STRUCTURE AND STRATEGRAPHY OF THE TRAVERSE GROUP IN THE LANSING AREA... MICHIGAN T'I'Iesls Ior III. Degree aI M. S. MICHIGAN STATE UNIVERSITY Lewis Allan Gust‘afson 1960 I I! um; lawn In I I I II III "II II , LIBRARY ' Michigan Stats . University STRUCTURE AND STRATIGRAPHY OF THE TRAVERSE GROUP IN THE LANSING AREA, MICHIGAN by Lewis Allan Gustafson AN ABSTRACT Submitted to the College of Science and Arts of Michigan State University in partial fulfillment of the requirements for the degree of MASTER OF SCIENCE Department of Geology 1960 Approved: LEWIS ALLAN GUSTAFSON ABSTRACT The Lansing area includes Ingham County, Eaton County, Clinton County, the east half of Ionia County and the west half of Shiawassee County. This area has seen little drilling activity in the last two decades. Yet, the Traverse group which underlies the Lansing area, at rela— tively shallow depths, has been productive in other parts of the state. The purpose of this investigation was to survey the Traverse group in the Lansing area to determine its petro- leum possibilities, and describe the structural and stratigraphic conditions. Due to the absence of Traverse outcrops in the Lansing area it was necessary to gather information from lithologic logs and well samples of the 163 wells which have reached the Traverse group. The Traverse group underlies most of the Lower Penin— sula of Michigan. It is composed of limestone, calcareous shale, dolomite, and chert. In the Lansing area the Traverse group is at depths ranging from 420 feet to 1840 feet below sea level, with a thickness which varies from 300 feet in the south part to 450 feet in the north part of the area. It dips generally to the north at less than one—half of one degree. Traverse stratigraphy in the Lansing area can be described best by dividing the Traverse group into K10 LEWIS ALLAN GUSTAFSON ABSTRACT lithologic units. From bottom to top these are: basal shale zone, gray—brown limestone, buff limestone, gray- cherty limestone, and "Traverse formation." "Traverse formation" is a term which refers to the transition zone between the Traverse limestone and the Antrim shale above. Three large structures are present in the Traverse rocks of the Lansing area. These are the northwest trending Howell anticline, a high structure trending northeast across Eaton County, and a northwest trending trough across Clinton County. I No structural or stratigraphic traps were discovered by this investigation. However, porous horizons which could serve as reservoir rocks exist within the upper part of the Traverse group. Also, high structures are present in the Lansing area and should closure be found on these structures there is a fair chance that they would contain petroleum. STRUCTURE AND STRATIGRAPHY OF THE TRAVERSE GROUP IN THE LANSING AREA, MICHIGAN by Lewis Allan Gustafson A THESIS Submitted to the College of Science and Arts of Michigan State University in partial fulfillment of the requirements for the degree of MASTER OF SCIENCE Department of Geology 1960 ACKNOWLEDGMENTS The author is grateful to Professors J. H. Fisher, B. T. Sandefur, and W. A. Kelly of the Geology Department, Michigan State University, for their suggestions and help. Friendly assistance in securing well samples came from the Petroleum Division of the Geological Survey of Michigan. Appreciation is due also to Mrs. P. L. Gustafson and Mr. S. w. Gustafson for proof-reading. Special thanks go to my wife, Joanne, for her constant encouragement and typing of the manuscript. CONTENTS Page INTRODUCTION. . . . . . . . . . . . . . 1 General Information 1 Purpose of Investigation 3 Drilling Activity. 3 Rock Exposures. . . . . . . . 4 Conduct of Investigation A REGIONAL STRATIGRAPHY. 5 General . . . 5 Bell Shale 8 Rockport Quarry Limestone 8 Ferron Point Formation 8 Genshaw Formation. 9 Newton Creek Limestone 9 Alpena Limestone 9 Four Mile Dam Formation. 9 Norway Point Formation lO Potter Farm Formation IO Thunder Bay Limestone . . . . . . . . . lO Squaw Bay Limestone . . . . . . . . . . 10 LOCAL STRATIGRAPHY. . . . . . . . . . . . 11 -General . . . . . i. . . . . . . . . ll Dundee—Traverse Unconformity . . . . . . . IA Basal Shale Zone . . . . . . . . . . . 14 iv Page Gray—Brown Limestone. . . . . . . . . . l6 Buff Limestone. . . . . . . . . . . . 17 Gray Cherty Limestone . . . . . . . . . l8 Traverse Formation . . . . . . . . . . l9 Traverse Formation in Eaton County . . . . . 20 REGIONAL STRUCTURE. . . . . . . . . . . . 23 LOCAL STRUCTURE. . . . . . . . . . . . . 25 General . . . . . . . . . . . . . . 25 Howell-Owosso Anticline. . . . . . . . . 26 The Eaton County High Trend . . . . . . . 28 Ingham County Structures . . . . . . . . 28 Clinton County Trough . . . . . . . . . 29 Ionia County . . . . . . . . . . . . 29 GEOLOGIC HISTORY . . . . . . . . . . . . 3O PETROLEUM POSSIBILITIES IN THE LANSING AREA . . . 33 General . . . . . . . . . . . . . . 33 Eaton County High Trend. . . . . . . . . 34 North Extension of the Howell-Owosso Anticline . 35 Clinton County Extension of Howell Anticline. . 36 Northwestern Corner of the Lansing Area . . . 36 Clinton County Trough . . . . . . . . . 37 Stratigraphic Traps . . . . . . . . . . 37 CONCLUSIONS AND RECOMMENDATIONS . . . . . . . 38 EXPLANATION OF PLATES 2, 3, 4, 5, and 6. . . . . 40 Plate 2--Well Log Correlation. . . . . . . 40 Plate 3--Top of the Traverse Limestone. . . . 40 Plate A--Isopach Map of the Traverse Group . . 41 Page Plate 5--Panel Diagram of the Traverse Group. . A2 Plate 6--Base of the Traverse Group. . . . . A2 EXPLANATION OF TABLES. . . . . . . ._ . . . 43 TABLE OF WELL INFORMATION, IONIA COUNTY. . . . . 44 TABLE OF WELL INFORMATION, CLINTON COUNTY . . . . 50 TABLE OF WELL INFORMATION, SHIAWASSEE COUNTY . . . 57 TABLE OF WELL INFORMATION, INGHAM COUNTY . . . . 59 TABLE OF WELL INFORMATION, EATON COUNTY. . . . . 60 BIBLIOGRAPHY. . . . . . . . . . . . . . 62 Figure Plate NmU'IJ—‘LUM ILLUSTRATIONS Index Map of Michigan. Traverse Nomenclature. Typical Well Log of Eaton County; Typical Well Log of Ingham County. Typical Well Log of Ionia County; Typical Well Log of Clinton County Traverse—Antrim Contact Well Location Map, Lansing Area Well Log Correlation Top of the Traverse Limestone Isopach Map of the Traverse Group. Panel Diagram of the Traverse Group Base of the Traverse Group Top of Traverse Group, Michigan Basin In In In In In In In Page 12 13 21 Pocket Pocket Pocket Pocket Pocket Pocket Pocket INTRODUCTION General Information Lansing, Michigan, is located eighty-five miles west— northwest of Detroit in the south central portion of the Lower Peninsula. The Lansing area, as defined in this investigation, includes Ingham County, Eaton County, Clinton County, the east half of Ionia County, and the west half of Shiawassee County (Figure 1). This area is well developed and populated. Lansing with a population of 110,000 people is the largest indus- trial city in the area. Farm lands occupy almost all of the area. The average farm is about 60 acres. Michigan was surveyed into townships, ranges, and sections, with the state retaining the right to place roads on all section lines. Consequently, there are secondary roads, gravel or macadam, on most section lines. A very good highway net covers the area. Average elevation is approximately 800 feet above sea level and ranges from 650 feet to 950 feet. Low gently rolling hills with intervening flat lands dominate the landscape. Maximum relief at any particular location does not exceed 200 feet. The Lansing area was glaciated during the Pleistocene and displays moraines, eskers, and outwash 2 LL ;___‘ a—fi MICHIGAN DEPARTMENT OF CONSERVATION . GEOLOGICAL SURVEY DIVISION Flgure 1. Index map of Michigan showing location of % the Lansing area. K E M L .4 K ER’ 0 R A f 5 UP \ DOMINION OF CANADA I; BARAGA ~__/ g: x? l MARQUETTE ‘ g 6%. ALGER I .\" cmppm c 0 ~\. "w" scuomcnan ”0,9,.” N DICKINSON ‘CK'N‘C c ”4 ”Nu ‘. ‘ LUCE I ' Q meow" I 0. go; to u a 0V) ' ( e mm: 0 mm 7 I . r ’7 EfV. T19 cuzaovcm +6 x1erav Ba } ‘ Y PRESOUE ISLE ffl‘ A51? Evoux 7 J . / 3 .....I ”.4ng 9 ‘ . 4, .' N LEELNW r Q / ° .' V 8mm GRAND KALKASKA caawroao OSCODA ALCONA I I b mucus: I \ C . a mu wtxroao msswmlnoscowou 050w Iosco to .'/ 9 o I \ (mason LAKE OSCEOLA CLARE GLADWIN n z I OCEANA MECOSTA ISABELLA quLAIIo : name I.) “MEL-607 uoumw Gamer *\ KENT / ‘. 0mm Io II c TON ‘ I . __ A “I si . ALLEGAN many I: on m /uLIVNos I m sum MLmAzoo CALHOUN mason wasmzum " BERRIEN “55 5‘ ./ JOSEPH J W- '_"—'ITI"I5- I A N A I I plains. Drainage is fair, although there are some small swamps located throughout the area. Soil trafficability is usually good. Rainfall in Michigan averages about 30 inches per year. The climate is moderate for Michigan's latitude due to the proximity of the Great Lakes. Yearly temperature averages about 45 degrees. Trees are confined to woodlots, along rivers,and on unmanageable soil. Purpose of Investigation The purpose of this investigation is to survey the Traverse group in the Lansing area with the intent of examining the structure and stratigraphy, and defining any possible structure which may have accumulated petroleum. Drilling Activity Drilling activity started in this area before the turn of the century and progressed very slowly until the oil boom of the 1930's. At that time the area received a great increase in drilling which subsequently declined to what it is today, practically nothing. Approximately 163 wells have reached or penetrated the Traverse group in the Lansing area up to the time of this investigation (Plate 1). Some production has been gained from the Traverse within this area. Most of the wells in the Lansing area were drilled by the cable tool method. Rock Exposures Rock exposures are practically non—existant and Traverse rocks are not exposed within the Lansing area. The Traverse group is exposed in three outcrop areas and several quarries in the northern Lower Peninsula. Outcrop areas are in the Alpena, Grand Traverse Bay, and Little Traverse Bay regions (Figure 1). Conduct of Investigation Due to the absence of exposures in the Lansing area this investigation was conducted entirely from subsurface records and samples. Sample logs of 163 wells which pene- trated or reached any part of the Traverse were examined and correlated on the basis of lithologic similarity, con- tinuity, and stratigraphic position. In addition, samples from 30 wells were examined megascopicly and samples from 6 wells were examined with the binocular microscope. Correlation proved difficult between many wells due to poor sampling, recording, and extreme variation in the Traverse rocks over short dis- tances. The maps accompanying this study were drawn with a contour interval of 25 feet. This allowed for inaccuracies arising from depth measurements, correlation, poor sampling, and poor recording. REGIONAL STRATIGRAPHY General The distinction between Traverse rocks and other Michigan strata was recognized as early as 1841. C. C. Douglass (Geological Reports of Douglass Houghton, 1928, p. 579) named these beds, in their northwestern occurrences, "Little Traverse Bay limestones." Winchell (1871, p. 28) renamed them "Little Traverse group." Still later the name was simplified by Dr. Lane (1895, p. 24) to "Traverse group." The latter nomenclature remains today. The name Traverse group is assigned to a series of limestones, shales, and shaly limestones, with dolomite, dolomitic limestone, and chert, of secondary importance. The texture of the limestone varies from lithographic to coarse crystalline to fragmental. Traverse rocks are exposed on the western shoreline of the northern Lower Peninsula in the Grand Traverse Bay and the Little Traverse Bay region (Figure 1). They are also exposed on the eastern side of the northern Lower Peninsula, in the Alpena and Thunder Bay region (Figure 1). In addition to these natural outcrops the Traverse group has been exposed by quarry operations in the same general area . "Saucer shaped" is a term which has been used to des- cribe rock units in the Michigan basin. This description also applies to the general aspect of the Traverse group. The rim of the Traverse saucer forms a circle of bedrock within the basin. This rim passes through the Michigan outcrop area, southwestern Ontario, northwestern Ohio, northern Indiana, Lake Michigan, and eastern Wisconsin. In the southeast, the Traverse group is mainly shale and relatively thin, 60 feet in Ontario, and 50 feet in Ohio (Pohl, 1929, pp. 30-31). In the northwest, it is mainly limestone, 500 to 800 feet thick. Pohl (1929, p. 33) has placed the Traverse group of Ontario between the Onondaga and the Hamilton. Actually, post-Onondaga pre-Moscow, with Ludlowville and Skaneateles times represented by an unconformity. This unconformity is directly above the Thunder Bay formation (Figure 2). Warthin and Cooper (1943, pp. 578-595) believe the forma- tions of the Traverse group below the Norway Point to be equivalent to Hamilton strata in New York, and those above to be in the upper Devonian (Figure 2). Numerous workers have described and divided the Traverse group of Michigan. Three generally accepted divisions are shown in Figure 2. Shown also is the strictly lithologic subsurface division of Traverse rocks in the Central Michigan area by Hake and Maebius (1938, pp. 451- 457). The units and descriptions below in ascending order, opSpmHocmEoz mmpo>mnB .w opswfim em mmocso em huflo mpowom mfiwnm Hamm mamnm HHmm mmamcm Hamm mg unoaxoom mg agenda upoaxoom mg oxmg omens pas: oCOpmoEfiA Em psaom connom momm oxmq wcoq Ucw mamzm mHUUaz hmDEmE CGHHHHM Em segmcmw .nom mHmH ozdmonm mwmpm pcfiom Hm>mnc mu smote couzoz adonu mg mcoaa< moahom mcoaaq mmno>mne was: mCOpmoEHA owmpm m>Hmmmz manna: Em Ema mHHz 930m xHo>oHLo£o Em pcfiom hasnoz em momepom weapom mom pmocsne II. I. I I Hm anew AMupdm I I I I I I I I I I I. I I I .I I flea 32m Beep 3- 1.1mm. timescale mu ham zmsvm mg Nam Sodom I Em EHLpC< mmma mama mama mmmfi mzfinomz one exam poaooo new Canned: :mpmpu acom coawmm coawmm coawmm coawom cmwfigoaz HmNpcmo mamaad mcoafid ham omnm>mpe HTGGIW Hflddfl from the Alpena type locality, are mainly those of Warthin and Cooper (1943, pp. 578-595). Bell Shale The Bell shale is the lowest unit of the Traverse group. It is separated from the Rogers City and Dundee formations below by an unconformity (Newcombe, 1930). The Bell has a thickness of 60 to 80 feet in the northern Lower Peninsula, over 200 feet in the central Michigan area, and thins ‘MD the south and west (Newcombe, 1933, p. 45). It is absent in the extreme southwestern counties. The Bell is a blue-gray calcareous shale. When it forms a thick deposit the Bell becomes dark and non- calareous at its base. It is correlated with the middle of the Skaneateles formation. Rockport Quarry Limestone This unit is represented, in its type locality, by 50 feet of gray and brown limestone. The Rockport Quarry becomes limy shale in central Michigan and dolomitic gray limestone in northwestern Michigan (Hake and Maebius, 1938, p. 452). Ferron Point Formation Gray calcareous shale and argillaceous limestone occupy the position above the Rockport Quarry. The Ferron Point totals 37 feet in exposure. Possibly, the Silica shale of Ohio corresponds to this formation. Genshaw Formation The Genshaw is gray shale and argillaceous limestone totaling 116 feet. At its top it contains the Killian member which is a 23 foot layer of black to dark gray lime- stone with thin black shale partings. Equivalence of the Ferron Point and Genshaw formations to the "middle shale and limestone unit" of Hake and Maebius is suggested (Hake and Maebius, 1938, p. 452). To the west the Ferron Point and Genshaw formations become massive lime- stone and dolomite (Hake and Maebius, 1938, p. 453). Newton Creek Limestone This limestone is dark brown, crystalline, and has a thickness in its type locality of 25 feet. It was distin- guished from the limestone above and below on faunal evidence alone. Alpena Limestone The Alpena is 79 feet thick in the type locality. It is a pure limestone, usually white, light brown, or light gray, and contains bioherms and biostromes. Porosity is greater in this limestone than the other units. This fact is due to the fossil material and lime sands associated with the organic structures. Four Mile Dam Formation This is a variable bed of brownish gray limestone or shale from 8 to 14 feet thick. It is believed to correspond to the Centerfield of New York. 10 Norway Point Formation The Norway Point is the youngest Michigan formation with "definite Hamilton affinities" (Warthin and Cooper, 1943, p. 589). It is represented by 45 feet of bluish gray shale and gray limestone. Potter Farm Formation The Potter Farm Formation is 68 to 74 feet of gray or brown limestone with some thin shale layers, in the type locality. Thunder Bay Limestone The Thunder Bay is 13 feet of gray shale and lime- stone. This formation and the Potter Farm are probably equivalent to the Petoskey (Pohl, 1929, p. 5 ) of western Michigan. Squaw Bay This is considered the upper-most bed of the Traverse group. It is probably equivalent to the Genundewa lime- stone of New York. The Squaw Bay is traceable over much of Michigan and in the type locality shows 8 feet of brown crystalline limestone or dolomitic limestone. Above the Squaw Bay is a transition zone of gray cal- careous shale. This zone varies greatly over small distances. The relationship between this shale and the overlying beds is not well understood. Kirkham (1932, pp. 136—137) has suggested the possibility of an unconformity at the top of the Traverse. LOCAL STRATIGRAPHY General The Traverse group in the Lansing area is composed of limestone, shale, chert, and dolomite (Figures 3, 4, and Plate 2). Minor amounts of pyrite and gypsum also have been encountered. In general, the Traverse dips to the north at a rate of less than one-half of one degree and thins to the south by about 150 feet (Plates 2, 3, 4, and 5). Total accumulation of Traverse sediments in the extreme north of the area are in the order of 450 feet and in the south, 300 feet. This thinning seems to be distributed among the various lithologic units which are described below, with the exception of the "Traverse formation." "Traverse form— ation" is a term which does not necessarily follow the scheme of geologic nomenclature, but has been usefully applied to the transition zone between the Traverse lime- stone and the overlying Antrim shale (Plate 2). Division of the Traverse group into units can be accomplished by examination of samples and well logs. How- ever, the boundaries between some units are indistinct due to the type of information used. Necessarily, these divisions are apparent as observed in samples and not absolute, as would be observed in outcrops. No attempt has been made in this investigation to correlate the individual 12 Figure 3. l in. = 40 feet. A. Scale: Chert: ocoumoEfiq =co«uth0h huh0£c ocovmoEwA mmzm ocoumcfiwq omho>mhbz swam czohnlhmhc w .1 o f h n n nu r h s .n r r “.b g s f s b r. b b n l n +. nri r. n n g k r lir r. r a rur r. u rrr r rr .0 b huo g g by w hub 8 ab .0 b gas .0 cog ~ \ ocom madam Honda fossilif fossilif brn gr gr gr gr . :J .mpczoo Emzmch no spaces Haws amendse wade ozoumofiad :coflusEhom omho>mub: gr,bl gr,b1 sh 1 r b .6 ......“.?_.._“J hvuong hwhw ocovmofiud mmzm buff brn buff gr cht gr.brn -gas show .aucsoo cousm mo whoooz HHQB Hoowmhb nn~* 4'. 4:. ocoumoEHA czohDI%MHU O OHmOEa Nu :COAWMEAOM hvhmno ocovmoEwA mmsm ocoumoEfiA :30hnlkdh0 mCON oaafim Hammm emu >ahH: knew w o f h .. t r t .t f s as h g h .n u c f c ,1 f c b f n +e n n:. f r. a n f n n r.r nah r rnuh u Uh“ r r u r r r,r r b8 wwb bbw b bw g b b 8b 8b 3 hucsoo coucflao mo Uhooom HHOE HNOHQME ooa% oceanoEaA :coHuthom xenon, omuw>wh8= hmhw ocoumoEaA muse ocoumoEaA czounIhaho QCON mamsm Hommm w n f f n f f . m ..._ A M m . m . r r .m n .m t n 1 w 9h r {i 9 b 9 g 9 g 5 no .0 u b r be S f a. f f 9 9 b 9 g 1 n f . .t 5 Pi n n .1 n f. n t n n n .. n n r 11r.urrha 0 u r r u r r u r a r r rr r r r r rrk 3 bob bggww f b b b b b g b b w 8 8 bob b b g b bgd . p \ _..._n__."..ru_.. zucsoo sH:OH mo Uncoom Haoa Haoammh om* .uoom o: u 50:“ H “mamom .3 ouzwflm 1L. lithologic units of the Traverse group in the Lansing area to the described units in the outcrop area since it was not deemed critical to the study. Dundee-Traverse Unconformity The stratigraphy of the Traverse group begins with what appears to be an unconformity (Newcombe, 1930). This unconformity is between the base of the Traverse group and the underlying Dundee and Rogers City (Plate 6). How far it extends into the Lansing area is not known. However, it probably is present throughout the entire area. No direct evidence has been discovered to prove the existence of this unconformity in the Lansing area. However, some facts tend to point toward this assumption. Primary among these is the fact that the water horizons of the Dundee are not always at the same interval below the basal Traverse shale zone. Some water horizons are at times missing completely (Newcombe, 1933, p. 195). Indicative also is the fact that different lithology is sometimes en- countered directly below the basal shale zone. There seems to be no transition zone or interfingering between the Traverse and Dundee. These conditions would not be likely to occur in a conformable series of strata. The time span represented by this unconformity has not been determined. Basal Shale Zone Cohee (1947) believes that the Bell shale is absent southwest of a northwest—southeast line across Clinton 15 County. However, there is a calcareous shale which goes further south and is found in several layers, but always in the lower part of the Traverse (Plate 5). Therefore, the name basal Traverse shale zone would perhaps be more appro- priate than the name Bell shale. The basal shale is light gray, dark gray, or bluish gray. It has fissile structure although not too well devel— oped. The rock is calcareous and may contain fossils and pyrite. One of the distinctive characteristics of this shale is its tendency to change to a mud while being drilled and a light gray powder when dry. Because of this it is sometimes washed out of-—or lost in——the sample collection. The basal shale is a complicated deposit. In general, it thins from over 100 feet in the northeast to nothing in the southwest. Specifically, it changes in thickness a substantial amount between closely spaced wells. For example, well #145 has gone through an accumulation of 79 feet of shale. Well #146, located one and a half miles east of #145, has penetrated only 23 feet; well #144, a little over two miles north of #146, has penetrated 13 feet of shale. The thinning between these wells is contrary to the direction of regional thinning. The basal shale zone usually comprises three layers, or less, of shale separated by limestone or shaly limestone. In the northeast part of the Lansing area the shale occurs in one or two relatively thick layers. In Ingham County it usually is in two layers, each in the order of 15 feet thick, l6 separated by about 50 feet of limestone. Of the 5 wells in Eaton County which have reached the lower Traverse, well #156 found a 16 foot layer of shale while the others found only traces of shale. In Ionia County the shale zone seems to be one or two layers close together totaling 30 feet, but variations can be found anywhere. Clinton County wells show two or three layers in the southern part, but again variations are common. Many factors combine to make the shale deposit in the basal shale zone difficult to interpret. Already mentioned is the fact that the shale can be lost during sample col- lection. The unconformity below may have left an undulating surface on the Dundee limestone; the associated low areas may have been filled with a greater thickness of shale than the surrounding high areas. No correlation has been observed between the thickness of the Dundee and the thickness of the shale accumulation. Further complicating the deposit is the probability that the shale laterally changes to limestone in the Lansing area. This may have created inter-tonguing and unequal distribution. In addition to these factors there is the possibility that variation of currents and source areas affected the deposition of shale in the Lansing area . Gray-brown Limestone Directly above the basal shale zone and interlayered with it, is an argillaceous limestone. Its color varies 17 from gray to brown, but it is usually gray-brown. This limestone may contain chert, fossils, and thin layers of shale. It also varies from fine and coarse crystalline to fragmental. Quartz grains have been reported throughout this part of the Traverse section in Ionia County. The gray—brown limestone tends to be gray and argill— aceous in the eastern half of the Lansing area, but brown and not as argillaceous in the western half. Because this corresponds to the thinning of the basal shale, it is inter- preted as representing the lateral variation or facies change from shale east of the Lansing area to pure carbon— ates west of this area. The gray-brown limestone is the largest single unit in the Traverse section. In the extreme south of the Lansing area it is about 100 feet thick, in the northwest, about 200 feet, and in the northeast, 150 feet. Buff Limestone Above the gray-brown limestone, and separated from it in certain places by a thin shale layer, is the relatively pure buff limestone. This horizon, on the average, is about 80 feet thick and easily recognized in the south half of the Lansing area. It is also recognized in some wells of the north half, but in others becomes gray and difficult to distinguish from the limestone above and below. The buff limestone is not composed entirely of buff colored limestone, but is a combination of white, buff, tan, light brown, and l8 gray limestone layers. There appears to be a gray-brown zone in the center of the buff. This gray-brown zone becomes better developed in northern Clinton County and splits the buff lime into two parts. The buff limestone horizon may contain dolomite, weathered or fresh chert, fossils, coralline material, quartz grains, fragmental limestone, and fine or coarse crystalline limestone. The most persistant salt water horizon of the Traverse group is found at the top or near the top of the buff limestone. Porosity causing this is probably of the vuggy type, which is readily observed in the samples. Gray Cherty Limestone Above the buff limestone is a section of gray or gray- brown limestone. This unit is of varying thickness but usually amounts to 50 feet. Like the other units described it is really a series of thin limestone layers of varying color and crystalline characteristics. It may in places carry dolomite, pyrite, and traces of shale. By far, the most distinctive characteristic of the gray limestone is its consistency in carrying large amounts of chert. Although chert is common in the other units, this horizon usually contains a larger proportion and is the first encountered in the Traverse with substantial amounts. An unusual but interesting example is well #32 (Plate 2), which penetrated 31 feet of mainly gray and light brown chert. Infrequently, sale water is found in this section of the Traverse. 19 Traverse Formation Above the gray cherty limestone and interlayered with it is gray calareous shale. This shale has many of the same lithologic characteristics as the basal shale. Lime- stone, dolomite, or dolomitic limestone are interlayered with this deposit and the shale may give way almost entirely to limestone in certain localities. This calareous shale, and associated limestone and dolomite, continues upward and appears to be interlayered with the black non-calcareous Antrim shale above. The Traverse formation is the most complicated section of the Traverse group. It should be divided into three separate parts, as it usually is seen in the samples. Directly above the gray cherty limestone is gray shale. Above this gray shale is a persistant bed of brown, tan, buff, or brown-gray limestone, dolomite, or dolomitic lime- stone. This bed frequently contains salt water and is some— times called the Squaw Bay in well logs. Between this carbonate and the overlying Antrim shale is another zone of gray calcareous shale. These three divisions comprise the Traverse formation. Limestone, dolomite, or black shale layers may be found among the three divisions complicating the above simplifi- cation. Any division may disappear or become too thin to be noticed.~ The Traverse formation varies greatly in thickness from well to well, but is usually between 10 and 20 100 feet thick. It is doubtful if any one division by itself would be over 50 feet thick. No evidence has been discovered to support the thought of an unconformity in this part of the Traverse section. Traverse Formation in Eaton County In Eaton County the Traverse formation takes on a dif- ferent aspect than that already mentioned. Here the thick- ness of sediments between the Traverse limestone and definite Antrim shale is usually 100 feet. Normal upward sequence of beds in the Traverse formation as previously mentioned was gray calcareous shale, dolomitic brown, or gray-brown limestone (usually correlated with the Squaw Bay), gray calcareous shale, and then typical black Antrim shale. In contrast, the wells in Eaton County show, for the same interval, approximately 20 feet of black and dark gray shale, 40 feet of gray—brown shaly limestone, 30 feet of black shale, 10 feet of gray dolomitic shale, and then typical Antrim shale. The simplest explanation for this apparent change in the Traverse formation would be that the normal gray cal- careous shales have become black or dark in Eaton County and the "Squaw Bay" limestone has become thick and shaly. However, careful examination of well logs of the Lansing and surrounding area indicates differently. Proceeding west and southwest of Eaton County the 40 foot section of gray- brown shaly limestone becomes less shaly. Proceeding east 21 .903200 8...”pr I cabbage .m mhswam I. .ocopmosfia whom I esp mo sewage: poem: QI—Ih-Ip-JI—I .mH omno>mp9 mo doe I QI-IQI—II—I --— mocmpmoeem seeped on. ~~ I II) IIIII mmm .Lm xomam w \ x \ l I l 9:» I]. L9 II / :g: II 1|}! H j I r.I 9». I (\ $0 e... . .9 .1.) A .. \ -I....I I I I T. LHHW m%M&W\IMHW ILHH \\\I IHI I_I I \re& ea. IIIII IIrII \ I M I. I 1 w (Ox/mow .IHIHI IMMT \ \ IHI .oocmAmmeem I _I I_ [HIM-II A IMIW IMW mwhwbwhhl mmm I —II I IIIIII . III / III II N \ I I I I l I / W .mH macaw cameo WI M u... I... / " I'll. lllll Ill-Ill ['1 III lIl Ill ll ['1 .em Etna 8.238 I I 'I 'I J 'I 'I l I II I I I I I II I I l ‘ ' IIIII\ \ IHIII. IIIIJ \ I I l .EHhPCd. 9.3 IHI WWI.“ \ IMI //I...IIIIH..HI \ \ IILI I 55%: Congo: he? III [kl I. / N I .hIIL \ I l x WIHI \ I II m mm... I I I l.....m.\ \ WWm WW I .38 cm I as: one a: 3: I a: as dead A angina _ Idu dIcwdfl Y'- uuotqemJoJ GSJGABJLu 22 and northeast of Eaton County the same limestone becomes thinner and eventually goes unnoticed in well logs. In Ingham County well #145 the Eaton County sequence overlies the normal Traverse formation sequence. Here the upward succession is 2 feet gray calcareous shale, 9 feet brown dolomitic limestone (Squaw Bay?), 19 feet black or brown shale (Antrim?), 7 feet gray-brown shaly limestone, 63 feet brown shale, and 8 feet gray dolomite. The Eaton County sequence can be traced throughout most of the Lansing area, even though the included limestone layer is quite thin. This sequence is usually placed in the basal part of the Antrim formation. A tongue of Traverse formation coming from the west and pinching out to the east in Antrim shale seems to be the logical conclusion concerning the above relationship (Figure 5). This was proposed by Cohee (1947). Hake and Maebius (1938, p. 457) believe that the Traverse—Antrim transition zone of western Michigan corresponds in strati- graphic position to Antrim shale in eastern Michigan. REGIONAL STRUCTURE The Lansing area is in the south central portion of the Michigan basin. The Michigan basin is surrounded by positive structural elements which have been intermittently active throughout the Paleozoic. To the southeast is the Findlay arch and to the southwest is the Kankakee arch. The Wisconsin highland is to the northwest and the Laurentian highland is to the northeast. Most Michigan strata dip away from these regional structures and thicken toward the center of the basin (Plate 7). Traverse rocks form a saucer structure in the Michigan basin with the northern rim much thicker than the southern rim. Top of the Traverse group reaches a depth of about 2300 feet below sea level in central Michigan. The main axes of subsidence during Traverse time were in the northern Lower Peninsula with a northwest trend (Newcombe, 1933, p. 108). Newcombe (1930, pp. 734-735) believes that the Traverse strata overlap successively older rocks to the southwest. Folding has occurred in Traverse rocks as well as other Paleozoic sediments of the Michigan basin. This folding takes the form of asymmetrical anticlines, troughs, terraces, domes, structural noses, and bending of strata over reef structures. It ranges from the smallest imaginable 2a to as large as that exemplified by the Howell anticline which extends for more than 50 miles. Causes of the folding are numerous. Most important are regional stresses, deep seated faulting, vertical compaction, solution, and reef effects (Newcombe, 1933, pp. 113-120). Michigan folds can be classified into four groups based on direction. The most prominent direction is northwest-southeast. Other directions are northeast- southwest, north—south, and east—west (Newcombe, 1933, p. 116). The folds everywhere seem to plunge toward the center of the basin. This indicates, perhaps, that the folds are mainly the result of deep seated faulting rather than the direct result of laterally transmitted forces. Periods of folding for Michigan rocks are difficult to determine. In general, most of the folds which affect the Traverse group appear to have begun by the middle Devonian and to have continued at least until the Applachian revolution. Every disturbance, major or minor, close enough to be felt in Michigan, probably accentuated the development of these folds (Newcombe, 1933, pp. 94-95). LOCAL STRUCTURE General Traverse rocks in the Lansing area form a deposit which dips generally northward and thickens from about 300 feet to 450 feet, also northward. The top of the Traverse group ranges from 420 feet below sea level in T5N, R2E, to 1840 feet below sea level in T8N, R5W. A comparison between Plate 3 (top of the Traverse limestone), and Plate 6 (base of the Traverse group) shows the Traverse group to have almost exactly the same struc— tures as the underlying rocks. Structures in Plate 3 are more detailed than those in Plate 6, due to the increase in well data. When Plates 3 and 6 are compared to Plate 4 (thickness of Traverse limestone), a relationship is seen to exist between high structures and thinning of the Traverse limestone. Traverse high structures and thinning may have resulted from one or more of three causes: vertical compaction of Traverse sediments over pre-existing topography during and after Traverse time, buckling of beds during Traverse sedi— mentation, post Traverse folding and thinning of beds at the crest of folds. Traverse structures were probably the result of all of the above causes and began forming during Traverse time. That there was erosion of the pre-Traverse (Dundee) surface is generally accepted (Newcombe, 1930). Newcombe (1933, p. 95) believes that this erosion along with contemporaneous folding resulted in Traverse folds which were later accentuated by other period of folding. Howell-Owosso Anticline Traverse rocks of the Lansing area contain many struc- tures. The most prominent of these is that which is shown on the northeast edge of the map (Plate 3). This is the "north extension" of the Howell anticline (Newcombe, 1933, p. 259). The Howell—Owosso anticline trends northwest— southeast in Livingston County and enters Ingham County and Shiawassee County in T4N, R2E, and T5N, R2E. It then plunges a few degrees west of north. The western dip off the north extension is two degrees, at a minimum, between Shiawassee County wells #134 and #135. The actual dip is probably somewhat greater. Off the crest the dip becomes north and northeast at about one-half of one degree. In general, the north extension appears to be the west edge of a tilted block which is raised on the south- west and dips to the northeast. The trend of this structure is seen to continue with a lessening of dip north and off the map. Newcombe (1933, Plate 111) has suggested that the north extension along with the main anticline in Livingston County may be faulted. There is a northwest-southeast high trend across the northeast part of Clinton County (Plate 3). This trend is 27 in perfect alinement with the southern or main part of the Howell—Owosso anticline which trends northeast-southwest across Livingston County (Newcombe, 1933, p. 206). On the extreme southeast edge of Plate 3 there appears a structure which is not well defined and which lies mainly in the southwestern Livingston County and northwestern Washtenaw County. This structure seems to have a north- south trend and a steep western dip. If this is true then this structure is in general alignment with the north extension of the Howell-Owosso anticline and quite similar to it. Further to the south in northwestern Ohio the Bowling Green fault (Carman and Stout, 1934, p. 521) and its associ- ated monocline, which enter southeastern Michigan (Newcombe, 1933, Figure 40), have a steep western dip and trend a few degrees west of north. The Bowling Green fault, the struc- ture in northwestern Washtenaw County, and the north exten- sion of the Howell-Owesso anticline are in general alignment with and similar to one another. It appears that there are two distinct zones of faulting or folding, one trending a few degrees west of north and the other trending northwest. The intersection of the two has produced the sharp change in direction of the Howell—Owosso anticline from northwest to north. Newcombe (1933, p. 206) has suggested that the north extension of the Howell-Owosso anticline may not be directly related to the southern part of the Howell—Owosso anticline. 28 The Eaton County High Trend Trending from the southwest corner to the northeast corner of Eaton County there is a "high" which is defined by several wells (Plate 3). The possible existence of this structure was surmised in 1912 (Smith, 1912, p. 158) when the Delta well (#151) was compared to the Charlotte well (#158). This structure in Eaton County appears to be a fold which plunges toward the northeast. The eastern dip off the fold is steeper than the northern dip on the northwestern flank. Exact location of the crest is difficult to deter- mine from the sparse data available, but it appears to run from the Charlotte well to the Delta well. The direction of this structure'agrees closely with one of the major directions of folding in the Michigan basin (Newcombe, 1933, p. 117). No closure has been found on this structure. The remainder of Eaton County is clear of folds, based on information presently available. Ingham County Structures Little can be inferred about the structures of Ingham County from Plate 3, due to the lack of well data. The dip is generally north at less than one-half of one degree. The eastern half of the county has a northwest dip. One well, -#l50, seems higher than expected and may be part of a large structure. The Howell anticline enters the extreme north- east corner of Ingham County from Livingston County. Con- figuration of the Traverse rocks in the southeastern most 29 township of Ingham County is in question, but well data in Livingston County indicate a structure just east of the Ingham County line. Clinton County Trough The main structural feature in Clinton County is the trough which extends from the northwest to the southeast. This trough is distinguished by a lessening of northward dip. Center of the trough dips northward at about seven minutes of angle. It is bounded on the northeast by the northwest- southeast trending high which is aligned with the Howell anticline. The trough is bounded on the southwest by the greater normal dip of Eaton and southern Ionia Counties. The Clinton County trough diminishes in width as Ingham County is approached on the south, where the dip becomes greater. Continuation of the trough with a change of direction to southwest may parallel the Eaton County high trend on its eastern side. Ionia County No structures are shown in southeastern Ionia County by Plate 3. The dip here is northeast at less than one-half of one degree. Northeastern Ionia County and northwestern Clinton County have had much drilling activity. The Traverse limestone surface is quite irregular in this area. However, there seems to be two north-south high trends paralleling each other, but separated by the Ionia-Clinton County line. These trends are shown best by Plates 4 and 6. GEOLOGIC HISTORY The history of the Traverse group begins with the Dundee unconformity. At this time the land surface was undergoing erdsion and slight folding (Newcombe, 1933, p.95). As the water level rose and the Traverse sea spread southward a elastic mud was distributed and laid down as the first Traverse deposit. This sediment later became lithofied to a calcareous shale. The basal shale zone is represented in the Lansing area by a maximum of 100 feet of Traverse rock. As could be expected of a wave distributed sediment on a low but undulating surface it thins and thickens irregu- larly (see Local Stratigraphy). The shale changes laterally westward to an argillaceous limestone (Plate 2) indicating that the source area was to the east. The Lansing area appears to have been on the western fringe of shale deposi- tion, consequently the shale deposit is interrupted by limestone layers. These limestone layers within the basal shale zone may be due to westward advance and eastward retreat of the area of shale deposition. They may equally as well be due to currents which deposited the shale in lobes. The lobes may or may not have covered the same area as before. Well logs 31 report sometimes one, sometimes several layers of shale in the basal zone. Finally, the elastic source could not supply enough sediment to form shale in the Lansing area. The area of shale deposition moved further east and northeast closer to the source. Lime deposition, which was active in the west, then began to dominate sedimentation in the Lansing area. Clastics were still arriving, however, at least in Clinton, Shiawassee, and Ingham Counties, but only with enough influence to cause the lime-muds to be argillaceous in places. This limestone together with the underlying shale zone compose the lower half of the Traverse section. Lime deposition was prevalent in the Lansing area during most of Traverse time. Shale deposition must have retreated still further as the argillaceous character of the lime—muds disappeared in all but the northern part of Clinton County. The record of this period of time consists of light colored pure lime- stone, chert, fragmental limestone, coralline material, and dolomite (whether primary or secondary is not clear). This Isection of the Traverse group represents a time during =3edimentation when the sea was shallow, the water was rela- tSively calm, and the highlands were low or far away. A Ekarsistant water horizon occurs at the top of this zone. 3311s porosity probably originated in fragmental limestone ‘Vitth recrystallization and secondary dolomitization modifying iUt somewhat. 32 After a period of clean limestone deposition the water again began transporting argillaceous material into the Lansing area. This elastic material was back to stay for the rest of the Devonian time. The record shows argillaceous limestone above the clean limestone, and calcareous shale above the argillaceous limestone. Within the calcareous shale are layers of limestone. One of these is widespread I and relatively pure, although rather thin. It testifies to the interruption of shale deposition for a short period. Above the gray calcareous shale is the black, non-calcareous shale of the Antrim formation. The base of the Antrim and the top of the Traverse appear to be intertongued in the western half of the Lansing area. Therefore, the upper Traverse beds in the west may be equivalent to the lower Antrim in eastern Michigan. An un- conformity is believed by Kirkham (1932, pp. 136—137) to be located at the top of the Traverse group. The ages of folding in Traverse rocks can not be deter- mined by this investigation. Newcombe (1933, p. 95) believes there was folding during the Dundee-Rogers City erosion interval and later folding along the same structures during Khost-Traverse periods. Thinning in Plate 4 indicates that Ikalding was proceeding while Traverse sediments were being léiid down. The Howell anticline in Livingston County began 'tCD fold and fault during Goldwater time, according to Kilborne (1947, p. 21). A different age may be possible 3F<>r the "north extension." PETROLEUM POSSIBILITIES IN THE LANSING AREA General When considering the petroleum possibilities of the Traverse group in the Lansing area certain facts are evident. These facts are as follows: the Traverse group is productive in other parts of the state, oil is present in the Traverse group in the northwest corner of the Lansing area, the sequ- ence of rocks in Central Michigan (a productive region) is the same as those in the Lansing area, Traverse strata are thinner in the Lansing area than the Central Michigan region. Only the last fact mentioned is detrimental to the likehood of oil being present in the Lansing area. This last fact is not considered too important. Traverse rocks in the Muskegon oil field, of approximately the same thickness as those in the Lansing area, produced oil. Another consideration which is important in determining the oil possibilities of an area is the presence of reservoir IPocks. A reservoir rock is present in the Traverse of the JLansing area in the form of the persistent water horizon of tune Buff limestone. This porous zone is usually several feet thick. Quite frequently it causes a well hole full of WEtter, indicating that the porous zone transmits the ‘33Cpected hydrostatic pressure and probably ranges as far as ‘3r1e of its surface exposures. However, not all wells have 34 found porosity at this horizon. Some wells received less than a hole full of water. This lessening of permeability may have been caused by an original lack of permeability, cementation at the time of deposition, or chemical action after consolidation. No relationship was seen to exist between Traverse structure and permeability in this water horizon. Other possible reservoir rocks indicated by water zones are the Gray Cherty limestone and the limestone of the "Traverse formation." Also, possible reservoirs might be found in the Traverse in the form of reefs, fractured rock, or layers of a fragmental texture. Since there is the possibility of both petroleum and reservoir rocks being in the Traverse of the Lansing area the only consideration remaining is that of favorable struc- tures. The possibility of favorable structures being in the area is fair. However, no traps either stratigraphic or structural have been defined by this investigation. Several structures are of interest for future exploration or investigation. Eaton County High Trend The structure in Eaton County, which trends northeast- southwest across probably the entire county, is a prime exploration target. This structure is asymmetrical with the southeastern dip greater than the northwestern dip. The crest is narrow in comparison to length. It plunges north- east and shows no closure along its length. However, if 35 closure should be found this structure would become a possible trap. Two gas shows and a rainbow of oil have been reported from different wells in the area of the high trend. All shows have been at different horizons. No shows were reported from well #158 which seems to be near the crest of the anticline. Thinning of the Traverse and succeeding formations over this structure indicate that it began during or prior to Traverse time. North Extension of the Howell-Owosso Anticline More information is needed before much can be said or interpreted about this structure. Its plunge is slightly west of north. The western limb of this structure dips west at a rate of at least 2 degrees. The age of this part of the Howell anticline and its cause are unanswered questions. No closure has been found on this structure. However, closely spaced wells may bring out irregularities along the crest, much the same as that in T7N, R2E. Here well #131 shows a reversal of the normal dip. Well #132 discovered a small accumulation of oil. If the north-extension has been created by faults which extend into Traverse rocks, such faults may have caused traps to form. Df these faults do not extend into Traverse but are at depth, then the extension of their fault planes into Traverse rocks may locate porous zones . 36 Clinton County Extension of the Howell Anticline This structure trends northwest-southeast across the northeast corner of Clinton County. By its location and direction it appears to be related to the Howell anticline. The Clinton County extension is broad in relation to its length. No closure has been found on this structure. Six wells all within approximately three miles of each other have had shows of oil on this structure. Two of these wells have had shows in the Dundee formation, as well as in the Traverse. Such an association of shows strongly suggest the possibility of an oil trap somewhere in this vicinity. If not in the Traverse, then perhaps in the Dundee. Northwestern Corner of the Lansing Area Three small but commercial oil pools have been found in this corner of the Lansing area. All seem to be con- trolled by structural and porosity conditions. Pay zones are in the Cherty limestone. Some Dundee production has been found in this area also. A great amount of drilling activity has taken place in this northwest corner. Structural conditions at the top of the Traverse are very irregular and complicated. Plates 4 and 6 show the general structural picture. Two highs paralleling each other extend northward. One is on the Clinton side and one is on the Ionia side of their mutual county line. Compaction over Dundee structures and uneven compaction due to varying sediments has probably caused the 37 Traverse surface to be uneven and irregular. Oil has been trapped in these minor high structures where porosity was good. This is exemplified by the three oil pools in this area. Similar irregularities at the top of the Traverse are probably present throughout the Lansing area. Clinton County Trough The Clinton County trough and its southwest extension into Ingham and Eaton Counties can be considered an area of possible petroleum traps. It is unlikely that the top of the Traverse could dip evenly at seven minutes of angle. Very likely there are high and low irregularities in the trough area, just as there are in the northwest corner. In the trough area little height is necessary to gain closure. Few shows of oil or gas have been reported from the trough. Stratigraphic Traps Many shows of oil in the Lansing area occur at the base of the Antrim or the top of the "Traverse formation." These shows occur in rock which is usually brown dolomite or dolomitic limestone. They appear to be caused by porosity traps and not by structural traps. The oil shows might also be caused by minor inter- fingering at the base of the Antrim, where brown dolomitic limestone layers, from the Traverse, pinch out in the Antrim shale above. CONCLUSIONS AND RECOMMENDATIONS The Traverse group in the Lansing area can be divided into several lithologic units. These units are from bottom to top: basal shale zone, gray-brown limestone, buff lime- stone, gray-cherty limestone, and "Traverse formation.” "Traverse formation" can be divided into three parts: lower gray shale, brown dolomitic limestone, and upper gray shale. These units are present throughout the Lansing area, with the exception of the basal shale zone which thins to the southwest and is missing in parts of Eaton County. All units except the "Traverse formation" thin to the south or southwest. The "Traverse formation" appears to thin eastward. The dip of the Traverse group in the Lansing area is generally to the north, but in the eastern part of the area the dip is northwest. In the western part of the area it is northeast. Large structures in the Lansing area include the Eaton County high trend, the north extension of the Howell anti- cline, and the Clinton County trough. The Eaton County high trend is an asymmetrical anticline or nose which plunges northeast. The east limb dips steeper than the west limb. The north extension of the Howell anticline is in Shiawassee County. It is an asymmetrical anticline which plunges a few 39 degrees west of north and has a steep western dip. The eastern flank of this structure dips northeast. The north extension may be the result of faulting. The Clinton County trough is a synclinal structure. It is wide in northern Clinton County and narrows down to the southeast as it approaches Ingham County. From northwest Ingham County this trough extends southwest across Eaton County. The Clinton County trough dips more gently to the north than the sur— rounding area. Closely spaced wells show the top of the Traverse limestone to be irregular with small domes, noses, and other structures. It is reasonable to believe that there are petroleum traps in the Lansing area. However, no traps were located by this investigation. Several structures or areas are of interest for future exploration and investigation. These are: the Eaton County high trend, the north extension of the Howell anticline, the Clinton County extension of the Howell anticline, the undefined structure in central Ingham County, the undefined structure in southeastern Ingham County and southwestern Livingston County, and the entire Clinton County trough. EXPLANATION OF PLATES 2, 3, 4, 5, and 6 Plate 2--Well Log Correlation This drawing was constructed to illustrate the thick- ness and southward thinning of the Traverse group. It also shows the relationship between the Traverse group and the ~Antrim shale. Between the Traverse limestone and the base of the Antrim shale is a transition zone composed of inter- calated calcareous shale and limestone. Cross section A-C shows the absence of the basal shale zone (Bell shale?). Wells #153 and #115 contain shaly lime- stone in the interval which corresponds to the basal shale zone of other wells. The same relationship occurs in wells #32 and #65 of cross section A—B. This introduces the ques- tion of whether the basal shale is absence due to latteral gradation and facies change. Plate 3--Structural Contour Map of the Traverse Limestone Top of the Traverse limestone was used for a marker horizon in the construction of this map. The top of the Traverse limestone is the upper limit of reservoir rock. All rock above is shale with the exception of the Squaw Bay and thin carbonate layers in the base of the Antrim, which are difficult to correlate. Top of the Traverse lime- stone is usually reported in well logs which otherwise give a minimum of information. 41 A 25 foot contour interval was used to allow for in- accuracies arising from depth measurements, correlation, poor sampling, and poor recording. The greatest inaccuracy is the means of location the top of the Traverse limestone. The limestone grades upward into shale, so the top of the Traverse limestone must be placed at that point below which there is no significant amount of shale. In the Eaton County area the top of the Traverse is overlain by shale and also a significant amount of limestone (see Local Stratigraphy). When the top of this limestone is mapped the structure is found to be essentially the same as that shown in Plate 3. The steep slope on the southwest side of the Howell anticline may indicate a fault, rather than the limb of a fold as shown. Plate 4--Isopach Map of the Traverse Limestone A contour interval of 50 feet was used in constructing this map. Most of the high trends seen on Plate 3 and Plate 6 are represented on Plate 4 as areas where the Traverse is thin. The north extension of the Howell-Owosso anticline is not clearly represented on this map. However, there is a lack of data of this area; faulting or abnormal dips may have complicated the existing data. Too much reliance should not be placed on the isopach lines in the south half of Plate 4. Sufficient data was not obtained. Isopach lines in T5N, R2W, and T5N, RlW, are in 42 question. If the base of the lower shale zone is placed higher in the Traverse column than is actually true, then the formation would show thinning. This situation is possible in the above mentioned townships. Plate 4 was constructed entirely from well information, and not by superimposing Plate 3 on Plate 6. Plate 5--Panel Diagram of the Traverse Group This diagram was constructed to illustrate the thinning and shale-limeStone relationship of the Traverse group in the Lansing area. Traverse lithology has been generalized in this drawing. Plate 6--Structural Contour Map on Base of Traverse Group This map corresponds very closely to Plate 3. It was contoured with the same interval (25 feet). The southern half of this map has been contoured with a 100 foot interval. So also, has the north extension of the Howell-Owosso anti— cline. The north extension may be faulted. Information in T5N, RlW, and T5N, R2W, is in question here, as it was in Plate 4. EXPLANATION OF TABLES Code No. Number assigned to a particular well by the author and used in the written material. Well samples have been examined if this number is underlined. State Permit Well permit number assigned by the State of Michigan. Name and Location Self-explanatory. Elev. Elevation of the rig floor in feet above sea level (approximate eleva- tion in some cases). Show Depth in feet below sea level at which a show of oil or gas was encountered. An asterisk indicate a show of oil. Two apostrophes indicates a show of gas. Water Depth in feet below sea level at which a salt water horizon was encountered. TTrL Depth in feet below sea level to the top of the Traverse limestone. BB Depth in feet below sea level to the base of the Traverse group. 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.as ossosoooz .o.m s .s.m oooa mma .3mm .zse oosa oosa mom .sa.oom .s\a-mz.s\aIsz .as sessom omoa mma mssa omm .me.zsa.0a.oom.s\aIzz .aaoz spams ama asseImm mm ates sous: zoom .soam noanoooa oos ossz passes .oz oooom oooo E7500 zoefim 61 .zom.2as.om.oom.s\aI3m.s\aIzz msm ooaa amm mom som .as .oo osoEoo osoaosom onoas mms moa .zom.zas .s.oom.s\a-3z mom omOa o.amm .s\a-mz.s\aImz .as mssoo.m.z mams moa .zmm.2ms .mm asOa amaa som .oom .s\aI32.s\aI3m .as bosses smm aoa asssImm mm anse soon: zoom .soam soaooooa oos osoz basses .oz spasm oooo .IIII IIlI n H F IIHI I1 boss.“ pCOOIIEZDO o zoedsm BIBLIOGRAPHY Carman, J. E., and Stout, W. (1934) "Relationship of Accumulation of Oil to Structural and Porosity in the Lima-Indiana Field," American Assoc. of Petroleum Geologist, Sidney Powers Memorial Volume, pp. 521—529. Cohee, G. V. (1947) ”Lithology and Thickness of the Traverse Group in the Michigan Basin," U. S. Geological Survey Oil and Gas Investigations, Preliminary Chart 28. Grabau, A. W. (1902) "Stratigraphy of the Traverse Group of Michigan," Michigan Geological Survey Annual Report Of 1901, pp. 161-210. Hake, B. F., and Maebius, J. B. (1938) "Lithology of the Traverse Group of Central Michigan," Michigan Academy of Science Papers, Vol. 23, pp. 447-461. Kilbourne, D. C. (1947) "The origin and Development of the Howell Anticline in Michigan," thesis, Michigan State College. Kirkham, v. R. D. (1932) "Unconformity at the Top of the Traverse Formation in Michigan," Geol. Soc. of America Bu11., VDl. 43,No. 1, pp. 136-137. Lane, A. C. (1895) "The Geology of Lower Michigan with Reference to Deep Borings," Geological Survey of Michigan, Vol. 5, Part 11. Michigan Historical Commission (1928) "Geological Reports of Douglass Houghton." Newcombe, R. B. (1930) "Middle Devonian Unconformity in Michigan," Bull. Geol. Soc. of America, Vol. 41, pp. 725-738. Newcombe, R. B- (1933) "Oil and Gas Fields of Michigan," Michigan Geological Survey Publication 38, Geology Series 32. Pohl, E. R. (1930) "The Middle Devonian Traverse Group of Rocks in Michigan," Proc. U. S. Natural Museum, Vol. 76, Art. 14, pp. 1—34. 63 Smith, R. A. (1912) "The Occurrence of Oil and Gas in Michigan," Michigan Geological Survey, Put. 1A, Geological Series 11. Warthin, A. S., and Cooper, G. A. (1943) "Traverse Rocks of the Thunder Bay Region," American Assoc. of Petroleum Geologists, Vol. 27, No. 5, pp. 571-595. Winchell, A. (1871) "Report on the Progress of the State Geological Survey of Michigan." ” JUL 151961 f ' ‘ Jitter—26496}- ho . __ ~—+————- —— rt%.;r————‘—“‘ “3 —— ————-———+ -- —— —- ——-|63 '22 o O . . 1 " ‘° 0 . 59 ’ 1o ' 9 1 0 $9 . :. 61 50 1 9| 4O 0 . " “$4 5% 1 , . 6° 0 . g 1 o 31 1 , ’ 85 $2 1 E3 ‘ 1 ” 1 . o . . . .1/ €12 6.4 6" 93 42 1—/ . . o o 0 E3 .8 ° ' 66 1;. 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