formations. Because the two forma-

tions are similar and very difficult to distinguish in the

-2-
subsurface throughout most of Michigan, they are combined
and referred to as the "Dundee" in this study.

The general outcrop pattern of the Paleozoic
sediments in the Michigan Basin resemble concentric,
elliptical rings with their major axes trending northeast.
The younger Pennsylvanian sediments form the center ring
and the older Paleozoic sediments in their outcrop pattern
form the succeeding outer rings. The Ordovician and
Cambrian sediments crop out irregularily in the upper
peninsula of Michigan.

Newcombe (1933) described the areal extent of the
Michigan Basin as an area comprising about 106,700 square
miles. It extends north from Ft. Wayne, Indiana to Whitefish
Point, near Sault Ste. Marie, Michigan. It extends east and
west about 370 miles. The center of the sedimentary basin
conforms approximately with the geographic center of the
lower peninsula of Michigan.

According to Pirtle (1932) the Michigan Basin is
bounded on the west by the Wisconsin.Arch and on the north
by pre-Cambrian rocks. Two diverging limbs from the
Cincinnati Dome, the Kankakee and Findlay Arches, form the
southwest and southeast boundaries, respectively. A
continuation of the Findlay Arch, the so-called Algonquin

Arch in Ontario, forms the eastern boundary.

......I it‘ll-'1‘ I!!! .

 

 

 

-3-
Facies Analysis

Geologists refer to individual variations in the
lithologic and biologic character of a sedimentary rock as
"facies." Examples of these are "marine facies," "aeolian
facies," and so forth. Geologists, similarly, agree that
lateral or vertical changes of lithologic or faunal character
are referred to as "facies changes."

Moore (1949) defines sedimentary facies as, "any
areally restricted part of a designated stratigraphic unit
which exhibits characters significantly different from those
of other parts of the unit involved."

Moore further defines two different types of facies:
lithofacies and biofacies. Lithofacies are "groups of strata
demonstrably different in lithologic aspect from laterally
equivalent rocks." Biofacies are "laterally equivalent
biotic assemblages differing in their biologic aspect."

Sloss, Krumbein and Dapples (1949) proposed a third
type, tectofacies, which is best described as a "group of
strata of different tectonic aspect from laterally equivalent:
strata." '

A tectofacies map would show the laterally varying
tectonic aspects on an areal basis, and permit delineation
of the tectonic elements which comprised the framework of
sedimentation. Therefore, such a tectofacies analysis would
give minor variations in the sedimentary environment within

the structure.

n...

*i,

 

n
‘\o.

 

a4-
Krumbein and Sloss (1951) stated; "In the average
case, lithofacies and biofacies maps of the same interval

express similar trends and limits."
Purpose

The purpose of this investigation is to attempt
to define the structures within the Michigan Basin by
lithofacies and statistical analyses at the time of the
deposition of the "Dundee" formation (middle Devonian).

The writer thinks that by quantitatively and
statistically analyzing a well-defined formation, a general,
but rather accurate and significant portrayal of the tectonic
environment during that period of deposition may be inferred.

The "Dundee" was selected for this study because the
complete section has been penetrated by numerous wells. It
is hoped that the data obtained from this thesis may add
evidence to the already determined structures, and further
indicate features which have not been found through earlier

research.

-5-

WELL SELECTION AND DISTRIBUTION

Stratigraphy of the Analyzed Section

The section analyzed in this report includes the
Dundee and Rogers City formations. These two sections are
stratigraphically located in the upper-middle Devonian
section of the Michigan Basin. -

The Dundee is a buff to light brown limestone,
cherty limestone and dolomite, varying from approximately
50 to 460 feet in thickness. It is very thin or absent
in southeastern Michigan.

The Rogers City is a brownish-huff dolomite lime-
stone or dolomite which rarely exceeds a thickness of
100 feet. It is absent in southeast Michigan.

Porous zones are found in both formations. The
porosity was probably caused by solution cavities in the
limestone and dolomite, including cavities produced by
dissolved fossils, corals and stylolites. The porous
zones of the Dundee are similar in character to those of
the Rogers City, but are probably somewhat less dolomitic.

Figure I is a generalized column of the Devonian

section in the Michigan Basin

GENERALIZED

FIGURE I

DEVONIAN COLUMN OF MICHIGAN

 

Remarks

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

it Name of Unit Thickness(') Descriptions
If
a.
3 TRAVERSE ICC-875 Limestone s
shole
ROGERS cm 0425 3m"
limestone
DUNDEE 0—450 Mm"
limestone
2' Dolomite,
u. 68- H24 onhydrite
m 8 salt
8
CL 3 ' Dolomite with
D _l Richfield 0-80
0 sandstone
o:
0
w 0— l5 0 lDork limestone
_J 8i dolomite
Q a:
u:
E 2
2 0: Filer Lentil O-lOO Sandstone
(9
a:
3 Dark block
'2 E 0— 200 limestone
g g; or dolomite
l— m
g i Sandstone
<1 Sylvonio 0-300 with dolomite
- 8i ‘chert
0: Chart
w BOIS BLANC O—IOOO limes one
3 or dolomite
o
.J
GARDEN ISLAND 0-30 Dolomite

 

 

Bell shale at base

Erosionol unconformity
Absent in SW Michigan

Absent in SW Michigan
Erosionol unconformity

Subsurface only. Mainly in

central 8 S. Michigan
ErosicmgLunconformity

Erratic distribution;

' thickest in W. Michigan

Only in eastern Michigan

Erosionol unconformity

Absent in SE 8 SW Michigan

firgsionol ungonf'ormity
Patchy distribution

 

MODIFIED AFTER

H. L. MARTIN

 

-7-
Selection of the TOp and Bottom of the Dundee

The base of the Bell shale was selected as a marker
for the upper limit of the "Dundee" formation. This shale
forms the base of the overlying Traverse group. Because of
its large areal extent the Bell shale is considered to be an
excellent marker horizon.

In selecting the lower limit of the "Dundee" it was
noted that the upper part of the underlying Detroit River
group, known as the Lucas-Anderdon formation, contained a
considerable amount of anhydrite.

The author feels that the soft, wray Bell shale above
and the anhydrite-rich limestone and dolomite of the upper

Detroit River group below, form well defined boundaries for

the section analyzed in this study.
Selection of the Wells

Map I shows the outcrop pattern of the "Dundee"
formation. No wells were selected which did not include
the complete "Dundee" section.

Map Il shows the location of the wells used in this
investigation.

Table I shows the well number, location, thickn as of
the "Dundee" formation, land description, the driller and the
farm owner. The well numbers that may be referred to from
place to place throughout this analysis are the same numbers

that are found in the first column of this table.

 

 

 

 

 

j

——’—

MEL—.4

DUNDEE OUTCROP AREA

LOWER PENINSULA OF MICHIGAN

AFTER H.L. MARTIN

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

M A P II
o 22 J
2 .. f j
L 2? I s
W

WELL LOCATIONS AND NUMBERS
l+ — ISOPACH canrnor. WELLS)

 

 

-10..

TABLE I

WELL DESCRIPTIONS

 

 

Well County & Driller Land Thickness
Number Township and Farm Description of Section
1 Bay Gulf Ref. Co. 34—15F-4E 300'
Kawkawlin Salina #1
2 Midland Dow Chem. Co. 2i—14N—2E 460'
Midland Fee #8
3 Lapeer Brazos 011 a Gas 14-7N~11 95'
Attica G. Smith #1
4 Sanilac McCoy and Black 35-10h-165 265'
Lexington John Tomczyk #1
5 Shiawassee Panhandle Eastern 23-5H-2E 265'
Perry S. Nemcik Comm. #1
6 Livingston Panhandle Eastern 25—2H-5E 264'
Genoa G. Bauer #1
7 Livingston Panhandle Eastern 22-3N-3E 239'
Handy E.C. Addison #1 -
8 Ionia Terry-Dale-Mich. 12-6N-7W 139'
Berlin Tew #1
9 Tuacola Shell Oil Co. 16-13N-11E 210'
Novesta Woiden #1
1O Antrim Ohio Oil Co.. 14-31N-8W 110'
Central L. Chamberlain #1
11 Otsego Brazos Oil & Gas 15-29N-2W 255'
Chester State-Chester HE#1
12 Cheboygan Roosevelt Oil Co. leAI-DW 187'
Ellis Ormsbee #1
13 Muskegon aggart Bros. Gas 20-l2N-17W 250'
Montague C.W.Nelson #1 -
14 Wayne Basin Oil Co. 22—13-8E 170'

Plymouth

E. Raetzel #1

-11..

TABLE I (Cont'd)

 

 

Well County & Driller Land Thickness
Number Township and Farm Description of Section
15 Alcona J.C.Arthurs, Inc. 10-26N-7E 152'
Millen A. Kohlman #2
16 Arenac Ward Oil Co. lS-l9R-7E 375'
Sims Daisy Petty #1
17 Huron Pure Oil Co. 22—17N-15E 339'
J. Stapleton #1 .
18 Manistee Carter Oil Co. 35-24N-15W 70'
Fred Crook #1
19 Alpena Alpena Exp. Co. 7-32K-6E 242'
Long Rapids Wilson #1
2o Kalkaska John Neyer 27-27N-5w 300'
State—Clrwtr. #1
21 Allegan Ford 011 Go. 30-4N—12w 278'
Dorr A. Scholten #1
22 Roscommon J.o. Hutch ' 2-24N-1w 276'
Au Sable E.B. Hollwell #1
23 Isabella Cities Service 33-16N-3W 266'
Wise Methner #3-1
24 Lake C.A.Floto Special 4—17N—11w 190'
Chase V. Warchell #1
25 Lenawee J.O. Mutch 5-58-2E

Cambridge

C.L. Billmeyer #1

-12..

LABORATORY PROCEDURE

Method of Sampling

Samples from the 25 wells used in this study were
obtained from the Michigan Geoloaic Survey, Lansiig, Michi: an

The wells wez-e selected in order to get a gen—ral
picture of the "Dundee" formation below the surfa e. Only
the wells that contained the complete section were used.
Wells drilled in an OLWt rop area or well: drilled in an
area that had a formation lyin; unCUnformaAly ou the "Dundee"
other ban the Bell sia e, were not used.

The "Dundee" formation was repressited by two to

e tr vs contained approximately

’4
F,

six 'rays of .ell cuttilgs. 'F

25, IO :rs m vials. The difference in the number of

due to the Varyih; thickness of the fort tion rd tre drill-
in; intervals used by the drilling contractors. The interval
at which the samples were aken varied from 2 to 15 1 at

with an average of 5 feet.

Wentworth (I926) states that in order to aclieve Bwso
results in a mechanical analysis of materials that are sand
sine or smaller a sample of about 125 grams should be used.
Since the vertical section studied ranged from 60 to 460 feet,
in order to approach Wentworth's fi ure it 1m necessary to

take a varying amount of sample pe1 foot in t

H wevor, the fact thszt in one tell 1 gram per foot was taken

-13-

and in another 0.3 gram per foot was taken should not detract

u

from the value of the analysis because the analytical anl

p

statistical data used in this study are expresses as per
cents or*ratios.

A 400 milliliter beaker was cleaned, labeled and
weished for each well studied. Each vial was sampled
accordin; to the calculated figure that would give a
composite sample of about 125 grams from each well.

Before final weighin; a ma3net was used on each of

the composite samples to remove metal frayuents that may

(.4
}_n

have come from drilling bits or we 1 casincs.

To check the accurate wei3ht of the samples, the
thickness of the section, multiplied by the amount of sample
taken per foot should equal the weight of the composite
sample. In only one well did the error exceed one gram and
this well was contaminated by drill bits or casing fragments,
which were sulsequently removed by the magnet. In this case
the weight of the composite sample was 1.65 grams less than
its computed value.

It was felt that the errors were not sufficient to

cause any misinterpretation of the results.
Removal of Water Solubles

In order to facilitate disaggregation the samples
should be free of electrolyte particles. Wiegner (1927)

found that by boiling a water-immersed sample containing

these electrolytes, the ionic particles were driven into

‘

solution and could be removed by siphoning or filterins.

Each sample was placed in 250 ml. of water and
boiled for approximately 2 hours. After the fine material
settled, 10 ml. of clear solution was withdrawn and placed
into a test tube. The salinity was checked by adding a
small crystal of silver nitrate. If the precipitate formed
was denser than the one formed by placing a small crystal
of silver nitrite in an equal amount of tap water, another
boiling water treatment was necessary. This was repeated
until the precipitate was equal to or less than that formed
by the tap water.

Three or four treatments were necessary to remove
the water-soluble salts. The remaining sample was filtered
and washed thoroughly. After this trea ment the sample was
returned to its original beaker and allowed to dry on a warm
sand bath.

The amount of water-soluble material was determined
by substractirg the wei;ht of the sample and th beaker after
it had been boiled and dried from the weight of the original
composite sample and beaker.

The amount of fine particles left on the filter paper
was determined by comparing the weight of the filter paper
before and after it was used. This small smount, which

averaged about 0.03 gram, was added to the clay fraction.

Removal of Acid-Solubles

Limestone, dolomite and perhaps a minor amount of
anhydrite are the remaining non-elastic materials.

Due to the high percentage of acid-solubles in the
"Dundee" there was danger of losing some material due to
severe effervescence. To minimize this danger, acid of
various strengths was added at three stages.

The first treatment, 100 ml. of 25% acid, was added
slowly to the sample. Stirring the solution with a glass rod
hastened the reaction. After the reaction ceased the solution
was allowed to settle for several hours, and the supernatant
liquid was siphoned.

The second and third treatments were similar to the

LI

first except that the strength of the acid was raise» to

(

50 and loo-per-cents respectively. After the reaction of the
100% acid had ceased the sample was placed in a hot sand bath
to remove the less soluble materials, such as anhydrite and
dolomite.

After cooling and settling, the excess liquid was
removed and the beaker was filled with water, which settled.
The clear solution was then removed in order to check the
acidity. This operation was repeated until there was no
change in the blue litmus paper.

After neutralization, the beaker and the remaining

sample were placed in a warm sand bath and dried. The

-16-

ments

('0
Q
cf-

difference in weight before and after the acid tr

denoted the amount of acid-solubles.
Disaggregation

Very little shale is present in the "Dundee" forma-
tion. Landes, Ehlers and Stanley (1945) noted that in an
exposed section of the "Dundee" strata at Rogers City,
Michigan, there was an eight inch band of shale near the
base of the formation. This 8 inch band is very minor since
the thickness of the section at this location exceeded
215 feet. However, to facilitate sieving, the author
thought it best to disaggregate each sample.

Krumbein and Pettijohn(1928) define disaggregation
as, "the breaking down of aggregates into smaller clusters
or individuals."

Most of the shale present was broken down during the
water and acid treatments. A few dark grey pieces which may
have been indigenous or contaminants from the overlying Bell
shale remained.

Cooke (1956) found that potassium hydroxide (KOH)
was the best compound to use for disaggregation. A
supersaturated solution was prepared. Care was taken not
to add the KGB too rapidly, as a violent exothermal reaction
could result. After boiling the supersaturated solution
for 10 hours on two successive days the shale was

disaggregated.

Sieving

Several water treatments were necessary to neutralize
the KOH solution. The neutrality was determined when it no
longer effected pink litmus paper.

Before attempting to sieve the sample just enough
was was added to form a paste. This paste was rubbed with
.the fingers and allowed to soak in water for several hours.

The sample was then washed through a 230 mesh Tyler
sieve. This mesh is small enough to retain the fine-grained
sand particles but also large enough to permit the passage
of the smaller silt and clay particles.

The solution carrying the silt and clay particles
through the sieve was not saved. The reason will be
explained later.

The sand retained by the 230 mesh sieve was dried
and placed in small vials and saved for later microscopic
analysis. This is known as the sand fraction. The weight
of the sand fraction was not recorded. The reason for this,

too, will be explained later.
Mounting and Analyzing the Sand Grains

The sand fraction saved from the disaggregation
process was sieved through 80 and 100 mesh Tyler sieves.
The fraction retained by the 100 mesh screen were believed

to be ideal size for microscopic identification.

-18-

The 3rains were mounted on a glass slide with
Canada balsam; a cover glass was placed over them. Each
slide represented the entire well. The percentages of quartz
and chert were estimated with the aid of a polarizing

microscope.
Accuracy of the Data

It is possible that with the necessary handling of
the samples, slight amounts of fine materials were lost.
These losses were considered insignificant.

The "Dundee" samples were probably contaminated by
cavihgs from the overlying Bell shale. Even though only
slight amounts of savings were present, however, it is very
probable that they were equal to or greater than the total
amount of shale indigenous to the entire "Dundee" section.
For this reason the writer feels that to have attempted a
sand-shale ratio would have been impractical and results
erroneous. Therefore the amount of silt size particles

sieved after the disaggregation was not recorded.
Results of the Quantitative Analysis

Table II represents the statistical summary of the
quantitative analysis of the 25 wells.

The lithologic ratios expressed in Table III were
computed according to the formulas presented in the following

section.

-19-

Table II

Results of Quantitate Analysis

 

Weight of ‘fiét. water Weight of Pot. Acid
Water Sols. Sols.x1000 Acid Sols. Soluables

 

Well ‘Total
Number Weight
2 118.569
3 123.394
4 125.710
5 129.185
6 130.502
8 111.428
9 120.886
10 71.615
11 131.562
12 118.777
13 123.258
14 119.849
15 115.329
16 120.794
17 97-079
18 120.760
19 117-337
20 107.348
21 112.951
23 118.528
24 126.008
25 121.770

.035
.431
.068

.452
.232
.011

.555
.469
.015

.419
.019
.083

.243
.162
.899

.032
.171
.773

.109
0513
.453

.021
.254
.212

.212

.274
3.630
.549

30600

1.794
.008

5.215
4.208
.012

5.712
..144
.697

1.971
1.352
7.795

.265
1.761
6.401

.929
4.778
4.010

.187
2.143
1.682

1.741

115.683
106.628
110.258

109.884
110.338
118.432

93.688
80.587
109.489

65.668

127.952
116.171

81.302
113.010
99.079

119.103
94.418
105.900

114.479
102.882
93-692

86.275
96.748
72.016

103.079

95.77
89.53
89.35

87.41
85.41
90-75

88.04
72.32
90.57

91.70
97.26
97.80

65.88
94.13
85.51

98060

97-23
87069

97.56
95.84
82.95

76.92
81.63
57-15

84.65

-20....

Table III

Lith0105ic Ratios

 

 

Well Evaporite Clastic Quartz-Chart
‘Egmber Ratio x1000 Ratio Ratio
1 .303 .048 .184
2 4.032 .110 .173
3 .617 0128 .176
4 4.113 .141 .217
5 2.102 .171 .094
6 .093 .102 .086
.7 5.924 .130 .088
8 5.819 .375 .071
9 .137 .104 .200
10 6.380 .084 .032
12 .713 .022 .105
13 2.992 .513 .091
14 1.433 .060 .200
15 9.073 .154 .294
16 .268 .014 .267
17 1.811 .263 .209
18 7.300 .132 .083
19 .952 .024 .158
20 4.986 .038 .054
21 4.835 .200 .051
22 .243 .300 .265
23 2.625 .222 .122
24 2.944 .745 .105
25 2.057 .180 .107

-21-

LITHOLOG 13 VARIATIONS

Lith0103ic Ratios

The recent availability of data through drillings,
cores and 1033 as increased the value of facies macs.
Krumbein and Sloss (1951) devised a system of ratios
for mapping purposes:
"Perhaps the most fundamental
differentiation of stratigraphic units
at a given point is into non-specific
lithotopes based on a division into
elastic and non-Clastic elements in the
_strati raphic section.‘
This is called the "elastic ratio" and to M-et rmine

it the relative percents es of the cla stic an; non-elastic

known.

r3
3...}
C+
(D
I w'

1

f a
.J
C)

(1}

f" .

O

C
H
C

O

(D

Clastic Ratio : Conglomerrte+sandstone+shale
limestone+dolOmite+evaporite

A lithologic unit consisting enti wly of sandstone
would be re3rese1te1 by a cl.:;tic ra‘ tio oI inI‘i nity, whereas
that of an entire unit of limestone would be zero.

The other lith0103ic ratios expressed in Taole III
were computed as follows:

Evaporite Ratio : evaporites
limestone+dolomite

C4

Quartz-Chert Ratio : ?0 nuartz
Ac chert

The evaporite ratio is used to illustrate vgriation

within the non-elastic materials. There were very little

-22-
evaporites in the "Dundee". Some of these may have bee

removes sy waters us

(0

d in the drillin; of the wcl
may have been removed by subsequent solutions. Otier

evaporites may have been taken out of the samsles when they

. . 1-. .: - - : in. . 1 , 0 -n , .,,.. "3 , 1 _
were washed prior to beln3 pi_ced in the Sauple vials.

‘, r‘ ‘ Q ‘ _- . .I if. .0 _ (x _‘ p 1 1‘ ._ V ' o ,' -v"‘v . o
For tiese reasons the Slmn;li0a003 oI tne evaporite Iatio

Figure 2 is intended to give a quick, reasonably

f‘ 1 ‘ 1‘ ‘ ‘. ‘ ' ~ 3 , 1— 3 .- .31 ‘A ‘ . n ' ‘ "fi ." (‘9 ‘. 1" .
acctzr-..te picture of the Lifi percent e oi non-Clastics 11
- 1. I. W 3 II p ‘ n q ‘ c 3. ,_ ,__ .,_ __ _ - 1-

tne uunuee lormatlcn. It is theFebtiUw to note the

homogeneity of the non-elastics in the "Dundee". The
smaller, dashef triangle, which contains the results
obtained from the 25 wells, comprises only about 4% of the
entire triangle.

Figure 3 illustrates the cuartz-ehert and elastic

ratios of the materials from all the samples analyzed.
Construction of the Facies Maps

To construct facies maps representing variations
within a certain lithologic ratio, the ratios were plotted
at their respective position on a 3001 base map. Contour
lines of equal ratio value were then drawn.

According to Krumhein (1952) the contour intervals

may be plotted geometrically or arithmetically. The lines

‘|

used in this stuay were plotted arithhetically.

 

 

FIGURE 2

IOOSS

\N
o.

huCJOOZOz

 

CLASTIC

oboe.

 

DIAGRAM

SCATTER

 

 

 

 

-2}:-

FIGURE 3
(”axes nepnaszrn 100%)

RNAL
CLASUCS

 

QUARTZ

SCATTER DIAGRAM

CHERT

 

An isoyach map was first constructed on semi-
transpar nt paper; the ratio maps were made on opaque paper.

Superimposin: the is09ach map on the ratio map facilitated

H.

interpretation. Th s was better than constructing isopach

lines on each of the ratio mags.

Maps IV, V, VI and VII are the isopach, Clastic

(I-
H.

ratio, evaporite ra o and quartz ratio mans, respectively.

.0

The data used in constructinj the maps was obtained irom

q

I I 1
the analysis of the 'Dundee' sarples used in this study.

To get a more accur te iSOpach map, seven addition

control wells were used. (See map II). These seven wells
did not contain enou3h sample for analysis, but the footage
of the "Dundee" was recorded and used in the corstruction

of the is0pach map.

-90—

GEOLOGIC IIIZLIRL”AIIOIS

Methods of Interpretation

Krumbein (1952) noted that the relations between
isopach and facies contours show at least 6 patterns which
may be useful in interpreting
c n itions. These patterns are shown in Fi Lre '.

conditions shown 1

t!)
N
9
F3
0
H
m
U)
:“
(D
W
O
O
l o
c,—
n
*4)
O
p.)
s
O
S

Fi3ure 4 by Krumoein (I 52) when he stated.

"The linear sub-p r ll el pattern may
occur under coniitions wlere Clastic sedinents
are eread over a sub siding area in decree sin3
amount away from the sou:ces, so that the
Clastic ratio lines tend to decrease as the
isopachs increase because of increasirg lime
deposition. ihe curvilinear discord? nt pattern
may arise when a loc.? l concentr;tion of elastics
is poured into a subsidin3 area, such as a delta.
Here the elastic atio lines may project farther
into th basin than normally. The concentric
ovate pattern is characteristic of evaporites
in an intracrator nic basi . ‘i‘he irregu ar spotty
pattern occurs neLr the deter iorating ed3es of
sheet sands, where the accuhulation beconse
patchy or spotty."

q

Krumbein 3oes on to snow that there are three
patterns suitable to an intracrttonic basin, such as the
Michigan Basin.

(1) A curviliniear ftis rdant pattern could indicate

a nearby or03enic source,

(2) A concentric ovate pattern could indicate

either a nearby or03:eni c so roe, a nearby

epeirogenic source or a distant sour

-27..

FIGURE 4

RELATIONS OF ISOPAGHS (SOLID) AND FAOIES LINES

KRUNBEIN “952)

 

 

 

 

 

/ \\
/ / \\ \
/ / \
// / / \
/
/
LINEAR LINEAR
SUBPARALLEL DISQORQANT

 

 

 

 

 

 

 

M
M

CURVILINEAR coucsu'rmc
DISOORQANT ovns

 

 

 

 

 

 

 

 

 

   

DISGORDANT IRREGULAR
OVATE SPOTTY

 

 

 

 

 

-28..

(3) a discordant ovate pattern could indicate
either a nearby or03enic source or a nearby
epeir03enic source.

The patterns formed by the isopach and the

lithofacies ratio lines should give a good basis for the

interpretation of the direction and distance from a source

area.
Errors in the Analysis

In analyzin3 and 'nterpreting this section it is
possible that some errors were unavoidable. One such error
is Sue to the interpolation necessary in constructing the
maps. Some minor features are probably omitted. The
large irregularities are believed to be brou3ht out and
perhaps even accentuated by this analysis.

Some of the minor irre3ularities may be brou ht
to light due to the fact that this is a study of a
relatively short time-rock unit. For example, some feature
that may have been noted during the deposition of the
"Dundee" formation would not be noticeable in a composite
study of the entire Devonian system.

Post-depositional erosion could have an erroneous
effect on the isopach and lithofacies maps. However, the
author found no evidence following deposition of si3nificantly
large scale erosion to cause any serious error; therefore
it is believed that the isopach and lithofacies maps are

quite accurate.

Analysis of Variance of Acid-Soluables in the "Dundee"

A statistical nethod of analyzing the amount of
scattering of the acid-solubles from the general mean of

4.1,.

the solubles can be determined by using the following

Pb
o
*‘5
E
c
I...’
m
(D

 

(1)
S = E X-i 2
. n-l

where S is the standard deviation (amount of
scattering)
n-represents sigma or summation;
x-is the per cent of acid-solubles;
i-is the general mean of the acid-solubles,
which in this example is 87.30%
n-is the number of wells used.
By substituting the figures obtained from Table II

the value of S is 11.35 units.

(2) S

where 3% is the standard deviation from the
mean of the acid-soluble per cent of the
samples.
The computed value for Si is 2.27 units.
Eaten (1957) states that when running an analysis
of variance of sanples from a similar environment, the mean

of the individual samples varies from the general mean of all

-30-

the samples according to the following figures: 1) 67%
of the individual sample averages will fall within one
standard deviation (plus or minus) from the general mean;
2) 95% will fall within two standard deviations of the
general mean; and 3) 99% will be within 3 standard
deviations.

Figure 5 shows the amount of deviation from the
general mean that is allowed by the three standard
deviations.

Figure 6 shows the analysis of variance of the
acid-solubles of all the sampler analyzed. The figures
in the theoretical column are 67, 95, and 99 per cents of
the total wells used in this study. The actual values
are the number of wells that are 1, 2, and 3 standard
deviations from the general mean.

The data needed to compute the analysis of variance

were taken from Table II.
Results of the Analysis

The results tend to show that the acid solubles
of the "Dundee" were probably deposited in different
environments. This would seem quite logical because of
the variance of the per cent of acid-solubles noted
between the individual samples.

A study of this nature would, however, be useful

in an area where the variations are not so large.

 

 

-31-

Si=2.27 ', GENERAL MEAN=87.30°/o

RANGE WITHIN: IS?! 8503—89577.»

 

 

 

2 S"? = 82.76 —9I.74°/.
3 s: = 80.49 — 94.01%
FIGURE 5
FIGURE 6
RANGE THEORETICAL ACTUAL
ISX I675 7
2 55: 23.75 :2

3 Si 24.75 I4

 

 

 

32-

Statistical Correlation of the "Dundee"

and Upper Detroit River Group

Seventeen wells used in this study penetrated the
upper members of the Detroit River group. The per cent
acid—solubles of the latter group was obtained from Dewey
(1957) and correlatei with those from the "Dundee". The
same wells were used in each analysis. These "simul—wells”
are numbered 2,3,4,5,6,7,9,10,12,13,14,17,18,19,20,21, and
23 in Table 1. They may be located on Map II.

To compare the acid-solubles in the "Dundee" and
the upper members of the Detroit River group (the Lucas-
Anderdon), a statistical method of correlation, as outlined
by Eaten (1957) and doulden (1952), was used.

By plotting the per cent acid-solubles and by
applying a statistical method of correlation a graphic
representation of environmental relationship may be
observed. (Figure 7).

The "Dundee" acid-solubles are plotted along the
horizontal axis while those of the Detroit River are plotted
along the vertical axis.

The predicting lines that parallel the line of
linear regression (LR) are spaced according to the standard
error of estimate, which is explained in the following
paragraph.

To compute the standard error of estimate the follow-

ing formulae were used:

q

_ th
(1) b — EXY '- ‘fi-I

Ex2’-— (Ex)2

n

 

where b is the slope of the line LR:
E-is the summation;
x-represents the "Dundee" acid solubles (fl);
y-represents the Detroit River acid sols.(%);
n—is the number of wells used.
The computed value for "b" equals 0.93
(2) a = y —- bx‘
where x and y are the averages of x and y

The calculated value for "a" is -11.96.

 

 

(3) 39 = §I3_::_a§l_::2§£l
n —- 2

where "be" is the standard error of

estimate, which inthis case is 6.8 units.

The distance that the predicting (dashed) lines are
placed above and below the line LR are equal to 1, 2, and 3
times the computed value of "Se", respectively, and measured
parallel to the vertical axis. (See Figure 7).

The dashed lines are called predicting lines because
within 1 "Se" (above and below LR) there should fall
approximately 65% of the wells tested. Within 2 "Se" 95%
of the wells tested should fall and within 3 "Se" there
should be 99%. when the materials tested are from a similar

environment.

 

-34.

Approximately 60% of the wells lie within 1 "Se" of
LR and only 1 well falls outside 3 "Se". (Figure 7). These
positions conform roughly with the values mentioned in the
preceding paragraph.

However, instead of the 95% of all wells that should
fall within 2 "Se", only 70% are within this range. On the
basis of this discrepancy, it is probable that the "Dundee"
and upper Detroit River sediments were deposited under

different environmenta conditions.

 

 

l0w%

l

UPPER DETROIT RIVER ACID SOLUBLES
500/0

 

-35..

FIGURE 7

 

 

 

5970
DU NDEE ACID SOLUBLES

CORRELATION OF "DUNDEE"8 UPPER DETROIT
RIVER GROUP ACID SOLUBLES

BASED ON THE STANDARD ERROR 0F ESTIMATE (Se)

 

loloo/o

 

 

-35-

INTERPRETATIOLS

L)

The three lithofacies raps were interpr tel

(

separately by superimposing the isopach map on each. Features
are located in reference to counties; therefore a small
map showing the Michigan counties is included in the

pocket. (Map III).
The Clastic Ratio Map

The greatest concentration of clastic sediments is
where Lake, Newayjo, Osceola and Mecosta counties meet.

In the highly calcareous "Dundee", it is significant to
mention that in this area about 43% of the material is

A Clastic. During "Dundee" time, the west-central part of the
state reveals the highest amount of clastic materials.

The elastic map indicates that these clastics were
derived from the west, quite probably from the Wisconsin
Dome. Landes (1951) states that there is good reason to
believe that many Clastic sediments were supplied to the
Michigan Basin from the erosion of the Wisconsin Dome and
that a large amount of this material was wind-blown.

A Clastic high is also noted in Huron county. It
would seem quite logical that the source of these sediments
is the Canadian Shield-Findlay Arch area in Canada.

In noting the relation of the isopach and facies

lines, a curvilinear-discordant pattern is located in Lake,

-37-

Newaygo, Osceola and Mecosta counties. By applying Krumbein's
theory of the tectonic factors controlling deposition in an
intracratonic basin this type pattern indicates a nearby
orogenic source. This indicates a local concentration of
clastics being poured into a moderately subsiding area.

The discordant-ovate patterin in Huron also indicates
a nearby orogenic source.

These interpretations strengthen the theory that the
Michigan Basin received clastic sediments from the erosion
of the Wisconsin Dome. These sediments accumulated in the
west-central counties of the lower peninsula of Michigan.
Also that the eastern part of the Michigan Basin received
sediments from the Canadian Shield-Findlay Arch area in
Canada.

Dice (1955) noted that the west-central part of the
state received the greatest amount of elastic materials
during Devonian time. Dewey (1957) noticed a elastic high
in the same area during the deposition of the Detroit River
group. In view of these it is assumed that the Wisconsin
area was supplying sediments to the Michigan Basin throughout
the early and middle Devonian period, rather than the sediments

being deposited in a relatively short time.
The Evaporite-Ratio Map

Evaporites are deficient in the "Dundee" formation.
It should be remembered that the samples have been subjected

to water in drilling, and washed before being bottled and

-38-
sent to Michigan Geologic Survey. None of the well samples
showed as much as a 1% concentration of evaporites. The
ratios expressed on the map have been increased a thousand-
fold in order to avoid confusion caused by so many zero
digits.

Krumbein (1952) predicted that evaporites in an
intracratonic basin form a concentric-ovate pattern with the
isOpach lines. This is quite obvious in Bay and Midland
counties and denotes the center of deposition during the
formation of the "Dundee".

Alcona County, in northeast Michigan, has the highest
concentration of evaporites. This indicates a small area of
basinal deposition.

A broad basinal feature is evident in Ingham, Eaton,
Barry and Ionia counties which could denote moderately deep
sedimentation.

An interesting feature is the linear trough that
runs nearly north-south through Huron, Sanilac, St. Clair,
Oakland, Macomb and wayne counties. This "drOpping-off"
effect tends to show local subsidence along the basin's
eastern edge.

In the northwestern counties, there is another high
which is probably the result of basinal deposition. The
isopach-facies lines form a curvilinear—discordant pattern
that indicate a nearby orogenic source, probably the

Wisconsin Dome.

Quartz-Chert Ratio Map

The slides revealed that the "Dundee" formation
contained very little quartz. As little as 0.4% quartz
was noted in some of the slides.

Chert was more dominant than the quartz although
the chert content of the slides never exceeded 10% of the
total grains mounted.

The map shows that the quartz-high region is in
northern Iosco and Arenas counties, where the quartz is
presumed to be detrital and to have been derived from the
Canadian Shield-Findlay Arch area.

The quartz-chert ratio is essentially a "primary
versus secondary“ affair. Care was taken while examining
the slides to note if there was any secondary growth on
primary crystals. Secondary enlargements of detrital
quartz crystals were not detected.

The map indicated a deep water deposition in Bay and
Midland counties which conforms to the isopach interpretation
of this area.

The southern and western parts of the state show
the greatest amount of chert. The same condition is also
present in the northwestern counties. These areas conform
to Krumbein's curvilinear-discordant pattern and indicate

a nearhy orogenic source.

.. 40..

PALEOTECTONICS AND CONCLUSIONS

The Lower Peninsula of Michigan, according to
Eardley (1951), is part of the central stable region which
is composed of a foundation of Precambrian crystalline rocks,
similar to those of the Canadian Shield, and overlain by a
mantle of sedimentary rock.

The sediments in the Lower Peninsula were deposited
in an elongate basin somewhat parallel to the Appalachian
Geosyncline. The deposits extend into the northern parts
of Illinois and Indiana, and western Ontario. Nine thousand
feet of sediments, mostly evaporites and carbonates, were
deposited in the Michigan Basin prior to the Devonian period.

The studies of many investigators indicate that in
early Devonian time the Michigan Basin was affected by the
uplift of two northern extensions of the Cincinnati Arch.
These two structures were the Findlay Arch, a northeast
arm extending through Ohio into Ontario, and the Kankakee
Arch which developed through Indiana, northern Illinois and
into southern Wisconsin.

The Findlay Arch, according to Cohee (1945), may
have been a low ridge at the beginning of Cambrian deposition
and subsequent uplift along this arch was localized and of
somewhat greater magnitude than uplifts along the Kankakee

axis.

 

-41-

Cohee further states that the Kankakee Arch
divided the original major basin into two units; thus the
Michigan and the Illinois Basins came into being as separate
structures.

Since the deposition of the St. Peter sandstone
(early Ordovician), and according to measurements made down
to the top of the Trenton limestone (Middle Ordovician), the
Michigan Basin has subsided about 10,000 feet.

Kay (1947) defines an autogeosyncline as an isolated
depositional area within a cratonic unit which accumulates
sediments at a greater rate then the surrounding area,
receiving those sediment: from cratonic sources. The
Michigan Basin fits this classification. To substantiate
this point, reference is made to Eardley (1951) and Krumbein
and Sloss (1951), who state that parts of the Canadian
Shield were emergent at intervals during Paleozoic time and
served as source areas for cratonic deposition.

By the end of the Devonian, the Findlay and Kankakee
Arches and the Wisconsin Dome were well established. Gentle
erosion of these uplands served as one source of sediments
that were deposited in the Michigan Basin during the period.

In view of these historical events and the lithofacies
maps prepared from data obtained by analyzing the "Dundee"
formation, certain conditions of sedimentation may be inferred.
These conditions, in relation to the Michigan Basin, are:

1) The thickest sediments in "Dundee time accumulated

2)

3)

4)

5)

-42-
in the Midland and Bay Counties area, where
the formation attained a thickness of 460 feet.
(Well #2, Midland County).
The thickness of the "Dundee" limestone deposit
portrays conditions that were most favorable for
direct precipitation in waters which were salty
and warm during the period.
Aside from fossil evidence, the thickness and
areal extent of the "Dundee" indicate marine
rather than fresh-water limestone. The term
fresh-water'limestone refers to the beds of lime
carbonates that are deposited as more or less
continuous beds in fresh-water. Pettijohn'(195fi,
concerning freshwater'limestone3 stateesr "They
are dense to friable (marl) deposits of small
thickness and areal extent."
The evaporite facies and isopach lines show a
concentric-ovate pattern in Midland and Bay
Counties. This agrees with Krumbein's heory of
deposition in an intracratonic basin and denotes
the center of deposition during the formation of
the "Dundee". Figure 4 shows a concentric-ovate
pattern.
The greatest amount of quartz is in Iosco and
Alcona Counties. A microscopic study of the

detritals in this area showed a marked degree of

6)

-43-
sphericity. In view of the fact that these
grains could be water-borne, the author believes
that a troufh may have been present in this
area and that this trough may have permitted
the passage of sea-water into the Basin during
"Dundee" time. Water entering_the Basin through
this trough may have transported the detritals
by traction and probably caused the sphericity.
The Findlay Arch was south of this trough and it
probably served as a source area for the sediments
that were transported by the water entering the
Mich gan Basin through this trough and subsequent-
ly deposited.
The greatest amount of chert in the "Dundee" is
in the south and west parts of the Lower Peninsula.
Tarr (1926) stated that chert is deposited from
sea-water as gelatinous silica. He concluded
that the coagulation of the colloidal silica
was produced through neutralization of the
negative charges on the silica by the positively
charged ions of sodium, potassium, calcium, and
magnesium. However, there are differences of
opinion amoung geologists as to the origin of
chert. The author believes that the small amount
of chert present in the "Dundee" is of secondar
origin and occurs in the formation as nodules and

cavity fillings.

 

4+1;—

7) The conditions indicated in the elastic-ration

map are:

a-

the greatest amount of elastic sediments
was deposited in the west-central part

of the Michigan Basin during "Dundee" time.
These sediments were derived from the
erosion of the Wisconsin upland as indi—
cated by a decrease of clastic material
eastward from Lake, Newaygo, Osceola and
Mecosta counties. This seems to sub—
stantiate the theory that the Wisconsin
Dome is the source for the elastic
materials deposited in the west-central
part of the Michigan Basin during "Dundee"
time.

the roundness noted in some of the
detritals derived from Wisconsin upholds
Landes's theory that part of the elastic
materials brought into the Michigan Basin
from the Wisconsin hiahland were possibly
wind-blown.

elastic sediments compose a significant
part of the "Dundee" in Huron County. The
source for this is probably the Findlay
Arch—Canadian Shield area.

the relationship of the isopach and facies

 

s)

-45-
lines shows a curvilinear-discordant
pattern (Figure 4) in Lake, Newago,
Osceola and Mecosta Counties. By
applying Krumbein's theory of tectonic
factors controlling deposition in an
intracratonic basin, this pattern is
typical of an area where a local con-
centration of clastics has been poured
into a moderately subsiding area.
Dice (1955) noted that the west-central part of
the Lower Peninsula received the greatest amount
of elastic material during the Devonian period.
His study does not indicate, however, whether
these clastics were being deposited throughout
the entire period or whether they accumulated
in a relatively short period of time. Dewey
(1957) noted a "elastic high" trend in the
west-central part of the state in his study of
the upper Detroit River group sediments.

In this analysis, the author also found a
"elastic high" in the west-central part of the
Lower Peninsula. In view of these findings it
seems quite probable that the Wisconsin Dome
was supplying elastic material to the west-
central part of the Michigan Basin throughout

early and middle Devonian time.

-45-

During the final stages of deposition of the under-
lying Detroit River group sediments, the Michidan Basin may
have been cut off from any major source of incoming water.
Evaporation within the Basin caused the precipitation of
anhydrite which marks the upper limit of the Detroit River
group.

A combination of subsidence of the Michigan Basin
and/or a rise in the level of waters surrounding the Basin
could have initiated the formation of the "Dundee" sediments.

Warm waters entered the Basin through a trough that
extended from Ontario into Iosco and Alcona Counties. Clastic
sediments, supplied by the Findlay Arch, were water-
transported into the Basin and subsequently deposited in
this area.

The salinity of the water in the Basin and the warm
incoming waters were ideal for the formation and deposition
of marine limestone.

The "Dundee" formation in the Michigan Basin is
primarily a carbonate deposit. The greatest amount of elastic
material deposited during "Dundee" time is found in two
areas. These areas are in Lake, Newaygo, Osceola and Mecosta
counties in the west-central part of the Basin and in Huron
County in the "Thumb" area of the Lower Peninsula of
Michigan.

The center of deposition during "Dundee" time is in

the Bay-Midland Counties area. The thickness (460 feet) and

._.——u
"‘l

 

 

-47-

the relatively small amount of elastic material in this area
lead the author to believe that the thickest deposit of
"Dundee" limestone was precipitated in an area where the
deposition was contemporaneous with subsidence.

There are several theories as to the environmental
conditions that existed during the final stages of the
"Dundee" fornation. One theory, which seems quite logical
to the author, is that in late "Dundee" time the Richigan

1

asin may :ave been emergent. Sea-water probably re-entered
1e Basin and transgressed westward.

Erosion in the western part of the Lower Peninsula
before the transgressing sea-water covered the "Dundee"
could possibly account for the thinning of the sediments of
the formation in this area.

The transgressing sea probably carried the nude that

eventually formed the overlying Bell shale and culminated

the "Dundee" formation in the Michigan Basin.

~48-
BIBLIOGRAPHY

Baten, w.D. (1957), Michigan State University Statistical
Department. Personal Communication

Cohee, G. V. (1948), Cambrian and Ordovician Rocks in
Michigan and Joining Areas, Am, Assoc. Petrol
Geol. Bull., Vol. 32, pp. 1417-1418.

Cooke, L. W. Jr., (1956), Unpublished thesis A gu uantitative
Sedimentary Analysis of the Ordovician Deposits in
the Michigan Basin, Michigan State University.

Dewey, D. E. (1957), Michigan State University Graduate
Student studying the Detroit River Group sediments.
Michis an State University. Personal Communication.

Dice, B. B. (1955), Unpublished thesis A gpantitative Study

of the Composite Devonian Lithofacies in the Michigan
Basin, Michigan State University.

Eardley, A. J., (1951), Structural Geolo. of North-America,
Harper and Bros., New York, pp. i-37.

Goulden, C. H. (1952), Methpds of Statistical Analysis,
John Wiley and Sons, Inc., New York, Chapters 4-7.

Kay, M. (1947), Geosynclinal nomenclature and the craton,
Amer. Assoc. PetrqliGegl. Bull., Vol. 31, pp. 1289-93.

Krumbein, W.C. (1952), Principle of Facies Map Interpretation,
Journal of Sed. Petrg;., Vol. 22, pp. 200-211.

Krumbein, W. C., and L.L. Sloss, (1951), Stratigraphy and
Sedimentation, W. H. Freeman and 00., San Francisco.

 

Landes, K.K. (1951), Detroit River Group in the Michigan Basin,
U. S. Geql. Survey Cifrcular 133.

Landes, K.K., G. M. Ehlers and G.M. Stanley, (1945), Geology
of the Mackinac Straits Region, Miph. Geol. Survey

Bull. 44.

Moore, R. C. (1949), The Meaning of Facies, Geol. Soc. Am.
Memoir 39, pp.1- 3A.

Newcombe, R.J.B. (1933), Oil and Gas Fields of Michigan
Mgch. Geol. Survey Di§., Pub. 38, Geol. Ser. 32.

Pettijohn, F.J. (1956), Sedimentary Rocks, 2nd. Edition,
Harper and Bros., New York, Chapters 9—15.

Pirtle, G.W., (1932), Michi3an Structural Basin and its
Relations hip to Surrounding Areas, Am. Assoc. Petrol.
Geol. Bull., Vol. 16, pp. 145- 152.

Sloss, L.L., W. C. Krumbein and E. C. Dapples (1949),
Inte3rated Facies Analysis, Geol. Soc. Ah.,

Tarr, W.A. (1926), The ori3in of chert and flint, Univ.
Missouri Studies pp. 1-54.

Memoir

Twenhofel, W. H. (1939), Principles of Sedimentation, 1st.
Edition, McGraw—Hill Book Co., Inc. New York and
London.

Wentworth, C. K. (1926), Methods of Mechanical Analysis of
Sediments, Univ. of Iowa Studiesfin Nat. History,
Vol. 11, No. 11.

Wiegner, G. (1927), Method of Preparation of Soil Suspension
and De3ree of Dispersion as measured by the Wie 3ner-
Gessner Apparatus, Soil *Science, Vol. 23, pp. 377- 390.
(Translated by R. M. Barnette).

 

 

 

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