Geological Controls on Stratigraphy and Sedimentation of the Mississippian Marshall Formation, Michigan Basin, U.S.A

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Geological Controls on Stratigraphy and Sedimentation of the Mississippian Marshall Formation, Michigan Basin, U.S.A.

Joseph G. Adducci

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Recommended Citation Adducci, Joseph G., "Geological Controls on Stratigraphy and Sedimentation of the Mississippian Marshall Formation, Michigan Basin, U.S.A." (2015). Master's Theses. 617. https://scholarworks.wmich.edu/masters_theses/617

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GEOLOGICAL CONTROLS ON STRATIGRAPHY AND SEDIMENTATION OF THE MISSISSIPPIAN MARSHALL FORMATION, MICHIGAN BASIN, U.S.A

Joseph G. Adducci

A thesis Submitted to the Graduate College in partial fulfillment of the requirements for the degree of Master of Science Geosciences Western Michigan University August 2015

Thesis Committee:

David A. Barnes, Ph.D. (Chair) William B. Harrison, III, Ph.D. Peter J. Voice, Ph.D.

GEOLOGICAL CONTROLS ON STRATIGRAPHY AND SEDIMENTATION OF THE MISSISSIPPIAN MARSHALL FORMATION, MICHIGAN BASIN, U.S.A.

Joseph G. Adducci, M.S.

Western Michigan University, 2015

An understanding of regional orogenic, climatic, and eustatic processes is critical to the interbasinal correlation of Paleozoic strata in eastern North America. Tectonic activity associated with the culmination of Appalachian Orogenic events has been shown to have regional influence on paleostructure and sediment dispersal in the Appalachian foreland basin and adjacent intracratonic Illinois and Michigan basins. The culmination of the Acadian Orogeny at the end of the Devonian represents the beginning of a period of general tectonic quiescence extending throughout the early and middle Mississippian in eastern North America. Early Mississippian strata in the Michigan basin is distinctive and marks the transition from marine shale and carbonate dominated sedimentation during much of the Late Ordovician through Late Devonian to siliciclastic dominated deposition throughout much of the Carboniferous. The Osagian, Marshall Formation constitutes an important coarse-grained siliciclastic formation in the Michigan basin. Despite numerous outcrop studies and early subsurface investigations, the Marshall remains poorly understood in terms of depositional controls and stratigraphic relationships to related Mississippian strata in Michigan and correlative strata in adjacent basins. This work documents sedimentological and sequence stratigraphic relationships in Early-Middle Mississippian, generally clastics-dominated strata of the Marshall and lower Michigan formations (as described in previous literature). New stratigraphic relationships are presented suggesting that the Marshall Formation and informal Stray sandstone units are genetically related and reflect tectonic, eustatic and climatic processes that occurred in the Michigan basin during the early Carboniferous in the Michigan basin.

ACKNOWLEDGEMENTS

I would like to sincerely thank my thesis committee chair, Dr. David Barnes for his unwavering support, unflinching confidence in my ability and fond characterization of myself as “the most cautious geologist”. Without his encouragement, I would not have had the courage to attempt this work. I also thank the other members of my committee,

Dr. William B. Harrison III and Dr. Peter Voice for their guidance and attentiveness to my research.

My parents Melinda Adducci, Gregory Adducci, Rebecca Adducci and Joseph

DuMouchelle will forever have my gratitude and thanks for their encouragement and support throughout this research, having been there with me every step of the way.

Lastly, I thank my girlfriend, Marie Samson for her compassion, kindness and monumental effort in helping me complete this work. From cooking late-night dinners at home to spending anniversaries professionally photographing cored rock samples, she has endured this work with me and for this; I dedicate this thesis to her.

Joseph G. Adducci

TABLE OF CONTENTS

ACKNOWLEDGEMENTS ...... ii

LIST OF TABLES ...... iii

LIST OF FIGURES ...... vii

CHAPTER

I. INTRODUCTION ...... 1

Michigan Basin Structure and Subsidence ...... 2

Early Carboniferous Regional Tectonics and Eustasy ...... 3

Regional Stratigraphy of the Early Mississippian ...... 6

Michigan Basin: Kinderhookian-Osagian Stratigraphy and Deposition ...... 10

Research Questions ...... 13

II. DATA AND METHODOLOGY ...... 15

Core Materials ...... 15

Wireline Log Data...... 18

Thin Sections ...... 18

III. SEDIMENTOLOGY ...... 21

Depositional Facies ...... 21

Facies D1: Fossiliferous Mudstone ...... 21

Facies D2-A: Cross Bedded Lithic Sandstone ...... 23

Facies D2-B: Intraclastic Lithic Sandstone...... 26

Facies D3: Bioturbated Lithic Sandstone ...... 26

Facies D4: Finely Laminated Lithic Sandstone ...... 30

iii

Table of Contents-continued

CHAPTER

Facies D5: Structureless Sandstone ...... 30

Facies D6: Heterolithic Sandstone/Mudstone ...... 32

Facies D7: Dolomitic Mudstone/Wackestone ...... 33

Facies D8: Laminated Dolomite/Anhydrite ...... 34

Wave-Dominated Clastic Depositional Systems ...... 37

Barrier Shoreface and Strandplain Environments ...... 38

Coastal Sabkhas and Shallow Marine Evaporites ...... 40

Western Canada Sedimentary Basin: Triassic Analogue ...... 42

Facies Associations and Interpretation ...... 47

Facies D1: Offshore Marine...... 47

Facies D2-A: Middle-Lower Shoreface ...... 49

Facies D2-B: Middle Shoreface ...... 49

Facies D3: Middle-Upper Shoreface ...... 50

Facies D4: Foreshore ...... 50

Facies D5: Backshore ...... 51

Facies D6: Intertidal ...... 51

Facies D7: Restricted Lagoon ...... 52

Facies D8: Coastal Sabkha ...... 53

Depositional Model ...... 57

Table of Contents-continued

CHAPTER

Flooding Surfaces and Associated Ravinement ...... 59

IV. PETROPHYSICAL ROCK MATRIX ANALYSIS ...... 64

Core-to-Log Correlation/Calibration ...... 67

Facies Association Mapping ...... 70

Log Facies L1-A/B ...... 72

Log Facies L2 ...... 73

Log Facies L3 ...... 73

Facies Mapping ...... 74

Isopach Map L1-A ...... 75

Isopach Map L1-B ...... 75

Isopach Map L2 ...... 76

Isopach Map L3 ...... 80

V. SEQUENCE STRATIGRAPHY ...... 83

VI. DISCUSSION AND CONCLUSIONS ...... 90

Early Mississippian Paleoclimate, Tectonics and Eustasy ...... 90

Paleoclimate ...... 91

Eustasy ...... 92

Tectonics ...... 93

Table of Contents-continued

CHAPTER

The Michigan “Stray” Problem ...... 95

Conclusions ...... 97

REFERENCES ...... 99

APPENDICES

A. Graphical Core Descriptions ...... 104

B. Photomicrograph Plates ...... 127

C. Fortran Programs for Calculating Rock Matrix Mineralogy...... 131

D. Well Data Listing For Marshall and Lower Michigan Formations...... 142

LIST OF TABLES

1. Core Data Listing for Marshall and Lower Michigan Formations ...... 21

2. Summary of Depositional Facies ...... 62

3. Petrophysical Properties of Common Minerals and Fluids ...... 65

4. Summary of Petrophysical Properties of Log Facies Units ...... 82

vii

LIST OF FIGURES

1. Major North American Tectonic Provinces ...... 5

2. Early Carboniferous Chronostratigraphy of the Eastern United States ... 8

3. Carboniferous Stratigraphy of the Michigan Basin ...... 9

4. Core Location Map ...... 17

5. Well Log Location Map ...... 19

6. Facies D1 ...... 22

7. Storm Generated Deposits ...... 24

8. Facies D2-A ...... 25

9. Facies D2-B ...... 27

10. Facies D3 ...... 29

11. Facies D4 ...... 31

12. Facies D5 ...... 32

13. Facies D6 ...... 33

14. Facies D7 ...... 34

15. Facies D8 ...... 36

16. Doig, Halfway and Charlie Lake Formations Depositional Model ...... 44

17. Paleographic Reconstruction of Doig, Halfway and Charlie Lake Formations ...... 45

18. Comparison of wells from the Doig, Halfway and Charlie Lake Formations and the Marshall and lower Michigan Formations...... 46

19. Core Description of the MCGS 8-31 Well ...... 54

viii

List of Figured-continued

20. Idealized Facies Succession ...... 56

21. Marshall and lower Michigan Formations Depositional Model ...... 58

22. Bioclastic Limestone ...... 60

23. Shoreline Ravinement Surface ...... 61

24. RHOmaa-Umaa Crossplot ...... 68

25. RHOmaa-Umaa “Impossible Solution” Fields ...... 69

26. Marshall and lower Michigan Formation Type Log ...... 71

27. L1-A Isopach Map ...... 77

28. L1-B Isopach Map ...... 78

29. L2 Isopach Map ...... 79

30. L3 Isopach Map ...... 81

31. Cross Section A-A’ ...... 86

32. Cross Section B-B’ ...... 87

33. Cross Section C-C’ ...... 88

34. Comprehensive Cross Section Map ...... 89

35. Sea Level and Paleoclimate Cycles of the Carboniferous ...... 91

CHAPTER I

INTRODUCTION

The Mississippian Marshall and Lower Michigan Formations have been of

interest to geoscientists for over 150 years beginning with the initial findings of Winchell

(1861). Early Mississippian sands were also among some of the first hydrocarbon

reservoirs in the Michigan Basin to be exploited, with significant gas discoveries in the

Marshall and Michigan “Stray” sands throughout the 1930’s. Like many other

Geological studies, the exploration and production of these resources prompted the earliest investigations of the origin and distribution of the early Mississippian sand units.

While many early researchers attempted to investigate these sand units including Stearns

(1933), Eddy (1936), Bergquist (1938), Hard (1938), Ball (1941), and Monnett (1948), these early investigations relied primarily on outcrops, drill cuttings and rare-poor

quality gamma ray well logs. Following these early investigations, few researchers have

attempted to further study the early Mississippian sands in detail, though notable

observations have been made using well logs and reviews of previous works by Lilienthal

(1978), Cohee (1979), Harrel (1991), and Westjohn (1998). While interest in the

Mississippian Coarse-grained clastics as hydrocarbon producers has largely waned, these

units have yet to benefit from a modern core-based sedimentological and sequence

stratigraphic analysis.

Advances in subsurface logging equipment along with calibration and correlation

of data to core intervals have continued to prove invaluable in furthering the

understanding of geological relationships in the subsurface. The objective of this study is

to establish sequence stratigraphic and sedimentary facies relationships within the

Marshall and Lower Michigan formations through the identification of mappable

lithofacies units using core-to-log calibration and correlation across the Michigan Basin.

This work will then be integrated into a depositional model for these units in the

Michigan basin subsurface. The depositional model with facilitate a better understanding of the geological origin and distribution of Mississippian sands. Additionally, this geological model will provide a context for better understanding the depositional response of the Marshall and Lower Michigan formations to both eustasy and orogenic activity related to the Appalachian Orogen.

Michigan Basin Structure and Subsidence

The Michigan basin is located within the cratonic interior of eastern North

America, adjacent to the Wisconsin Highlands and Canadian Shield to the north, a series

of positive features or arches (the Wisconsin, Kankakee, Findlay-Waverly, and

Algonquin) to the west, south, and east, and the cratonic interior Illinois and Appalachian

basins (Boothroyd, 2012, Figure 1). A series of northwest-southeast trending anticlines

are present throughout the basin, which are historically significant with respect to

hydrocarbon exploration and production (Ells, 1979; Catacosinos et al., 1991). Many of

these structures are interpreted to result from periodically reactivated basement faulting

that was active during the Paleozoic (Ells, 1979; Cohee, 1979).

The mechanisms responsible for the-nearly symmetrical subsidence of the

Michigan basin have been proposed as thermal contraction associated with a 1.1 Billion year old rift, Midcontinent rift system (Catacosinos et al, 1991; Howell & van der Pluijm,

1999). Previous researchers have identified alternating periods of narrow and broad basin centered subsidence (Howell & van der Pluijm, 1999). Periods of narrow subsidence are attributed to load induced weakening of the lower crust during regional tectonism associated with periods of intense Appalachian orogenesis. In contrast, broad basin-centered subsidence is attributed to crustal attenuation. Howell & van der Pluijm

(1999) also note periodic eastward tilting events during the Ordovician and Devonian, possibly due to flexural effects of Taconic and Acadian collisional events (respectively) in the Appalachian Orogen to the east.

Early Carboniferous Regional Tectonics and Eustasy

The Acadian orogeny is the third of four orogenic events within the Appalachian

Orogen, and spans upper Devonian through lower Mississippian time (Ettensohn, 1987,

2004, 2008). Four tectophases constitute Acadian orogenic activity with the fourth and

final tectophase also known as the Neo-Acadian. The culmination of the Neo-Acadian

tectophase occurs at the Devonian/Mississippian boundary (~360 Ma) (Ettensohn, 2008).

This orogenic activity generated sufficient lithospheric loading and flexure, in the form of

elongate peripheral arches, such that the Appalachian foreland basin was separated from

the intracratonic Illinois and Michigan basins during the early Carboniferous (Quinlan &

Beaumont, 1984; Howell & van der Pluijm, 1990; Ettensohn, 2008).

Plate tectonic reconstruction by Scotese and McKerrow (1990) show the steady closure of a narrow seaway separating Gondwana and Euramerica during Appalachian collisional events creating orogenic belts with a northeast southwest orientation. A prolonged period of tectonic quiescence is thought to have existed following Late

Devonian - Early Mississippian Acadian tectonism coincident with widespread siliciclastic sedimentation in the Appalachian, Illinois, and Michigan basins (Ettensohn,

2008). In the Appalachian foreland basin, both Taconic and Acadian tectonism is recorded by the deposition of large volumes of siliciclastic material known as clastic

“wedges” (Sloss, 1963; Ettensohn, 2004, 2008). These deposits are characterized by progradational deltaic deposits, which thin towards the continental interior to the west

(Ettensohn, 2004).

Although the early Carboniferous is not known as a time of intense glaciations across the Gondwana paleo-continent, evidence indicates late Paleozoic glaciations occurred in the mid-Visean (338 Ma) (Crowell, 1999). However, recent workers (e.g.

Richardson, 2006; Matchen & Kammer, 2006) have also shown lithologic evidence for possible Gondwanan glaciations and resultant fluctuations in eustasy, particularly during the Kinderhookian-Osagean following Acadian orogenesis. These glacio-eustatic fluctuations may have influenced deposition of the Marshall formation in the Michigan basin during the Kinderhookian-Osagean. While the extent of these glaciations is poorly understood, other Gondwanan glacial events, possibly equivalent to the Kinderhookian-

Osagean boundary have been recognized in the basins of Brazil as well as age equivalent strata in Idaho and Nevada (Crowell, 1999; Matchen & Kammer, 2006).

Figure 1: Generalized structure map showing the position of major North America tectonic provinces and features in relation to adjacent sedimentary basins in the northeastern United States (Modified from Boothroyd, 2012; modified from Potter & Siever, 1956; Structural arches from Cohee, 1965; and Root et al, 1998).

Regional Stratigraphy of the Early Mississippian

Previous workers (Ettensohn, 2004; 2008) suggest that the Neo-Acadian tectophase resulted in repeated down warping flexural response and subsequent deposition of the Sunbury Shale during the early Kinderhookian. This black organic-rich shale formation is geographically extensive with deposition reaching into the western

Appalachian and Michigan basins. Figure 2 shows regional stratigraphic correlation for the Early Carboniferous within the eastern United States. The Sunbury Shale is conformably overlain by the Kinderhookian-Osagean Borden-Price Formations in

Kentucky with Borden deposition extending as far west as eastern Indiana (Gray, 1979;

Ettensohn, 2009). In Ohio, the Sunbury Shale is conformably overlain by the

Kinderhookian Cuyahoga Formation that is in turn unconformably overlain by the

Kinderhookian-Osagian Black Hand Formation in the central portion of the state

(Matchen & Kammer, 2006). The Sunbury Shale in the Michigan basin is likewise conformably overlain by the Kinderhookian Coldwater Shale and Osagian Marshall

Sandstone (Cohee, 1979; Harrell, 1991) although uncertainties exist with respect to the stratigraphic position of the Marshall formation.

Formations possibly equivalent to the Marshall and Lower Michigan are the

Borden, Cuyahoga, Logan, and Black Hand, Figure 2 (Matchen & Kammer, 2006;

Ettensohn et al, 2009). The Farmer’s Member of the Borden Formation comprises a prodeltaic sequence of alternating very fine grained sandstones, siltstones and mudstone

(Ettensohn et al, 2009). The Logan Formation similarly, is a siliciclastic unit present in

6 southern Ohio comprising various marine shale and sandstone of marine origin (Matchen

& Kammer, 2006).

The Cuyahoga and Logan Formations are an intercalated succession of shale, siltstone, and sandstones of marine origin. Trace fossils are common throughout the

Cuyahoga Formation except where the Black Hand Sandstone is present (Matchen &

Kammer, 2006). Recent work from Matchen & Kammer (2006) suggests that the Black

Hand Sandstone is an incised valley fill deposit. This interpretation is consistent with a eustatic drop in sea level due to Gondwana glaciation presumably near the

Kinderhookian-Osagean boundary.

Figure 2: Early Carboniferous chronostratigraphy for the northeastern United States region. (1) Eon, system/period, series, North American stages and glacial intervals (Haq and Schutter, 2008), (2) Orogenic events and Eastern Kentucky stratigraphy (Ettensohn, 2008), (3) Southeast Illinois and western Kentucky stratigraphy (Gray, 1979), (4) Michigan basin stratigraphy (Towne, 2013), (5) Central Ohio stratigraphy (Matchen and Kammer, 2006).

Figure 3: Current stratigraphic nomenclature of the Carboniferous within the Michigan basin. The possibility of an unconformity separating the Marshall and Michigan formations is recognized within this stratigraphic column. (Towne, 2013; modified from Fisher et al, 1988).

Michigan Basin: Kinderhookian-Osagean Stratigraphy and Deposition

Early Mississippian, predominantly sandstone Marshall Formation conformably

overlies the Kinderhookian Coldwater Shale, which is turn conformably overlies the

Sunbury Shale, also of Kinderhookian age (Cohee, 1979; Harrell, 1991) These formations

constitute the onset of aerially extensive and voluminous, fine-to-coarse-grained

siliciclastic deposition during the upper Paleozoic. Palynologic study of the Marshall

indicates an Osagian age (Richardson, 2005, 2006). Previous studies of the Marshall

Sandstone (e.g. Winchell, 1861; Stearns, 1933; Hard, 1938; Monnett, 1948; Harrell et al,

1991; Westjohn and Weaver, 1998.) document the occurrence of locally abundant marine

fossil beds and other sedimentological features indicating a shallow marine, possibly delta-front origin. Previous studies (see above) subdivide the Marshall into two laterally continuous “blanket” sandstones; the Upper (Napoleon) and Lower Marshall separated by a sequence of shale, siltstone, carbonate, and evaporite strata.

The lower Marshall has historically been recognized as the first aerially extensive sandstone unit conformably overlying the Coldwater Shale and is thought to be present throughout the basin where the Marshall is not eroded below the Pleistocene

Unconformity by glacial scour. In many places throughout the basin a second sandstone unit overlies the lower Marshall and is separated from it by an intercalated sequence of shale, siltstone, carbonate, and evaporite strata (Westjohn, 1998). Many researchers have postulated that the overlying second, upper Marshall sandstone is Osagian in the south

and southwestern portion of the basin and indistinguishably interfingers with a similar

blanket sandstone unit of Michigan (Meramecian) age in the central and northeastern

portion of the basin. The upper sandstone, where separated by carbonate and evaporite

10 strata from the lower Marshall are interpreted to be part of the Michigan Formation and are informally referred to as the “stray” sand. Where the lower Marshall is separated from the upper sandstone by siltstone and shale, this upper sandstone unit is interpreted to be of Marshall (Meramecian) age (referred to as the Napoleon) member of the Marshall.

However, parts of the basin show only the Lower Marshall sandstone present, conformably overlain by the Michigan formation. Interpretations vary greatly as to the origin and stratigraphic relationships of the upper Marshall, or Napoleon member, and the

Michigan Formation. The Michigan Formation overlies the Marshall and is typically interpreted to contain the uppermost “stray” blanket sandstone unit in the north and central parts of the basin as previously mentioned. Both sands are overlain by a sequence of shale, carbonate, evaporite, and laterally discontinuous sandstone beds that comprise the Michigan Formation.

Monnett (1948) suggested a subdivision of the Marshall Sandstone into two distinct members in the southern part of the basin with the fossiliferous, fine-grained, lower Marshall Sandstone overlain by non-fossiliferous, coarse-grained upper Marshall, or Napoleon sandstone. The two units are typically separated by a lithologic change to siltstone/shale although this relationship is not observed in all wells. In the central and western portion of the basin the lower Marshall is observed as fine-grained, reddish sandstone-siltstone, although the reddish color is absent in the eastern part of the basin.

The Michigan “stray” sandstone overlies the lower Marshall in the central and northern parts of the basin and is recognized as sandstone that overlies the lowest dolomite and shale separating the two sandstone units. The presence and stratigraphic position of the lithologically distinct, basal Michigan Formation dolomite and shale lithofacies below the

“stray” sandstone are the basis for the inclusion of the “stray” sandstone lithofacies into

the Michigan Formation (Monnett, 1948). Monnett (1948) also noted that the

stratigraphic relationship of these dolomite and shale lithofacies to the sandstones of the

Marshall Formation is a primary stratigraphic problem that is yet to be adequately

explained. A large isopach thickness change occurs within the Marshall between the

northern and central portions of the basin and the south central basin, making correlation

between Michigan “stray” sands and those of the Napoleon member irregular and

unclear. However, two explanations have been offered by previous researchers as to the

relationship between the Napoleon member and Michigan “stray” sands.

An initial hypothesis was introduced by Bergquist (1938) suggesting that the

“stray” sand is reworked and redeposited Marshall Sandstone. This depositional hiatus

implies an interruption in Marshall deposition and an unconformity of unknown

magnitude between the Marshall and Michigan formations. Following erosion of the top of the Marshall formation, these “stray” sands were deposited as sandbars during early

Michigan deposition. Stearns (1933), Eddy (1936), and Ball et al, (1941) support this hypothesis.

Another hypothesis, introduced by Hard (1938), suggests a gradational contact between the Napoleon and “stray” sands with irregular, interfingering sandstone, shale, and dolomite at the contact. This explanation implies that both the “stray” sands and portions of the Napoleon Sandstone were deposited simultaneously in different portions of the basin. This second interpretation is supported by more recent studies (Monnett,

1948; Cohee, 1979; Ells, 1979; Lilienthal, 1978; and Westjohn et al, 1998) with minor variations in depositional mechanisms.

Research Questions

The purpose of this study is to investigate stratigraphic and sedimentologic relationships in the Marshall Sandstone and related Lower Carboniferous strata in conventional core and wire-line logs in order to better understand the geological controls on deposition of these Lower Carboniferous, mixed-carbonate, evaporite and siliciclastic strata - in the Michigan basin. While several studies have been conducted by previous workers, many have relied on vertically and aerially limited outcrop exposures due to lack of conventional core material. Only more recent studies (Lilienthal, 1978; Westjohn and Weaver, 1998) utilize gamma ray well logs for subsurface correlation. The combination of detailed sedimentologic analysis of subsurface core and core calibration/correlation to modern well log suites will allow for a better understanding of these units in a sequence stratigraphic context. Geological controls during deposition will be inferred from stratigraphic/sedimentologic relationships in these units including observation and interpretation of: 1) sedimentary lithofacies; 2) sedimentary successions and stacking patterns; 3) important stratigraphic bounding surfaces; and 4) unit thickness, spatial distribution and geometry. Furthermore, regional comparison with correlative strata from adjacent cratonic interior basins, the Illinois and Appalachian basins, will be evaluated to investigate large scale geological controls on deposition including tectonic and eustatic mechanism. This regional correlation exercise will be facilitated by chronostratigraphic studies focusing on palynomorphs (conducted by consultants). The main questions to be addressed in the course of this research are summarized below:

1: What are the sedimentary lithofacies present in the Marshall and Michigan “stray” in the Michigan Basin?

2: What are the distribution, geometry, contact relationships, and stacking patterns of sedimentary lithofacies in the Marshall and Michigan “stray” in the Michigan Basin?

3: What are the primary depositional environments represented by lithofacies in the Marshall and Michigan “stray”? 4: What were the depositional controls on the Marshall and Michigan “stray” in relationship to regional tectonics and eustasy?

CHAPTER II

DATA AND METHODOLOGY

All cores, samples, and wire-line log data used in this study are housed at the

Michigan Geological Repository for Research and Education (MGRRE) at Western

Michigan University. This facility contains well records, data, and boxed cores for

thousands of wells within the Michigan basin and also serves as the base of operations for

the Michigan Geological Survey (MGS). Query of the digital database at the MGRRE

facility was used to identify 537 wells containing either core or wire-line logs from the

Lower Carboniferous interval in the basin. While most cores used in this study contain

one or more associated well logs, only one well was found to contain a full suite of wire-

line log data in addition to cored rock. This enabled calibration of well logs to identified

facies in core and further refinement of the petrophysical methods used in this study.

These core to log calibration methods are considered to be essential in delineating the

lithological complexity of the Marshall and Lower Michigan Formations.

Core Materials

A common challenge in modern sequence stratigraphic and sedimentary facies- oriented investigation of subsurface formations is the limited access to core materials suitable for identification of features key to a sequence-oriented stratigraphic analysis.

This study focuses on numerous key wells containing “type section” cores covering the

Marshall and Lower Michigan Formations across the Michigan basin. Critical stratigraphic relationships were documented in core and then geographically extrapolated

15 using a much larger well-log data set. Many of these cores are confined to the central portion of the basin with measured depths between 1800 – 2500 ft where good quality and relatively modern wire-line log suites can be used in calibration of core materials.

Ten cores were originally considered for this study but upon investigation three of these cores were of poor recovery and quality. These cores also were found to be incorrectly labeled and mismatched in their arrangement within loose boxes. The lack of reasonable confidence in stratal relationships in these cores led to the discarding of this material from this study. Seven remaining cores (shown in figure 4) were examined, including three cores from the north central portion of the Michigan basin in Clare

County, three cores from the central basin area in Isabella, Mecosta, and Montcalm counties, and a single core from Ingham County in the southern portion of the basin. Of the seven cores, five contain at least some form of well log, with two cores (including one in Clare and one in Ingham counties) required a “pseudo correlation” to nearby well logs.

A table providing location and associated well log data for each core can be found in

Table 1.

Figure 4: Map showing the locations of wells containing core from the Marshall and Michigan formations used in this study and the subcrop of the Marshall (Red) and Michigan (Green) formations.

Wireline Log Data

Wire-line logs, especially more modern log suites (those recorded subsequent to about the mid-1970’s,provide a much more complete 3 dimensional coverage of lithological relationships established through core studies in subsurface investigations.

Well logs provide a continuous, albeit indirect, record of rock properties in the wellbore and were used to identify common mineralogy within sedimentary rocks. In order to establish subsurface distribution and geometry of sedimentary lithofacies as well as sedimentary successions, well logs were used as an important tool after calibration to conventional core. Either gamma ray (GR), compensated neutron porosity (NPHI/CNL), compensated bulk density (RHOB/FDC), and photoelectric factor (PE/PEF) logs are available from 535 wells that penetrate the interval of interest in this study. Of the 535 wells with useful logs, 279 wells were found to contain “modern” log curves (see above) and were used in the construction of cross sections as well as petrophysical calculations referred to later in this study.

Thin Sections

Thin sections housed at the MGRRE facility were available for some cores used in this study. Representative thin sections were examined for each depositional facies identified in this study including: framework grain composition, microfossils, and other primary depositional characteristics, although this was not a significant component of this study. Thin section observations are attached; Plate 1 through Plate 5.

Figure 5: Map showing the locations of 535 wells containing well logs. Wells with any type of digital or raster log are shown in blue while those wells containing a complete suite of “modern” logs are highlighted in purple. Subcrop of the Marshall (Red) and Michigan (Green) Formations is also show

Table 1: Core Data Listing for Marshall and lower Michigan Formations Total Linear Core Linear Total (ft) Footage Max. Core Depth (ft) Depth Core Max. Min. Core Depth (ft) Depth Core Min. Well Logs Present Logs Well API/UWI # API/UWI Well Name Permit # Permit County

GR, RHOB, 21035259950000 MCGS 8-31 25995 Clare 1477 1330 147 NPHI 21035242390000 Yake et al 1 24239 Clare 1550 1478 72 GR, RHOB, 21035260460000 MCGS 9-71 26046 Clare 1502 1374 128 NPHI GR, RHOB, Moeggenberg NPHI, 21073352980000 2 35298 Isabella 1302 1250 52 PEF GR, RHOB, 21107315300000 SL-217A 31530 Mecosta 1346 1228 118 NPHI GR, RHOB, 21117314970000 SL175A 31497 Montcalm 1370 1255 115 NPHI NP SB15 07108 Ingham 468 310 158

CHAPTER III

SEDIMENTOLOGY

Depositional Facies

Description of cored materials in this study was conducted using depositional

facies rather than gross lithofacies. Depositional facies were identified on the basis of

primary lithology and sedimentary structures formed at the time of deposition, rather than

those fabrics that originate from diagenetic or other post depositional mechanisms (Rock,

2011). A summary of the depositional facies identified in this study is presented in Table

2 at the end of this chapter.

Facies D1: Fossiliferous Mudstone-Shale

Description: Facies D1 is a dark gray, fossiliferous, fissile mudstone/shale.

Facies D1 is observed only in the Moeggenberg 2 well located in Isabella County,

Michigan. In this core, Facies D1 overlies a sharp, abraded contact above underlying

Facies D7 and includes a thin ~3.5ft bioclastic limestone (Figure 7) containing various unidentified skeletal grains. Lingulid brachiopods, including Orbiculoidea sp., along with bivalves are common in Facies D1 and are typically found in planar orientation, as lags along bedding planes (Figure 7). Pyrite mineralization is also observed in the lower portions of this facies.

Figure 6: Fossiliferous Mudstone Facies D1. (A) Dark gray mudstone with interstratification of fine siltstone lenses. (B) Bioclastic limestone marking the lowermost contact of Facies D1 with underlying lagoonal dolomite. (C) Oribiculoidea. Sp. (OB) brachiopod preserved intact along bedding plane. (D-E) Bivalve (BV) fossil accumulations preserved along bedding planes. (F) Contact of D1 and D2 Facies at the top/base of cyclic depositional packages.

Facies D2-A: Cross bedded Lithic Sandstone

Description: Facies D2-A is an olive green to red brown, moderately to well sorted, subangular to subrounded, crossbedded to low angle, planar bedded, locally bioclastic, fine- to medium-grained, micaceous quartz and lithic sandstone that is most commonly observed in the lower portions of cored Marshall intervals in the Six Lakes

Field in Montcalm and Mecosta Counties, MI. The most prominent sedimentary structures include low angle (10-15°) cross stratification that gradually fines upward in core in 1-1.5 ft cycles. The base of these cycles is identified by the presence of poorly sorted bioclastic lag deposits and thin discontinuous laminations, typical of swaley cross stratification (SCS). Bedsets typically are centimeter to millimeter thick with inclined bedding that fines upward. These strata are then overlain by higher angle cross-bedding.

Lag deposits are composed of poorly-sorted, typically disarticulated brachiopod fossil fragments and other unidentifiable skeletal grains. Facies D2-A is observed in well logs as a coarsening upward succession of shale facies below transitional upwards into a coarse-grained, sandy clastics-dominated facies. These rocks are inferred to be underlain by more distal marine facies in a conformable succession. Facies D2-A also occurs in conformable and gradational contact with the overlying Facies D3.

Figure 7: Schematic illustrating the idealized development of storm generated deposits as a result of combined flow. Vertical successions shown in example B are recognized in Facies D2 with strong combined flow conditions creating coarse-grained crossbeds with skeletal lag deposits that fine upward and grade in low angle to planar laminated deposits. Internal stratification records the transition to dominant oscillatory condition during the waning of storm conditions (From Plint, in James & Dalrymple, 2004; Based on Cheel, 1991; Cheel and Leckie, 1993).

Figure 8: Storm Dominated Facies D2-A. (A) Swaley Cross Stratification (SCS) associated with strong combined flow conditions to produce crossbedding (XB). Inclined bedding is also shown (IB). (B) Fossiliferous crossbedded and planar laminated coarse to fine sandstone, typical of storm influence acting on mixtures of coarse and fine sandstone. Note lag deposits (LD) composed of Brachiopods (BP) overlying truncated sandstone (TR). (C) Further example of storm influence found in the Facies D2 including lag deposits overlain by planar laminated sandstone. Refer to figure 7 for wave processes associated with storm influence.

Facies D2-B: Intraclastic Lithic Sandstone

Description: Facies D2 is typically found immediately overlying Facies D1 in

cored intervals and is composed of olive green to light tan, moderately- to poorly-sorted,

subangular to subrounded, planar bedded, truncated, sparsely burrowed, intraclastic, fine-

to very coarse- grained, micaceous quartz and lithic sandstone. Common sedimentary

structures in this facies include 1-1.5 ft thick, planar bedded (0.25-2.5”) intervals with

scour contact overlying coarse-grained sandstone. The overlying coarse-grained

sandstone intervals fine upward in 0.5-1 ft sections, grading into fine planar bedded units.

Lag deposits are common at the base of coarse intervals with large, up to 1.5” intraclasts.

Large intraclasts show slight to minimal differences in (1-10°) angular orientation from

original underlying beds. Burrow structures are also found at the scour interface with

burrows extending down into the fine planar bedded units. Burrowed morphology

generally suggest Skolithos ichnofacies particularly Arenicolites in the form of J-shaped

burrows that exhibit vertical escape orientation and subsequent filling of the burrow with

coarse grained sediment.

Facies D3: Bioturbated Lithic Sandstone

Description: Facies D3 ranges from light green to light red in color and is

moderately to well-sorted, subrounded, bioturbated, sparsely intraclastic, fine- to medium-grained, micaceous quartz and lithic sandstone. Physical sedimentary structures

in this facies are sparse, however 2-D asymmetrical ripples, local mud intraclasts, and discrete interbeds ranging from cm to dm in scale are common. Facies D3 is the most heavily bioturbated unit in the Marshall and Michigan Stray units. Bioturbation reworks and homogenizes physical sedimentary structures. Bioturbation typically occurs, although not always, in discrete beds with both horizontal and vertical burrows. Vertical burrows extend above and below the bioturbated beds, and are best described members of the Skolithos ichnofacies.

Figure 9: Intraclastic/Bioturbated Facies D2-B. (A) Planar laminated fine- to medium- grained sandstone truncated by coarse grained intraclastic sandstone. Note planar laminations (PL) and surface of truncation (TR) by storm influence wave action. Intraclasts (ITC) appear to be derived from underlying planar laminated sandstone. (B)

Planar laminated sandstone with Skolithos burrows (SK) filled by overlying coarse grained sandstone.

Figure 10: Bioturbated/Mottled Sandstone Facies D3. (A) Highly mottled fine grained sandstone with remnants of both vertical and horizontal burrow traces. (B) Discrete centimeter-scale beds of bioturbation reflecting alternating wave energy frequency commonly associated with storm events in upper shoreface settings. (C) A further example of discrete bioturbation beds containing recognizable vertical burrows associated with the Skolithos ichnofacies. (D) Physical sedimentary structures overprinted by burrow mottling.

Facies D4: Finely Laminated Lithic Sandstone

Description: Facies D4 is characterized by light to medium red-brown, very well-

sorted, subrounded, thinly bedded and laminated, fine-grained micaceous quartz and

lithic sandstone. Facies D4 is easily distinguished from other facies in core due to its fine

(millimeter to centimeter) planar bedding/laminations. Laminations are defined by

micaceous concentrations with sparse bioturbation found between bedsets. Thin

interbeds often display slight variation in grain size, indicating high frequency, albeit

slight changes in energy during deposition. Bioturbation is sparse in this unit and

consists of vertically oriented burrows. Facies D4 is consistently found in the uppermost

section of cored clastic intervals in the Marshall and Michigan Stray units across the

basin and shows conformable and gradational contact with both underlying and overlying

facies units.

Facies D5: Structureless Sandstone

Description: Facies D5 is comprised of a light tan to light brown, very well sorted, subrounded, structureless, very fine grained sandstone. The lack of sedimentary

structures in the Facies D5 distinguishes it from all other facies in cored intervals of the

Marshall and Michigan Stray. This Facies D5 marks an apparent change in framework

mineralogy composition from more lithics-rich, shallow marine shoreface facies (D2-5)

to fine-grained quartzose sandstone largely devoid of sedimentary structures although

faint discontinuous laminations are recognized as well as zones of increased oxidation

capping the uppermost portions of the facies.

Figure 11: Finely laminated Lithic Sandstone Facies D4. (A) Planar laminated fine- grained sandstone with stained overprint of laminations possibly from poor handling of cored materials from the shallow depths of the MCGS 8-31 well. (B) Planar laminated sandstone similar to the previous example from similar foreshore deposits observed in the deeper portions of the MCGS 8-31 well. (C) Additional example of foreshore deposits from the SL-217A well.

Figure 12: Structureless Quartzose Sandstone Facies D5. (A) Fine-grained sandstone devoid of sedimentary structures as well as rust colored iron oxidization resulting from limited subareal exposure. (B) Contact between the D5 structureless sandstone and underlying foreshore deposits denoted from planar laminations seen at the bottom of the sample.

Facies D6: Heterolithic Sandstone/Mudstone

Description: Facies D6 consists of dark gray to light tan, very well to poorly

sorted, subrounded, flaser to lenticular bedded, bioclastic, fine- to very fine-grained sandstone and mudstone. Bioturbation and skeletal material is common in this facies including both vertical and horizontal burrows of the Skolithos ichnofacies. 2-D wave ripples and foresets are also observed in Facies D6 and are represented in lenticularly bedded sandstones that are encased in mud drapes. The full spectrum of lenticular to flaser bedding (Figure 13) is represented in this facies though the entire range of this spectrum is not present in every core studied.

Figure 13: Heterolithic Sandstone Mudstone Facies D6. (A) Very fine-grained sandstone and mudstone contain flaser textures with alternating rippled sand and mud with horizontal burrows. Opposing dip direction, cross-laminations suggest bidirectional current energy. (B) Wavy to lenticular bedded sandstone and mudstone with ripple structures. (C) A further example of lenticular bedded sand and mud.

Facies D7: Dolomitic Mudstone/Wackestone

Description: Facies D7 marks a transition to carbonate dominated deposition in a specific facies succession in the Marshall and Michigan Stray units. Facies D7 is medium to dark brown, finely bedded, intraclastic, laminated, dolomitic mudstone to wackestone. Dolomitic intraclasts are present in discrete beds, although they are typically confined to the lower portions of the deposited interval. Unidentified skeletal grains are present throughout D7, although dissolution has removed them and subsequently filled the remaining vugs with anhydrite. Horizontal burrowing is present, though sparse, and algal laminations are abundant. Facies D7 is found in conformable contact with the underlying Facies D5 or D6 and typically shows a gradational mixing of quartz and micrite at the contact between the two units.

Figure 14: Dolomitic Mudstone/Wackestone of Facies D7. (A) Dolomitic wackestone with disarticulated brachiopods and other unidentified skeletal grains. (B) Brachiopod fossil fragments occur at the contact with overlying upper shoreface deposits of Facies D5. (C) Fossiliferous dolomite with anhydrite filled molds found beneath overlying sabkha facies D8. (D) Planar laminated dolomitic mudstone possibly originating from algal laminations typical of lagoonal and sabkha settings. (E) Planar laminated dolomite overlain by burrowed dolomitic mudstone.

Facies D8: Laminated Dolomite/Anhydrite

Description: Facies D8 is typically found as the uppermost unit in facies successions in both the Marshall and Michigan Stray units. Facies D8 is a light to medium gray/brown, finely laminated, dolomitic mudstone, to nodular and enterolithic anhydrite. Facies D8 is typically observed as an intercalated succession of mudstone,

34 dolomite, and anhydrite in cored intervals. Mudstone is typically the basal lithology of this facies and is found to be in conformable contact with any underlying facies.

Typically Facies D8 represents the shallowest/most proximal facies found in the studied cored intervals.

Figure 15: Cumulative/Nodular Anhydrite and dolomite Facies D8. (A) Alternating cumulative and nodular anhydrite, typical of sabkha and salina settings. Note the enterolithic nature of the nodular anhydrite, displacing dolomitic mudstone/wackestone. (B) A further example of the displacive nature of nodular anhydrite found in dolomitic sediments. (C) Cumulative anhydrite deposits shown adjacent to nodular/enterolithic anhydrite, suggesting contemporaneous deposition in a sabkha/salina pond setting.

Wave-Dominated Clastic Depositional Systems

By nature of wave influenced currents, wave dominated shorelines typically exhibit

geometrically simple "sheets" of shoreface sand that reflect the balance of the seaward

transport of sediment during storm activity and the landward or lateral transport of

sediment during normal wind-induced wave action. Preservation of shoreline

successions is also noted by Clifton (2006) as simple and consistent with additional

accumulation of sediments promoting shoreline progradation. Progradation results in

simple, tabular shoreface successions with relatively low geometric complexity. These

successions are typically represented by sand-dominated deposition in environments ranging from the distal offshore and lower shoreface through more proximal foreshore and backshore settings up-section. "Swaley" and "Hummocky" cross stratification is diagnostic of and common in lower to middle shoreface facies. Hummocky cross stratification or "HCS" are a product of large wave-induced currents accompanied by weak currents that record combined flow conditions with a strong oscillatory component

(Snedden et al, 1994), typical of storm deposits. While HCS are commonly observed within interbedded mudstone and sandstone successions in slightly lower energy zones, swaley cross stratification or "SCS" is characterized by gently undulating fine laminations with shallow, broadly circular scours that fill with upward flattening laminae.

Similar to HCS, SCS are formed during oscillatory-dominant combined flow conditions with erosional swales overlying constructional hummocks, creating the SCS facies structure. SCS is common in the middle shoreface environment offshore of foreshore and upper shoreface settings. Additionally, in response to energy associated with shoaling waves, wave dominated shorelines tend to exhibit a progressive, "coarsening upward"

profile in vertical succession when associated with shoreline progradation (Clifton,

2006). Modern wave dominated systems are also shown to encompass elements that are

subject to tidal influence such as tidal inlets, lagoons and other back-barrier settings,

which are protected from regular wave action by sub-aerial, barrier island systems.

Shallow marine, coastal depositional systems are especially subject to the influence of relative sea level fluctuation due to eustatic, sediment supply and subsidence factors. These factors determine the internal structure of wave dominated successions relative to retrogradational, progradational, "normal" regressive or "forced" regressive profiles. While many examples of ancient shoreface deposits are formed under progradational conditions, modern examples such as Galveston Island, Texas are scarce as modern post-glacial seas gradually rise and clastic sediment input is anthropogenically reduced (Clifton, 2006). These factors, specific to many modern coastal settings, make direct analogue to ancient progradational shore-line successions difficult. An understanding of physical processes that act on these few modern environments, though, is invaluable for interpretation of ancient deposits.

Barrier Shoreface and Strandplain Environments

According to Glaeser (1978; in Clifton, 2006), nearly 15% of the worlds present

coastline is fronted by sandy barrier island or barrier spit complexes. Many of these

modern examples reflect accumulations of sand that migrated landward under slow

transgression however models of progradational shoreface systems differ greatly in

lithologic succession and stratigraphic preservation. Transgressive barrier systems are

characterized as sand-poor, as the relative rise in sea level results in sediment trapping in

landward fluvial and estuary systems, thereby reducing the amount of sediment delivered

to open portions of the coast (Clifton, 2006). Additionally, transgressive-barrier models

promote a depositional trend in which landward terrestrial and backshore facies are

overlain and often truncated by shoreface and deeper marine facies in an overall seaward

driven succession.

Progradational barrier systems differ from other transgressive variations in that

sediment delivered to the open coast is likely to be far more abundant and thus the distribution of sand may extend further seaward during deposition. Mobilization of the sandy sediment by waves, storm events, and longshore currents deliver sediment across shelf particularly in low-gradient, basin margin ramp settings. Tabular sand "sheets" with simple coarsening and shallowing upward internal facies successions are common.

Additionally, sedimentation rates, relative sea level rise and longshore transport currents may be sufficient to form barrier island complexes that may occur with the formation of back-barrier deposits and lagoons (Clifton, 2006). Sea water circulation within back- barrier or lagoonal systems may fluctuate resulting in differing degrees in salinity due to restriction from normal sea water conditions, particularly in tropical arid climates (Pratt, in James and Dalyrmple, 2010).

Strandplain successions similarly develop under progradational conditions, with an internal "shallowing upward" facies successions as seen in barrier models. Clifton

(2006) suggests that distinguishing barrier from strandplain systems requires recognition of differences in geometry and facies associations. While barrier systems are associated with lagoonal and back-shore facies assemblages, strandplain systems show more

simplistic shallowing upward successions that are devoid of these topset beds. These

differences in facies association are thought to reflect a more limited outpacing of

accommodation space by sedimentation during strandplain formation, whereas barred

prograding systems may be produced by a more abundant sediment supply under the

same sea level conditions (Clifton, 2006).

Coastal Sabkhas and Shallow Marine Evaporites

The occurrence of marine evaporites represents an important part of the geologic

record and numerous detailed studies provide a basis for interpreting these deposits in

terms of depositional processes and environmental conditions. While various modes of

deposition exist for marine evaporites, some of the most well known deposits include

marginal marine sabkhas. Schreiber and Tabakh (2000) suggest that sabkhas are best

characterized as accumulations of evaporites as part of the outbuilding of topset beds that

occur generally along regressive or progradational shorelines in low gradient ramp

settings. Studies of modern sabkhas also show that accumulations of evaporite sediment can be deposited over broad areas during relatively short periods of geologic time. The climatic conditions necessary for evaporite deposition in sabkhas include arid and often windy conditions that accelerate evaporation along coastal areas that lie 1-2 meters above sea level (Schreiber and Tabakh, 2000).

Gypsum and anhydrite are common components of sabkha deposits and are formed within the vadose and capillary groundwater zones of those coastal areas that are subaerially exposed just above the shoreline. A 1-2 meter elevation of coastal areas

relative to sea level results in sediments that lie within the phreatic and capillary zones

typically remaining wet (Kendall, in James and Dalrymple, 2010). Brine evaporation

within the capillary zone results in the precipitation of gypsum, which under extreme

conditions, can be further dehydrated to anhydrite. Rehydration of anhydrite to gypsum

may occur during periods of increased rainfall while still resembling their dehydrated

form. Repeated periods of hydration and dehydration promote increased size of these

nodules that merge to become continuous layers of mosaic anhydrite or gypsum

(Schreiber and Tabakh, 2000).

Alternately, instances of shallow subaqueous evaporite deposition along sabkha

profiles has been documented in previous studies. Progradation of sabkha deposits

advance through accumulation and stabilization of bacterial mats and early cementation.

Partial erosion of these areas is a common feature that creates localized ponds that may

undergo periodic flooding (Schreiber and Tabakh, 2000). It is proposed by Shearman

(1978) that given the 1-2 meter difference in elevation of sabkhas above sea level that

storm driven flooding of these areas is a common occurrence that acts to replenish marine

waters across ponded areas. Under the appropriate salinities, from 150-320 g/L

according to Schreiber and Tabakh, (2000), shallow water evaporites occur as vertically

aligned, elongate gypsum crystals that exhibit swallow-tail and other cumulate

morphologies. Burial depths of these deposits at a few hundred meters result in

dehydration and conversion of shallow marine gypsum to palmate anhydrite that can be

identified as clusters of parallel to sub-parallel anhydrite crystals (Kendall, in James and

Dalrymple, 2010).

Western Canada Sedimentary Basin: Triassic Analogue

While modern examples of mixed siliciclastic/carbonate progradational systems may be sparse, ancient analogues from the Jurassic and Triassic periods across the North

American craton are well studied. Triassic strata within the Alberta Basin in Canada were deposited within the Peace River Embayment bordering the eastern edge of the

Rocky Mountain Front Ranges produced by the Cretaceous Laramide Orogeny. Triassic rocks within the Peace Rive Embayment mark a regional transition from siliciclastic to carbonate-and evaporite-dominated deposition (Edwards et al, 1994).

The Doig, Halfway and Charlie Lake Formations in the western foothills of the

Peace River Embayment represent mixed carbonate/siliciclastic deposition as part of a progradational, shallow marine system. While stratigraphic relationships vary across the

Alberta Basin, the Doig and Halfway formations represent lower shoreface sand deposits that are gradationally overlain by barrier island and upper shoreface sandstones (Edwards et al, 1994). Deposits from the lower Charlie Lake Formation lie above the Doig and

Halfway sands and are dominated by restricted shallow marine strata representing a variety of depositional environments such as sabkhas, coastal dunes, and nearshore lagoonal carbonates. Regional stratigraphic studies have determined that in places where these formations are conformable, the Doig, Halfway and Charlie Lake Formations represent a mixed carbonate/siliciclastic progradational barrier system (Edwards et al,

1994). Barrier and shoreface sands dispersed along the shoreline by longshore currents acted to restrict large lagoonal areas landward during deposition, creating an extensive carbonate-dominated lagoon system with marginal marine sabkhas and associated eolian dunes (Figure 16) (Edwards et al, 1994).

Three facies assemblages were identified within the lowermost Charlie Lake

Formation; (1) Sandstone assemblage, (2) Grey-bed assemblage and the (3) Red-bed assemblage with each assemblage representing shoreface/barrier, lagoonal and sabkha deposits respectively. Regional mapping of these three facies assemblages as synoptic facies belts yielded a simple east to west distribution that was used to reconstruct the paleogeography during deposition of the lowermost Charlie Lake beds (Figure 17)

(Edwards et al. 1994). This paleogeographic reconstruction across the Alberta basin demonstrates the occurrence of progradational barred successions across large expanses of an intracratonic basin with lagoonal and sabkha settings spanning ~50-100 km.

Facies successions in the Marshall and lower Michigan Formations are similar in character to those found in the Triassic strata of the Alberta basin. Both successions exhibit a shallowing upward depositional trend with shoreface sandstone facies overlain by argillaceous lagoonal and evaporitic sabkha deposits. Inspection of geophysical well logs (Figure 18) covering the Doig, Halfway and Charlie Lake Formations reveal a coarsening upward gamma ray profile similar to that of the Marshall and lower Michigan

Formations in the Michigan basin. Similarly, both lithologic logs for the Triassic

Formations and log derived lithology tracks from the Marshall and lower Michigan

Formations (Figure 18) show a gradational transition from basal marine shale to sandstone with overlying lagoonal carbonates and evaporites. While Mississippian examples of this depositional system are not recognized in the adjacent Illinois and

Appalachian basins, the unique position of the Michigan basin adjacent to the Wisconsin

Highlands and the Canadian shield create the potential for substantial clastic sediment sources that in combination with arid paleo-climatic conditions during the early

Carboniferous may have driven a mixed progradational siliciclastic/carbonate system

similar to the Triassic strata of the Alberta basin.

Figure 16: Progradational model for the Doig, Halfway and Charlie Lake Formations (Edwards et al, 1994).

Figure 17: Paleogeographic reconstruction of facies belts from the Doig, Halfway and Charlie Lake Formations. Shoreface facies from the Doig and Halfway Formations are presented in the form of barrier island complexes within the reconstructed map while the Charlie Lake Formation is represented by lagoonal and sabkha facies. This analogous example of an ancient barrier-lagoonal-sabkha system shows widespread facies belts that stretch more than 50 km (Dixon, 2007).

Figure 18: Comparison of electric and lithologic well logs from the Triassic Doig, Halfway and Charlie Lake Formations (left)(Edwards et al, 1994) and well logs with calculated lithologies from the Mississippian Marshall and Michigan Formations. Note both successions show a transitional "cleaning upward" gamma ray log signature with a lithologic change from shale to sandstone. Sandstone lithologies in both logs are overlain by argillaceous and dolomitic sediments that are interstratified with evaporites. Vertical scales: 50 m/in (left) and 25 m/in (right).

Facies Associations and Interpretation

Analyses of depositional facies and sedimentary structures are consistent with wave dominated shoreline systems and were documented in the form of storm deposits and lags, swaley and hummocky cross stratification and planar laminated sands. Core descriptions in Appendix A reveal a shallowing-upward depositional motif for Marshall and lower Michigan sands that display facies successions and wireline log signatures that are typical of prograding wave-dominated shorelines. While sedimentary structures and characteristics are helpful in determining the processes in which a single facies may have developed, recognition of vertical and lateral relationships between facies assemblages is critical when attempting reconstruction of a depositional model. The interpretation of individual facies and depositional systems in this study rely on the integration of these factors. In addition, realistic constraints must be placed on any reconstructed depositional model as input to this model from the rock record is commonly specific to factors such as tectonic setting, eustasy, paleogeography, climate and diagenesis (Clifton,

2006). Depositional facies characteristics and interpretations are summarized in table 2.

Facies D1: Offshore Marine

The environmental interpretation for the D1 Facies is challenging due to the ambiguity of primary sedimentary structures and observed fossil assemblages.

Mudstones in particular are known to range in depositional occurrence from intertidal and supratidal settings to offshore deposits that develop below fair-weather wave base. Due to the range of possible shale/mudstone occurrences in marine depositional systems,

47 emphasis is on fossil content and the relationships of Facies D1 to vertically adjacent strata for interpretation.

Lingulid Brachiopods are observed throughout Facies D1 (figure 7) and are most common in dense lags along bedding planes. Individual fossils typically comprise whole and intact valves with orientations parallel to bedding planes. Lingulid brachiopods, including Orbiculoidea sp., are characterized by very thin valves and are thus quite susceptible to mechanical disaggregation by wave action. The presence of whole fossil valves in dense lag accumulations indicates that minimal transport occurred during short episodic events, such as storms, by waves and wave generated currents was likely (Zabini et al, 2010). Similarly, whole fossil casts and molds of Bivalves are also observed in concentrations along bedding planes in Facies D1 (Figure 7). A similar mode of occurrence for these fossil deposits likewise suggests they were formed during the action of short duration, episodic events such as storms, below fair weather wave base.

Sedimentary structures are rare in the Facies D1, however vertically adjacent sedimentary facies and the contact surfaces shared between them provide evidence for an offshore marine environment with strata being deposited below normal wave base. The base of the lowermost Facies D1 in core is in sharp contact with the underlying D7 facies, which is largely composed of dolomitic mudstone. This contact is denoted by a thin bioclastic limestone (Figure 7). Differences in primary sedimentary structures and lithology between the Facies D1 and D7 suggests a dramatic increase in water depth taking place between the times in which both of these facies were deposited. The bioclastic limestone is therefore interpreted as lag deposits following an abrupt flooding event prior the lowermost Facies D1 being deposited.

Additionally, the D1 facies shows both gradational as well as sharp contact with

Facies D2. The relationship between the Facies D1 and D2 is best described in the

Moeggenberg 2 core as a series of minor "coarsening upward "depositional packages comprised of Facies D1 mudstone with a gradational transition to finer-grained Facies

D2, the top of which have an abrupt contact with the overlying Facies D1, the beginnings

of an additional cycle. These depositional cycles progressively grade into sandy facies

that are eventually succeeded by the D7 and D8 facies of lagoonal/sabkha origin.

Facies D2-A:Middle-Lower Shoreface

The presence of low angle cross-bedded, fine- to medium-grained and graded sandstone beds punctuated with bioclastic lag deposits indicates oscillatory and combined-flow conditions that are attributed to storm wave-action in shallow marine environments below normal wave base. Cross stratification observed in Facies D2-A exhibit concave alignment of a series of successively truncating beds indicating an environment in which the aggradation rate is lower and scouring more frequent in the shoreface setting (Plint in James & Dalrymple, 2004).

Facies D2-B: Middle Shoreface

Sedimentary structures in the D2-B Facies including truncation of firmly-lithified,

lower-energy bedsets, overlain by coarse-grained, fining upward intervals in alternating succession is indicative of alternating periods of energy as related to oscillatory/unidirectional combined-flow conditions. Oscillatory conditions with

increased wave action are dominant at the onset of storm activity in which firm and loose

sediment may be eroded and suspended. As storm activity wanes, suspension settling in

waning oscillatory conditions results in the deposition of fining upward, planar laminated

bedsets at the termination of the storm sequence (Plint in James & Dalrymple, 2004).

The presence of Skolithos burrows at storm sequence boundaries, also provide evidence

for middle shoreface deposition in which bioturbation is more intense during periods of

relative low energy between storm events.

Facies D3: Middle-Upper Shoreface

Wave induced sedimentary structures such as asymmetrical ripples indicate a

gradational transition from combined-flow, oscillatory dominated wave influence to increased unidirectional flow associated with shallowing water depths. The presence of local cm-scale mud intraclasts in non-bioturbated intervals may indicate periods of increased wave action as related to storm activity. Similarly, bioturbated intervals exhibit both horizontal and vertical burrowing indicating some alternating frequency of periods of relative tranquility and elevated energy conditions. Influences associated with the observed sedimentary structures suggest wave action consistent with upper shoreface conditions in a low gradient, ramp setting.

Facies D4: Foreshore

The highly rhythmic interbedding of thinly bedded, planar laminated fine-grained

sandstone suggests rapidly alternating energy during the time of deposition. Such high

frequency changes in energy can occur in both tide dominated and wave dominated settings with different modes of deposition. Ebb and flood energy in tidal dominated

systems provides this consistent frequency change, though deposition of interbedded mud

and sand lenses typically occur in relation to diurnal and neap-spring tides. An alternative mechanism, in wave dominated, typically sandy depositional systems, as seen in this facies would be that breaking wave energy controlled deposition in a foreshore setting. As waves head landward, wave height above still water level increases until water depths are nearly 1.3 times the wave height resulting in wave-break in the surf zone. Energy from wave-break is translated as a landward rush of water further landward in the swash zone, a zone of shoreface lying just above the low tide line (Plint, in James

& Dalrymple, 2004).

Facies D5: Backshore

The absence of sedimentary structures and the presence of apparent syndepositional oxidation suggests that the Facies D5 sandstone facies was subjected to a limited degree of subareal exposure as part of a shallowing upward marine succession.

Winnowing of lithic sand grains in the Facies D5 may be further evidence of subareal exposure and subsequent reworking by eolian and biologic processes.

Facies D6: Intertidal

The presence of skeletal grains throughout this Facies D6 indicates a marine

origin, though the presence of different fossil types in cored intervals may indicate

similar energy condition common to a number of depositional settings. Thus, depositional

setting may be best determined depending upon vertically adjacent facies associations.

The D6 facies is typically found in association with backshore and lagoonal facies, which

reflect a depositional setting that encompasses areas of tidal influence. Facies D6 is

typically seen as transitional in core between super- and subjacent facies with some minor occurrence amongst shoreface sandstones. On the basis of facies association

Facies D6was deposited in a tidally influenced settings such as tidal inlets, intertidal zones and tidal flats within an environment also influenced by a prograding, wave dominated/influenced shoreline.

Facies D7: Restricted Lagoon

The lithologic transition from coarse-grained, siliciclastics-dominated facies

(below) to muddy, carbonate-dominated Facies D7 (above) indicates progressive restriction and isolation from open marine environments up-section. Interpretation of the underlying, genetically related facies successions subjacent toFacies D7 indicates a wave- dominated, shallow marine setting. Longshore drift is shown to be a major component of subaerial, barrier island features, capable of isolating back-barrier facies from normal marine circulation and shoreface deposition (Edwards et al, 1994). This isolation and restriction provides elevated salinity levels and decreased influence on sedimentation due to open marine wave and current processes. The presence of algal laminations and local anhydrite are consistent with a tropical-arid, restricted marine setting in which

chloroalgal associations areknown to thrive (Lees and Buller, 1972). Facies D7 is also

distinct in that it occurs with scour-erosional contact with overlying coarse grained facies.

This contact is discussed later in this paper as a possible shoreface ravinement surface.

Facies D8: Coastal Sabkha

The occurrence of displacive evaporite textures in Facies L8 is diagnostic of

deposition in an evaporative, mud flat setting. The origin of laminated dolomite may be similar to that of the Facies L7, in which shallow water restriction of the depositional setting and tropical-arid paleoclimate conditions resulted in a highly restricted environment suitable for chloroalgal associations, only,in a supratidal setting. These strata were then partially replaced by primary gypsum formed by capillary evaporation and groundwater flux in a coastal setting. Periodic surface flooding due to wind or storm activity may also have provided sufficient recharge to produce cumulative evaporites deposited in saline ponds, a contemporaneous feature observed in coastal sabkha environments (Schreiber and Tabakh, 2000).

Examination of cored intervals in wells such as the MCGS 8-31(Figures 19) reveal a predictable and repeatable succession of facies units that are for the purposes of this study have been arranged into facies associations (Figure 20). These associations reflect the shallowing-upward character of a single prograding shoreface succession with individual associations being separated and marked by a transition to facies that indicate an abrupt increase in water depth relative to the underlying association. Core analysis of the MCGS 8-31 well provides an excellent example of these facies relationships.

Figure 19: (next two pages) MCGS 8-31 core description including sedimentary structures, facies type, and associated well log curves. Further reference to shallowing-upward cycles and facies unit colors can be found in figure 20.

Figure 20: Idealized facies succession for a prograding clastic shoreline association including color coded depositional facies and shallowing-upward motif (inverted red triangle) used in core descriptions.

Depositional Model

The depositional model developed for the Marshall and lower Michigan strata

was constructed based primarily on the diagnostic characteristics of facies identified as

well as regionally recognized facies successions. Wave dominated facies in core are

interpreted as shoreface sandstones (D1-D5) that were deposited as part of a

progradational barrier-strand plain facies succession. Heterolithic and laminated

dolomite lithologies (D6-D7) were deposited as tidal inlet or restricted lagoonal facies

with overlying anhydrite and minor dolomitic deposits (D8), are interpreted as supratidal

sabkha environments.

The presence of coarsening-upward siliciclastic facies with internal shallowing- upward wave dominated structures conformably overlain by restricted lagoonal facies and peritidal carbonates and evaporites (Figure 21) is strong evidence for a progradational Barrier-Shoreface/Strandplain system. Evaporite facies in core and well logs appear to be laterally extensive across the basin and are almost always present at the top of shallowing-upward successions. Contact between shallowing-upward successions is variable, though the transition is marked in core and well logs by an abrupt return to deeper facies marking the base of the overlying succession.

Throughout the Mississippian, the Michigan basin was characterized as a shallow marine ramped-embayment that was open to the modern south during the Carboniferous

(Smith and Read, 2001; Miall and Blakey, 2008). The position of the Michigan basin adjacent to positive features such as the Wisconsin highlands and the Canadian Shield to the north and northeast almost certainly were clastic sediment sources during the

Mississippian.

Figure 21: Idealized depositional model proposed for the Marshall and lower Michigan Formations. Offshore and shoreface deposits (D1-D4) are overlain by barrier, intertidal and lagoonal deposits (D5-D7) during basinward progradation with topset beds of supratial dolomite and evaporites representing the culmination of individual facies successions. An example of an idealized facies succession represented by this model is shown in the upper left section.

Flooding Surfaces and Associated Ravinement

The contact relationships between individual facies and facies successions is of particular importance in determining chronostratigraphically significant events such as relative sea-level rise and fall that directly impact sedimentation in diverse depositional systems. Instances of abraded and abrupt contact between facies successions were identified in the Marshall and lower Michigan Formations. Contact relationships observed in core from the Moeggenberg 2 (Figure 22), MCGS 8-31 (Figure 23), and

MCGS 9-71 wells showing abrupt and sometimes erosional contacts between lagoonal dolomite (D7) facies and overlying upper shoreface (D3) or offshore marine (D1) facies.

These abrupt changes in lithology can be traced as a single chronostratigraphically

(sequence stratigraphic) significant surface from the northeastern limits of the study area extending south and southwest towards the center of the basin where the contact appears to grade into the upper portion of the Coldwater Formation (discussed in Chapter V). In sequence stratigraphic analysis, these contacts imply an abrupt increase in water depth with minor submarine erosion and constitute "flooding surfaces" according to Van

Wagoner et al., (1990).

Embry (2009) postulates that flooding surfaces exists in both gradational or scoured forms representing "maximum regressive surfaces" and "unconformable shoreline ravinement surfaces” respectively. Textures associated with flooding surfaces may include erosional lag deposits, reworked sands and fossil skeletal debris (Matchen and Kammer, 1994). Flooding surfaces often contain evidence of submarine erosion or

"ravinement surfaces" comprised of centimeter to decimeter, sand and gravel lags lying just above a subjacent erosional surface (Plint, in James and Dalyrmple, 2010). Clasts in

59 these lag deposits are derived directly from underlying facies. This physical evidence for unconformable shoreface ravinement can be attributed to erosion by wave action and turbulent flow in the surf zone, typical of shoreline erosion (Plint, in James and

Dalyrmple, 2010). Further discussion of these surfaces and sequence stratigraphy is discussed in Chapter VI.

Figure 22: Bioclastic limestone at 1,299' marking the lowermost contact of Facies D1 with underlying lagoonal dolomite (D7) in the Moeggenberg 2 well.

Figure 23: Shoreline ravinement surface at 1,395.5' in the MCGS 8-31 well separating lagoonal facies D7 and overlying upper shoreface facies D3. Note intraclastic lags (LD) near the 4" tick mark, probably derived from the immediately underlying lagoonal dolomite (D7).

Table 2: Summary of Depositional Facies Grain type Sedimentary Ichnofacies/ Facies/Lithology Occurrence Color Interpretation and Texture Structures Biota Concentrate d Identified in Very fine Orbiculoide Offshore the lower grained a and dark deposition D1/Fossiliferous portions of sandstone/sha Horizontal bivalve gray to below fair- mudstone-shale the le, thin basal bedding assemblages black weather wave- Moeggenber bioclastic on bedding base g 2 Core limestone planes with vertical burrows Lower portions of SL-175A, Low angle SL-217A Fine to Swaley cross and SB-15 Unidentified medium stratification cored Olive brachiopod D2-A/Cross grained (SCS) with intervals. green to fossils Middle-Lower bedded lithic micaceous bioclastic lag Typically red amongst Shoreface sandstone quartz and deposits, representativ brown Skolithos lithic crossbedding e of the ichnofacies sandstone and rare vertical central burrows portions of sandstone lithologies Lower portions of cored SL- 175A and Fine to very Vertical burrows SL-217A coarse filled with Olive intervals. grained coarser grained D2-B/Intraclastic green to Skolithos Middle-Lower Typically micaceous sediment, lithic sandstone red ichnofacies Shoreface representativ quartz and intraclasts brown e of the lithic derived from central sandstone underlying beds portions of sandstone lithologies Fine to Upper medium Heavily Light portions of grained bioturbated with D-3/Bioturbated green to Skolithos Upper sandstone micaceous sparse lithic sandstone light ichnofacies Shoreface lithologies in quartz and sandstone/mudst red all cores lithic one intraclasts sandstone Upper portions of Fine grained sandstone Light to D-4/Finely micacerous lithologies in medium Sparse Rare Foreshore- laminated lithic quartz and all cores red bioturbation Skolithos Swash Zone sandstone lithic except brown sandstone Moeggenber g 2

62 Table 2 - Continued Grain type Sedimentary Ichnofacies/ Facies/Lithology Occurrence Color Interpretation and Texture Structures Biota Observed beneath Light Very fine D-5/Structureless lagoonal tan to Backshore/Barr grained None None Sandstone deposits only light ier sandstone in the MCGS brown 8-31 Observed in Dark Very fine Horizontal and D-6/Heterolithic all cores gray Rare grained vertical burrows, sandstone- except the to Skolithos Intertidal sandstone/m wave rippes and mudstone Moeggenberg light ichnofacies udstone wave foresets 2 tan Laminated, rare Observed in horizontal the MCGS 8- Mediu burrows, Rare D-7/Dolomitic 31, MCGS 9- m to Mudstone/W unidentified horizontal Restricted mudstone- 71, dark ackestone skeletal grains, burrows and Lagoon Wackestone Moeggenberg brown anhydrite brachiopods 2 and Yake et cemented vugs al 1 and fossil molds Light Mudstone Observed in to with "Chickenwire" D-8/Cumulative- all cores mediu enterolithic mosaic and nodular anhydrite except the None Coastal Sabkha m and/or Palmate and dolomite Moeggenberg gray cumulative anhydrite 2 and SB-15 brown anhydrite

63 CHAPTER IV

PETROPHYSICAL ROCK MATRIX ANALYSIS

The integration of core and wire-line log data using correlation/calibration techniques has proven invaluable and critical to modern subsurface geological studies.

While conventional core provides an unequivocal representation of rock types in the subsurface, the coring of every well that is drilled is impractical due to time and cost.

The development and calibration of modern lithology log packages such as CNL-FDC-

PEF logs to conventional core facilitates interpretation and extrapolation of wellbore lithology and other properties in the subsurface (Rock, 2011). The use of the geological software IHS® PETRA in conjunction with core sample observations was used to execute petrophysical analysis and ultimately demonstrate lithofacies distribution and geometry in the Marshal-Michigan formations in this study.

The use of well logs in the absence of cored materials to determine wellbore lithology is fundamental to many subsurface geologic studies. Well log analysis and identification of log facies in this study rely primarily on calculated, log-derived lithology that require a specific set of well log curves as inputs. These calculations are based on the author’s FORTRAN program, using IHS® PETRA software to execute the analysis

(Appendix. C). The core of this program is based on Doveton’s (1994) rock matrix composition program and in part on a very similar analysis conducted by Rock (2011) on

Devonian strata in the Michigan basin. The original rock composition program written by Doveton (1994) requires three input logs, NPHI, RHOB and PEF. Mineral and fluid values (Table 3) relative to each input log are used to construct a matrix value table, from

which inverse coefficients of four outputs (Quartz, Dolomite, Calcite, & Porosity) can be

calculated using matrix row operations. Proportional rock matrix composition can then

be determined by taking the product of the well log values and inverse coefficients,

including a value of unity.

This lithology-based well log analysis in particular was used effectively by Rock

(2011) investigating the mixed carbonate-siliciclastic Sylvania Sandstone in the Michigan basin, however the need to identify shale and evaporite facies in the Marshall and lower

Michigan Formations required additional modification of the log analysis program in order to correctly identify these lithologies. Doveton (1994) provided additional insight into well log response relative to the original matrix composition program and the erroneous determination of other lithologies, including shale and evaporite.

Table 3: Petrophysical Properties of Common Minerals and Fluids

RHOB & NPHI Actual Density Measured Density Photoelectric Curve Mineral/Fluid (g/cc3) (g/cc3) (barns/e) Separation RHOB left of Quartz/Silica 2.654 2.644 1.810 NPHI Limestone 2.710 2.710 5.080 No Separation RHOB right of Dolomite 2.870 2.877 3.140 NPHI RHOB right of Anhydrite 2.960 2.960 5.050 NPHI NPHI left of Salt/Halite 1.000 2.040 4.650 RHOB Fresh Water 1.000 1.000 0.358 N/A Salt Water 1.150 1.135 0.807 N/A

Doveton (1994) described the three-mineral matrix model (Quartz, Calcite and

Dolomite) as a numerical representation of the RHOmaa-Umaa crossplot (Figure 24).

Well log values of additional lithologies such as shale and anhydrite will numerically

solve as impossible solutions outside of the RHOmaa-Umaa crossplot triangle (Figure

25). Doveton (1994) described the influence of measured physical properties in both

anhydrite and shale in well logs using the three-mineral model as resulting in negative

field solutions relative to the RHOmaa-Umaa crossplot triangle (Figure 25). Using the

negative field solutions of shale and anhydrite provided in Doveton’s work, end-member

compensation in the original Quartz, Calcite and Dolomite model can be correctly

normalized to include additional log-derived lithologies.

While the addition of shale and anhydrite to the original model requires the ability to correctly normalize the existing output end-members, it also requires the ability to independently calculate the proportions of these lithologies. The gamma ray log (GR) has been widely used in stratigraphic and petroleum geology applications as a “shale log” from which “clean” shale-free rock is distinguished from those rocks containing some amount of shale. The absorption of thorium by clay minerals typically found in shale provides a pronounced gamma ray signature when compared to carbonate, evaporite and quartzose sandstones, which typically retain relatively low levels of radioactivity.

Doveton (1994) describes the volumetric estimation of shale proportion can be obtained by locating both “clean” shale-free rock as well as rock completely comprised of shale that can be directly measured in terms of gamma ray API value. Interpolation of the two extreme values can then be applied to gamma ray values measured along the wellbore to

estimate the proportional amount of shale in those zones (Doveton, 1994). This method

was used to determine shale content in this petrophysical analysis and subsequent

normalization to other end-members of Doveton’s (1994) original mineral matrix model.

Parameters for shale volume are shown in table 3.

Marine evaporite, most commonly anhydrite, are present in the Marshall and

lower Michigan formations and are similar to clean carbonates and non-feldspathic

sandstones with low gamma ray signature. This property makes the recognition of these

interbedded rock types difficult to distinguish. However, the high density of anhydrite,

when compared to the average density of other lithologies (Table 3), is a diagnostic

property for calculating the proportion of anhydrite. Similar to the previously described

interpolation method using gamma ray to calculate shale volume, bulk density (RHOB)

was used to establish an anhydrite-free baseline from which anhydrite proportions are

calculated.

Core-to-Log Correlation/Calibration

Core-to-log correlation/calibration is an analytical process that can be performed

on wells that have both core and wire-line logs. Cores used in this study were initially

characterized in terms of lithofacies and depositional facies and then compared to wire- line log data. Using comparison of this data allows for depth shift and calibration of log derived properties and cored lithologies in addition to providing log signature definition for individual facies and facies trends.

Figure 24: RHOmaa-Umaa crossplot diagram showing graphical solutions for various minerals that commonly compose sedimentary rocks (Doveton, 1994).

Figure 25: RHOmaa-Umaa crossplot diagram showing "impossible solution" fields for Doveton's (2004) original three-mineral model. Negative fields for quartz, dolomite and calcite are indicated as well as the corresponding fields of shale and anhydrite lithologies (Doveton, 1994).

The core-to-log correlation/calibration analysis in this study was difficult since only one of the cored wells contained all of the necessary logs to generate calculated matrix values. Nevertheless 6 of 7 studied cores contained one or more well logs upon which confident correlation could be established to nearby wells with full log suites. An example of indirect core-to-log correlation of the MCGS 8-31 cored interval is shown in

Figure 19. Other difficulties were encountered with incomplete core coverage throughout the entire interval of interest in the Marshall and lower Michigan formations. While cored intervals containing important stratigraphic contacts and successions were studied, a continuous and comprehensive core encompassing the entire interval of interest was not available, particularly the contact between the Marshall and Coldwater formations. In this case, in lieu of conventional core, stratigraphic relationships observed by previous researchers in outcrop and interpreted from drill cuttings were relied upon for the construction of a depositional model and stratigraphic delineation.

Facies Association Mapping

Mapping of the subsurface distribution and geometry of lithologic units and successions has a wide range of geologic applications that in particular have been used successfully in oil, gas and mineral exploration efforts. The recognition of genetically related facies associations, each being comprised of one or more depositional facies allow for predictive efforts in mapping the spatial distribution of these associations in paleo- depositional systems. Four log facies units were identified in Marshall and lower

Michigan strata and are representative of depositional facies recognized in core. A type log including log facies characteristics and facies associations can be found in figure 26.

Figure 26 (previous page): Type log covering the upper Coldwater Shale through the Marshall and lower Michigan formations according to well log signatures described by Westjohn & Weaver (1994). The top of the Coldwater Shale is picked at the first high radioactive response below the Marshall Sandstone and the top of the Upper Marshall/Michigan Stray is the first high radioactive "kick" before the Shales and evaporites of the Michigan Formation. Associated log facies, depositional facies and environmental interpretations derived from core analysis and core-to-log calibration for this study are also shown.

Log Facies L1-A/B

Log Facies L1-A/B are the main clastic log facies recognized in this study and

while these units are identical in terms of well log signature and representative

depositional facies, they constitute two separate stratigraphic entities. Log Facies L1-

A/B are characterized in wire-line logs by moderate to low gamma ray values ranging

from 75 - 25 API units. The NPHI log lies to the right of the RHOB log in the upper

portions of Log Facies 1-A/B and is accompanied by a low gamma ray log signature (25 -

65 API) and PEF values near 2 barns/e, consistent with sandstone lithology. In the lower

portions of Log Facies L1 and in particular those portions directly overlying Log Facies

2, the NPHI log lies to the left of the RHOB log accompanied by higher range gamma ray

values (65 - 75 API) and elevated PEF values near 3 barns/e which is consistent with the

increased siltstone content, mentioned by previous workers (Lilienthal, 1978; Westjohn

& Weaver, 1998) in the lower portions of the Marshall. Core-to-log calibration indicates

that Log Facies L1-A/B represents barrier/shoreface depositional facies D2-D6 from core studies (Chapter 3 and Figure 26). The contact between the Log Facies L1 and L3 in core is recognized as both erosional as well as conformable depending on the nature of the transition.

Log Facies L2

The upper and central portions of the Marshall and lower Michigan formations are

represented by Log Facies L2. Gamma ray log values of Log Facies L2 range from 75 to

>10 API units. Log facies L2 is perhaps the most complex log facies in that three

primary lithologies are represented, including heterolithic mudstone/sandstone, dolomite and anhydrite of the D6-D8 depositional facies. The NPHI log lies to the left of the

RHOB log throughout Log Facies L2 though higher gamma ray log values (60-75 API)

indicate the heterolithic Facies D6. Lower range gamma ray log values (>10 API), PEF values near 5 barns/e and RHOB values in excess of 2.9 g/cm3 are indicative of anhydrite

of Facies D8. Dolomitic Facies D7 typically display moderate gamma ray log values

from 15-40 API and PEF values near 3 barns/e. Core-to-log calibration of depositional facies indicates that the L2 log facies encompasses deposits of lagoonal/sabkha origin.

Contacts between the L2 and other log facies are discussed in the previous facies sections.

Log Facies L3

Log facies L3 is the basal log facies observed in this study and represents the upper part of the Coldwater Shale. Log Facies L3 is characterized by a high gamma ray log signature in the range of 110 - 130 API units. The NPHI log is right (higher apparent porosity) of the RHOB log and, along with high gamma ray log value, is consistent with typical clay mineral-rich shale/mudstone lithology. From west to east across the

Michigan basin, the character of Log Facies 3 is transitional to an increasingly "saw-

toothed" gamma ray log response with interstratified spikes of lower gamma ray values

from 75-90 API (Figure 26). These observations are consistent with previous studies

who note an increased presence of sand in the upper portions of the Coldwater. Log

Facies L3 is only recognized in core as the D1 shale/mudstone depositional facies and is

interpreted as offshore, marine shelf deposits formed below fair-weather wave base

(Figure 26). Contact between log facies L3 and L1 is gradational and is marked by the

appearance of the last high gamma ray spike (110 - 130 API) below the base of the

Marshall sandstone. Contact between Log Facies 3 and Log Facies 2 is also recognized in core and wire-line logs and is characterized by an abraded/erosional contact at an abrupt lithologic change in core from dolomite to mudstone/shale, upwards.

Investigation of the Coldwater Shale as described in previous literature is not a

primary focus of this study and this unit was not present in any of the available cored

intervals. However, interstratified extensions of "Coldwater-like" facies have been

recognized by other researchers including Westjohn and Weaver (1998). These

"Coldwater-like" facies are present in core and wire-line logs and are of particular interest

to this study.

Facies Mapping

Correlation and mapping of log facies is a fundamental component of this study that, in conjunction with stratigraphically significant surfaces recognized in core and in well logs, aid in the identification of genetically related successions in lower

Mississippian strata in the Michigan basin. Individual log facies units were identified and

mapped across the Michigan basin and are shown in figures 27 - 30. Cross sections

across the study area are also shown in figures 31-34 of Chapter V. Recognition of the

L1-A and B units as separate occurrences of progradational shoreface sandstone deposits is of paramount importance in this study and provides the basis of discussion concerning depositional mechanisms affecting the Michigan Basin during the Mississippian.

Isopach Map L1-A

The L1-A Isopach map (figure 27) encompasses the lowermost stratigraphic unit in this study and consists of barrier/shoreface facies that lie directly on the Coldwater

Shale. The L1-A isopach attains a maximum thickness of nearly 230 ft in the

easternmost portion of the study area in Bay County, thinning progressively to the west

and south where stratigraphic "pinchout" of the unit is observed. Direct observation of

stratigraphic pinchout in cross section with closely spaced wells is observed along the

western border of Mecosta County in Figure 27 and is extrapolated along depositional

strike to the southeast. Apparent thickening of the L1-A isopach is observed in the

northwest portion of the study area in northwest Osceola county where isopach

thicknesses as high as 170 ft are present. The L1-A Unit is overlain by the L2 log facies

in the northeast as well as the L3 log facies in the south and southwest where the L1-A

unit thins to a stratigraphic pinchout (Figure 31).

Isopach Map L1-B

A similar log facies unit is recognized in this study as Log Facies L1-B. Log

Facies L1-B is the uppermost unit as well as the most aerially extensive unit mapped in the Marshall Sandstone and is found throughout the Michigan basin with the exception of

those areas where the L1-A unit is thickest. Examination of Log Facies L1-A and L1-B

isopach maps shows an inverse relationship of depositional thickness. Where one unit is

thick the other is thin, an observation that has been previously noted by Westjohn and

Weaver (1998) (figure 28). Similarly, the L1-B unit is comprised of barrier/shoreface

facies deposited in a shallow marine system. This unit is overlain by transitional

mudstones and evaporites of the Michigan Formation that are representative of marginal

marine sabkha deposits.

Isopach Map L2

Log Facies L2 lies stratigraphically above Log Facies L1-A in the northern part of

the study area where L2 is the basal portion of the Michigan Formation. The L2 unit

represents lagoonal/sabkha depositional facies (depositional facies D6-D8) and thins to

the west and south, where it is interstratified with and overlain by Log Facies L1-B and

L3 units. Log Facies L2 thickens to a maximum of 70 ft in southeastern Roscommon

County, and shows an increase in evaporite content to the northeast. Log Facies L2 exhibits a stratigraphic pinchout trend similar to that of Log Facies L1-A. This relationship is demonstrated in all cross sections (Figures 31-34). Log Facies L2 always directly overlies Log Facies L1-A and these strata are interpreted to be genetically related representing a progradational shoreline-barrier island, and back barrier lagoon.

Figure 27: Isopach map of the L1-A Unit. Warm colors indicate greater isopach thicknesses with maximum thickness of 230 ft in Bay County while cool colors indicate lower isopach thicknesses. Subcrop of the Marshall (Red) and Michigan (Green) Formations is also shown.

Figure 28: Isopach map of the L1-B Unit. Warm colors indicate greater isopach thicknesses with maximum thickness of 220 ft in Ingham County while cool colors indicate lower isopach thicknesses. Subcrop of the Marshall (Red) and Michigan (Green) Formations is also shown.

Figure 29: Isopach map of the L3 Unit. Warm colors indicate greater isopach thicknesses with maximum thickness of 70 ft in Roscommon County while cool colors indicate lower isopach thicknesses. Subcrop of the Marshall (Red) and Michigan (Green) Formations is also shown.

Isopach Map L3

Log Facies L3 is the least aerially extensive unit recognized in this study. Log

Facies L3 was previously described by Westjohn and Weaver (1998) as a siltstone/shale

"corridor" roughly 15 miles wide overlying the base of the lower Marshall Sandstone and

contains intercalated evaporite and dolomite. Inspection this entity in well logs as

described by Westjohn and Weaver (1998) and overlay of this feature on isopach map

values of the Log Facies L3 unit show that they are in fact the same stratigraphic entity

(Figure 30).

Westjohn and Weaver (1998) describe the L3 unit as a discrete feature or

“corridor” of “Coldwater-like” siltstone and shale that thins stratigraphically in all directions, grading into Marshall Sandstone units. Detailed mapping of this feature conducted in the course of this study, which include newly drilled wells (2008) along the flanks of this northwest-southeast trending “corridor” indicate an even greater lateral extent of this unit. Log Facies L3 merges into strata equivalence with the upper

Coldwater Shale to the southwest. The thickening of Log Facies L3 occurs in association with thinning of the underlying L1-A unit to eventual stratigraphic pinchout. This inverse thickness relationship was probably controlled by some stratigraphic event. Log Facies

L1 also extends further northeast than originally described by Westjohn and Weaver

(1998), thinning across a broad front towards subcrop in the northeast in Isabella,

Osceola and southwestern Clare counties where it grades into sandstone. The L3 Log

Facies unit in cross sections (Figures 31-34) is shown to directly overlie the L1-A as well as the L2 Log Facies units where present and is always gradationally overlain by the L1-

B Log Facies.

Figure 30: Isopach map of the L3 Unit. Warm colors indicate greater isopach thicknesses with maximum thickness of 40 ft in Montcalm County while cool colors indicate lower isopach thicknesses. Subcrop of the Marshall (Red) and Michigan (Green) Formations is also shown. Location of "silt/shale corridor" previously identified by Westjohn and Weaver (1998) is shown with the dashed red line.

Table 4: Summary of Petrophysical Properties of Log Facies Units

Log Separation GR (API PEF RHOB NPHI Depositional Environmental facies of RHOB units) (b/e) (g/cc ) (%) Facies Interpretation Units and NPHI 3 Log Low to RHOB right Barrier/ facies very low, 2 2.2-2.35 17-19 D2-D5 of NPHI Shoreface L1 - A/B >35 Log Low to RHOB left 3.0- Restricted facies very low, 2.78-3.0 16-7.5 D6-D8 of NPHI 5.5 Lagoon/Sabkha L2 >20 Log RHOB right Offshore facies High, 90< 3 2.6-2.7 14-17 D1 of NPHI Marine L3

CHAPTER V

SEQUENCE STRATIGRAPHY

A sequence stratigraphic approach to the subdivision and correlation of various strata is based on the fluctuation of local and/or eustatic sea level (Van Wagoner et al,

1990; Matchen and Kammer, 1994). Relative sea level rise produces transgressive deposits while sea level fall produces regressive or progradational deposits with each type exhibiting different characteristics, textures and spatial variability (Matchen and

Kammer, 1994). Sequence stratigraphic units are divided into three basic units; sequence, systems tract, and parasequence with each representing the relative magnitude of a depositional event (Embry, 2009). The term "parasequence" was originally defined by Van Wagoner et al (1988) as "a relatively conformable succession of bed or bedsets bound by marine-flooding surfaces". These flooding surfaces are further described as a surface separating younger strata from older, across which there is an abrupt increase in water depth (Van Wagoner et al, 1988). Instances of marine flooding in the Marshall

Sandstone were described in cored intervals in this study and resulted in formation of important sequence stratigraphic surfaces. These surfaces are used to delineate depositional units, including parasequences, identified in this and previous studies and their spatial distribution in a chronostratigraphic framework.

The Marshall sandstone is characterized in core as a progradational barrier/shoreface deposits (Chapter 3 & 4) that resulted in a widespread "shallowing upward" facies successions throughout the Michigan basin. The progradational nature of these deposits suggests that sedimentation rates exceeded the rate of accommodation

space within the basin during Marshall deposition. Progradational shoreline successions

in the Marshall Formation also show widespread lateral continuity, typical of wave-

dominated siliciclastic shoreline deposits, and supports spatial interpolation and

extrapolation of facies units by means of wire-lines logs.

A single, widespread flooding surface is identified in core and well logs across the

Michigan basin that effectively subdivides the Marshall Sandstone into two genetically- related stratigraphic units. For the purpose of this study these units are referred to as parasequences, though additional bounding flooding surfaces above and below the

Marshall are not present in this study. The lower, Parasequence "A" consists of the conformable Log Facies L1-A and L2 (Figures 31-32) that exhibit progradational geometries from the east and northeast, southwestward into the Michigan basin. An extensive flooding surface is traced above these units, represented by backward-stepping log facies from shoreface sandstones to distal marine shale along the southwestern margin of the facies tract. This transgressive "tongue" is mapped as the Log Facies L3

(Figure 30) and thins progressively landward to the northeast (Figures 31-34). Landward translation of this flooding surface to the northeast is mappable with evidence in core as well as wire-line logs in the form of proximal lagoonal carbonates (Log Facies L2) erosionally overlain at a shoreline ravinement surface by more basinal, shoreface sandstones (Log Facies L1-B) upsection. Log Facies L1-B has inverse depositional thickness relationship with parasequence "A”, which suggests that local accommodation space for this unit was probably controlled by the previous deposition of parasequence

"A" during middle to late Marshall deposition (Figures 31-34).

Parasequence "B" is the uppermost and most aerially extensive sequence

stratigraphic unit identified within the Marshall Formation, consisting of Log Facies L3

and L1-B underlain by parasequence "A". Progradational facies successions in

parasequence "B" are indistinguishable compared to parasequence "A" in core and well

logs and are thickest in those areas not underlain by that unit. Parasequence "B" is

directly overlain by mudstones, carbonates and evaporites of the Michigan Formation in

core and in well logs with no apparent break in deposition.

Three cross sections were constructed illustrating the stratigraphic relationships of

the Marshall Formation across the Michigan basin (Figures 31-34). These progradational

facies units distributed across the Michigan basin suggests ample sediment supply during

an overall relative sea level high stand during Marshall deposition with at least two periods of progradation separated by a single flooding event. It is difficult extrapolating and resolving stratigraphic relationships in the Marshall Sandstone because of a lack of well data in the southern Michigan basin as well as along the basin margins.

Figures 31-34 (Next pages): Constructed cross sections showing lateral distribution and correlation of identified log facies units. A single flooding surface (solid-dashed line) is correlated throughout the Michigan basin in all three cross sections and separates two distinct sequence stratigraphic successions that comprise the Marshall Formation.

Figure 31

Figure 32

Figure 33

Figure 34: Cross section map for figures 31-33 showing locations of wells and lines of section across the Michigan Basin. Subcrop of the Marshall (Red) and Michigan (Green) Formations is also shown.

CHAPTER VI

DISCUSSION AND CONCLUSIONS

Early Mississippian Paleoclimate, Tectonics and Eustasy

Stratigraphic analysis of the Carboniferous in the eastern United States was the focus of numerous studies, which included factors such as glacio-eustasy, tectonic uplift, and climate fluctuation. Plate tectonic reconstructions of the early Mississippian show

Euramerica in humid -tropical latitudes during the Kinderhookian and early Osagian.

This relatively wet climate produced an influx of coarse-grained, siliciclastic sediment of the Borden and Slade Formations in the Appalachian foreland basin (Scotese and

McKerrow, 1990; Cecil, 1990; Ettensohn et al., 2009; Towne, 2013). Sedimentation later transitioned to marine carbonates and evaporites as Euramerica drifted into arid latitudes during the late Osagian and Meramecian (Scotese and McKerrow, 1990; Cecil, 1990;

Town, 2013). A similar sedimentological transition is recorded in the Michigan basin during the Osagian through the Meramecian with deposition of coarse-grained siliciclastics of the Marshall Sandstone overlain by marine carbonates and evaporites of the Michigan Formation (Figure 35).

Figure 35: Stratigraphic column illustrating long and short term sea level changes (Haq and Schutter, 2008) and paleoclimate curves (Cecil, 1990) during the Carboniferous with respective correlation to Michigan basin Stratigraphy (Towne, 2013; Catacosinos, 2000). Inspection of the Osagean Marshall Formation (Green) Paleoclimate interpretation across the eastern United States during the late Devonian and early Mississippian was conducted by Cecil (1990) through the correlation of climate-sensitive rocks in the Appalachian and Illinois basins. Examination of these paleoclimate curves shows tropical conditions and indicates that Marshall sedimentation initially took place during relative sea level highstand conditions in a tropical wet-dry paleoclimate. These conditions transitioned to an arid paleoclimate during declining sea level during late Osagian time.

Paleoclimate

Paleoclimate interpretation across the eastern United States during the late

Devonian and early Mississippian was conducted by Cecil (1990) through the correlation of climate-sensitive strata across the Appalachian and Illinois basins. These paleoclimate curves (Figure 35) show tropical conditions with a seasonal wet-dry climate persisting across the eastern United States during the Kinderhookian and early Osagian. During the late Osagian and into the early Meramecian, climate shift to tropical-arid conditions occurred and continued throughout much of the Mississippian. Correlation of these

climate curves to Michigan basin strata (Figure 35) place deposition of the Marshall

Sandstone during a predominantly tropical wet-dry climate with transition to tropical-arid

conditions during the early Meramecian and deposition of the Michigan Formation.

Cecil (1990) also discusses the occurrence of coarse-grained siliciclastic units as, in-part,

related to prevailing tropical-wet conditions that would have accelerated weathering and

overall input of siliciclastics into cratonic interior basins in the eastern United States.

Inversely, arid conditions would have a reversing effect, limiting siliciclastic input due to

decreased weathering and erosion of clastic materials (Cecil, 1990).

Eustasy

Sea level fluctuations during the Paleozoic presented by Haq and Schutter (2008

Figure 35) indicate sea level fall during the late Devonian with a punctuated fall near the

Devonian/Carboniferous boundary. Deposition of clastics-dominated deltaic deposits of the Bedford and Berea Formations in the Michigan and Appalachian basins (Harrell,

1991; Lilienthal, 1978; Vail et al, 1977) coincide with this event. Subsequently, at the beginning of the Carboniferous, relatively minor sea level rise occurred with deposition of the Sunbury Shale across the Appalachian and Michigan basins (Haq and Schutter,

2008; Ettensohn, 2008; Harrell, 1991). In the Michigan basin, the Sunbury Shale is conformably overlain by the Coldwater Shale and Marshall Sandstone. The deltaic

Borden Formation is acknowledged as the stratigraphic equivalent of these units in the

Appalachian and eastern Illinois basin, represent regional progradation and coincide with a period of sea level fall through the rest of the Mississippian in the eastern United States

(Figure 35).

The study of cored intervals in the Marshall and lower Michigan formations reveal progradational barrier/shoreface and back-barrier lagoonal/sabkha deposits overlying the Coldwater Shale throughout the Michigan basin. Basinward progradation during highstand conditions are interpreted to develop during the waning stages of sea level rise and the early portions of sea level fall (Embry, 2009). Miospore studies of samples from the contact between the Coldwater and Marshall formations by Richardson

(2006) confirm a late-Kinderhookian to early-Osagean age, respectively for these units.

Correlation of these time-units to sea level curves constructed by Haq and Schutter (2008,

Figure 35) indicate that deposition of the Marshall Formation occurred during relative sea level highstand with further sea level regression during the late Osagean and into the

Meramecian during deposition of the overlying Michigan Formation (Figure 35).

Tectonics

Early Mississippian strata (early Tournaisian; Kinderhookian) in the Appalachian basin is in-part reflective of the tectonic activity associated with the Neo-Acadian phase of the Acadian orogeny (Ettensohn, 2008). Sea level rise and deformational loading associated with renewed orogenic activity in the Appalachian orogen led to regional deposition of the Sunbury Shale. This unit was deposited in a stratified, coarse-grained clastics-starved, marine setting across the Appalachian basin extending into central Ohio and the Michigan basin during the early Mississippian (Ettensohn, 2008; Matchen and

Kammer, 2006; Harrell, 1991). Following deposition of the Sunbury Shale in the

Appalachian and parts of the eastern Illinois basin, two distinct progradational "clastic wedges" were deposited in the Price and Borden Formations. The Borden Formation is

93 interpreted as deltaic in origin, including prodelta turbidites, delta slope shale, and thick delta-front deposits, thought to reflect increased clastic input to the Appalachian basin associated with the Neo-Acadian tectophase (Ettensohn, 2008).

According to Howell and Van Der Pluijm (1999) subsidence patterns in the Michigan basin are varied with both westward (anomalous) and eastward tilting subsidence occurring from the late Devonian through the Mississippian respectively.

Mississippian eastward tilting subsidence is thought to have reflected the final collision between Laurentia and Gondwana and tectonic loading in the Appalachian orogen.

Howell and Van Der Pluijm (1999) acknowledge that while the limited preservation of

Mississippian deposits across the Michigan basin provide unclear evidence as to the specific mechanisms that might be responsible for eastward tilting, this final episode of tectonism had a strong effect on the nature of subsidence during that time. Consequently, mapping of isopach values of the Sunbury through the Marshall Formations by Howell and Van Der Pluijm (1999) show eastward thickening of section due to eastward tilting subsidence. Well log analysis and log facies mapping of basal sequence stratigraphic units in the Marshall (Chapter 4, Figures 27-28) shows east-northeast isopach maximums and supports eastward tilting of the Michigan basin during Marshall time.

Evidence of eastward tilting subsidence during deposition of the lower Marshall

Sandstone is significant in regards to regional tectonism resulting from the Appalachian orogen. Eastward tilting subsidence and a significant influx of terrigenous clastics during lower Marshall deposition strongly point towards tectonic activation of a nearby source terrain to the East-Northeast in the early Mississippian. Crystalline rocks of the Canadian shield have been proposed as a significant source terrain by both Stearns (1933) and

Boothroyd (2012) in petrologic studies. This idea is further supported by isopach maps in this study and suggests the uplift of a crystalline Canadian shield source terrain in response to Appalachian orogenic activity.

Mapping of the Upper Marshall Sandstone isopach pattern oddly enough, shows an inverse relationship to that of the lower Marshall with isopach maximums in the south and southwest of the Michigan basin. While evidence of eastward tilting is expressed in the lower Marshall, the transition of depositional maximums to other areas of the basin in the upper Marshall may signify a change in the mechanism of basin subsidence that is coincident with a shift in sediment supply sourcing. While the spatial limitations of data in the Marshall and Michigan formations make regional correlations difficult as stated by

Howell and Van Der Pluijm (1999), this study provides new insight as to the possible regional effects on stratal architecture in the Michigan basin during the early

Mississippian by both tectonic and eustatic forces.

The Michigan "Stray" Problem

Stratigraphic subdivision and interpretation of depositional conditions for the

Marshall and lower Michigan formations is a long standing problem in Michigan basin geology. The Michigan "Stray" problem, as described by Hard (1938), is primarily stratigraphic contributing to confusion concerning subdivision of the Marshall and lower

Michigan formations. Informal terms proposed by Hard (1938), such as the "Stray Stray" and "Stray Stray Stray", for portions of the lower Michigan Formation are discouraged on the basis of this sequence stratigraphic investigation. The term Michigan "Stray" originated as an informal driller's term with the discovery of the Clare gas field in

southern Clare County, MI. Significant gas volumes were encountered in relatively thick

sandstone beds thought to belong to the Marshall Formation until an offset well

penetrated 40-50' of sandy dolomite, limestone, shale and evaporites typical of the

Michigan Formation (Hard, 1938). Stratigraphic correlation at that time suggested that

the Marshall Sandstone was subjacent to the basal carbonates and evaporites of the

Michigan Formation. The presence of relatively thick sandstone beds bounded above and

below by carbonates and evaporites led to the use of informal, stratigraphic terminology

that included these sands into the Michigan Formation as the Michigan "Stray

Sandstone". Similarly, the stratigraphic occurrence of carbonates and evaporites below

the Michigan "Stray" resulted in the informal driller's designation of "Stray Dolomite"

(Hard, 1938).

One of the primary objectives of this study is the delineation of genetic

stratigraphic relationships in the Marshall Sandstone and related strata. Integrated core

and wire-line log analysis, especially in three wells with cored intervals in the Marshall

and lower Michigan strata in Clare County provide a basis for resolution of the Michigan

"Stray" problem as described by Hard (1938). A modern, sedimentological and sequence

stratigraphic interpretation of these units is described in this study and supports the

"Stray" dolomite unit as lagoonal/sabkha deposits (L2) that is genetically related to the

Marshall Sandstone (L1-A), and in part , contemporaneous. In turn, the laterally

continuous "Stray Sandstone" (L1-B) is separated from the underlying "Stray" dolomite by a marked, disconformable, flooding surface and regional correlative facies successions. This important chronostratigraphic surface provides a more sensible explanation for the "Stray Sandstone" and clarifies the genetic relationship of the Stray to

96 other Marshall Sandstone units in the south and southwestern portions of the Michigan basin (Figures 31-34). All L3 and L1-B strata are younger (above the disconformity) than L2 and L1-A strata. These correlations establish the relationship of "stray" units, as described by Hard (1938), to Marshall Sandstone and thus the need for informal terminology is no longer relevant.

Conclusions

- The Mississippian Marshall Sandstone was deposited in a wave-dominated

paralic-shoreline environment along with genetically related strata ranging from

shoreface, to a possibly subaerial barrier, to restricted lagoonal and sabkha

environments.

- Observations of climate sensitive strata, such as primary marine evaporites,

indicate that the Marshall was deposited during a period of increasingly arid

paleoclimatic conditions during the Osagean Stage of the Mississippian in eastern

North America.

- Eustatic sea-level fluctuations and a relatively high-frequency, flooding event

played a major role in the stratigraphic architecture of the Marshall Sandstone.

These allocyclic events help to explain complex lithostratigraphic relationships in

the Marshall throughout the Michigan basin.

- Observations in core from the Marshall and lower Michigan formations show no

evidence of a significant subaerial exposure surface/unconformity separating

these units.

- Isopach mapping of basal units of the Marshall Formation support an eastward-

tilting subsidence pattern with generally northeast to southwest progradation in

the Michigan basin during the early Mississippian.

- Michigan "Stray" sandstone units are laterally continuous and genetically related

to the Marshall Sandstone in the Michigan basin. These relationships support

incorporation of these stratigraphic units in the Marshall Formation. The informal

driller’s terminology of the "Stray" sandstone for these units is discouraged.

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APPENDIX A

Graphical Core Descriptions

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APPENDIX B

Photomicrograph Plates

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Facies D2

Plate 1:(A-B) Cross-polarized light (XPL) image of poor to moderately sorted lithic sandstone of the D2 facies. Individual grains are subround to angular and include common quartz, polycrystalline quartz, detrital feldspars, amphiboles and micas in addition to other various plutonic and metamorphic framework grains.

Facies D3

Plate 2: (A) Plane-polarized light (PPL) image showing poorly sorted sandstone with variable intergranular cementation. (B) Cross-polarized light (XPL) image showing angular to subangular metamorphic and igneous framework grains with some high birefringence anhydrite cementation.

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Facies D4

Plate 3: (A-B) XPL images of poorly to moderately sorted lithic sandstone of the D4 facies. Common and polycrystalline quartz, plagioclase feldspars, alkali feldspar in the form of microcline, as well as amphibole and micas.

Facies D5

Plate 4: (A) PPL image showing framework grains with relatively high intergranular porosity. (B) XPL image showing poorly sorted lithic sandstone with predominantly coarse common quartz grains exhibiting high birefringence anhydrite rimmed cements.

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Facies D7-D8

Plate 5: (A) XPL image of sucrosic dolomite within the D7 facies with quartz grains distributed throughout a vuggy matrix. (B) XPL image of sucrosic dolomite with high birefringence anhydrite cemented vugs. (C) XPL image of vuggy sucrosic dolomite with recystallized dolomite rhombs lining individual vugs. (D) XPL image of sabkha dolomite matrix in contact with high birefringence massive anhydrite.

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APPENDIX C

Fortran Programs for Calculating Rock Matrix Mineralogy

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! ------! VSHGR.TXT - SHALE VOLUME FROM GAMMA RAY ! Text after exclamation marks is comment/explanation and is not part of the program’s ! code ! Geologist/Program Writer: Joseph Adducci (2015) ! Program is written in FORTRAN format and is written for execution in IHS PETRA ! software. ! Program is based on Asquith, G., and D. Krygowski’s (2004), Basic Well Log Analysis: ! AAPG Methods in Exploration 16, p. 31-35 ! ------! INPUT LOGS: ! ------! GR = GAMMA RAY (API) ! ! ------! INPUT VARIABLES: ! ------! GRCL = GR VALUE IN CLEAN ZONE (API) ! GRSH = GR VALUE IN 100% SHALE ZONE (API) ! ! ------! OUTPUT LOGS: ! ------! VSH = SHALE VOLUME FROM GAMMA RAY (FRACTION BTWN 0-1) ! ! ------! DEFINE OUTPUT LOG ! ------LOGDEF NAME(VSH) UNITS(%) DESC(SHALE VOLUME FROM GR); ! ! ------! OUTPUT LOGS USED IN THE MODEL ! ------LOG VSH OUT; ! ! ------! CONSTANTS USED IN THE MODEL ! ------CONST GRCL 15.0; ! GR READING IN CLEAN ZONE CONST GRSH 115.0; ! GR READING IN SHALE ZONE CONST NULL; VSH = NULL;

IF ( GR = NULL ) THEN GOTO DONE; IF ( GRCL = GRSH ) THEN GOTO DONE;

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! ------! COMPUTE SHALE VOLUME ! ------VSH = ( GR - GRCL ) / ( GRSH - GRCL ); VSH = MIN(1.0,VSH); VSH = MAX(0.0,VSH); END;

CHECK: VSH = MIN(1.0,VSH); VSH = MAX(0.0,VSH);

DONE: ENDMOD;

133

! ------! VAHRHOB.TXT - ANHYDRITE VOLUME FROM BULK DENSITY ! Text after exclamation marks is comment/explanation and is not part of the program’s ! code ! Geologist/Program Writer: Joseph Adducci (2015) ! Program is written in FORTRAN format and is written for execution in IHS PETRA ! software. ! Program is based on Asquith, G., and D. Krygowski’s (2004), Basic Well Log Analysis: ! AAPG Methods in Exploration 16, p. 37-76. ! ------! INPUT VARIABLES: ! ------! RHOB = Bulk Density (g/cc3) ! RHOBCL = Bulk Density VALUE IN ANHYDRITE FREE ZONE (g/cc3) ! RHOBAH = Bulk Density VALUE IN 100% ANHYDRITE ZONE (g/cc3) ! ! ------! OUTPUT VARIABLES: ! ------! VAH = SHALE VOLUME FROM GAMMA RAY (FRACTION BTWN 0-1) ! ! ------! DEFINE OUTPUT LOG IN DATABASE ! ------LOGDEF NAME(VAH) UNITS(%) DESC(ANHYDRITE VOLUME FROM RHOB); ! ------! ! ------! INPUT LOGS USED IN THE MODEL ! ------LOG RHOB IN; ! ! ! ------! OUTPUT LOGS USED IN THE MODEL ! ------LOG VAH OUT; ! ! ------! CONSTANTS USED IN THE MODEL ! ------CONST RHOBCL 2.80; ! RHOB READING IN ANHYDRITE FREE ZONE CONST RHOBAH 2.95; ! RHOB READING IN ANHYDRITE ZONE CONST NULL;

VAH = NULL;

134

IF ( RHOB = NULL ) THEN GOTO DONE; IF ( RHOBCL = RHOBAH ) THEN GOTO DONE;

! ------! COMPUTE ANHYDRITE VOLUME ! ------VAH = ( RHOB - RHOBCL ) / ( RHOBAH - RHOBCL ); VAH = MIN(1.0,VAH); VAH = MAX(0.0,VAH);

DONE: ENDMOD;

135

! ------! MATRIXMOD.TXT - INTEGRATED MATRIX CALCULATION ! Text after exclamation marks is comment/explanation and is not part of the program’s ! code ! Geologist/Program Writer: Joseph Adducci (2015); modified from Rock (2011) ! Program is written in FORTRAN format and is written for execution in IHS PETRA ! software. ! Program is based on Doveton’s (2004) algebraic matrix solution and KIWI program as ! well as inputs based on works from ! Asquith, G., and D. Krygowski’s (2004), Basic Well Log Analysis: AAPG Methods in ! Exploration 16. For these models ! refer to Shale and Anhydrite volumetric models present in this study ! ------! INPUT LOGS: ! ------! RHOB = Compensated Bulk Density ! NPHI = Compensated Neutron Porosity ! ! ------! OUTPUT LOGS: ! ------! P = Porosity in decimal% units ! Q = Quartz% ! C = Calcite% ! D = Dolomite% ! C&D = Calcite&dolomite% ! C&D&Q = Calcite&dolomite&quartz% ! C&D&Q&P = Calcite,dolomite&quartz&porosity% ! QN = Quartz%, normalized by excluding porosity ! CN = Calcite%, normalized by excluding porosity ! DN = Dolomite%, normalized by excluding porosity ! CN&DN = Sum of normalized calcite% and dolomite% ! CN&DN&QN = Sum of normalized calcite, dolomite, quartz% ! VSHN = Shale%, normalized by replacing dolomite% ! VAHN = Anhydrite%, normalized by replacing calcite% ! and dolomite% ! VCN = Calcite%, remaining after normalization of Shale ! and Anhydrite% ! VDN = Dolomite%, remaining after normalization of ! Shale and Anhydrite% ! VSHN&VAHN = Sum of normalized Shale, anhydrite% ! VSHN&VAHN&VCN = Sum of normalized Shale, anhydrite, calcite% ! VSHN&VAHN&VCN&VDN = Sum of normalized Shale, anhydrite, calcite, ! dolomite% ! ! ------

136

! METHODS & ASSUMPTIONS: ! ------! Four unknowns (D, Q, C, PHI) are determined by solving the below system of equations ! simultaneously: ! ! NEUTRON POROSITY: 0.05D - 0.05Q + 0C + 1PHI ! = NPHI ! BULK DENSITY: 2.87D + 2.65Q + 2.71C + 1.1PHI ! = RHOB ! VOLUMETRIC PHOTOELECTRIC: 9D + 4.79Q + 13.77C + 1.36PHI ! = U (U = PEF * RHOB) ! UNITY: 1D + 1Q + 1C + 1PHI ! = 1 ! Rock matrix and fluid values comprising the matrix of coefficients: ! DOLOMITE QUARTZ CALCITE POROSITY ! NPHI 0.05 -0.05 0 1 ! RHOB 2.87 2.65 2.71 1.1 ! U 9 4.79 13.77 1.36 ! UNITY 1 1 1 1 ! ! Inverse of matrix of coefficients (calculated in Microsoft Excel): ! DOLOMITE QUARTZ CALCITE POROSITY ! NPHI 4.741893376 3.319761059 -0.048583556 -8.327556904 ! Inverse ! coefficients used to calculate dolomite% ! RHOB -3.342168279 -1.434857405 -0.083162599 5.033612559 ! Inverse ! coefficients used to calculate quartz% ! U -1.995522014 -1.647172731 0.133475107 3.625885872 ! Inverse ! coefficients used to calculate calcite% ! UNITY 0.595796917 -0.237730923 -0.001728952 0.668058473 ! Inverse ! coefficients ! used to calculate porosity% ! ! Proportional composition is determined by multiplying known log values and unity by ! inverse of coefficients: ! ! P= (0.595796917*NPHI)+(-0.237730923 * RHOB)+(-0.001728952 * ! UMAA)+(0.668058473 * 1); !Porosity dec% is !calculated ! Q = (-3.342168279 * NPHI)+(-1.434857405 * RHOB)+(-0.083162599 * ! UMAA)+(5.033612559 * 1); !Quartz% is !calculated ! C = (-1.995522014 * NPHI)+(-1.647172731 * RHOB)+(0.133475107 * ! UMAA)+(3.625885872 * 1); !Calcite% is calculated ! ------! START OF PROGRAM ! ------! DEFINE OUTPUT LOGS:

137

! ------LOGDEF NAME(UMAA) UNITS(BARNS/CC^3) DESC(U OF MATRIX); LOGDEF NAME(P) UNITS(DEC%) DESC(DECIMAL POROSITY); LOGDEF NAME(Q) UNITS(DEC%) DESC(QUARTZ%); LOGDEF NAME(C) UNITS(DEC%) DESC(CALCITE%); LOGDEF NAME(D) UNITS(DEC%) DESC(DOLOMITE%); LOGDEF NAME(C&D) UNITS(DEC%) DESC(CALCITE&DOLOMITE%); LOGDEF NAME(C&D&Q) UNITS(DEC%) DESC(CALCITE,DOLOMITE&QUARTZ%); LOGDEF NAME(C&D&Q&P) UNITS(DEC%) DESC(CALCITE,DOLOMITE&QUARTZ&POROSITY%); LOGDEF NAME(QN) UNITS(DEC%) DESC(QUARTZ%,NORMALIZED); LOGDEF NAME(CN) UNITS(DEC%) DESC(CALCITE%,NORMALIZED); LOGDEF NAME(DN) UNITS(DEC%) DESC(DOLOMITE%,NORMALIZED); LOGDEF NAME(CN&DN) UNITS(DEC%) DESC(CALCITE%DOLOMITE%, NORMALIZED); LOGDEF NAME(CN&DN&QN) UNITS(DEC%) DESC(CALCITE&DOLOMITE&QUARTZ%, NORMALIZED); LOGDEF NAME(VAHN) UNITS(DEC%) DESC(ANHYDRITE%, NORMALIZED); LOGDEF NAME(VCN) UNITS(DEC%) DESC(CALCITE%, NORMALIZED); LOGDEF NAME(VDN) UNITS(DEC%) DESC(DOLOMITE%, NORMALIZED); LOGDEF NAME(VSH&VAHN) UNITS(DEC%) DESC(SHALE,ANHYDRITE%, NORMALIZED); LOGDEF NAME(VSH&VAHN&VCN) UNITS(DEC%) DESC(SHALE,ANHYDRITE,CALCITE%, NORMALIZED); LOGDEF NAME(VSH&VAHN&VCN&VDN) UNITS(DEC%) DESC(SHALE,ANHYDRITE,CALCITE,DOLOMITE%, NORMALIZED); ! ------! INPUT LOGS: ! ------LOG RHOB IN; LOG NPHI IN; LOG PEF IN; LOG VAH IN; LOG VSH IN; ! ------! OUTPUT LOGS: ! ------LOG P OUT; LOG Q OUT; LOG C OUT; LOG D OUT; LOG C&D OUT; LOG C&D&Q OUT; LOG C&D&Q&P OUT; LOG QN OUT;

138

LOG CN OUT; LOG DN OUT; LOG CN&DN OUT; LOG CN&DN&QN OUT; LOG VAHN OUT; LOG VCN OUT; LOG VDN OUT; LOG VSH&VAHN OUT; LOG VSH&VAHN&VCN OUT; LOG VSH&VAHN&VCN&VDN OUT; ! ------! SET OUTPUT LOGS TO NULL ! ------UMAA = NULL; P = NULL; Q = NULL; C = NULL; D = NULL; C&D = NULL; C&D&Q = NULL; C&D&Q&P = NULL; QN = NULL; CN = NULL; DN = NULL; CN&DN = NULL; CN&DN&QN = NULL; VAHN = NULL; VCN = NULL; VDN = NULL; VSH&VAHN = NULL; VSH&VAHN&VCN = NULL; VSH&VAHN&VCN&VDN = NULL; ! ------! ABORT OPERATION IF RHOB OR NPHI OR PEF CURVE IS NULL ! ------IF ( NPHI = 0.0 ) THEN GOTO SKIP; IF ( NPHI = NULL ) THEN GOTO DONE; SKIP: IF ( RHOB = NULL ) THEN GOTO DONE; IF ( PEF = NULL ) THEN GOTO DONE; ! ------! CALCULATE UMAA, MINERAL%, AND POROSITY% ! ------UMAA = (RHOB * PEF); !Calculate UMAA

139

P = (0.595796917 * NPHI)+(-0.237730923 * RHOB) + (-0.001728952 * UMAA) + (0.668058473); ! Calculate porosity dec.% Q = (-3.342168279 * NPHI) + (-1.434857405 * RHOB) + (-0.083162599 * UMAA) + (5.033612559); Calculate Quartz% C = (-1.995522014 * NPHI) + (-1.647172731 * RHOB) + (0.133475107 * UMAA) + (3.625885872); Calculate Calcite% D = (4.741893376 * NPHI) + (3.319761059 * RHOB) + (-0.048583556 * UMAA) + (- 8.327556904); Calculate Dolomite%

C&D = C + D; ! Sum calcite% and dolomite% C&D&Q = C + D + Q; ! Sum calcite%, dolomite% and Quartz% C&D&Q&P = C + D + Q + P; ! Sum calcite%, dolomite%, Quartz% and Porositydec.% ! ------! CALCULATE NORMALIZED MINERAL% - (POROSITY EXCLUDED) ! ------X=0.0; ! Set X equal to zero IF (Q.LT.X) THEN Q=0; ! Set Quartz% to zero if Q<0 IF ( C.LT.X) THEN C=0; ! Set Calcite% to zero if Q<0 IF ( D.LT.X) THEN D=0; ! Set Dolomite% to zero if Q<0

QN = (Q) / (Q + C + D); ! Normalized Quartz% CN = (C) / (Q + C + D); ! Normalized Calcite% DN = (D) / (Q + C + D); ! Normalized Dolomite%

CN&DN = CN+DN; ! Sum normalized calcite% and dolomite% CN&DN&QN = CN+DN+QN; ! Sum normalized calcite%, dolomite% and Quartz% ! ------! CALCULATE NORMALIZED MINERAL% - (SHALE AND ANHYDRITE VOLUMES INCLUDED) ! ------VAHN = (VAH - VSH); IF (VAHN.LT.0) THEN VAHN = 0; ! Set Anhydrite% to zero if VAHN<0

VCN = (CN – VAH); IF (VCN.LT.0) THEN VCN = 0; ! Set Calcite% to zero if VCN<0

VDN = (DN – VSH); IF (VDN.LT.0) THEN VDN = 0; ! Set Dolomite% to zero if VDN<0

VSH&VAHN = (VSH + VAHN); VSH&VAHN&VCN = (VSH&VAHN + VCN);

140

IF (VSH&VAHN&VCN.GT.1) THEN VSH&VAHN&VCN = 1;

VSH&VAHN&VCN&VDN = (VSH&VAHN&VCN + VDN); IF (VSH&VAHN&VCN&VDN.GT.1) THEN VSH&VAHN&VCN&VDN = 1;

DONE: ENDMOD;

141

APPENDIX D

Well Data Listing for Marshall and Lower Michigan Formations

142

GR GR - NPHI Well Name Well Well Label Well - Township UWI/API NPHI County Well # Well Range Core GR - RHOB

# -

RHOB

- PEF

210055546 ALLEG 02 11 1 50000 55465 MCALLISTER 1-6 AN N W X 210055839 ALLEG 03 11 2 70000 58397 JACKSON D2-1 AN N W X 210113870 ARENA 19 04 3 80000 38708 SWAFFIELD 1-19 C N E X X 210152357 ALLERDING, 04 08 4 30000 23573 JACK M 1 BARRY N W X 210153013 TIMM 03 08 5 70000 30137 KENNEDY UNIT 1-14 BARRY N W X 210155647 CARTER 02 10 6 00000 56470 FAMILY L.L 1-3 BARRY N W X 210173119 MIESKE, 15 03 7 10000 31191 FREDERICK 1-10 BAY N E X X 210173120 MIESKE, 15 03 8 60000 31206 FREDERICK 2-10 BAY N E X X 210173452 15 03 9 70000 34527 JENKINS 2-8 BAY N E X X 210173481 ZIMMERMAN & 14 03 10 70000 34817 KRUEG 1-8 BAY N E X X 210173485 14 03 11 90000 34859 FICK 2-6 BAY N E X X 210173488 14 03 12 60000 34886 PFUND 1 BAY N E X X 210173488 14 03 13 90000 34889 GANDY 2-17 BAY N E X X 1- 210173503 MIESKE & 31SW 15 03 14 30000 35033 HOLEY D BAY N E X X 210173529 15 03 15 90000 35299 BRADSHAW 1-31 BAY N E X X 210173541 15 03 16 80000 35418 RYTLEWSKI 1 BAY N E X X X 210173625 TOMLINSON, C 14 03 17 60000 36256 E 1 BAY N E X X X 210173720 14 03 18 60000 37206 FICK 2-5 BAY N E X X 210173721 15 03 19 00000 37210 BRANDT, N 1-21 BAY N E X X X 210173725 FICK & 14 03 20 90000 37259 EMERSON 1-5 BAY N E X X 210173733 15 03 21 00000 37330 MIESKE, R 1-16 BAY N E X X X 210173782 14 03 22 40000 37824 FICK, N 3-5 BAY N E X X

143

GR GR - NPHI Well Name Well Well Label Well - Township UWI/API NPHI County Well # Well Range Core GR - RHOB

# -

RHOB

- PEF

210173782 14 03 23 60000 37826 FICK, A 1-5 BAY N E X X 210173953 14 03 24 60000 39536 CNUDDE 1-4 BAY N E X X 210173993 14 03 25 00000 39930 COLTER FARMS 2-9 BAY N E X X 210174018 14 03 26 40000 40184 WIRSING 1-4 BAY N E X X 210174018 14 03 27 60000 40186 WIRSING 1-9 BAY N E X X X 210174028 14 03 28 20000 40282 HOPCROFT 1-3 BAY N E X X 210174028 14 03 29 30000 40283 WIRSING 1-3 BAY N E X X 210174035 14 03 30 10000 40351 ZIMMERMAN 1-8 BAY N E X X 210174055 WALTERS & 14 03 31 70000 40557 WEGENE 1-4 BAY N E X X 210174611 14 03 32 50000 46115 JENKINS 2-8 BAY N E X X 210175183 14 03 33 20000 51832 SHEETS 3-6 BAY N E X X X 210175250 16 03 34 70000 52507 GUNN D1-10 BAY N E X X X 210351354 18 05 35 30100 13543 STATE LINCOLN 49 CLARE N W X X 210352898 18 06 36 60000 28986 MCGS F-171 CLARE N W X X 210353254 HARRINGTON, 17 03 37 60000 32546 JAMES 1-8 CLARE N W X X 210353289 20 06 38 00000 32890 BENCHLEY A 2-31 CLARE N W X X 210353461 WEINGARTZ ET 17 04 39 10000 34611 AL 1-7 CLARE N W X X X 210353479 17 06 40 00000 34790 BRANDT 1-34 CLARE N W X X X 210353596 20 03 41 30000 35963 SINCIC 1-36 CLARE N E X X X 210353651 PRIMARK 18 05 42 10000 36511 STORAGE L L-131 CLARE N W X X X 210353843 17 03 43 40000 38434 EBERHART 1-31 CLARE N W X X 210353856 18 03 44 80000 38568 DOUGHERTY 1-21 CLARE N E X X X 210353915 18 05 45 50000 39155 FREIER 1-23 CLARE N W X X X

144

GR GR - NPHI Well Name Well Well Label Well - Township UWI/API NPHI County Well # Well Range Core GR - RHOB

# -

RHOB

- PEF

210354400 19 03 46 40000 44004 GRANGER 1-22 CLARE N E X X X 210354476 ANR PIPELINE 18 05 47 00000 44760 CO L-144 CLARE N W X X X 210355403 19 05 48 00000 54030 STOCKING 1-14 CLARE N W X X X 210355836 19 03 49 50000 58365 FANSLAU, R & P 1-22 CLARE N E X X X 210372234 ZISCHKE, CLINT 05 03 50 80000 22348 ERVIN W 1 ON N W X 210373332 HEBELER, CLINT 07 01 51 10000 33321 ROBERT S 1-9 ON N W X X 210373538 CLINT 07 04 52 30000 35383 FARLEY 1-10 ON N W X X X 210453482 01 04 53 50000 34825 AMES T. 1-10 EATON N W X 210453950 02 05 54 70000 39507 FULLERTON 1-24 EATON N W X 210454142 04 05 55 30000 41423 ARNOLD UNIT 1-8 EATON N W X X X 210494066 GENES 09 08 56 20000 40662 BROWN 42040 EE N E X 210494066 GENES 09 08 57 40000 40664 BROWN 1-5 EE N E X 210513480 GLAD 17 02 58 50000 34805 CROCKETT 1-13 WIN N W X X X 210513528 GLAD 17 01 59 40000 35284 POINTEK, D & K 1-31 WIN N W X X X 210513539 GLAD 17 01 60 50000 35395 STALEY 1-32 WIN N W X X X 210513552 BRUBAKER- GLAD 17 01 61 30000 35523 MYERS 1-30 WIN N W X X X 210513574 GLAD 20 01 62 60000 35746 WILLIAMS 1-12 WIN N W X X X 210513736 GLAD 17 01 63 10000 37361 BWAB HUNT 10-44 WIN N E X X X 210513777 SCHALL, GLAD 17 02 64 40000 37774 FREDERICK 1-36 WIN N W X X 210513820 STATE GLAD 18 01 65 80000 38208 BUCKEYE K 1 WIN N W X X X 210513898 STATE BUTMAN GLAD 20 01 66 00000 38980 A 1 WIN N W X X X 210513939 GLAD 18 02 67 60000 39396 TLUCZEK 1-13 WIN N W X X 210513960 GLAD 20 01 68 70000 39607 KRIGNER 1-35 WIN N W X X

145

GR GR - NPHI Well Name Well Well Label Well - Township UWI/API NPHI County Well # Well Range Core GR - RHOB

# -

RHOB

- PEF

210514025 GLAD 18 02 69 20000 40252 DUNN 1-14 WIN N W X X 210514074 GLAD 18 02 70 80000 40748 TLUCZEK 2-13 WIN N W X X X 210514101 GLAD 18 01 71 50000 41015 ARMSTRONG 1-0 WIN N W X X 210514101 COTTRELL & GLAD 18 01 72 80000 41018 HECK 3-0 WIN N W X X X 210514101 GLAD 18 01 73 90000 41019 STURM 3 WIN N W X X 210514222 GLAD 18 02 74 60000 42226 GROUT 1-14 WIN N W X X X 210514266 GLAD 18 01 75 40000 42664 MONTELIUS 1-0 WIN N W X X X 210514266 GLAD 18 01 76 50000 42665 RUCK 3-0 WIN N W X X X 210514506 SMITH- GLAD 17 01 77 90000 45069 BILLINGS 4-W WIN N E X X X 210514507 SMITH- GLAD 17 01 78 00000 45070 BILLINGS 5-0 WIN N E X X X 210514507 GLAD 18 01 79 10000 45071 MCMAHON 2-W WIN N W X X X 210514862 COTTRELL- GLAD 18 01 80 70000 48627 HECK 1-0 WIN N W X X X 210515864 STATE SOUTH GLAD 17 01 81 00000 58640 BUCKE 41-1 WIN N W X X X 210573050 MACLAREN, GRATI 10 04 82 90000 30509 MRS ADD 42016 OT N W X X 210573088 NH GRATI 10 04 83 40000 30884 MCGC 162-A OT N W X X 210573088 NH GRATI 10 04 84 60000 30886 MCGC 328-A OT N W X X 210574099 GRATI 12 01 85 40000 40994 FROST 1-1 OT N W X X X 210574289 GRATI 10 03 86 60000 42896 HIBNER 1-9 OT N W X X X 210574352 GRATI 12 02 87 30000 43523 SHERWOOD 1-27 OT N W X X X 210654304 INGHA 01 02 88 20000 43042 EATON RAPIDS 36-5 M N W X X X 210673089 WILSON, JOHN 06 06 89 20000 30892 C & 1-14 IONIA N W X X 210673643 STOWE & 08 06 90 50000 36435 LUMBERT 1-11 IONIA N W X X 210673670 FERRIS & 06 06 91 40000 36704 STATE OR 1-28 IONIA N W X X X

146

GR GR - NPHI Well Name Well Well Label Well - Township UWI/API NPHI County Well # Well Range Core GR - RHOB

# -

RHOB

- PEF

210674165 BEHRENWALD 06 08 92 60000 41656 UNIT 1-34 IONIA N W X 210674875 05 08 93 50000 48755 MCCONNON D1-10 IONIA N W X 210692306 ERICKSON, 21 05 94 00000 23060 NEIL R 1 IOSCO N E X 210692664 WASILEWSKI, 21 05 95 00000 26640 AGNES 2 IOSCO N E X 210693392 23 05 96 30000 33923 WILKINSON 1-34 IOSCO N E X 210732773 CW- ISABEL 16 06 97 90000 27739 MCGC 22 L N W X X 210733020 RECKER, ISABEL 13 04 98 80000 30208 WILLIAM, 1-28 L N W X X 210733040 BIGELOW, PAUL ISABEL 13 04 99 40000 30404 J & 1-30 L N W X X 10 210733074 HOLP, DON ET ISABEL 13 04 0 60000 30746 AL 1-10 L N W X X 10 210733271 PHIPPS, ISABEL 16 05 1 80000 32718 WARREN C 1 L N W X X 10 210733323 ISABEL 14 06 2 30000 33233 MCARTHUR, G 1-9 L N W X X 10 210733430 ISABEL 13 06 3 70000 34307 MOSS, MILAN 1-24 L N W X X 10 210733445 ISABEL 13 06 4 00000 34450 MOSS, MILAN 4-24 L N W X X 10 210733448 ISABEL 13 06 5 80000 34488 COOPER 1-24 L N W X X 10 210733457 ISABEL 16 03 6 20000 34572 PAISLEY 1-B L N W X X X 10 210733478 ISABEL 15 03 7 10000 34781 MOEGGENBERG 1 L N W X X X 10 210733506 LAKE ISABELLA ISABEL 14 06 8 80000 35068 COR 1-10A L N W X X X 10 210733509 ISABEL 16 04 9 10000 35091 MCGUIRE 1-26 L N W X X X 11 210733520 ISABEL 15 03 0 60000 35206 WEZENSKY 1-19 L N W X X X 11 210733525 ISABEL 14 03 1 20000 35252 MCLINTIC 1 L N W X X X 11 210733526 ISABEL 14 06 2 00000 35260 MCARTHUR 4-9 L N W X X X 11 210733529 ISABEL 15 03 3 80000 35298 Moeggenberg 2 L N W X X X X 11 210733542 ISABEL 15 04 4 50000 35425 HORAN 1-B L N W X X X

147

GR GR - NPHI Well Name Well Well Label Well - Township UWI/API NPHI County Well # Well Range Core GR - RHOB

# -

RHOB

- PEF

11 210733553 CW- ISABEL 16 06 5 50000 35535 MWPLC 73 L N W X X X 11 210733554 ISABEL 14 03 6 00000 35540 SMITH, VERA A. 1 L N W X X X 11 210733554 ISABEL 16 04 7 60000 35546 FIKE 1-36 L N W X X X 11 210733558 ISABEL 15 03 8 60000 35586 WEZENSKY 1-30 L N W X X X 11 210733562 ISABEL 15 03 9 20000 35622 EPPLE 3-30 L N W X X X 12 210733563 ISABEL 15 03 0 70000 35637 WEZENSKY 2-30 L N W X X X 12 210733571 ISABEL 15 03 1 10000 35711 BURROWS 1 L N W X X X 12 210733573 ISABEL 14 03 2 50000 35735 WILCOX, G & E 1-1 L N W X X X 12 210733574 ISABEL 15 04 3 40000 35744 HOVEY 1-2 L N W X X X 12 210733575 ISABEL 15 04 4 70000 35757 PAPPAS 1-11 L N W X X X 12 210733583 ISABEL 15 04 5 10000 35831 HORAN 1-C L N W X X X 12 210733598 ISABEL 15 04 6 60000 35986 HOVEY ET AL 2-2 L N W X X X 12 210733598 ISABEL 15 04 7 70000 35987 FITZPATRICK 1-12 L N W X X X 12 210733599 ISABEL 16 03 8 10000 35991 DRAKE 3-21 L N W X X X 12 210733600 ISABEL 15 04 9 50000 36005 FITZPATRICK 2-12 L N W X X X 13 210733604 ISABEL 15 04 0 00000 36040 POLLARD 1-1 L N W X X X 13 210733604 ISABEL 15 03 1 70000 36047 EPPLE 4-30 L N W X X X 13 210733604 ISABEL 14 03 2 90000 36049 MCCLINTIC 4 L N W X X X 13 210733607 ISABEL 15 04 3 30000 36073 SHARF ET AL 1-12 L N W X X X 13 210733614 ISABEL 15 04 4 20000 36142 HUDAK 1-11 L N W X X X 13 210733614 ISABEL 15 04 5 60000 36146 PAPPAS 3-11 L N W X X X 13 210733614 ISABEL 15 04 6 70000 36147 PAPPAS 2-11 L N W X X X 13 210733615 ISABEL 14 03 7 10000 36151 MCCLINTIC 2 L N W X X X

148

GR GR - NPHI Well Name Well Well Label Well - Township UWI/API NPHI County Well # Well Range Core GR - RHOB

# -

RHOB

- PEF

13 210733616 ISABEL 16 03 8 80000 36168 MOLL 1-A L N W X X X 13 210733618 ISABEL 15 04 9 10000 36181 WALTON 1-12 L N W X X X 14 210733620 ISABEL 15 04 0 20000 36202 PROUT 1-14 L N W X X X 14 210733626 LEISURE ISABEL 14 06 1 20100 36262 CONCEPTS 1-9 L N W X X X 14 210733626 FITZPATRICK & ISABEL 15 04 2 40000 36264 COL 1-12 L N W X X X 14 210733627 ISABEL 15 04 3 00000 36270 POLLARD 2-1 L N W X X X 14 210733627 ISABEL 15 04 4 10000 36271 POLLARD 3-1 L N W X X X 14 210733636 ISABEL 14 03 5 50000 36365 SMITH, VERA A 2 L N W X X X 14 210733636 WHEELER, ISABEL 14 03 6 60000 36366 ROLAND 1 L N W X X X 14 210733636 ISABEL 14 03 7 70000 36367 MCCLINTIC 3 L N W X X X 14 210733638 ISABEL 14 03 8 70000 36387 MILLER, VIOLA 1 L N W X X X 14 210733639 ISABEL 15 04 9 00000 36390 MOGG, K 1-12 L N W X X X 15 210733643 ISABEL 15 04 0 70000 36437 MOGG 1-11 L N W X X X 15 210733654 ISABEL 16 04 1 80000 36548 MCGUIRE 3-36 L N W X X X 15 210733654 ISABEL 15 04 2 90000 36549 WALTON ALVIN 1-12 L N W X X X 15 210733655 ISABEL 15 04 3 00000 36550 WEST & MOGG 1-12 L N W X X X 15 210733655 ISABEL 15 04 4 10000 36551 FITZPATRICK 3-12 L N W X X X 15 210733655 ISABEL 16 04 5 60000 36556 HOUSE ARNOLD 2-26 L N W X X X 15 210733660 ISABEL 15 04 6 70000 36607 POLLARD 4-1 L N W X X X 15 210733663 ISABEL 16 04 7 80000 36638 SHEAHAN 2-26 L N W X X X 15 210733664 MAEDER ISABEL 14 03 8 70000 36647 GRACE L 1 L N W X X X 15 210733665 ISABEL 14 03 9 30000 36653 BISHOP UNIT 1 L N W X X X 16 210733667 ISABEL 14 03 0 50000 36675 THORN ROGER 1 L N W X X X

149

GR GR - NPHI Well Name Well Well Label Well - Township UWI/API NPHI County Well # Well Range Core GR - RHOB

# -

RHOB

- PEF

16 210733669 ISABEL 16 04 1 60000 36696 MCGUIRE 4-35 L N W X X X 16 210733669 ISABEL 15 04 2 70000 36697 TOPE A-3 L N W X X X 16 210733676 ISABEL 16 04 3 20000 36762 HOVEY SADA 1-35 L N W X X X 16 210733678 ISABEL 16 04 4 30000 36783 PAPPAS 1-35 L N W X X X 16 210733678 ISABEL 16 03 5 40000 36784 METHNER A-2 L N W X X X 16 210733679 ISABEL 16 04 6 70000 36797 KIRKPATRICK C 1-26 L N W X X X 16 210733680 MOGG & ISABEL 15 04 7 70000 36807 POLLARD 1-1 L N W X X X 16 210733681 FISHER ISABEL 14 03 8 00000 36810 BROTHERS 2 L N W X X X 16 210733681 ISABEL 14 03 9 10000 36811 FISHER BROS 1 L N W X X X 17 210733681 FISHER BROS ISABEL 14 03 0 20000 36812 A 3 L N W X X X 17 210733681 FISHER ISABEL 14 03 1 30000 36813 BROTHERS 2 L N W X X X 17 210733681 ISABEL 14 03 2 50000 36815 MCCLINTIC 5 L N W X X X 17 210733681 ISABEL 14 03 3 60000 36816 MCCLINTIC 7 L N W X X X 17 210733681 ISABEL 14 03 4 80000 36818 BISHOP UNIT A 1 L N W X X X 17 210733681 FISHER ISABEL 14 03 5 90000 36819 BROTHERS 1 L N W X X X 17 210733682 ISABEL 14 03 6 00000 36820 MCCLINTIC 10 L N W X X X 17 210733682 ISABEL 14 03 7 10000 36821 MCCLINTIC 8 L N W X X X 17 210733682 ISABEL 14 03 8 20000 36822 MCCLINTIC 6 L N W X X X 17 210733682 FISHER BROS ISABEL 14 03 9 30000 36823 UNIT 1 L N W X X X 18 210733682 ISABEL 16 04 0 60000 36826 HOVEY SADA 2-36 L N W X X X 18 210733683 FISHER ISABEL 14 03 1 20000 36832 BROTHERS 3 L N W X X X 18 210733683 ISABEL 14 03 2 30000 36833 MCCLINTIC 9 L N W X X X 18 210733683 ISABEL 16 03 3 90000 36839 MCDONALD 1-33 L N W X X X

150

GR GR - NPHI Well Name Well Well Label Well - Township UWI/API NPHI County Well # Well Range Core GR - RHOB

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18 210733684 ISABEL 14 03 4 90000 36849 LOWERY E J 1 L N W X X X 18 210733685 FISHER ISABEL 14 03 5 10000 36851 BROTHERS 4 L N W X X X 18 210733685 ISABEL 14 03 6 40000 36854 BISHOP J 1 L N W X X X 18 210733688 STATE ISABEL 14 03 7 40000 36884 CHIPPEWA 2 L N W X X X 18 210733688 STATE ISABEL 14 03 8 50000 36885 CHIPPEWA 1 L N W X X X 18 210733690 ISABEL 16 04 9 00000 36900 MCCONNELL M 3-C-35 L N W X X X 19 210733690 ISABEL 14 03 0 40000 36904 MCCLINTIC, V 11 L N W X X X 19 210733690 ISABEL 14 03 1 50000 36905 BISHOP, J 2 L N W X X X 19 210733691 STATE ISABEL 14 03 2 00000 36910 CHIPPEWA 4 L N W X X X 19 210733691 STATE ISABEL 14 03 3 10000 36911 CHIPPEWA 3 L N W X X X 19 210733691 MAEDER, ISABEL 14 03 4 20000 36912 GRACE L 2 L N W X X X 19 210733691 ISABEL 14 03 5 40000 36914 MCCLINTIC 12 L N W X X X 19 210733691 ISABEL 14 03 6 50000 36915 LOWERY, E J 2 L N W X X X 19 210733692 ISABEL 16 04 7 80000 36928 PAPPAS 2-35 L N W X X X 19 210733693 FISHER ISABEL 14 03 8 20000 36932 BROTHERS 5 L N W X X X 19 210733693 ISABEL 15 03 9 60000 36936 KREINER 1-19 L N W X X X 20 210733694 ISABEL 15 04 0 30000 36943 MITCHELL 1-24 L N W X X X 20 210733694 ISABEL 15 04 1 40000 36944 WEZENSKY 1-25 L N W X X X 20 210733695 ISABEL 16 06 2 10000 36951 BARRON, W 1-18 L N W X X X 20 210733697 PORTERFIELD, ISABEL 14 03 3 40000 36974 JOHN 1 L N W X X X 20 210733697 ISABEL 14 03 4 80000 36978 YOST, H. UNIT 1 L N W X X X 20 210733703 ISABEL 16 04 5 60000 37036 VANAS 1-36 L N W X X X 20 210733703 ISABEL 16 04 6 80000 37038 FIKE 5-36 L N W X X X

151

GR GR - NPHI Well Name Well Well Label Well - Township UWI/API NPHI County Well # Well Range Core GR - RHOB

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20 210733706 EMMONS ISABEL 14 03 7 90000 37069 BROTHERS 1 L N W X X X 20 210733707 COUITER & ISABEL 16 03 8 50000 37075 MCDONAL 1-32 L N W X X X 20 210733707 MCCONNELL & ISABEL 16 04 9 70000 37077 STATE 1B-35 L N W X X X 21 210733707 MCCONNELL & ISABEL 16 04 0 80000 37078 STATE 2B-35 L N W X X X 21 210733711 ISABEL 15 04 1 30000 37113 HAMILTON 1-18 L N W X X X 21 210733713 RAWSON, ISABEL 16 05 2 30000 37133 ALLEN UNI 1 L N W X X 21 210733714 ISABEL 16 03 3 70000 37147 RUSSELL 2-29 L N W X X X 21 210733714 ISABEL 16 03 4 80000 37148 SLOCUM 2-28 L N W X X X 21 210733716 ISABEL 15 05 5 90000 37169 FINNERTY 1-12 L N W X X X 21 210733717 FITZPATRICK & ISABEL 15 04 6 00000 37170 PRO 1-12 L N W X X X 21 210733717 WALTON, ISABEL 15 04 7 90000 37179 ALVIN 2-12 L N W X X X 21 210733720 ISABEL 16 04 8 90000 37209 CAMPBELL 1-35 L N W X X X 21 210733724 ISABEL 15 03 9 20000 37242 LATTIMER 1 L N W X X X 22 210733724 BEUTLER CARL ISABEL 15 06 0 30000 37243 & HO 1-34 L N W X X 22 210733729 METHNER & ISABEL 16 03 1 00000 37290 MAXWELL 1-33 L N W X X X 22 210733738 ISABEL 16 03 2 00000 37380 STRAUCH M 1-33 L N W X X X 22 210733748 ISABEL 16 04 3 20000 37482 SMOCK, ALGER 2-36 L N W X X X 22 210733759 ISABEL 15 04 4 10000 37591 BISSELL 1-25 L N W X X X 22 210733774 ISABEL 15 04 5 40000 37744 KREINER 1-24 L N W X X X 22 210733790 ISABEL 14 05 6 90000 37909 MCDONALD 1-16 L N W X X X 22 210733800 ISABEL 16 04 7 70000 38007 MCCONNELL 1 L N W X X X 22 210733816 MT PLEASANT ISABEL 14 03 8 20000 38162 UNIT 4 L N W X X X 22 210733816 MT PLEASANT ISABEL 14 03 9 40000 38164 UNIT 4 L N W X X X

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23 210733825 ISABEL 15 04 0 60000 38256 HOUSE 2-18 L N W X X 23 210733851 ISABEL 14 03 1 20000 38512 DAVIS, N. 9 L N W X X X 23 210733853 ISABEL 15 03 2 70000 38537 WEZENSKY 2-19 L N W X X X 23 210733982 MT PLEASANT ISABEL 14 03 3 00000 39820 UNIT 2 L N W X X X 23 210733982 MT. PLEASANT ISABEL 14 03 4 40000 39824 UNIT 6 L N W X X X 23 210733992 ISABEL 13 06 5 50000 39925 DRIER 1-19 L N W X X 23 210734019 MT PLEASANT ISABEL 14 03 6 90000 40199 UNIT 5 L N W X X X 23 210734029 ISABEL 15 03 7 20000 40292 OBOYLE UNIT 1-31 L N W X X X 23 210734817 ISABEL 15 06 8 50000 48175 WHITE, ET AL 1-20 L N W X X X 23 210734874 STEGMAN & ISABEL 15 06 9 10000 48741 ANDERSO 1-33 L N W X X X 24 210735254 ISABEL 16 03 0 30000 52543 DENNIS 1 HD1 L N W X X X 24 210735362 ISABEL 15 06 1 40000 53624 INDIAN CREEK 1-32 L N W X X X 24 210735715 ISABEL 13 06 2 90000 57159 PRITCHARD 1-14 L N W X X X 24 210735716 ISABEL 15 05 3 00000 57160 HAUCK 1-24 L N W X X X 24 210735716 ISABEL 15 06 4 10000 57161 PEDERSON 1-32 L N W X X X 24 210735756 ISABEL 13 06 5 50000 57565 WONSEY A1-24 L N W X X X 24 210735818 WATERLAND ISABEL 14 05 6 50000 58185 TRUCKIN 3-18 L N W X X X 24 210735822 ISABEL 14 05 7 10000 58221 REID 1-30 L N W X X X 24 210735825 STATE & ISABEL 14 05 8 80000 58258 COUNTY OF 1-19 L N W X X X 24 210735834 ISABEL 13 05 9 50000 58345 PEACOCK 1-22 L N W X X X 25 210735834 ISABEL 14 06 0 60000 58346 NEWMAN 1-33 L N W X X X 25 210812089 06 12 1 10000 20891 JOHNSON, REX 3-A KENT N W X 25 210812462 FRANCISCO, 08 09 2 70000 24627 GEORGE 1 KENT N W X

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25 210813553 09 09 3 90000 35539 DAVIS 1-19 KENT N W X X X 25 210813737 WILK, 10 11 4 20000 37372 FREDERICK 1-21 KENT N W X X 25 210813916 09 09 5 20000 39162 CARLSON ET AL 1-7 KENT N W X 25 210813963 10 09 6 90000 39639 NEILSON 1-16 KENT N W X X X 25 210814055 05 10 7 30000 40553 REUHS 1-19 KENT N W X 25 210814143 05 11 8 60000 41436 WORKMAN 1-23 KENT N W X 25 210814208 05 11 9 90000 42089 TUINSTRA 1-13 KENT N W X 26 210814442 10 09 0 90000 44429 ASH 1-15 KENT N W X X X 26 210815547 09 11 1 70000 55477 SWITZER 1-13 KENT N W X X X 26 210852836 ZOUBEK, CHAS 20 12 2 90000 28369 ET A 1-27 LAKE N W X 26 210855521 18 12 3 50000 55215 WOODS ET AL 1-24 LAKE N W X X X 26 210855599 18 11 4 70000 55997 STATE PINORA 1-27 LAKE N W X X X 26 210855601 17 12 5 10000 56011 STATE YATES 1-27 LAKE N W X X X 26 210855601 17 12 6 20000 56012 STATE YATES 3-22 LAKE N W X X X 26 210855647 17 12 7 20000 56472 STATE YATES 2-27 LAKE N W X X X 26 210855717 U S A & STATE 17 12 8 70000 57177 YAT 3-27 LAKE N W X X X 26 210855719 17 12 9 70000 57197 STATE YATES 4-22 LAKE N W X X X 27 210934874 LIVING 04 03 0 90000 48749 KUBIAK D1-20 S N E X 27 211072631 COLEGROVE, MECOS 14 08 1 00000 26310 AMENIA 1 TA N W 27 211072644 MECOS 13 10 2 70000 26447 HERRING, G 1 TA N W X 27 211072728 MECOS 14 09 3 00000 27280 MCGC A-138 TA N W X X 27 211072756 MECOS 13 09 4 70100 34517 ROGERS 1 TA N W X X 27 211073153 SL- MECOS 13 07 5 00000 31530 MCGS 217-A TA N W X X X

154

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27 211073154 MECOS 14 09 6 00000 31540 MCGC A-146 TA N W X X 27 211073183 MECOS 14 09 7 00000 31830 MCGC A-157 TA N W X X 27 211073232 SL- MECOS 13 08 8 10000 32321 MCGC 394 TA N W X X 27 211073292 MECOS 14 09 9 10000 32921 MCGC A-161 TA N W X X 28 211073292 MECOS 14 09 0 20000 32922 MCGC A-160 TA N W X X 28 211073292 MECOS 14 09 1 30000 32923 MCGC A-159 TA N W X X 28 211073352 SL- MECOS 13 08 2 00000 33520 MCGC 413 TA N W X X 28 211073462 A- MECOS 14 09 3 20000 34622 MCGC 170B TA N W X X X 28 211073462 MECOS 15 09 4 30000 34623 MCGC A-169 TA N W X X X 28 211073481 MECOS 14 09 5 40000 34814 MCGC A-224 TA N W X X X 28 211073525 MECOS 14 07 6 90000 35259 WAGER 42047 TA N W X X X 28 211073596 HOLBECK & MECOS 14 08 7 50000 35965 REIHL 1 TA N W X X X 28 211073606 MECOS 16 08 8 70000 36067 JOHNSON ET AL 1-6 TA N W X X X 28 211073618 MECOS 16 08 9 70000 36187 STEIN 1-7 TA N W X X X 29 211073628 MECOS 16 09 0 30000 36283 PARK 1-12 TA N W X X X 29 211073645 MECOS 16 09 1 50000 36455 BOYD 1-10 TA N W X X X 29 211073686 MECOS 16 09 2 40000 36864 WARD 1-11 TA N W X X X 29 211073689 MECOS 16 08 3 00000 36890 STEIN 1-18 TA N W X X X 29 211073718 MECOS 16 09 4 80000 37188 JENSEN 1-2 TA N W X X X 29 211073772 MECOS 15 07 5 30000 37723 MAY 29-23 TA N W X X 29 211073796 PACKAGING MECOS 16 07 6 30000 37963 CORPORA 1-5 TA N W X X X 29 211073855 MECOS 14 08 7 60000 38556 DEAN 25-42 TA N W X X 29 211074031 BUCHHOLZ, ET MECOS 15 07 8 20000 40312 AL 1-13 TA N W X X X

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29 211074068 PPG MECOS 16 09 9 20000 40682 VERMEULEN 1-8 TA N W X X X 30 211074096 MECOS 14 10 0 60000 40966 ANDERSON 1-20 TA N W X X X 30 211074111 MECOS 15 09 1 60000 41116 HUDSON 1-19 TA N W X X X 30 211074113 MECOS 15 09 2 70000 41137 ANGER 1-20 TA N W X X X 30 211074126 MECOS 13 07 3 70000 41267 ORR 42013 TA N W X X X 30 211074206 MECOS 16 09 4 80000 42068 STATE GRANT 1-32 TA N W X X 30 211074226 STATE COLFAX MECOS 15 09 5 40000 42264 & KN 1-31 TA N W X X X 30 211074231 MECOS 16 09 6 40000 42314 FRY 1-19 TA N W X X X 30 211074255 MECOS 15 09 7 30000 42553 BEARD 1-5 TA N W X X X 30 211074281 MECOS 15 10 8 70000 42817 HILL 1-36 TA N W X X X 30 211074352 PRIMARK MECOS 14 09 9 20000 43522 STORAGE L A-225 TA N W X X X 31 211075262 MECOS 13 10 0 00000 52620 WHITING 1-20 TA N W X X X 31 211075348 MECOS 15 09 1 90000 53489 AUSTIN 226 TA N W X X X 31 211075723 MECOS 15 07 2 10000 57231 PERRY 1-34 TA N W X X X 31 211113012 BERTHUME, MIDLA 15 02 3 60000 30126 ADDIE E 1-4 ND N W X X 31 211113037 MIDLA 15 02 4 80000 30378 DRAVES ET AL 1-12 ND N E X X 31 211113045 MIDDLETON ET MIDLA 15 02 5 70000 30457 AL 1 ND N W X X 31 211113113 MIDLA 15 02 6 40000 31134 GALLINA ET AL 1 ND N W X X 31 211113119 CLARKE, MIDLA 15 02 7 20000 31192 DONALD A 2-4 ND N W X X 31 211113251 NARMORE, MIDLA 13 01 8 30000 32513 MINA B 46 ND N W X X 31 211113457 BOWER, LILA A. MIDLA 16 01 9 50100 34575 AN 1 ND N W X X X 32 211113478 TRAVERSO MIDLA 16 01 0 70000 34787 FRANK 1 ND N W X X X 32 211113507 MIDLA 14 02 1 40000 35074 PETERS 42005 ND N E X X

156

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32 211113518 TRAVERSO, MIDLA 16 01 2 00000 35180 FRANK 2 ND N W X X X 32 211113523 MIDLA 16 01 3 70100 35237 BOWER 3-5 ND N W X X X 32 211113533 MIDLA 16 01 4 80000 35338 STALEY 1-6 ND N W X X X 32 211113546 SIERRA LAND MIDLA 14 02 5 10000 35461 CO., 1 ND N W X X X 32 211113568 FOSTER, MARY MIDLA 14 02 6 00000 35680 W. 1 ND N W X X X 32 211113568 VINCENT, MIDLA 16 01 7 80000 35688 ROBERT A 2-15 ND N W X X X 32 211113568 MIDLA 16 01 8 90000 35689 MANNING, D L 1-16 ND N W X X X 32 211113576 MIDLA 14 02 9 40000 35764 AMES, C W 1 ND N W X X X 33 211113604 MIDLA 15 02 0 60000 36046 MIESKE, EVA 2-36 ND N E X X X 33 211113614 TRAVERSO, MIDLA 16 01 1 30000 36143 FRANK 3-15 ND N W X X X 33 211113622 SOKOLOWSKI, MIDLA 14 02 2 70000 36227 C T 1 ND N W X X X 33 211113622 BREEDLOVE MIDLA 14 02 3 80000 36228 UNIT 1 ND N W X X X 33 211113625 VAN GAEVER & MIDLA 14 02 4 80000 36258 LOCK 1 ND N W X X X 33 211113625 MIDLA 14 02 5 90000 36259 PFUND, W 1 ND N W X X X 33 211113693 PLONA, MIDLA 14 02 6 00000 36930 CHESTER S 1 ND N W X X X 33 211113693 MIDLA 14 02 7 10000 36931 PLONA UNIT 1 ND N W X X X 33 211113697 LITTLE, B. F. MIDLA 14 02 8 70000 36977 UNI 1 ND N W X X X 33 211113698 MIDLA 14 02 9 30000 36983 SCHROT, JOHN J 1 ND N W X X X 34 211113702 MIDLA 14 02 0 00000 37020 CARROL UNIT 1 ND N W X X X 34 211113702 MIDLA 14 02 1 80000 37028 CLARK UNIT 1 ND N W X X X 34 211113702 MIDLA 14 02 2 90000 37029 PFUND, W 2 ND N W X X X 34 211113708 HARNICK & MIDLA 14 02 3 30000 37083 STAHL U 1 ND N W X X X 34 211113713 MIDLA 14 02 4 50000 37135 PETERS 2-1 ND N E X X

157

GR GR - NPHI Well Name Well Well Label Well - Township UWI/API NPHI County Well # Well Range Core GR - RHOB

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34 211113715 MIDLA 16 02 5 00000 37150 BOKER 1-15 ND N W X X X 34 211113717 MIDLA 15 02 6 70000 37177 MIESKE 3-36 ND N E X X X 34 211113782 MIDLA 15 02 7 10000 37821 MIESKE, E. 13241 ND N E X X 34 211113782 MIDLA 15 02 8 20000 37822 GERSTACKER 1-36 ND N E X X 34 211113793 MIDLA 15 02 9 60000 37936 DOW 1-34 ND N E X X X 35 211113796 MIDLA 15 01 0 80000 37968 NIGHTLINGER 2-23 ND N E X X 35 211113813 PLONA, MIDLA 14 02 1 10000 38131 CHESTER S 2 ND N W X X X 35 211113816 MT PLEASANT MIDLA 14 02 2 00000 38160 UNIT 5 ND N W X X X 35 211113816 MT PLEASANT MIDLA 14 02 3 60000 38166 UNIT 3 ND N W X X 35 211113816 MT PLEASANT MIDLA 14 02 4 70000 38167 UNIT 3 ND N W X X X 35 211113816 MT PLEASANT MIDLA 14 02 5 80000 38168 UNIT 5 ND N W X X X 35 211113817 MT PLEASANT MIDLA 14 02 6 00000 38170 UNIT 8 ND N W X X 35 211113843 MIDLA 15 02 7 80000 38438 SKALNICAN, M. 1 ND N E X X X 35 211113843 MIDLA 15 02 8 90000 38439 KOSCIUSZKO, E. 1 ND N E X X X 35 211113853 TRAVERSO, MIDLA 16 01 9 80000 38538 FRANK 4-15 ND N W X X X 36 211113860 MIDLA 15 02 0 50000 38605 KOSCIUSZKO, E 2 ND N E X X X 36 211113878 SKALNICAN, M. MIDLA 15 02 1 20000 38782 A 1 ND N E X X X 36 211113895 MIDLA 15 02 2 40000 38954 GERSTACKER 3-36 ND N E X X X 36 211113897 MIDLA 15 02 3 90000 38979 HOENICKE, K.R. 1 ND N E X X X 36 211113899 HOENICKE, M. MIDLA 15 02 4 10000 38991 W. 1 ND N E X X 36 211113899 SCHOFIELD MIDLA 15 01 5 80000 38998 ESTATE 1-9 ND N E X X 36 211113901 SHAHEEN, S.H. MIDLA 15 02 6 80000 39018 A 1 ND N E X X 36 211113902 MIDLA 15 02 7 00000 39020 HOENICKE, K.R. 1 ND N E X X X

158

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36 211113902 MIDLA 15 02 8 10000 39021 SHAHEEN, S.H. 1 ND N E X X 36 211113904 HOENICKE, MIDLA 15 02 9 90000 39049 M.W. 1 ND N E X X X 37 211113909 DOW MIDLA 15 02 0 30000 39093 CHEMICAL 1-26 ND N E X X X 37 211113918 WASKEVICH, ET MIDLA 15 02 1 80000 39188 AL 2-28 ND N E X X 37 211113924 MIDLA 15 02 2 70000 39247 SPITTKA, F. 1 ND N E X X 37 211113924 MIDLA 15 02 3 80000 39248 ZONDLAK, D. 1 ND N E X X X 37 211113930 MIDLA 16 01 4 90000 39309 VINCENT, R. 3-15 ND N W X X X 37 211113940 DOW MIDLA 15 02 5 10000 39401 CHEMICAL 2-35 ND N E X X 37 211113956 MIDLA 14 02 6 50000 39565 SOPER 1 ND N E X X 37 211113961 MIDLA 14 02 7 10000 39611 MEIER, C. 1-1 ND N E X X 37 211113975 MIDLA 15 02 8 70000 39757 ZONDLAK, D. 2 ND N E X X X 37 211114029 MIDLA 13 01 9 30000 40293 WARNER 1-34 ND N W X X 38 211114139 MIDLA 16 02 0 00000 41390 WHITNEY 1-33 ND N W X X X 38 211114179 CONLEY & MIDLA 13 02 1 10000 41791 STATE JA 1-3 ND N W X X X 38 211114267 STATE LEE & MIDLA 14 01 2 30000 42673 WELLI 1-15 ND N W X X X 38 211115689 MIDLA 13 02 3 80000 56898 CITY OF MASON 6-2 ND N W X X X 38 211115695 MIDLA 13 02 4 80000 56958 CITY OF MASON 13-3 ND N W X X X 38 211132749 STATE WEST MISSA 23 06 5 90000 27499 BRANCH 1 UK N W X 38 211133209 AGEMA, ALVIN MISSA 22 06 6 20000 32092 & GE 3-31 UK N W X X 38 211133376 COFFIELD MISSA 22 06 7 00000 33760 ESTATE 1-35 UK N W X X 38 211133435 MISSA 22 06 8 70000 34357 WORKMAN 10-31 UK N W X X 38 211133439 COFFIELD MISSA 22 06 9 90000 34399 ESTATE 2-35 UK N W X X 39 211133445 MISSA 22 06 0 90000 34459 THROOP, B.O. 1 UK N W X X X

159

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39 211133496 SHOENMAKER MISSA 21 06 1 40000 34964 ET AL 1-7 UK N W X X X 39 211133589 MISSA 22 07 2 90000 35899 GILDE ET AL 1-25 UK N W X X X 39 211133617 MISSA 21 08 3 30000 36173 KUIPERS A 1-29 UK N W X X X 39 211133729 MISSA 21 08 4 80000 37298 KOETJA A 1-16 UK N W X X X 39 211133868 BARTHOLOME MISSA 22 07 5 20000 38682 W 1-8 UK N W X X X 39 211133972 VANDER MISSA 23 07 6 50000 39725 VLUCHT 1-17 UK N W X X X 39 211134117 MISSA 21 06 7 90000 41179 CLAM UNION 1-31 UK N W X X X 39 211134170 STATE MISSA 21 05 8 10000 41701 HOLLAND 2-30 UK N W 39 211134171 MISSA 21 06 9 70000 41717 CLAM UNION 1-30 UK N W X X X 40 211134181 MISSA 21 05 0 40000 41814 JONES 1-19 UK N W 40 211134276 STATE MISSA 21 05 1 50000 42765 HOLLAND 3-30 UK N W 40 211134632 MISSA 21 07 2 20000 46322 QUIST 2-3 UK N W X X X 40 211172876 MONT 12 09 3 10000 28761 W-46 CAL N W X X 40 211172995 375- MONT 12 07 4 20100 30878 MCGC 1A CAL N W X X 40 211173002 BETHAM & MONT 10 07 5 70100 30027 CLARK UN 1-26 CAL N W X X 40 211173010 LONGNECKER MONT 12 05 6 70100 30107 ET AL 1-18 CAL N W X X 40 211173014 BRAYTON, EVA MONT 10 07 7 50000 30145 E ET 1-26 CAL N W X X 40 211173014 KOUTZ, MONT 11 06 8 70000 30147 LEONARD 1-30 CAL N W X X 40 211173051 MONT 12 07 9 50000 30515 MIEL, M 2 CAL N W X X 41 211173149 SL MONT 12 07 0 70000 31497 MCGC 175-A CAL N W X X X 41 211173365 MONT 12 07 1 90000 33659 WHITCOMB 1 CAL N W X X 41 211173515 SL- MONT 12 07 2 40000 35154 MCGC 425 CAL N W X X X 41 211173636 MONT 12 06 3 80000 36368 TOWLE, D 1A CAL N W X X X

160

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41 211173808 MONT 11 07 4 10000 38081 TIESNER 1-27 CAL N W X X X 41 211173948 MONT 11 05 5 30000 39483 WALDRON 2-30 CAL N W X X 41 211173950 MONT 09 06 6 30000 39503 HECHT ET AL 1-24 CAL N W X X 41 211175144 MONT 11 08 7 70000 51447 EVANS 1-6 CAL N W X 41 211175859 MONT 12 06 8 40000 58594 NEAL 2-10 CAL N W X X X 41 211232187 NEWA 14 11 9 10000 21871 MCGC 59 YGO N W 42 211232332 VAN WYLEN, NEWA 11 12 0 90000 23329 GERRIT 1 YGO N W X 42 211232700 WEMPLE, ANNA NEWA 13 11 1 10000 27001 L ET 1 YGO N W X 42 211232813 BRYDGES, NEWA 11 13 2 70000 28137 BLAIR 1 YGO N W X 42 211232864 NEWA 12 11 3 80000 28648 MWPLC C YGO N W X 42 211233388 NEWA 16 11 4 40000 33884 COUSINEAU, D. 1-33 YGO N W X X 42 211233413 NEWA 16 11 5 00100 34130 ENGLUND 1-30 YGO N W X X 42 211233444 NEWA 16 11 6 10000 34441 DEVRIES, B. 1-27 YGO N W X X 42 211233490 NEWA 16 11 7 60000 34906 LUTZ 42031 YGO N W X X X 42 211233531 NEWA 16 11 8 10000 35311 BAKER 1-28 YGO N W X X X 42 211233856 NEWA 13 12 9 10100 38561 ROSS 1-9 YGO N W X X 43 211233919 NEWA 15 11 0 20000 39192 KAILING 1-35 YGO N W X X X 43 211233944 NEWA 15 12 1 30000 39443 THOMPSON 1-27 YGO N W X X X 43 211233995 NEWA 13 11 2 20000 39952 WISE, ET AT 42007 YGO N W X X 43 211234162 STATE NEWA 15 11 3 80000 41628 NORWICH 1-22 YGO N W X X X 43 211234254 STATE NEWA 14 11 4 80000 42548 GOODWELL & 1-11 YGO N W X X X 43 211234583 NEWA 15 11 5 10000 45831 GOODWELL 1 YGO N W X X X 43 211234865 NEWA 14 11 6 90000 48659 VIVODA, ET AL 1-21 YGO N W X X

161

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RHOB

- PEF

43 211235099 NEWA 14 11 7 20000 50992 GOODWELL 1 YGO N W X X X 43 211235808 NEWA 14 11 8 10000 58081 WELLMASTER 1-1 YGO N W X X X 43 211235919 NEWA 15 12 9 00000 59190 STATE MONROE C1-6 YGO N W X X X 44 211292700 OGEM 21 01 0 60000 27006 LEHMAN, E A 1 AW N E X 44 211295760 OGEM 21 04 1 10000 57601 CLAYTON UNIT 14-31 AW N E X 44 211332642 LR- OSCEO 18 10 2 70000 26427 MCGS 13-5 LA N W X 44 211333221 DUDDLES, OSCEO 18 10 3 60000 32216 RICHARD 1-9 LA N W X X 44 211333381 OSCEO 18 08 4 30000 33813 MCCORMICK 1-27 LA N W X X 44 211333453 MCCORMICK ET OSCEO 18 08 5 60000 34536 AL 2-27 LA N W X X X 44 211333455 OSCEO 17 08 6 80000 34558 FREUDENBURG 1-31 LA N W X X X 44 211333508 RICHARD OSCEO 20 07 7 90000 35089 QUAST 1-20 LA N W X X X 44 211333548 OSCEO 19 07 8 20000 35482 ROBINSON 1-31 LA N W X X X 44 211333597 OSCEO 17 08 9 70000 35977 WARK 1-30 LA N W X X X 45 211333603 OSCEO 17 09 0 30000 36033 GREIN ET AL 2-36 LA N W X X X 45 211333606 BABCOCK ET OSCEO 17 09 1 80000 36068 AL 1-36 LA N W X X X 45 211333611 OSCEO 17 09 2 00000 36110 THOMPSON 3-36 LA N W X X X 45 211333618 OSCEO 17 09 3 60000 36186 PAINE 1-35 LA N W X X X 45 211333633 OSCEO 17 08 4 60000 36336 PARK 1-31 LA N W X X X 45 211333635 OSCEO 17 09 5 50000 36355 STATE HERSEY 2-35 LA N W X X X 45 211333642 OSCEO 17 08 6 60000 36426 MCCLAIN 1-28 LA N W X X X 45 211333650 OSCEO 17 09 7 60000 36506 COMPTON 1-13 LA N W X X X 45 211333660 OSCEO 17 09 8 00000 36600 THOMAS 1-26 LA N W X X X 45 211333664 OSCEO 17 09 9 80000 36648 BASS 1-32 LA N W X X X

162

GR GR - NPHI Well Name Well Well Label Well - Township UWI/API NPHI County Well # Well Range Core GR - RHOB

# -

RHOB

- PEF

46 211333692 OSCEO 17 09 0 50000 36925 BALDINO 1-36 LA N W X X X 46 211333694 WOODWARD ET OSCEO 17 09 1 20000 36942 AL 1-26 LA N W X X X 46 211333710 OSCEO 19 07 2 90000 37109 VANSCOYOC 1-32 LA N W X X X 46 211333719 OSCEO 20 09 3 30000 37193 EGGLE A 1-4 LA N W X X X 46 211333730 OSCEO 17 08 4 00000 37300 KOZITZKI 1-16 LA N W X X 46 211333751 OSCEO 17 09 5 90000 37519 MILLER 1-25 LA N W X X X 46 211333765 OSCEO 17 08 6 50000 37655 BARKER 1-15 LA N W X X 46 211333800 OSCEO 17 07 7 50000 38005 BRADY 7-12 LA N W X X X 46 211333820 OSCEO 20 09 8 10000 38201 EGGLE A 2 LA N W X X X 46 211333846 OSCEO 17 08 9 30000 38463 VUKIN UNIT 1-19 LA N W X X X 47 211333943 SUNDMACHER OSCEO 18 09 0 30000 39433 ET AL 1-33 LA N W X X 47 211334013 OSCEO 18 10 1 70000 40137 ZINGER, H. 1-1 LA N W X X X 47 211334015 OSCEO 18 10 2 60000 40156 GREENWALD 1-27 LA N W X X X 47 211334033 OSCEO 17 08 3 30000 40333 PETERSON 1-12 LA N W X X X 47 211334055 OSCEO 19 10 4 60000 40556 LOWE 1-27 LA N W X 47 211334063 OSCEO 18 10 5 70000 40637 BRUSKE 1-26 LA N W X X X 47 211334066 OSCEO 18 10 6 50000 40665 GIESE 1-34 LA N W X X 47 211334076 OSCEO 18 10 7 40000 40764 HOPMEIER, M. 1 LA N W X X X 47 211334078 OSCEO 20 07 8 30000 40783 QUAST 1-9 LA N W X X X 47 211334081 OSCEO 20 07 9 00000 40810 EISENGA UNIT 1-29 LA N W X X X 48 211334083 OSCEO 19 09 0 70000 40837 WANNER 1-32 LA N W X X X 48 211334092 OSCEO 18 09 1 40000 40924 LOOP 1-6 LA N W X X X 48 211334094 PARMELEE, OSCEO 18 09 2 50000 40945 LEON 1-7 LA N W X X X

163

GR GR - NPHI Well Name Well Well Label Well - Township UWI/API NPHI County Well # Well Range Core GR - RHOB

# -

RHOB

- PEF

48 211334161 NELSON & OSCEO 19 09 3 20000 41612 STATE RO 1-10 LA N W X X X 48 211334174 OSCEO 20 08 4 20000 41742 VEDDLER 1-11 LA N W X X X 48 211334177 OSCEO 19 08 5 70000 41777 FAUBLE 1-1 LA N W X X X 48 211334178 EISENGA OSCEO 20 08 6 80000 41788 BROTHERS 11-24 LA N W X X X 48 211334182 OSCEO 18 08 7 50000 41825 ERSKINE 1-35 LA N W X X X 48 211334229 OSCEO 17 10 8 20000 42292 HAYES 1-29 LA N W X X X 48 211334231 OSCEO 20 08 9 30000 42313 HIGHLAND 1-17 LA N W X X X 49 211334259 OSCEO 17 07 0 60000 42596 HARTER 1-32 LA N W X X X 49 211334294 STATE OSCEO 19 08 1 50000 42945 HARTWICK & 1-27 LA N W X X X 49 211334336 MOOMEY, OSCEO 20 08 2 50000 43365 DELORES 1-19 LA N W X X X 49 211334480 RC- OSCEO 18 10 3 00000 44800 Reed City 132 LA N W X X X 49 211335452 OSCEO 18 10 4 60000 54526 BRUSKE 2-26 LA N W X X X 49 211335670 OSCEO 17 09 5 50000 56705 OEHRLI 1-30 LA N W X X X 49 211335738 OSCEO 17 10 6 10000 57381 SCHMIDT 1-35 LA N W X X X 49 211335872 STATE EVART & OSCEO 17 08 7 00000 58720 FOR 3-12 LA N W X X X 49 211335917 OSCEO 17 10 8 30000 59173 SOPER 1-25 LA N W X X X 49 211433354 PORTER HOGAN ROSCO 22 04 9 40000 33544 TRUS 3-17 MM N W X 50 211433597 ROSCO 22 02 0 00000 35970 STATE BACKUS 1-27 MM N W X X X 50 211433626 ROSCO 22 02 1 90000 36269 STATE BACKUS 2-27 MM N W X X X 50 211433630 ROSCO 22 02 2 90000 36309 STATE BACKUS 5-27 MM N W X X X 50 211433631 ROSCO 22 02 3 00000 36310 STATE BACKUS 1-28 MM N W X X X 50 211433668 STATE BACKUS ROSCO 22 02 4 40000 36684 A 1-27 MM N W X X X 50 211433677 ROSCO 22 02 5 50000 36775 STATE BACKUS 4-28 MM N W X X X

164

GR GR - NPHI Well Name Well Well Label Well - Township UWI/API NPHI County Well # Well Range Core GR - RHOB

# -

RHOB

- PEF

50 211433677 ROSCO 22 02 6 60000 36776 STATE BACKUS 3-28 MM N W X X X 50 211433710 ROSCO 21 01 7 20000 37102 HAHN 1-12 MM N W X X X 50 211433740 ROSEVILLE ROSCO 21 01 8 90000 37409 GUN CLUB 1-17 MM N W X X X 50 211433776 ROSCO 21 01 9 10000 37761 GRIFFIN 1-12 MM N W X X 51 211433861 ROSCO 24 04 0 10000 38611 STATE LYON A 1-35 MM N W X 51 211433911 STATE ROSCO 23 01 1 30000 39113 RICHFIELD 1-26 MM N W X X X 51 211433982 BGHL & ROSCO 22 03 2 60000 39826 SCHMALTZ 1-23 MM N W X 51 211433994 STATE ROSCO 21 03 3 10000 39941 ROSCOMMON U 1-29 MM N W X X 51 211434137 STATE ROSCO 21 03 4 80000 41378 ROSCOMMON 1-30 MM N W X X X 51 211453613 SAGIN 12 05 5 70000 36137 MAURER 1-25 AW N E X 51 211453636 UNION TEXAS & SAGIN 13 04 6 30000 36363 THO 1-27 AW N E X 51 211453971 SAGIN 12 03 7 60000 39716 MURPHY 1-16 AW N E X X X 51 211454011 SAGIN 09 02 8 10000 40111 COONROD 1 AW N E X X X 51 211454025 BIRCHMEIER, SAGIN 09 04 9 90000 40259 DAVID 1 AW N E X 52 211454103 SAGIN 11 03 0 70000 41037 BLONIARCZYK 1-31 AW N E X 52 211454146 FITZGERALD SAGIN 09 02 1 50000 41465 UNIT 1 AW N E X 52 211455054 SAGIN 09 03 2 40000 50544 VRABLE 3-24 AW N E X 52 211455078 HUNTING SAGIN 09 04 3 70000 50787 EXPLORATI 4-18 AW N E X 52 211455502 SAGIN 13 05 4 40000 55024 SCHULTE 1-20 AW N E X X X 52 211553072 HASSELBRING SHIAW 06 01 5 70000 30727 ET AL 1-5 AS N E X 52 211554521 SHIAW 08 02 6 40000 45214 SAWER 1-2 AS N E X 52 211574147 TUSCO 14 08 7 00000 41470 AKRON 1-36 LA N E X 52 211653586 WEXFO 23 10 8 60000 35866 LANGE 1-5 RD N W X X X

165

GR GR - NPHI Well Name Well Well Label Well - Township UWI/API NPHI County Well # Well Range Core GR - RHOB

# -

RHOB

- PEF

52 211654021 WEXFO 21 12 9 00000 40210 DOSTAL, ET AL 1-27 RD N W X X X 53 211654086 WEXFO 21 09 0 10000 40861 GEORGE ET AL 23-6 RD N W X X X 53 210350956 210350956 1 90000 90000 MODER, E A 1 53 210352423 210352423 2 90000 90000 Yake et al 1 CLARE X 53 210352546 210352546 20 06 3 20000 20000 MGSC 9 CLARE N W X 53 210352599 210352599 4 50000 50000 MCGS 42247 CLARE X 53 210352604 210352604 5 60000 60000 MCGS 9-71 CLARE X 53 210731049 210731049 ISABEL 16 03 6 00000 00000 METHNER, F 1 LA N W X X X 53 210731139 210731139 7 40000 40000 HOFFMAN, F 2 53 210733984 210733984 ISABEL 14 03 8 30000 30000 MT PLEASAN 1 LA N W X X X 53 211232187 211232187 9 10100 10100 MCGC 5 CLARE 54 INGHA 01 02 0 2 NP07108 SB 15 M N W X

166