JUN 0 3"}‘999 i1 4 NW 2007 A PRE—PENNSYLVANIAN PALEOGEOLOGIC STUDY OF MICHIGAN By Timothy Arthur Strutz A THESIS Submitted to Michigan State University in partial fulfillment of the requirements for the degree of MASTER OF SCIENCE Department of Geology 1978 I _ 7|- L ti ABSTRACT A PRE-PENNSYLVANIAN PALEOGEOLOGIC STUDY OF MICHIGAN By Timothy Arthur Strutz A study of gamma—ray/neutron logs of four units: the Mississippian Bayport Limestone, the Pennsylvanian System, the Jurassic "Red Beds", and the Pleistocene glacial drift provided the framework for determining the regional distri— butional patterns and interrelationships of these sediments in the Michigan Basin. Isopach maps were constructed for each of these along with structure contour maps of the Bayport and the Mississippian—Pennsylvanian unconformity, and a pre- Pennsylvanian paleogeologic map. Stable tectonic conditions have existed in the Michigan Basin since the Late Mississippian. In many areas the Bayport is completely eroded away and is reflective of river drainage systems. Bayport structural "highs" often are indicative of closures in the underlying Michigan Stray sandstone which are known to be productive of gas. Depocenters of all these units are located near the center of the Lower Peninsula of Michigan. The Jurassic implies an asymmetrical aspect to the Michigan Basin configuration. ACKNOWLEDGEMENTS The author wishes to thank Dr. James H. Fisher, my thesis committee chairman, for his advice, assistance, and friendship during the preparation of this study. Appreciation is also extended to Dr. A.T. Cross and Dr. F.W. Cambray for their ad- vice and review of the thesis. I am also grateful to Garland Ells of the Michigan Geolog— ical Survey for his cooperation in obtaining data, and the late Harold McClure of McClure Oil Company for allowing me the use of their files. Gratitude is also extended to the Tenneco Oil Company for their financial assistance which enabled the completion of this paper, and to Tom Campbell of Merritt Enter— prises forthe many hours of help with the computer programing and mapping. Thanks are also extended to Mike Puzio for the final drafting of many of the maps and to Deb Kirchen for the typing of this manuscript. Finally, I would like to thank my parents, Mr. and Mrs. Arthur C. Strutz, for all their encouragement both prior to and during this study. ii TABLE OF CONTENTS LIST OF FIGURES. LIST OF PLATES I. INTRODUCTION Purpose of the Study, Methodology Previous Investigations II. GENERAL STRUCTURE. III. GENERAL STRATIGRAPHY Mississippian Pennsylvanian Jurassic. Pleistocene Generalized Cross-Sections. IV. CONCLUSIONS. APPENDIX BIBLIOGRAPHY iii Page iv 13 13 22 26 3O 31 3A 38 66 Figure l. 2. LIST OF FIGURES Control point distribution. Michigan Basin and surrounding structural elements. . . . . . . . . . . . . . . Stratigraphic succession in Michigan, Mississippian through Recent. . . . . . . . . . . . . . . . . . Combined depocenters. Distribution of Mississippian, Pennsylvanian, and Jurassic strata in the Michigan Basin . . . . . The Pennsylvanian System in Michigan. Generalized lithologic cross—section A~A' Generalized lithologic cross—section B-B' iv IO 14 I7 23 25 32 33 LIST OF PLATES Plate All plates in pocket I. Isopach map of Bayport Limestone 2. Structure contour map on the base of the Bayport 3. Major Michigan Stray sandstone gas fields in relation to Bayport structural "highs” map A. Pre-Pennsylvanian paleogeologic map 5. Structure contour map on the Pennsylvanian unconformity 6. Isopach map of Pennsylvanian 7. Isopach map of Jurassic "Red Beds" 8. Isopach map of Pleistocene glacial drift INTRODUCTION Purpose of the Study The intent of this study is to determine the regional distributional patterns and interrelationships of sediments that range from Late Mississippian through the Pleistocene in the Michigan Basin. It should also be helpful in deter— mining whether the time of deformation of the Michigan Basin is restricted to the Mississippian or if it is evident in the Pennsylvanian. Interpretations of the paleodrainage pat— terns, origin of the sediments, and the possibility of traps for oil and gas in this area of the Michigan Basin will also be determined. Methodology This study is concerned with four different units which range in age from the Late Mississippian to the Pleistocene. They include: the Mississippian Bayport Limestone, the Penn— sylvanian Saginaw and Grand River Formations, the Jurassic "Red Beds", and the Pleistocene glacial drift. The mapping of these units isbased uponwell dataobtained from Michigan State University, the Geology Division of the Michigan Depart— ment of Natural Resources, and local oil companies. E Extensive well coverage (Figure l) is available in almost all of the study area and the data used in mapping these units came almost exclusively from gamma—ray (Figure 2), neutron and gamma-ray, and sonic well logs. Additional information was available through core hole records and well samples. The gamma-ray log is the most consistent and accurate means for delineating lithologies in the Michigan Basin while the neutron and sonic logs are useful when looking for variations in por— osity. Mechanical logs are made on nearly all the oil and gas wells drilled in Michigan and are valuable data sources for studying the lithology of the subsurface. They have the added advantage of being continuous which alleviates the problems of sample lag, lost samples, sample mixing, and lost circulation. Sample coverage is fairly extensive and can be valuable. However, sampling error is common and because of this, the ac- curacy of sample tops may be questionable. Thus, samples were examined only on certain wells to determine the top of the Jurassic "Red Beds" on the mechanical logs, and in an attempt to differentiate between the Pennsylvanian Grand River and Saginaw Formations. Sample descriptions were also of value. These were from published survey logs and served as an aid in checking lithologies in areas where facies merged or units %gh‘ fluctuated markedly. Over 670 well logs were used in this ‘fi; study. First correlations were made along the Albion—Scipio a fault trend due to the dense well coverage of that area. From ‘ this initial point, extensions were made to include the re— mainder of the study area. I I u | I I I *- JIQMI I .. ° ‘ ' £‘4.?'£—£ —' i 2‘32. .2“- . - I I I I! I . — Llllgu :u'“. ' I I : I ”Ig‘ll.*gm. "In. I . I - - - Lio- "Av. I ' “‘uIIIII I . 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I “I ‘ I '--II_'I-.“' I... ...!:I'I .|I'.. .- I I I I r-' WAS»: my}; w ago. ' | . I I an .. .0 I.) | ' & .it. 1-" A O I'IN I ' ' I N' .z ’ —-—“:.2~ o. . IV“! I I. I... I I 2"2-4 ... I . o _ I -03." “I‘ll-“10° I '. .0 #1:: u . I I I I ' ._ _‘ (in: u" x ...3 . a a I —. .2 3.... I u I II'INN I I I I I I... - ’IILIILII' I w" I (‘3. I" : ' . '[ "" -- .-N.E. ~ ’03:". II‘NCN I I . ”Nauru FIGURE‘I CONTROL POINT DISTRIBUTION PLEISTOCENE JURASSIC numvmumj “no" . l 4. MICII IOAN MARSHA“ COLDWATER III“! 0" OWN III! ITIAY IMOSTONI FIGURE-2 STRATIGRAPHIC SECTION WITH TYPICAL GAMMA RAY CURVE Eight maps were constructed based on the data obtained from the well logs. A Pre—Pennsylvanian paleogeologic map was constructed along with structure contour maps for the Mississippian—Pennsylvanian unconformity and the Mississip- pian Bayport Limestone. Isopach maps were made for the Pleistocene glacial drift, the Jurassic "Red Beds", strata of the Pennsylvanian System, and the Mississippian Bayport Limestone. A map showing the major Michigan Stray sandstone gas fields in relation to Bayport structural "highs” was also constructed. The General Purpose Computer Program (GPCP) was used in the initial phase of the construction of many of these maps. This FORTRAN computer program displays functions of two var- iables graphically as contour maps. It is suited for a number of contouring applications such as, gravitational and magnetic fields, strata depths in geophysics, temperature and baromet- ric pressure in meterology, and in electrical and magnetic field intensity. It is very flexible and is able to present the contours in a form suitable for display on a Calcomp plot- ter. The surface can be specified either by giving its values at the mesh points of a rectangular array, or by giving its values at random points in a region of interest. This program will grid data. That is, the values of the function at the mesh points of a rectangular array are estimated as are the contours produced from this gridded data. These data are gen— erated from random data by a procedure which analytically constructs a smooth surface passing through every data point. The resulting contour may be influenced by the 35 nearest data points or less. This feature is of much value in cer- tain problems, such as in geologic mapping where the user needs a certain amount of control over the shape of the con— tours. These computer maps were then subject to alteration wherever it was deemed necessary. Previous Investigations Studies of the Late Mississippian and younger strata in the Michigan Basin have been limited and for the most part, have not been concerned with showing relations between sys- tems. However, there have been some investigations of indi- vidual formations or systems from this geologic time sequence. Work on the Bayport Limestone has been limited. Cohee (1951) and McGregor (1953) both did work on the Mississippian but neither placed much emphasis on the Bayport. Bacon (1971), concluded from his study on the Bayport of the Wallace Stone Company Quarry at Bayport, Michigan, that the formation was deposited in a sabkha environment. Lasemi (1975) did an an- alysis of the stratigraphy and subsurface geology of the Bayport in the Michigan Basin. He subdivided the formation into three units and drew isopach and lithofacies maps of each unit. From these, he concluded that the upper and lower units were deposited in intertidal or lower supratidal en- vironments, while the middle one was deposited after a major transgression. The most comprehensive studies of the Pennsylvanian System in the Michigan Basin have been conducted by Kelly (1936) and Shideler (1965). Kelly, provided valuable in- formation regarding Michigan faunas and floras of Pennsyl- vaniarxageand also provided needed lithologic and strati- graphic descriptions. Shideler, divided the Pennsylvanian into three intervals and constructed isopach maps for each. The sediments of the oldest interval are Morrowan in age and formed in either a neritic or deltaic environment. The mid- dle unit resulted from alluvial flood plain and shallow neri- tic conditions and is Atokan in age. The youngest unit is Desmoinesian in age and is mostly fluvial sediments with some minor shallow neritic deposits. According to the Michigan Geological Survey, the youngest Pennsylvanian sediments are Conemaugh. However, no sediments of this series have ever been found in the Michigan Basin (Cross, 1978). Shideler, also provided important information regarding the variability and thickness of the lithology of the Pennsylvanian System in Michigan, and constructed a Pre—Pennsylvanian paleogeologic map of the basin. He found Bayport Limestone to be the pre- valent formation below the unconformity while Michigan Forma- tion strata were found along the edges of the basin and in scattered locations in the center. Additional work on the Pennsylvanian was conducted by Cohee, et a1. (1950), and Kalliokoski and Welch (1976). They compiled a great deal of subsurface data and through it, pre- pared estimates of Michigan's coal reserves. Prior to 1931, the term "Red Beds" had been referred to only occasionally in the geologic literature of Michigan. Newcombe (1931), referred to them as a series of shales, sand- stones, and gypsum which were widespread in the center of the Michigan Basin. From this, Martin (1936) listed them as Permo-Carboniferous. A more recent study was done by Sander (1959). He applied mineralogical, sedimentological, and thickness distribution analyses to paleogeographic consider- ations and concluded that they formed under marine conditions. Cross (1966) was the first to assign the "Red Beds" of the Michigan Basin to the Jurassic. Shaffer (1969) palynological- 1y determined that they are Jurassic in age. There have been many studies of the Pleistocene drift of the Michigan Basin. Hough (1958) was concerned with the evo- lution of the Great Lakes basins. Kelly and Farrand (1967) constructed various maps which show the boundaries of the Wisconsin drift, preglacial drainage patterns, and the prin- ciple morainic systems. A more recent investigation was done by Welsh (1971) on thepatterns of compositional variation in some glaciofluvial sediments in the Lower Peninsula of Michi- gan. GENERAL STRUCTURE The Michigan Basin is a roughly circular intracratonic basin with an areal extent of approximately 122,000 square miles. It consists of the entire Lower Peninsula of Michigan, the eastern half of the Upper Peninsula, the area underlain by Lake Michigan and Lake Huron, and small portions of Ontario, Ohio, Indiana, Illinois, and Wisconsin. The basin is surrounded by major positive tectonic struc- tures (Figure 3) that have greatly influenced and partially controlled the configuration of the basin (Ells, 1969). It is bounded to the north and northeast by the Canadian Shield, on the northwest and west by the Wisconsin Arch and Highlands, and to the east by the Algonquin Arch. The Findlay Arch sep- arates it on the southeast from the Appalachian Basin, while the Kankakee Arch marks the boundary between the Michigan Basin and the Illinois Basin. All of these structures have been active in the geologic past and are believed to have originated in either the Precambrian (Pirtle, 1932; Newcombe, 1933) or in the Cambrian (Cohee, 1951). The Michigan Basin has within it many intrabasinal struc— tural features that include a number of joint systems, and fault patterns. There are two recognizable major trends. The dominant one has a northwest-southeast direction and is 10 CANADIAN SHIELD I am I . 2‘ . MAJOR ‘ 2‘ I / STRUCTURAL ‘ TRENDS ,I ,l \N ‘\ E \\\/ 2.3.: I \ ‘ 3 \/ ¢ § {9/ ‘ ALBION- 13°26? w:sco~sm\ “TOE E""\ I I Q ILLINOIS\ \R\\ 8*” \ ImcmGAN 4“ I,“ \\ V INDIANA omo ' \ I I}! sf. FRANCISVILLE j 3:”, $/ HOWELL Mic“ . >\+,’ *0 A, ANTICLINE aka, '9“? I \\‘°¢ I LOOANSPORT FAULT \ FIGURE-3 MICHIGAN BASIN AND SURROUNDING STRUCTURAL ELEMENTS (uoomeo AFTER ELLS,1969) 11 concentrated in the eastern, southeastern, and central parts of the Lower Peninsula of Michigan. It includes such features as the Albion-Scipio fault trend and the Howell Anticline. A northeast trend is also distinguishabletnu;occures mostly in the western and southwestern portions of the Lower Peninsula. It is generally accepted that the Precambrian basement complex is primarily responsible for these structural patterns (Pirtle, 1932). Folding occurred throughout the Paleozoic while the major deformation is Late Mississippian (Landes, 19A8). The Michigan Basin in approximately its present day out- line first formed in Middle Ordovician time (Fisher, 1969) and is fairly shallow with the depth to the Precambrian being only 1U,000 to 15,000 feet. The largest structural feature in the basin is the Howell Anticline. It trends in a north- west direction and is located in Livingston and Shiawassee Counties. It is believed to have formed at the beginning of Goldwater time (Paris, 1977) and is due to recurrent movements along old lines of weakness in the Precambrian basement (Kil- bourn, 19A7). Thus, the anticline formed as a result of faulting which caused the northeast side of the fault to be uplifted. There are three dominant theories which have been pre- sented on the orgin of the Michigan Basin. Many (Newcombe, 1933; Fisher, 1978) believe that the structural features of the basin are due to faulting and zones of weakness in the Precambrian basement complex. Hinze (1963) claimed that the formation was due to the addition of basic rocks to the 12 Precambrian basement which was followed by an increase in isostatic subsidence as a result of the added weight. In 1976, Haxby, et a1., suggested that diapirs of mantle material moved upward and penetrated the lower crust. The intense heat re- sulting from this upward progression caused the metastable gabbro to change to ecologite. After cooling, this newly form- ed denser material caused the basin to subside in an effort to achieve isostatic equilibrium. GENERAL STRATIGRAPHY Some of the names used in this study are based on the State of Michigan stratigraphic chart (Figure A). Lithologic contacts, with the exception of the Jurassic, were based on work done by the Michigan Basin Geological Society (Fisher, et a1., 1969). The Jurassic was picked from mechanical logs after the top was determined through sample analysis and could be consistently correlated with most of the written descriptions. Mississippian The Bayport Limestone Formation is Late Mississippian in age and forms a part of the Grand Rapids Group in the Michigan Basin area. It is a buff colored, dense limestone and dolomite that has minor amounts of chert, sand, and shale (Kropschot, 1953). It lies with minor disconformity upon the Michigan Formation which consists mostly of shale, with some dolomite, sand, and gypsum. The Michigan Formation is made up of informal subunits which include: the Triple Gyp, Brown Lime, Stray—stray sandstone, Stray dolomite, and Stray sand- stone. Of these, only the Stray-stray and Stray sandstones are known to be producers of hydrocarbons in economic quanti- ties. The Saginaw Formation of Pennsylvanian age unconformably l3 114 PLEISTOCENE NOMENCLATURE ERA SYSTEM SERIES STAGE U RECENT — V“! Sui- 9: “T" man... 0 QUATERNARY PLEISTOCENE am (a u I z Tun-I III-l mm U MGM OUTCROP NOMENCLATURE , “$3?“ TlME-STRAYIGRADHIC ROCK-STRAYIGMIC J o 2 g 2 g 5 SERIES GROUP FORMATION MEMBER w >- lfl A. w «n 2 U u 8a-a o g 3 g KIMEIIDGIAN a 2 a 2 i i u...— E I; 5 CONEMAUGH Cir-d n.- r. d...“ g g b.- i‘ F‘ § _§ 55% POTTSVILLE Soon-In 1...... (ND 3: “‘ a‘ O z w z I W U LIJ g 2 g MERAMECIAN am we: _ . _’ 2 .1 E undo-I in < 2:2 OsAOIAN W5; W“ a 3 a: 3 Li 5 2 KINDERHOOKIAN an... 9, EXPLANATION e -. .-.'_'.I'- I. I“; M . ' ' a“: SLBSURFACE NOMENCLATURE ROCK-STRATIGIA'HIC I FORMATION jMEMBERl GROUP WW mind“ ”It.“ Wmmtnbd.dndm and“ . "' "led “dz" unnamed mo] hummus '1 ‘ v, ‘ x «no . Manny.” “J‘WV‘VI' 3 7 '_ cad...» Sh“ a”. INFORMAL TERMS wadmedMme-dnm ”dW-Mdmuumnh dubs mm mm RAYS “*d ht _* uh hhmd bun: w "3—“ and ~n “A“ Hui-ls: a-oou Educ-u- wfi wand—G- au-a-od 4L FIGURE-4 STRATIGRAPl-IIC SUCCESSION IN MICHIGAN NISSISSIPPIAN (AFTER mcchN DEPARTNENT OF NATURAL RESOURCES) THROUGH RECENT 15 overlies the Bayport Formation and fills the irregular surface which is the result of the post-Bayport erosion. Brachiopod studies (Oden, 1952) have been used to correlate the Bayport with the lower part of the Maxville limestone of Ohio, and the St. Genevieve and St. Louis limestones of the Mississippi Valley. Lithologic observations indicate that the Bayport was deposited in a fairly stable tectonic environment. It may be subdivided into three units on the basis of lithology and fos- sil rich zones (Lasemi, 1975). The initial Bayport sediments were deposited after the cessation of the predominantly late evaporite depositional phase of the Michigan Formation. A slight rise in sea level caused the evaporite lagoons to give way to carbonate flat de- position. Both the lower and upper units are similar in lith- ology and consist mostly of dolomite with some chert and inter- bedded sandstone. They were deposited in an intertidal or lower supratidal environment (Lasemi, 1975). The middle unit is comprised of a relatively pure fossil- iferous limestone that was deposited after a major transgres— sion. This provided an excellent environment for the develop- ment of organisms. It may also indicate that the Michigan Basin was connected to adjacent basins where the open circula- tion of sea water produced fairly similar environments (Lasemi, 1975). A gradual regression preceded this which provided a similar environment of deposition to that of the lower unit. Fluctuations in sea level did occur and are indicated by sand- stone lenses. 16 After the deposition of the upper unit, the entire area was uplifted and extensive erosion resulted in the removal of much of the upper unit. The major area of subsidence was in the northeastern part of the basin while the major pos- itive features were located to the south, east, and northwest. An isopach map (Plate 1) illustrates the thickness var- iations of the Bayport strata. This displays a generally progressive thickening from the peripheral areas towards the interior. However, irregularities in this trend do exist and are due to post-Mississippian erosion. In fact, in many areas of the basin, the Bayport has been completely eroded away as river systems cut downward through the strata as they moved towards the interior of the basin. The major depocenter (Figure 5) is in southwestern Clare and northwestern Isabella Counties. Smaller centers are found in eastern Mecosta, northeastern and west central Mont- calm Counties. The structural center and depocenter of this formation conform quite well with the present basin depocenter which is located in northwestern Arenac and northeastern Gladwin Counties (Fisher, 1978). This suggests that relatively stable tectonic conditions have existed since the Meramecian. The maximum thickness of the Bayport is 252 feet and occurs in Montcalm County. There are areas of abnormal thickness that are found in the east and northeast portions of the basin. These are primarily due to greater post depositionsl erosion of the upper Bayport in the west and southwest areas of the basin. 17 I I I I I I ' I £45". I LCIIIOVO‘I‘J "“00! "ll _ _1 . _, _ . . .- ..¢_nluv°u] . .: I a I I I . I I nun- . ounce ammo-Ina; ALIINA "um“ _ -.- - - -.. _ -- .. . . - _. .. .— - . . - . I ' I l I . 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I I ' l l ' I I ' - I I I "nun (An ’31. Jenna II II I I I "‘I must-nu , ”nun! memo: FIGURE-5 COMBINED DEPOCENTERS. IAYPORI’ fl JURASSIC PENNSYLVAN IAN 73.55:, PRESENT {III I M” 18 A structure contour map (Plate 2) constructed on the base of the Bayport Formation reflects the irregular thickness of the Michigan Formation. It indicates that a number of local basins and domes were present at the time of deposition, or were produced by subsidence at the time of deposition. There is a good relationship between structure and thickness. Thicker Bayport accumulations can be found associated with structurally lower areas while thinner accumulations lie on structurally higher topography. Many of the Bayport structural highs reflect known closures in the Michigan Stray sandstone (Plate 3). These Stray closures are quite small with most not exceeding 125 feet of relief (Elowski, 1978). These are of economic sig- nificance as many are associated with natural gas production. Stray production can be found in Newaygo, Osceola, Clare, Missaukee, Montcalm, Roscommon, and Isabella Counties. These areas besides producting natural gas, are also becoming val— uable for natural gas storage. Not all Bayport structural "highs" correspond to known closures in the Michigan Stray sandstone. Four large closures are located south of all known Stray production. The closest significant structural "high" is in southeastern Montcalm County while the others are found in south central Gratiot, northeastern Clinton, and northeastern Eaton Counties. The one in southeastern Montcalm County is the most probable ap- parent structure for Stray production. Thiszhsbased ontflmafact thattflueStray undergoe521facies changetx>the southeast and thus, 19 is primarily restricted to the seven county area where there is known Stray production. Thus, it may not be found under- lying any of the Bayport "highs". There are five structural highs that are surrounded by Stray production but are themselves non—productive. These areas are located in southwestern Missaukee, eastern Osceola, northeastern Newaygo, eastern Mecosta, and eastern Isabella Counties. The total thickness of the Michigan Formation does fluctuate and it is possible that these highs reflect a thicker sequence of Michigan strata between the top of the Stray sand- stone and the Bayport. Thus, the structural closure exhibited in the Bayport may not be present in the Stray. The struc- tures could also lack a necessary source and thus, not be pro- ductive. However, there is the possiblity that natural gas may be found associated with these highs and may be located as further drilling defines the apparent structure. It is possible that the Bayport highs may become more pronounced in the lower strata. Thus, drilling of these areas may prove profitable for the accumulation of hydrocarbons from not just the Michigan Stray sandstone, but from other lower formations as well. Existing Stray structural gas fields may also be indicative of structural closure in deeper for- mations that may subsequently also be of economic value. The Mississipian System is separated in the Michigan Basin from the overlying Pennsylvanian strata by a major un- conformity. The Mississippian strata have been subjected to 2O much post—depositional erosion and the resulting pattern is illustrated by a Pre-Pennsylvanian paleogoelogic map (Plate u). The strata below the unconformity are entirely of Missis- sippian age and range from Kinderhookian Goldwater Shale to the Bayport Limestone of Meramecian age. The Bayport is the most extensive paleosurface directly underlying the Pennsyl- vanian strata. It is of quite variable thickness and is found underlying most of the central portion of the Lower Pen— insula of Michigan. The Michigan Formation underlies the Pennsylvanian throughout much of the structurally higher peripheral areas and occurs in the interior as inliers most likely due to ero- sional activity. Shideler (1965), did paleoslope studies and indicated that Michigan was essentially a topographic basin at the beginning of Pennsylvanian time with stream deposits being dominant over other types of sedimentation. He also speculated that a centripetal drainage system may have existed immediately prior to Bayport time. He based this on the crenulate pattern of the contact between the two formations as an indication of extensive stream dissection. The Michigan Formation exhibits evidence of stream dis- section in at least four areas. The most prominent one can be seen extending towards the center of the basin, northwest and west off the Howell Anticline and the surrounding high peripheral areas. Bayport sediments have also been eroded away by a similar process in Baton County. This river ran to the northeast and Michigan sediments are exposed as far as 21 Clinton County. Michigan strata can also be found along the periphery of Arenac County. This channel ran to the south- east towards the interior of the basin. A fourth channel can be seen in Missaukee County. This channel flowed in a south- erly direction towards the basin interior. Marshall Sandstone subcrOps below the Michigan Strata are limited in extent and are generally found scattered along the periphery of the basin. Most of them are located along the northwest flank of the Howell Anticline in Shiawassee County and are attributed to the greater uplift and subse- quent erosional activity of this area. Smaller subcrops are found in Bay, Eaton, Genessee, Livingston, and Tuscola Coun— ties, and are also due to erosional activity. The most pronounced erosional effects are exhibited along the axis of the Howell Anticline which trends northwest through Livingston and Shiawassee Counties. In this area, pre-Pennsylvanian deformation and subsequent erosion have resulted in Coldwater Shale being exposed along the crest of the structure. The Coldwater is restricted to Livingston and Shiawassee Counties and represents the oldest formational unit directly underlying the Pennsylvanian strata. There is no apparent relationship in the Michigan Basin between the structures at the base of the Bayport and the unconformity between the Mississippian and Pennsylvanian Systems (Plate 5). This is due to the nature of the two sur— faces as the base of the Bayport reflects the topography of the underlying Michigan Formation. Pennsylvanian Pennsylvanian strata underlie an area of approximately 11,200 square miles in the Michigan Basin and are confined to the central portion of the Lower Peninsula (Figure 6). The roughly elliptical distribution pattern extends from cen- tral Missaukee and Boscommon Counties in the north to Jackson County in the south. The eastern limit is in Tuscola County while the western boundary is found in Newaygo and Lake Coun- ties. The Pennsylvanian System of Michigan is divided into two major formations, the Saginaw below and the Grand River (Kelly, 1936). These have been divided into a number of in— formal subunits. The basal sandstones of the Saginaw Forma— tion have been referred to as the Parma sandstone while the Grand River Formation includes the Woodville, Eaton, and lonia sandstone members. The Parma is a clean, white, quart— tzose sandstone that has some localized conglomeratic, dark shale lenses. It varies in thickness and has its maximum thickness in Shiawassee County where it is 220 feet locally (Shideler, 1965). The Saginaw Formation was originally called the "Coal Measures" (Winchell, 1861). This was in reference to the coal bearing strata located between the Parma and Woodville sandstones. It later was expanded (Lane, 1909) to include the other lithologic units of the formation. Presently, the Sag- inaw is described as a heterogeneous association of terres- trial and marine strata thatconsistscfi'interbedded sandstones, 22 23 o / /I/ K ifiu‘lx ‘R _I v,» . /“ $2.3. l 6* l‘I ” 56.....(15 "SI , F I \z ...:v ANIAN I! I '\ 0' “'1’" (7 / I . 1 \./A§‘¢_ I 0 fl \ :6 l 1 F / V JMICHIGAN W11 1J4... fi\2v -—____ PPIAN FIGURE-6 DISTRIBUTION OF MISSISSI , PENNSYLANIAN, AND IURASSIC STRATA IN THE MICHIGAN BASIN. 2M shale, coal, and carbonate units. The sandstone is usually argillaceous and fine—grained. The shale is abundantly fos- siliferous and ranges from a dark fissile marine shale to a light colored underclay (Schideler, 1965). The coals are quite thin, limited in areal extent, and of little economic value. The main workable seams are usually two to four feet thick and consist of blocky bituminous grade coal (Kalliokoski and Welch, 1976). The carbonate units are thin, very argil- laceous, and commonly fossiliferous (Shideler, 1965). Located above the Saginaw Formation and resting uncon- formably on it is the Grand River Group. This includes all the post-Saginaw formations of Pennsylvanian age and repre— sents the youngest Pennsylvanian strata within the Michigan Basin. It has been divided into three members (Kelly, 1936), the Woodville, Ionia, and Eaton. It has a distinctive brown— ish-red color and the basal portions may be conglomeratic. Shideler (1965) separated the Pennsylvanian of the Mich- igan Basin into three time-stratigraphic units (Figure 7). The oldest is Morrowan in age and includes all the strata from the Mississippian-Pennsylvanian unconformity up through the shale that usually overlies the Saginaw coal. The next unit is Atokan in age and includes all the strata found be- tween the shale overlying the Saginaw coal and the Verne Limestone member. The youngest Pennsylvanian sediments are Desmoinesian in age and are made up of all the strata from the base of the Verne member up to the base of the Jurassic "Red Beds" or, where the Jurassic is absent, to the Pleistocene 25 SHIDELER KELLY SER'ES FORMATION MEMBER DESMOINES IONIA s. GRAND RIVER EATON S: VERNE LI THIN COAL UNITS ATQKAN MORROWA N SAGINAW WOODVILLE 5: COM. UN ITS PARMA S: FIGURE-7 TIIE PENNSYLVANIAN SYSTEM IN MICHIGAN. 26 drift. The actual age of the youngest interval is difficult to determine due to the sparse fossil content and the uncon- formable relationship of the assemblage. The Pennsylvanian strata of the Michigan Basin have been subjected to extensive post-Pennsylvanian erosion and are is- olated from the Pennsylvaian strata of adjoining basins. Kelly (1936) postulated that there was a seaway connection between the Michigan and Illinois Basins. This was based on similarities between the marine faunal assemblages of the two areas. The thickness variations of Pennsylvanian strata are il— lustrated in an isopach map (Plate 6). The map indicates a progressive thickening from the peripheral areas of the basin towards the interior. Its steepest gradients are located along the western flank of the Howell Anticline and in the northeast in Arenac County. The apparent depocenter (Figure 5) is located in southeastern Clare, southwestern Gladwin, northwestern Midland, and northeastern Isabella Counties. The maximum reported thickness is 721 feet which is found in Gladwin County. There are several areas of thick sediment accumulation which can be attributed to post-deposi— tional erosion, differential compaction, and to the pre-Penn- sylvanian topography. Jurassic The Pennsylvanian System of the Michigan Basin is nor- mally overlain by thick deposits of Pleistocene drift. However, in some localities the material directly overlying the Pennsylvanian is a series of red impure sandstones and shales with interbedded gypsum, which have been identified as the Jurassic "Red Beds". The Jurassic "Red Beds" are restricted to the subsurface of the central Michigan Basin (Figure 6) and volumetrically represent less than one percent of the sedimentary'accumulation in Michigan. The evidence of their distribution, lithology, stratigraphic position and thickness was unavailable until the advent of deeper exploratory drilling towards the center of the basin. The "Bed Beds" were seldom mentioned prior to 1931. Some of the early accounts were by Lane (1909) and Smith (1917). They tended to include the "Red Beds" in a sequence of sandstones in the Grand River Group of Pennsylva- nian age. Newcombe (1931) introduced the term into the Michigan stratigraphic nomenclature and Martin (1936) claimed that they were Permo-Carboniferous in age. Cross (1966) is credited with correctly placing them in the Jurassic. He based this on the distinctive mid-mesozoic, pre-Angiosperm pollen and spore flora. The Jurassic of the Michigan Basin has an irregular oval distributional pattern and has an areal extent of ap- proximately 5,500 square miles (Shaffer, 1969). The "Red Beds" are confined to the central portion of the Lower Pen- insula and are present over most or all of Clare, Osceola, Mecosta, Isabella, Gratiot, and Montcalm Counties. Periph- eral deposits and scattered erosional remants can be found 28 in sections of Ogemaw, Roscommon, Missaukee, Wexford, Lake, Newaygo, Kent, Ionia, Clinton, Saginaw, Midland, Gladwin, and 0ceana.Counties. The "Red Beds" lie unconformably below the Pleistocene glacial drift and unconformably above the under- lying strata. These underlying strata are mostly Pennsylva- nian in age, however, some periperal Jurassic beds to the west, directly overlie Mississippian rocks. The bulk of the "Red Beds" lies somewhat west of the center of the present Michigan Basin configuration and the apparent depocenter (Figure 5) is located in southeastern Mecosta and north central Montcalm Counties. The Jurassic sediments are dominantly a reddish-brown shale with some sand— stone and siltstone lenses. Fairly pure gypsum may also occur as a bedded evaporite and be up to eighty feet thick (Sander, 1959)- Color has been the chief criterion used in differentia— ting the Jurassic strata from the underlying beds. Most of the Pennsylvanian and Mississippian strata that are directly below the Jurassic are gray to black siltstones and sand- stones. Besides this, the sandstones of the Grand River Group are usually micaceous and slightly feldspathic while those of the Jurassic are not (Shaffer, 1969). The maximum thickness of the Jurassic, slightly over 350 feet, is found in Mecosta County. The thickness does vary considerably (Plate 7) within the area of distribution. This is due to the modification by irregularities of the pre-Jur- assic topography and by post-"Red Bed" erosion modified by 29 Pleistocene glacial scouring. The thickest Jurassic areas are situated slightly west of the present depositional center, and because of this, an asymmetrical aspect is imparted to the Jurassic basin. This may be reflective of greater abra- sion on the eastern side of the basin, especially by the Saginaw glacial lobe, an originally asymmetrical basin which received Jurassic sediments, or a greater amount of sediment deposition in this area (Shaffer, 1969). The present distri- bution and thickness of the Jurassic conforms to, and was most likely strOngly influenced by the configuration of the Michigan Basin and the pre—exisitng topography. However, in a general sense, the Jurassic slopes basinward at a somewhat more gentle angle on the eastern flanks of the basin than on the west. This may be attributed to the underlying topography. It is possible that the Jurassic "Red Beds" of the Mich- igan Basin are not basin related. Recent drillings in Ontario have uncovered "Red Beds" with a Jurassic flora. This has enabled Cross (1978) to postulate that the "Red Beds" of the fiichigan Basin were derived from the Canadian Shield and trans- ported into the Michigan Basin area. The Jurassic sediments taper to the southwest and were deposited in the Michigan Basin as a thin cover on the Pennsylvanian topography (Cross, 1978). The sediment cover was apparently always fairly thin as the pollen and spores of this flora have undergone very little catagenic metamorphism (Cross, 1978). Following the Jurassic and preceding the Pleistocene epochtflmnwewas a long time interval represented only by 3O erosion in the Michigan Basin. Thereis no evidence for de- position of strata during this interval which indicates either erosion and/or non-deposition is occurring. Evidence for a dissected erosional surface can be found in the surface pro- file of the underlying bedrock. That surface is marked by drainage systems whose main channels appear to have followed the axial trends of Lakes Erie, Huron, and Michigan (Travis, 1966). Pleistocene The Michigan Basin was subjected to repeated glaciation during the Pleistocene. The Nebraskan, Kansan, and Illinoian glacial intervals preceeded the Wisconsin and may have affect- ed much of the area. The Wisconsin had four major glacial advances and retreats which apparently removed all recogniz- able remnants of previously deposited unconsolidated material, as well as some of the underlying bedrock. Three principle ice lobes, the Lake Michigan, Lake Erie, and Saginaw affected the Lower Peninsula of Michigan. The Pleistocene drift un- conformably overlies Jurassic and Pennsylvanian strata in the study area. The thickness varies and is illustrated by an isopach map (Plate 8). It shows the thin cover of the Sagi- naw lobe which extends southwest from the Saginaw Bay area. A progressive thickening occurs to the northwest and the thickest accumulation of drift, nearly 1,100 feet, is found in northeastern Osceola County. Generalized Cross-Sections The litholgic cross—sections are constructed with sea level as a datum plane. They are intendedto illustrate the gross lithologic variability and the structural attitudes of all the strata found above the Mississippian Michigan Formation in the Michigan Basin. Cross section A—A' (Figure 8) is based on seven points and it extends across the center of the basin in a southeast direction from southwest Wexford County to eastern Livingston County. It illustrates the general variabilities of the lithologies of the study and their relation to the basin. In particular, it shows that strata have a steeper dip in the southeastern section of the basin than in the northwest. It also indicates that the beds have been restricted in extend due to erosional effects caused by the uplift of the Howell Anticline and that the Jurassic sediments have imparted an asymmetrical appearance to the basin. Cross section B-B' (Figure 9) is based on six wells and trends across the Michigan Basin in a southwest direction from northwestern Arenac County to southeastern Kent County. 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m .omw mwma mmoa mm0a 0N2 amw amo mama :mmmm m .omm :mma amm 0mm 002 mam mam moaa mammm a .omm 32mI20mB amma 2mm 0mm OH2 I Oa2 mmaa mm20m mm .omm 0mma 0:0 :00 mm2 I mm2 2maa mmmmm am .owm amma :00a mmm :m2 I :m2 mwaa oqmwm 0m .owm 0mma 000 M00 000 I 000 2maa :ma0m mm .owm m0ma mmm mmm 000 I 000 omaa 2m20m 0m .omm <2 :20 OMO mmO 0mm Omm OmaH mmm2m ma .omw mama :00a mmm aww 00: 00: mwaa mmwmm ma .owm mHmH mmm O20 O2 I O2O 2aaa mzomm 2H .omm mmma N20 0mm mw2 I mw2 mmaa mmoam m .omm moma ma0a 000 mam I mam amaa ©022m m .omm 30amIZmaE mwma 020 0mm mom I M00 mmaa mazam mm .omm 022a mom 2mm 0m2 I 0N2 2aaa 0200m 0m .omm 002a am0a 00a a02 I a02 mmma aammm mm .omw 30amI20aB a02a :mma 2aaa m:@ I mam m0ma moamm 2a .omm 3wmI20mB <2 :mma 0mma mz2 00m 00m mwaa wwwmm 0m .omw mama :20a :00a m02 amm amm 2aaa 2002m am .omm wmza mmaa ma0a 0N2 mam mam :zoa ©002m 0a .omm p2 p22 pmz um um 00 >mqm 22 COapmooq 63 ma2 mom 0H: m2 I m2 20m 0m:mm mm .owm MmmIZHHB a0m mmm 0mm maa I maa 0N0 m020m a .omm MmmlzaaB a22 22: mmm 00a I 00a 00m 02mmm m .omm m0mI2maB 3<2H0mqm 20 Coapwooq 6H 2::a :moa 020 002 I 002 MNMH 2m0mm Om .omw <2 m:aa m0aa amw I aww w0ma 0m00m 2m .omm mama 2:0a :20 0:2 I 0:2 w:ma :0m2m mm .omm 20ma 200 ::0 N00 I N00 woma m2®am 2 .omw 20mI2amB <2 m00 I 020 I 020 wmma 0m0mm mm .omm <2 M00 I 002 I 002 w0ma mommm :a .owm 30amI2amB amomxmz mmm 0mm I mma I mma a0m 0002a mm .omm M2mI2:aE m:m m0a I I I m0a ::0 :oawm :a .omw 2am mom I I I mom mmw ammmm ma .owm M0mI20aB 0aa m: I I I m: 2N2 000mm 0a .omm cm I I I I om mm2 000mm 0 .omm mHamIZmaB 000 0mm mam m2a I m2a m®2 00:0m mm .omm a0m a0a I 0:a I 0:a a22 2mm0m am .omm MmmI20aB 02m mma mma I I mma 0m2 0m00m mm .omm M0amI2:aB a2a m0 I I I m0 :m0 mw:mm ma .omm M0mI2:aB 0am mmm m0a 00a I 00a 000 000mm 0 .omm m0mI2maB mmm 02 I m: I m: ma0 2mm0m mm .omw mmmlz:aB <400m28 20m 00 I I I 00 m:w 02mmm m .omm mmmIZmB I I I I I 0aa a2w m2mmm ma .oww MmmIZmB mmmm<3mqm 22 coapmooq 65 2:ma N00 I I I N00 aa:a :a:mm 0 .omw 30amI2mmB 2mma mmm I I I mmm 0mma 0000m mm .oww 3aamI2amB m:ma 0m0 am0 wm2 I wm2 m0ma 000mm mm .omm 30mI2mmB 02 p22 pm2 pm 90 20 >242 22 COaQMOOA BIBLIOGRAPHY BIBLIOGRAPHY Bacon, D.J., 1971, Chert Genesis in a Mississippian Sabkha Environment, Unpubl. 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