DEPOSIT‘ONAL ENVIRONMENT OF
THE UPPER SILURIAN OF THE
MICHIGAN BASIN

Thesis for the Degree of M. S.
MlCHlGAN STATE UNIVERSITY
AYAD H. DALI
197.5

 

 

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ABSTRACT

DEPOSITIONAL ENVIRONMENT OF THE UPPER
SILURIAN OF THE MICHIGAN BASIN

BY
Ayad H. Dali

The Silurian sediments of North America are
economically important. There are many problems associated
with their mode of deposition and conflicting hypotheses
have been offered concerning their origin, particularly
with regard to the water depths involved in the deposition
of the evaporites.

This study is focused on the Upper Salina group and
the Bass Islands «3 thru H units) with respect to lateral
variation in thickness and probable environments of
deposition. Isopach and lithofacies maps were constructed
for these units.

More than 400 wells were utilized and information
was obtained from gamma ray-neutron logs, cores, and
samples, thus presenting an adequate density of control
points.

Differentiation between the units presents a problem

only near the margins of the Michigan Basin. Pure salt

Ayad H. Dali

beds in the center of the basin grade into an anhydrite
facies which in turn grades into dolomite beds. Thin bands
of salt are present in the dolomite. Isolated anhydrite
zones occur in the northern part of the basin in the F
unit.

During late Salina time, the Michigan Basin was a
flat area covered by a shallow restricted sea, which at
times was replaced with a sabkha environment. The
depositional center of the basin changed for each unit,
generally moving toward the north-northeast suggesting
variations in tectonism.

Rates of subsidence varied considerably during Late
Silurian time. The basin started to sink rapidly during F
unit time. The depocenter of the basin became smaller and
smaller during Salina time. The E unit of the Upper
Silurian in the Michigan Basin is the only unit in the

Upper Salina that has produced oil (Allegan County).

DEPOSITIONAL ENVIRONMENT OF THE UPPER

SILURIAN OF THE MICHIGAN BASIN

BY

Ayad H. Dali

A THESIS

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

MASTER OF SCIENCE

Department of Geology

1975

AC KNOWLEDGMENT S

The writer gratefully acknowledges the invaluable
assistance and criticism of Dr. James H. Fisher. The
writer also thanks Dr. C. E. Prouty, B. T. Sandefur, for
their criticisms and suggestions.

Special thanks are due to the Michigan Geological
Survey and Department of Geology of the University of
Michigan for furnishing numerous logs and well data that

are vital to this investigation.

ii

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TABLE OF CONTENTS

Page

INTRODUCTION 0 O O O I O O O O O 0 O O O 1
Previous Work . . . . . . . . . . . . . 1
Purpose of the Investigation . . . . . . . . 2
Methods of Study . . . . . . . . . . . . 3
STRUCTURE O O O O O O O O O O O O O O O 5
STRATIGRAPHY O O O O O O O O O O O O O O 8
Age and Stratigraphic Nomenclature . . . . . . 8

C unit 0 O O C O O O O O O O O O O O 9

D unit 0 O O O O O O O O O O O O O O 11

E unit 0 O O O O O O O O O O O O O O 11

F unit 0 O O O I O O O O O O O O O O 11

G unit 0 I O O C O O O O O O O O O O 12
Bass ISlandS (H unit) I O O O O O O O O O 14
DEPOSITIONAL ENVIRONMENT . . . . . . . . . . 15
Conditions in the Early Basin. . . . . . . . 15
Sabkha Environment . . . . . . . . . . . 15
Transgression and Regression . . . . . . . . 17
The Origin of the Upper Silurian Evaporites . . . 17
Temperature Effect on Evaporation . . . . . . 20
CONCLUSIONS . . . . . . . . . . . . . . 21
REFERENCES 0 O O O O O O O O O O O O O 0 2 2
APPENDIX 0 O O O O O O O O O O O O O O 25

iii

LIST OF FIGURES

Figure Page
1. Geologic map and tectonic setting of the area . 4
2. Rate of subsidence diagram . . . . . . . 6
3. Depocenter changes during Late Silurian time . 10
4. Stratigraphic column of Michigan . . . . . l3
5. Sabkha type features . . . . . . . . . l6

6. Salt deposits in a desert climate sabkha
environment. . . . . . . . . . . . 19

iv

INTRODUCTION

The Silurian sediments in the Michigan Basin have
recently been investigated by several petroleum companies
to determine the depositional environment and oil potential.
Other studies have focused on the feasibility of using the
salt beds for the disposal of radioactive waste which can
be of great assistance to Michigan in competing with other
geographic areas for nuclear power develOpments.

The Salina group and the Bass Islands dolomite

comprise the Upper Silurian sediments in the Michigan Basin.

Previous Work

The Salina was named by Dana (1862). Clark (1903)
divided the Salina into a number of distinct members which
can be traced throughout most of the Michigan Basin.
Dellwig (1954) determined the depositional temperature of
the Salina as being between 32-48 degrees centigrade, and
he stated that "Salt was deposited in layers or bands of
three distinct types, as a result of seasonal changes."

Matthews (1970), states that

Sylvanite underlies some 13,000 square miles of the
Michigan Basin. The potash facies occurs as a lense
within a bed of halite. The potash deposit increases
in thickness and purity basinward. The bromine content
of halite increases from the base of the A-l salt to a
maximum in and above the potash zone in the Upper
Salina.

Alling and Briggs (1961) concluded that the
regional stratigraphy reflects sedimentary environments of
the similar but separate Michigan, and Appalachian Basins.
These separate basins were the result of a great Niagaran
reef complex which formed the physiographic setting for the
deposition of the Cayugan evaporites. The stratigraphy of
the basin margins and the basin center are better under-
stood, when treated as a unit with regional facies vari-
ations.

In the Michigan Basin the system of stratigraphic
classification devised by Landes (1954) is widely used by
subsurface stratigraphers in Michigan and Ontario, and in
1960 Landes summarized the stratigraphy of the entire
Salina group.

The most comprehensive petrographic studies were
done by: Alling (1928) for the New York section, Dellwig
(1955) for the Michigan area, Briggs and Lucas (1954) for

the evaporite facies of the Michigan Basin, and Briggs,

and Matthews (1970) for the Salina salt.

Purpose of the Investigation
The purpose of this study is to delineate the

various facies present in the Upper Salina and Bass Islands

units, and to expand and update the work done by Lucas
(1954), and Burns (1954), by studying in detail the
depositional environment of the various units. This study
was conducted over the Southern Peninsula of Michigan

(Fig. l), and was in general limited to the region enclosed

by the crest of the massive Niagaran reef.

Methods of Study

The information used in this study was obtained
through the correlation of 400 gamma ray-neutron logs.
Formation tops were determined from these logs and used in
the construction of maps of the Salina and Bass Islands
units. Gamma ray-neutron logs are mainly used in the
Michigan Basin because of the carbonate-evaporite sequences
present there. Written logs published by the Michigan
Basin Geological Survey were obtained for 30 key wells which
were used in conjunction with the formation tops determined
from gamma ray-neutron logs. Some cores and samples from
the University of Michigan, the Michigan Geological Survey,

and Michigan State University were examined.

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STRUCTURE

The Michigan Basin is an intracratonic gravity sag
basin or autogeosyncline without a well defined hinge line
that is characteristic of most tectonic basins. The basin
first developed in Middle and Late Ordovician time as
evidenced by Ordovician rocks thickening slightly in the
central basin area (Babb, 1969).

The Michigan Basin features are characteristic of
basins in the stable area of the North American continent.
The positive features surrounding the basin

(Fig. l) are not very high and these areas include the
Michigan Highland to the north in the Upper Peninsula, the
Wisconsin Dome to the west, the Kankakee Arch to the south—
west, and the Findlay Arch to the southeast.

A massive Niagaran reef formed in Middle Siluruan
time which barricaded the Michigan Basin and caused a
sabkha or restricted sea to develop as the basin subsided
rapidly in Late Silurian time. Fig. 2 shows the maximum
subsidence of the Michigan Basin during Late Salina time.
The subsidence at the center of the basin was quite

irregular. Fig. 3 shows the basin center changing

Unit C Unit D Unit B Unit F Unit G

Bass
Islands
fm

 

200 ft

400 ft

600 ft

800 ft

 

1000 ft

Fig.

 

2.

 

 

 

 

 

 

 

 

 

 

Rate of subsidence diagram.

 

J

 

 

during the deposition of the Upper Silurian from (C thru H)
units. This map indicates that the center of the basin
moved to the north-northeast, except during the deposition
of the E unit. This suggests continuous influx of clay

sized particles from the south inlets.

STRATIGRAPHY

The Upper Salina group and the Bass Islands units
(Upper Silurian), began with the widespread deposition of
carbonates, shale, salt, and anhydrite. The earlier growth
of a massive Niagaran reef created a barrier within which
the A-l Evaporite was deposited suggesting the development
of a silled or barred basin in which late intermittent
influxes of normal marine water caused the deposition of
carbonates that became interbedded with the salt section

of the Salina.

Age and Stratigraphic Nomenclature

 

This study includes the Upper Salina group and the
Bass Islands Units of Upper Silurian age (Fig. 4). The
Salina was first named by Dana (1863). Clarke (1903)
divided the Salina into several units, most of them used
today. Landes (1945, 1960) summarized the description of
the entire Salina salt deposits, and devised the system of
stratigraphic classification used in the Michigan Basin
today.

The quantitative analysis of the evaporite facies

was deve10ped by Lucas (1954), Briggs and Lucas (1954),

Briggs (1957, 1958), and Matthews (1973), in addition to the
work done by Alling (1928), who studied the petrography of
the New York section, and Dellwig (1955), who made the most
comprehensive petrographic studies concerning the Michigan
salt deposits.

There is an excellent case for the elevation of the
Salina formation to group level (Burns, 1954). This would
be in line with recent trends in stratigraphy and also
present usage by a number of authors.

The Salina group in the Michigan Basin is composed
mainly of thick evaporites interbedded with carbonate beds
which can be traced eaSily throughout the basin using gamma
ray-neutron logs. Near the margins of the basin the units
thin and the separate units are difficult to differentiate.
Recent work suggests that additional subdivisions of the
Salina units should be made (e.g., the F unit further sub-

divided into six sub-units).

C Unit

The C unit is the lowest stratigraphic unit involved
in this study. It consists of greenish-gray shale with
minor amounts of anhydrite. It is present over almost all
the basin (Plate 1). The C unit varies in thickness from
about 110 feet near the center of the basin to 50 feet in
Muskegon and Ottawa Counties to the southwest. The
depocenter of the basin during the deposition of the C unit

shifted to the east (Fig. 3).

10

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Fig. 3. Depocenter changes during Late Silurian
time.

11

D Unit

The D unit consists mainly of two salt beds separated
by dolomitic shale in the center of the basin. It grades
into argillaceous anhydrite on the margins of the basin.

The D unit varies in thickness from about 80 feet
near the center of the basin to zero thickness in the south-
west corner of Allegan County (Plate 2). The depocenter
of the basin during the deposition of the D unit shifted to

the northeast.

E Unit

The E unit generally consists of two beds: a basal
dark gray-brown crystalline dolomite with a good porosity
zone at the base, which grades upward into a gray-brown
shale at the top.

The E unit (Plate 3) extends over all the Michigan
Basin and its thickness ranges between 180 feet near the
center to 40 feet at the south margin with the exception
of relatively thick sections in southwest Allegan County,
and southeast Missaukee County. Oil is produced from this

unit in the Diamond Springs field of Allegan County (Ells,

1960).

F Unit
The F unit is the most interesting portion of the
Upper Salina. There has been much work done on this unit,

and there is more to be done on the potash, bromine, and

12

other rare salts, that have economic potential. In this
study, the writer tried to concentrate on the environment
of deposition, and its reflection of the tectonic history
of the Upper Silurian in the Michigan Basin.

The F unit consists of six salt units interbedded
with brown-gray shale beds. The isopach map of this unit
(Plate 4) shows the thickness of this unit to be more than
900 feet. The unit changes gradually from salt beds in the
center of the basin to anhydrite toward the margins.

The lithofacies map (Plate 5) shows some interesting
anomalies which indicate different possibilities of inter-
pretation of the history of the depositional environment
of the Upper Salina in Michigan Basin. There is a great
thickness of pure salt in the center of the basin, which
grades outward into anhydrite which in turn grades into
dolomite at the basin margins. Anomalies in the litho-
facies map include the presence of salt beds within the
anhydrite-dolomite facies in both the northern and southern
margins of the basin. The lithofacies map also shows an
unusually broad area of anhydrite on the southwest margin
of the basin. The presence of traces of hematite in the
salt beds in St. Clair County indicates that oxidation

occurred in a shallow water zone.

G Unit
The G Unit is the uppermost unit in the Salina

group, and is composed mainly of green to dark-gray

13

 

Silurian

Mid.

Upper

LOW.

Bass Islands

 

G Unit

 

F Salt

 

E Unit

 

D Salt

 

C Shale

 

Salina

B Salt

 

 

A-Z Evap.

 

A-l Carb.

 

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Cambrian

 

Up.

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Upper

Upper Cincinn.

 

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Middle

Bayport

 

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LOW 0

UP. I

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Sunbury

 

Ellsworth

 

Antrim

 

 

 

Middle

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Traverse LS.

 

Bell

 

Dundee

 

Detroit River

 

 

Bois Blanc

 

Stratigraphic column of Michigan.

 

14

dolomitic shale. The G Unit isopach map (Plate 6) shows a
thickness of about 100 feet near the center of the basin,
and less than 10 feet on the south margin.

In the northern part of the basin the G unit con-
sists of two shale units separated by a salt section. In
the south, and western portions of the basin, the G Unit
changes to dolomite. It is a good marker bed on the gamma

ray-neutron log.

Bass Islands (H Unit)

Near the close of the Late Silurian the Bass
Islands dolomite was deposited. The lithology of this unit
changes from place to place. Near the center of the basin
it consists of salt and anhydrite interbedded with lenses
of buff to gray shale, which grades outward to dolomite.
The thickness map (Plate 7) shows the distribution of this
bed over the basin. It varies from 730 feet near the center
of the basin, to 100 feet in Barry, Ottawa, and Muskegon
Counties.

The close of Bass Islands time is marked by a
widespread unconformity which developed during the general
uplift of the Silurian throughout the midwest (Burns,
1954). As one proceeds outward from the center of the
Michigan Basin, one Silurian unit after another is trun-
cated (Ells, 1958), this truncation is shown clearly in the

G unit isopach map (Plate 6).

DEPOSITIONAL ENVIRONMENT

Before discussing the depositional environment of
the Upper Silurian in the Michigan Basin, the following

facts should be reviewed.

Conditions in the Early Basin
The early basin consisted of a deepening depression
in which sediments accumulated at such a rate as to keep the
sea relatively shallow. Considering the flatness of the
basin floor, and the water temperatures during that time,
which Dellwig (1954), states is between 32 and 48 degrees
centrigrade, the conditions are comparable to a modern day

sabkha.

Sabkha Environment
Work was done by the writer and S. B. Upchurch on
a sabkha in northwest Libya. Fig. 5 shows the features
of the sabkha which was studied. It is a flat area in which
sedimentation keeps pace with subsidence. Small inlets
permit influx of sea water during high tides, the water
varying from 2 to 20 feet in depth. The arid environment

causes precipitation of a succession of evaporitic facies

15

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17

similar to those sediments of the Upper Salina in the

Michigan Basin. Pure salt in the center of the depression
grades into anhydrite, and then to black shale-dolomite at
the edges of the depression. If we compare the conditions
and the sediments of the Upper Salina in the Michigan Basin
with the modern sabkha environment today, it appears to be

very similar.

Transgression and Regression

The Upper Salina units in the Michigan Basin (C
through H) were deposited by a regressing Silurian sea
(Burns, 1954). At the time the basin was characterized by
a shallow flat depression covered with shallow, highly
saline water.

Sediments were deposited with salt in the middle of
the basin and anhydrite-dolomite toward the edges with
scattered salt beds in the northern part of the basin in
the dolomite-anhydrite facies zone.

The recent study (Dali, and Upchurch, 1974) on the
sabkha in northwest Libya shows the development of the
anhydrite toward the edges of a sabkha where water is less

than 4 feet deep.

The Origin of the Upper Silurian Evaporites
There is considerable evidence supporting the
shallow water depositional origin of the evaporites of the

Upper Salina in the Michigan Basin. As mentioned before:

18

The deposition of pure salt beds occurs in a
sabkha today (Fig. 6).

Fossils has been found in the Upper Salina group in
the Michigan basin, in the form of long tubes of
carbon, which resemble those of Devonian-Silurian
plant, Protaxities, which some workers took to be
evidence of deep water (600 feet deep). Arnold
(1952) has questioned the origin of this plant as
to whether it is marine or terrestial.

The presence of salt beds in the northern part of
the basin within the anhydrite-dolomite facies,
suggests that the basin floor in the northern part
was irregular.

Ripple marks in the International Salt mine in the
evaporite section (Kaufman and Slawson, 1950), and
the presence of 20 feet of shaly conglomerate in
southeastern Huron County, suggests shallow water
deposition.

A grest number of minute angular unconformaties in
the salt section, several of these have been noted
in the core samples of gas storage wells in western
Michigan (Burns, 1954) show shallow water depo-
sition.

The presence of hematite in St. Clair County

indicates oxidizing conditions in the salt beds.

.
L"
, v
v
u 0"“
u

' i n ‘1'? "
'%'.S:WA“>¢"Y

 

A. Salt deposits at the B. Salt crust on top of
surface of a sabkha. black shale.

o. - .— ' .0 . . . .
‘0 o '0‘. "u"-"".'
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C

. . .l '
_'V' ' ‘—:.\"‘ .1
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.-.~ 'V'R'. ..~ “

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C. Dolomite shale-anhydriate D. Sabkha boundary type.
facies.

Fig. 6. Salt deposition in a desert climate
sabkha environment.

20

7. The faunal study reported by Alling and Briggs

(1961) shows that "out of a total of 243 species

82% are reported only from one locality," which

indicates that the water in the basin was highly

saline, most organisms are not adapted to these
conditions.

Fig. 5 shows the spreading of the anhydrite facies
at the southwest margin, of the basin, and the shrinking
of the depocenter of the basin, indicating that the water
became shallower and shallower. The situation was demon-
strated in the recent study on the sabkha of northwest

Libya (Dali and Upchurch, 1974).

Temperature Effect on Evaporation
Evaporation rates are directly related to the
temperature. In the Michigan Basin during Late Salina time
(C through H) the temperature ranges between 32-48 degree
centigrade (Dellwig, 1955).
Dellwig (1955), stated

The salt was deposited in layers or bands of three
distinct types: (1) Cloudy layers of inclusion rich
pyramidal shaped hopper crystals of halite. (2) Clear
layers of inclusion free halite. (3) Laminae of
anhydrite and dolomite. These units are in part
obscured in the crystallized salt. The alternation of
bands of clear and cloudy halite was the result of
temperature changes probably related to the seasons.
The deposition of anhydrite-dolomite laminae may be
considered to have been the result of the influx of
normal sea water.

CONCLUS IONS

In summary, the depositional environment of the
Upper Salina and Bass Islands units in the Michigan Basin
is as follows. The Michigan Basin at that time was a
deepening depression in which sedimentation kept pace with
subsidence. The inlets to the basin were very narrow due
to the configuration of the Niagaran reefs which separated
the Michigan, and Appalachian Basins. These reefs were
also responsible for the formation of a restricted sea or
sabkha type environment in the Michigan Basin (Shearman,
1970; Friedman, 1972; and Matthews and Briggs, personal
communication).

The Michigan Basin evaporites are of a great
importance due to the potash, bromine and sodium chloride
content besides the possibility of other rare salts which
gives the State of Michigan a good potential for the

chemical industry, and nuclear power potential.

21

REFERENCES

REFERENCES

Adams, 8. S. 1970. Ore Controls Carlsbad Potash District
S.W. New Mexico. In Rau, J. L., and Dellwig.
Third Symposium on Salt. Northern Ohio Geological
Soc., Cleveland, Ohio, V. I., pp. 246-257.

Alling, H. L. 1928. The Geology and Origin of the
Silurian Salt of New York State. New York State
Mus. Bull. 275.

, and Briggs, L. I. 1961. Stratigraphy of Upper
Silurian Cayugan Evaporites Bull. A.A.P.G. V. 45,
pp. 515-547.

Branson, E. B. 1915. Origin of Thick Gypsum and Salt
Deposits. Bull. G.S.A. V. 26, pp. 231-242.

Briggs, L. I. 1958. Evaporite Facies. Jour. Sed. Petro-
graphy, V. 28, pp. 46-48.

, and Lucas, P. T. 1954. Mechanism of Salina Salt
Deposition in the Michigan Basin. Bull. G.S.A., V.
65, No. 12, p. 1233.

Burns, J. W. 1954. Regional Study of the Upper Silurian,
Salina Evaporites in the Michigan Basin. Michigan
State University (unpublished M.S. thesis).

Cloud, P. E. 1952. Facies Relationships of Organic Reefs.
31.111. A.A.P.G. V. 36' pp. 21.25-2149.

Dellwig, L. F. 1954. Origin of the Salina Salt of
Michigan. Jour. Sed. Petrology, V. 25, pp. 83-110.

, and Evans, R. 1969. Depositional Processes in
Salina Salt Michigan. Ohio and New York: A.A.P.G.
V. 53' pp. 949-9560

. 1953. Hopper Crystals of Halite in Salina of
Michigan. Am. Mineralogist, V. 38, pp. 730-731.

22

23

Douglas, G. V., and Goodman, N. R. 1957. The Deposition
of Gypsum and Anhydrite. Bull. Soc. Econ. Geol.
V. 52' pp. 831-838.

Fisher, J. H., et a1. 1969. Stratigraphic Cross-Sections
Michigan Basin. Michigan Geological Soc. Bull.

Friedman, G. M. 1964. Early Diagenesis and Lithification
in Carbonate Sediments. Jour. of Sed. Petrology,
V. 34' NO. 4' pp. 777-813.

. 1972. Significance of Red Sea in Problems of
Evaporites and Basinal Limestones. A.A.P.G. V. 56,
pp. 1072-1086.

Garret, D. E. 1970. The Chemistry and Origin of Potash
Deposits. Third Symposium on Salt. North Ohio
G601. SOC. V. 1' pp. 48-66.

Landes, K. K. 1945. Salina and Bass Islands Rocks in the
Michigan Basin. U.S.G.S.

Lucas, P. T. 1954. Environment of Salina Salt Deposition.
University of Michigan (unpublished M.S. thesis).

Matthews, R. D., and Egleson, G. C. 1973. The Origin and
Implications of a Mid—Basin Potash Facies in the
Salina Salt of Michigan. Dow Chemical Company,
Houston, Texas.

Scruton, P. C. 1953. Deposition of Evaporites. Bull.
A.A.P.G. V. 37' NO. 11' pp. 2498—2512.

Schmalz, R. F. 1969. Deep Water Evaporite Deposition, a
Genetic MOdel. A.A.P.G. V. 53' pp. 798—823.

Shearman, D. J. 1970. Evaporite-Carbonate Relations in
Basin Development. A.A.P.G. V. 54, p. 870.

The Baltimore and Ohio Railroad Company. Salt Report for
the Area Served by the Baltimore and Ohio Railroad.

Treesh, M. I. 1973. Depositional Environments of the
Salina Group (Upper Silurian) in New York State.
Rensselaer Polytechnic Institue, Troy, New York
(unpublished Ph.D. thesis).

Tremper, L. R. 1973. Lithofacies and Stratigraphic
Analysis of the Salina Group of the "North Slope"
of the Michigan Basin. University of Michigan
(unpublished M.S. thesis).

24

Omer, B. R. 1970. Brine Mixing, an Additional Mechanism
for the Formation of Basin Evaporites. Bull.
A.A.P.G. V. 12' pp. 2246-2259.

Upchurch, S. B., and Dali, A. H. 1974. Depositional
Environment in Sabkha Type. Northwest Libya.

APPENDIX

FORMATION TOPS

 

 

 

 

ILLIZIIFLLIWEILI'Q'LQIZTE'LLI:'B'LLIZFLLIZ'VE'LQZ‘E'LLIZ'EZm"
No. (KB) 1
......... 4.-----.-----»------q~-----4------§------4------1------4-------
1.1-1611-1611 22801 984 3870- 3810 3787; 3680 3482 3473 3364
134311-1811 28182 699 2983 2915 28953 2796 2664 2661; 2631
144411—1811 28178 722! .3035 2982 2958; 2870 2725 2706' 2640
65.41:.88 282581048 3591 3510 3473; 3362 2758 27241 2474
34411.72. 19411 1043 2763 2688 26513 2545 1975 1943: 2100
1-311.112 23407 770 2680 2529 2495? 2381 2017 1943! 1873
11-5N-11E 281241006} 3476 3400 3360! 3262 27641 2736; 2535
3.511.111: !266491121 3680 3602 3554; 3450 2930 2902 -—-'
0-11N-12W 23149 812 4140 4070 4052: 4000 3890 3794 3668
1.241235: 23711 1245 6802 6706 6648 g 6505 5622 5570 ' 5003
213.21.11.23 250991477 7o84 6977? 69on 6765 5865 g 57951 5172
2.411.155: 26319 629 2053 2002; 1974? 1886 1703; 1661 ; 1520
FLBN-WE f 23820 606 2554 2488: 2450 g 2362 1802 ' 1772 . 1460
Lien-148 25859 820 3672 3587i 3550 g 3457 2454 2988 ' 2886
-6N—13E 22406 804 3000 2930] 2895 5 2808 2495 2408 2171
8.611.133 22468 804 3195 3126!: 3089 2995 2655 2515 ; 2301
114111-1311 28137 888 3984 3930: 3904 3820 3745 3656i 3570
234111.11: 29492 935 4398 4330: 4279 4149 3399 33185 3038
ZZ-BZN-ZE. 28695 899 390“ 3310' 37551 3630 2890 2854; 2650
214111.48 28866 798 3990 3922: 3868 3739 2992 2934; 2608
31-351162 70194 669 2015 1966i 1915 1874 1155 1105) 888
20-348.62 29440 778 2373 2343‘ 2285 2157 1482 1443i 1149
24.351142 27725 730 2280 2242' 2188 2054 1410 1348; 1240
294511.215 127576 801 2355 2316: 2268 2152 1490 1455! 1286
17-35ME1 29068 800“ 2244 27021 2155 2025 1610 353.11-133.11

 

 

 

 

 

 

 

 

 

 

 

 

 

25

 

. .........

location

......... 4------4

33- 3311.78
35-341440
12— BBME
20-3’+N-5E
6- 3411.52

12-8N—1 BE

1
Perm. 1E lev.

No.

 

5.34N-5E

23-33N-ZE'

3-33N-ZE

21-8N—1W
32-6N-15W
30-5N-13W
17-5N-13W
35-5N-15W

11--5N--15WI

1&mmw
3—29N—3W

29-30N-2w
21-301921:
1&mmm
28-30Nuww
zyamw
1mew

29272
27674

27677

 

1-29NAflw

 

‘ 27906

35-31N-2W 29236

 

(KB)

785
881
867
658

685
737
679

1‘E37
1425
1306
1331
1334

1289
1298
1304
1124

 

2745

2583
2695
579“

5388
5320
5300
5116
5537
5“52
5906
4812

2 6
FORVISIOH

1P

TOPS

.............. I
D unitIE unit ‘

 

53771
5379;

 

47481 4704

2894
2820
2690

; 2792

2522
2650
5666
5530
5262
5212
5190
5020
5397
5334
5296

”a -.- m--v.u--—-l—~ - o..- 0..

 

2754
2875
2650
2768
2490
2560
5515
5395
5128
5078
5065
4894
5255
5194

1 5157
[4575

 

 

 

 

 

 

p unit'EB I
....... f-------
1822 1606
1705 1 1454
1895 i 1640
1620 g 1390
1503 3 1399
3034 7 2782
1432 1269
2147 1832
1995 170“

2682 8 2672'
E 2609 1935
. 2455 2356
2603 2520
2336 2290
2652 i 2382
4682 ‘ 4350
4604 E 4272
4315 3994
1.... gm,
4260 E 3930
4105 3 3772
4417 i 4077
4379 34045
4345 i4006
3288 32.62.

i---------------

 

 

2.3-3111-2111
3-32N41W
6—37N-10W 23478
27-384-1011 23435
15-32N-6W ! 2811-38
34.311N-1E 28084
3-33N-1W : 27976
24918
24359
20930
23462
'28965
23-26N—11W‘ 28954
34-261141 27977
5-264.101: ‘ 27454

 

22—35N—1E
20-27N—8E
16-hN-12w
17~hN—15W
8-26N-11W

 

32-271mm} 27860
2-25N-9W i 291404
24.258121? 29349
25-26N-12H‘18566
3022611421115 27321
3258“ 3&9
26-30N-5W 27750
10.24.1211 23685
17-3“.11w ,22622

 

 

857
909
789
912

 

 

30-1 8.71: 124782

3358
2224
4775
2785
2575
4865
5086
5202
5036
5055
6174
5314
4976
4578
5946
5164
2792
2877
2700

 

27

FORMATION

r ...... '1 .......
. 8 unit C unit

 

141110! 111104

1298!

l
36411
2871;

3776
2250

4700;
1
2730;

 

1291
3603
2828
3230
2195
#633
2705

~

g 4770
5005!

“975

5130; 5102
49681 4935

4990;
6088?
5...;
' 4878
? 4492

 

4960
6053
5218

5836

TOPS

 

 

r ...... 1 OOOOOOOO I .......
D unit 8 unit ‘

 

 

r unitéB.I.
3682 i353
2649 E2532
1031 i 805
866 % 666
2725 g 2418
1956 1660
2344 2038
1419 1115
3707 3370
2480 ‘ 2413
; 2350 - 2316
3952 . 3656
4162 3863
4292 3995
11092 ; 3786
4116 E 3805
5142 E 4830
4467 g 4203
4102 i 3740
3762 1 3386
4848 5414
4100 i 3773
2523 i 2452
2611 1 2593
2.5.8.9 '228:

 

 

 

 

 

28
FDRVATION TOPS

I ooooooooooooooo : ---------------- Our ...... 7 ........ 1 OOOOOOOOOOOOOOOOOOOOO .-
Location WPerm. 1E1ev.FB unit13 unit D unitiE unit F unit C unith.I.

 

 

36.2N-7W 29092 959 2945 2878; 2850 12770 2700 2635 12568
12-3N-10W’ 24506 7761 2910 286 2850 :2810 2620 2612 12590
36.48.88 26516 1010 3569 36721 3431 3324 2696 266412360
116.411.3111 ‘19848 912 3498 3380 3348 ;323o 2773 2653 '2361
B1-UN;15E PD 139 616‘ 1878 18282 1800 11717 1531 1520 1669

9-311.131: 26864 8161 2734 2675 2634 12595 2480121439 2374
12.31N-8E 29138 663 2880 2830 2768 :2648 196111927 1580
12-31N-8E 29513 669 2893 2841i 2779 :2659 1974 1921 1593
5.314-911: 25690 697 2745 268112677 ;2518 1859 1813 .1523
211-294—711 27483 1113 5448 538415345 {5210 4438:4394 4068
p5-31N-6W 29058 1062 4508 445314416 14286 3535 '3486 .3180
27-29N—6W 28324 13201 5820 574515705 ;5561 4765 4721 .4390
26.791451: 29019 1331 5905 58323 5790 15655 4883 4830 4420
13.291151 27931 124 5694 562015580 35438 4667 4618 ;4281
35-3N-6E 26760 950 3098 301413982 i2870 2322 2243 s1912
311-311-148 26775 897 3068 2997§ 2970 12859 2309 2233 %1917
7.311.473 .28440 921 3104 30221 2890 12750 2920 2255 31960 1
12.38.38. ’28283 928 3046 298212935 12850 2418 2360 g2195 i
5-28.58 26104 961 3203 3136: 3100 2984 2380 2347 22004
18-2N-5E 26106 934 3197 31373 3112 3009 2732 2716 :2382
10-1N—6E 25801 961 3050 2978 2944 2878 2315 2226 31820

 

 

 

 

 

 

 

 

—_-_ “- --_. ...

 

 

 

 

 

 

 

 

 

 

 

1
23.114941 27731 964 2922 28661 2848 .. _ 2649 32631
24-311-7w 23589 950 3284 3225? 3205 3130 2964 2951 12904
3.1N.12w 122646 76 2553 2497; 2479 2396 2283 2282 1
0 . i . 1

__ .........-- -0- o—“L

 

29

 

 

FORMATION TOPS
ELQ2ILI."§;;;""£Z;C'Q'LQEZ1253521132;21173331213821?22.112733:m'
No (KB) ; '

......... 4-----—------L------1------0------.------4------4---«--4-------
‘2-1N-6W 22497 948 3038 2764 2932 . 2866 2770 2908 i 2626
17-18.6w 22541 954 2972 2904, 2890 § 2783 2654 2644 1 2600 '
25-1N—6W 28372 882 3152 3083; 3054 g 2984 2890 2818 i 2714 '
15-24-4w 28902 941 3644 3588! 3567 3545 3358 3318 3000
2.368.541l 28177 798 2203 20501 2025 f .__. 1685 1627 i 1385
35-37N-4w 28712 71% 1950 1860i 1855 g 1815 1353. 1313 Q 1095
12-6N-8E 24028 926 4275 4201 4157 g 4052 34641 3438 3080
4-98.88 I 24079 837 5262 51823 5133 i 5019 42401 4200 3793
29-6N-7E 23948 862 4350 42721 4234 .4128 3502 3496 3065
36-48.38 29021 932 2998 2960? 2917 I 2797 2240 2230 2060
3-5N—9W 29489 831 3378 33101 3264 2 3204 31211 3030 . 2916
27-9N-10W 20103 903' 11050 3994: 3955 3930 3752. 3725 3574 1
1-3N-3E 1 23727 934 2985 2903; 2865 : 2750 2196 2174 1906 1
17-5N.11w 20993 7611 3050 27821 2955 f 2900 2015 2755 2505 E
6-8N-9W $211826 867‘ 4025 39631 3935 ' 3863 3693 3670 - 3515 :
18-6N—12E 22534 908 3565 35061 3466 3356 2817 2790 2575
10-8N—9E 23946 801 4737 46603 4614 4506 3842 3828 i 3708
21.911.118; 26142 836 4688 4606i 4561 4456 3822 3803 g 3640 '
6-304-11w 22627 925 3195 34091 3396 ; 3332 2673 2678 2347
32-27N—1ZW 28041 886 4390 4347; 4313 4198 3607 3582 1 3314
3.25N-11W 29205 1087 5350 5280! 5250 5130 4472 4440 3 4145
16-258211w 29049 1113 5528 5454 5425 5305 4660 4626 i 4285
2#-25NL11W 29242 1115 5684 56051 5572 5442 4775 4738 i 4437
9-25N.10w 18512 1110 5706 5601? 5586 5553 4750 4720 1 4365
1-26N—9W 27004 990 5795 371012672 5535 4880 4760JW1~4~fi

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

' """" W
Location

28-27N-9W
3‘1-27N-9W
26-8N-2w
35-8N-4w
14-58.31
21-251444:
2-28NJMJ

 

13.28N-W
36-26N-jd
13.231077:
35-33NLSW
16-211221:
4-611.811 .
28-24-28
5-71N-9E
20-34-58

No.

 

84. 314.48
8.311.552

 

1
4311-1411

-1242149
15-114.137
9-88-14w
75-27N.8w

 

22899
22918

22852

 

128773

284711-8111 L29289

 

 

 

993
901

749
816

695
1021

 

787

3973
3666
3990
3026
5852
5848

30

FORMATION TOPS

 

 

 

 

VB-LQIZEE-LQEZ1E'LQEZ”B'LLEZEBTI:'-.'
...... .------7------1------3------?-------
5410 5375 8 5250 1‘’552 “515 1 4205
5424; 5392 7 5262 4532 4494 1 4180 :
5550! 5518 ; 5383 4655 4615 i 4300
46821 465 ; 4535 4065 4250 E 3822
45541 4526 1 4406 4065 4035 ; 3975
4105i 4085 1 3960 3668 3655 3480
6680 6628 1 6472 5590 5545 5156
5665' 5620 g 5482 4710 4668 4322
61901 6148 3 6006 5205 5158 . 4715
68401 6745 2 6640 5796 5740 ' 5315
26651 2640 1 2500 1915 ;1885 1620
3420: 3375 1 3243 2534 :2495 2195 .
34293 3410 1 3310 3120 3112 3005
36201 3614 1 3524 3332 3247 3204 '
69761 6970 i 6766 5865 5812 5175 '
26821 2635 i 2518 1859 1814 f1484
2553; 2496 1 2362 1665 1620 g 1302
2997i 2970 12859 2270 2233 g 1917 '
3246i 3214 13190 2574 2500 12148
3912; 3887 3800 3657 3644 3495
3614’ 3588 3502 3366 3353 ;3168
3880 3854 3756 3608 3594 1 3445
29781 2956 2840 2744 2744 1
5765? 5732 5593 4833 4789 14484
276812231 5589 4834 4732 1447311

 

 

 

 

 

 

I QQQQQQQQQ

Location

uuuuuuuuu d

352711.811
12mmw
2h-28N-7W
33—28N-7W
5-28N.8w

21-1 3N—1W

No.

 

21-1 311.114
.26-1l1N-2E
1-25N-14w

7-5N-1 3E
ZO-SN-13E
12. 511.1 38
2.311.142
5-3N-114E
29-3N.14E
34-1N-7E
2-26N-8W
8-26N-8w
.8-28N-6w
19—28N-6W
30-28N-6w
3-27N-6w
07-27111-611!

 

23899

1
- BR 1001

28109

29-254.1qu 27899

26358
27392
28569
27073
23918
27769
22681
28830
28679
28108
28479
28089
29375
29716

1

 

f-Z7N-7W i28622

 

773

8838*

617
63?

970
1048

974
1226
1112
1141
1220
1231
1072

 

 

6021
5788
5955
5892
5938
6274
6226
5929

 

31

FORMATION

7080
4186 ‘

5784
5451
5751

6123
6290

6291

#164

 

4062.
28582
2791
2760?
1964i
19951
18151
27961
59445
5714
5873:
513103
5856‘
6185]
6134?

58412

3980
2827
2761

2723 ’

1934

1969 :

2757
5906
5682
5833
5774
5819
6143
6093
5798

5720 5

7020 T

TOPS

V """ T """"" I
- D unitiE unit ‘

5770
5596
5689
5628
5672
5993
59“?
5649

 

4778
5232

5411

35““
3380
2h05

2148
1602
1724
1531
2158
5024
4822
4892
4842
4880
5184
5140
4856

 

 

2232'

 

 

2114

1476
1510
1354

 

. “"0- -- u...- a..-“ —..-

 

 

7-28N-5w
14.3141 32
27.3114 32
34.411442
1-4N-13E

 

04u.13E
5-“N-13E

 

1

28187
29187
28325

28691
28004

26068
26660
29283
26431
24127

 

511.1413 128039

9-5N-14E
5511.142
-uN-1ZE
6.411.121:
~18—8E

26957
28183
27169
22816

 

25726

19.29.1121 125560

 

 

815112;;
(KB)

..... 1------2
1034 5964
1064 6086

982 5768
1 307 3735
1210 5923
1 359 6362
12421 6935
1293 6301

1126 6627
1212 6350
1211 5895
1221 6178

6091 2065
604 2014
627 7056
692 2449
677 2526
626 2250
764 2632
761 2667
725 23714

762 2747

871 2830

926 2455

588 1508

 

32

FORMATION

.......

5708 '

 

5667

5837’ 5787

6274! 6232 4
6794 7

6841
6209
6526
6258

 

6161
6474
6122

53201 5776

6094i
1940:
1948i 1923
1981'

2001

2176 i

2568

2600 §
2308 !

2674

6053

1951

e 23%
2459

2419
2140
2536
2566
2274
2639

27581 2724

1
2390’

23%

1412; 1379

TOPS

, ...... 1 ........
D unitiE unic'

 

 

2002
1887
2143
2166

a 001:;8.I.

 

 

 

 

 

 

 

 

33-33-102 '1 27430

10.48.1013
19-25-11E
30-13-9E
3-18-78
31-4N-14E
7-5N-17E
28-7N-1BE
17-2N-16E
29-38-16E
31-7N-16E
3-7N-16E
35-38-16E
30-7N-16E
2411-134
N-11E

 

 

 

11-4N-11E I23072
18.5N-10E 124471

 

 

 

46:6 12164

No. (KB)
23778 610 958
146 609 980
25535 9831 2447
l22639 8781 3465
24627 872’ 3983
24904 7411 1754
'26024 729 2158
579 1130
24851 606 1093
25560 588 1508
26016 706 2079
23743 1040 2753
1 an 616 1876
ED 152 632 1908
25632 813 3440
25780 579 1550
23201 586 1758
26468 698 2570
26724 749 2845
25186 579 1520
24210 690 3055
24557 908 4770
23655 1036 3262
977 3128
1077 3842

 

1
2222‘:

 

33

FORVATIOPI

 

1412.
2009;
2680i
1827i

 

18501
33721
14781
16001
~7- 1
27781
.172;
29985
4700
my
3056

,,. ‘ ...
1
2333 g 2224
3343 1 3205
3902 33798
1671 g 1520
2052 5191.1
950 1 848
983 3 866
1379 1 1280
1971 1 1857
2645 1 2540
1800 i 1710
1818 1 1733
3322 1 3223
1533 1433
2472 2369
2738 1 2643
"" 2895
4645 4557
3152 3054
3020 2918
3737 36345

TOPS

 

 

, ...... '1 ........
- D unitiE unit

 

 

 

 

 

 

193:112'6'352'1'1'137'"
....... 1------1-------
704 6321 453
720 585 1 470
1776 1732 i 1426
25881 2561 1 2263
3668 3658 3522
13221 1276 1 1042
.— 1 1377 1141
798i — 596
795 721 497
946 881 528
14781 1317 5 1076
2087‘ 2030 . 1730 1
1531 1521 1448 1
1473 1326 j 1224 E
2713 2687 1 2450 1
1336 1244 :1080 1
1434 1340 i 1197 1
2014 1876 1 1732 1
2055 2026 11717
——' 1214 : 1073
2640 2626 E 1672
4035 3995 13640 }
2559 2531 1 2328
2444 2414 1 2222
3164 3.194.122.7321

 

 

 

 

 

 

 

34

 

 

 

 

 

 

 

 

 

 

 

-- “- —.-—1~-.—

 

 

FORVATIOH TOPS
ILLQZILL"1?;;;"'122;U'22.};133522112521E'L;;Z'1E'LQIZ"BELIZE?”
No. (:(B) 1
......... 4------4-----1------1------0------2------1--.---1------1-------
19.421415 22665 1004 3922 3898 3860 1 3562 3150 3070 12762
1

34.4N—8E 24516 1018 3550 3472 1 3431 ;3324 2696 2664 .2340
35.94.1011 27296 9““1 4083 4020 2 ’ 7" 2752 1 -
35-8N-9W 211-627 872 3934 3922 1 “2 "' 3761 3671 13515
12.60.94 16734 636 .2 —-- -—- -—- 3466 341513015
2.711.911 26946 85713910 3850, «1 "' “' 3610 3480
11-“3N-5E 129936 980 3509 3‘13“ 339“ 13230 2620 12555 2310
21-13N-1W'23849 695 6450 6344 16291 16162 5370 15339 4990
28.24N-2E 25099 1476 7084 6976 16920 16766 5865 5812 .5317
6-711.111 27811 773 4721 4650 14617 14507 4016 4004 '3757
13.33.84 22352 952 2235 2102 12083 1 1976 11976 .1924
2.294.411 25873 1413 5481 5408 15364 15216 4432 14390 4054
27-384.1011231135 678 1293 1242 11227 11092 887 866 666
2411.131: 24557 909 4770 4700 14675 14557 4035 3995 3690
3011.111: 22627 925 3495 3410 13382 “3254 2673 2638 12350
1611-1711 29168 615 3204 3138 13112 3028 2988 2890 2801
0.144.171: 28203 797 3170 3102 13075 12990 2847 2840 ;2804
4511-1714128“ 913 3170 3400 13370 3290 3136 3123 13073
2134171128169 718 3192 3125 13098 '3005 2850 2848 ;2805
4.154.184 28220 714 3114 3061 13028 2833 2789 2782 ;2737
3-3011-341 29085 1310 5323 5248 15205 5071 4790 4253 13921
5-3011-311 29074 1321 5327 5253 15212 5073 4301 4257 13930
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