-~.-‘.': .~ -- a.“ A.-...\~ 1 Cunu’El m . k-.l.,....‘ ... n... «J— 2..._”:‘-§&.st.~. _.. - h ,_ v .» hwy—“.3. SL3“ ‘ A. (.3..1«,N:.‘:.-W ‘ ~ .-. ‘524. - 3.1....3; v .m... .— .. ‘T,~:.~.~.-.<.x‘~~—~. _ ”3.“:5; . .1.g...~.12;-J ’5‘“:- L, ~ 1 1. “10,223"; .. ‘ l 1;. \ ~ ._ .p. .. ‘ rig?” 5v”. .‘. .Vl . ‘- no»-.- _, _~ . "vb, \-.‘_. .. ‘ . .. ::. ,. -.\ "5:11. _‘_ ‘ v N W. 1 3 2‘ .c.‘r\-.‘. .1; .___ v \ . "315K .FJJ.’ ‘,“‘1‘s‘<\ ‘-\-‘h‘<:fi.¥-E~.w . . “~53: " “"v' ~ \.‘,~._- ' “ow - n , 2a." ‘ ‘ develop an effective and efficient method for studying thick slwale sequences possessing variable lateral and vertical proper- ties. Standardized color descriptions of cuttings from hh3 wells distributed throughout the Southern Peninsula of the state formed a major source of the data which were later analysed and plotted by computer techniques. Other variables included thicknesses and lithologic textures. Interpretations were based on both intraformational and inter- formational variations. These interpretations suggest that the factors controlling local deposition were established in Antrim time and persisted until the deposition of the Sunbury Shale. The post-Antrim sediments were derived from two source areas, northeast and northwest. The former produced the birdfoot Bedford- Berea delta, while the latter resulted in the deposition of a thick mass of green shale which may represent the pro-delta of some delta farther west. The development of these Early Mississippian deltas may represent the first indication of greater deltaic sequences in L. Olayinka _Asseez the PennSylvanian period. The blanket nature of the Berea Sandstone with local thickenings serve to identify the formation as apron sands and bars rather than the anastomosing channel deposits farther east of the state boundary. The Bedford Shale is the pro—delta deposit of this delta. If this interpretation is correct, the Bedford Shale and theBerea Sandstone cannot represent totally different times of deposition. Thus to some extent they are time equivalent. The restriction of the Bedford-Berea sequence and the Ellsworth Shale to their respective basins was effected, not by a structural or topographic barrier, but by an environmental barrier where all sediments deposited were turned black. The black shales owe their origin to the preservation of their organic content in a reducing shallow water environment. The green shales, on the other hand, were deposited in a mildly reducing environment,“ which the organic matter was: not preserved. The green color is due to the abundance of green clay minerals, glauconite and ferrous ions ° ...-,_- — ~.—-. *‘ -. . l -—.—- w‘l- — n. STRATIGRAPHY AND PALEOGEOGRAPHY OF THE LOWER MISSISSIPPIAN SEDIMENTS OF THE MICHIGAN BASIN By 'lgd’Y‘J _ L. Olayinka Asseez A THESIS Submitted to Michigan State University in partial fulfillment of the requirements for the degree of DOCTOR OF PHILOSOPHY Department of Geology 1967 7.731219 v 0/23/07 DEDICATION To my wife, Teleolé Ajike, whose patience, encouragement, forbearance and support have made it possible for me to assemble the material for this manuscript - F—r—“fl” ' “M""wmqur “NI .19." TABLE OF CONTENTS Page DEDICATION . . . . . . . . . . .. . . . . . . . . . . . . ., .. ii ACKNOWLEDGEMENTS . . . . . . . . . . . . . . . . . . ., . . . . v HGURES . .. .. .. . .. .. .. .. . .. .. .. .. . . vH PUNTES . . . . . . .... . . . . . . . . . . . . . .. . . . viii APPENDICES .. . . .. . .. . . .. . .. . . .. . .. . . x TABLES . . .. .. . .. .. . .. .. . .. .. . .. .. . xi Chapter I. INTRODUCTION . l 1| , PREVIOUS WORK. . 2. Stratigraphy 2 Antrim Shale 2 Bedford Shale A Berea Sandstone u Ellsworth Shale 7 Sunbury Shale 8 Structural Setting 8 Michigan Basin 8 Intra-basinal Structure ll Boundary Elements of the Michigan Basin l2 Wisconsin Arch I2 Kankakee Arch I2 Laurentian Highlands I3 II I. r4ETHODS OF INVESTIGATION , IA Field ”I Antrim Outcrop Locations lh Ellsworth Outcrop Locations I6 Laboratory I6 Methods of Analysis l8 Computer Analysis l9 Maps and Charts 19 IV [RESULTS AND ENVIRONMENTAL INTERPRETATION , 21 Post Traverse.Structural Controls 21 Pre-Mississippian Occurrence of Structures 26 Stratigraphic Variation Antrim Shale Environment of Antrim Deposition Effects of Compaction Stratigraphic Subdivision of the Antrim Shale Post-Antrim Sedimentation Facies Barrier Ellsworth Shale Geologic and Environmental Interpre- tation Bedford Shale and Berea Sandstone Bedford Shale Berea Sandstone Environment of Deposition Sunbury Shale Geologic and Environmental Interpre- tation Petrographic Notes V. CONCLUSION. VI _ BIBLIOGRAPHY, VI I. APPENDICES. l. X-ray Diffraction II. Computer Analyses Page 38 III 51 )I 5] 5a. 60 66 67 79 BI 8h 103 IO6 nu 151; ACKNOWLEDGEMENTS 1Wwe author would like to express his profound gratitude to the fol lovving individuals and departments. To Dr. Chilton E. Prouty and Dr. Robert Ehrlich for their sincere ilwterest, guidance and very helpful suggestions and criticisms during the study and preparation of the manuscript. To Dr. Jane E. Smith, Dr. William J. Trow and Dr. James H. Fisher for reviewing the manuscript and making helpful suggestions. To John 0. Kopf, for his assistance in preparing the computer programs. To Dr. Charles C. Hughes, Director of the African Studies Center, for giving the writer access to the office equipment in the Center. To Dr. Cross for his personal interest in the welfare and progress of the writer. To the Nigerian Government for financing the university education of the writer. To the staffs of the Geological Survey of Michigan, especially Garland Ells, Beverly Champion and Floyd Layton, and the Subsurface Laboratory of the University of Michigan, particularly Dr. L. I. Briggs, for giving the writer free access to their samples. To Karl Hoover, Ohio Geological Survey, for sending some Ohio samples to the writer. To Dr. M. M. Mortland, Soil Science Department and Dr. D. E. Scher- pereel, Metallurgy Department, for allowing the writer to use their X-ray diffractometers. To all the graduate students in the Department of Geology who have been helpful in one way or another, particularly Jack Travis for reviewing the manuscript, and James Zaitzeff, Z. Syed and John Kowalski. 2 2 Ail A) :— L» 0\ \n “1 FIGURES Simplified geologic map of Michigan Regional structure of Michigan basin and adjoining areas observed on top of Trenton Limestone Magnetic map of the Southern Peninsula. Michigan Gravity map of the Southern Peninsula, Michigan Structure contours on top of Dundee-Rogers City sequence Paleogeographic map, Early Berea time Locations of samples used in petrographic analyses Locations of x-rayed Antrim Shale Locations of x-rayed samples (Ellsworth and Bedford) Locations of x—rayed samples (Sunbury and Goldwater) Locations of samples from Ohio ll9 l2l I23 150 I9. 20. PLATES Isopach: Antrim Shale Aritrim Shale: Percent black shale Isopach: Bedford Shale Isopach Berea Sandstone Thickness of Ellsworth Shale in the west Isopach: Sunbury Shale Isopach: Ellsworth Shale and Bedford-Berea sequence Isopach: Top of Traverse Group to bottom of Coldwater Shale .~ Structure contours on top of Antrim Shale Major structures observed on top of the Antrim Shale Structure contours on top of Bedford Shale SS/SH ratio map: Bedford Shale-Berea Sandstone Isopach: Bedford Shale-Berea Sandstone >Sections from top of the Traverse Group to the Sunbury Shale top Cross sections: Top of Traverse Group to the top of Sunbury Shale Cross sections: Bedford Shale—Berea Sandstone Paleogeographic map: Bedford-Berea delta Index of well locations Approximate area distribution of carbonates in the Ellsworth Shale Generalized cross section of the Lower Mississippian formations showing lateral relationships interpreted from Plates l3 and IA Micrographs: Shales Micrographs: Berea Sandstone viii 27 28 29 30 3I 32 33 3h 35 37 39 1+2 1+3 Ah 225 M6 27 #8 55 56 83 87 2l. Correlation Charts (a-j) 2.2. X—ray diffraction patterns of three shale samples APPENDICES X- ray Analyses IIA Analytical techniques llA ldentifkmtion IIA Geology and environmental indication of clay minerals Il6 Results llT a. Antrim Shale II? b. Ellsworth Shale ll8 c. Bedford Shale I20 d. ‘Sunbury Shale I22 e. Coldwater Shale I22 f. X-ray data I25 i. Antrim Shale I25 ii. .Ellsworth Shale I33 Bedford Shale I39 Sunbury Shale IAI Coldwater Shale IAT Ohio samples IA9 Computer Analyses I5A Coding I5A Envidep I55 -Data input 155 Input format statements l5? County codes IE9 Data plotting I63 Maplot I6l Parameter cards I62 Computer analyses (input and output data) I6A a. Envidep I65 b. Identification of wells gIT'l c. Well records l8l d. Card output (Bedford-Berea) 29A e. Card output (Antrim, Ellsworth and Sunbury) 302 f. Maplot 3I2 TABLES Correlation Chart Generalized section of Devonian-Mississippian Systems in Michigan Definition of color reference standards of shales xi FACULTY Department of Geology The followingis a panflal under whonil studied: Chilton E. Prouty Professor and Chairman Aureal T. Cross Professor, Geology and Botany James W. Trow Professor, Structural Geology and Petrofabrics Maynard M.Miller Professor, Glaciology W.J. Hinze Professor, Geophysics Justin Zinn R.|.P Professor, Precambrian Geol. Robert Ehrlich Asst.Professor, Sedimentology Harold B.Stonehouse Assoc.Prof; Mineralogy JamesIL Fisher Assoc. Prof; Petrol. GeoI. Jane E. Smith As soc. Prof. Paleontology The Ph.D.Committee was composed of xii list of the Faculty, Department of Geology, : Prouty and Ehrlich Co-Chairman Trow . Smith and Zinn . Chapter I INTRODUCTION This study is an attempt to develop an effective and efficient method for studying thick sequences of shales possessing variable lateral and stratigraphic characteristics. Four shale formations (the Antrim, Bedford, Ellsworth and Sunbury) and an included sand— stone unit (the Berea) occurring in the Michigan basin were selected for this purpose. The five formations average a thickness of about AOO feet. Over 500 wells covering most of the Southern Peninsula of Michigan were studied. Cuttings were described texturally and according to color standards selected for this purpose. The resulting data were ana- lysed and plotted with the aid of computer techniques. The effectiveness of the method was tested by evaluating the relative success achieved in determining the: l. Stratigraphic relationships 2. response of sedimentation to tectonic history of the basin 3. depositional environments A. possible correlation between the physical properties of the well cuttings and the fluctuations in the gamma ray and elec- trical logs. Chapter II PREVIOUS 'WORK ' _'" _—v Stratigraphy: The Antrim Shale is a part of the Devonian-Mississippian black shale sequence widespread in the United States. It is overlain grada- tionally by the Bedford Shale in the east and the Ellsworth Shale in the west of Michigan. The Bedford Shale as well as the overlying Berea Sandstone are lateral equivalents of the Ellsworth Shale. A thin blanket of black shale, the Sunbury, overlies the Berea Sand- stone and the Ellsworth Shale except wher the red phase of the Cold- water Shale, the Coldwater 'red rock', directly caps the Ellsworth Shale in the western parts of Michigan. Antrim Shale: The type locality of the formation is in Norwood in Antrim County, Michigan, after which it was named by Lane (I90l). Devonian age was first suggested, but the discovery of Mississippian fossils in it (Newcombe, I933) confirmed that it was deposited, at least in part, during the latter period. The recognition of erosion surfaces on top of the Traverse Limestone in the southwest (Bishop, I9AO) may indicate the Devonian-Mississippian contact at the bottom of this formation. The Antrim Shale may be correlatable with the black shales in the adjacent areas--Long Rapids Formation in James Bay, Kettle Point Formation in southwestern Ontario, Ohio Shale in Ohio and Pennsylvania, New Albany Shale of Indiana and Illinois and the Kenwood Shale of Milwaukee, Wisconsin (Table l). The lithology of these formations DEVONIAN LST. Mlsiismiplan S.W. Texas a WOODFORD mes one 3 S HUNTON Mis s iis igpian Oklahoma 1m F LOWER ARKANSAS MIDDLE ARKANSAS NOVACUL— Uiper ‘3“??? i; NOVACULITEH‘ ' ITE Né‘f/agfiifie uac 1 as Q " g a 2:20 2 _ (Cut 5 g E; St.Joe N.W.Arkansas*i “ <1 as CHATTANOOGA m DEVONIAN LST ' g E.Kansas g l . V g ‘€.h out e a u $.13, é; (t3 Nebraska 3 ‘ C E D A R m h Lime Maple Hill 5 Hampton Central Iowa“, VALLE-Y Creek Eu "” g - . m Grassy alver— Hannlbal N.E.Missouri H Creek on m E, ’ . ‘ h o u t e a 11‘ lg Cent.IllinoiI E“ NEW ALBANY :1 SELLERSB ' G Rockford Indiana 05‘ 9% KELLSWORTH W.Michigan g m .TRAVERSE GROUP _ AN Coldwater _' w m TR I M E g g E.Michigan H: m o" 3 9’ ti SILURIAN DOL. \ 94 C u y a h o g a S.Ohio DEVONIAN LST. OHIO New Provmce E.Cent.KY. F 9, or E.Central $21 SILURIAN/ORDOV. H _ 23D Tennessee Q .d CHATTANOOGA - ‘ ‘a (D SDI— EH 938 9 y W.Tennessee m - :3 a, e L'L I ISLAND HILL WEETSTONE BRANCH camaCk N.E.Miss. ‘ FROG MTN. CHATTANOOGA F0? N'Alaba‘ma hw. ayne is so similar that they are at least partially correlatable with the Antrim Shale of Michigan. Bedford Shale: Newberry (l870) named the Bedford Shale after the town of Bedford, Cuyahoga County, Ohio. It is typically a bluish gray shale that is sandy to silty in places. It is restricted to the eastern parts of the Michigan basin and overlies the Antrim Shale with a gradational contact while it is in turn overlain gradationally by the Berea Sandstone. Berea Sandstone: The Berea Sandstone was also named by Newberry (IBTO) after the town of Berea, Cuyahoga County, Ohio, where it is exposed. It is also restricted to the east of the basin (Hale, l9AO). Cohee (l95l) recognized three lithologic units in the Berea of Michigan. I. Lower sandstone, light gray, fine-grained; silty, shaly micaceous and pyritic with silica and dolomite cement. 2. Middle friable sandstone, angular quartz, interbedded shale and tightly cemented sandstone. 3. Upper sandstone similar to (I) but less shaly and less pyritic. He also observed that the maximum thickness for the formation was in the Saginaw Bay area. A comprehensive study of the Bedford-Berea sequence of Ohio was reported by Pepper, De Witt and Demarest in I95A. They con- cluded that the formations are deltaic deposits with several sources, notably east and north. They represent a cycle of depo- FifiLSianlified Geologic Map of Michigan (MGS. 196A ) . Juras " No Record Pennsylvanian Mississippian Devonian-Mis s . Devonian f. 341:; Silurian ., -- =..- . . :o-Ozz- ‘. o. Ordovm mm 6 e e - e e; Cambrian e e e6 7”: 7,? Precambrian 4 4+ Q 2.5 5.0 '“ miles 1; -SYSTEM SERIES GROUP FORMATION THICKNESS [FT] I Mermec Bayport Limestone 120— 100 I IS 0 Meramec- Michigan formation 0— 500 Osage, S W I Napoleon Sandstone 50- 100 S A S Coldwater Shale 500- 1000 , N I P Sunbury Shale 10— 90 P I Berea Sandstone O- 210 A N Bedford Shale 10— 500 Ellsworth Shale 30-AOO Antrim Shale loo- l+50 SENECAN D Thunder Bay Limestone lAO E E V Alpena Limestone 120 O R N I Long Lake Limestone 190- 200 I A A N Bell Shale so— 80 N ULSTERIAN Table . 2 Generalized section of Devonian-Mississippian Systems in Michigan [modified after MGS Geol.map 1956] sition during the oscillation of land and sea between two periods c>f quiescence and that the bottom of the Bedford Shale probably marks the Devonian-Mississippian boundary. However, they sug- gested that the Bedford and Berea be regarded as a genetic unit wherever the location of this contact. Although their work was terminated at the Michigan-Ohio border, they suggested that the Ontario river system that depo- sited the Ohio formations was probably diverted into Michigan to deposit the Berea sands after a similar deposition had been com- pleted in Ohio. The study outlined the course of the Bedford River and the Red Bedford delta. According to them, the Chatham sag, a low area between the Findlay and Algonquin arches, might have been sufficiently down-warped in Bedford time to permit a continuous belt of sediment from Ohio into Michigan. Their paleo- geographic map indicated that the Cincinnati arch was not very emergent at this time and that the epeiric sea extended well into the Michigan basin. Ellsworth Shale: On the western parts of the basin, the Antrim Shale is over- lain by the Ellsworth Shale (Bishop, l9AO). It was named by Newcombe (I933) after the town of Ellsworth, Antrim County, Michi- gan, in which it is exposed. It was described (Newcombe, I933) as a greenish gray, sandy shale with thick interbedded dolomitic lime- stone. The formation is siltier in southwestern Michigan. Sunbury Shale: The Sunbury Shale overlies the Berea Sandstone in the eastern part and the Ellsworth Shale in western Michigan. it was named by Hicks (l878) after the town of Sunbury, Delaware County, Ohio, where it is exposed. It is a distinctly black, carbonaceous shale and is usually less than 40 feet thick. Some of the earlier work on the Devonian-Mississippian formations of the basin include that of Hale (l9hl), Fisher (l953), Kropschot (I953), McGregor (l95h) based on l68 wells, and Lemone (l96h). In these studies all or some of the five formations studied by the writer were included in addition to other formations between the Traverse Limestone and the Bayport Limestone. The present study is focused upon the exact stratigraphic rela— tion between the formations which is often lost when a whole system or a considerable part of it is included in a single study. Structural Setting: Although the basinal influence was the dominant factor, other structures, both within and without the basin, influenced Paleo- zoic sedimentation in Michigan. Michigan Basin: Reported data from isopach and structure contour studies have led to the widely accepted view that the size and form of the basin have changed from one period to another. The Michigan basin is bordered in the west by the Wisconsin arch, by the Laurentian highlands in the north and in the south by the Laurentian highlands wisconsin highlands MICHIGAN 8 // ‘D E -H 22 190 Miles H 0 Z H [—2] i—‘i ‘H Fig.2. Regional structure of Michigan basin and the adjoining areas,observed on Trenton Limestone [modified after Pirtle, 1932 ] . lO Cincinnati arch which bifurcates into the Findlay and Kankakee arches (Figure 2). The northeast arm, the Findlay, maintains its northeastward course until it is separated from the Algon- quin arch by the broad low area called the Chatham sag. The sag was recognized by Pirtle (I932) but named by Kay in l9h2. Pepper and others suggested that it was probably suf- ficiently down-warped during Berea time to permit a continuous belt of sediments from northern Ohio into eastern Michigan. Lockett (l9h7) estimated the downwarp at 2,000 feet since Ordo- vician time. The Michigan basin, measuring approximately #50 miles in diameter, apparently originated in Precambrian time and existed throughout the Paleozoic period (Pirtle, I932). Cohee (l9h8) speculated that it originated as a autogeosyncline in post-Shake- pee pre-Black River time, with major movements in post-Bois Blanc pre-Salina; post-Bayport pre-Pennsylvanian; and post-Pennsylvanian pre-Red Beds. Smaller movements of local extent have also been observed. It was isolated from time to time as shown by thick evaporite sequences, but it is known to have been connected to the Illinois basin at various times during the Paleozoic by the Logansport sag (Lockett, I9h7). The sag was first recognized by Orton (l882). In I957, Green observed the northeast-southwest trending Logansport fault about seventy miles long with a displace- ment of 200 feet, thus establishing the origin of the sag. Intra-basinal structures: The Clinton sag, the Lucas-Monroe monocline and the Howell anticline are three of the other relatively smaller structures which also influenced the east-west sedimentation in the basin. The first was indicated by the Silurian isopach studies (Lemone, l96h) while the second, the northwest extension of the Bowling Green fault, was interpreted from a recorded structural drop of ISO—ITO feet within a distance of 1,200 feet (Orton, l888) and hence owes its origin, at least in part, to faulting. Newcombe (I933) was the first to ascribe the Howell anticline to faulting, when he noted that 88 feet of the section was missing on the western flank. It is highly asymmetrical and is the largest intra-basinal structure. The origin of the intra-basinal structures has been a con- troversial subject. Lemone (l96h) grouped the major theories as follows: I. Differential compaction on Precambrian highs. 2. Basin settling 3. Gliding tectonics h. Salt dome bulging It does not seem that any one of these could adequately explain all the known structural features and so a combination of two or more of them appears necessary. This view is borne out by Pirtle (I932) when he concluded: "...that the folds now known in the central parts of the basin are the results of vertical forces pri- marily active during the early subsidence of the basin, together with horizontal compression which l2 has been effective during successive periods of the deposition and structural history. In other words, it is believed that the principal folds now existing in the later sediments are controlled by trends of folding or lines of structural weakness which existed in the old basement rocks." Boundary Elements of the Michigan Basin: Wisconsin Arch: The Wisconsin arch is a broad fold whose axis trends N200W from Illinois into Wisconsin (Pirtle, I932) and probably into the Laurentian highlands. It originated in the Cambrian period (Eckblaw, I938) and maintained intermittent movements during most of the subsequent periods. Its last major movement (Levorson, 1960) occurred in pre-Upper Pennsylvanian and post-Upper Chester time. Monett (l9h8) suggested that it influenced Coldwater sedimentation. Kankakee Arch: The western bifurcation of the Cincinnati arch the Kankakee arch, serves as the conneCtion between the Wisconsin arch (to which it appears to be more genetically related) and the Cincin- nati arch. It trends NMSOW in northeastern Illinois and south- western Indiana. Pirtle (I932) suggested that the arch is pro- bably the southeast extension of the Precambrian deformation. It originated in pre-St. Peter, but post-Shakopee, time (Eckblaw, I938). The area including the present Illinois and Michigan ‘.‘._._ basins were connected to the Appalachian basin before St. Peter time (Weller, I9MO). fi—v fit-- w,—W_ W i ‘fi‘_ ‘ Laurentian Highlands: The Laurentian highlands is a positive area stretching from northern Ontario to the Wisconsin arch. Paleontological work of Martison and others (I952) has indicated the probable existence of a seaway between the basin and the James Bay lowland. This could be inferred from Pirtle’s structure contour map (I932) on which the contours change direction from a northeasterly to a northerly course on the eastern side of the Wisconsin arch. Lemone (l96h) suggested that this be called the ”Ontario Seaway". Chapter III METHODS OF INVESTIGATION Field: Except for the eleven locations (listed below) where the Antrim and the Ellsworth shales have been exposed by quarries, road, rail-, road and river cuts, all the formations included in this study are covered by thick Pleistocene or younger Paleozoic sediments and so only the subsurface methods are applicable. During the early parts of Spring I966, the writer visited most of them with a view to studying the exposures, but this was possible only at the three locations marked * below. Each exposure was measured and the lithologic characteristics recorded. Three thin sections were prepared from the samples collected at these locations (see pictures 23, 25 and 26, Plates l9 and 20). The following is a list of the locations as reported by the Michigan Geological Survey: Antrim Outcrop Locations: l. Shore and bluffs on Lake Michigan, approximately one mile south of Norwood, Charlevoix County, but in Antrim County; east side of southeast l/h section 3, T.32 north R.9 west Antrim type locality. *2. Ditch beside north-south road parallel to Pennsylvania railroad and l/h mile south of Walloon Lake Station, Charlevoix County. Near north boundary of l/h section l5, T.33 north R.5 west. 3. Pit along road leading west from Lake Cardon on north arm of Walloon Lake, Emmet County, south line of section 36, T.3h north R.6 west. Antrim/Norwood shale. 15 13%” Definition of color rgfgpgnce stanfiards of shales ,- * * td Description Streak Color . Light olive gray Medium dark gray 20 _Graylsh black shale 5Y 6/1 5YR Nh-NS Olive gray to olive Grayish black 22 Black shale black SY'u/l-SY 2/l syn N2 Olive black SY 2/l Graylsh black-black.Closer 2h Very black shale to N1 SYR Nl/N2 Dark yellowish brown, Brownish black 26 Brown shale lOYR h/2 syn 2/l Dark yellowish brown, Olive gray 5Y 3/2 27 Bluish Gray shale a litlle darker than lOYR 4/2 Grayish yellow green Grayish yellow green 28 Green shale just lighter than 5GY 7/2 5GY 7/2 Grayish yellow green Graylsh yellow green-dusky 29 Grayish green shale yellow green SGY 7/2 SGY 7/2- SGY . 5/2 ' Pale yellowish brown Medium dark gray 50 Brownish green shale lOYR 6/2 5YR Nu Dark green shale Grayish yellow green Dusky yellow green . A 51 5GY‘7/2 darker little darker SGY 5/2 - Olive gray .32 Brownish gray shale Moderately yellOWlsh 5y u l brown lOYR i/h 53 Dolomitic shale,red Pale yellowish orange ge lOYR 6/6—8/6 to dark yellowish oran— Pale yellowish brown lOYR 6/2 5h Calcareous gray shale Greenish- -light olive gray SGY 6/1- at 6/1 medium gray 5YR N5-N6 l. * 21 is intermediate between 20 and 22, 23 between 22 and 2n and 25 between 2% and 26. . Number used in computer analysis. Referred tORock Color Chart, National Research Council (l9h8). I "v l6 *h. Huron Portland Cement Company quarry near Paxton, eight miles west of Alpena, Alpena CounfiY, Michigan. North- east l/h section 30, T.3l north R.7 east. Excellent location for studying the Antrim Shale. 5. Point on Alpena-Hillman road at northern edge of Paxton quarry, Alpena County, I/8 mile west of northeast corner; section 30, T.33 north R.6 east. 1! 6. Dump pile by old gold" mine shaft on north side of a nortthest road l/h mile from Huron, Alpena County, 3 miles west of southeast corner, section 36 T.3l north R.6 east. Ellsworth Outcrop Locations: *1. Shale pit, Petoskey Cement Company, I mile south of Ellsworth, Antrim County; southeast l/h section 23, T.32 north R.8 west. Ellsworth shale type locality. 2. Abandoned shale pit, Boyne City Brick Company in north- west corner of Boyne City, Charlevoix County; southwest I/h section 25, T.33 north R.6 west. 3. Bluff on Lake Michigan shore about I mile southwest of Eastport, Antrim Coutny west of center, section l2, T.3l north R.9 west. h. Abandoned shale pit about I mile northeast of corner of East Jordan, Charlevoix Coutny, northwest l/h section 2h, T.32 north R.7 west. Laboratory: At the beginning of the investigation the writer made a cur- sory examination of about fifty wells to determine the nature and extent of the variation in the physical characteristics (chiefly the color in the shales) and mineralogical properties of the formations. On the basis of the results thereby obtained, he selected cuttings representing each rock type in an attempt to describe the shale samples more precisely and at the same time insure uniformity of description from well to well. IT The physical appearance of the Antrim and the Sunbury shales is so similar that three standards are applicable to the descrip- tion of both formations. In addition to these three (20-22, see Table 3), six additional standards were selected for the Antrim Shale because it is more variable on account of its greater thick- ness. The Ellsworth Shale had six standards (28-33) while the Bedford Shale had two (26-27), No standards were selected for the Berea Sandstone because no consistent and significant variation was observable in color. However, the sphericity, roundness and grain size were described with reference to standards on a sand grain folder made by the Geological Specialty Company, Texas. The folder consists of sand standards glued to a cardboard with all the values of each vari- able indicated. Much emphasis was laid on the binocular description of the well cuttings. During the examination, attention was paid to special peculiarities such as size of chips, observable minera- logy, apparent organic content, oxidation of the iron compounds, color and grain size, shape, roundness, stains, cement and acces- sory mineralogy were described. The relative abundance of the components of a given lithologic unit was estimated. Such a re— cord was effective in distinguishing contamination due to caving from mixing at gradational contacts. Wells were selected randomly with not more than three conse- cutive wells from the same county. The selection of the county was also random, no two adjacent counties were studied consecutively. I8 The writer attempted to see if there is a significant cor- relation between color variation and radioactive and electric log kicks. After studying about forty wells, the writer was convinced that no such correlation exists. However, these logs were utilized whenever available, to check the contacts of two formations especially when such a boundary was difficult to de— limit on lithologic basis alone. Over 500 wells were examined by the writer but only hh3 of these were later employed in the interpretation of the problem. The rest were discarded either because the record was question- able (due to improper sampling and storing by the drillers) or because it was very incomplete and there was no means of deter- mining the nature of the missing samples (such as well records). In so far as was possible, cable tool samples collected at five foot intervals were used. In some cases, however, it was necessary to use rotary drill samples as well as those collected at IO foot intervals. It was hoped that by studying each of the formations sepa- rately and relating it to the adjacent formations, a considerable insight would be gained into the changing environmental conditions that produced such complexly related lithologic units. Methods of Analyses: The writer X-rayed sixty samples to determine the clay min— eralogy as well as to see if the lithogic variation from one for- mation to another is a reflection of the changing clay mineral characteristics. A summary of this is included in Appendix I. Computer Analyses: It was earlier stated that hh3 of over 500 wells examined were utilized in the final analysis. When one realizes that in most cases, the five formations average about #00 feet thick, mostly sampled at five foot intervals, the data thus accumulated was so voluminous that conventional methods of analysis become impracticable. Hence it was necessary to venture into the realms of computer work. Two computer programs were prepared for this.purpose with the assistance of John Kopf. The first, the Envidep (Environment of Deposition) analysed the data for each well according to the for- mations and plotted a columnal section representing the variation in the lithologic characteristics of that same well. Some of these sections were later used in drawing correlation charts (Plate 2i). The resulting output data were later plotted mecha- nically by means of a second Fortran program, the Maplot (Map Plotter). Only the well locations and the variables were plotted by the computer. Contouring was done later by the writer. A description of the operation of these programs is included in 'Appendix II. The various outputs of the Envidep and a partial record of the well data are also included in the same appendix. Maps and Charts: Eight isopach, two structural and two isopleth maps and twenty- two cross sections were prepared from the resulting data. These, in addition to three structural maps taken from the literature (Cohee, l9h5 and Hinze, I963) were employed in the stratigraphic and environ- M 2O mental interpretations of the Lower Mississippian sediments. The larger scale maps are available in the Department of Geology for reference purposes. _-. - .. Chapter IV RESULTS AND ENVIRONMENTAL INTERPRETATION Post—Traverse Structural Control: The area around Clare, Isabella, Gladwin and Midland Counties was the site of maximum subsidence as shown by the isopach map (Plate 8) and the structure contour map constructed on top of the Antrim Shale (Plate 9). The basinal structure is well shown on the structure contour maps (Plates 9 and IO) where the contour lines run-concentrically around the center. Although this basinal structure was dominant, other minor intra-basinal structures, located mostly in the peripheral regions, were identifiable (Plate 9). The Howell anticline was probably active during this epoch. It trends southeast-northwest through Oakland, Wayne, Livingstone and Shiawassee Counties with a branch into Washtenaw County. It probably exerted a significant influence on the Early Mississippian sedimentation as shown by the thinness of the formations around the axis (Plates 7 and 8). The Clinton sag is a broad synclinal structure with an axis trend- ing essentially parallel to that of the Howell anticline which lies to the northeast (Plate 9). The post-Antrim structure map reflects three positive struc— tures north of the Howell anticline. The most southerly is located in St. Clair and Lapeer Counties, the second in Sanilac County, and the third is in Huron County (Plate 9). They all possess east- 2l 5W7 nH /‘ /’—\IN LIVINGSTON COUNTY. DOWNTH THE ROWN SIDE IS SOUTHWEST SEQUENCE ST CLAIR 26 The Battle Creek trough, the northern extension of the Logans- port sag that probably served as the Paleozoic connection between the Michigan and Illinois basins (Lockett, lghT), appears as a broad syncline on the Antrim surface today. It probably did not extend very far into the Michigan basin in Antrim time. Pre-Mississippian Occurrence of Structures: Most of these structures were identified on the top of Trenton Limestone by Pirtle (l932) although they were not so distinct. They are also evident on top of the Dundee——Rogers City sequence shown in Figure 5. Those in the west show an axial trend that is perpendicular to the Wisconsin and Kankakee axes while the axes of those in the east show the same relation to the Findlay and Algonquin axes. They are believed related to these larger structures and are probably the same age. This suggests that they probably originated during the Precambrian and showed minor movements thmogghout the Paleozoic. The observed structural pattern in the Paleozoic rocks closely follows that shown on the magnetic and gravity maps by Hinze (repro— duced as Figures 3 and M) which he interpreted as Precambrian. This further suggests a Precambrian origin. They are not as prominent on these two maps as observable on the writer's maps (Plates 9 and 10). A structure contour map was prepared on top of the Bedford Shale and after the recognition of the features discussed above, no irregu- larities remain that could be ascribed to erosional effects connected wfith channels, except those defined on Plate 15. Recognition of channels was attempted because other previous workers (Lemone, l96h) 27 u .9. a . . '- ’ I _. ’ ‘ u A I m . u h l— o . N E L a A H m. . C 47 m m 9 H O s C I w M N . A w .... o u w a. .u. 1 . m m _o . m w... I. A I “.1. M .I... L .\I,.Il _C W P . u. u o z m . ....: _ _ .. .11....“5. . new. .I fiwfimwwmwfimmsflwe I- n _ A. gay. n. u .65.”...- - A“... m M .. “ 28 III] [0/ ll . fl 25 -5 o -2_%' Elate 2 . Antrim : Percent Black Shale . I[Black Sh./ Total sh.x lOO]l 'L.01gxim;a. Asseez. .1955. _ f’a 29 MICHIGAN ISOPACH 50 MICHIGAN Bl MICHIGAN THICKNESS OF EL LSWORTH SHALE IN THE WEST ’ 52 ISOPACI-I THIN SUNBURY SHALE THICK thk \‘ \l\ —20— y/ , \ courouu INT. 2d ‘ no I \ WELL no . mus. N... pLAft 6 L. OLAYINKA Assea I9“ MICHIGAN I ‘P ICH IL\ mkrm m WT, CONTOUR MHES UL AY NKA ASSEEZ 966 L 3h Plate 8 Isopach : Bottom of Coldwater Shale to the top of Traverse group. ( Asseez.l966) 35 MICHIGAN STRLCTURE CONTOURS ON TOP OF ANTRIM SHA . i: FF \e..§at S: . ca . mama ......_ I n , h \ . . _. . 4. a . .. .a _ r. M. .II — . _.. .. n, ~ \. .fi._ — . . ~ . .. . .I. . . . m V v ,.. _, ,m ._ . _. ,, .. s .4. m _ . . . . u n . F D I _ II , m . u . . . m." _. , . a .. - . m m u a .ry . . 4.5.1; . v 2 . ?I W b. \\,/, /. 1 — 36 have suggested channels in the Bedford—Berea sequence in the east. The shift in the position of the Howell axis and elimination of its branch into Washtenaw County may indicate minor movements in Bedford time (Plate IO). MICHIGAN OBSEQI/ED m II N? II ~I L: 33 MAL/OI? STQUCEQ FD 5 mm M MILES L OLAYINKA ASSEEZ WELL 0 I966 'IvEEW L .. EL SHYENAW I411 W KALAMAZmOO 38 Stratigraphic Variations: Antrim Shale: The Antrim Shale is underlain by the Traverse Group and over- lain by the Ellsworth Shale in the west and the Bedford Shale in the east. In some places around the center of the state, these forma- tions are partly or totally absent and so may be overlain directly by the Sunbury. This relationship is common within a belt about ten miles on either side of a north-south line passing through the tri— state corner of Michigan—Indiana-Ohio. The bottom of the formation is marked by a gray calcareous shale which is often underlain by a very thin bed of black shale that is identical with the Antrim black shale (type 22). Hence the bottom of the formation is placed at the bottom of this black shale when it is present or at the bottom of the gray calcareous shale-~that is on top of the limestone. The Antrim is dominantly black to very black fissile, carbona- ceous shale. This dominance of the black color has often led to the erroneous assumption that it is wholly black. Other lithologic types-- mostly brown to gray--occur in addition to the black ones. The eight standards used in this study are 20-26 and 3% (Table 3 ), The non— black colors tend to be associated with thinner Antrim sections. The formation owes its dominant black color to the preservation of the organic matter which is believed to have been abundant in the basin of deposition. It occurs in all parts of the southern peninsula except where it has been eroded in the north and the southeast. It is thickest 59 STRUCTURE GOA/TOURS ON TOP OF BEDFORD SI-IALE I MICHIGAN ho in the central parts of the state and is generally over 300 feet thick between latitude MAC and ABC and longitude SAC and 85°]2'. 0n the western side of the state, the sediments are generally thin with local thick lenses. The thinning and local thickening of the formation in the west is strongly suggestive that the sedimenta— tion was controlled by the structures hitherto described (Plates 9 and IO). For example, ten patches of locally thickened Antrim sec— tions occur west of longitude 85°. Eight of these are arranged in three sets showing southwest-northeast trend (Plate I). These sets occupy geographic positions corresponding to those of the troughs indicated on the post-Antrim structure contour map (Plate 9). Be- cause of the general thinning of the Antrim in the west, the fifty foot contour interval is probably not sufficient to delineate the structure very effectively. Only three of the five anticlines evi- dent on the structure map (Plate 98) show up on the Antrim isopach map on Plate l (Berrien, Ottawa and Lake anticlines). The sediment is thin near or along the crests of the anticlines. In the other two, the relationship is not obvious, because the shale is generally about 250 feet thick and so the 50 foot contour interval is probably not sufficient to delineate them. Except for one local lens (250-300 feet thick) the Antrim is relatively thin east of longitude 8&0 and south of latitude MAO where it is generally less- than 250 feet. The general trend of the Howell anticline is obvious in the thinning of the formation on the axis and the thickening on either side. The Clinton sag is featured by a broad nose of thickening Antrim along the axis. North of the Howell hi anticline, 200 and 250 foot contours are so widely spaced that only a smaller interval would show any thinning that could delineate the position of the anticlinal structures in this area. It is about 300 feet thick in the 'thumb' area. The east-west trending anticlinal structure of Bay-Gladwin Coun- ties is observable on the isopach map by the thinning of this shale along its crest and thickening on the northern side. South of the axis, the trend is lacking. This is because the formation possesses nearly uniform thickness in these areas. North of latitude hh°30', the formation is generally thin and the contours appear as concentric bands approximating the geometry of the coast in Antrim time. Environment of Antrim Deposition: The lithologic characteristics and distribution of the Antrim Shale suggest the widespread nature of the Antrim sea. If the for- nation was deposited farther north and in the southeast of the state (where it is absent today), it has since been eroded. It was the most widespread of alllaten Mississippian transgressions. Bishop (l9h0) implied that the Devonian-Mississippian boundary be placed at the bottom of the Antrim Shale. She wrote (p. 2l51), "Evidence of erosion and weathering at the top of the limestone in southwestern Michigan further suggests a break between limestone and shale periods of deposition..." Although not defined by Bishop, the writer assumes that they include karst features, truncation of beds, residual deposits and several others. Present observations reveal no such features in the MICHIGAN 5 SH PAT/O O S BFDFORD SH. $35954 ss. ................29_ MILES L OLAYINKA ASSEEZ I966 30 E N V/PONME N TS. ____ . Afi—i—r‘r—‘i 45 MICHIGAN ISOPACI-I BEDFORD SHALE AND BEREA SANDSTONE F ROM THE TOP TRAVERSE GROUP TO SHA I. E TOP. LATITUDE 43" LATITUDE 44° SA - I’E’f" SHAL IILI Mafi: “9?: NT GR Lu U) 0: Lu > <( Q I\ 45 CROSS SECT/ONS FROM THE TOP OF TRAVERSE GROUP TO TOP OF SUNBURY SI-IAILE DATUM I TRAVERSE SURFACE HOR/ZONTAL 2 POSTANTR/M STRUCTURE SURFACE VERT. SCALE 1' PLATE 733 . 400FT. ASSEEZ o 66 SEA LEI/EL TODAY SEA [.5ka TODAY #6 ZRQIQE as: 20: wood .5. $323 .6 Stem $33 a Seem was: “83 .méom Em) mzokaZ 1m "Emmi Imfixlm QQOILQmm WZOEUMW mmomo I GRAND TRAVER g I MICHIGAN BAY I" l\\‘ i 'I I I ,1 . L? I M. A ! lND/ANAI OHIO— u' — I [ER/CONTINENTAL S 2T" -; - 2“ -.:_3.-I T53" ‘ 1' “ U V x_ - chm/m PALEOGEOLOG/CMAP EARLY BEREA TIME PEPPER [954 ARLEVO . ‘_ . ." ¥ I l I CI‘IEeoIGAN t I PLAT: I. MICHIGAN RAEEOGEOGRAPHC MAP BEDFORD BEREA DELTA FRO—DELTA @ DE_TA FRONT D/STR/BUTARIES 0 WHO WELL . M MILES ' L OLAY'NKA ASSEEZ I966 PRE SQ LIE ISLE \ LL‘L’ I \ _. __,, , 7 "_ . I1 I g u' I I , MICHIGAN I I 1 /NDE\’ MAP OF WELL LOLA-IT/ONb ‘ 'I I o B 20 30 V I WELL . I ' . L. I Plate 10 OLAYINKA ASSEEZ I966 I I I x I I as I I I \ I CI'IEBOVGAVSI W I ‘ \ I I _— I —I "' PRE s Q u E I s L E v 0 I x 33 F * I __H I I I ¢ In I I 'I I w wI ‘ ‘74 I I ~ I I I I I “ I 3| I m IoTssooI’ -27-’- ALPENAL\\\ N T a I M I 30' MONT Mutt!” I I >MORE~CY w {I : . I .199 1,, _ I u- I ’9‘ 29I ~ I W“ R- fi—I ’4 ,. , - '1’ if *1 # _I ‘ ‘25 r” . I I . - A L K A S ~.A I GRAND YRAVERS I / 25 ”33 E ‘ '2,’ 7, £200 ,,. I 1 ‘5 .ISI mg mg I ‘2 —¢ '0 __I9 a ‘ 1 . 6 s 24 I 150 ‘ k 23 3B '235 I w E ‘KFO R D M I s g A U K E EI 7 2? I m 2| v , .366 E 5; L‘ .23; 2'84; iv "7 i‘sL, ,, I, , , m.“ 7 A V 77/ 20 358I I '6). I .231 -11/ .33 mo. 20 n. 43- Q ‘ “ I c I I I - I: a: I , , ~ 5-, ~ L L‘gw NI ,_ - r ‘ €50 35/ . 356. C L A R E I Ila/1’, g; , LI’3‘7I N In,“ “I h 17 [3,, 0 S C E 0 I, 'AI *' ’16-$‘ 2’ I \' ' n ’4" :‘335’ .3.9 3U: I ’27 ’a. . :4; I . 7 I‘ .st . Z . “BI ' “7 ,ifi I. , , ' 171’ 273 ' 17}; I 272. ' 7/ \ 2 I I I ME C o s T 3 I 269 I S A ‘5 5 2‘7. 2“ I I79 § I ‘L. 7 6 5 V. I I M U N ‘I L A I u I - ~3os 7 , 7 ~ - “'.- I I ,n - 12; I , ‘ I. r. I MUS 'KEGON "3" I w a I , .1 a ' I 90'- I.27§' .2,I7 .11/ I ‘W ‘59- I ’ I LU 7 I'fog I K :1 y .51 f" 4437 7’35 _- ‘4" I 1.3; a 3554- I I I '21; - 2/ u- I 4’“ IE 4:: ' I 2 ~ I 9 c 237 7“ H 7 W 7 ,7 .120 ‘2’? I7 ‘ ,6? , ....m7 .m5 ‘ . .419 gr III ;£ E . A “I r R .388 ,/ d. ‘ fi ’0 ma; ‘407 I I . I I V 1 I / I‘ 6 II X 0 TI T A w A 3.1, 2;, 'I I Q N I A f5 6- SHIA‘IWAS.SEE I 'er II I 213 ll 2.. r I I / . 'I ' ' LI QNI, 4'06 I I 5v CLAIP I _ 2.5, I q“ 45; 4:. . ‘u . 21¢ . I 2 I .m. 445- .4” ,1 . 156 I I Mr :7 ' .104 I I ~- " I 539. ‘q ‘ '3’” 33" ‘ 31" 156 J i—I— - 7&1. 75°in 7 I ;5 40/ ' ’402 I :518 15.3 I 2 ‘C I I, ' ”7 . 13 I ;‘ 1:7 ,, ,, I; , , w I . .317 ‘ . ‘ 55 - I I . :2. '8 ’1 ‘ if...“ 4 247 - Z O A K I A II II a“ I I1] '59:, ‘I6 I - .l/J ‘ 248I MACOM "51 I ,2 I07 .3 I 4“ ‘ 25/ 1ng r “W I .. I B A R R x I I\ 2 H A M 245 . 252 \I A: I“ , . I 250 ~ I L LEGgN 5 A 1 C\ ‘ «a /6/ LIVINIQSION 5 I' I/ J A u. I“, ; I- 2“ I “a: [I I 42; IN "T" I., 7: '2‘? I 324 .I ’ I’ Is .5 .4 -e I2 . 12/ 3“ 32? I ,_ 2 I3 ‘41 I 4A5 '4 4 3 g »~ E c - a 5, “7544—13 , * '5 I‘I . ' " ' ’ ' ’ ’ 7 ’ '*' I \ J \V . gs ,, 6? Ir 7’] . 7 ’ S 434 won 4 I . 7 V7 _ 42 I a a. 2 ’ I an. I2 '91 7-? .2 "‘7 .111 y 3 .- 2,! Z L—VA N B U R E N I ”W . I? v ~ A C ” 52° ’~ ‘ 430 Q .m. y a. " ' I / I IJKALAMAZVOOI 7" W x g; W-ASH'E “Aw w A ( NE. D A N A J A so I “5 ' ‘ '" '75 3 43/ :6.‘ ”76 I 53'. /95’ :34 ‘179 I I I; m. 82 as, ‘ . ' _ ‘ I ‘ m I. ‘ ’80 ‘ 4 I / *4 I L/EZ‘JSI'DA L 5 ._.-... _.___ ___ II9 study area. Assuming an erosional bodndary, the precise position of the Devonian-Mississippian boundary is thus still unresolved, and Grabau's contention that it is somewhere within the black shale still has validity. The distribution of the black shale as shown by the_Black Shale Percent Map (Black Shale/Total Shale X IOO) on Plate 2 offers some help in the interpretation of the Antrim deposition. Although the Antrim Shale has often been described as a black carbonaceous shale, eight different types were observed on the basis of color differen- tiation. Five of these are black (2l-25), one is gray (20), one brown (26) and the eighth is a calcareous gray shale (3h). The predominance of the black component makes the use of the 'highs' less important in the interpretation of the black shale depo- sition and so the 'lows' appear to offer more meaningful evidence for interpretation. More often than not, the lower black (less than 50 percent) content is associated with, or at least close to, anticli- nal features observed on top of the Antrim Shale today. In the cen- ter of the basin, it is geographically related to areas where the overlying Bedford and Ellsworth shales are thin. As can be seen on the correlation charts (@late 2]) one type of color may be carried laterally from one well to the adjacent well which may be separated as much as 20 miles. Greater distances are even possible in some other cases. But such correlation cannot be carried too far laterally. The change in lithology is therefore moderately rapid but not random and appears to have been controlled by the pre-existing structures. If the sea had been deep, one would evm' \I 50 have expected a relatively uniform color over very long distances. The relationship of the sand lenses in the Bedford-Berea delta sequence and the underlying Antrim Shale is interesting. Plates 3, h and 2 show locally thick sandstone sections corresponding to thin Bedford shale and high black shale content in the Antrim (75—100 per— cent black). This suggests one or a combination of two factors: 1. The Antrim surface was topographically low in Bedford—Berea time, possibly with local pockets, and so influenced the de- velopment of the delta. 2. The Antrim black shale environment still persisted during the deposition of the Bedford—Berea deltaic deposits and so the initial mud deposits were turned black. The dominantly black color of the Antrim Shale, the abundance of pyrite and spore cases in thick sections, the high percentage of the organic content as observed in the chemical and petrographic analyses indicate an environment that was strongly reducing. Under the microscope, the organic component often constitutes the second most abundant fraction after silt and clay particles. Although the identity of the components of these organic bodies could not be deter- mined, it is suggested that the type of environment just described-— turbid water with a soft muddy bottom, euxinic, totally or partially stagnant with only periodic wave and current action--is, to say the least, unsuitable to life, at least in abundance. It is suggested that planktonic organisms were dominant over all kinds of life during the deposition of the Antrim Shale. The dense spots of pollen sacs observed on the surfaces of most cuttings may be algal, and if this is later supported, it would also corroborate the speculation made by Fisher (l953) that an algal mat existed in this environment. V 44 44v u 5i However, restriction is not a pre—requisite for black shale deposition. Effects of Compaction: Compaction has long been recognized as a significant factor in the post—depositional history of all sediments, especially shales. Heldberg (1927) estimated that at a depth of 3,000 feet, l00 feet of freshly deposited mud would be compressed to 60 feet, while a l00 foot section of shale with eight percent porosity must have been at least l80 feet thick at the time of deposition. Hence over l,000 feet of mud must have been deposited in the basin center in early Mississippian time. Stratigraphic Subdivision of the Antrim Shale: Lemone (196A) divided the Antrim Shale into an upper and a lower unit because they show up differently on Gamma Ray logs. The writer did not observe any marked or consistent lithologic variation that could be used to define these upper and lower units. Post-Antrim Sedimentation: Facies Barrier: The apparent separation of the Ellsworth and Bedford-Berea lithologies could have been effected by five possible factors: l. A structural barrier 2. A topographic barrier 3. A lack of sedimentation h, A hydro-dynamic barrier v,‘ fl m 52 5. An environmental barrier The fifth factor is the most acceptable one. Section two of PJate 13 shows no positive structure in the region where the three formations are absent. Section l of the same plate also shows that the Antrim Shale is very thick with a relatively fiat surface. It is concluded therefore that the barrier was not structural. It is difficult to see how the unconsolidated, jelly-like Antrim mud could have stood up as a topographic ridge during the deposition of the succeeding sediments. Hence no such ridge is believed to have occurred. The westward thinning of the Bedford-Berea sequence is a function of distance from source area and one may argue that its apparent absence in the barrier area was due to lack of sedimen- tation. The same argument is discredited by the observation that the Ellsworth Shale attains such great thickness within a short distance from the west coast of Michigan. if waves and currents occurred in these regions, they could only have been minor and periodic and so could not have been so restrictive as is observed today. it is also difficult to pic— ture the occurrence of such hydrodynamic factors, with limited north-south and east-west extent, in the center of the basin. The writer believes that as the terrigenous sediments were being brought into the basin, they were turned black by a very reducing environment that occurred during Antrim deposition. Progressive sedimentation overcame the effects of this black 53 shale environment which was being pushed basinward on both sides by deltaic sediments. Such a progressive displacement accounts for the obgerved interfingering relation between the Antrim shale and the succeeding formations. With a decrease in the rate and amount of sedimentation in the barrier area, the black shale en- vironment persisted and all sediments deposited there were turned black. The black shale environment was dominant throughout the de- position of the Antrim Shale. At the end of this deposition some movements occurred that changed the pattern of sedimenta- tion in the east and west while black shale deposition persisted in the center. The nature of the movement is uncertain but its end result was an increase in the relief between the basin floor and the adjoining uplands. it could have been due to contemporaneous uplift in the Wisconsin and Laurentian highlands, but it seems that subsidence in the basin is a better explanation. It is also the easier explanation and is capable of producing the observed concurrent change in sedimentation on both sides of the basin. The poi-Antrim conditions were ideal for the development of the Bedford-Berea delta in the east. The brown shale was depo- sited gradationally on the Antrim Shale in the east as the first indication of the delta. This brown shale might have been the western extension of the Ohio Bedford-Berea delta into Michigan. In the west, rapid sedimentation of the Ellsworth Shale v 5h resulted from this downwanp of the basin. The Ellsworth-Antrim transition zone developed as the green sediments were being trans- formed to black and geenish brown in the black shale sea. .With continuing Ellsworth sedimentation, the black shale environment was progressively pushed basinward. Farther east, around the facies barrier, the black shale environment persisted over the green and bluish gray environments and so all sediments deposited here were turned black. Around this facies barrier (Plate 93) the identity of the Bedford or Ellsworth shale is lost and the Sunbury Shale rests directly on a similar black shale interpreted as the Antrim Shale (Plate l8). Ellsworth Shale: The Ellsworth Shale appears near latitude 85° and thickens westward- as the underlying Antrim Shale thins. This correspon- dence indicates an eastward displacement of the black shale environment. The blackest Antrim (75—100 percent) occurs where the Ellsworth Shale is relatively thin and the Antrim Shale is relatively thick. This suggests the transformation of the green into the black sedi- ments. The two formations are separated by a transition zone which also thickens west and where the two lithologies are mixed in varied proportions. This zone is believed to be more related to the Ells- worth Shale. The Ellsworth lithology is typified by the exposure near the town of Ellsworth, Antrim County, Michigan. Here the exposed shale is grayish green and sandy with thick interbedded dolomitic limestone. The writer observed about 30 feet of exposuren-hostly ———-—»--4.~—~’ v _' .— «MA J '55 Benzie exford Osceola Dolomite,calcarv -ous Limestone,dolo- mitic Ooolitic Lst. and dolomite. Oil and Gas Development . [MGS 0&G Summa- 593’: 1961* J /mth ”mucoN_Lo: "Enumo o _ o m a xoo_ ” :o_umeommmxo _mo_ucm> .0__E m\A :_ u m_mom _mu_uem> .mm__E om :_ " 0—mum _mucoN_co: ..7. ill ’ {.f \l’) i i, i 2 l 7 > 5 57 calcareous--with a thick bed (l-3 feet) of dolomitic limestone (slides23 and 25). Six color variations were noted in the for- mation (28-33) although the green varieties (28, 29 and 3i) were dominant. Towards the center of the state, around the facies barrier (Plate 98), the dark greenish brown variety (type 30) is the most abundant Ellsworth lithology and accounts for some of the difficulty in assigning the rocks of the "masked zone' into appropriate formations. It also records the attempt of the black shale environment to turn the green sediments black. The Ellsworth Shale averages 500 feet thick in most places in the west, with a maximum of about 550 feet in two lenses north of latitude MAO. This thickness indicates the proximity to the source area. The isopach map is the most complex of the five formations and reflects the degree of influence exerted by the structural features shown on plates 9 and 9B. Near the pre- sent-day coast of Lake Michigan, the isopach lines follow the trend of the anticlines fairly closely, but farther basinward, the basinal control was dominant. The irregularity of the eastern boundary of the formation indicates the extent to which the formation had been turned black by reducing conditions pre- vailing in this area. The Ellsworth Shale thins towards the center of the basin with a general southwest-northeast trend. North of latitude hho it occurs as far east as longitude 83030“ (Crawford, Roscommon and Otsego Counties) where it intertongues with the Bedford Shale. A similar relationship occurs farther south around the border of V— w-v—ia—fi . 58 Eaton and Barry Counties (Plate 7). The eastern limit of the formation is marked by a north-south line passing through the tri-state corner of Ohio, Michigan and lndiana. The writer suggests that any shale occurring east of this line and at the same stratigraphic horizon as the Ellsworth should be called Bedford Shale. The restriction of the Ellsworth and the Bedford shales to the western and eastern sides of the basin respectively, was effected by an environmental barrier herein referred to as the facies barrier. However, this restriction was not complete as can be seen on Plate 7. It appears that this environmental barrier had a northern and a southern limit. A greater rate of deposition due to proximity to the source area and the influence of the western structures (see Plates 9 and 98) may be factors account- ing for the suppression of this barrier. The structures are marked by thinning of sediments along or near the anticlinal axes and thickening (mostly in lenticular forms) in the troughs (Plate IS). The Berrien anticline was responsible for the southwest—northeast linearity in the south and probably was one of the factors responsible for preserving the identity of the Ellsworth Shale where it intertongues with the Bedford. At the close of Ellsworth deposition a sequence of inter- bedded shales, limestones and dolomites were formed in the western parts of the state. This sequence is finally overlain K a... ’V ~—-"——v—-‘ Wgeef 4—? ' \ 59 by green shale and in some places by the Sunbury Shale near the facies barrier. Hale showed the approximate distribution of these carbonates in her work (l9hl, p. Tl6). This study confirms her observation except that the carbonates are more widespread than she showed. They are observed as far east as the facies barrier area although such occurrence is less significant. The beds are thicker and greater in number near the west coast of the state and decrease eastward. The occurrence of carbonate beds elsewhere within the formation makes it impracticable to draw a carbonate isopleth map. The limestone is gray to dark gray and dolomitic while the dolomite is brown, calcareous and weathered in places. Both limestone and dolomite are silty and sandy, but the occurrence of sand grains is not limited to them. The two carbonates are separated by a zone of oolitic lime- stone and dolomite in Barry, Kent and Ottawa Counties (Plate 17). The oolites are perfectly spherical, and although the writer did not study their internal geometry, Hale (l9hl, p. Tl9) reported: "They are composed of concentric layers of buff colored limestone with central cores of crystals--many of perfect rhombs-—of brown dolomite." The sand grains are fine to very fine—grained, sub-angular and frosted. Hale (l9hl, p. 7l6) wrote: ”It seems highly pro— bable that they are wind-Blown from some sandstone formation cropping out in the southwest.” if the proposed deltaic origin is correct, the presence of sand may indicate the proximity of b. V“ 60 the boundary between the delta front and the pro-delta areas. Geologic and Environmental Interpretation: .All previous studies on the Ellsworth Shale (Bishop, l9h0; Hale, l9hl; and Lemone, l96h) suggested that the source area for this formation was north and west. The writer sees no evi- dence from his work in support of a northern source. If there was indeed a significant source area in the north, it seems reasonable to expect that: l. The Ellsworth Shale should occur in most places in the northern parts of the state west of longitude 85°. 2. The sediments should be coarser to the north (as they are in the west). 3. The thickness in the north should approximate that in the west. A. Some degree of linearity should be observable in the north. None of these conditions is satisfied by the writer's observa- tion (Plate 5) and so the northern source appears discredited. Local land areas might have occurred in the northern parts of the basin.in Ellsworth time and hence the absence of the forma- tion. Even if there were no such land areas, one is certain that deposition of the Ellsworth in these areas was very thin. Such a deposit has since been eroded. If a thick section had been deposited here, it is difficult to see why erosion could have been so effective that it left no patches of the shale here. If erosion had been that effective, its influence would be recorded on the Antrim surface. Hence it appears that the previously postulated northern source of the Ellsworth is ques- 6l tionable and a revision is in order. It is natural to think that at least part of the sediments in the basin had a source in the Precambrian uplands to the north. This may be true, but any sediments derived from the north during Ellsworth time must have been minor and of no consequence. The northwestern source, on the other hand, is supported by all these features. The southwest-northeast linearity of the isopach (Plate 5) is structurally controlled and is probably one of the factors for the interfingering relation of the Ellsworth- Bedford-Berea in the south (Plate 7). The green color of the sediment has been ascribed to ferrous ions by these same workers. According to Hale (l9hl, p. 7l6): "The green color of this shale was no doubt derived from the iron-bearing areas at the north either in primary deposition or by later reduction of the ferric, to the green ferrous sediments.'I It is the opinion of the writer that several factors pro- duced the green coloration of the Ellsworth shale. Important among these were the abundance of green varieties of clay minerals, chiefly glauconite, as well as the abundance of fer- rous ions and the scarcity of organic matter. The geology of glauconite and pyrite in recent sediments (Challenger Expedi- tion, l89l; Krumbein and Garrells, I952) supports this view. It is therefore concluded that a mildly reducing condition, the formation of abundant green clay minerals and ferrous ions and the lack of preservation of organic matter were the factors responsible for the dominant.green coloration of the Ellsworth Shale. Local and periodic oxidizing conditions are indicated _ -. ..-....—— w 62 by the changes to dolomite and limestone in the formation. The abundance of pyrite was nowhere comparable to that of the Antrim Shale. A strongly reducing environment would have pro- duced an abundance of pyrite in this formation as it did in the Antrim. It was earlier stated that the Ellsworth is strictly marine with a well defined source area to the northwest. Very little information is available on this formation outside Michigan. The Milwaukee Formation is the only Upper Devonian (7) unit exposed west of Michigan. It is a poor exposure in the vicinity of Milwaukee and so offers little supporting evidence in the interpretation of the Ellsworth Shale. Alden (I906) described the Milwaukee Fermation as follows: "Only lower l5-25 feet exposed but (the) following generalized section is based on exposures and well records (descending): black shale, IS feet; soft bluish magnesian limestone ('cement rock‘); 12 feet; bluish limestone and softer bluish 'soapy clay', 3i feet. Very fossilifereous Hamilton fauna. Overlies Waubakee formation, underlies Pleistocene drift. Named for exposures near Milwaukee." In spite of this limitation the writer believes that the pattern of Ellsworth sedimentation is so similar to that of the Bedford-Berea sequence that a deltaic origin is suggested. The evidence for this supposition is: (i) Its interfingering relation with the underlying Antrim and the laterally equivalent Bedford-Berea sequence; (ii) Occurrence of sand and carbonates. It is therefore concluded that a delta probably occurred in the west as it did in the east of the state. The Ellsworth Shale '_V fiA—v—fi J ' \u—ny, 63 could represent the pro-delta sub-environment of this delta and the occurrence of sand grains near the west coast of Michi- gan.would suggest the proximity of the delta front. -Subsequent erosion has removed all evidence for this delta. .The present basin of Lake Michigan may contain some of the sand bodies of this delta. The difference observed between the Ellsworth and the Bed- ford shales was a function of the difference in the.geography of their basins, source areas and types of sediments supplied, Bedford Shale and Berea Sandstone: Although the distribution and lithology of the Berea Sand- stone are here described independently of the Bedford Shale, it should be realised that the two formations form a genetically related unit whose separation is only for convenience. The contact is often represented by a sequence of interbedded thin shales and sandstones and where one places the contact is a matter of personal discretion. The difficulty of placing the contact may be illustrated with well lh9 (T. ISN; R. l2E, Sec. 32) in Huron County: Please see table on following page. -' Nvfi‘w ‘TF. M. fl/ ~fif’“ ‘ E P "I c "o N T I N E N T A L :4 —/ 1‘1 =l 2 El —-I a :\ ‘—'\ ——\ :3 :I 6h Fig.6 . Paleogeographic map ,Early Berea Time [modified after Pepper, '51l] Shore line [Asseez] Shore line Pe r Bedford:~ 'rea \' .ltBJCAfiSe z) ‘\ \L_\ ,7"—"0HIo BA'Y " _V N M. “,q‘ N‘s 65 ' Depth §i ill lhO6-lhl5 f.g.ss. 90% 1070 Ihl5-lh23 f.g.ss. 85io 1502o lI-i23-ll-130 v.f.g.ss. 9502, 5% .lI-I3O-II-II-I2 v.f.g.ss. 85?, 15% 11111241150 v. f.g.ss. 9002, 10?, “150—11159 v.f.g.ss. 90% IO% 11159-11167 v.f.g.ss. 9842. 242. lh67-Ih80 v.f.g.ss. lOOQQ .l1180-l1188 v.f.g.ss. 85% IS”), “488-.“492 v.f.g.ss. 90% IO% 11192-1502 v.f.g.ss. 100?” 1502-1552 siltstone 90% 10% ggdford Shale 1552- 1708 10?» 90?. Antrim Shale l708-l898 black shale l598-l9l8 brown shale I9I8-l958 85% black shale liagray calc. shale All the other descriptions have been left out of this summary. The shale component of the Bedford-Berea sequence is about I68.6 feet (56%;) while the sandstone is about 13l.9' (twat). This gives a sandstone/shale ratio of 0.783. From the above figures the difficulty of marking a contact becomes obvious. For working pur- poses, the writer selected the first appearance of a dominant and consistent shale section as the Berea-Bedford contact. It should be re-emphasized that this is for working purposes alone. The formations are intimately related and should be treated as parts of a single unit. The Bedford-Berea isopach map (Plate l2) shows a regional 11.. -vfi _. 66 southwest-northeast trend and also has a triangular shape with apices in Huron, Lenawee and Iosco Counties. The maximum thick- ness of about #50 feet is attained in the region of well number I55 (Plate l6). The surface gradient of the sequence is gentle from this region as far west as longitude 8h° where the gradient becomes steeper. This change in surface slope is interpreted as representing the change from delta front to the pro-delta environment. The noses seen on the Berea-Bedford iSOpach map are similar to those obtained for either of the formations and indicate external control. The trend indicates that the source area was to the northeast. Bedford Shale: The contact between the Bedford and the underlying Antrim Shale is marked by brown shale (type 26) which usually averages about 25 feet in thickness. The bottom of the Bedford is placed at the bottom of this shale. A great thickness of the brown shale was observed in some places. When the difference in the expected and observed thickness approached 50 feet, it was con- sidered that this abnormal thickness represented errors in the sampling. Such occurrences were small in number and erratic in distribution. The brown shale is thicker in the east and disappears into the bluish gray lithology farther basinward. It represents a gradational change of the black shale environment into the blu- ish gray type (Figure l3). The shale is typically bluish gray (type 27). It is gene- V W. 67 rally silty and in most cases sandy in the upper parts espe- cially in the east. The formation is restricted to the eastern side of the basin where it controls the trend of the thicknesses of the Bedford-Berea sequence (Plate 12). It occurs in its typi- cal form In the area east of longitude 8h° and becomes diffi- cult to distinguish from the overlying sandstone progressively westward where the latter occurs as very fine sandstone, silt- stone and clayey siltstone--mostly gray colored. The distribution of the formation (Plate 3) is very similar to that of the Bedford-Berea sequence (Plate12). The northeast- southwest trend is very prominent and is the one that controls a similar trend on the Bedford-Berea isopach map. The thickest section occurs in the 'thumb' area and the anticlinal axes are marked by the thinning of the shale near or along their crests. Its western limit is irregular, and appears to have been con- trolled by the intrabasinal structures and the facies barrier. Berea Sandstone: This formation occurs in the same general areas as the Bed- ford except that its western extent is more limited. Its uppb} parts in the east are often rich in Iimonite which is probably due to the oxidation by ground water. The observed sand grains are subrounded and well sorted, indicating a probable second cycle sandstone and/or long transport. Shale partings and beds of the Bedford type occur interbedded with it and the transi- tion between the two is marked by alternating beds of sandstone and shale. The sandstone is often, if not always, very fine- 68 grained. The medium-grained variety which has been described by Pepper (l95h) in Ohio was not observed by the writer in Michigan. This formation thins westward until it is hardly distinguishable in bedded form west of longitude 8u°. Wells l3h and I37 show the typical lithologic makevup of the Bedford Shale-Berea Sandstone sequence in this area. In the first well, ten feet of sandstone, silty, very fine-grained, overlies 35 feet of shale. The second well shows no sandstone while the shale is 5h feet thick. This well is located about 20 miles northeast of the first (Plate l6). They are both located in the pro-delta area (Plate l5). Cohee (l95l) recognized three members in the Berea Sandstone: l. Lower unit of light-gray, fine-grained, dolomitic sandstone, cemented with silica and dolomite. It is micaceous and pyritic. 2. Middle unit of friable sandstone, fine-grained, inter- bedded with shale. Its grains are subangular. 3. Upper unit similar to the lower unit, but less shaly and less pyritic. “ Although this type of variation was observed by the writer, such well-defined members were exceptions rather than the rule and so such a division of the Berea into members is not recommended. Calcite is the dominant cement in the formation and silica is even less significant than dolomite. It is generally true, however, that the middle section is often friable to such an extent in some places that they have been disaggregated into individual grains by the drill. Other cementing agents observed by the writer are ferric minerals--chiefly Iimonite. 69 Generally the lower contact of the Berea Sandstone with the underlying Bedford Shale is marked by interbedded shale, silty sandstone and sandy siltstone. This is in turn overlain by a section of clean, well-sorted, white, fine-grained sandstone. On t0p of this is a section of fine and very fine-grained sand- stonee-most often subequal--but in some cases dominantly very fine-grained. Each of these sections contains partings and small bands of Bedford type shale. The top exhibits a grada- tional contact with the Sunbury. This contact is often easy to recognize on a lithologic basis. The Berea Sandstone is a blanket deposit with local thick lenses (Plate h). The thickest section occurs in the ‘thumb' area (Huron County) where it reaches a thickness of about 200 feet. Elsewhere it is generally less than 50 feet except where patches occur in which the thickness may be as much as ISO feet. The patches are interpreted as offshore bars and apron sands of a deltaic system. Some show a distinctive branching pattern (Plate h, latitude M2O3O', longitude Bho; latitude A39, longi- tude 83°; and latitude hho, longitude 8h0). They are oriented at steep angles to the source direction. The same pattern shows up very clearly on the sandstone/shale ratio map (Plate II). The bars are bounded by very argillaceous sediments both late- rally as well as vertically (Plate II). The textural composi- tion of the patches is fine and very fine sandstone with an underlying Bedford Shale. A significant relation that will be discussed further at a later stage is the association of the Vflfiy—V-vv~a "WI!— ,.._——qfi—_ . ~_\‘—_'_-\’_‘u __ ’1 70 thick sandstone lenses with thin Bedford Shale in places where the Antrim is blackest. The upper parts of these lenses are silty. The central portion is clean sandstone, very dominantly fine grained. The lower portion shows a gradational contact with the thin Bedford Shale--the contact being silty to argil- laceous--with distinct interbeds of shales and very fine-grained sandstone. The two dimensional geometry of the sand bodies is best shown on the cross sections in Plate lh. These sections show a general thinning of the formation in the basinward direction. The bodies show a flat surface and a downward convexity. This convexity indicates the sinking of the sand bodies into the underlying mud at the time of deposition. It suggests the bar nature of these sand patches. A channel-fill explanation is not tenable for these sands (except where channels are defined on Plate l5). .Apart from the lenses interpreted as bars, the sandstone occurs as a blan- ket. If they were due to channel-filling the trend of these channels would be marked with linear sand bodies parallel to the direction of the river flow. A structure map was prepared on top of the Bedford Shale to see if channels could be identi- fied. Plate I0 shows no such channels. One could probably ar- gue the existence of a small one in Iosco County, but this does not seem probable in view of the observed depositional charac- teristics. The lithologic character of each formation may be seen more clearly by quoting some well records located in some of these supposed bars: Well No. 382 (Plate I6) is located in the bar in Saginaw County and a summary of its record is as follows: 1875-1906 f. g. 55 v.f 9. ss 90%, IOQD sh 1906-1918 55 as above 7500 25%? 5h l9l8-l930 55, f. 9. red 989g 2?. sh 1930-]9h2 white f. g.-v f.g. ss 95% 5% Sh 191,2-1956 f.g.ss. red spots 70% 30% Sh 19564993 v. f, g.,ss. 9552. 5‘30 Sh 1993-2012 silty 55, v. f. g. 9590 5%» 5h 2012-2020 silty ss 60% 30% Sh 2020-2032 silty ss-sand siltstone H3% 8590 sh About ten miles south of well No. 382, No. 376 has lhO feet of sandstone--the bottom 25 feet being silty sandstone to very fine sandy siltstone. Five miles west of well No. 382, No. 38% has the following record: 21911-2200 60% ss 110% sh 2200-2220 75% 55 25% sh 2220-22110 80% $5 20029 sh 22110-22116 5%» $5 90420 sh 22116-2260 50% ss 59% sh 2260-22711 60% ss 110% sh 22711-23l16 85% ss 15 “lo sh 23L16-23511 , 10% ss 90% sh The shale is bluish gray, calcareous. The sandstone is fine- grained, silty near the middle and micaceous. The marshy nature of the area around Huron County, during the deposition of the Bedford-Berea sequence, is reflected by the lithologic character of the samples from the three wells: Nos. l5l, l5h.and I57 (Plate l6). The sandstone in well No. I5h at a depth of 830'-870' is dark colored, indicating the influence of organic matter prevalent in this environment. Pyrite indicates 72 the presence of a reducing environment at the time of deposition. Red Spots present are interpreted as later oxidation of part of the pyrite by ground water action. Some interesting features are noticeable in well No. l57 in which the upper l8 feet are a shaly sandstone (90%,sandstone and l07éshale). The sandstone is dirty white, calcareous and micaceous. The underlying 60 feet are composed of six alternating bands (subequal) of light and dark-colored fine grained and very fine grained sandstone, both of which are slightly silty. The dark bands are brown, reddish, calcareous, shaly or silty. The light-colored bands are clean. Well No. l5l is similar to No. I57 except that the sandstone is not banded. Petrographic examinations reveal a small suite of heavy minerals, the most common being.zircon and tourmaline. Other accessory minerals observed include garnet, apatite, mucovite and hornblende. The non-quartz minerals generally average about l%>in most thin sections. Occurrence of hornblende was erratic. This heavy mineral suite offers no aid in the source or environ- mental interpretation. The birdfoot geometry of the delta is well defined by the sandstone/shale ratio map (Plate II) on which the logarithmic scale has been used. The highest ratio is hz8. About 50 per- cent of the Berea Sandstone subcrop area is covered by sandstone and shale in which the ratio of sandstone to shale is less than 0.5. About 25 percent shows a ratio of 0.5:l; 13 percent for I22; l0 percent for 2zh; and 2 percent for #:8. Most of what has 73 been defined as the pro-delta environment (Plate l5) shows a ratio of less than 0.5. The geometry of the bars is well shown on the same map. The bars are oriented almost at right angles to the source direction and can be used to predict the relative position of the shoreline during the deposition of the Bedford- Berea sequence. The dotted lines and blank Spaces on the map indicate areas where control is lacking. Plates 3, h and I2 show that thick sandstone sections cor- respond to locations of high black content (75-l00 «) of the Antrim Shale and thin sections of the Bedford. This is signi- ficant in that it indicates that the Antrim surface was probably topographically low in Bedford-Berea time and thus influenced the devel0pment of the delta. Several lenses showing the rela- tion may be observed on the maps (Plates 2 and h). The lens on the southwestern side of Howell anticline coincides with a small patch of high black shale percentage. Another lens defined by the loo foot thickness line around latitude h2O3O' and longi- tude 8&0 lies mostly in the 75-l00 percent pattern. Environment of Deposition: llmafOregoing description oFthe lithology and distribution of the Bedford Shale and Berea Sandstone indicates a deltaic origin, the sandstone occurring as bars in places. Other cri- teria which may be re-emphasized here are: l. The underlying Bedford Shale grades upwards into silty shale and argillaceous siltstone. 2. The sandstone bodies were built by coalescing apron sands. 7h 3. The birdfoot geometry shown by the sandstone/shale ratio map and evident on the Bedford-Berea isopach map (Plates I2 and II). M. The higher abundance of the siltstone and shale, often approaching 65 percent of the total section. 5. Recognition of the deltaic sub-environments similar to those seen in modern deltas. 6. The distributary channels that tranSported the sediments into the basin. These are defined by the sandstone/shale ratio and are shown on Plate l5. If the present is truly the key to the past, one might look at the features of modern deltas and see if some of the charac- teristics in them are observable in the Bedford-Berea delta as defined in this report. Review of literature on modern deltas indicates that this is the case. The reader is referred to such articles by Bates, I953; Fisk, I955, l96l; Moore, I966; Van Straa- ten, l96h; and Scruton, I960. These papers contain adequate in- formation on the stratigraphy, geometry, despositional charac- teristics and theory of formation of modern deltas that are not discussed herein. The distinction of the various sub-environments (pro-delta, delta front and intra-delta) have been made from PlatesI2, 3, h and II and are shown on Plate l5. The change from the delta front to the pro-delta is marked by the change in gradient seen on the Bedford-Berea isopach map (PlateIE). This corresponds with the 50 foot thickness line on the Berea isopach and the two features have been used in interpreting the boundary between the pro-delta and the delta front. The predominance of shale (Plate II), the occurrence of organic matter in the sandstone, 75 and abundance of pyrite have been used as the major criteria for distinguishing the marsh sub-environment and hence the shore line. It is also in this area that some linearity is shown by the sand bodies and the high sandstone/shale ratio patterns. They are interpreted as being associated with the 'dying' ends of the distributaries that transported the sedi- ments into the basin. The dispersal center of the delta as well as most of the intra—delta area are not within the limits of the state and the study area. They are related to the Bed- ford-Berea delta of Ohio and may be the more western extension of the same. The sands of the delta front are cleaner than those of the other two sub-environments due to winnowing and redeposition. They are typically fine grained and very fine—grained sand- stones with some siltstones, and grade laterally and vertically into clayey silts. The sand bodies show three typical zones: l. Upper silty sandstone and sandy siltstone 2. Central clean sandstone, fine grained to very fine grain- ed with less than 20 percent silt and little clay. 3. Lower siltstone, sandstOne and clayey siltstone. Lami- nae of plant remains are common in them. The pro-delta area lies in a more seaward area of the delta front and is the site of fine clastic deposition--about 75 per- cent of which consists of clay and silt particles. It is com- posed of siltstone and shale with little sandstone near the con- tact with the delta front. Mixing of siltstone and shale was probably due to the flocculating action of the sea water on the " 76 colloidal clay particles so that they settled with the coarser materials. The rate of deposition decreased basinward. A re- view of the petrographic information included in Plates I9 and 20 confirms the deltaic interpretation of the Bedford-Berea se- quence and is in agreement with earlier interpretations both in Michigan (Cohee, l95l) and in Ohio. At the beginning of the Bedford-Berea sedimentation, the mingling of fresh and salt water reduced the stagnation that characterized the Antrim desposition. The bluish gray shale was deposited on top of the earlier brown shale that separates the Bedford from the Antrim Shale. The condition was mildly re- ducing and hence the preservation of the dark color of the mud that was deposited in it. The Bedford-Berea deposition was restricted east of the bar- rier except at the two areas where it interfingers with the Ells- worth Shale (Plate 7). The Bedford Shale samples tend to be darker colored towards the center of the basin due to the progressively more reducing conditions in the basinward direction. Its color is lighter than that of the Antrim Shale either because the organic matter was less abundant or the preservation was not as complete as in the case of the latter. The Bedford-Berea sequence is related to a similar sequence in Ohio but the exact nature of the relation is uncertain. Petro- graphic, lithologic and clay mineral studies indicate they were derived from the same source area, the Laurentian highlands. 77 Two hypotheses are possible for the origin of the deltaic sequence in Michigan: I. It is the western part of the Ohio sequence deposited laterally across the Cincinnati arch from Ohio into the Michigan basin. 2. It was deposited in Michigan by the same river that de- posited the Ohio sequence and hence is a separate, but related delta. The first hypothesis is not backed by the sedimentary record. If this had been the case, very little sandstone should be ex- pected in Michigan, the distribution of the Bedford-Berea se- quence should indicate a source to the east rather than the north- east, and finally, the red variety of the Bedford Shale--the domi- nant color in Ohio--should be commonly observed in Michigan. The red variety has been noted on well records in St. Clair County, but the writer did not observe such an occurrence. Hence it appears that this hypothesis is untenable. The second hypothesis is supported by the inferred direction of the source area (northeast of Port Hope, Michigan). The iden- tifiable distributaries are located in Huron and Arenac Counties. It is therefore believed that as a result of the post-Antrim downwarp of the basin, the Ontario River (which deposited the Bedford-Berea in Ohio) was diverted into Michigan. The di5per- sal center of the delta that developed from this river is out- side the state boundary today. The Bedford Shale is therefore the progressive forward build- ing of the pro-delta environment. The sandstone represents the peak of the delta development and the blanket appearance suggests 78 that it was formed as apron sands in the delta front environ- ment. The local lenses (Plate h) represent offshore bars. The various sub-environments (pro-delta, delta front and marsh) are defined on Plate l5. They have been interpreted from 'Platesl2, 3, h and II. The sharp gradient evident on the Bed- ford-Berea isopach map defines the change from the delta front to the pro-delta area and correSponds with the 50 foot thick- ness line on Plate h (Berea isopach map). These two factors have been employed in defining the pro-delta. The configura- tion of the delta is obvious from Platesl2 and II. The sand- stone/shale map (Plate ll) defines the position of the distri- butaries in the marsh area by elongate bodies of high sandstone/ shale ratios. The origin of the brown shale at the Bedford-Antrim contact is uncertain. The red shale deposition was dominant in the Ohio Bedford-Berea sequence. It is possible that the initial shale deposit of the Bedford-Berea in Michigan was also red and has been partially reduced by the black shale environment. On the other hand, it might have been deposited at the initial stage of the Bedford-Berea delta when the river currents were still strong and hence its greater state of oxidation. The clay mineralogy and the petrographic properties of the formations are similar for Ohio and Michigan. However, the exact age relation is unknown although it appears that the sequence in Michigan is younger than that in Ohio. The age relation of the BereaeBedford and Ellsworth is also 79 uncertain. However, their gradational contact with the Antrim shows that each is a lateral equivalent of some part of the Antrim Shale. Also the occurrence of dolomite in the Ellsworth at the same stratigraphic horizon as the Berea Sandstone may indicate partial or total time equivalence of the Ellsworth to the Bedford-Berea sequence. The Bedford Shale is the pro-delta component of the Bedford- Berea delta. -Although the sandstone is concentrated on top of the shale, they possess a gradational contact. The sequence is progressively younger in the basinward direction and so the Berea is a time equivalent of some part of the Bedford Shale. Sunbury Shale: The Sunbury Shale blankets the Bedford-Berea sequence in the east and the Ellsworth Shale in the west. Around the facies bar- rier, it lies directly on top of the Antrim Shale, with an inde- terminable contact. Its bottom is marked in the west by the first appearance of a greenish shale while in the east the first appearance of a siltstone marks the bottom of the shale. The red phase of the Coldwater Shale, the Coldwater 'red rock', lies on top of the Sunbury Shale in most places and its bottom marks the top of the latter formation. Where it is absent in the east, the bottom of the green Coldwater Shale is selected as the top of the Sunbury. The color of the Sunbury Shale is identical to that of the Antrim and hence the first three standards for the latter (20-22) were used for the Sunbury Shale. 80 Dominion of Canada LAKE SUPERIOR \ I I \ \ ‘ ‘7 N o r t h e r n g?» P e n l n S u l a Michigan ‘ North'Channel " ‘0 s $0 0‘0 V) L f e I n l \ l .19 l I o 511 / 0.20 I Indiana l Ohio qLfiEIEEQ Cl Sand Grains 0 Thin Sections Fig. 7 . Locations of samples used in petrographic analysis . \ 8l Its iSOpach map reveals a northeast-southwest trend. The maximum thickness, like the Bedford-Berea sequence, occurs in the 'thumb' area. It thins out westward with the thickening of the Antrim Shale. This thinning is even more rapid as the lat- ter in turn thins with the thickening of the Ellsworth. The two thick zones in the east are geographically related to the troughs in Huron and Sanilac Counties. Along Howell anti- cline, it is generally less than 20 feet in thickness. A simi- lar observation was made by Kilbourne (l9h7). Local thickening in Osceola and Wexford Counties appears to be anomalous and resulted from the alteration of the Ellsworth and Bedford lithologies. In the absence of these, the place- ment of the Sunbury-Antrim contact is difficult and uncertain. A thickness of 20 to 60 feet appears more probable. Geologic and Environmental Interpretation: The Sunbury deposition marked the death of the deltas and the re-establishment of a marine environment all over the basin. The continuity of the formation from the eastern states into the basin probably indicates a eustatic movement of the sea level. A thin cover of mud, derived from the same general areas as the Bedford-Berea sequence, was deposited in this sea; The maximum thickness of the formation in Huron County is compatible with this interpretation. The depositional environment was very similar, if not iden- tical to that of the Antrim Shale. The water was shallow and reducing and so the organic matter deposited was preserved. 82 Such a preservation, like the Antrim, accounts for the black color observed today. Farther west, the disappearance of the Sunbury Shale is ac- companied by the thickening of the Coldwater 'red rock‘ which occurs on.top of the Sunbury to the east. This 'red rock’ in- dicates deposition and/or preservation of ferric ions or the development of the same after deposition. It suggests that the Sunbury sea was oxidizing west of the barrier. The red shale was derived from the northwest. Petrographic and X-ray evidence suggest that, when present, the calcareous- dolomitic component is minor. The red color is due to ferric ion which might have been primary or secondary. 85 A N TP/M _ r: w" . .- -- Kr; , - a»- u- .- . FLA-E Ll‘lT 25 Pun LN" “fig LG: (, 3r a ELLSWOE’TH SHALE SUqu s~_ M101; s. to...) = i . 1:. 1-" ’ ‘-‘ . 9‘ i ‘. ~ ‘ . I. ,5 .r . - \- - . x u .‘v . - . . ‘.‘ 2‘ ‘ 0 . - -- . ‘ '. -. .7 ' ‘3 ~ I" I -- "* . ~ - 12 Pun: LL‘H" 15 x Pun: L.c.ur ‘2 xi (. W 9.9. 8 ‘0 FL“ 5 Llil' Bean 5: 2 an” H a: l 9 ”sun PL. /9. SHALES 3. SAND GPA/NS "8 :- Pun: Lunar In. 8h Petrographic Notes: Plate I9 20 Permit: 253h5 » Depth: 679'—685' Very carbonaceous black shale. The superficial nature of the organic matter makes it seem to be up to 50 percent. It is concentrated as bands in places and probably averages about l5 percent. Occasional segregation of very fine silt-sized parti— cles into patches and lenses about l00-200 in diameter orien- ted parallel to laminations. The particles in them average l/200mm. Occasional crystals of pyrite with dark, red, Iimoni- tic rims. 2l Permit: 23208 Depth: 570'-580' Black carbonaceous shale, but less carbonaceous than the above (20). Up to 5 percent coarse-grained silt particles averaging l/25 mm--often arranged around clay particles. Orga- nic matter probably about l0 percent. 22 Sample I Location 6 (see p. ) Black carbonaceous shale. Organic content appears to be about 30 percent due to its superficial nature. It is also concentrated as irregular patches and stringers. Pyrite rimmed by Iimonite. About I percent of very fine-grained quartz parti- cles, 3 percent silt particles averaging about l/25 mm. Fine shreds of biotite, glauconite and apatite. 26 Sample 3 Location (see p. ) Very carbonaceous black shale with about l5 percent orga- nic matter. Chert concretion about I mm in diameter, filled with silt particles. Clay particles are mostly quartz. Seri- cite-coated andalusite, rutile and tourmaline crystals observed but minor. b- 8% 39 Permit: lhh32 Depth: h50'-h55' Highly carbonaceous black shale. The organic matter forms an inter-lacing network in which the clay paricles are imbedded. Concretions of low-birefringent, amorphous silica (chalcedony ?) occur with abundant geodes which average about 0.06-0.l mm. across. Organic matter over l5 percent. Fine-grained, silt-siZed parti- cles of tourmaline, rutile and zircon also were observed. 23 Sample 2 Location (see p. ) Calcareous shale. Calcite content about ho percent, luta- ceous texture, average size is about l2yl, although a few grains are up to 2 . The calcite crystals are concentrated in para- llel bands separated by clay particles. The bands average l-3 mm thick. The shale is silty and minor dark brown patches of orga- nic matter occur. 2h and 25 Sample 2 Location (see p. ) Calcareous, green shale, laminated. Probably up to 30 per- cent calcite. Silty. Isolated occurence of organic matter. (The sample was collected 8 feet below 23). Sample No. 2h was sectioned parallel to bedding while No. 25 was perpendicular to the bedding. MO Permit: l8697 Depth: 970'-990' Argillaceous limestone-calcareous shale. In the nine chips examined, the shale/limestone ratio varied from A5 per- cent to 55 percent. Some irregular bodies of chert (with in- clusions of calcite and clay particles) occur in places. Orga- nic matter is about 5 percent and in some cases presents a pesudo-stylolitic appearance. Occasional Stingers of Iimonite. l5 Very carbonaceous, pyritic black shale. Organic matter over l5 percent. Very similar to No. 20. 86 ‘9 Permit: 229h5 Depth: l680'-85' Carbonaceous, black, silty shale. The organic matter is probably l0 percent or more. 5-l0 percent silt-sized quartz particles, averaging l/30 mm in diameter. Pyrite, tourmaline and leucoxene occur in minor amounts. 38 (Bedford Shale) Permit: 22l58 Depth: 830'-850' Silty shale. Silt particles mostly elongate and average 30-h0 . Sub-rounded to rounded. Roundness coefficient about hO percent (Krynine, I957). Banded appearance due to differen- tial concentration of organic matter. The organic matter is variously shaped. Some are rod-shaped and average 60'. Pyri- tic,pyrite crystals are pseudo-hedral, often with red Iimonitic rims. Sand Grains l, 2, and 3: l. Permit: l7786 Depth: l320'-l350" Location: lfi7N., R.llE., Section Ih. Fine-grained sandstone with some medium grains. 2. Permit: 2689 Depth: 1560'-1585' Locatknn'TZ8N., RLllE; Section l7. Fine-grained dolomitic sandstone. 3. Permit: l8882 Depth: 16u0'-1690' Location: T. II-IN., R.9E., Section l0. Clean, white, fine-grained sandstone. W 14*. a -.fi BEPEA SA NDS TONE L. 0- Ass“: I9“ 88 Plate 20 6 (Ohio) Fine—grained sandstone with about 25 percent medium l5 percent coarse and IS percent very fine grains. Quartz con- tent: 99 percent. Cement: silica. Grains sub-rounded. Acces- sory minerals: biotite, rutile, zircon, apatite. Local concen- tration of scricitic clay particles and some hematite stains and patches. 8 (Ohio) Bedford-Berea contact Fine-grained sandstone with up to MO percent medium-grained crystals. Quartz content: 98 percent . Clean, well-sorted. Rounded to sub-rounded. Silica cement. Accessory minerals. Tourmaline, zircon, topaz and chalcedony. 9 (Ohio) Location 7: 28 feet above base. Medium-grained sandstone, with up to 25 percent coarse- grained crystals. Mean size about l/3 mm. Silica cement (chal- cedonic). Grains are mostly tabular, rounded to sub-rounded. Accessory minerals (less than I percent): rutile, zircon, and muscovite. Occasional large patches of hematite. 1D Permit: 11u32 Depth: 1651-175' Very fine-grained sandstone, mean grain size l/IO mm; grains tabular, sub-rounded. Quartz content 98 percent Clean, well-sorted. Little clay or silt particles. Cement: calcareous and a little silica. Accessory minerals: pyrite, muscovite, zircon, tourmaline and chalcedony. l6 Permit: l9l96 Depth: composite Very fine-grained silty to argillaceous sandstone, calca- reous cement. Calcite content about 25 percent. Subangular grains, locally stained by hematite. Accessory minerals, less than I percent; garnet, pyrite, chalcedony, hematite, biotite, zircon, rutile and tourmaline. 89 l7 Permit: l753h Depth: lh5'-I50' Fine-grained to very fine-grained sandstone. Mean grain size: l/6 mm. Quartz content over 95 percent. Sub-angular to suberounded, elongate to sub-spherical grains. Calcite crystals mostly larger than quartz crystals, finely arenaceous. Occurs in irregular bodies as interstitial cement. Clay particles minor. -Accessory minerals: plagioclase (?), andalusite, tour- maline, hematite, pyrite and muscovite. l8 Permit: 2h359 Depth: 530'-5h0' Very fine-grained sandstone. Mean grain size: l/l0 mm. Up to 5 percent fine-grained sandstone (average size l/6 mm). Well-sorted, little or no clay particles. Quartz content: 97 percent . Sub-rounded. About 50 percent of the grains are sub-Spherical, the rest are elongate. Cement: dominantly cal- cite. .Accessory minerals: chalcedony, pyrite, rutile, andalu- site and zircon. 28 Permit: 1hh32 Depth: 2l5'-220' Very fine-grained sandstone with IS percent fine-grained component.averaging l/6 mm. Quartz content: 97 percent. Minor silt and Clay particles. Cement;.dominantly calcite, with a little silica. Grains are mostly sub-rounded. Accessory mine- rals: pyrite, tourmaline, hornblende, andalusite, zircon and biotite. 29 Permit: l753h Depth: lh5'-l50 Very fine-grained sandstone with 2 percent fine-grained component. Occasional interstitial calcite cement, but mostly cemented by silica and clay minerals. 5 hemptite blotches ave- raging 0.3 mm in diameter. Clay.p silt about 5 percent. Quartz content 97 percent. Sub-angular, mostly equant. Accessory minerals: biotite, pyrite, hematite, rutile and zircon. 9O 30 Permit: l9l96 Depth: 165-175l Very fine-grained silty to argillaceous sandstone. Quartz content: 90 percent . Silt-r clay particles: 25 percent Cement: dominantly calcite with a little silica. One chip strongly limy. Accessory minerals: chalcedony, andalusite, zir— con, hornblende, rutile, tourmaline, (last three being dominant. 3l Permit: 3h359 Depth: 530'-5h0' Silt particles 50 percent, very fine-grained sandstone particles 30 percent, fine-grained particles 20 percent, clay 5 percent. Fine-grained particles are su-rounded to rounded. Cement: silica clay. Accessory minerals: rutile, zircon, garnet and pyrite. 32 Permit: lhh32 Depth: 1651-175' Very fine-grained sandstone. Average size: l/lOmm. Quartz content: 95 percent . Grains are angular to sub-angular. Clean, well-sorted. Very little clay or silt particles. Cement: cal- cite, concentrated on the rims of the chips which are held toge- ther by clay with occasional calcite and silica cement. Acces- sory minerals: garnet, pyrite, biotite, tourmaline, apatite and zircon. 33 Permit: 33h0 Depth: 2282'-90' Very fine-grained sandstone. Grain size averages l/lhmm. Quartz content 98 percent. . Organic matter occurs as irregu- lar bodies and Spots. Grains are sub-angular and equant. Cement: silica and very little calcite. Accessory minerals: hematite, andalusite, glauconite, pyrite and tourmaline. 3h Permit: 18777 Depth: 760'-777' Sandy siltstone. Sand grains are very fine-grained. Silt particles are angular to subJangular. Sand particles about IO percent. Calcite occurs as aggregates and interstitial cement, mostly of lutaceous texture (about IO/l). Occasional dolomite 9] crystals. Accessory minerals: zircon, tourmaline, rutile, apatite and leucoxene (7). 35 Permit: 22l58 Depth: 830'-850' Very fine-grained and fine-grained sandstone; little silt and clay. Grains sub-rounded, equant to elogate. Accessory minerals: pyrite, topaz, rutile, apatite, glauconite, garnet and biotite. 36 Permit: 23832 Depth: l85"l95' Very fine-grained sandstone with occasional occurrence of fine-grained particles, mostly less than l/6 mm. Quartz con- tent: 97 percent . Sub—rounded. Cement: dominantly calcite with a little silica. Some spots and irregular bodies of orga- nic matter, mostly as grain coatings. Accessory minerals: zir- con, rutile, chalcedony, topaz and andalusite. 37 Permit: ll3hl Depth: 225'-2h5' Fine-grained and very fine-grained sandstone with less than 5 percent clay. Cement: silica with little patchy calcite. Quartz content: 95 Percent, mostly sub-rounded, elongate-sub-spherical. Accessory minerals: rutile, sericite, apatite, hornblende and tourmaline. bl Permit: h72l Depth: lh60'-80' Sandy siltstone. Mean size l/lh to l/l6 mm. Cement: cal— cite with silica and clay. Quartz content: 95 percent. Clay particles occur as interstitial fillings. Little organic mat- ter. Grains are sub-angular. Accessory minerals: pyrite, horn- blende, zircon, hematite and apatite. 92 82 Permit: ? Location: l9N. 3E. 3i Depth: 1728'-50' Fine-grained sandstone. Quartz content: 97 Percent. Mostly elongate to tabular. Well sorted, little clay and silt particles. Cement; very little calcite, dominantly silica. Grains are sub- rounded. Accessory minerals: glauconite, sericite, topaz, apa- tite, zircon and rutile. HELL 199 FFF‘FIFiiiiiriiririi (Ffiririiiiiitsii.r. 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HHNHNNHHNNHHHHHb-Nb m4 HMNMMNMVNVHHHNM—Hv-w- " wunmuuuww~mmm .... . . :MHHNHHNHHHHdHH-m-4u WWWWWWWWWW \<««<«««««u« HHHHFNHH»MHAHH~N‘44 IHIHIIIIIIIHHII "WMNWHWNWMW" 4. "1 IHIIHIHIIIIIIIIH "NW”HHHW a “W“ \i ‘5 \“ llllllllllllllllllll “""NWWHMWWH 4" u ‘6, {4 \E lllllllllllllllllll! u"uNNNHNHflkH44H-H>~4u \v l4 :§ ‘z lllllllllllllllllil' HHHNHHHHHkuH-fldr-(“Nr-4H * l I ‘ lllllllllllllll I ll "HWWHHW'WW"“ H "’ \! ~< llllllllllllllllllll "WHHHMW WWW" E ‘5 \3 ‘4 llllllllllllllllllll "WWW” 4WHH‘ * ~§ ‘K g 4,, lllllllllllllllllill ”HHNNNHU‘HENH ”H ”+4 t Q K ‘ . (<<<<<(<0- rrrrrrrrrrrrrrrrrrrr xxxxxxxxxxxrrrrrrnr rrrrrrrrrrrrrrrrrrrr KKKKKKKKKKFFFFFFKKFAFFFFFFFFVFF‘V‘FFFFF GRAPH/C SECTIONS SYMBOLS $ Mam Lt. Dkgr—Hrd. -‘ But... :I-. Slash. ‘2 u.s..,/. Bier: .41. ) caps/.5044 Mk. #5. < 8r. 3L Gr-Cdr. SI. 3 Ht. 5;; x4 THICKNESS é LITHOLDGY p 5‘ a ANTR/M SH, OBEDFORD 91g BEREA ssfiswsum SH. VERV." SCALE:1L/NE=IOFI I-fOR/ZSCALEISEE MAF.’ flqi/I. Dal. 3 Mfg”: ASSEEZ 66 um .44. - 2,1. am...) a Plate 213' . ——"\____.._F LOCATION MAP CHMOZJXNIQ‘HN Chapter V CONCLUSIONS CONCLUSlONS The study proved the feasibility of examining well cuttings of large-shale sequences. In addition to the thicknesses of the stratigraphic units, careful examination of the color variation within a formation proves the effectiveness of this technique. The analysis of the great quantities of data generated from such a study is greatly simplified by computer techniques. Analysis of the data suggests that the interval studied in general represents the influx of sediments into a black shale basin from two separate sources--northeast and northwest. The northeastern source was more robu5t and actually resulted in the deposition of the bird-fOOt type delta in the basin9 whereas the northweStern influx resulted only in deposition of a large mass of green shale which may be related to some deltaic sequence farther west. Both influxes were relatively short-lived and with their pasSing, the black shale environment was re-estab- lished in the basin. The devel0pment of the delta in the early Mississippian epoch may be the first indication of the later deltaic and terreStrial sedimentation in the Pennsylvanian sys- tem. The Antrim Shale represents the pre-delta stage. Its sur- face was t0pographically low and influenced the develOpment of the deltas, probably more strongly in the east than the west. The shale is dominantly black. 10h Maps and cmoss sections portraying the variation of the Bed- ford-Berea sequence strikingly delineate the deltaic complex. The fact that the Berea Sandstone exhibits a blanket nature with local thickenings serves to identify the sediment as apron sands and bars rather than the anastomosing channel deposits farther east of the state boundary. The Bedford and Ellsworth shales may represent pro-delta clay deposits of two separate deltas, in the east and west respec- tively. While the evidence for the former is strongiand more convincing, that of the latter is obscure. If this interpreta- tion is correct, the Bedford Shale and Berea Sandstone cannot represent totally different times of deposition. Thus, to some extent they are time equivalents. The restriction of the Bedford and the Ellsworth shales to their reSpecitve basins was effected by an environmental barrier where all sediments were turned black. The black shales owe their color to the preservation of the organic matter. The water was shallow. Poor circulation created a reducing acid environment and hence the preservation of the organic matter. The green shales were deposited in a mildly reducing environ- ment in which the organic matter was not preserved. The green color is due to the presence of green clay minerals and ferrous ions. The deposition of the Sunbury Shale blanket and the develop- ment of the carbonates on top of the Ellsworth in the west, signal v-7“,—fi . - l l05 the end of active detrital sedimentation and the re-establish- ment of marine deposition. These interprEtations were based on both inter-formational and intra—fonmational variations. Variations within one forma- tion are related to those within another formation. For example, the black color in the Antrim Shale is not uniform but the darkest parts are related to the thickest Antrim, These two are in turn correlated with thick Berea Sandstone and thin Bedford Shale. In the west the blackest Antrim correSponds with the relatively thick Antrim and thin Ellsworth. The same relation is true for the Antrim and Sunbury shales. Therefore it appears that the factors controlling local deposition were established in Antrim time and perSisted until the deposition of the Sunbury Shale. In addition to environmental control over sedimentation intra- basinal structures also influenced the deposition. Illite and kaolinite are the dominating clay minerals of these Paleozoic formations. Chlorite and interlayered chlorite and montmorillonite were indicated in some samples, but the limi- tation of the laboratory techniques made it difficult to deter- mine their occurrence. These results confirm the usefulness of observing color va- riations within shale masses and the feasibility of doing so with well cuttings. Such descriptions yield an enormous volume of data, but appropriate computer techniques, such as those used herein, facilitate such analyses. BIBLIOGRAPHY ALDEN, W. C., I906, Middle quonian, S.E. Wisconsin, Milwapkee and vicinity, U.S.G.S. Milwaukee folio No. lhO. ALLEN, J. R. L., l96h, Sedimentation in the modern delta of the River Niger, West Africa; in Deltaic and shallow marine deposits; pp. 26-3h. Elsvier Press, Amsterdam. -------- , I965, Late Quarternary Niger delta and_adjacent areas: sedimentary environments and lithofacies, A:A:P,G. Bull. M9, pp. 5&7-600. BARRELL, J,, I9l2, Criteria for the recognition of ancient delta de- posits, Geol. Soc. of America Bull. 23, pp. 377-hh6. BATES, c. c., 1953, Rational theory of delta formation, A.A.fitc. ’Bull. 37. pp. 2119-62. BATES, T. F. et al, I957, Mineralogy, petrogrpphy and radioactivity of representative samples of Chattanooga Shale, Geol. Soc. of America, Bull. 68, pp. I305-lh. BISHOP, M. 3., l9hO, IsoPachous studies of Ellsworth to Traverse Limestone section S. W. Michigan, A.A.P.G. Bull. 2h, pp. 2150-2162. BREGER, l. A., et al, 1955, Germanium and uranium in coalified wood from Upper Devonian black shale, Geochm. Cosmo. Acta. vol. 7, pp. 287-293. BROWN, 6., et al, I96], X-ray identification and structures of clay minerals, Miner. Soc. of Gt. Britain, Monograph l96l. BURNS, J. W., I962, Regional study of the Upper Silurian, Salina evaporites in the Michigan basin, Unpublished MJS. Thesis, Michigan State University. BUSCH, D. A., I953, PrOSpecting for stratigraphic traps, A.A.P.G. Bull. #3, pp. 2829-28h3. CAROZZI, A. V., I960, Microscopic sedimentary petrography, J. Wiley: New York, h8h pp. 106 IOT CLARK, J. M., I90h, Naples fauna, W. New York: New York State Mus. Rept. 57. Mem. 6, pt. 2 pp. l97-h5h. COHEE, G. V., I9h5, Sections and maps of Lower Ordovician and Cam- brian rocks in the Michigan basin... -------- , I9h5, Sections and thicknesses of Dundee and Rogers City. limestone, Michigan. Oil and Gas Map No. 38 U.S.G.S. -------- , l9h7, Oil and Gas preliminary map, OC AI; U.S. Geol. Surv. COLEMAN, J. N., et al., I965, Sedimentary structures; Mississippi river deltaic plain; in Fkimary sedimentary structures... Spec. Publ. No. I2, Soc. of Econ. Petr. and Mineral, pp. l33-Ih8. “ CLIFTON, H. E., I956, The carbonate concretions of the Ohio Shale, Ohio Jour. Sci., vol. 57, PP. 11u-12u. DUMBAR, C. 0., I9l9, Stratigraphy and correlation of the Devonian Vin Western Tennessee, Tenn. Geol. Div. Bull. 2i, pp.l-I27. EARDLEY, A. J., I938, Sediments of the Great Salt Lake, Utah, A.A.P.G., Bull. 22, pp. EDWARDS, I., I922, Notes on the occurrence of U. Devonian strata in Wisconsin, I92I Yearbook of the PubI. Mus. of the City of Mil- waukee, pp. ELLISON, S. P. Jr., I950, Subsurface Woodford black shale, W. Texas and S.E. New Mexico, Texas Bur. of Econ. Geol. Rept. Inv. 7, pp. I-20. FISHER, J. H., I953, Paleoecodogy of the Chattanooga-Kinderhook Shale, Ph.D. Thesis, University of Illinois. FISK, H. N., I95h, Sedimentary framework of the modern Mississippi delta, Jour. Sed. Pet., vol. 2h, pp. 76-99. -------- , 1955. Sand facies of recent Mississippi deIta deposits, hth World Petroleum Congress (Rome) Proc. Sec. 1-c pp. 377-398. -------- , I96I, Bar finger sands of the Mississippi delta: in Geome- try of sandstone bodies, A.A.P.G. Symposium, pp. 29-52. GALLIHER, E. W., I935, Glauconite genesis, Geol. Soc. of America Bull. h6, pp. 1351-1365. GRABAU, A. W., I906, Types of sedimentary overlap, Geol. Soc. Amer. Bull. l7, pp. 567-636. b. .-ififlu ——-.._..2 .-. , _. I08 GREEN, D. A., I957, Trenton structures in Ohio, Indiana and N. IlIi- nois, A.A.P.G. Bull. AI, pp. 627-6h2. GRIFFIN, G. M., et aI, I96h, Development of clay mineral zones during delta migration, A.A.P.G. Bull. #8, pp. 57-69. GRIM, R. E., et al, I9h9,,CIay mineral composition of some sediments from the Pacific Ocean, Geol. Soc. Amer. Bull. 60, pp. I785-I805. -------- I95I,.Depositi0nal environments of red and green shales, Jour. Sed. Pet., voI. 2I, pp. 226-232. -------- , I953, Clay Mineralogy, McGraw Hill Co. -------- , I958, Concept of diagenesis in argillaceous sediments, A.A.P.G. Bull.h2, pp. 2561253. GOLDMAN, M. I., I92h, Black shale formation in and about Chesapeake Bay, A.A.P.G. Bull. 8. pp. 195-201. GUTSCHICK, R. C., I9h7, Origin of bitumen in Devonian-Mississippian black shales, Geol. Soc. Amer. Bull. 58, p. II85. HAKE, I938, Geologic occurrence of oil and gas in Michigan, A.A.P.G. vol. 22, pp. 393-h15. HALE, L., I9hl, Sediments of Lower Mississippian of W. Michigan, ‘A.A.P.G. Bull. 25, PP. 713-723. HARD, E. W., I93I, Black shale deposition in central New York, A.A.P.G. Bull. I5, pp. I65-I8I. HAUN, J. 0., I958, Subsurface geology in petroleum exploration, .Colorado School of Mines, 887 pp. HICKS, L. E., I878, Amer. Jour. Sci. 3d., voI. I6, pp. 2I6-220. HINZE, W. J., I963, Regional gravity and magnetic anomaly maps of the S. P. Michigan, R. I. No. I, M. G. S. HOOVER, K. V, I960, Devonian—Mississippian shaIe sequence in Ohio, Ohio Geol. Survey, ISM pp. KAY, M., I9h8, Development of northern Alleghney synclinorium and adjoining areas, Geo. Soc. Amer. Bull. 53. KILBOURNE, D. E., I9h7, Origin and development of the Howell anti- cline, Unpublished M.S. Thesis, Michigan State University. _,H‘ .— ... v —‘AF—'—’A.-V/ I09 KROPSCHOT, R. E., I953, A quantitative sedimentary analysis of the . Mississippian deposits in the Michigan basin, Unpublished M.S. 5 Thesis, Michigan State University. KRUMBEIN, W. C., I9h8, Lithofacies maps and regional sedimentary- stratigraphic analysis, A.A.P.G. Bull. 23, pp. I233—I26I. -------- , I952, Principles of facies map interpretation, Jour. Sed. Pet., vol. 22, pp. 200-2Il. --------- and GARRELLS, R. M., I952, Origin and classification of chemical sediments in terms of oxidation-reduction potentials and pH, Jour. Geol., vol. 60, pp. I-33. -------- and SLOSS, I963, Stratigraphy and Sedimentation, Freeman and Co., 660 pp. KRYNINE, P. D., I9h0, Petrology and genesis of the third Badford sand (N.Y.-Pa.), Pennsylvania State College Min. Ind. Expert Bull. 29. -------- , I957, The megascopic study and field classification of sedimentary rocks, Tech. Paper I30, Penn. State University. LANE, A. C., I909, Michigan Miner, vol. 3, No. I, p. 9. -------- , I909, Notes on the geological section of Michigan, Mich. Geol. Survey, Annual Report, pp. 73-75. LEMONE, D. V., I96A, The Uppper Devonian and Lower Mississippian sediments of the Michigan basin and Bay County, Michigan, Unpublished Ph.D. Thesis, Michigan State University. LEVORSEN, A. I., I960, PaIeogeoIogic Maps, Freeman and Co., ITA pp. LOCKETT, J. R., I9h7, DeveIopment of structures in basin areas of N.E. United States, A.A.P.G. Bull. 31, pp. 529-AA6. LOW, J., I95I, Subsurface maps and illustrations: in Subsurface geologic mehtods, Colorado School of Mines. (ed. Leroy, W.). MARTISON, N. W., I952, Petroleum possibilities of the James Bay lowland area, Ontario Dept. of Mines, AnnuaI Report, vol. 6], pp. 1-58. MILLOT, G., I9h9, Relations entre la Constitution et Ia genese de Roches sedimentaires argilleuses, University of Nancy, vol. II, N05. 2, 3, Ll; 352 PP- IIO MCFARIAN, A. C., 1939, A.A.P.G. Bull. 23, pp. 18A7-52. MILNE, I. H., et al, I958, Effects of source and environments on clay minerals, A-A.P.G. Bull. A2, pp. 328-338. MILNER, H. 8., I962, Sedimentary Petrography, Vols. I and 2, 7I5 pp., McMillan and Co. MONNETT, V. B., I9A8, Mississippian Marshall formation of Michigan, A.A.P.G, Bull. 32, pp, 629-688, MOORE, C. A., I963, Handbook of subsurface geology, Harper Bros. MOORE, 0., I966, Deltaic sedimentation, Earth Sci. Reviews, Elsevier, Vol. I, pp. 87—I05. MORSE, M. L., I938, Conodonts from the Norwood and Antrim shales of Michigan, University of Michigan, Ph.D. Thesis. MOSER, F., I963, A computer oriented system in stratigraphic analysis, Institute of Science and Technology, University of Michigan. MURRAY, I89l, Report on the deep sea deposits, Challenger Expedi- tion. NANZ, R. H. Jr., I95h, Genesis of Oligocene sandstone reservoir, A-A.P.G. Vol. 38, pp- 96-II7. NOLL, W., I935, MineraIbiddung in system Al20 ~SI02-H2O. Neues Jahrb. f. Min. BeiI. Bd., 70, Abt. A. pp. 65-115. ’ NEWBERRY, J. 3., I870, Ohio Geological Survey Report of Progress, I869, pp. 2l-29. 1NEWCOMBE, R. J. 8., I932, Geology of Muskegon Field, Michigan, A.A.P.G. BuII. I6, pp. I53-I68. -------- , I933, Oil and gas fields of Michigan, Mich. Dept. Conserv., Pub. 38, Geol. Ser. 32, pp. I-293. ORTON, E., I882, A source of bituminous matter in the Deva and sub- Carboniferous black shales of Ohio, A. J. Sci., Ser. 3, vol. 2h, pp. ITI-ITS. PARHAM, W. E., I96h, Lateral clay mineral variation in certain Penn- Sylvanian underclays in Illinois basin; Clay and clay mineralogy, Earth Sci., Ser. I9, p. 581. PELLETIER, B. R., I958, Pocono paleocurrents in Pa. and Md., Geol. Soc. Amer. Bull. 69, pp. I033-I06h. lII :PEPPER, J. F. de WITT, et aI, I95h, Geology of the Bedford Shale and Berea Sandstone in the Appalachian basin, U.S. Geo. Surv. P.P. 259. PETERSON, M. N. A., I96I, Expandable chIoritic clay mineral from Up- per Mississippian carbonate rocks, Am. Mineralogist, vol. 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L., I95I, Probable origin of Marcellus-Ohio-New Albany-Chat- tanooga bituminous shales, A.A.P.G. Bull. 35, pp. 20I7-20h0. ROSS, C. S., I93l, The clay minerals and their identity, Jour. Sed. /~/ Pet. Vol. 1, pp. 55-65. RUBEY, I925, The geology of Russell County, Kansas, Geol. Surv. BuII. I0, pp. I-86. RUDEMANN, R., I93h, Paleozoic plankton of No. America, Geol. Soc. Amer. Memoir 2, pp. I-Ihl. SCHLEE, J. 5., I96I, "Jackpile" sandstone, Laguna, New Mexico; Geometry of sandstone bodies; Symp. A.A.P.G., pp. I3h-I50. SCHUCHERT, C., I9I0, Biologic principles of paleogeography, Pop. Sci. Mo., No. 76, pp. 59I—600. II2 -------- , I9A3, Stratigraphy of the eastern and centraI U.S.A., J. Wiley, New York, pp. 567-570. SHEPARD, F, F., I9A8, Submarine Geology, Harper Bros., New York. -------- , I956, Marginal sediments of the Mississippi delta, A.A.P.G., Vol. A0, pp. 2537-2623. SIEVER, R., 1951, The Miss.-Penn. unconformity in Illinois, A.A.P.G. Bull. 35, PP. 5A2-58I. STOCKDALE, P. 8., I939, Lower Mississippian rocks of the east-central interior, Geol. Soc. Amer. Spec. Paper 22, pp. I-2A8. SCRUTON, P. C., I960, Delta building and the deltaic sequence in recent seds. of the Gulf of Mexico, A.A.P.G. Symposium, (ed. F. P. Shepard et al), pp. 82-I03. TARBELL, E., I9AI, Antrim-Ellsworth Coldwater formations in Michi- gan, A.A.P.G. BuII. 25, pp. 72A-733. TAYLOR, J. H., I963, Sedimentary features of an ancient delta complex, (S.E. England), Sedimentology, vol. 2, pp. 2-28. THOMPSON, W. 0., I937, Original structures of beaches, bars and dunes, Geol. Soc. Amer. BuII. A8, pp. 723-752. TOWE, K. M., I962, Clay mineral diagenesis as a possible cource of silica cement in sed. rocks; J. Sed. Pet., vol. 32, pp. 26-28. -------- , I963, Variations in clay mineralogy across facies bounda- ries in M. Devonian (Ludlowville), N.E.; A. J. Sci., vol. 26I, pp. 839-6I. TWENHOFEL, W. H., I9I5, Black shaIe in the making, A. J. Sci., ser. A voI. A0, pp. 272-280. -------- I932, Treatise of sedimentation, Williams and Wilkins Co., , Md., 926 pp. -------- I939, Environments of origin of black shales; A.A.P.G. Bull. 23, pp. II78-II98, TROWBRIDGE, A. C., I930, Building of the Mississippi delta; A.A.P.G. Bull. IA, pp. 867-90I. ULRICH, E. 0., I9II, Chattanooga series with reference to the Ohio Shale problem; AM. J. Sci., vol. 3A, pp. I57-I83. VAN STRAATEN, L. M. J. U., I96A, Deltaic and shallow marine deposits, Elsvier Co., A6I pp. II3 WEAVER, C. E., I958, Geologic interpretation of argillaceous sediments; A.A.P.G., Vol. A2, pp. 251-27I. -------- , I959, Clay petrology of sediments, Clay and clay mins.; 6th Conf., Pargamon Press, New York, pp. I5A-87, -------- , I960, Possible uses of clay minerals in search for oil; A.A.P.G., Bull. AA, pp. 1505-1518. WELLER, J. M., I9A0, Mississippian border of eastern interior basin; A.A.P.G. Bull. 59. pp. 765-858. -------- , I9A8, Correlation of the Mississippian formations of No. .America; Geol. Soc. Amer. Bull. 59, pp. 9I-I96. -------- I959, Stratigraphic principles and practice; Harper Bros., 9 New York. William, H., et I95A, Petrography; Freeman Press, A05 pp. APPENDICES IIA Analytical Techniques: Sixty selected samples were X—rayed on a NoreIco diffrac— tometer equipped with a copper target. Each sample was run through atKIeast A00 of 20 at a sweep rate of l0 per minute, scale factor of I6 and a time constant of 0.6. At first both powder samples (-7AF) and sedimentation slides were x-rayed. The slides were prepared by the method outlined by Towe (I963). The former was chosen because it gave comparable (and often better) results than the latter. After all the samples had been run, each diffractogram was examined and every peak with an intensity of O.I inch or more was measured and a record of its angle, d-spacing, intensity and intensity/maximum intensity was compiled. In all cases except one, the I/Imax maximum corresponds to the OOI illite at a d—spacing of about 3.3 A0. A record of the clay mineralogy and description of the diffractograms is presented later in this appendix. Identification: Kaolinite, as a group, is generally very simple to identify. The prominent basal reflections at about 7.2 A0 (OOI) and 3.51 A0 (002) are usually consistently indicative of the presence of kaolinite. The identification of a particular member of the group is often more difficult and requires that the X-ray tech- nique be supplemented with other methods. Such identification was not attempted in this work. In some cases chlorite may be confused with kaolinite par- ticularly if the experimental technique is not adequate to re- veal the presence of the IA.2 AO (OOI) reflection. Grim (I953, p. 87) suggested that a A.7 AO reflection (003) is often suf- ficient to identify chlorite. However, the situation is fur- ther complicated by the fact that iron chlorites show weak (OOI) and (003) reflections and so are often difficult to distinguish from kaolinite. They may be identified either by heating the sample to 6000 C. or treating it with weak hydrochloric acid. Kaolinite loses its crystallinity at this temperature while the partial dehydration of the chlorite results in a higher peak of the iA A’ reflection. Illite, on the other hand, is relatively easy to identify. Only completely collapsed montmorillonite may be confused with it at a basal reflection of IO A0. However, the OOI reflection of the latter is lower than that of illite. The identification of the various types of chlorite is dif- ficult and mquires optical as well as chemical treatments. Varia— tions in the types of chlorite present are often indicated by small changes in the intensity and lattice spacings. The fine- ness of the chlorite crystals causes some of the diffusiveness or absence of some of its reflections. While most chlorites give four or five clear reflections from IA.2 A0 0.2 basal spacing, the iron rich species give weak 00l and 003 and strong 002 and 00A reflections. its IA.2 AO reflection is sharper 116 than those of vermiculite and montmorillonite, with which it may be confused. Moreover, it is not changed appreciably by heat as the others are- Finally most chlorites do not expand when treated with organic molecules. The 003 reflection was used as the major basis of identification by the writer. Geology and Environmental Indication of Clay Minerals: Grim, in his study of Paleozoic shales (1951), observed the consistent presence of chlorite and illite and the rarity of kaolinite and montmorillonite. Hence he concluded that the last two are altered to illite and chlorite after deposition. Weaver (1958), however, suggested that post-depositional altera- tion of clay minerals is minor and involves nothing more than adsorptions of cations. According to him, kaolinite is domi- nant in continental and near—shore sediments which are preferen- tially eroded, and hence its rarity. Montmorillonite, on the other hand, occurs interlayered with chlorite and illite. Noll (1951) showed, by laboratory synthesis, that kaolinite is favored by low pH and the other threexby higher pH and the abundance of K+ and Mg“ . The prevailing view appears to indicate that kaolinite forms in near-shore areas while the other three occur in more marine areas. It is the relative abundance of K+ and Mgfi that deter- mines which of the three is formed in this environment. Il7 ‘ Clay Mineralogy of Lower Mississippian Sediments: The writer's objective was to determine the gross clay mineral composition of each of the formations and see if lateral variations are observable within each formation. No attempt was made to determine the end member components of each group. The foregoing summary of X-ray properties of clay minerals was employed in the determination of the clay minerals. The reflections of each diffractogram were referred to a list com- piled from the ASTM Powder Data File. The relative abundance of each component was estimated on the convenient assumption that only the abundance influences the intensity of the reflection. This, however, is contrary to the known facts that the intensity is a function of the composition, grain size, orientation, crystallinity, abundance, and other factors. Results: Antrim Shale: Fourteen samples from eleven locations (Figure 8) were X-rayed. Nine of these were black (type 22), two very black (type 2A) and the rest were various shades of grey. Kaolinite is more abun- dant than illite in seven samples (9, 23, 26, 27, 28, AI and AA) while it is subordinate to the latter in the rest. Only four samples contain "chlorite" (8, 9, 10 and 59), and in all cases it is the least abundant of the three. They are all located in the northern parts of the state except sample 8. The four were 118 taken from relatively deep zones and so depth (from the present day surface) may be a significant factor for the formation or preservation of "chlorite". That depth may not be the only factor is shown by the sample No. 8 taken from comparable depth zone to Nos. 23, 27 and 28, all of which show no chlorite. Ex- cept sample No. 9, all the "chlorite" containing samples are black and so may indicate organic control. The Cleveland Shale of Ohio appears to be similar to this formation as all the four samples contain more kaolinite than illite and only one shows "chlorite". The Cleveland Shale samples contain more kaolinite than illite and only one of them contains ”chlorite". The Same is true for the Chagrin Shale, but it contains no "chlorite". Ellsworth Shale: Ten samples from seven locations (Figure 8) were X-rayed for the Ellsworth Shale. Five of these were green (type 28), two gray (type 29) and two (samples Nos. 29 and 57) were dark green (type 31). The tenth sample (No. 21) was brown (type 30). Only sample No. 7 shows a positive illite dominance over kaoli- nite. The same sample and No. 55 contain "chlorite". The lat- ter contains little or no kaolinite. All the others indicate either subequal amounts of kaolinite and illite (Nos. 15, 22, 2A and 21) or appear to contain more kaolinite than illite. While the non-clay component of the samples may be similar, only samples Nos. 15, 21, 2A and 29 contain dolomite in minor quantities. This is significant because dolomite occurs in the ll9 A2 0 AA 0 51° 56 °59 o 9 o 10 50 _= Miles 0 25 26 o 08 2 2 Fig.8 Locations of X-rayed Antrim Samples I20 southwest of the state. The mineralogy does not seem to vary stratigraphicaliy as shown by samples Nos. 7, 22, 15, 21, 2A and 29 in which illite and kaolinite are subequal in most cases. Sample No. 7 (790'-805), however, contains chlorite in addition to the other two. Whether this is related to the difference in stratigraphic position (compare with No. 22, II75'-ll90' which shows no chlorite) or the nature of the source area is uncertain. It is important to note, however, that the only other sample that contains ”chlorite" is located about twenty-five miles directly due east and was sampled at 630i-50'. Hence the rela- tion leads one to conclude that the "chlorite" may be related to a higher stratigraphic horizon. The more northern samples are consistently dominant in kao- linite while the southern samples contain subequal quantities of illite and kaolinite. Bedford Shale: FOur samples, all bluish gray, were X-rayed. Three of them (Nos. 11, A and 16) show illite dominance over kaolinite while the relation is reversed in sample No. 17 (Figure 9). Chlorite may be present in samples Nos. 16 and 17. The mineral association and the relative abundance appears to indicate a progressive increase in illite and "chlorite" at the expense of kaolinite in a basinward direction. The high kaolinite content may be related to the shore areas of the Bed- ford deposition. However, the expected increase in chlorite in the basinward direction is not apparent. l2i -Ellsworth Shale: Bedford Shale: Fig.9. locations of X-rayed Samples. I22 Kaolinite is dominant in all the Bedford samples while "chlorite" occurs in two of them (Nos. 11 and 12). The mineralogical association of the Ohio Bedford shale is very similar to that of Michigan except that no chlorite is ob- served in the Ohio samples. Also only one Michigan sample con- tains more kaolinite than illite. If the Bedford of Ohio and of Michigan have the same source area (which the writer suggests) the clay mineral association recorded in this report indicates that kaolinite is lost, away from the source area. Sunbury Shale: Twelve samples from the ten locations shown in Figure 10 were analysed in this work. The lithology of the samples range from gray shale through grayish black to black shale. Kaolinite is more abundant than illite in three (Nos. 25, 50 and 18) of the samples while illite is dominant in six (Nos. 30-32, 20, 3 and 12). Determination of the relative abundance in samples Nos. 19 and 35 is uncertain. Four of the samples (Nos. 20, 3, I2 and 50) possess ”chlorite". All the samples are associated with relatively high areas and except for sample No. 19, they were taken from areas where the formation is less than 20 feet thick. Kaolinite appears to be associated with more positive areas than illite. Coldwater "red rock": All the three Coldwater samples (Figure 10) contain kaoli- nite and illite while sample No. 13 contains "chlorite" in I23 mmHdem cwzwaix wo mQOHpmooq roa.wflm r ma mmHHE Om "madam housewaoo mm ome mm Om "madam kHSQGSw 12A addition to these two. This is the only sample with more illite than kaolinite. The non-clay components are dolomite, calcite and possibly hematite in sample No. 13. No calcite was detected in sample No. 60. Kaolinite increases outwards from the basin center. The reverse is true for "chlorite". Only one sample shows any sig- nificant dolomite content. This indicates that the red rock is not a dolomite as originally believed. If it were, all samples should show a high dolomite reflection. Hematite is the color- ing agent of this shale. I25 X‘Ray Data--Antrim Shale sample 2 IdEntlflcatlon d-Spac1ng l/lmax . Remarks . 9.8 6.6 Illite 001 Lith: V. Bk. Sh. 7 3.8 Kaolinite 001 . A.87 5.7 Illite 002 Permit: 23072 A.6A A.7 , . A.32 5.7 Kaolinite 110 Dépth: 1136-56' u.18 7.5 Kaolinite 111 3.50 5.7 Kaolinite 002 'max==5-3 3.28 100 Illite 003, Quartz 101 3.08 A.7 Kaolinite Ni 2.93 5.7 Sample 8 Bk. Sh. 22 13.75 3 3 Chlorite 001 9,9 22 2 Illite 001 Permit: L8653 A.15 8 9 Kaolinite 001 6.90 12 2 Chlorite 002 Depth 11201-30t A.92 9 h Illite 002 A.68 6 7 Chlorite 003 l = 9 A.3A 7 8 Kaolinite ITO max p.22 26,7 3,68 6 7 Illite 023 3.50 8.9 Koalinite 110 3.31 100 Illite 003, Quartz 101 3.18 10 Illite 113, 023 2.96 6.7 Kaolinite 002, Chlorite 00A 2.9uu u.u Illite 003 2.885 A.A Dolomite 10A ? 2.680 2.2 Dolomite 006 ? 2.55 7.8 _ _ 2.AA 13.A Kaolinite 130, 201, 130 Illite 202, I33, Chlorite I32, 203 126 100 - T i we ,0 _ -..-.. ,, .ANTRIM SHALE PERrra 18653 LOC0 “65 BLACK 514111.: __ _ .-,, ,- _,.. ,0 'SAm'PLEl 8 -.. 5F - 16 TC = 2. — — To — 10 ~ —~ — 00 ' 0° 1 ANI‘RIM SHALE PERMIT- I9|3S 6&5“. SMALI 90 ,, Lot. 2211-3111- 16 SF - 16 TC . 2 10 3'07 4.122 4,92 00 6345 ‘1th 1417.91 ,, ELLSWORTH SHALE ,, PERmr: 5506 p Ggegn SHALE °° Loc- 3m— /4w °° SF = 16 - --70 TC. " 2' 7° ‘_ 5:42 5:7 7 4.22 “fife an .745 9:9 634:7?! ———ubw—-—u-—.—‘ —--— n-Il—r' —---.. Plate22. X-ray diffraction patterns of three shale samples. [ Asseez, 1966 ] 127 Sample 9 Identification d-Spacing A6 l/ImaxXIOO Remarks Permit: 19135 3.008 35.9 2,885 15.2 Dolomite 10A ? Depth: 27601-651 2.68 A.3 ‘Dolomite 006- _ 2.56 8.7 Kaol. I30,‘I30, 201, Chlor.‘l32, 201 Loc. 22N-3W-16 2.A8 8.7 Kaolinite 13T, 200, 112 _ 2.A5 12 Illite 202, 133, Chlorite 132, 203 Lith: Gr. Bk. Sh. (2I)IA.366 A.9 Chlorite 001 +1 imestpne i395 A.9 Chlorite 001 10.5 7.6 Illite 001 . 9.9 20.7 Illite 001 '-- ~ ( 7.15 13.0 Kaolinite 001, Chlorite 002 Imaxe 9.2 5.A2 3.3 A.92 9.2 Illite 002 K0717 C A,73 3.8 Chlorite 003 A.3A 7.6 A.22 18.5 3.8 A.9 3.6 6.0 Chlorite 00A 3.51 9.2 Kaolinite 002 3.36 100 Illite 003, Quartz 101 Sample 10 ~ 1 Lith. Bk. Sh. 17.76 3.3 iA.2 A.9 Chlorite 001 Permit: ? 11,6 A.3 10. 20.7 Illite 001 :Depth: I8AO'-50' 7.71 3.3 7.1 10.3 Kaolinite 001, Chlorite 002 lmax= 9.2 55.0 8.7 Illite 002 A.68 3.3 Chlorite 003 1>1<>c 11,314 9.2 Kaolinite 1'1'0 A,22 23.9 3.91 2.2 3.83 2.2 Kaolinite 021 3.76 3.3 3.66 6.6 3.51 9.8 Kaolinite 002, Chlorite 00A 3.3 100 Illite 003 3.18 6.6 2.98 A.3 Albite I28 ..éaiple 23 ' Identification d-Spacing AU I/IméxXIOO Remarks Lithi‘V- bk. Sh- Poor Resolution .' A.IA 21.6 Permit: 23072 3.73 6.8 Kaolinite 021 , 3.5 6.8 Kaolinite 002 Depth: 1136-56 3.A7 8.1 Kaolinite 002 ? 3.28 100 Illite 003, Quartz 101 Imax=I 3 7 Sample 27 ll Lith: gr. sh. A.I8 18.8 Kaolinite Iii 3.28 100 Illite 003, Quartz 101 Permit: IBAOS 2.86 6.3 Illite 115 , _, 2.52 12.5 Kaolinite 131, 112 Depth: 1105-10 2.A92 15.6 , 2.25 12.5 Illite 221 | = 3.2 max K.>I Sample.Al Lith: Bk. sh. Poor Resolution _ A.3A IA Kaolir1ite IIC) Loc. 7N-6E 3.5 7 Kaolinite 002 3.26 100 Illite 003 ?_ Quartz 101 ? iDepth 18AA'-65' 3.16 9.3 Kaolinite II2 (K>-1) ? 129 Sample 26 fdentification d-Spacing AU I/lmaXXIOO Remarks Lith: Bk. Sh. ‘Poor Resolution 7.1 6.3 Kaolinite 001 Permit: 18A05 6.8 6.3 Kaolinite 001 A.9 6.8 Illite 002 :Depth: 10201.301 A.3 8.3 Illite III A.I8 20.8 Kaolinite III I : A.8 3.63 6.3 Kaolinite 111 max 3.51 8.3 Kaolinite 002 K7'I 3.A2 6.3 3.28 100 Illite 003, Quartz 101 3.18 6.3 _ 3.08 A.2 Kaolinite II2 2.9A 5.2 Albite 2.86 5.6 Illite 115 _ 2.5A 12.6 Kaolite I30, 201, I30 2.A92 6.3 2.A3 12.6 2.26 10.A 2,22 8,3 Quartz 200 2.1 12.6 Kaolinite 023, 0A1 2.26 10.A 2.22 8.3 Quartz 200 2.1 12.6 Kaolinite 023, 0A1 Sample 28 ‘ Lith: Dk. gr. sh. Poor Resolution A.22 Permit: 18A05 A,]2 Kaolinite 11 '3,63 Orthoclase I31 Depth: ll35'-A0' 3.50 Kaolinite 002 3.28 100 Illite 003, Quartz lOl Imax1=1.3 3.18 1.5 Albite '2,88 92.3 Dolomite 10A ? l<>l 2.52 2.7 Kaolinite 131, 112 2,A3 3.1 Chlorite I32, 203 3.A0 2.3 Dolomite 110 2.25 3.1 Illite 221 130 ,Sample 3A Identification dQSpacing AO l/lmax X100 Remarks Poor Resodution Lith: Bk. Sh. 3.5 16.7 Kaolinite 002 3.3 100.0 Illite 003, Quartz 101 Permitz2AI82 2.873 A1.7 Illite 115 :Depth: I850'-I870' 'max==l'2 |>'K Sample A2 Lith: Br. bk. sh. 7.1 2.A Kaolinite 001 (25) A.89 3.5 Illite 002 ? A.3 A.I Illite III _ Sample: 1 A.l8 16,5 Kaolinite 111 3.63 5.9 Illite 023 ? . 3.28 100.0 Illite 00A, Quartz 3.16 5.9 Kaolinite 112 ? Imax'8.5 2.96 3. Albite 2.93 3.5 Illite 113 ? 1,.K 2.8M 5.9 Illite 115 7 .. 2.53 A.7 Kaolinite 13T, 112 2.AA 10.6 Illite 115 ? 2.26 9.A Illite 22T' _ _ 2.22 u.7 Kaolinite (201, 132, 220) ? 2.1 8 Kaolinite O23 ?, 0A1 ? Sample AA, .Poor Resolution _ Bk. sh. (22) A.I8 21 Kolinite 111 3,66 Illite 023 _ Sample: 3 3.62 Orthoclpse 131 3.5 Kaolinite 002 Loc. Ohio 3.28 0 Illite 003, Quartz 3.16 A.8 Kaolinite 112 K>| 3.05 6.5 2.83 6.5 2.67 u.8 _ _ 2.53 6.5 Kaolinite I31, 112 2.AA 9.6 Illite 202, 133 I31 Sample 56 A Identification d-Spacing A” I/lmaxXIOO Remarks Lith: Bk. sh. 9.7 1.1 Illite OOI ? 6.88 5.6 Kaolinite OOI ? Permit: 22627 A.9 A.A Illite 002 ? A.5A 3.3 'Depth: 520'-30' A.32 5,6 _ A.l6 I.I Kaolinite 111 Loc. 3ON-llW-6 3.7 3.3 3,6A A.A Illite O23 Imax=-9-O 3.A8 5.6 Kaolinite 002 ? 3.28 O Illite 003, Quartz |7K 3.718 5.6 Albite? _ 3.1M 5.6 Kaolinite 112 2.99 5.0 Albite ? 2.86 7.8 Illite 115 2.67 5.6 Illite 023 _ _ 2.52 5.6 Kaolinite I31, 112 2.A3 0 Illite (202, 133) ? 2.A 5.6 _ 2.26 7.8 Illite 221 2.21 Quartz 200 2.19 Quartz 200 2. Kaolinite 023 ?, 0A1 ? 132 Sample 59 2 Identification d-Spacing Ao I/ImaxXIOO Remarks Lith: Bk. Sh. 13.75 3.3 Chlorite 001 9.8 30. Illite 001 Permit: 18697 7.05 18. Kaolinite 001, Chlorite 002 A.92 11.1 Illite 002 'Depth: 15801-95' A.68 Chlorite 003 11.3u Kaolirlite 110 Loc. 22N-IAW-IA A.20 _ 3.8 22. Kaolinite 021 lmax‘ 9.0 3.72 33 Kaolinite 021 3,68 10 Illite 113, 023 I>l<7(: 3.51 6.7 Kaolinite 002, Chlorite 00A 3.28 100.0 Illite 003, Quartz 3.20 6.7 Albite 3.16 ‘ 7.8 Kaolinite 112 2.98 Albite 2.9A Albite 2.87 Illite 115 2.68 _ 2.5A Kaolinite 13g, 130, 201 2.A9 Kaolinite l3l,_200, 112 2,55 Illite 202, 133, Chlorite, 132, 203 133 Ellsworth Shale Sample 7 Identification d-Spacing l/Imax X100 Remarks 13.75 3.0 Chlorite 00] Lith: Gn. sh. 10.1 16.0 Illite 001 7.l ll.0 Kaolinite 00l, Chlorite 002 Well: 1633 6.u9 1.0 Chlorite 002 ? n.98 6.5 Illite 002 'DePth: 790'805' h.68 h.0 Chlorite 003 u.36 6.5 Kaolinite 170 | = 10.0 4.22 nu.5 max- . 3.67 9.5 llllte (113, 023) 7 3.50 7.0 Kaolinite 002; Chlorite 00h 3.3l l00.0 Illite 003: Quartz 3.22 32.0 3.18 h7.0 3.08 h.0 2,885 8.5 Dolomite l0h ? _ 2.56 9.0 Kaolinite 130, 201, 130 2.1a 17.0 !llite (202, 133) ? Sample l5 0-9.0 Poor Resolution Lith: Gr. sh. 9.9 8.2 Illite 00] 7.l 2 Kaolinite 001 Well: 22 6.58 h l Chlorite 002 ? 1 1 A.92 3 l Chlorite 003 ? Depth: lOl0-15 h.7 3 l Kaolinite 110 H.36 7 l Kaolqnite ll0 h.3h 6 l Illite lll ? h.3 3 l 1.22 25 5 b.02 3 l Dolomite 102 ? 3.775 11 1 3.70 6.1 Dolomite 102 3.51 M.l Kaolinite 002; Chlorite 00h ? 3.3 100 0 Illite 003; Quartz 3.18 11 2 _ 2.56 9 2 Kaolinite 130, 201, 130 2.A92 2 0 Kaolinite (131, 200, 112) ? 2.15 11 2 illite 202, 133 2,27 Quartz l02 2.l Kaolinite 023 ? Dolomite 20l ? Sample 2l Identification d-Spacing l/lmax Remarks Lith: Br. sh. 9.8 7.5 Illite 00] 7.1 5.0 Kaolinite 001 Well: 22 (M50) n.92 3.8 Illite 002 _ A.3u 5.6 Kaolir1ite 110 Depth: 1570-75 u.18 20.0 Kaolinite 117 3.73 3.8 Kaolinite 021 3 8.0 3.67 5.0 1111te'023 ? max 3.5 3.8 Kaolinite 002 Loc. 9N-15w-30 3.u2 2.5 3.3 l00.0 lllite 003, Quartz l0l 3.18 5.0 2.98 5.6 2.86 13.8 illite 115 2.68 6.3 Dolomite 006 ? _ _ 2.5u 6.3 Kaolinite 130, 201. 130 2,25 8.1 Illite 202, 133 2.26 7.5 Quartz 102 ? Sample 22 Lith: Cal. sh. 9.8 8.1 Illite 001 7.0 8.l Kaolinite 00] -Wellz I633 u.87 3.5 Illite 002 ’ 8.32 3.5 Kaolinite llg "Depth: 1175-90' n.18 18.6 Kaolinite 111 3.63 5.2 lllite 023 ? 'max: 86 3.50 7.0 Kaolinite 002 3.28 l00.0 illite 003, Quartz l0l 3.20 12.8 _ 3.l5 l8.6 Kaolinite ll2 2.9M 3.5 2.86 59.3 illite 115 _ 2.56 H.7 Kaolinite 130, 1309 20l 2.53 7.0 Koalinite 137, 172 2.uu 8.7 lllite (202. 133)? 135— Sample 28 Identification d-Spacing I/Imax X100 Remarks 0-12 Poor Resolution Lith: Gn. sh. (28) 7.0 2.9 Kaolinite 001 ? 5.8 2.9 Permit: 18805 8.32 2.9 , 8.18 18.6 Kaolinite III Depth: 8001-057 3.67 5.8 1111te 023 ? 3.50 8.3 .Kaolinite 002 lmax' 7.0 3.2 100.0 Illite 003. Quartz 101 3.18 8.6 2.86 31.11 1111te115 2.67 3.6 Dolomite 006 ? _ 2.58 ;.7 Kaolinite 130. 130‘ 201 2.88 12.9 Illite 202. 133 2.26 10.0 Quartz 102 2.22 7.1 _ 2.18 7.1 KaoIinite 201. 132 220 Sample 29 0-21 Poor Resolution Lith: Dk. Gn. sh. (311 8.18 18.0 Kaolinite 002 ? 3.5 12.0 Permit? 18805 3.28 100 0 IIIite 003. Quartz 3.18 12.0 , Depth: 970'-98’ 3.16 10.0 Kaolinite 112 ? 2.98 10.0 lmax= 2°5 5.86 18.0 111116 115 2.78 18.0 Kaolinite 002 ? 2.538 18.0 Dolomite 221 ? 2.83 12.0 2.25 18.0 1|11te 227 7 Sample 83 136 Identification d-Spacing I/imaxXIOO Remarks Lith: Gn. sh. (28) 0-9 Poor Resolution 9.8 2.3 illite 001 ? Imax 8.8 7.0 3.8 Kaolinite 001 8.18 15.9 Kaolinite 111 ~ 3.96 3.8 Sample NO° 3 3.68 8.6 Kaolinite 002 3.5 3.8 3.28 66.3 Illite 003. Quartz 101 3.22 13.2 3.18 15.9 2.86 100.0 illite 115 2.65 3.9 Illite 20i. 130 2.88 9.1 lllite 202. 133 2.26 6.8 Quartz 102 ? 2.22 51.1 2.13 10.2 Kaolinite 023, 081 2.1 8.0 Sample 58 Lith: Gn. sh. (28) 0—9 Poor Resolution with 15 (29) 9.8 11.1 111ite 001 70] 13.5 .Kaolinite 001, Chlorite 002 Permit: 9198 8.92 6.3 Illite 002 8.68 6.3 Chlorite 003 Depth: 2350'-65' 8.63 6.3 , 8.32 6.3 Kaolinite 110 I 2 6.3 8.18 17.5 Kaolinite 111 max 3.67 8.0 Illite (113, 023) ? 3.51 10.3 Kaolinite 002; Chlorite 008 3.85 11.1 3.28 100.0 Illite 003. Quartz 101 3.18 6.3 2.98 6.3 1111te118? 2.863 89.2 2.72 8.8 Illite 115 2.53 7.9 2.87 8.8 .Kaolinite 131. 112; Chlorite 008 2.88 9.6 Illite 201 ? Chlorite 132. 203 2.38 7.9 2.27 11.1 Quartz 102 137 Sample 55 Q[ffihfification d-SBacing l/lmaxX‘QO Remarks .Lithz Gn. sh° (28) 13.11 3.8 Chlorite 001 7 9.6 13.8 Illite 001 ? Permit: 6308 6.88 10.3 Chlorite . ' 6.5 2.3 'Depth:‘630-50 6.3 2.3 ‘ ‘uu 8 5.8 2.3 I =3 .7 8.82 5.7 max 8.68 3.8 Chlorite 003 8.32 5.2 Kaolinite 110 8.10 2.9 _ ‘3.83 3.8 Kaolinite 111 3.72 8.0 Kaolinite 021 3.68 6.8 Kaolinite 021 3.5 100.0 3.28 10.3 Kaolinite 002 ? Chlorite 008 3.18 11.5 3.16 16.1 Illite 112 2.9 5.2 2.872 35.6 Illite 115 _ _ 2.53 7.8 Kaolinite 131, 112 2.88 11.5 2.38 2.9 2.26 8.0 2.22 8.0 2.17 5.7 2.1 9.2 138 Sample 57 Identification d-Spacing I/ImaXXIOO Remarks Lith::Dk.'gn;’Sh. 8 Illite 00. 31) 52 . Depth: 910-25 9 Kaolinite 001 58 Illite 002 Permit: 18697 85 68 Chlorite 003 lmax’:'8'8 32 Kaolinite 110 18 2 Kaolinite 111 LOC..22N 15W 18 Kaolinite 021 Illite 023 Kaolinite 002 ? Chlorite 008 [\3 OO —.5 Kaolinite 112 CO 0\ Illite 115 _ _ Kaolinite 131, 112 Illite (202. 133)? Chlor. 132, 203 Quartz m1010 m m m mt»cutucuoao)o):’:-:—cwm axono if 0\ . . . :r #7 42" 00 :“0 Qt» Ow» U)O\O\O\m FWNKN —\m(» t‘m-4 mi» m—mrm—nvmmONmrrmNrommmr 139 Bedford shale Sample 8 ‘ Identification d-Spacing l/lmaxXIOO Remarks Lith: Gr.sh (27) 9.7 17.3 Illite 001 ? 6.88 10.7 Kaolinite 001 Permit: 23072 8.85 8.0 Illite 002 8.3 9.3 Illite 111 Depth: 1115-30 8.22 8.0 _ 8.16 16.0 Kaolinite 111 I-max=7«5 3.79 5.3 3.65 8.0 Illite 023 3.50 9.3 Kaolinite 002 3.26 100.0 Illite 003, Quartz 101 Sample 11 Lith: Gr.sh (27) 18.2 3.5 Chlorite 001 12.8 2,8 Permit: 25158 10.0 28.1 Illite 001 8.76 3_5 Depth: 1010-20 7.1 20.5 Kaolinite 001, Chlorite 002 5.08 8.8 Illite 002 Ima£=8.3 8.98 10.8 Illite 002 7 8.68 5.8 Chlorite 003 8.38 10.8 Kaolinite 110 8.28 3.6 Illite 111 8.22 18.1 _ 3.89 3.5 Illite 113 7 3.67 6.9 Illite 023 7 3.51 18.8 Kaolinite 002, Chlorite 008 3.3 100.0 Illite 003, Quartz 101 3.22 3.18 2.96 Illite 025 7 180 Sample 16 identification d-Spacing I/ImaXXIOO Remarks Lith: Gr. sh (27) 13 75 5.8 Chlorite 001 9.9 29.1 illite 001 Well: 1398 7.10 19.6 Kaolinite 001. Chlorite 002 8.92 9.8 11111e 002 Depth: 15'5'-25' 8.70 5.8 Chlorite 003 8.38 8.7 Kaolinite 110 Imax==9.2 8.22 38.8 _ 3. 5 8.3 Kaolinite 021 K4|7C 3.70 6.5 Dolomite 102 7 3.51 11.9 Kaolinite 002. Chlorite 008 3.3 100.0 Illite 003. Quartz 102 3.22 8.7 3.18 8.3 illite 118 2.96 3.3 2.885 6.5 Dolomite 108 ? 2.635 7.6 ‘ Illite 200. 131 illite 008 illite (202. 133)? Chlorite 132. 203 Sample 17 Lith: gr. sh. (27) 10.0 10.0 Illite 001 7.0 13.3 Kaolinite 001 Permit: 25357 8.92 5.0 Illite 002 _ 8.38 83.0 Kaolinite 110 Depth: 7601-701 8.22 5.0 3.51 13.0 Kaolinite 002 Loc. 9N. 15E 3.29 100.0 Illite 003. Quartz 101 K?! 3.18 5.8 11|ite 118 2.96 8.2 2.86 6.7 illite 115 275150 _ __ 2 5. 11.7 Kaolinite 130. 201. 130 2.88 11.7 Illite 202. 133 2.365 5.0 181 Sunbury shale Sample 3 Identification d-Spacing I/lmaxXIOO Remarks Permit: 23072 9.8 17.9 Illite 001 6.88 8.9 Kaolinite 001 Lith: Gr. bk. sh. 8.92 3.8 111ite 002__ 8.32 6.8 Kao1inite 110 lmax 78 11.18 21.8 Kao1inite 111— 3.68 5.1 Illite 023 Loc. 8N-8E 3.5 6.8 Kaolinite 002 3,28 100 Illite 003, Quartz 17 K 3.16 6.8 Kao1inite 112 3.08 20.5 Kao1inite 1T2 2.98 5 1 Albite 7 ‘Sample 6 Lith: Bk. sh. 18.16 5.3 Chlorite 001 10.2 28.0 Illite 001 Permit: 11381 7.2 12.0 Kaolinite 001, Chlorite 002 5.07 8.0 l11ite 002 'Depth: 2101-151 8.98 9.3 Illite 002 7 8.73 5.3 Ch1orite 003 |>'K>’C 8.81 9.3 Kao11nite 020 ? 8.28 21.2 Quartz 100 ? 3,72 8,7 .Kaolinite 021 3.60 5.3 3.511 9.3 Kaolinite 002, Chlorite 008 3.325 100 0 1111te 006 7 3.18 5.3 Illite 112 ?_ 3.18 5.3 Kaolinite 112 2.98 5.3 111ite 025 2.9 5.3 l111te 113 2.7 10.6 _ _ _ 2,56 12 Kaol. 130, 201, 130; Chlor. 132, 201 2.8 11.18 Illite 208, 133 2.275 10 Illite 080, 132 2.13 13 Kao1. 023, 081; I1Iite 206, 083 182 figmple 12 -ldehtiflcation d-Spacing l/ImaXXIOO Remarks Permit:.22995 18,2 8,8 Chlorite 001 11.13 8.8 Lith: Bk. sh. 10,1 21,1 |11ite 001 8.6 27.7 Depth: 780'-90‘ 7,9 3,3 7.67 3.3 Loc. 7N-6E- 7.2 11.8 Kaolinite 001, Chlorite 002 5.0 7.8 Illite 002 lmax 9.0 8_73 8,8 Chlorite 003 8,38 8,8 Kaolinite 110 17 K7 c 8.22 21.1 8.0 3.3 Dolomite 101 ? 3,68 6,6 Illite 207, 130; Dolomite 102 7 3.51 5.6 Kaolinite 002, Chflorite 008 3.35 100.0 Illite 003; Quartz 3.d8 11.1 Illite 112 2,96 6.1 Albite 7 2,88 9,8 Dolomite 108 2.68 5.6 Dolomite 106 - _ 2.56 7.8 Kaol. 130, 201, 130; Chlor.132, 201 2.85 11.1 Illite 201, 202, 133 Sample 18 47.0 Poor Resolution Lith: Bk. sh. 7.1 8.6 Kaolinite 001 Permit: ? 8.92 5.2 |11ite 002 8.38 3.8 Kaolinite 110 ~Depth: 1380'-95’ 8.18 17.2 Kaolinite 111 3.85 5.2 Kaolinite 021 lmax : 8,5- 3.65 8.3 Illite 023 3.51 8.6 Kaolinite 002 L0G. N19‘ELL 3.28 100.0 lllite 003, Quartz 3.16 6.9 Kaolinite 112 7, |11ite 112 ? 1<>1 2.98 8.3 Illite 113 2.56 5.3 Kaolinite 130, 201, 130 2.88 12.1 Illite (202, 133)? 183 Sample 19 . - Identification d-Spating Ao" l/lmaxXIOO Rematks Lith: Gr. sh. 2 15 Illite 002 Permit: 22l58 Chlorite 003_? Kaolinite lll Kaolinite 002; Chlorite 008 ? illite 003, Quartz , .53 Kaolinite l3l,_ll2; Chlor. 132, 201 .88 Illite 202, 133 Depth: 710'220' 0\ :— \J‘1\J'l\l\}l C)vw:r:r~1:- , .2 lmax 5 101000004?er (13 Poor sample Sample 20- Lith: Bk. sh. 13.2 5.2 Chlorite 001 ? 9.9 7.9 |11ite 001 Permit: 19396 7. 3.9 Kaolinite 001 ? Chlorite 002 8.98 6.6 |11ite 002 _ Depth: 1070'-75' 8.38 7.2 Kaolinite 110 8.28 2.6 Illite 111 ’ Imax 7.6 8.22 18.8 Orthoc10$e 201 ? 3.67 5.2 |11ite 023, Dolomite 102 ? |> K>'C 3.51 5.2 Kaolinite 002; Chlorite 008 3.3 100.0 Illite 003 2,885 25.0 Dolomite 108 2.70 7.2 Dolomite 006 7 2.58 5.2 Illite 202 ’ _ 2,56 6,6 Kaolinite 130, 201, 130 2.58 7.9 Kaolinite 130, 130, 201; 001. 105 2.85 9.9 Illite 202, 133 2.81 8.6 Dolomite 110 ‘3 2,27 7,9 Chlorite £133, 208) ? 2,23 2.6 Illite 221 _ g 2.19 3.9 Kaolinite 201, 132, 220; 001. 113 2.1 9.2 188 Sample 25 ., - Identification d-Spae¢ng #0 ’ ‘l/lmaxXlOO Remarks PO6r Resolution _ Lith: Br. bk. sh. 8.18 15.8, Kaolinite 111 3.63 5.3 Illite 023 Permit: 18805 3.89 6.6 ‘Kaolinite 002 3.28 100.0 Illite 003, Quartz Depth: 7951-800t 2.98 6.6 Albite ? 3 2.93 6.6 Illite 113 LOC. $5-9w 2.86 13 1 Illite 115 Imax: 3.8 K7 I Sample 30 Poor Resolution _’ Lith: Bk. Sh. 8.12 ‘ 12.8 Kaolinite 111 3.63 18.9 Kaolinite 002 Permit: 13501-13701 3.89 76.6 Illite 003 3.28 100.0 |11ite 003, Quartz Depth 2.98 85-1 - _ 2.93 12.8 Kaolinite 112, 131 imax 2.35 2.86 8.5 lllite (202, 133) ? 17K Sample 35 x . ‘P05?Resolution Lith: Gr. bk. sh. 3.5' 16.7 Kaolinite 002 3.5 100.0. Illite 003, Quartz Permit: 13939 2.53 i 25.0 Kaolinite 181, 112 Depth: 805'-17‘ Imax 1'2 185 Sample-31 _fif Identification d-Spacing lflméxXWOO Remarks Poor-Resolutiofi— I Lith: Bk. sh. 8312 7.5 . Kaolinite 111 3.5 12:5 Kaolinite 002 Permit: 28182 3.28 100 0 _ - _|1lite 003, Quartz 3.26 95.0 ‘ |11ite 003 7 Quartz 101 7 Depth: l820'-80' Loc..27N-5w-29 Poor Sample 32 " Poor Résolution ‘ Lith: Bk. sh. 8.18 15.0 Kaolinite 111 3.5 12.5 Kaolfinite 002 .Depth: 1880'-1500' 3.3 95. , |11ite 003, Quartz 3,28 100. Illite 003, Quart; ,_ Loc. 27N-5w-29 2,56 20 -Kaolinite 130, 201, 133 2.85 15 |11ite 202, 133 I7 K 2-27 15 2.21 10 Quartz 200 ’__ _ 2.18 10 Kaolinite 201, 132, 220 Samdje 36 I 7 Poor Reéolution Lith: Gr. bk. sh. 3.5 15.8 Kaolinite 002 ? 3.3 88.6 Illite 003 Permit: 17328 3.26 100. |11ite 003, Quartz 2.885 19.2 Dolomite 108 ? Loc. N26-w8-33 2.56 23.1 _ ‘_ 2.83 86.2 |11ite 202, 133 7 lmax=1.3 38,5 K7'I 186 .Sample 58 IdefitificatiOn d-Spacing I/ImaXXlQO ‘ Remarks Chlorite 001 Illite 001 Illite 001 Kaolinite 001; Illite 002 Illite 002 Chlorite 003 Kaolinite 179 Kaolinite 111 Kaolinite 021 |11ite 113, 023 Dllite 023 Kaolinite 002, Chlorite 008 Quartz 101 |11ite 003, Quartz 101 Illite 118 Illite 113 ? ,lllite 115 U1 Lith: Gr. bkL.Sh. 1 1 .Permit: 13939 Depth: 9101-917 I 9.8 max 1° h):rowtntnkal-nairkntntnlq-—Lukn§3k>&>tnlq O\-F-‘O\\O\]-P’CDODO K, 1’13 0 O oacnoacnxro\n> C) 10 ‘ . t'C>£T~JUJ£rLrCD~JUJv1C)CDUJ#: b\2>6K>C 3.70 7.5 Kaolinite 021, Dolomite 102 3.65 725 |11ite 023 3.51 12.5 Kaolinite 002, Chlorite 008 3.31 100.0 |11ite 003, Quartz 101 3.20 6.3 Illite (025, 115) 7 3.18 7.5 lllité 112 ? ’ " “ 2.96 6.3 Hematite 220 ? Albite ? 2.885 30.0 Dolomite 108 2.68 7.5 Dolomite 006 '_ 2,56 15.0 Kaol. 130, 291; Chlorite 132, 201 2,52 6.3 KaOl: 131,,112;,|Tlite'008, 113. f g 2,85 12,5 iiiite1292, 133,2201; Chlo. 132, 203 2,80 8,8 Kaol; 131, 112, 200; Dolomite 110 2.39 “8.8 Illite 208, 133 2.365 7.5 2.27 10.0 |11ite (080, 132) 7 2.25 3.8 |11ite 221 2,23 6.30 |11ite 221 2.2 12.5 Quartz 200 188 Sample 18 Identification d-Spacing l/ImaxXIOO Remarks 10.0 3.0 Illite 001 Lith: Red sh. 8.22 8.9 _ 3.83 6.8 Kaolinite 021 Permit: ? 3.70 8.8 Illite 113, 023 3.51 3.0 Kaolinite 002 ? Depth: 982-95 3.3 36.6 |11ite 003, Quartz 101 3.20 8.0 Loc. 9N, 15w 3 008 98.0 2.855 97.0 Illite 115, Dolomite 108 I _ 10.1 2.68 3.8 max 2.56 3.8 Illite 202 _ 17K 2.882 10.0 Kaolinite 200,_131, 112 2.88 3.0 Illite 202, 133 2.8 5.9 Illite 208, 133 2.26 18.8 |11ite (080, 132) 7 2.2 10.0 Quartz 200 Sample 60 0-20 Poor Resolution Lith: Red sh. 9.6 3.6 |11ite 001 7 6.88 7.1 Kaolinite OOl ? Permit: 18697 8.18 18.2 Kaolinite 111 3.79 7.1 Kaolinite 111 Depth: 880-90' 3.89 7.1 Kaolinite 002 7 3.28 100.0 |11ite 003, Quartz 101 lmax= 2.8 2.97 96.8 Hematite 220 ? 2 863 60.7 Illite 115 _ _ Loc. 22N 18w 18 2.58 7.1 Ka61inite 130, 201, 130 2.86 17.9 |11ite 202, T33 K>| 2.83 7.9 Illite (202, 133) 7 2.26 32.1 |11ite 080, 132 189 Ohio Samples 'Sample 85 (Ohio No. l) Identification 'd-Spacing I/lmaxXIOO Remarks 8.32 7.3 8.22 15.9 3 5 15.9 Kaolinite 002 3.28 100 0 Illite 003, Quartz 101 3.16 9 8 Kaolinite_ll2 2.93 9 8 Illite 113 2.88 7 3 Sample 86 (Ohio No. 2) 929 11.5 Illite OOI Lith: Bk. sh. 7.1 13.5 Kaolinite 001 6.9 13.5 Kaolinite 001 7 1max 5.2 8.98 7.7 |11ite 002 8.9 11.5 Illite 002 7 8.3 5.8 11lite 111 , 8.18 17.3 Kaolinite 117 3.67 5.8 Illite (023, 113) 3.5 12.5 Kaolinite 002 3.28 10.0 Illite 003, Quartz 101 3.18 5.8 _ 2.67 :518 Illite 201, 112 ,_ 2.53 7.7 Kaolinite 202, 133 2.88 11.5 Illite 202, 133 2.21 8.7 150 A mwmaaho>oom.m mo mpsmsflagaoo v mmamadm occuqumm use wawnm 0250 no acowpdooq Ha.mam K OH 222m eu>um Crossview Rd. 151 Sample 88 £§%io No. 5) Identification d-Spacing l/ImaxXIOO Remarks Lith: Dk. gn. sh. 9.6 12.5 * Illite 001 7 (31) 6.88 8.8 "Kaolinite 001 7 8.87 7.5 |11ite 002 7 8.3 16.3 . Imag= 8.0 8.18 7 5 Kaolinite 117 3.68 15 0 3.5 15.0 Kaolinite 002 3,27 00 0 Illite 003, Quartz 101 3.16 6 3 Illite 112 2.93 7 5 |11ite 113 2.76 17 5 Kaolinite 022 3 2.53 15 0 Kaolinite 112, 131 2.83 12 5 2.365 5 0 2.25 12 5 2.21 20.0 Sample 89 (phio NO. 7) Lith: Gn. Sh. (28) 9.8 3.6 Illite 001 7 6.88 8.9 Kaolinite 001 8.92 5.8 Illite 002 7 8.89 6.3 Illite 002 7 lmax: 5.6 8.62 5.8 _ 8.16 16.1 Kaolinite 111 3.63 5.5 |11ite 023 7 3.88 12.5 Kaolinite 002 3.28 100 Illite 003, Quartz 101 3.16 |11ite 112 , _ 2.52 Kaolinite 131, 112 2.83 1 |11ite 201 7 2. 2. 2 2. 2. 03:43—E;b\01c>l2 152 Sample 50 {Ohio No. 10) Identification d-Spacing l/lmaxXIOO Remarks Lith: Red sh. 6.99 6.5 Kaolinite 001 ? 6.86 9.7 8.87 9.7 Illite 002 8.82 11.7 Imax= 3.1 8.3 12.9 |11ite 111-7_ 8.18 17.7 Kaolinite 111 3.8 6.5 3.52 8.1 Kaolinite 002 3.87 8.1 3.28 100.00 Illite 003, Quartz 101 3.16 8.1 Kaolinite 112 ? 2.98 8.1 2.68 9.7 . - 2.52 19.8 .Kaolinite 131, 112 2.892 12.9 2.88 12.9 |11ite 202, 133 Sample 51 (Ohio No. 11) Kaolinite 001 Lith: Red sh. 7,15 11.8 6.99 11.8 Chlorite 002 8.92 18.7 |11ite 003 8.72 8.8 Chlorite 003 Imax=3.8 8.68 8.8 Chlorite 003 8. 2 8.8 8.32 11.8 _ 8.18 20.6 Kaolinite 111 3.50 17.6 Kaolinite 002, Chlorite 008 3.88 18.7 3.28 00.0 _Illite 003, Quartz 101 3.18 10.3 Illite,118 7 2,75 8, Kao inite 022 _ 2.58 18.7 Kaol. 130, 207, 130; Chlo. 132, 201 2.88 16.2 |11ite (202, 133) 7, Chlo. 132, 203 2.35 11.8 _ _ 2.26 11.8 Kaolinite (201, 132, 220) 7 2 6 .20 17. Kaolinite 023, 081 153 Sample 52 (Ohio N0. 12) Identification d-Spacing l/ImaXXIOO Remarks Lith: Red sh. 9.8 11.9 |11ite 001 7.1 15.3 Kaolinite 001, Chlor. 002 7 8.87 8.3 .Illite 002 8.66 8.2 Chlorite 003 lmaifi 6.9 21L-32 8-3 ~ 8.18 19.8 Kaolinite 111 3.66 5.6 |11ite 023 3.52 9.7 Kaolinite 002, Chlor. 008 7 3.87 11.1 3.360 8.2 Kaolinite 111, Illinite 003 ? 3.28 100.0 Illite 003, Quartz 101 2.75 8.3 Kaolinite 022 2.673 8.9 _ _ _ 2.53 5.6 Kaoli 131, 112; Chlor. 132, 201 2.85 10.8 |11ite 202, 133; Chlor. 132, 203 2.273 9.0 |11ite 080, 132 2.22 6.9 2.1 8.3 Illite 023, 081 Sample 53 (Ohio No. 8) Lith: Bk. sh. (23) 13.6 2.8 Chflorite 001 10.1 3.3 |11ite 001 9.5 10. Illite 001 7.336 2.2 Chlorite 002 lmax=‘9.0 7.0 10.0 Kaolinite 001 8.87 5.6 |11ite 002 8.60 8.8 Chlorite 003 7 |11ite (110, 020) 7 8.30 6.6 .Illite 111 7, 8.16 30.0 Kaolinite 111 3.88 2.2 3.68 6.6 Illite 113, 023 3.88 8.9 3 28 100.0 |11ite 003, Quartz 101 3.18 6.6 Kaolinite 112. 3.08 2.2 Kaolinite 112 2.82 38.9 2.75 3.3 Kaolinite 022 2.69 _ _ 2.53 6.6 Kaolinite 131, 112 2.83 12.2 APPENDIX 11 Computer Analyses Coding: Three columns were assigned for the lithologic descriptions and so up to 999 rock types can be analysed by the program (Envidep). However, only 53 lithologies were coded as follows: 1. Sandstone 10. Silffitone, sandy 2. Sandstone, fine-grained 11. Siltstone, shaly 3. Sandstone, very fine-grained 12. Siltstone, calcareous 8. Sandstone, calcareous 13. Siltstone, dolomitic 5. Sandstone, dolomitic 18. Siltstone, ferruginous 6. Sandstone, ferruginous 15. Siltstone 7. Sandstone, argillaceous 8. Sandstone, medium-grained 20.. Shale, grayish black 28. Shale, green 21. Shale, dark, grayish black 29. Shale, grayish green 22. Shale, black 30. Shale, brownish green 23. Shale, blacker 31. Shale, dark green 28. Shale, very black 32. Shale, grayish brown, dolomitic 25. Shale, brownish black 33. Shale, reddish, dolomitic 26. Shale, brown 38. Shale, gray, calcareous 27. Shale, bluish gray 80. Limestone 50. -Dolomite 81. Limestone, argillaceous 51. Dolomite, calcareous 82. Calcareous mud 52. Dolomite, argillaceous 83. Limestone, dolomitic 58. Dolomite, cherty 60. Hematite 63. Dark (Hue) 61. 'Limonite 68. White 62. Light (Hue) 65. Gray 66. Red 69. Buff 67. Tan 70. .Muddy 68, Carbonaceous 71. Unconsolidated 158 155 Mississippian-Devonian systems 31 Series 0 Fermations: 30. Traverse Limestone 35. Antrim-Traverse 80. Antrim Shale 85. Ellsworth-Antrim shales 50. Ellsworth Shale 60. Bedford Shale 65. Berea-Bedford formations 70. Berea Sandstone 75. Sunbury-Ellsworth shales 78. SunbUry-Berea formations 80. Sunbury Shale State code: 21. Michigan County codes: See page 159 Envidep: Data Input: An identification card and a series of lithologic cards com- prised the input data for each well. The first fifty-two columns of the identification card were used to record all relevant infor- mation for each weII. 1-5 Permit number 6-7 State code 8-10 County code 11-18 Township, Range and Section 19-28 Latitude 26-31 Longitude assigned as follows: 33-35 36-81 82-83 88-86 87-52 The columns Were assigned as follows: Number of Cards for well Elevation RB, RF, KB etc. Well number 1/8, 1/8, 1/8; 1/8, 1/8; 1/8 In the case of the lithologic card, all the eighty columns were 156 In the case of the lithologic card, all the eighty columns were assigned as follows: 1-5 Permit number 37-39 Lithology No. 3 6-8 Card sequence (first to 999th card) 80-81 Percentage 9410 System code 82-83 Cement 11 Series code 88-85 Hue 12-13 Formation code 86-87 Color 18-16 Lithology number 1 - 88-50 Lithology No. 8 17-19 Percentage 51-52 Percentage 20-21 Cement 53-58 Cement 22-23 Hue 55156 Hue 28-25 Color 57—58 Color 26-28 Lithology number 2 59-63 Top of unit 29-30 Percentage 68-68 Bottom of unit 31-32 Cement 69-71 Well number 33-38 Hue 78-70 Elevation 35136 Color 80 Total number of Iithologies on card For example, well No. 91 has fourteen lithologic units and was therefore represented by a decklet one identification card and five lithologic cards. One of each type is reproduced as follows: I1 215591 Hansen 52' .8118 —8 .722 s 552.121 11:12711zn1: ES x . n- - .-.--. fl. = H__H___JlJLJL_ 651%.LFIH1U4UUHinfl 0228u 0 51w' 121 1 23 “n A'vn : . ' '1 ‘4 .I . L! a: 5+5! -.. . r. .. ,.;_-.;:..I .. I I'l-Hji 1 Pi": '1"; :‘j '71:: . u,— FOR C finnm‘r STATEMENT NU“ BEN ““00” H2341 'Pfli 42222222222222222222z22222772222222222222222222722222222222722227222222222222228 FORTRAN STAT E M E N T IDEMIFIcATIou oaniunun717777777777777777777771inianuuo7777777F7777777777777777787777777T 1IImunuuuunnnmunauuannuNWinnm anaaw Hauuuuuuammanussn aaunuuuuuuaann nunmnun- I'I‘Illll' IlllllIlllIIlIlIllIIll'lllllllllllllllIllIlllllllIIIllqlllllllil - " a WYIIIIATIOI 83333333'33333”3333333333333”333333333333333333333333333333333333333333333333q33 fl4441444444’444‘4444444‘44444444441144444444444444I444414444’44444414441144444fi4 I J 5fi5555555555'5555555555555555555555555555555555555555555555555555555555555555555 - Ann-AAI 'F 157 It is important to note that the zeroes may be left out as shown in the two variations of each card (a,b and c,d), as long as the other two numbers are punched 'right justified' . They are decimated by shifting them to wrong columns . For example, two in column 6] of the lithologic card indicates a top of 2,h00 feet . it becomes 2h0 feet if the two is punched in column 62 and 2h,000 when punChed in column 60 . input Format Statements: The format statement number one reads in the identification card while the lithologic card is read in by the second statement . No data instruction card was necessary because all required analyses were performed and printed for every well . Both print and punch outputs were produced by the program .The information on both was essentially the same . in the print output, all the required information was printed as follows : Elevation «1016.l GD Well 268 Permit 12309 State 2l, County 107 Township th,Range 7w x 831580, Y 85.090 Bedford-Berea Thickness of Bedford Formation 0.0 Thickness of Berea Formation 1.6 Total thickness of both formations 1.6 Total sandstone 0.0 Total shale 1.6 Ratio of sandstone to shale 0.000 Percent sandstone in Bedford 0.0 Percent shale in Berea 0.0 Antrim Total thickness of Antrim Shale 270.0 Percent black shale 91.1 Ellsworth Total thickness of Ellsworth formation 288.0 Percent green shale 6.0 Total thickness of carbonates 0.0 Total thickness of Ellsworth-Antrim transition zone 0.0 Sunbury Total thickness of Sunbury formation 30.4 158 Total thickness of formations 590.0 Top Antrim -1863.9 Top Bedford-1016.1 T0p Berea 415h5.5 Top Ellsworth -1575.9 Top Sunbury -15h3.9 Note : All figures are in feet and 'top' means sub-sea elevation . The above information was set up in graphical form as follows: EEEEEEEEEEEEEEEEEERQ Dept“ 2560 E=Dk.grayish black shale 0.95 EEEEEEEEEEEEEEEEEER' R= Shaly limestone 0.05 EEEEEEEEEEEEEEEEEER $$$$$$$$$$$$$$$$$$$ Depth 2590 $= Brownish green shale 1.00 9999999999999999999 Depth 2600 No sample 9999999999999999999 Depth 2610 9= No sample 9999999999999999999 _ 9999999999999999999 Depth 26h0 $=Brownish green shale 1.0 Depth 2700 $= Br.gn.sh 0.855 No sample 0.15 Depth 2780 $=Br.gn.sh 0.55 No sample 0.85 9999999 Depth 28h0 $ =Br.gn.sh 0.55; No sample 0.35 )= Grayish green shale 0.10 )) . GGGGGGGGGGGGGGGGGGG Depth 2880 G='Blacker' shale 1.0 GGGGGGGGGGGGGGGGGGG GGGGGGGGGGGGGGGGGGG GGGGGGGGGGGGGGGGGGG ( section continues to 3000 ) Note : All depths are in feet . Each row represents an interval of ten feet while each lithologic symbol is 5% of the lithologic unit . Begausetof lack of space, the bottom 1h0 feet of the section is omitted .Descriptions on the right were abbreviated on original section . 1 State Alconae------__-__-___ 2i Alger- .----..----__ 21 Allegan-----_--..-_-__ 21 -Alpena. ........... . ..... 21 Antrim ................ - 21 ‘Arenae— --------------- 21 1 Baraga ---------------- 21 Barry ----------------- 21 Bay ------------------- 21 Benzie ---------------- 21 Berrien --------------- 21 Branch ---------------- 21 'Calhoun --------------- 21 Cass ------------------ 21 Charlevoix ------------ 21 Cheboygan ------------- 21 Chippewa -------------- 21 Clare ----------------- 21 Clinton --------------- 21 Crawford -------------- 21 Delta ----------------- 21 Dickinson ------------- 21 Eaton ----------------- 21 - Emmet ----------------- 21 Genessee -------------- 21 Gladwin --------------- 21 Gogebic --------------- 21 Grand Traverse -------- 21 Gratiot --------------- 21 Hillsdale ------------- 2J Houghton -------------- 21 Huron ----------------- 21 Ingham ---------------- 21 lonia ----------------- 21 Iosco ----------------- 21 Iron ------------------ 21 Isabella--r ----------- 21 Jackson --------------- 21 Kalamazoo ------------- 21 Kalkaska -------------- 21 159 County Codes, Michigan County 001 003 005 007 009 011 013 015 0l7 019 02 l 023 025 027 029 031 033 O35 O37 039 081 083 085 087 089 051 053 055 057 059 061 063 065 067 069 071 073 075 077 079 State Kent-' ----------------------- 2] Keweenaw .................... 2] Lake ------------------------ 2] Lapeer ---------------------- 2] Leelanau ____________________ 2] Lenawee --------------------- 2] Livingstone _________________ 2] Luce ........................ 2] Mackinac -------------------- 2] Macomb ______________________ 2] Manistee -------------------- 2]‘ Marquette ------------------- 2] Mason ----------------------- 2] Mecosta ..................... 2] Menominee ------------------- 2] Midland --------------------- 2] Missaukee ------------------- 2] Monroe ---------------------- 2] Monttalm -------------------- 2] Montmorency ----------------- 2] Muskegon -------------------- 2] Newaygo --------------------- 2] Oakland --------------------- 2] Oceana ---------------------- 2] Ogemaw ---------------------- 2] Ontonagon ------------------- 2] Osceola --------------------- 2] Oscoda ---------------------- 2] Otsego ---------------------- 2] Ottawa ---------------------- 2] Presque Isle ---------------- 21 Roscommon ------------------- 2] Saginaw --------------------- 2] St. Clair ------------------- 2] St. Joseph ------------------ 2] Sanilac --------------------- 2] SChoolcraft ----------------- 2] Shiawassee ------------------ 2] Tuscola --------------------- 2] Van Buren ------------------- 2] County 08 l 083 085 087 089 091 093 095 O97 099 101 l03 105 l07 109 111 H3 115 H7 119 121 123 125 127 129 131 133 135 137 139 l8l l83 185 I87 189 151 153 155 157 159 l60 County Codes, Michigan State County .Washtenaw ------------- 21 161 Wayne ----------------- 21 163 Wexford --------------- 21 l65 State Code 21 The coding systems (lithologic, identification, county and state) were patterned after those used in the Data Center, Department of Geology, Michigan State University. l6l The columnal diagram was produced by Formats 3-9 while the well summary in the first part of the print output was produced by state- ment No. 10. Correlation charts (Plates 21a-21j) were prepared from the columnal diagrams by pasting selected wells together. All the above information was automatically punched (2 cards per well) by means of format and punch statements 20 and 21. The first card contains all information and punch statments 20 and 21. The first card contains all information for the Bedford-Berea sequence, while the other three formations are accomodated on the second card. The following is a sample punch output for well 268: E?0.0—1863.9 91.1 288.0—1575.9 i l l Ilulallnnuounnnannunnnul]olnnannnuulaInnunolnlololuunlnunnoouuuuulllllllnonnoull 11 2 C S I 1 I IInnnunuIIIInnaunuaanaanmnauuannalouaouaununwunaunannaunnuuaunnunnnnunnnnnu llllllllllllllllllllllllllllllllllllllllllllllllllllllllllllllllllllllllllllllll 21122221222222222222122222222222222222222222222222222222222222222222222222221221 3333l333334lazlaa4333331333333133333133333133333133343ll333311333333133333333333 44444lllllll4444lllllllalll444444l444444lll4444lll44lllllllllillllllllllllllllll 5555555555555555555555555551515555555555555.5555!)r555555555-155555515555555555.5555 The identification of each of the eighty columns is presented in sections d and e of this appendix. Data Plotting: Maplot: The cards above were used for plotting the variables of each well on the base map generated by the Maplot program (Appendix llf). To write the program, it was necessary to mark out 183 points on the outline of the state and 108 county corners. The longitude and latitude 162 for each of these 287 points were calculated because the X and Y co-ordinates for the state, now in preparation, were not available. These were entered as X—out, Y-out, X-cent and Y-cent; where X stands for the latitude, Y for longitude, out for outline and cent for the county corners. During the computation of the longitude and latitude, each longitude degree was 6.5 inches while the latitude was 8.5 inches. Between latitudes 880 and 860, a scale of 9 inches per degree was adopted and hence it was necessary to indicate a different dX for the two intervals might look natural. Two cards per well (as shown above) are required for the operation of this program. In order to use this program for more or less than 883 wells, format statement No. 1 has t be changed accordingly. This is effected by entering the number of wells (1-999) instead of 883. All the data cards are inserted after the 'Run card' of the program and must be arranged in order. Parameter Cards: The data cards are succeeded by a card indicating the number of wells (883 in this case) in the first three columns. This is followed by a set of "parameter” cards (1 card for each map to be produced). On each card, the first 88 columns indicate the title of the map as desired by the author. Columns 50-80 are assigned, six columns each, to Xmax, Xmin. Ymax. Ymin and scale. Columns89 and 50 indicate the number of the variable to be plotted. In this study there were 22 variables of which the thickness of Bedford Shale was number 1. Hence 1 was entered in column 50. 163 The scale of 6.5 inches per degree of longitude represents l/500,000. The output map shows well locations by-+ and the variable is plotted just to the right of itchhe state boundary is indicated by 0, while the county corners are marked by Y. .Each map consists of two sets of sheets which can be glued together for the whole state. When gluing the sheets together, the latitude lines must be aligned and the longitude lines must not be more than 6.5 inches .(or the desired map scale) apart. The appendices have been arranged in the order in which they were used. Section A, the Envidep program, analysed all the data in 118 and C. Sections D and E were produced from the data contained in the former. These were in turn fed into the Maplot program, section F. APPENDFX ll COMPJTER ANALYSES This Appendix is divided into six seCtions as follows: a. Envidep--A fortran program for stratigraphic analyses. b. identification of wells. c. Well records. do Card outpur--Bedford-Berea sequence, e. Card output—-Antrim, Ellsworth and Sunbury shales. f. Maplot--a fortran program for automatic data plotting. ENVIDEP--A FORTRAN PROGRAM FOR STRKHGRAPHIC ANALYSIS 'JOB.600900.374969.3.ASSEEZ.OLAYINKA 'FTN.L.*.X PROGRAM ENVIDEP DIMENSION FORMiSO).MLITH(SO).TOP(50).BOT(50).LITH(50.4).PERC(50.4) 13CEMENT150.4T.HUE(50.4).COLOR(50.4).ID(10).LIST(5) ' 'DIMENSION TITLE(71).LINE(20).LINT(100) TYPE INTEGER FORM.CEMENT.HUE.COLOR.TITLE DATAISTEP=IO 0) DATA (TITLE=2HSS. 7HFINE SS. 8HVFINE SS. 7HCALC SS.6HDOL SS. 7HFE IRR SS. 7HARGL $5.6HM G SS ).(TITLE(10)=8HSDY STSN. 7HSH STSN. 8HCA 2L STSN. BHDOL STSN. BHFER STSN ).(TITLE(20)=5HGR SH. 8HDKGRBKSH. 5 BHBK SH. 7HBKER SH. 7HV BK SH. 7HBRBK SH.5HBR'SH.5HGR SH. 7HGRGN SH 4‘).(TITLE(30)=8HBR GN SH. BHDK GN SH. 6HDOL SH. BHV DOL SH. 8HGRCA 5L SH).(TITLE(40)= 3HLST. 6HSH LST. 4HCALC. 7HDOL LST ).(TITLE(50)= 63HDOL. SHSH'OOL. SHDOLTC. SHCHER DOL ).(TITLE(60)=3HHEM. 3HLI 7M. 4HLITE .4HDARK.4HWHIT . 4HGREY. SHRED. 3HTAN. 4HCARB. 4HBU BFF. 3HMUD. 3HLOS ) ' ‘ c ' INPUT FORMATS 1 FORMAT(A5.12.13.2(A1.12).12.2F7.4.13.F6-1.A2.I3.3A2) 2 FORMATIIIX.12.I3.F3.2.312.3(13.F2.2.312).2F5.0.IIX.II> c ‘OUTPUT FORMATS FOR COLUMN' ‘ 3 FORMATI*I WELL *13.* ELEVATION *Fe.1/l 4 FORMAT(*9*20R1.* DEPTH *Fe.1. 2x. IOORI) 7 FORMATI*9*20R1) 8 FORMATISRII 9 FoRMAT.EO.26lGO To 420 IF(LITH(I.J).EO.27)GO T0 420 so To 410 ' CONTINUE1 so To 290 I66 on 200 250 290 291 BEDFORD FORMATION DO 210J=10M FR=PERC(I.J)*THK IFtPERC(IoJ)-E0.0)FR=THK ASSIGN 210 TO JUMP IF IFORMII).EO.60> GO TO 420 IF ILITHII.J).CT.IAICO To 420 GO To 430 CONTINUE GO TO 290 BEREA FORMATION 00 230J=1oM ASSIGN 230 T0 JUMP FR=PERCII.JI*THK IFIPERCII.J).EO.0>FR=THK IFILITHII.J).E0.20) GO To 440 IFILITHII.J).EO.2I) 00 TO 440 IFILITHII.J).LE.14I GO To 430 IF(LITH(I¢J)OEQ.22) GO TO 440 IFILITH(I.J).GE.40)GO T0 430 GOTO 420 ‘ CONTINUE GO TO 290 SUNBURY FORMATION 00 250J=1.M ASSIGN 250 T0 JUMP FR=PERC(IoJ)*THK IFIPERCII.J).E0.0)FR=THK IFILITHII.J).LE.14) GO TO 430 IFILITHII.J).CT.34)CO TO 430 IFILITH GO TO 298 MI=M1+2' DECODE TITLE M2=MI+7 OECOOEI8.5.TITLEILI).ILINTIN).N=MI.M2> IFIL.E0.1R ) L = 0 N2 = 20.*PERCII.J) N2 = N2 + N1 — I IFIN2.GT.2O) N2 = 20 00 291 N = N1. N2 LINEINI = L N1=N2+1 LINT(M1-2)=L LINTIMI F l) = IR 00 292 N = 1. 8 I67 292 293 2941 2942 295 2951 2952 296 2961 2962 C C C 297 299 299 300 IFILINTIMI - N + e I.NE.IR I GO TO 293 CONTINUE‘ ” MI': MI 2 N + 10 LINTIMI'h II = IR DECOOE HUE IF PRESENT L a HUEII. J) ‘ IF(LoLT. 60) GO TO 295 M2=M1+7 DECODE(808 TITLE(L))I(LINT(N)oNleoME) 'DO 2941 N 10’8 'IN(LINT(M1.- N 4 8).NE.1R ) GO TO 2942 CONTINUE” MI'= NI'+ 10 a N LINTIMI « II = IR DECODE COLOR IF PRESENT COLOR(I¢ J) " IFIL.LT 60) GO TO 295 M2=MI+T ” ' OECOOEIS.S. TITLEILII .ILINTINI.N=MI.M2I DO 2951 N = I. 8 IFILINTIMI - N + SI.NE. IR I 60 TO 2952 CONTINUE ‘ . NI = MI + I0 9 N LINTIMI H II c IR . OECOOE CEMENT IF PRESENT L a CEMENTII. UI ' IFIL.LT; 60) C0 T0 297 M2=MI+7 OECOOEIS.S.TITLEILII.ILINTINI.N= MI.M2I Do 2961 N a I. e IFILINTIMI - N + SI.NE.IR I GO TO 2962 CONTINUE ' M1 M1 + 10 - N LINTIMI E II = IR ENCOO PERCENTAGE ENCODII4.9 TEMP). PERCII. J) MzéMIIS ' i ‘ ' DECQQEI4.8. TEMPI.ILINTINI.N= MI.M2I ”M1 = N1 + 6‘ ' . LINTIMI 4 l) = LINTIMI ~ 2I = IR CONTINUE ' “ OO 299 J = NI. 20 LINEIJI = 1R Mlj? M1 ‘ 1 PRINT 4. LINE. TOPS. (LINTIJ). J = I. MII L=(BOT(I)-TOPS)/$TEP ' TORSasTEP*L+T0PS ‘ IFIL. GT.1)PRINT7.(LINE.J= 2.LI CONTINUE PRINT OUT RESULTS PRINT IDENTIFICATION PRINTIOIELEVILIST(1)OLIST(2)I(ID(I)oI=193)oID(5)olD(4)oID(7)9 1ID(6)oID(8)9(LIST(I)91:395)oID(9)oID(10) 168 IL 400 410 420 430 IOTPssaaHKSSUO/THKBEJ*IUO. TQTPSHéTHKSHBR/THKBER*10b. THK: THKANT+THKBER+THKBED+THKSUN+THKELS TOPELEE ELEV— -TOPELS TORONT=ELEv-TOPANT TOPBER=ELEv-TOPSER TOPBEOzELEv~TOPBEO TOPSUNzeLEVHTOPSUN PRINTII.THKBEO.THKBERIBBTOT.THKSS.THKSH.FR TOTPSS TOTPSH FRaTHKBKSH/THKANT*100. PUNCH2O. IOI9I. ID(10)ITHKBED TOPSEO THKSERITOPSERIFR ESTOT. lTHKSSsTHKSHITOTPSSI TOTPSH. LISTI2I ' PRINT12ITHKANT FR ' FPaTHKCNSH/THKELS PRINTIS.THKELS.FP.THKCARB.THKEAT2 PUNCH2IITHKANT TOPANT FR.THKELS TOPELS.THKEAT2.FP THKCARS.THKSUN. ITOPSUN T HKILISTIEI ‘ PRINT IO.THKSUN ' PRINTIA.THK ToPANT.TOPBER.TOPELS.TOPBEO TOPSUN CO TO 100 " OPEN SUBROUTINE TO CALCULATE ANTRIM LITHOLOCIES IFIToPANT. EO. OITOPANTzTOPIII THKANT= THKANT+FR ‘ IFILITHIIIJI.EO. 26) GO TO UUMP IFILITHII.JI.CE. 21ITHKSKSH= THKBKSH+FR GO TO JUMP OPEN SUBROUTINE TO CALCULATE ELLSWQRTH LITHOLOGIES IFITOPELS. EO OITOPELs= TQP(I) THKELS= THKELS+FR IFIFORMIJI.EO 45ITHKEAT2=THKEAT2+FR IFILITHII.JI.EO.28ITHKCNSH=THKCNSH+FR IF(LITH(I-J).EQ;31)THKGNSH=THKGNSH+FR IFILITHIIIJIICT'40ITHKCARB: THKCARB+FR IFILITHII.JI/2. EO.16ITHKCARE= THKCARB+FR GO TO JUMP OPEN SUBROUTINE TO CALCULATE BEOFORO LITHOLOGIES IFITOPEEO. EO OITOPBEO= TOPIII THKBEO= THKBEO+FR IFILITHII.JI.CT.2OITHKSH=THKSH+FR IFILITHII.JI.OT.IOI GO TO JUMP IFILITH(IoJ)oEQoO)GO TO JUMP THKSS=THKSS+FR THKSSBO=THKSSBO+FR GO TO JUMP OPEN SUBROUTINE TO CALCULATE BEREA LITHOLOGIES IF(TOPBER.EQ.O)TOPBERRTOPII) THKBER=THKBER+FR IFILITHII.JI.LT.IOITHKSS=THKSS+FR IFILITHII.JI.LT.2OI GO TO JUMP THKSHPTHKSH+FR THKSHBRPTHKSHBR+FR so To JUMP C OPEN SUEROUTINE To CALCLATE SUNBURY LITHOLOGIES 440 IF(TOPSUNIEQ.O)TOPSUNaTOP(I) THKSUNuTHKSUN+FR GO TO JUMP END ' -RUNI3Iaoooo I 70 l7l lib Identification of Wells: This section of Appendix II contains all the relevant information for locating the hh3 wells included in this study. The fifty—two possible charactershave been grouped into thirteen columns (A-M) as follows: A E H | m l 3 J c In 4.) l I: l 3 A 7? O v O. O —- I (U L‘ O C L. 01 .C O] I. 01 Q) 4-1 '- m m '01 «A - u _D Q) U v — . L DJ E Q) ‘0 V - (D Q) 3 "o O Q) '4— C 0 .Q U? c o 0 PI m '01 ol 0 IL -E U -- C '0 3 d ~--- g: :5 I. 4-: .C o :3] 4—: s. 4—: '1 c a) v— Q) “I In a) -- +4 .... (D (U m 4.: E «H C c CT I.» .. CT .3 > n: I—T L L m :I 3 C U 4—: C l a) - ~ to O +4 o o m w m o 3 —- m: 0) £1 a. U) L) #1 tr (0 .4 —| 2: UN :6 23 5 2 3 3 3 2 6 6 3 6 2 3 6 The number of Characters in each column is indicated at the bottom. A 2_c,40, E .F c Q44OJZJOOIN2 E071044.597 2325421001N2 E071044.592 2320821001N2 E092244.648 2435921001N27an2044.649 7000221001N27E092244.649 25T6121001N27E092344.652 0840421001N285092o44.730 3415021005701w132942.419 0502521005N03w122242.608 0492121005N03W130942.640 0494421005N03W130842.645 0506421005N03WI41042.643 H 83.568 83.569 383. 307 83. 509 63 304 83.288 83.408 85.788 85.629 85.773 85.792 85.872 0382321005No4w12142.725 85.632 0503021005N04w122942.680 1800221105N19W172043.998 0491921005N04W123342.662 0503621005N04w131642.719 0842621005N04w131842.718 0530421005N04w142142.705 0519921005N04WI42142.698 0522421005N04W142542.672 0057621007N308062544.880 1664521009N29w061944.802 1393921007N29Eo71344.83o 1001921009N30w060344.929 0242921009N31wO50445.012 1000421009N31WO81444.994 1324221011N18E042243.902 1346921011N18E060643.952 0866621011N19E030944.018 0746321011N19E032243.989 0236721011N19E033143.956 0001Y21011N19E033143.961 1f45121011N19EO40944.021 1919621011N19E041543.996 0878421011N19E041744.002 0241221011N19Eo42743.97o 1801821011N19E041144.017 0530621005N03W140142.660 1920521011N20Eo32744.061 0472121011N205033444.046 0374221011N208051844.094 1140621011N20w072644.067 0787321015N03w090842.641 2336321015N04w080342.731 0630821015N04W100346.739 2563211638 2E 81242.280 0865521017N14Eo40244.604 0544121017N14E040243.582 0866121017N14Eo41243.590 0009321017N14E051543.575 A '8 c 0 E F G 85.670 86.216 850651 85.780 85.725 85.878 85.878 85.915 83.741 84.942 84.931 84.854 85.150 83.958 83.779 84.084 84.064 84.129 84.128 83.982 83.956 83.986 83.952 83.940 85.826 84.070 84.069 83.894 83.544 85.339 85.177 850 408 83.440 83.942 83.935 83.916 83.738 H J 00 831.7 OOJNENENE 16 837. 3 0002NEszE 140733. 060003NENwNw 120912. OGDOO4C SENW 0040740. 000005NENE5E 0120808. 060006NENWNE 007 815. 560007SENwsw 0100770.7GDOOBSENESE 0060737.480009SENESE 0060818.3oooioSWSESw 0090734.4GDOIISESENW 0110672.860012NWNwsw 5‘729.160013NENWSE 0060788oéGDOI4SWNWSE 0160676.3RE015NWNwsw 0060742. OGDOIéSESWSE 0060684. 300017SENwNw 0090906. 960018N88w8w 0070688. OGDOI9SESWNE 0070656. 560020N SESE 0080630. 9800218ESWsE 0060840. 060022NENENE OIIIIO4.160023$WSWSE 0121141.2GDO24SEszw 0100906.3GDOZSC NWSE 0080950.860026NWNWSW 0070437.560027s SWNE 0160622.160028NWNwsw 0180583.900029NWNENw 0170781.IGDO3OSESENW 0060789.160031NEszE 0140783.560032c Nw$w 0060784.060033NEszw 0180763.3GDo34SWNwNw 0110738.60003SSWSEsw 0170759.780036NwNwsE 0170657. 560037NESESw 0130597.180038c Nwa 0050676.760039NEsENw 0130775. 3GDO4OSWNENW 0120772.0GDO4ISWSWNW 0140799.060042NWNWNE 0609.6GDO4BNWNWSW 0160796.260044NWNWNW 0100880.460045NwsEsE 0100823.960046SWNENw 3 660.060047SWSENE 0080594.2Goo48Nwszw 0120599.000049s SESE 0120590.2600508WSWNE 0250587.SGDOSISWNENE I 3 K L M I .‘ (:2: l... 0127021017N14EO62143.562 0871321017N155043443.614 83.760 83.962 0864821017N15E04343.618 83.950' 0512121051N17E021843.834 0477021017N18E032843.884 1927921019N25WIBI344.485 1592121019N25W142944.495 0612621021504w181042.126 0096921021804w181542.108 2354521021806W171442.932 2436921021506w190141.972 2186221023805w050542.029 2035521023805w070242.030 2363921023806w063641.862 2070021023506W083041.889 1852821023507w071041.832 2557521025801w072342.332 0829021025802w041542.258 2182521025502wo43442.208 0981621025N02w051242.274 0086421025802WO61442.262 2471521025502Wo72542.228 1001621025503w030142.193 1016021025503wo40442.201 0833321025803w071442.175 2329221025503w072342.154 0728421025so3w081342.175 1988021025803w082442.115 2164721025804w061742.085 1244321025804w070242.110 0761821025504WO70342.119 0774921025504WO81742.082 2328921027507W140841.858 0658721027508w151441.842 0807521027808W151541.752 0791721027508w152241.742 ”2153211635 25 8 342.289 0057921027508W160241.784 1919421029N32w052445.054 1668721029N32w051845.066 1709621029N32w061345.068 1874721029N32WO61444.989 0016321031N33w031245.175 236921117N12w071443.401 0868921035N17W042243.800 0973721037N05wo12042.770 0827 21037N0 w031442.770 1361 21037N0 wo12 42.839 0285 21037N0 w013242.906 1180 21037N0 w0202 2.989 0903 21037N0 w0421 2.942 0234121037N08 0104 3.075 84.239 84.089 88.877 85.688 86.315 86.320 86.182 86.405 84.815 85.061 84.920 85.252 85.070 85.056 84.742 84.738 84.812 84.930 85.040 84.578 84.756 85.055 85.054 85.146 85.140 85.995 85.050 85.066 85.218 85.906 85.958 85.984 85.980 83.472 86.083 84.782 84.880 84.896 85.921 84.552 85.048 44.710 84.413 84.596 84.41 84.416 84.478 84.731 84.396 I l ‘1’! 140586.860053NENWNE 0090601.960054Nwswsw ‘160597.8GDOSSSWNENE 0100710.560056szENw 0130706.IGD057SESWSW 0130863.700058swsESE 0100794.160059NENENE 0110666.86006OE E'sw 0080645.000061Nw5Esw 0120783.5000628EswsE 0120654.000063c NESE 0070965.86D064NWNWNW 0070928o360065NWNWNW 01o1004.700066NENE5E 0080906.360067NESWNW 0060961.1600685ESWSE 0091174.0RT069C c sw 0080955.36007oswszw 0120974.SGDO7ISENESW OO7OQSI.4GDO72NWNWSW 0110963.SGDO735ESWNE 0090933.0GDO74SWNWSW 140991.500075c'NwsE 0120966.260076c SENw 0100923.660077NEszw 0220925.IGDO78C SESW 0120950.4600795E5ENw 0090931.0GDOBONENESE 0100963.7GDOBISESENW 0100934.1000825WNW8E 0080948.500083NENWNE 0120885.600084SWSE8E 0110864.8RBOBSSENENW 0080806.960086NENWSE 0150791.7GDOB7SWSESW 0160804.260088SENWNE 4 691.100 89 NESE 0060854.500090555wsw 0050968.4R8091NESENE 0110722.760092NWSWSE 0090737.760093s NWSE 0110782.800094SENWNE 0020778.0GDO9SSESENE 005 924.560096NESWNE OO7OBBOOOGD097CESWSE 0170865.803098CNNENE 01 0828.QGDOQQSWSWNW 0200819. 0010 szENw 0140817.400101NwNWNE 02 0723.800102NEszw 015 728.260103NWNESE 013 687.500104NWNWNE A (B c 0 |E El 6 H IlJKLM 1407621001N288093344. 710 0273221037N08w022243.019 1139021037N08w033043. 012 1927221037N08W042743. 022 1220921037No8wo43243.005 1845921045N01wo41442.449 2267221045N02w051842.519 0317721037N05w021242.792 0180621045N03wo40542.636 2294521045N03w062242. 594 0727521049N06E051342 865 1091321049N09E052943.108 2407921049N09E080443 168 0486921051N17E022043.800 0857121051N17E022943.796 0112621051N18E032143.892 0384121051N18wo10243.935 0378221051N18w011143. 920 0380821051N18w011143 921 0378121051N18w011143 925 0384021051N18w011243 926 0379021051N18w011443 914 0514021051N18w012743 879 0258521051N18w020643 940 0523821051N19w021843 988 0858721051N20w013344 036 1372221ossm25w101944 478 0986721055N25w121144. 509 0274821055N26W112344. 570 0328921057N09w011843.136 1199121057N09wo31343.126 0425621057N10WO31343.219 0245721057N10w040743.234 1916321059805w033241.952 1865321059805w040742.006 2174521059806WO40141.932 2112021059807w020641. 842 1939621059so7w031141 838 0197521059$OBWOIII41 069 2221621059808W040141 762 1230721059508wo42441 714 1250821063N15E100743 698 1622221063N158102743 651 3459321063N15E111543 684 0116621063N15E123243 644 1290721063N16E100243. 796 0367921063N16E112743.750 0551921063N16E132743. 751 1512421049N096080643. 172 05045 1063N168151 43. 795 07387 1063N17 140 43.87 11928 1063 18 12 43.95 83.285 84.516 84.665 84.712 840 755 84.710 84.902 84.456 84.758 84962‘ 84.802 85.975 85.195 84. 524 84. 529 84.620 84.344 84.470 84.354 84.346 84.835 84.354 84.541 84.540 84.539 84.500 85.458 85.591 85.486 84.435 84.560 84.558 84.772 84.653 84.796 84.688 84.565 84.596 84.315 84.695 84.696 83.344 83.272 83.172 83.172 83.275 83.172 82.959 83.562 0040807.300105NflNwNw 0100735.000106NwNwNw 0100734.260107SESEsw 0110746.860108NwNENE 0080764.360109NwszE 0110932. 060110NENENw OO90923.2RBIIISWSESW 0080856.70011258NESE 0060866.060113NESESE 0080896.0GDII4CSSWSW 0100796. éGDIISSWSWSW 0100676. 860116swszw 0070836.598117058wsw 0120742. 060118NENE8w 0120729. 460119NENwNw 0080711.0GDI2OSWSWNE 0100753. 8001215WNESE 0080750. 060122NE5W8 0110752. 660123SENE5 0090747. 4001248Esw5E 0090745. 7601258WNENw 0090745. 660126NENENw 0110731.SGDIZ7SWSENE- 0090898. 060128c NENw 0080854. 0601295E8E8w 0070813.460130NESENE. OO91081.660131NWNWNW 0071062.0601320N5E8E 0070904.400133NwsWNw 0140662.360134NENWNE 0090701.3GDIBSSENWSE 0090757.160136CEsENE 0110773.000137NWNEsw 0051122.080138NWNWNE 0091009.060139Nw558w 0081095.0GDI4OSWNESE 0101107.860141NWNwsw 0051217.498142NWNWNW 0090880. 8 143N‘SENE OO71094.2RBI44NWNWNW 0091061.10014SSEsENE 0280629.IGDI46CNNWNW 0150640. 4001470 NWNW 0230713. 800148NEsENE 0190744.300149NENwNw 016062S.0GDISOCWNWNE 0170656.0GDISINESENW 0210777.660152NWNWNW 0020783.460153NwsENE 82.72 0022 675.1 D154NWNESE 82.88 83.10 08107 1063 18 13 743°95082.9740 A BC D E F G H 0210704.7 015 SESESW 02 0593.4 015 SENwsE 33)0661.0 015 szESE 1 J L M 13 VAC- El \ 2056621065N04E010242.729 2451821065N02w021642.524 2267621065N03w013342.557 0947721065N028010142.544 0599321067N06w050542. 898 0315421067N06w071242 899 0389621067N06w081642 874 1133021067N07w053342. 920 0173721067N08w051843. 042 0264821067N08w053043.018 0261921067N08W061043.066 0313521067N08w082943. 030 0352821069N215050944.180 1548121069N22E053344. 202 1216321069N228080144. 282 1073221069N23E052944 298 1063221069N23E093342. 504 0286921087N085111743. 062 0376821073N13wo50343. 512 0276021073N15W041243. 311 21992210755015126 42. 311 05739210755038023142. 127 1944421075804E021342. 074 o978121075501W033442. 294 0988121075502W010842. 275 1948221075803w030242.194 21514210755048010942.092 2153421075804wo20842.096 0687521075504w021342.081 2143921075504W032042.064 2057221077501w102742.324 0731321077501w111342.371 0686321077301w121942.342 0641321077so2w090542.300 0670421077502W103642.224 0506221077802w122642.248 0687621077503w090842.190 0718621077804w100642.121 0644221077SO4W123142.052 1612121079N25W063144.449 1465921079N25w082744.461 1732821079N26w083344.535 2418221079N27w052944.623 2463321079N28w061144.750 0710321081N05w092342.778 2138821081N05w102142.779 0660321081N05w103042.768 0696021081N05W111042.806 0498921081N W121442.794 1673421081N06w091242.899 0847 2108 N0 W101 42.882 0615221081N0 W112 42.860 0369121 81N0 w092 42.931 0916 1 81N07 123042-941 A 8 C C) E F C3 84.276 84.515 84.404 84.244 84.866 85.025 0110942.16D158$ESWNW 0100916. ORBIS9NENENE 0170915.0981605ESWSW 0090898.4GD161$WSE5W 0070772. OGD162CESWSE 0090846. OGD1635WSWNE 85. 20 00160874. OGDI64NWNESW 84.848 84.880 84.890 84.922 85.218 83.810 83.818 83.357 83.841 83.312 83.215 84.821 84.253 84.253 84.219 84.124 84.621 84.423 84.600 84.412 84.532 84.468 84.534 85.398 85.492 85.698 85.332 85.410 85.615 85.338 85 462 85.702 85.000 85.137 85.171 84.856 84.915 85.270 85.304 85.455 85.522 85.619 85.26 85.39 85.49 85.26 85.68 H 0100676. 280165N N NE 0051101.0801665E8E5E OO70758.6GD167NENESW 0030856.280168NW5WNw 0090900. 4GDIé9SWNWNW 0180794. 4GD17ONWNWNE 0120784. 36D171NENWSW 0150603.86D172NENWNE 0080893.SGDI73CNSWNW 0330591.4GD174SESWSW 0180936.1801755ENwsw 0070883.6GDI76NENESE QO40760.0GDI77SESESE '14 922.7RBI78NENWSE 0100963.7GDI79SENWNE 111012.3RF1805ESWSE 0111004.0GD181NESWSW 0130990.1601820‘NENE 90974.6981830 NEsw 0181034.8RE184NENEsw 0101034.0601855ESWNE 0061001.880186NE3ENw 0091001.860187NwNw8w 0100916.0R8189NESESE 0110952.50019oc NESW 0170744.8 1913Wswsw 0120872.BGD192NWNENW 0110882.36D193CSSWNW 0180985.86D194NWNENW 0100923.4801958wNwsw 0080874.260196SENWSE 0150893.3GD197NWNwsw 0081135.788198NWSESW 0131020.1GD1995E5E3E 0101075.3GD200NE3ENE 91188.6RBEOINESESE OO71282.5RBZOZNWNWSE 0120821.4GD203NWNWSW 0130782.2RBZO4SWSWNW 0160800.0602058E3ENw 0130755.260206$ENESW 0090705.580207SWNEsw 0200635.7GDZOBNENWNW 00 0774.38 20 SESENE 01 0731.70 210NENENE 0140656.1 2115ESESE 0150738.56 ZIECESESE I J 1< L. 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0190827.2GD404$ESENE 0190844.0GD405NENWNE 0220758.0GD406NWNWNW 0150740.060407 stw 15 811.260408 SWNE 16 745.080409C SESE 17 741.060410NwNWNE 16 706.060411C SWNE 18 873.160412’ NEsE 22 733.780413NENESE 22 730.560414NWNWSW 22 759.380415c NENw 20 666.760416NESWSE 31 773.260417SESWNW 22 738.560418NWNWNW 22 598.1604IQSWSWNW 21 598.060420NWNWNW 18 634.7GD4ZISWNENW 21 666.660422NWSWSE 14 582.080423Nw5ENw 16 605.860424SWSWNE 7 770.700425NwNw3E 179 c G 1598 2.373 1595 2. 255 1598 2.154 1815 2. 382 1813 2. 205 ,1513 ~2'105 18777211815 45 42842.145 2292211518 45 62842. 058 11341211835 25 71242. 278 2561211535 22 8 542. 288 2674221165N21w101344 r74 919821165N23W103544 289 117721165N23w112644 384 38752 117N 9w 81244. 289 285721117N11w 53543. 285 447721117N10w 73143.180 239521117N10w 5 243.247 1408821117N 9w 52843.105 919021117N18w 71143. 235 1485421117N10w 6 343. 280 H 85.889 85. 781 85.734 83.724 83.958 83.792 83.958 83. 728 83. 556 83. 551 85.357 85. 371 85. 499 85.372 84.814 85. 1'10 84. 799 54 $12 359028 84-945 1 a K L M 6 750.550 26$ESUSE 8 720.1 D 27SENWNE 7 904.080 2 NENWSW 9 951.59823353wNw 8 9 1 3 7 918.268.3 SESWSW 947.8984315wNesw ” 859.1884azcwsw3w , 785.0804338552Nw 11 818. 38043452N2Nw 11 821.4804355wswsw 131354. 8RF436SESENE 131485. 480437cwsaNE 71186. 080438553wNw 11 815.180439N5Nwsw 8 806.66044OSWNWSE 18 887. 3804415wsws82 ‘9_787.0584425wsw55 7 749.2604435WSWNW 15 888.430444058582 27 897. 280445NwNwNw I80 I‘ll 18] Well Records: The following is a record of the wells used in the interpretation of the problem. Originally, all the eighty columns were used, but in this reproduction the permit number, elevation and the number of litho- logies in a given unit have been left out because of lack of Space. The first two of these appear in Appendix Ilbt The third can be counted on each line. The information as grouped into twenty-six columns as follows: B C D E F G H I a K L M N 0 P Q R S T U V W X Y Z I F —+— OJ - (U m i '0 :r O L. \— s. L U a) :1) <1) a) a) .o .o .0 .o +4 0.) m 'U E E E E '- 0 41) o :1 3 3 3 C C ~— 0 C C C C :s L Q) L a) a) a) a) .. m g a) g a on g m > cn > m ‘ Cl-i—~ .Q m i to to m to CD to a) I .- o 44 o u o 4.1 o ‘i—J D 0 g m E 4—1 - C 4—2 — C u — C u -— C u u— E C a) r0 0 a) C L 0 <1) C L 0 <1) C L o (D C L- O 0 '0 4—1 E .C 0 <1) 0 .C U (D o .C U a) o ..C U a) o +2 -— L m L- u L E (U -— +4 L E 0) ~ +4 1— E (D -— u L E (u -— c.» -— (u > o -— (D (D :1 o -- <1) 0) :3 o -— G) <1) :3 o -— a) '1) 3 o o o a) Q m LI. ...: a. c.) :l: o ,J o. c.) I c.) _I o. 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931070 1031065 1131060 1231060 1331060 1431060 1531060 1631060 1731060 1831060 1931040 2031040 2131040 2231040 27 70 2 9540 9871 60 000 7060 80 00 00 22 70 22 9540 H I J K L M N 0 P Q R 64 98606266 66 95406266 65406265 131080022100436265 231070002055436265 33107000208571 431070 531070 631070 731070 831070 931060 1031060 1131060 1231060 1331060 1431060 1531060 1631060 1731060 1831040 205571 2 9071 2 6571 66 2 80606266 27 9511 27 6560 2 90 2740 325 310 330 3 5 2610 3435 2030 230 27 5 27 2 27 2 2640 2730 27 5 2735 32040 67 2740 2740 112550 69 111550 69 3430 3430 41 5 2745 2715 2745 2710 2735 272060 50 5606366 23560 66 271060 271560 3 5 340 330 2740 310 4125 320 32060 66 283 S T U V W X Y Z l 0174401754412 0175401770412 0177001810412 0181001878412 0187801908412 0190801940412 0194002050412 0205002084412 0208402090412 0209002100412 0210002104412 0210402128412 1595413 1600413 1616413 1632413 1646413 1654413 1661413 1674413 1710413 1725413 1734413 1738413 1756413 1771413 1771 1780413 1780 1790413 0179001833413 1800 1812413 1812 1830413 1830 1995413 1995 2020413 2020 2048413 1530 1595 1600 1616 1632 1646 1654 1661 1674 1710 1725 1734 1738 1756 1748414 1754414 1762414 1770414 1810414 1815414 1830414 1835414 1840414 1845414 1880414 1895414 1915414 1958414 1998414 2022414 2030414 2090414 1710 1748 1754 1762 1770 1810 1815 1830 1835 1840 1845 1880 1895 1915 1958 1998 2022 2030 B C D 1931040 2031040 2131040 2231040 131088 231080 331070 431070 531070 631070 731070 831060 931060 1031060 1131060 1231060 1331060 1431060 1531060 1631040 1731040 1831040 1931040 2031040 2131040 2231035 131080 231070 331070 431070 531065 631065 731060 831060 931060 1031060 1131060 1231060 1331040 1431040 1531040 1631040 1731040 1831040 1931040 2031040 131080 231080 E F G 22100 26100 22 40 22100 22100 21100 2 80 210043 H I J K L M N O P Q R 2630 3430 2220 64 2 90436265 2710 2 95436265 27 5 2 9043 27 85 27100 27 7070 27 65 27 60 27 8570 27100 23100 22100 26100 24100 34 75 23100 40 55 21100 2100 27065 2 85 2 65 27 65 27 85 27100 27 90 27100 27 80 27 95 22100 21100 20100 26100 26 65 25100 26 50 26 90 22100 21100 64 2710 215 230706365 235 240 21570 4025 2135 2610 235 6265 2715 6265 2735 235 215 6265 6265 6265 31011 32011 3 511 3435 2025 4125 4110 284 S T U V W X Y 2090 2135 2235 2250 1715 1720 1780 1790 1820 1830 1840 1850 1860 1874 1885 1950 1958 1964 1994 2035 2080 2180 2230 2235 2245 2275 1552 1595 1600 1621 1680 1694 1714 1720 1766 1804 1826 1830 1860 1882 1920 1930 1946 1965 Z 1 2135414 2235414 2250414 2285414 1720415 1780415 1790415 1820415 1830415 1840415 1850415 1860415 1874415 1885415 1950415 1958415 1964415 1994415 2035415 2080415 2180415 2230415 2235415 2245415 2275415 2290415 1595416 1600416 1621416 1680416 1994416 1714416 1720416 1766416 1804416 1826416 1830416 1860416 1882416 1920416 1930416 1945416 1965416 1990416 0199002100416 2100 1728 1740 2106416 1740417 1740417 F'T—f 1 -'—:.‘_—‘L_“-_- 52*” B C D 331080 431080 531070 631070 731070 831070 931070 1031070 1131070 1231070 1331070 1431070 1531070 1631070 1731065 1831060 1931060 2031060 E F G H 1 20100 22100 3100406265 27 9011 2 95406366 2100716366 210071 64 52 5070 2100716366 52 5070 2100516366 2 90 3100116265 3 6550 50 70 3 66 27100 2610050 J K L M N O P Q R S T U V W X 310 27 5 275070 275070 2710 2635 2715 31550 Y '1749 1760 1778 1788 1800 1818 1830 1858 1868 1872 1894 1899 1904 1920 1930 1940 1955 1980 Z 1 1749417 1778417 1788417 1800417 1813417 1830417 1858417 1868417 1872417 1894417 1899417 1904417 1920417 1930417 1940417 1955417 1980417 1995417 B C D E F G H I J K L M N 0 P Q R S T U V W X Y Z 1 2131060 27100 1995 2010417 2231060 2710050 2010 2030417 2331060 2710011 2030 2056417 2431040 24100 2056 2066417 2531040 22100 2066 2078417 2631040 24100 2078 2100417 2731040 25100 2100 2175417 2831040 22100 2175 2200417 2931040 23100 2200 2240417 3031040 22 65 2620 2240 2270417 3131040 22100 2270 2314417 131080 2210060 1310 1376418 231070 3 6560 273560 1376 1390418 331070 210043 1390 1405418 431070 1405 1410418 531070 210051 1410 1450418 631070 2 75 4025 1450 1470418 731060 43 85 2715 1470 1480418 831060 43 60 2740 1480 1490418 931060 27 95 43 5 1490 1510418 1031060 27 70 4330 1510 1520418 1131060 27 75 4325 1520 1530418 1231060 27 85 4315 1530 1540418 1331060 43 70 2730 1540 1550418 1431060 27 75 4325 h 1550 1560418 1531060 43 90 2710 1560 1580418 1631060 27 65 4035 1580 1600418 1731060 27 90 4110 1600 1640418 1831040 26100 1640 1660418 1931040 22100 1660 1690418 2031040 26100 1690 1830418 2131040 26 70 4130 1830 1850418 286 . o“,".-':" --"o"'" ' 1H,. B C 0 2231040 131080 231080 331070 431070 531070 631070 731070 831070 931070 1031070 1131060 1231060 1331060 1431040 1531040 1631040 1731040 1831040 1931040 2031040 2131040 2231040 131080 231080 331080 431070 531070 631070 731060 831060 931060 1031060 1131060 1231060 1331040 1431040 1531040 1631040 1731040 1831040 1931040 2031040 2131040 131080 231080 331080 431070 531070 631070 731070 E F G H I 22100 24100 310040 9840 90 9571 8540 NNNNN 2 8540 27 9O 52 6060 26100 22100 24100 24 50 24 70 21100 22100 22 85 23 95 22100 22100 3 98 27 65 2 9571 2710070 2 60 2 9571 27 8560 2710060 27 45 24100 21100 24100 23100 26100 24100 22100 22 55 22 95 22100 20100 22100 3 8540 210071 210070 310060 64 55406265 66 66 66 66 66 66 66 66 64 66 66 J K L M N O P Q R 2745 50 260 2710 27 5 2715 66 2715 501060 2740 66 2250 3430 4115 41 5 27 2 235 27 5 512060 66 272060 27 5 501060 66 60 5 504560 6010 2645 41 5 2715 287 S T U V W X Y 1850 1360 1400 1405 1410 1435 1460 1470 1476 1490 1505 1508 1582 1606 1615 1623 1629 1690 1836 1852 1870 1882 1894 1400 1440 1445 1447 1456 1465 1500 1505 1510 1530 1600 1640 1650 1660 1674 1690 1770 1814 1830 1910 1924 1565 1576 1590 1624 1628 1634 1638 Z 1 1882418 1400419 1405419 1410419 1435419 1460419 1470419 1476419 1490419 1505419 1508419 1582419 1606419 1615419 1623419 1629419 1690419 1836419 1852419 1870419 1882419 1894419 1910419 1440420 1445420 1447420 1456420 1465420 1500420 1505420 1510420 1530420 1600420 1640420 1650420 1660420 1674420 1690420 1770420 1814420 1830420 1910420 1924420 1959420 1576421 1590421 1624421 1628421 1634421 1638421 1646421 B C D 831070 931060 1031060 1131060 1231040 1331040 1431040 1531040 1631040 1731040 1831040 131080 231070 331070 431070 531070 631065 731060 831060 931060 1031060 1131060 1231060 1331060 1431060 1531060 1631040 1731040 1831040 1931040 2031040 2131035 131080 231070 331070 431060 531060 631040 731040 831040 931040 1031040 1131040 1231040 1331040 1431040 131080 231080 331080 431070 E F G H I J K L M N O P Q R 210071 64 2710070 27100 2710040 22100 26100 22100 26 60 22100 26100 22100 2220 21100 2 7540 64 2725 2 95406265 27 5 3 95 27 5 3 55 2745 27 96 3 4 27 85 315 27 60 340 27 90 310 27 98 3 2 5010011 66 27100 2610050 27100 22100 24100 22100 22 50 22 55 22 55 2035 2645 4145 210040 2710040 20100 21100 22100 41 65 3420 22100 21100 22100 20100 2100406265 3420 3415 2215 2&3 S T U V W X Y 1646 1690 1740 1780 1874 1896 1976 2070 2104 2120 2136 1376 1445 1460 1513 1525 1530 1580 1590 1600 1614 1624 1680 1690 1700 1715 1730 1755 1900 1912 1938 1986 1500 1545 1555 1575 1580 1720 1725 1780 1810 1815 1946 1952 1980 1985 1580 1593 1620 1635 Z 1 1690421 1740421 1780421 1874421 1896421 1976421 2070421 2104421 2120421 2136421 2150421 1445422 1460422 1513422 1525422 1530422 1580422 1590422 1600422 1614422 1624422 1680422 1690422 1700422 1715422 1730422 1755422 1900422 1912422 1938422 1986422 1992422 1545423 1555423 1575423 1580423 1720423 1725423 1780423 1810423 1815423 1946423 1952423 1980423 1985423 2030423 1593424 1620424 1635424 1658424 B C D 531070 631070 731060 831060 931060 1031060 1131060 1231040 1331040 1431040 1531040 1631040 131050 231050 331050 431045 E F G H I 2 9550 2 80436265 27 65 2610060 2710060 27100 27 60 24100 25100 25 80 20100 22 55 28 65 28 60 28 55 28 50 5310040 22100 631040 731035 131050 231050 331050 431050 531045 631040 731040 831040 931040 1031035 131050 231050 331050 431040 531040 631035 131050 231050 331050 431045 22 65 34 70 28100 28 90 28 80 28 55 21 85 22100 21100 34 60 29100 28 40 22100 26100 34 60 28190 31100 28 4o 28 4o J K L M N O P Q R 27 5 2720 235 2640 3420 2145 1135 1120 3025 2135 2135 4030 3010 3020 2145 2815 4040 3130 4040 2930 2240 S T U V W X Y 1658 1690 1709 1725 1759 1774 1806 1824 1840 2060 2078 2103 727 1024 1099 1171 1177 1280 1297 3020 2120 3015 600 612 622 960 990 1020 1037 1055 1145 1170 630 680091 3030 910 1045 1130 1155 650 680 3030 850 3020 1050 289 Z 1 1690424 1709424 1725424 1759424 1774424 1806424 1824424 1840424 2060424 2078424 2103424 2130424 1024425 1099425 1171425 1177425 1280425 1297425 1330425 612426 622426 960426 990426 1020426 1037426 1055426 1145426 1170426 1221426 680427 0427 1045427 1130427 1155427 1170427 680428 850428 1050428 1075428 B C D 531040 631040 731040 131080 231070 331070 431070 531070 631060 731040 831040 931040 131080 231070 331070 431070 531065 631065 731065 831065 931060 1031060 E F G H I 25100 21100 22100 210043 64 2 95 210040 64 3 75406265 27 9511 26100 21100 25100 22100 2100516266 2 85516265 2 8540 64 27 9011 27 50 3 70 3 50 3 6O 27 9011 113104025100 1231040 1331040 1431040 1531040 1631040 131080 231070 331070 431070 531060 631060 731040 831040 931040 131080 231070 331065 431065 531060 631060 731040 831040 931040 1031040 1131040 20100 26100 20100 24100 26100 22 85 2 9540 64 2710011 2 8040 64 27 9069 65 2710040 25100 20 50 26100 3 6040 64 3 5540 64 27 6011 27 8011 271011 2610011 40100 2610011 34100 26100 J K L M 27 5 2720 51 5 5015 3 2715 31011 350 2730 2750 2740 21011 31543 27 5 2720 21050 2625 274011 274511 34040 32040 N O P Q R 11 5 64 65 4325 64 64 290 Y 1075 1145 1145 810 825 895 905 930 970 1020 1120 1165 692 697 700 705 725 735 745 755 770 805 845 955 970 975 985 990 660 675 700 715 740 800 825 938 970 745 760 770 780 795 810 850 880 890 960 970 Z 1 1145428 1175428 1225428 825429 895429 905429 930429 970429 1020429 1120429 1165429 1190429 697430 700430 705430 725430 735430 745430 755430 770430 805430 845430 955430 970430 975430 985430 990430 1025430 675431 700431 715431 740431 800431 825431 938431 970431 1005431 760432 770432 780432 795432 810432 850432 880432 890432 960432 970432 1010432 B C D 131040 231040 331040 131080 231070 331070 431070 531070 631060 731060 831060 931040 1031040 1131040 131080 231080 331070 431070 531070 631070 731070 831070 931060 1031060 1131040 131080 231050 331050 431050 531050 631050 731050 831050 931045 1031040 1131040 1231040 1331040 131080 231050 331050 431050 531050 631050 731040 831040 931040 1031040 1131040 E F G H I J K L M N O P Q R 24100 2010040 2110040 2210050 210051 65 2 75406265 2725 2 80 27 9011 2710011 27100 3 21100 22100 26100 22100 3100 27 60 2 75 2 90 310040 2710050 22100 22100 29 55 32 60 31 60 28 5O 30 9040 29 65 26 50 21100 24100 21 75 2610040 21100 28 70 30 50 30 5550 28 5050 28 65 21 85 2510040 2010040 20100 21 40 2720 210 240 2725 2710 5145 3040 3220 3030 3110 3035 3050 3425 2930 334040 283050 2930 2920 2815 2030 5120 2120 2910 5115 3020 3015 2630 291 S T U V W X Y 119 170 175 210 235 275 280 294 353 383 420 453 460 537 210 265 270 275 295 306 320 335 345 380 430 2275 2290 2325 2358 2395 2450 2800 2810 2860 2880 2895 3025 3070 2280 2300 2400 2540 2600 2710 2820 2840 2880 2890 2960 170433 175433 218433 235434 275434 280434 294434 353434 383434 420434 453434 460434 537434 585434 265435 270435 275435 295435 306435 320435 335435 345435 380435 430435 566435 2290436 2325436 2358436 2395436 2450436 2800436 2810436 2860436 2880436 2895436 3025436 3070436 3145436 2300437 2400437 2540437 2600437 2710437 2820437 2840437 2880437 2890437 2960437 3005437 B C D 1231040 1331040 131080 231050 331050 431050 531040 631040 731040 131070 231040 331040 431040 531040 631040 731040 831040 931040 1031040 1131040 131080 231060 331040 431040 531040 631040 131080 231040 331040 431040 531040 631040 731040 831040 931040 1031035 131040 231040 331040 431040 531040 631040 731040 831040 931049 131040 231040 E F G H I J K L M N 0 P Q R 22 85 34 70 00000 28 85 29 65 2110040 20 50 2610040 20 6011 22100 22 90 22100 22100 21 60 24100 2110040 00000 22100 20100 22100 22 85 21 80 22 90 22100 31 60 25 65 22100 24100 34 70 22100 21 70 22100 22 90 22100 23100 24 85 22100 24100 26100 2615 2030 2915 2835 3425 2140 2110 3440 3415 112040 3110 2240 2135 2030 4130 2010 2215 4125 292 S T U V W X Y 3005 3080 1660 1700 1725 1950 2250 2415 2430 2244 2251 2260 2270 2290 2315 2366 2540 2576 2580 2620 2230 2250 2270 2295 2310 2630 2215 2230 2300 2400 2460 2520 2580 2630 2645 2686 2278 2300 2315 2350 2370 2446 2456 Z 1 3080437 3100437 1700438 1725438 1950438 2250438 2415438 2430438 2490438 2251439 2260439 2270439 2290439 2315439 2366439 2540439 2576439 2580439 2620439 2654439 2250440 2270440 2295440 2310440 2630440 2710440 2230441 2300441 2400441 2460441 2520441 2580441 2630441 2645441 2686441 2725441 2300442 2315442 2350442 2370442 2446442 2456442 2494442 0249402656442 2656 2225 2255 2715442 2255443 2485443 B C D 331040 431040 531040 631040 731040 131080 231050 331040 431040 531040 631040 731040 831040 931040 1031040 1131040 1231040 1331040 E F G H I J K L M N O P Q R 25100 24100 34 45 22100 2110040 20100 20100 22 85 2010040 22100 21100 26100 22100 21 85 22100 2310070 22100 1431040 21 85 1531040 131080 231080 331040 431040 531040 631040 731040 831040 931040 1031040 1131040 1231040 1331040 1431040 1531040 1631040 1731040 1831040 1931040 2031040 2131040 2231040 2331040 2431040 2531040 2631040 2731040 F RUN 22 80 20 70 22100 22100 22100 22100 21100 20100 2010040 22 90 24100 22100 22100 25100 22100 24100 22100 22 85 4135 2015 2015 2215 3410 2230 2010 4115 293 2120 4010 S T U V W X Y 2485 2500 2543 2570 2584 2290 2296 2306 2365 2442 2464 2505 2515 2545 2580 2605 2615 2625 2650 2700 2384 2410 2415 2430 2436 2452 2483 2526 2534 2550 2558 2576 2584 2600 2616 2642 2670 2674 2680 2710 2728 2736 2750 2760 2776 2800 2827 Z 1 2500443 2543443 2570443 2584443 2602443 2296444 2306444 2365444 2442444 2465444 2505444 2515444 2545444 2580444 2605444 2615444 2625444 2650444 2700444 2800444 2410445 2415445 2430445 2436445 2452445 2483445 2526445 2534445 2550445 2558445 2576445 2584445 2600445 2616445 2642445 2670445 2674445 2680445 2710445 2728445 2736445 2750445 2760445 2776445 2800445 2827445 2850445 294 lld Card Output: Bedford-Berea Sequence: Two cards were punched for each well. The firsr had one punched in column 80 and contained the analysed data fro the Bedford-Berea sequence. The second card contained information for the Antrim, Ellsworth and Sunbury shales“ The following is a summary of the results for the Bedtord—Berea sequence. The wells left out are located in the weStern parts of the State and so show no Bedford Shale or Berea SandSLone. The results have been grouped into I} columns (A—M) as f'ollows: A B C D4 E F” G H5 I J K L M -U-ni—_— L. .0 Q) 1.... A C ,r\ ru "0 (1) ° 0 (U fl) (D — ‘4—- 1—1 (1) \- (U no ('0 'U U] L O Q) /-\ ll) .1: 0) '0 cu .- m a 1. C m an 1: no u l u a) -—- /'\ /'\ \_/ ('0 ~_/ (U 'C 9- m (I) a) 13 m 1. L. V A (1) cu <1) L c C o +4 C 1: m L o o m o w W w W- -— o 1. 01 u— -— <1) .— — U c \-/ 4—1 m <1) '0 H x— 4.» m (I) o (D tn (D ‘0 CD 11) G) (U .C m H -— ‘0 'D V (O > m > V) U1 0) (D C \— \_/ . a q) o 6 Q) a . o u ‘0 ,— .C {U a) Cl) 11) -— m — Cl) U) C ru 61‘ U) .0 Cl) '0 (h a) m (D C as m .C E "o :1 0) OJ 0 a) tn tn .2 u :1 3 w 1: r0 1: m +4 c c 1: z 1—1 -— x (U .1 (U W x "— '- Q’ (D -- 01 U tn U m 'U U m m U U r- 4; C ._ _Q ._ _Q C ... 1.) 1.; 1. 1. —~ m o I 3 .5 3 m L o _o m w m .1 .1 i— nn i—v U) m D-m i- 1-- o. o. 3 *When a formation 15 absent In a given well the negatlve of the elevation (see Appendix llby column 5) is recorded in this column. Such information was discarded when plotting the structure contour maps. 295 A l B 0 E F G H 1 J K L Mf 4405977830568 365.0 +96o7l 5000 +146o7l0013795 41500 50.0 0.0 0.0 000 ll 44.59283o569 .23.0 +47.“ 147.5 +92.3 6.164 170.5 146.7 23.8 0.0 0.5 2 44.648336307 66.0 +319.0 74.0 +393.0 3.895 140.0 74.0 19.0 0.0 0.0 3' .44.649fi3.504 100.0 +277. 94.8 +392. 0.948 194.7 94.8 100.0 0.0:. 0.0 4 44.65233o28 18.8 +469.0 23.3 +469. 1.240 42.1 23.3 18.8 0.0 0.0 06 43.64585.792 28.5 -315.6 0.0 +734.4 0.0 28.5 0.0 28.5 0.0 0.0 11 44.80284.942 0.0+1104.1 40.0 +354.1 0.0 40.0 40.0 0.0 0.0 0.0 23 43.90283o958 94.0 —861.9 71.00 —817.9 0.755 165.0 71.0 74-0 28 43.95283.779 37.0-4050.1 163.0-4050.1 7.590 200.0 159.4 21.0 0.0 0.0 29 44.01884.084 62.2 -831.9 75.8 -801.9 1.060 138.0 71.0 67.0 0.7 6.9 30 43.93984.064 426.4 -806.9 76.0 -806.9 19.976 502.4 478.4 23.9 94.4 0.0 31 43.95684.129 61.3 '916.5 90.7 -882.5 1.736 152.0 82.1 47.3 3.3 0.0 32 43.96184.128 69.0 -987.0 40.8 -936.0 0.591 109.8 47.7 62.1 10.0 0.0 33 44.02183.982 50.0 -806.7 97.3 —734.7 1.946 147.3 74.6 63.0 3.0 14.9 34 43.99683.956 81.9 "731.4 76.1 —717.4 0.643 158.0 52.7 81.9 0.0 0.0 35 44.00283.986 69.4 -759.3 63.5 —681.3 0.593 132.9 63.3 66.5 1.4 0.0 36 43.97083.952 107.0 -755.5 98.8 —722.5 1.273 205.8 115.3 90.5 15.4 0.0 37 44.01783.940 95.0 -987.9 106.8 -872.9 1.124 201.8 106.8 0.0 0.0 0.0 38 44.061846070 88.0 ‘804.7 68.0 .194.7 0.930 156.0 66.0 71.0 3.4 0.0 40 44.04684.069 39.2 “828.0 87.8 -J78.0 2.236 127.0 87.8 39.2 0.0 0.0 41 44.09483.894 72.8 -575.0 75.2 -675.0 1.011 3 148.0 71.6 70.8 2.7 0.0 42 42.64185.339 23.4 :587.8 0.0 +796.2 0.0 23.4 0.0 23.4 0.0 0.0 44 42.73185o177 0.0 +880.4 30.0 ‘849.6 0.0 30.0 30.0 0.0 0.0 0.0 45 >44.60483.942 29.4 '911.8 121.5 -870.8 1.240 150.9 83.5 67.4 2.6 31.9 48 43.58283.935 41.6 -921.0 136.1 —9l3.0 3.275 177.7 136.1 41.6 0.0 0.0 49 43.59083o9l6 95.7 -969.8 124.3 —924.8 1.926 220.0 144.8 75.2 21.4 0.0 50 43.57583.738 52.4 4204.5 122.7 3199.5 3.398 175.1 135.3 39.8 31.2 3.1 51 43.56283.760 111.6 -928.2 73.4 _928.2 0.6613 185.0 80.9 104.1 6.7 0.0 53 43.61483.962 77.8 ‘963.1 170.6 '873.1 2.220 ~ 248.4 171.3 77.2 2.6 0.8 54 ‘43.61933.95O 93.6 -950.2 95.3 -945.2 1.363 189.0 109.0 80.0 14.6 0.0 55 43.83484.239 34.9 4414.5 87.8 4414.5 2.777 122.8 90.3 32.5 6.9 0.0 56‘ '43.83484.089 78.0 945.9 70.0 —94l.9 0.942 148.0 71.8 76.2 2.3 0.0 57 42002931290815 2700 -10202 000 +96508 0.0! 2700 000 2603 0.0 0.0 64 42.030859061 50.0 -21.7 0.0 +928o3 0.0 50.0 0.0 30.0 0.0 0.0 65 41.88985.252 0.4 +146.3 3.0 +166.3 0.0 3.4 0.0 3.4 0.0 100.0 67 42.25884.742 ‘0.0 +955.3 23.0 ‘444.7 6.67 23.0 20.0 3.0 0.0 13.0 70 42.20884.738 24.0 ~375.5 0.0 +974.5 0.0 24.0 0.0 24.0 0.0 0.0 71‘ ’42.27484.812 15.0 -458.6 5.0 "438.6 0.0 20.0 0.0 20.0 0.0 100.0 721 42.26284.930 0.0 +963.5 9.0 -361.5 0.0 9.0 0.0 9.0 0.0 100.0 73 42.19384.578 46.0 ~407.5 0.0 +991.5 0.0 46.0 0.0 46.0 0.0 0.0 75 42.17585o055 0.0 +923.6 1.0 ‘176.4 0.0 1.0 1.0 0.0 0.0 0.0 77' 42.08285o218 9.9 466.4 1.2 —14.4 0.0 11.1 0.0 11.1 0.0 100.0 84' 41.75285.984 2.4'+345.7 0.0 +791.7 0.0 2.4 0.0 2.4 0.0 0.0 87 42.289830472 66.0 +567.1 46.0 +613.1 0.697 112.0 46.0 66.0 0.0 0.0 89 43.80044.710 50.0?6275.0 0.0+8800.0 0.0 50.0 0.0 50.0 0.0 0.0 97: 42.77084o413 44.5—1234.2 49.5-4222.2 1.178 94.0 49.5 42.0 5.5 0.0 98 42.77084.596 39.5-4221.1 6.5-1221.1 0.185 46.0 6.0 32.5 0.0 0.0 99: 42.83984.418 62.0-4256.0 24.0-4264.0 0.523 86.0 29.0 55.4 10.6 0.0100' 142.90684.416 55.0-1217.6 126.(" 2.620 181.0 131.0, 50.0 9.1 0.0101 42.93904.478 42.4~1276.2 25.6—1266.2 0.825 68.0 30.2 36.6 13.7 0.0102 42.94234.731 18.0 4336.8 0.0 #728.2 0.0 18.0 0.0 18.0 0.0 0.0103 43.07584.396 50.1 4352.5 9.9-1352.5 0.198 '60.0 9.9 50.1 0.0 0.0104 43.01984.516 27.2-1305.0 12.8-1305.0 0.538 40.0 14.0 26.0 4.4 0.0106 43.01284.665 7.0'1393.8 0.0 +734.2 0.0 7.0 0.0 5.9 0.0 0.0107 A B c D E F G H I J K 1. M 1- 43.022.84.712 71.0r‘1122.2 6.4‘1106.2 0.179 77.4 11.0 61.4 6.51 0.0E08 43.005;84.755 9.0-1371.7 0.0 4764.3 0.0 9.0 0.0 9.0 0.0; 0.0 09 42.41.984.710 0.0 +932.0 1.3 -752.0 0.0 1.3 0.0 0.0 0.0 0.0 10 42.519384.902 35.0 "731.8 0.7 6716.8 0.0 35.8 0.0 35.8 0.0 100.0111 42.79284.456 17.0—1269.3 27.1—1266.3 2.099 44.1 25.4 12.1 8.2 0.0 12 42.63684.758 23.0 ”999.0 0.0 +866.0 0.0 23.0 0.0 23.0 0.0 0.0113 42.86584.802 148.0 ”590.4 58.3 -563.4 0.478 206.3 65.7 137.6 5.9 2.3115 043.108.95.975 131.7-1023.2 113.2 -981.2 0.6040 244.9 90.4 149.7 0.0 15.9116 43.16885.195 89.5 ‘493.5 100.5 ‘493.5 1.123 190.0 100.5 89.5 0.0 0.0117 43.80084.524 51.3-1388.0 78.2-1378.0 1.765 129.5 78.2 44.3 0.0 0.0118 43.79684.529 75.7’1375.6 53.3 —1375.6 0.728 129.0 52.5 72.1 4.8 0.0119 43.89284.620 368.0 ~912.0 30.8 —879.0 22.877 398.8 382.0 16.7 95.5 0.012 43.93584.344 31.8 -1540.2 47.3 —1540.2 1.362 79.0 45.5 33.4 0.0 3.6121 43.92084.470 62.7 -l480.0 38.3—1460.0 0.595 101.0 .37.3 62.7 0.0 0.0122 43.92184.354 215.8—1495.4 3.0 -1492.40.246 218.8 11.0 44.6 3.7 0.0123 43.92584.346 43.0-‘1534.6 72.0 -1462.6 1.674 115.0 72.0 0.0 0.0 0.0124 43.92684.335 28.0’1591.3 74.4 -1479.3 2.850 102.4 75.8 26.6 5.0 0.0125 43.87984.541 25.8—1521.5 52.2,-1480.52.164 78.0 53.3 24.6 4.3 0.0127 43.94084.540 20.0 -1747.0 13.0—1709.0 0.650 33.0 13.0 20.0 0.0 0.0128 43.98884.539 22.0—1628.0 0.0 +854.0 0.0 22.0 0.0 22.0 0.0 0.0129 44.03684.500 82.0-1436.6 0.0 +813.4 0.0 82.0 0.0 82.0 0.0 0.013C 43.13684.435 31.7—1422.7 7.6~1422.7 0.267 39.3 8.3 31.0 2.2 0.0134 43.12684.560 30.0-1403.7 20.0 —l403.70.667 50.0 20.0 30.0 0.0 0.0135 43.21984.558 34.5-1482.9 25.5—1482.9 0.951 60.0 29.0 30.5 11.6 0.0136 43.23484.772 35.0-1547.0 0.0 +773.0 0.0 35.0 0.0 20.0 0.0 0.0137 41.95284.653 21.0 -21.0 0.0+1122.0 0.0 21.0 0.0 18.9 0.0 0.0136 420006840796 15.0 "9800 1.03 ”7100 00053 16.4 007 1403 500 000139 41.93284.688 13.0 +3.0 0.0 +1095.0 0.0 .0 0.0 0.0 0.0 0.0 14C 41.84284.565 17.0 +83.8 0.0+1107.8 0.0 17.0 0.0 17.0 0.0 0.0141 41.83884.596 14.0 +139.4 0.0+1217.4 0.0 14.0 0.0 14.0 0.0 0.0142 41.06984.315 20.0 4220.8 55.0 4275.8 2.750 75.0 55.0 20.0 0.0 0.0143 41.76.284.695 59.5 +344.2 0.0+1094.2 0.0 59.5 0.0 59.5 0.0 0.0144 41.71484.696 45.0 +306.1 0.0+1061.1 0.0 45.0 0.0 0.0 0.0 0.0145 43.69883.344 145.6 —846.9 103.3 ~781.9 0.836 249.0 102.6 122.6 0.0 0.0146 43.65183.272 115.3 ~759.6 162.7 -699.6 1.281 278.0 151.4 118.3 0.0 1.8147 43.68483.172 68.0 -880.2 101.0 —776.2 1.649 169.0 99.6 60.4 0.0 1.4145 43.64483.l72 168.6 ~67’0.7 131.9 “661.7 0.713 300.5 118.6 166.3 0.0 10.1145 43.79683.275 118.0 '909.0 209.9 “805.0 1.721 328.0 203.1 118.0 0.0 0.015C 43.75083.172 227.6 ‘908.0 76.4 4828.00.415 304.0 82.9 199.8 2.8 0.0151 43.75182.959 139.3 -507.4 170.7 ‘462.4 1.871 310.0 183.0 97.8 9.7 0.0152 43.17283.562 0.0 +783.4 9.0 -656.6 0.0 9.0 9.0 0.0 0.0 0.0153 43.79582.722 170.9 *94.9 70.1 “-1.1 1.187 241.0 109.1 91.9 22.8 0.0154 43.87582.882 265.2 -195.3 223.8 435.3 0.792 489.0 212.4 268.1 1.7 3.3155 43.956.33.109 278.1 -632.6 135.6 ~621.62.260 413.7 258.2 114.3 47.1 6.2156 43.95182.974 296.8 -379.0 74.1 ~327.0 0.009 370.9‘ 77.5 228.4 1.1 0.0157 42.72984.276 66.0 -1122.9 45.0-1113.9 0.273 111.0 16.5 60.6 2.0 0.0155 42.52484.515 47.0 ~922.0 0.0 +916.0 0.0 47.0 0.0 47.0 0.0 0.0155 42.55784.4O 83.0 -985. 12.00 -985.0 0.157 95.0 17.75 77.75 0.016C 42.54484.244 39.2 -947.6 32.8 «929.6 0.834 72.0 32.8 39.2 0.0 0.016] 42.89884.866 10.0-1258.0 2.1 -1248.0 0.210 12.1 0.0 4.5 0.0 0.0162 42.92084.648 15.4 ~1289.8 0.0 +676.2 0.0 15.4 0.0 11.9 0.0 0.0165 +785.6 297 A 8 c D E F G H I J L M . 1 I * 44.180583.810 91.0 -989. 66.0 ~925.6 0.672 157. 62.7 93.2 0.0' 3.4170 44.20283.818 92.7 ~800. 58.3 -795.7 0.623 151.0 55.3 88.7 4.3 0.09.71 44.28283.357 109.1 -756.2 94.1 -721.2 0.831 03.2 90.6 109.1 0.0 0.0172 44.298183.841 124.5 -962.5 19.5 -962.5 0.868 144. 35.6 41.0 16.2' 0.0173 62.504.83.312 143.8 ~638.6 140.1 -558.6 1.388 83. 117.8 84.8 0.07 12.2174 43.06.263.215 77.0 ~533. 162.3 -533.9 2.110 39. 154.9 84.4 2.4] 4.5 ‘75 43.51284.821 34.0 4727.4 0.0 +883.6 0.0 34.0 0.0 34.0 0.0 0.0176 43.31184.253 35.0-1724.0 0.0 +760.0 96.976 35.0 0.0 35.0 0.0 0.0177 42.31184.253 62.0 —595.4 56.8 —547.4 0.980 118.8 58.8 60.0 3.2 0.0178 42.12784.219 35.6 —296.3 54.9 —291.3 1.910 90.5 59.4 31.1 12.6 0.0179 42.07484.124 105.0 -182.7 10.0 —172.7 0.262 115.0 23.8 91.2 13.2 0.0180 142.294.84.621 45.0 —571.o~ o.o+1ooa.o 0.0 45.0 0.0 31.0 0.0 0.0181 42.27584.423 37.8 -567.9 34.2 —567.90.905 72.0 34.2 37.8 0.0 0.0182 42.19484.600 50.0 —395.4 0.0 1974.6 0.0 50.0 0.0 47.5 0.0 0.0183 42.09284.412 72.0 —228.2 7.3 —210.2 0.145 79.3 10.1 69.3 3.8 0.0184 42.09684.532 42.0 —208.0 o.o+1o3a.oo.111 . 42.0 4.2 37.8 10.0 0.0185 42.08184.468 64.0 -228.2 o.o+1001.8 0.059 64.0 3.2 ' 54.4 5.0 0.0186 42.06484.534 30.0 -168.2 0.0+1001.8 0.0 30.0 0.0 30.0 0.0 0.0187 .43.13283.309 40.0-1142.8 15.0 —1127.8 0.0 5.0 12.75 42.25 0.0 15.0 188 42.30085.332 0.0 +872.8 6.0 —137.2 0.0 6.0 0.0 0.0 0.0 0.0192 42.22485.410 0.0 +882.3 3.9 ~5.7 0.0 3.9 0.0 2.7 0.0 69.2193 42.24885.615 10.0 —274.2 0.0 +985.8 0.0 10.0 0.0 10.0 0.0 0.0194 42.19085.338 0.0 +923.4 3.3 +3.4 -' 0.0 3.3 0.0 0.0 0.0 0.0195 44.44985.000 o.o+1135.7 45.0 4719.3 0.0 45.0 45.0 0.0 0.,0 0.0198 44.62384.856 13.0 —251.4 0.0+1188.6 0.0 13.0 0.0 13.0 0.0 0.0201 44.75084.915 75.0 +52.5 0.0+1282.5 0.0 75.0 0.0 75.0 0.0 0.0202 42.77885.27O o.o +821.4 8.0 —748.6 0.0 8.0 8.0 0.0 0.0 0.0203 42.89985.260 0.0 +635.7 20.0 —9oa.3 0.0 20.0 20.0 0.0 0.0 0.0208 42.86085.496 0.0 +731.7 1.4 —624.3 0.0 1.4 0.0 1.4 0.0 100.0210 42.93185.269 63.5 1018.9 0.0 1656.1 0.0 63.5 0.0 63.5 0.0 0.0211 42.09485.686 0.0 +738.5 6.0 4459.5 0.0 6.0 6.0 0.0 0.0 0.0212 42.92985.692 0.0 4674.6 1.3 —480.4 0.0 1.3 0.0 1.3 0.0 100.0213 43.08185.436 0.0 +873.4 7.5 —896.6 »-o.o 7.5 0.0 7.5 0.0 100.0216 43.06085.542 18.5 795. 21.8 ~22.5 0.541 28.5 10.0 18.5 0.0 0.0218 43.78285.695 0.0 +836.6 70.0 «663.4 0.0 70.0 70.0 0.0 0.0 0.0225 43.90785.498 0.0+1256.o 1.9 4984.0 0.0 1.9 0.0 1.9 0.0 100.0226 43.89485.551 16.0 7976.3 20.0 ~956.3 1.250 36.0 20.0 16.0 0.0 0.0227 44.05785.594 o.o+1o54.o 35.0 ~711.o. 0.0 35.0 35.0 0.0 0.0 0.0231 44.10385.803 0.0 +850.4 10.0 ~189.6 0.0 10.0 10.0 0.0 0.0 0.0233 42.82083.441 64.8 4265.3 18.2 ~217.3 0.516 83.0 24.2 46.8 9.3 0.0234 42.93283.349 30.9 ~453.9 202.0 4441.9 6.537 232.9 202.0 30.9 0.0 0.0235 42.98083.145 130.2-499.3 88.2 415.3 0.677 219.4 74.8 143.6 0.31 3.5 236 43.05883.367 123.2~1142.8 106.8-648.0 0.847 230.0 105.5 124.5 5 11.84237 43.22283.287 76.0 -816.1 lB6.5~642.6 2.625 262.5 187.3 75.2 2.39 238 42.015.34.109 31.5114.o5 53.5~7I+.o 1.125 85.0 45.0 40.0 18.69240 42.00083.952 111.0 1206.0 0.0 +795.6 0.293 111.0 25.3 85.70 29.3 0.0 241 41.89984.112 95.0 +218.2 0.0 +888.20.473 95.0 30.0 65.0 0.0242 41.85183.841 15.3 +563.o 40.8 +573.0 2.237 56.0 0.0 17.3 4.9243 41.84983.845 64.8 +423.o 35.2 +431.o 0.399 100.0 25.5 63.9 5.7244- 42.55283.923 48.5 +800.5 123.5 +810.5 2.546 172.0 123.5 48.5 0.0245 42.52683.904 40.5 +74.9 149.5 +74.93.935 190.0 151.5 38.5 0.0246 42.65284.042 120.0 +504.8 55.0 +559.8 0.458 175.0 55.0 120.0 0.0247 42.67883.759 85.5 965.0 156.5 +145.o 2.270 242.0 168.0 74.0 0.0248 42.46083.902 70.3 99.8 +785.6 1.586 170.0 104.3 65.8 0.0249 c ' D E F 0 H I J K L M A B 420659g20799 17800 +40205 367.0 +4520 20062 5450 36700 17800 000 000251 420712820057 11001 +12304 111.9 +123. 10016 22200 11109 11001 0.0 000253 420679820741 20502 +429. 102080 +4720 11.571 10001 30800 20709 000 207254 '420720820596 7600 +36400 000 +6220 000 7600 000 7600 000 000255 44032085082 O00 +84300 5500 —170 000 5500 5500 000 000 000258 “440329850834 501 +10203 000 +76803 000 ‘ 501 000 501 000 000259 430821850958 000 +74300 204 “35900 000 204 0.0 204 0.0 10000262 430990860294 504 ‘43703 000 +64007 030 504 000 504 000 000263 430580850090 000*101601 106-354309 000 106 000 106 000 10000268 430579850308 000+112100 10500-136400‘ 000 10500 10500 000 0.0 000270 430752850099 000+107902 000+107902 000 000 000 000 000 000273 430694850144 000+101505 1000 449605 000 1000 10.0 000 0.0 000274 430133830312 13205 —66007 9007 “60807 00845 22302 10202 12100 11.6 403276 436128830031 10306 747600 14805 ‘38100 10526 25201 14404 9406 100 304277 430464840268 5904-464602 14906-164602 20519 20900 14906 5904 000 000279 430478 40432 14900-158500 24200-134300 20863 39100 28309 9901 2801 000280 430728840375 5200'481509 5100-181509 10050 10300‘ 5208 5003 304 000281 430702840425 6503'183402 7908-483402 10222 14500 7908 6503 000 000282 430688840399 4909‘183003 58077480503 10282 10806 6100 4706 406 000283 440121850000 000+119400 19600-&30800 000 19600 19600 000 000 000284 ‘ 430253840835 000 +79806 10007153104 000 1000 1000' 000 000 000287 440832830993 3500 +29900 '000 +81700 000 3500 000 3500 0.0 000289 440907840032 4700 +58901 '000 +91301 .000 4700 000 3700 000 000291 440904840034 4500 +59400 007 +60900 l000 4508 000 3508 0.0 10000292 440898840049 3800 +54004 100 +55004 10140 3900 408 34.2 1000 000293 440908840048 5105 +56903 000 +92403 5105 000 3605 000 000294 440872830973 1600 +49706 .000 +81106 000 1600 000 800 000 000295 430128850878 000 +64701 000 +6 701 000 000 000 000 000297 430164850922 000 +66103 000 +6 103 000 000 000 000 000298 ‘430135850982 000 +64409 000 +6 409 000 000 000 000 000299 430110850986 000 +63902 000 +6 902 000 000 000 000 000300 430451850912 000 +77304 000 +7 304 000 000 000 000 000301 430126860126 000 +61801 000 +6 801 .000 000 O00 000 000302 430252850734 000 +87203 0.0 +8 203 f '000 000 000 0.0 000303 43.23085.962 0.0 +668.0 0.0 +6 8.0 ‘ ‘ 0.0 0.0 0.0 0.0 0.0304 430264860208 000 +64207 000 +6 207 000 000 000 0.0 000305 430336860069 000 463500 000 +6 500 000' 000 000 000 000306 430420860242 000 +66000 000 +6 000 000 000 000 000 000307 430308350650 500 ~89002 000 +7 508 500 000 500 000 000308 430298850654 908 ‘86600 000 48 400 908 '0.0 908 0.0 000309 430342850709 1300 779700 500 ‘7 700 1800 000 1800 000 10000310 430334850781 000 +75701 000 +7 701 000 .000 000 0.0 000311 430292850825 000 +72202 000 +7 202 000 000 000 000 000312 430438850488 1000 410508 000 +8 402 1000 000 1000 000 000313 430425850715 700 ~74804 000 +8 106 700 000 700 000 000314' 430399850818 300 ~67300 000 +7 200 300 000 300 000 060316 430479850722 700 ~85000 000 +9 000 700 000 700 000 000317 430534850532 1800-406803 000 +9 107 1800 000 1800 000 000318 43.534850522 000+100200 000+10 200 000 000 000 000 000319 430602850705 000 +97504 500 ‘8 906 500 500 000 000 000320 420454830724 000 +90607 13905 -— 803 13905 13905 000 000 000321 420406830541 5000 +60607 3000 +6 60 00600 8000 3000 5000 000 000322 420706830541 2100 457704 000 ‘9 104 2100 000 000 000 000323 9205 +61300 19205 +6 300 20295 28500 19805 8605 605 000324 42058283.578 298 ~ 6 H I ‘ J K L M A 5 C D E r . 7 l __ x ‘ ; F l 42.493183.54:{124.1 +546031 5001 '4'50603l 0.404 17402. 50.1 124.1 000 0.03525 43.93686.28 0.0 64202 0.0 l+602.2 0.0 0.0 ”' O '0 ‘O-O 0.0 026 42.72083o48 186. -94.4 44.0 “ 4.41.117 230.0 67.0_ 60.0 12.4I 0.0327 42.73383o482 202. +111.6 52.’ +1019600263 255.0 53.9 201.1 0.7: 0.0528 43.99886.21d 38.3 ”175.0-127.3 —105.C 3.847 166.0I131.8I.34.3 10.5 0.0029 42.79483o392 99.4 ‘143.6 142.1.‘103.6 1.431 241.5 142.1 99.4 0.0 05CP30 42.79353o154 180.0 ~3.0 99.0 - 3.0‘0.550 279.0 99.0 180.0 0.0 0.0331 7 43.51885u980 0.0 +698.0 0.0 +608.0 0.0 . 0.0 0.0 0.0 0.0332 43.49286.148 5.3 —425.0 0.0 +605.0_§ 5.3 0.0 5.3 0.0 0.0333 43.55986o231 0.0 +782.o ‘ 0.0 +702.0' 0.0 0,0 0,0 0.0 0,0334 43.678 3.612 0.0 T764.4 0.0 +704.4 0.0 0.0 0.0 0.0 0.0335 42.442859164 0.0 +918.0 18.0 ‘407.0 ' 18.0 18.0 0.0 0.0 0.0336 43.755 6.096 10.0 —193.4 0.0 ‘5806.6' . 10.0 0.0 10.0 0.0 0.0337 43.77666.244 0.0 +648.3 10.0 - 137' 10.0 10.0 0.0 '0.0 0.0338 43.79586.27O 4.0 —584.6 0.0 +605.4 4.0 0.0 ~ 4.0 0.0 0.0339 44.11683.968 101.6 —341.6 51.3 ‘301.6 0.562 153.0 55.0 97.9 3.6 0.0340 44.24283.980 93.0 —599.0 47.0 ~502.00.505 140.0 47.0 93.0 0.0 0.0341 ‘4537284ul56 92.5 ’174.0 9.8 ~101.00.079 102.3 0.0 94.8 0.0 23.534? 43.84085.029 0.0+1044.6 0.0+1004.6 0.0 0.0 - 0.0 0.0 0.0343 43.84285o204 '0.0+1068.0 4.0‘1502.0 4.0 4.0 0.0 0.0 0.0344 43.76985.149 p.0+1106.0 5.0~1508.0. 5.0 0.0 5.0 0.0 100.0343 43.84985.438, 0.0+1093.4 -0.0T1003.4 0.0 0.0 0.0 0.0 0.0346 43.81285.389 0.0+1147.3 0.0+1107.3 0.0 0.0 0.0 0.0 0.0347 43.91885.062 0.0*1038.0 0.0+1008.0 0.0 p 0.0 0.0 0.0 0.0348 43.887859249 0.0?1275.5 0.0+1205o5 0.0 0.0 0.0 0.0 0.0349 43.94485o432 13.5-1000.1 0.0+1104s9 13.5 0.0 13.5 0. 0.0350 43038585.422 0.0+1058.7 0.0+1008.7 0.0 0.0 0.0 0. 0.0351 43.80334.454 0.0+1167.6 0.0+1107e6 0.0 0.0 0.0 0. 0.0352 43.87885o442 0.0+1117.7 0.0+1107.7 0.0 0.0 0.0 0. 0.0353 430359350691 0.0+1144.6, 0.04‘110406‘ 0.0 0.0 0.0 0. 0.0354 43.83935n691 0.0 +860.2 ‘ 0.0 $800.2 0.0 0.0 0.0 0.0355 43.91485oo44 0.0+1065o7 0.0+1005.7 0.0 0.0 0.0 0.0350 43o96065.139 0.0T1253u4 0.0+1203e4 0.0 0.0V 0.0 0.0357 44.11365o112 0.0+1185.4 0.0+1105o4‘ 0.0 0.0 'OoO 0.0353 44.046659248 0.0+1376.6 0.0+13oéo6 0.0 0.0 0.0 0.0359 44.450543122 73.6 ‘48703 809 ~409.3 82.5 8.4 7401 5.6300 44.39354.080 86.2 ‘442.6 10.3 “407.6 0.120 96.5 10.3 86.2 0.0361 44.379840054 88.0 ”480.5 8.0 ”400.5 0.203 96.0 16.2 79.8 0.0362 44.53383.966 54.0 ‘549.3 16.0 ‘503.3 0.449 70.0 21.7 48.3 1 000353 44.828340690 0.0+1389.8 0.0+130908 0.0 0.0‘ 0.0 0.0364 420779850942 0.0 +594.6_ 3.6 ~10504- 3.6 0.0 0.0 0 0.0365_ 44.148.34.415 15.0 ’139308 40.0—120308 0.019 55.0 1.0 5400 0 9705366 44.01.584.640 . 0001‘1199o7 ‘ 0.0+1109n7 0.0 0.0 0.0 0.0 000367 44.27034o542 29.0-1200.0 0.0+1107.0 29.0 0.0 29.0 0.0 0.0368 44.23934.616 0.0+1155.6 0.0+1105a6 010 0.0 0.0 0.0 0.0369 44o38184.416 3.0 '375.4 0.0+1104oé 3.0 0.0 3.0 0.0 0.0370 43.09883.939 66.1-1008.0 155.9‘1006.02.367. 222.0 156.1 65.9 0.8 0.2371 43.238840052 26.1-i309.0 111.8~1309a0 4.576 133.0 113.3 24.7 5.4 0.0372 43.19883.719 115.8 ‘848.0 159.2 ‘80700 1.860 275.0 178.8 96.1 20.4 2.5373 43.33484oz46 72.2 4536.3 16.0~1506.30.420 88.2 26.1 62.1 14.0 0.0374 43.34684.199 99.8 3465.2 23.6—1405o2 0.234 123.4 27.3 96.1 5.8 8.9375 3.290840004 25.5—1288.4 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I I i l f ‘ I 43.35734.270 88.F‘1490.6 26.:—1400.& 0.299 115.0 26.5 88.5 0.0 0.0P80 43.361E4ol32 41.,-4450.0 103.1’1400.0 2.461 h45oo 103.1 41.9 0.0 0.0 81 43.41283.960 26.1-1253.0 135.9—120300P.588 162.0 135.8 24.3 6.9 0.0 82 43.360k3o955 79. ‘1240.5 98.1‘1203ofl 1.242 178.0 97.1 78.2 2.5 0.3 83 43.42834.05% 48. ‘1597.0 113.4‘1507.0Q.389 162.0 114.21 47.8 1.6 0.0 84 5 42.81. 2.99é 189.1 +70.1 85.9 + 0.1; 0.455 E75.0 85.9 189.11 0.0 0.0 85 i 42.85282.962 182.5 +42.8 109.5 + 2.8 0.770 792.0 127.0 165.0 9.6 000586 I 43.173835558 20.0 ‘736.4 68.0 ’60804 3.4000 88.0 68.0 20.0 0.0 0.0387 ’ 43.005820808 205.0 +83.5 99.0 +103o51.219 304.0 167.0 137.0 33.2 0.0385 43.18682.689 134.0 +320.6 66.0 +320.6 78.233 200.0 78.0 122.0 9.0 0.0393 43.17282.689 211.0 +218.6 62.7 +288.6 87.930 273.7 66.4 207.2- 3.3 21.9394 43.14282o704 459.9 +422.8 98.8 *500.8 91.467 558.7 98.1 459.9 0.0 0.0396 43.22282.602 198.0 +431.7 87.0 +520.7 60.668 285.0 87.0 198.0 0.0 0.0397 43.33082.748 194.1 #102.0 86.8 +190.0 ‘10n356 281.0 86.8 194.1 090 0.0398 43.51282o952 211.6 -393.0 168.4 “239.0 67.647 380.0 164.4 217.6 0.0 2.4399 43.59883.005 200.7 ‘644.2 88.3 ~627.2 67.594 289.0 134.2 154.8 22.9 0.0400 42.60485ol40 206.3 ~107.0 110.8 —59.0 43.750 317.0 112.8 204.3 1.0 0.0401 42.76584.030 0.0 $855.0 109.0 _100a0 0.000 109.0 109.0 0.0 0.0 0.0402 42.73.284.120 42.8 +88.7 121.2 $88.7 46.781 164.0 119.7 44.3 0.0 1.2403 42.81683a966 68.0 ~427.8 108.0 -315.8 1.6 174.0 108.0 68.0 0.0 0.0404 4Z.83084.069 61.2 ‘454.0 118.8 ‘426.0 71.429 180.0 118.8 61.2 0.0 0.0405 42.89684.018 57.5 ~636.0 129.4 ‘62690 40.090 187.0 129.9 7.0 0.9 0.0406 42.992843232 111.3‘1061.0 1007—1008w0 0.772 122.0 53.1 68.8 38.2 0.0407 42.91984.089 47.3 “788.8 134.1 “768.8 54.000 181.4 134.1 38.9 0.0 0.0408 43.01934a235 103.2‘1225.0 4a§~1205a0 0.760 113.0 48.8 64.2 40.7 000409 43.01.284.161 12495—1059.0 35.5‘100900 1.878 160.0 104.4 55.6 55.3 0.0410 43.20083aé48 165.6 ~812.0 6804 “802.0 0.935 234.0 113.1 120.9 27.0 0.0411 43.267839434 223.2 ~796.9 62./~1- —70509 0.336 285.5 71.9 213.7 4.3 0:04-12 439270839499 139.0 ”861.3 110.9 ”‘80103 1.236 25000 116.6 94.3 4.0 0004-13 430431830312 209.3—101795 72.8‘10079510393 252.0 164.1 117.8 43.7 0.0414 43.43933.210 186.5-106097 72.6—1000a70.633 259.1 96.2 151.9 16.5 9.8415 43052883¢433 291.4 «933.3 273.6 ~903~53 0.987 565.0 280.6 284.4 2.4 0004-16 43.51953o315 15495-101408 146.4‘1004.8 0.765 301.0 130.4 170.5 0.0 10094-17 430513833160 l74.9-637.5 89.1 ~607a‘3 0.467 264.0 84.1 179.9 0.0 5.6418 43.51033.592 122.1 ~-811.9 127.9 ‘701a910039 250.0 127.4 122.6 0.0 0.4419 43.56133.591 157.8 ‘849.0 50.2 ~802.0 0.532 208.0 72.2 135.8 ‘3.9 0.0420 43.61.183.410 184.6 ‘989.3 21.4 “9090.3 0.116 206.0 21.4 184.6 0.0 0.0421 43.620834291 179.2 ~778.4 105.8 "708.4 0.681 285.0 115.5 169.5 5.4 0.0422 43.64383e478 145.0 ~993.0 75.0 ‘908m0 15.00 220.0 75.0 5.0 0.0 0.0423 43.539839545 120.4 ‘1052.2 6806100962 0.646 189.0 74.2 114.8 4.? 0.0424 420420850792 0.0 +770.7 0.0 +?OO&7 090 0.0 0.0 0.0 0.0/+25 42.37785o869 0.0 +750.5 ‘0.0 4700.5 0.0 0.0 0.0 0.0 0.0426 42.25585a761 0.0 +720.1 0.0 +7003} 0.0 0.0 0.0 0.0 0.0427 420154853734 0.0 +9G4ao 0.0 +90£+00 OeO 0.0 0.0 0.0 000428 42.30283e724 58.5 +56.5 136.5 +106a5 2.299 195.0 134.5 58.5 0.0 0.0429 42.20583n958 102.5 $213.2 45.5 +201.2 0.891 148.0 69.8 78.3 24.4 1.6430 42.108830792 106.3 $272.6 46.0 +207u6 0.519 152.3 52.0 100.3 5.6 0.0431 42.145833958 72.9 +99.1 32.5 +10401 0.508 105.4 35.5 69.9 4.1 0.0432 42.278830556 115.3 $538.3 102.7 T5o3e3 0.941 218.0 105.7 112.3 2.6 0.0434 42.28683.551 96.6 +526.4 118.4 +601.410922 215.0 118.4 61.6 0.0 000435 44.1748545357 0.0+135408 0.0+1304‘08 000 0.0 0.0 0.0 0.0436 44.2898‘5e371 0.0+1465.4 0.0+1405.4 0.0 0.0 0.0 030 0.0437 (4'4030485o499 0.0+116000 40.0 ‘5’:an 40.0 40.0 0.0 0.0 0.0435 44.28985o372 0.0 +815.l 7.0‘140809 710 7.0 0.0 0.0 0.0439 300 A B D E F G‘ {H I .J .K L ‘M , 43.26484g814 0.0—1443.4 20. 4403.4 1.000 40.0 20.0 0.0 0.0 ooogwo ' 43.180i85.110 0.0 +887.3 3.0—1307.7 3.0 0.0 0.0 0.0 05.03441 43.247i84.799 0.0 +787.0 0.0 +707.0 0.0 0.0 0.0 0.0 0.03442 43.105isa.812 0.0 +749.2 0.0 1409.2 0.0 0,0. 0.0 0.0 0.0!!043 lv3.235)35.028 0.0 +868.4 0.0 +808.4 ~ 0.0 0.0. 0.0 0.0 0,0[444 43o260’84.945 0.0 +897.2 0.0 +807.2 0.0 0.0 0.0 0.0‘ ouorzms £ i ‘I :I. I“. g; I; ! .VT 30] A L Card Output: Antrim, Ellsworth and Sunbury shales: The results for the Antrim, Ellsworth and Sunbury formations were punched on the second card. Each card represents a well and the hh3 wells are reproduced in this section of Appendix ll. All the information has been grouped into l2 columns (A-L) as follows: A B* C D E* F G H | J* K L F . A l' : l-’ L H. V /'\ V ‘ /‘\ 4—1 /'\ .C U3 A q— .0 ' *4 A C - \_/ (1) 4.! L. . O ‘-’ +4 H- O .4.) .. '4— 0.) (u v 2 H— i.) \J .— -— V) \_/ 'm (D u a) -— E (U .C c C -—— a) x. — A (n A Cl) 0 LL! A '— A O (U ' ' L N V - r5 .. q. _C 4.; J: u (U 4‘. J: 44 m u- a) u u- w— : a.) u— m 4. q) \J '— 1— v '4— O -— \_/ V > E to O -— -— m > ._ '— C .C 3 C 'U 4—1 _C ll) 3. C q. x— o m U) o C -- in G) 3 O 44 '— -— -— 3 m 4.: _Q ._ ._ C u x .——- 4.; C C m ‘C H ,_ < m U Lu (0 ‘4— m (U C 3 (D < > m > o L (U o m > x. " <1) — .. 0.) 4—1 L _Q .. q) .. q) 3 I! '0 m :1 m cn L U) *-' us .0 m m m ru lll Lu in g E (1) Cl) -— 4—1 U (1) Q) g (D C (U C '— C C C 2 x (1) Cl) x 0.) x LIJ (D — Al 8 J U U) U U In U I L) (D L) US U r“ E .0 a -— _o -— 4.: L 4.: -- _Q ._ .— :J .x: :1 _C C a) o _C 3 _C (1) F’ W a F m F-q: m F~ F- m P 3 *When a formation IS absent In a given well, the negative of the elevation (see Appendix llb, column J) is indicated in this column. Such information was discarded when plotting the structure contour maps. ID EU 0 U rn '11 O I H L. 7< [— 164.1 ~268.3 89.4 9.9 ~394o3 0.0 0.0 9.6 0.0 +83l.7 589.0 1 370.0 ‘82.7 43.2 0.0 4837.3 0.0 0.0 0.0 39.5 +127.3 580.0 2 420.0 +253.0 76.2 0.0 +733.0 0.0 0.0 0.0 0.0 +733.0 560.0 3 ' 325.0 +177.0 86.6 0.0 +912.0 0.0 0.0 0.0 62.3 +434.0 582.0 _ 4 ‘1 312.8 +444.0 92.9 0.0 +740.0 0.0 0.0 0.0 I 0.0 +740.0 312.8; 05 5 324.0 +427 38.0 0.0 +808.0 0.0 0.0 0.0 0.0 +808.0 366.0 06 137.5 +438.5 8.0 10.5 +345.5 0.0 0.0 10.5 0.0 +815.5 148.0 7 106.8 ‘342.3 23.8 460.2 +45.7 0.0 0.6 2.0 0.0 +770.7 567.0 8 241.5 —642.6 100.0 471.5 ~272o6 0.0 1.0 0.0 0.0 +737.4 713.0 9 190.0 “551.7 80.0 429.0 ~137.7 0.0 1.2 0.0 0.0 +818.3 619.0 10 236.5 '625.6 100.0 445.0 —210.6 0.0 1.5 0.0 0.0 +734.4 710.0 11 162.5 -629.2 100.0 546.0 ~83.2 0.0 1.7 0.0 0.0 +672.8 708.5 12 210.7-328.9 100.0 427.3—320.0 0.0 5.1 0.0 ' 0.0 +729.1 638.0 013 156.0 —606.4 18.3 430.0 —207.4 0.0 5.3 1.5 0.0 +788.6 586.0 14 175.0 -553.7 62.4 481.3 ~26.7 0.0 0.7 12.0 0.0 +676.3 656.3 15 211.0 —558.0 100.0 369.0 “218.0 0.0 6.9 0.0 0.0 +742.0 580.0 16 234.0 —655.7 99.0 432.0 ‘223.7 0.0 1.9 0.0 0.0 $684.3 666.0 . 17 115.0 —53.1 95.4 520.0 +456.9 0.0 1.6 0.0 0.0 +906.9 635.0 18 166.3 —637.0 78.1 556.6 ‘112.0 13.5 4.7 0.0, 0.0 +688.0 723.0 19 201.7 ~508.5 97.5 432.3 ~118.5 0.0 6.0 0.0 0.0 +656o5 634.0 20 208.9 ~590.1 63.5 25.3 —581.1 0.0 103.2 0.0 0.0 +630.9 234.3 21 237.0 +590.0 100.0' 0.0 +840.0 0.0 0.0 0.0 0.0 +840.0 237.0 22 166.9 —150.9 84.4 314.5 +234.1 0.0 8.6 19.0 84.5 +314.1 605.9 23 298.6 —44.8 76.9 410.4 +351.2 0.0 7.4 0.0 26.0 +377.2 735.0 24 149.5 +266.3 86.1 285.5 +551.3 0.0 11.4 0.0 0.0 +906.3 435.0 25‘ 155.0 +490.8 88.2 130.0 +620.8 0.0 0.4 8.1 0.0 +950.8 285.0 26 145.0 +187.5 100.0 145.0 +317.5 3.0 1.1 0.0 0.0 +437.5 290.0 27 182.0 ‘982.9 67.1 0.8-4324.9 0.0 194.5 0.8 30.0 “78709 377.8r 28 373.8-4240.1 81.3 1.2 fl582.1 0.0 297.8 _1.2 38.0 4012.1 613.0 29 376.2 —942.9 86.4 4.8 4250.9 0.0 0.0 4.8 26.0 ~778.9 545.0 30 388.2-4050.5 42.5 7.8 fl368.5 0.0 0.0 7.8 16.0 ~896.5 564.0 32 390.0‘1056.0 98.3 0.0 4784.0 0.0 0.0 0.0 10.2 —936.0 510.0 33 357.0 ~884.7 84.7 31.6-fl164o7 0.0 0.0 31.6 32.5 ’708.7 568.4 34 376.0 *875.4 76.3 0.0 4738.6 0.0 0.0 0.0 34.0 —683.4 568.0 35 369.0 —836.3 89.2 0.0 +759a7 0.0 0.0 0.0 53.0 —650.3 555.0 36 370.0 ‘897.5 100.0 0.0 4657.5 0.0 0.0 0.0 23.2 ~722.5 599.0 37 365.0-4082.9 5.1 0.0 +597.1 0.0 0.0 0.0 53.3 -827.9 620.0 38 99.0 .588.3 45.5 481.0 —113.3 0.0 0.3 0.0 0.0 +676o7 580.0 39 380.0 —958.7 15.0 0.0 +775o3 0.0 0.0 0.0 28.0 ‘774.7 564.0 40 391.0 —937.0 92.6 0.0 +772.0 0.0 0.0 0.0 52.0 ~758.0 570.0 41 378.0 ~723.0 57.5 0.0 +799.0 0.0 0.0 0.0 34.0 ~541.0 560.0' 42 .0 +609.6 0.0 0.0 +609o6 0.0 0.0 0.0 0.0 +609.6 0.0 43 194.6 ~803.8 74.8 254.7 —533.8 0.0 1.6 5.5 0.0 +796.2 472.8 44 179.0-4019.6 95.8 138.0 .899.6 0.0 0.1 10.0 20.0 7879.6 367.0' 45. 185.3 ‘776.1 97.4 310.7 —566.1 0.0 0.8 33.7 0.0 +823.9 496.0 46 92.0 +572.0 84.8 0.0 +660.0 0.0 0.0 0.0 0.0 +660.0 92.0 47 355.0 8095.8 45.5 0.0 +594.2 0.0 0.0 0.0 459.5 ‘870.8 665.3 ' 48 286.0'1156ao 92.0 0.0 +599a0 0.0 0.0 0.0 32.3 ‘886.0 496.0 49 337.0'1144.8 94.7 0.0 +590.2 0.0 0.0 0.0 0.0 +590.2 557.0 50 337.2-4375.5 55.0 3.0 4604.5 0.0 82.7 0.0 32.0-1167.5 547.3 51 319.0-4113.2 75.9 1.0 4373.2 0.0 0.0 1.0 43.0 —885.2 548.0 53 329.6-1148.1 20.3 0.0 +601.9 0.0 0.0 0.0 26.6 ‘935.1 604.6 .54 348.0'1134.2 26.4 0.0 +597.8 0.0 0.0 0.0 20.0 ‘925.2 557.0 55‘ 432.0 {455.5 3.9 0.0 +710.5 0.0 0.0 0.0 30.0~1384.5 584.8 56 A B 388.0’108909 204.4 —147.9 147.0 +41.8 109.2 —-5.0 194.8 +146.5‘ 80.0 +154.0 _ 205.0 ~129.2 220.0 —71.7 103.4 +24.7 120.0 +26.3 98.3 +31.1 180.0 -326.0 244.8 —464.7 234.0 —399.5 230.0 —473.6 266.0 —406.5 254.0 —269.0 201.2 -453.5 266.9 —373.8 201.7 -250.4 31.8 —429.9 .0 +950.4 117.0 —349.0 762.6-—J44.3 171.3 ~157.9 219.0 -467.5 82.0 .20034 80.0 +124.8 111.0 +306.9 93.5 +323.7 80.0 +284.2 110.0 +501.1 107.5 +304o5 135.0 +728.4 167.3 +560.7 33.5 +607.7 119.5 +547.8 6.0 +698.0 267.0'1570.5 473.0+6225.0 288.9-4316.2 325.1-3267.1 332.1-1342.0 268.0 4297.6 309.3'1340.2 373.0—1354.8 330.0-1412o5 125.0 *428.3 350.6—1345.0 37505'140008 382.4-1409.2 423.3‘1380.7 200.7 .790.0 199.1 -766.8 C D 52.4 0.0 19.8 540.0 98.8 325.4 15.0 359.0 93.1 415.8 93.8 283.1 ‘81.3 375.0 75.6 106 100.0 0.0 86.5 116.8 94.6 96.2 89.3 136.7' 50.0 132.3 42.6 16.3 53.9 3.9 55.0 0.0 20.2 10.0 90.6 43.0 81.2 7.8 20.4 19.1 100.0 88.3 100.0 256.2 0.0 0.0 43.3 183.0 12.5 48.0 3.1 45.5 100.0 38.0 100.0 168.1 62.5 355.0 100.0.24l.0 97.9 117.1 97.8 186.0 100.0 0.0 68.4 252.5 61.1 35.0 60.5. 47.8 0.0 89.5 36.4 151.5 100.0 0.0 E +7060]. *22307 *15461 +400.8 +395.0 +529.5 +529.0 —91.2 +928.3 +1040? #14603 +166.1 ‘181.0 —644.7 —555.5 +951o4 ~686.5 ‘226.0 —618.5 ‘533.8 —186.4' —176.9 +950.4 4169.0 ‘100.3 ‘115.9 -123.5 722.4 447908 +526.9 +426.7 +47802 4691.1 +55405 +728.4 +595.7 4671.7 +697.8 +778.0 100.0 15.0 1555.5 88.4 0.0+8800.0 89.3 2.1~1584.2 81.5 6.9‘1553.1 76.4 0.0 +819.0 94.8 0.0 +817o4 75.0 0.7-1636.2 41.3 0.0 +728.2 12.0 2.0-4724.5 20.0 7.0 +332o3 41.1 3.4-4665.0 86.7 0.0 +734.2 12.7 0.0 +746.8 17.2 1.7—1771.7 88.6 14.2 —778.0 86.7 34.3 —766.8 I 0000 'n .00.... 0000 p... 0...... 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O O C O ... \lOJ-‘OOWOOOOOOO ... -181.0 -44407 —365o5 ‘43806 "361.5 +933.0 ~378o5 35.0 ~338.8 900 —176.4 10.0 —166.9 000 T95004 1000 ’15900 1600 —-84.3 10.0 —105.9 0 "115.5 8 -—14.4 0 +864o8 0 +806o9 0 +79107 0 f80402 0 +69101 0 0 0 0 0 0 N .widFJH \OOO‘U‘ON 0.0... 000000 +85405 +722.7 +737.7 +782o8 +778.0 0.0+880000 14.0—1208.2 1700-1204.1 17.0-{239.0 22.0-4185.6 322.0‘4250.2 8.0-1328.8' 24.0-4328.5 000x+807o3 16. ‘1289.0 2300-4370.8 906-4106.2 0.0 +764.3 24.7 -J52.0 14.3 -716.8 +666.8‘ +783o5 +171.1f 7968.4. 564.0 80300 529.8 506oQA 525.0 478.0 455.0 243.0 280.0 230.1 232.0. 240.00 325.0 301.0 271.9 265.0 321.0 297.0 284.0 321.0 300.0 298.0 310.0 826.6 226.8 265.0 268.0 435.0 352.0 213.0 274.0 222.0 360.0 170.0 215.0 123.0 271.0 6.0 299.0 523.0 399.0 ,395.0 435.1 471.0 700.0 399.0 416.0 132.0 410.0 405.5 469.4 434.0 240.9 283.5 , 305 A B C- 0 E F G H I J K L 328.7—1313.3 16.7 0.0 +856.7 0.0 0.0 0.0 16.9.1252.3 389.7 112 237.0-1022.0 75.9 0.0 +866.o 0.0 .0.0 0.0 24.0 .975.0 284.0 113 290.0 —814.0 46.6 13.0 —801.0 0.0 0.9 0.0 17.0 —784.0 320.0 114 192.0 —795.4 38.0 0.0 +796.6 0.0 0.0 0.0 25.6 ~563.4 424.0 115 225.0-1228.2 100.0 0.0 +676.8 0.0 - 0.0 0.0 30.1 _953.2 500.0 116 445.0 —683.5 96.5 0.0 +836.5 0.0 , 0.0 0.0 0.0 +836.5 635.0 117 430.0-1508.0 32.9 0.0 +742.0 0.0 7 0.0 0.0 40.5—1338.0 600.0 118 432.2—1504.6 72.0 8.8—1832.6 0.0 1.3 8.8 27.0—1348.6 597.0 119 459.0 —980.0 9.8 0.0 +711.0 0.0 0.0 0.0 2.2 —897.0 860.0 120 474.0—1619.2 30.0 0.0 +753.8 0.0 0.0 0.0 24.0—1516.2 577.0 121 411.0'1580.0 17.3 9.0—1950.0 0.0. ,0.0 9.0 l9.0-1460.0 540.0 122 443.3-1587.4 22.9 1.8-1997.4 » 0.0 0.0 1.8 27.0—1465.4 690.8 123 455.0'1577.6 33.4 0.0 +747.4 0.0 0.0 0.0 0.0 +747.4 570.0 124 455.0-1619.3 34.1 0.0 +745.7 0.0 0.0 0.0 37.6—1504.3 595.0 125 455.0 1579.4 30.8 0.0 +745.6 0.0 0.0 0.0 40.0-1450.4 584.0 126 478.2 1558.5 31.1 0.0 +731.5 0.0 0.0 0.0 34.0-1446.5 590.2 127 ‘ 530.0-1767.0 100.0 0.0 +898.0 0.0 0.0 0.0 25.0—1722.0 588.0 128 490.1-165o.o 98.6 37.0—1576.0 0.0 1.0 0.0 35.8—1576.0 585.0 129 460.6 8518.6 87.1 12.4—1878.6 0.0 3.0 12.4 33.0—1403.6 588.0 130 255.2 —5o3.4 34.3 477.8 -43.4 0.0 0.4 25.3 0.0+1081.6 733.0 131 187.0 —288.0 82.9 478.0 +132.0 0.0 0.7 37.0 0.0+1062.0 665.0 132 189.1 ~285.6 91.8 582.4 4294.4 0.0 0.6 18.4 0.0 +904.4 771.5 133 g 347.5-1467.7 91.4 2.5-1757.7 0.0 142.0 2.5 29.0—1393.7 418.3 134 i 350.0-1453.7 36.7 0.0 +701.3 0.0 0.0 0.0 21.0—1382.7 421.0 155 ' 354.0-1542.9 99.4 0.0 +757.1 0.0 0.0 0.0 20.0-1462.9 434.0 136 360.3-1582.o 90.3 0.0 +773.o 0.0 0.0 0.0 34.0—1513.0 429.3 137 188.0 —42.0 92.3 0.0+1122.o 0.0 0.0 0.0 15.0 _ 6.0 224.0 138 206.6 -113.0 88.4 -o.0+1009.0 0.0 0.0 0.0 25.6 _ 71.0 248.6 139 223.8 40.0 90.7 1.2 -155.0 0.0 0.0 1.2 18.0 +21.0 266.0 _ 140 196.0 +66.8 48.8 0.0+1107.8 0.0 0.0 0.0 23.0 +106.8 236.0 141 220.0 +125.4 33.2 0.0+1217.4 0.0 0.0 0.0 13.0 +152.4 247.0 142 183.7 +200.8 46.1 6.3 +52.8 0.0 ~v0.0 6.3 0.0 +880.8 265.0 143 180.8 +274.2 64.7 12.3 +274.2 0.0 0.0 12.3 10.5 +344.2 263.0 144 219.5 +261.1 40.8 5.0 +101.1 0.0 0.0 5.0 7.0 +313.1 276.5 145 269.5-1o3o.9 50.8 0.0 +629.1 0.0 0.0 0.0 61.0 ~720.9 579.5 146 240.1.4034.6 53.2 0.0 +64o.4 0.0 0.0 0.0 ~57.0 —699.6 575.1 147 338.0 -948.2 11.8 0.0 +713.8 0.0 0.0 0.0 '43.0 -736.2 550.0 148 242.0 —963.7 95.0 0.0 +744.3 0.0 0.0 0.0 69.9 —592.7 612.4 149 282.0-1133.0 31.6 0.0 +625.0 0.0 0.0 0.0 0.0 +625.o 610.0 150 254.0-1178.0 31.3 0.0 +656.0 0.0 0.0 0.0 55.0 —819.0 613.0 151 262.0 —497.4 93.1 0.0 +777.6 0.0 0.0 0.0 96.0 —366.4 668.0 152 .o +783.4 0.0 0.0 +783.4 0.0 0.0 0.0 45.0 —611.6 54.0 153 285.0 —324.9 42.1 0.0 +675.1 0.0 0.0 0.0 123.0 +49.1 649.0 154 240.0 -490.3 28.6 0.0 +704.7 0.0 0.0 0.0 103.8 —-35.3 832.8 155 286.0 -892.6 41.6 0.0 +593.4 0.0 0.0 0.0 105.0 —516.6 804.7 , 156 251.0 .679.0 .45.4 3.0 —913.0 0.0 0.0 3.0 103.0 ~269.o 727.9 157 273.0-1224.9 100.0 0.0 +942.1 0.0 0.0 0.0 21.0—1092.9 405.0 , 158 250.0 -969.0 54.0 0.0 +916.0 0.0 0.0 0.0 28.0 -894.0 325.0 159 214.5-1085.o 75.5 5.5-1240.0 0.0 0.0 5.5 10.0 -975.0 325.0 16c 275.041001.6 92.0 0.0 4898.4 0.0 0.0 0.0 15.0 -914.6 362.0 161 381.5~1268.0 93.0 10.4-1611.o 0.0 0.0 8.1 7.9-4248.o 412.0 162 350.0—1219.0 93.6 0.0 +846.0 0.0 0.0 0.0 0.0 +846.o 350.0 162 169.3-1213.o 61.6 315.0 -946.0 0.0 0.0 58.8 0.0 4874.0 484.3 164 367.O~1303.8H_87.3‘,_0.Q +676.2 _o.o ”$0.05 0.0 0.0 4676.2 382.4 165 A 8 200.0-1939.0 363.0—1365.4 429.5—1363.8 418.2-1133.6 398.4-1080.6 408.0 354.0 “946.7 —926.2 4 390.0—1106.5 303.0-—835.6 230.0 *773.9 496.0'1759.0 267.2 229.0 199.0 251.4 248.5 257.6 231.5 216.0 221.2 237.4 260.0 188.0 146.5 82.0 171.9 159.9 125.9 195.3 117.4 119.9 215.5 229.0 301.4 240.5 170.0 231.9 199.6 184.6 188.5 224.0 89.0 —695.4 ~382.3 ~287.7 e616.0 -639.9 ‘445.4 ~300.2 —250.0 —292.2 ”198.2 4282.8 “544.0 ~417.5 ~325.2 —357.2 -217.7 -324.2 -176.6 “125.8 -20.7 ~1301.3 4043.9 -“737.7 “491.4 7357.5 -1003.6 '885.8 “980.0 \694.8 “794.5 -1274.3 190.0“1045o7 199.2-980.3 182.9-1243.9 232.4 175.8 135.2 «777.5 «965.4 ‘96800 401.8~1132.9 213.9—4286.6 195.0“1246.8 230.5‘1158.0 100.0 C D E 93.9 390.0-1549.0 14.0-1351.4 51.0—1343.8 51.8-1129.6 6.6'3441.6 64.3 94.2 47.9 67.0 7.5 31.2 71.8 '75.98 18.1 97.0 44.9 84.0 27.6 56.5 87.8 39.4 65.4 50.2 21.9 52.4 4.0 34.4 52.7 92.7 57.8 62.6 82.5 46.6 0.0 56.7 78.0 34.3 76.8 68.3 83.8 42.7 68.2 66.5 g49.3 52.5 17.7 22.6 37.9 84.3 13.1 94.3 100.0 40.1 73.4 53.1 1.5 4784.3 +603o8 4893.5 #591.4 —999.9 +883.6 +760.0 4873.4 4963.7 ~671.4 ~501.2 0.0+1034.0 2.8 -488.2 0.0+1001.8 0'0 442 .0 169.3 308.5 400.0 227.5 254.0 405.0 199.8 302.6 342.1 554.5 565.0 473.6 324.5 310.0 271.6 352.4 391.0 259.5 422.0 351.0 312.3 364.8 225.2 394.0 488.2 484.8 54.3 376.0 385.41 354.5 —104.0 ‘157.5 +44.8 “147.2 —11.7 +83.8 - 1.6 +144.2 +283.3 "764.3 '488.9 ‘329.7 ’271.4 -47.5 ’756.6 -549.8 —600.0 -574.8 —404.5 “924.3 .730.7 ~631.3 —958.9 -465.5 —485.4 7488.0 —1112.9 ~911.6: “894.8. .842.0' 0 C)OO(DCDOCDC)OC)OO<3CDOOCDOJOC)OO<3C>OO '71 m P<3C>OP\fiUJO #94 m ......OOOOOOOOO ......OOOOOOOOOOOOOO \O#‘ONOCDCDOCDC)Oo<3c3c>o<3c>o<> O F‘Hrd Ova)$‘O(DC)O O O O O O O O O O‘WCDO‘OCDCDO -bfiflN\»UJbdeJwrdhaOOOOCDC>OO ......OOOOOOOOOOOOO 2 _, N *_ 2" . “ A Cbfi‘wahJHFAFJOCDC)vaFJOCDO‘O (DO‘OFVO§0‘41)N\»UJb\fiu>me~J®PUODNKPK)DCD~JNC)OO‘DC)O(D H ; OL»C>O{DMD®\fiC>O(DC)UHVC>O\fiC)O OCDCDOCDCDOO ‘9 J 0.0*1101.0 14.3’1337.4 0.0 +856o2 10.0-1119.6 30.0-—895.6 —765.7 —658.2 ’930.5 —550.6 *473.9 31.0-1696.4 16.0—1708.0 129.2 —547.4 “264.3 “152.7 '561.0 ~549.9 —383.4 4210.2 ~190.0 ”214.2 22.0 5146.2 42.0-1085.2 +916.0 +952.5 $744.8 ~137.2 -5.7 $985.8 +3.4 +874.2 $893.3 +1135.7 .0 “434.9 ~276.7 -161.4 *107.5 +821.4 ~546.8 —582.0 —521.8 +705.5 +635.7 ~730.7 ~624.3 “929.9 f738.5 ”480.4 ~478.0 K 590.0 391.3 '480.5 480.0; 592.0 589.0 622.0 566.0 620.8 530.0 505.0 547.0 423.0 347.0 334.0 306.4 340.0 322.0 323.0 276.0 302.0 289.4 357 357.2 455.0 482.0 409.4 420.0 540.9 400.0 420.0 462.0 815.0 848.0 828.0 675.0 635.0 511.5 555.0 593.6 ‘456.0 646.0 460.0 ‘506.5 571.0 ‘500.6 632.4 669.0 630.0 506.0 605.0 587.2 632.0 166 167 168 169 170 171 172 173 174 175 176 177 178 179 180 181 182 183 184 185 186 187 188 189 190 191 192 193 194 195 196 197 198 199 200 201 202 203 204 205 206 207 208 209 210 211 212 213 214 215 215 217 218 A 260.8 224.0 219.6 347.0 302.6 282.0 201.8 347.0 307.7 .289.5 267.0 297.5 321.0 8 '782.0 998.6 1479.53 1214.5 1505.0 1439.7 1249.4 1394.0 1356.3 1299.8 1388.0 1045.1 1206.0 348.4 1060.4 256.0 .0“ 68.0 789.6 1000.7 679.9 C 50.4 100.0 89.4 91.9 88.8 100.0 100.0 100.0 96.7 48.5 64.1 96.6 80.4 13.8 71.8 0.0 100.0 2113.0 634.3 71.83 217.2 888.0 77.9 905.1 99.5 55. 0 ~445. 4 63.63 213.0 372.0 56.3 19310 168. 0 ”95.6 180.0 -123. 2 139 .4 “517.0 174.0 -331. 0 198.5 ~690. 5 220.0 115.1 203.8 -384.8 140.0 .95.0 197.5 -615.6 210.0 -497.0 179.0 “224.5 27006 -487.7 190.0 98.6 167.5 -164.1 220.0 “288.0 270.0 -70.0 244.5 121.0 179.0 657.0 232.8 401.7 223.0.'331.0 216.3 153.5 266.0 877.0 217.8 464.3 230.4 393.0 204.3 343.6 606.0 1376.6 210.0 1662.3 270.0 1863.9 557.0 1603.0 321.6 1545.0 464.0 1707.7 388.5 1537.7 558.0 1530.8 458.6 1674.5 298.0 1535.5 205.8 750.7 53. 8 83.3 55.8 50.6 77.2 9.2 82.2 92.5 83.8 67.1 100.0 42.7 100.0 100.0 50.5 77.8 100.0 83.4 100.0 43.9 92.6 88.2 53.3 89.3 51.6 42.9 43.8 91.1 89.8 53.5 22.7 53.7 61.3 62.9 100.0‘ 78.1 D 310.5 467.8 366.9 283.0 773.3 438.0 534.2 399.0 362.3 529.5 556.6 522.5 499.0 519.6 588.2 0.0‘ 0.0 0 0. .0 0.0 0.0 .0 0. 0 0.0 0.0 0.0 4.5 0.0 6.3 0.0 7.5 0.0 0.0 0.0 0.0 0.0 0.0 0.0 140. 5 606.1 499.3 547.0 343.7 485.4 496.9 365.6 351.7 0.0 398.0 288.0 3.0 218.4 210.0 200.5 92.0 74.4 306.0 000 E 812.0 563.6 1124.5 931.5 1096.0 1009.7 733.4 1028.0 1016.3 817.8 864.0 595.1 746.0 'f572.4 217.6 1000.7 “870.1 ”900.7 0.0 ”925.4 ~1006.0 “795.6 -888.2 #683.0 -749.0 ~490.5 “969.9 ”229.8 ‘945.0 ’520.6 ‘597.0 -602.5 ’59707 “871.4 ’614.1 “622.0 ”710.0 “19.0 172.0 485.3 5190.0 “186.5 359.0 ‘30.7 ’37.0 3.6 “981.4' 1264.3 1575.9. 2133.0 1469.0 1497.7.‘ 1404.7 1530.8 1631.5‘ 1281.5 “839.3 fl ..‘o ..1. ..u. o. . .. .... OCDC)OCDC)OCDC)OOOCDC>OO¢DCDUJOO O . QC) 0 0 O° OCDG O O O O OCDC)OOO o .o o .e 91.. . OOCDOCDO(3C) . m 1 q C)®~qwxooamLpOMbC>bLumrah-OCDOCDC>O ""52 H - O'OCDC>OOOCDC>O(3C)OCDC>OOOCDC)QOOCDC)OO(D G C>O-9U3W1V*‘O-PUJNP0FJNtuF4H . O O O O 0 Q C O O O O O O O O O . O 0 OOOCDCDOO<3C>C>O O O 0 O O O O O O O O O C>OOOO\OC>OO(DC>OCDO\xGDO C)OCDC)O\fiC>O(DUJO\OC)OCDO\fih*o CDUMPU1OO(D C)0<3()N\OU1OO O(DC)O(DO(DC)O(DC)O(DC>OOO H 2 ¢)O m m-d~40‘b 4.61» w vakHC)P‘H(DC)C)C)O O ......OOOOOOOOOOCOOOOOOO oxm:w‘b<3~40~oxnc>p wOO1~DUO\O<3C)O 00000000000 4)O\OC)OOOO W m ’(3C>O\»C)OC>OO<3CDC>OCDC>OO C)O(DC>OOCDC)O 00000000090000.00000090000. OO<3C>OOOP~C>OCD$‘OCDODOCDwFfiCDNOCDCDOP~C>OPUOJOCDR)OPJC)O 0 0 0 0 0 0 0 0 Orv~JOCDC)OO OCDP‘ F 000 000 000 000 27 000 0.0 0.0 100 00 00 1 00 00 00 16 00_ “ 00 00 00 2 00 .0 90 00 00 00 00 00 00 00 . 71 . 51 2 C>Or~CDC>OOk»O‘O>dO OCDC>OCDC>OOOC>OCDC>OknO P‘H H «Jw CDC-4C>OCDO~O:4U1WOO. LINE(139.3). COL1200.4). TYPE INTEGER OUT. COL. REF. CHAR ' ' ' ' - DATAtXOUT=45.663. 45.640. 45.629. 45.595. 45. 578. 45. 552.45. 547. 4 A5.4833‘45.448. 45.385. 45.378. 45.355. 45. 314. 45. 807. 45.302. 45; 8265.'45.260.'45.247.'45.246.“45.211. 45.124. 45 119.45.110 45. 059. c45.056.45.o18.44.994.44.982.44.948;44;935.44. 931 44.924. 44. 916.44. 0908;44.904. 44.896. 443895.‘44.890.'441871{”44.8593 44.856. 44.835 Eg44;830.”44.822. 44.816;*44.803. 44.786.”44.775J“44.772.'44.?65844 F.71504407080440698044069104406740440666044064604406450440488074404 672044.463. 44.452. 44.3250 44.274. 44.185. 44.145. 44.0560 44.036. H44.026. 44.008. 43.962. 43.940. 43.883. 43.881.‘43.871. 43.3680 43 1.812. 43.8110 43.791. 43.760. 43.758. 43.722. 43.680. 43.659. 4306 J54. 43.652. 43.651. 43.542. 43.5150 43.362.“4303020 43.285.43.220. K4301250 4301100 4300420 4300009 4209580 42094704208600'42077604206 L26. 42.605. 42.5900 42.5860 42.5610 4205130 4204750'420445 M.42.405042.311.42.293.42.264042.1200420110.42.040.4109900410965041 . .. .. 1 \ .l 1 .4 2.. . .... . . .....A ll . 0 0000 ENCODE (4. I. TEMP). 2(1) DECODEI4. 2. TEMP). (CHAR(I.J). 3 = 1. 4) PACK LEFT AND COUNT CHARACTERS DO 100 K = 1. 4 ’ IF(CHAR(I.1).NE.1R ) GO TO 110 DO 100 3 = I. 3 100 CHAR(I. J) = CHAR(1.J+1) IIO NCHAR(I) = S-K DEFINE DIMENSIONS OF MAP YSCALE = 10.*SCALE DY = 1./YSCALE DX: .12745/SCALE Y0 = YMAX + 4.*DY YLow=YMIN~4.*DY XTOP a XMAX + 2.*DX XLOW . XMIN — 2.*DX FIND FIRST ELEMENT OF xOUT INSIDE MAP DO 120 IOUT = I. NOUT IF(XOUT(IOUT).LE.XTOP) GO To 130 120 CONTINUE PRINT 3 RETURN FIND FIRST ELEMENT OF XCENT INSIDE MAP 130 Do 140 ICENT = I. NCENT IF(XCENT(ICENT).LE.XTOP) GO TO 150 I40 CONTINUE PRINT 3 RETURN CLEAR COLUMNS 150 DO 160 I = I. 800 I60 COLcl) = 0 SET UP MAP IN GENERAL NSHEET = I MOUT = 135 THIS ROUTINE ASSUMES A LINE PRINTER OF136 CHARACTER/LINE MOUT MAY BE INITIALIZED TO ANY VALUE FOR A GIVEN LINE PRINTER SET UP SPECIFIC SHEET 200 PRINT 4. TITLE. NSHEET Y1 = YO — MOUT*DY IF(YI.GT.YLOW) GO TO 205 Y1 = YLOW MOUT = (Y0 “ Y1)*YSCALE 205 Y2 = Y1 * 4.*DY YOO = YO “ 4.*DY ILINE=1 NXCENT n ICENT NXOUT = IOUT CLEAR LINES DO 210 J = 1. 417 210 LINE(J) E 0 SET UP REFERENCE LINE FOR OUTLINE DO 220 J = 1. 135 OUT(J91)=OUT(J.2)=1R 220 REF(J) = 1R TEMP = INTF(YO) + I. 230 TEMP = TEMP * I IF(TEMP.LT.Y1) GO TO 240 J = (YO - TEMP)*YSCALE REFIJ) = IRI .5...— 3M- . —- N.955.41.941.41.932.4I.880.41.862.41.857.41.817.41.815.41.814.41.76 05.41.764.41.761.41.760.41.751.4I.731.41.702.41.701.41.7OI.4I.698.4 PI.675.41.666941.665.41.661o41.657o41.650)‘ DATAIYOUT=84.674. 84.914. 84.743. 84.520. 84.865. 84.378. 84.290. A85.OOOOB401100 84.061. 83.906.83.542.'84.897. 83.909. 84.8220 8 54.891.85.000.55.1I7.83.73508502080830424.8504240850276085852108502 C71.85.549.85.460.83.420. 85.302. 83.302. 85.635. 85.490. 83.476.85 0644. 85.361. 85.384. 85.276. 85.784. 85.412. 85.732. 85.372. 85.89 20. 85.910. 85.508. 85.306. 83.341. 83.338. 85.442. 85.345. 85. 392. F85,513, 85.922. 85.514. 85.394. 85.412. 86.000. 86.070.83. 282.86. 6076.83.321.86.083.83.331.86.115.83.349.83.461.86. 241. 83. 565. 86.35 H4. 82.975. 83.581. 86.326. 83.267. 83.870. 82.719. 83.399.86.302. 183.903. 82.685. 86.283. 83.431. 86.297. 83.930.83.514. 83.512. 86. J386. 82.643. 83.934. 83.672. 86.351.86.351. 86.572. 86.252._86.221 K. 82.535. 86.158. 82.517. 86.126. 82.460. 86.120.‘82.493.‘86.120. L82.680. 82.785. 82.536. 82.524. 86.153; 82.795. 82.889. 82.448. 82 M.888. 82.934. 86.247. 82.590. 83.170. 86.421. 83.194.‘83.062. 86.5 NOO. 83.188. 86.560. 82.937. 83 .265. 86. 598. 82. 526.‘86. 670.83.375; 083.358.83.418. 86.753. 86.598. 86.722.86. 171. 83. 447.85. 250.84.800. P84. 780.85. 712. 83. 451.83. 694. 83. 761.83. 990. 84. 572.84.780) DATA(XCENT= 45. 226. 45.119. 45.188. 45,.185. 45.106. 45.102. 45.099. A45,098.45.098.45.o19,45,019.45.018.45.016.44.940.44.935.44.93O.44. 8786. 44.769.44.768. '44.7I‘2.44. ‘2944.445344044404404390440434.44 c.434 44 130.44.127.44.123.44.‘ O.44.120.44.I20.44.118.44.II6.44.1I 05. 44.114. 44. 108.44. 108. 43. 9’ .43. 788.43. 788. 43. 782. 43.775.43.774. 4 53. 773.43. 635.43. 458. 43. 430.43. 439.43. 435.43. 425.43. 424. 4L 420.43. F281 43. 281 43 274 43 ?74.43. 268. 43. 266.43. 2620430257043. 250.43. 240 6,43 238,43 191,4a.188.43. 176.43. 175.43. 111. 43. 103. 43.096. 43.088. 42 H850.42 846 44 54 .42. 834. 42. 747. 42. 741-.42. 740.42. 735. 42. 732.42. 731 1.42 731.42 73..42. 728. 42. 727.42. 721.42. 668.42. 412.42. 412.42. 410.42 J4OO 42 398 2 395.42: 389. 42.381. 42. 377.42.372.42. 372. 42.061.42.048 K 42. oa¢v42o 031042. 022 I D‘ A.YCENT= 84. 960. 84.211. 84.168. 85.395. 86.124. 83.874. 84.660. vA64.322.84.211.85.123.84.950.84.661.84.?72.83.864.84.782.83.873.85. , , 8676.84.775.83.866.84.321.85.6B4.85.235.83.861.84.779.84.3I9.86.025 //' c.85.910.85.7oo.85.24o.85.008.84.787.84.558.85.006.83.858.84.328.84 0.556.84.128.84.021.84.322.84.I34.85.916.85.412.843782;85.012.84.32 53.83.128.83.117.83.785.83.33o.85.467.83.330.84.774.85.010.83.I40.“ F83.I28.85.925.83.362.85.684.85.472.85.226.84.781.84.765.83.018.83. CI33.83.357.83.414.83.414.83.908.83.008.85.801.85.688.82.232.82.760 H.83.002.83.I18.83.452.85.693.85.239.85.464.86.014.83.668.84.324.83 1.904. 84. 124. 84. 556.84. 780.84. 329. 83.638.86. 189. 86. 160.86.695.86.13 J8.85. 478.83. 011.85. 245. 83. 553. 83. 662.83. 335.84. 563. 86. 155.85.254.8 K5. 200.84. 792.84.684 ) DATA(NOUT : I43). (NCENT = 104) C NOUT SPECIFIES NUMBER OF OUTLINE POINTS ' C NCENT SPECIFIES NUMBER OF COUNTY BOUNDARY POINTS C YOUT SPECIFIES Y-VALUES OF STATE BOUNDARY POINTS 0 XOUT SPECIFIES X-VALUES OF STATE BOUNDARY POINTS YCENT SPECIFIES Y-VALUES OF COUNTY BOUNDARY POINTS XCENT SPECIFIES X-VALUES OF COUNTY BOUNDARY POINTS THESE HAVE UNITS OF DEGREES OF LATITUDE AND LONGITUDE EACH ARRAY PAIR IS ORDERED FROM TOP TO BOTTOM (DECREASING X) FORMATIF400) FORMAT(4RI) FORMAT(*INOT ON MAP*) FORMAT(*I*8A89* SHEET *12) C DECODE ALL 2 INTO CHARACTERS FORMAT(*9*135RII DO 110 I 3 I0 NWELBS -—________L, 0000 hum» w 260 270 280 290 300 320 330 340 00 ‘K1 1 GO To 230 315 x0 = XTOP SET UP SPECIFIC LINE x1 = x0 2 0x TEMP = INTF GO TO 300 J 2 (YO - YCENT/256 N = NCHARIM) DO 400 L = I. N IEILINE ILINE=ILINE+1 IF(XO.GE.XLOW) GO TO 250 C SHEET ABOUT DONE DO 560 I = lo MOUT IFILINEIIv1)oGE.64)OUT(Iv 560 OUT(Io3) = 1R TEMP = INTF(YO) 570 IF(TEMP.LT.Y1) GO TO 580 J = (YO - TEMP)*YSCALE JL = J + 3 1)=LINE(I¢1) ENCODE(4~ 19 TEMPl). TEMP DECODE (4o 29 TEMPI). (OUT(L~293)0 L = Jo JL) TEMP = TEMP * 19 GO TO 570 580 DO 590 K=lc3 590 PRINT5v(OUT(J9K)oJ=19MOUT) C END OF SHEET Y0 = Y] NSHEET = NSHEET + 1 IF(YOoGToYLOW> GO TO 200 C END OF MAP END 'LOAD 'RUN921140000 443 ISOPACH MAP OF BEDFORD SHALE STRUCTURAL MAP OF BEDFORD SHALE ISDPACH MAP OF BEREA SANDSTONE 0145.20041.65085o50082o4406os 0245.20041065085.50082o4406.5 0345.20041.65085o50082-4406o5 STRUCTURAL MAP OF BEREA SANDSTONE 0445.20041o65085.50082.4406.5 SANDSTONE/SHALE RATIO IN BEREA AND BEDFORD 0545.20041.65085.5608254406.5 ISOPACH MAP OF BEREA—BEDFORD FORMATIONS 0645-20041o65082.4408254406.5 ISOPACH MAP OF TOTAL SANDSTONE IN BEREA-BEDFORD 0745.20041o65085.50082o4406o5 ISOPACH MAP OF SHALE IN BEREA-BEDFORD FORMATIONSOB45o20041.65085o50082o4406.5 ISOPLETH OF SANDSTONE IN BEDFORD SHALE 0945.20041o65085.50082o4406.5 ISOPLETH OF SHALE IN BEREA SANDSTONE 10450200410650850500820440605 LOCATIONS OF WELL SAMPLES STUDIED 1145.38041.65086.76082.4206.5 ISOPACH MAP OF ANTRIM SHALE 1245.38041.65086.76082.4206.5 HnAl-C IEAH‘ (Ann Ann:- ‘3 ., -_.__.;—.——v —‘ ‘s . .. -'--W "A.” : ‘. Uh". - BLACK SHALE/TOTAL ANTRIM SHALE ISOPLETH 1445.38041o65086.76082.4206.5 ISOPACH MAP OF ELLSWORTH SHALE 1545.37841.65086.76084o2006.5 STRUCTURAL MAP OF ELLSWORTH SHALE 1645.37841.65086.76084.2006.5 ISOPACH MAP OF ANTRIM-ELLSWORTH TRANSITION ZONE 1745.38041.65086.76084o0006o5 ISOPLETH OF GREEN SHALE/TOTAL ELLSWORTH 1845.37841.65086o76084o2006o5 ISOPACH MAP OF CARBONATES IN ELLSWORTH 1945.37841.65086.76084.2006.5 ISOPACH MAP OF SUNBURY SHALE 2045.20042.50082.88082.620655 STRUCTURAL MAP OF SUNBURY SHALE 2145.20042o50084o88082o6206.5 ISOPACH MAP OF ALL THE FIVE FORMATIONS 2245.38041.65086.76082.4206.5 "IIIII‘IIIII‘IIIIIIII