MIDDLE 0RDOVICIAN OF THE MICHIGAN BASIN Thesis for the Degree of M. S. MICHIGAN STATE UNIVERSITY DOUGLAS 1. SEYLER 197.4 1 mESIS _ 3v . SET-'3’ BIIUK BINUERY 'NB. LIBRARY SINL‘;H$ II mmsronr. maxim ABSTRACT MIDDLE ORDOVICIAN OF THE MICHIGAN BASIN by Douglas J. Seyler The Michigan Basin in its present fOrm began during the late Middle Ordovician time. During Glenwood time, the basin area experienced the initial transgression of the Middle Ordovician sea over the pre-Middle Ordovician unconfbrmity surface. Basinal subsidence created an embayment of the Middle Ordovician sea in the area during Black River time. Increased subsidence created a closed basin centering in southern Lake Huron during Trenton time. Basement block movement took place during Trenton time in the northern Lower Peninsula, creating wrench faulting in the overlying sediments. Due to the similarity of this structure to the structure in the Albion-Scipio trend of petroleum production, it is viewed as a prime area for future petroleum exploration. With this structural model in mind, several other possibly similar structures are suggested. MIDDLE ORDOVICIAN OF THE MICHIGAN BASIN by Douglas J. Seyler A THESIS Submitted to Michigan State University in partial fulfillment of the requirements for the degree of MASTER OF SCIENCE Department of Geology 1974 ACKNOWLEDGMENTS The writer expresses appreciation to Dr. J.H. Fisher for suggesting this thesis problem and for aid and encouragement during its preparation. Thanks are extended to the other committee members, Dr. C.E. Prouty and Dr. B.T. Sandefur. In addition, hte author is grateful to the McClure Oil Company for the use of their well log files, as well as for encourage- ment and criticism. Appreciation is also extended to the Union Oil Company of California fOr assistance in the completion of this study. Finally, deep appreciation is expressed to John Preston for the inumerable late night discussions without which this thesis would never have been completed. ii TABLE OF CONTENTS ‘ INTRODUCTION PURPOSE . . . METHODS AND MATERIALS PREVIOUS WORK STRATIGRAPHY GLENWOOD UNIT BLACK RIVER UNIT TRENTON UNIT STRUCTURE . . . . . . . MIDDLE ORDOVICIAN HISTORY OF THE MICHIGAN BASIN PETROLEUM POSSIBILITIES SUGGESTIONS FOR EXPLORATION CONCLUSIONS BIBLIOGRAPHY APPENDIX iii Page DINO-A \IU'IJ'i 11 15 16 18 20 23 LIST OF FIGURES A typical Gamma-ray well log Correlation chart NE-SW cross-section of Michigan NW-SE cross-section of Michigan . Major structural trends in the Michigan Basin. Cardboard model representation of basement block movement Trenton thickness in Michigan and Southwest Ontario . . . . Diagram of the proposed type of faulting Cross-section of northern Michigan iv Page 2A 5A 11A 11B 11C 11D 12A 13A 138 LIST OF PLATES 2.1.22 1.- Glenwood Isopach 2.- Black River Isopach 3.- Trenton Isopach 4.- Structure on Middle Ordovician Trenton (In Pocket) INTRODUCTION The Middle Ordovician carbonates of the Michigan Basin are in some localities a prolific producer of petroleum. However, little detailed work has been done on these important units on a regional scale. Total Ordovician isopach maps have shown a closed basin centered slightly south of Saginaw Bay, and previous work has placed the formation of the basin during Middle Ordovician time. As this is a critical period in the history of the basin, additional work is warranted. The Michigan Basin is considered in this study to be the closed depression which is now centered to the northwest of Saginaw Bay, and is bounded by stable, relatively positive areas in eastern Wisconsin, north-central Indiana, southwest Ontario, and the stable shield area in western Ontario. PURPOSE Recently several new wells in the upper half of the Southern Peninsula of Michigan have added vital correlation points for the study of the Middle Ordovician of the Michigan Basin. These data have facili- tated a realistic evaluation of Middle Ordovician stratigraphy in the Michigan Basin, and have suggested new petroleum possibilities. The goals of this study, then, are: 1), to study the stratigraphy of the various units of the Middle Ordovician in the Michigan Basin; 2), to relate this stratigraphy to the evolution of the Michigan Basin; 3), to employ these studies in the prediction of future areas of petroleum 1 2 potential in the Michigan Basin. Since Middle Ordovician rocks cr0p out in the Upper Peninsula, very few useful wells are available in that portion of the basin. As a result, this study utilizes only wells from the Lower Peninsula, which can be correlated to adjacent states and southwestern Ontario. METHODS AND MATERIALS This study was conducted primarily through the use of geOphysical logs as these logs are often sensitive to physical variables that are not noticeable in samples. Since this was a regional study, character- istic patterns on the logs were selected for correlation which may not, in some cases, correspond to lithologic formation tOps. This is parti- cularly true of the Glenwood formation, where an interval was rather arbitrarily selected on the basis of a recognizeable pattern throughout the basin. The three intervals which were selected are shown in Figure 1. Further subdivision of the formations was attempted, but was found to be practical only in local areas. The density of Middle Ordovician wells varies tremendously-~from hundreds per county in Hillsdale, Calhoun, and Jackson counties, to less than one-half a well average per county in the northern half of the Lower Peninsula. As a result, in areas of high density only a sufficient number of wells was picked to delineate stratigraphy and structure in the area. In addition, well sample descriptions were examined in inter- esting areas. It” GLENWOOD { TRENTON Figurel- 2 Atypical ( 4”" Gamma-ray , Well log E ' J1...» 4m 2 BLACK RIVER % I“ PREVIOUS WORK Due to the lack of well control, few workers have looked at the Middle Ordovician of the Michigan Basin. Pirtle (1932) wrote a classic article on the Michigan Basin and its origin, without any well control into the Cambrian. Lockett (1947) did a similar broad form study of basins in the northeastern United States. Hussey (1950) examined the Middle Ordovician rocks in outcrop in the vacinity of Escanaba, Michigan in the Upper Peninsula. With better well control came more detailed studies, notably Cohee and Landes (1958), who utilized isopach maps to- gether with current petroleum occurrences to characterize petroleum pro- duction in the Michigan Basin. Ordovician studies have been carried out in adjacent areas: Gutstadt (1958) in Indiana; Buschbach (1964) in north- eastern Illinois; Calvert (1974) in Ohio; and Sanford (1961) in south- western Ontario. Hinze and Merritt (1969) have studied the Michigan Basin with respect to gravity and magnetics. Most recently, Harding (1974) has applied a wrench faulting model to the Albion-Scipio trend of oil production in the southern Lower Peninsula. No work to date has dealt with the individual formations of the Middle Ordovician in the Michigan Basin on a regional basis, as in the present study. STRATIGRAPHY GLENWOOD UNIT The "Glenwood" that was studied during this work does not neces- sarily coincide with that formation which has been correlated with the Glenwood Shale of Illinois and Wisconsin, but rather is an interval between the base of the Black River limestone and the underlying Lower Ordovician or Cambrian sediments which is recognizable regionally on geophysical logs. This interval is characterized in Michigan by green and gray sandy shale and limestone and dolomite. Since this interval rests on or near an eroded Cambrian-Lower Ordovician surface, one would expect the thickness to reflect an irregular, eroded topography. This, —in fact, is shown by the Glenwood i50pach map, Plate 1. Observed thickness ranges from less than 18 feet to 86 feet. Although well control is sparse for this map, one can readily notice similarities to present-day topOgraphy in areas marked by large drainage systems and karst topo- graphy. Similar features have been noted in northeastern Illinois (Buschbach, 1961) for the Glenwood-St. Peter interval. There is a sinuous thin which runs down the center of the state, which could have been a topographically high area. This corresponds to the "mid-Michigan high" which has been observed in gravity surveys of the state. To the west of this is a long, narrow thick which is remini- scent of a drainage valley. This thickening corresponds to a thickening which has been observed in the underlying St. Peter sandstone GM. Balombin, 4 S 1974, personal communication of thesis research material). To the east and northeast are local thickenings, interpreted as local basins. These are somewhat elongated and are roughly parallel to each other. In adjacent states, the Glenwood is similar in character. In north- western Ohio, the interval between the Black River limestone and the Un- conformity, called the Chazy, is characterized by green and greenish- gray argillaceous dolomite, with a thickness on the order of 10 feet (Gutstadt, 1958, p. 59). In northern Indiana, the equivalent section, again called the Chazy, varies from a St. Peter-type sandstone in the extreme west which is 95 to 135 feet thick, to a few feet of greenish dolomitic shale in the east (Gutstadt, 1958, p. 53). In northeastern Illinois the Glenwood consists of sandstone, dolomite, and shale, which varies in thickness from a few to 80 feet (Buschbach, 1964, p. 52). In southwest Ontario, an equivalent formation is called the Shadow Lake, which is placed as basal Black River, and is characterized by green shaly and sandy dolomite, dolomitic shale, and reddish arkose. It varies in thickness from 2 to 50 feet (Sanford, 1961, p. 5). These correlations are shown in Figure 2. The Glenwood appears to represent deposits derived from the erosion of Upper Cambrian-Lower Ordovician sediments, and the marine transgression of the Middle Ordovician sea. BLACK RIVER UNIT The Black River is characterized in the Michigan Basin by 90 to 485 feet of light brown and gray, fossiliferous, dense to crystalline lime- stone and dolomite. There is locallized secondary dolomitization, and the unit becomes generally more dolomitic toward the west. It occurs NJE N Nw sw ] ILLINOIs INDIANA OHIO ONTARIO MICHIGAN ff GALENA TRENTON TRENTON TRENTON TRENTON COBOCONK BLACK BLACK BLACK IPLATTEVILLE RIVER RIVER GULI. RIVER RIVER CLENwoooI CHAZY CHAZY SHADOW LK GLENWOOD Figure 2-Correlation Chart 6 between a very argillaceous limestone and shale at the base of the Trenton, and the argillaceous limestone and shale at the top of the Glenwood. Although it has been suggested that an "extra section" is present at the base of the Black River in the eastern portion of the basin, the inter- val could not be reliably identified, and was not broken out. The iso- pach map of this unit, Plate 2, shows that during Black River time, the region was an embayment of the Middle Ordovician sea, Open toward the southeast, and with a local thickening into the area of southern Lake Huron. In northwestern Ohio, the Black River consists of light tan to dark tan lithographic argillaceous limestone ranging in thickness from 300 to 500 feet (Gutstadt, 1958, p. 71). In northern Indiana, Gutstadt (1958, p. 62), describes the Black River as light tan to dark tan, lithographic limestone, in part argillaceous and dolomitic, which is about 200 feet in thickness. Buschbach (1964, pp. 53-4) describes the equivalent Platteville group as consisting of gray to brown dolomite interbedded southward with very-fine-grained limestone, and having a thickness of from 100 to 150 feet. The equivalent Black River unit in southwestern Ontario consists of the Gull River and Coboconk fOrmations, the former being characterized by brown to cream-colored, lithographic to pure lime- stone, which thickens toward the west to over 400 feet. The latter is described as consisting of buff to buff-brown and tan-colored limestone, which is finely crystalline to granular in texture, and which thickens to more than 100 feet toward the west. In the Upper Peninsula of Michigan, it is described (Cohee, 1948, p. 1432) as 67 to 86 feet of buff to brown, fine-grained, crystalline limestone and dolomite with small amounts of gray argillaceous limestone. 7 The Black River fOrmation in the Michigan Basin represents a subsiding embayment of the Middle Ordovician sea. The embayment was Open toward the southeast, and was probably rather shallow, as evidenced by the abun- dance of fossils and thick carbonates. TRENTON UNIT The Trenton of the Michigan Basin is lithologically very similar to the Black River; it consists of between 157 and 561 feet of brown and gray, fossiliferous, crystalline limestone and dolomite, occurring between the Utica shale above and a very argillaceous limestone and shale section at its base. The upper 10 to 40 feet of the unit is often dolomitic and argillaceous, and the shaly break at its base becomes more pure limestone and dolomite toward the extreme western part of the basin. It is generally more fossiliferous than the Black River, and tends to become more dolomitic toward the west. As with the Black River, the Trenton contains localized secondary dolomitization along fractures and unconformities. The isopach map of the Trenton formation, Plate 3, shows that in Trenton time the Michigan area became a closed basin, with a depositional center in the area of Sanilac County and the southern end of Lake Huron. The Trenton in neighboring regions is also similar to the Black River in those regions. In the Upper Peninsula, the Trenton is charac- terized (Cohee, 1948, p. 1432) as 175 to 206 feet of buff-brown to brown crystalline limestone with some dolomite and gray to dark gray argilla- ceous limestone. The limestone is more argillaceous in the western part of the Upper Peninsula than in the eastern part. The Trenton of north- western Ohio consists of light tan to medium tan crystalline limestone 8 which is from 50 to 200 feet in thickness (Gutstadt, 1958, p. 71). In northern Indiana the Trenton consists of about 225 feet of light to medium tan fossiliferous dolomitic limestone. It becomes more dolomitic toward the west and consists entirely of dolomite in northwest Indiana (Gutstadt, 1958, pp. 62-4). In northeastern Illinois, the equivalent fOrmation is called the Galena dolomite, and consists of about 200 feet of medium- grained, buff-colored dolomite (Buschbach, 1964, p. 56). The Trenton of southwestern Ontario consists of from 300 to 500 feet of gray to brown, finely crystalline to fragmental limestone, with abundant shale partings, grading into brown, finely crystalline limestone at the top. In the extreme southwest, the uppermost 5 to 30 feet consist of brown, medium crystalline dolomite with considerable amounts of bioclastic material (Sanford, 1961, pp. 9-11). The Trenton formation in the Michigan Basin represents a locally closed basin. It was rather shallow, but steadily subsiding, as shown by the abundance of fossils and the thick carbonates. STRUCTURE The origin of the Michigan Basin has been a controversy fOr some time. Pirtle (1932) stated that the Michigan Basin probably originated as a long, broad geosyncline paralleling old mountains extending from central Wisconsin into northwestern Indiana. As such, he believed that the basin probably originated in the Precambrian. He felt that the prin- ciple fOlds which are fOund in later sediments are controlled by lines of structural weakness in the old basement rocks. In 1948, Cohee (p. 1432) stated that the basin was depressed in an area similar to its present form as early as Middle Ordovician time. Yet in 1958, he asserted (Cohee and Landes, 1958, p. 490) that a study of isopach maps had suggested that the Michigan Basin first became a depression in the earth's crust in Late Silurian time. Green (1957, p. 637) also held this view, stating that the Michigan Basin began near the close of the Niagaran time; before that it was a part of the sea floor which sloped gently toward the southeast. Fisher (1969, p. 92) returned to earlier interpretations that the basin was created during Middle Ordovician time, based on much more well control than was previously utilized. Controversy also exists concerning features bordering the Michigan Basin. Pirtle's "Kankakee Arch" (1932) has been drawn in several locations, and Green (1957) has discounted its existance altogether. Although there is a positive feature in northeastern Illinois, Green states that it is a misinterpretation of the Sandwich Fault. 9 10 The Findlay Arch has had several origins ascribed to it. Lockett (1947) tied the Findlay Arch to the Algonquin Arch, saying that they are underlain by the cores of Precambrian mountains which extended from Canada through western Ohio and on south, the reflection of which remains in the sedimentary rocks as the Findlay Arch. Pirtle (1932) stated that the Findlay Arch developed largely during the Cincinnatian. Cohee (1948) infered the presence of a Findlay Arch in Upper Cambrian time by the apparent offlap Of uppermost Cambrian units. Woodward (1961) showed a Findlay Arch existing as early as the Upper Cambrian. Sanford (1961), citing southwestern Ontario isopach and lithologic data, stated that the Findlay Arch, erroneously associated with the Algonquin Arch, was not prominent until Upper Ordovician time. However, he felt that the bioclas- tics which occur in the upper section of the Trenton in extreme southwestern Ontario could indicate that the Findlay Arch was emerging during late Trenton time. Most recently, Calvert (1974) has published isopach maps, constructed in 1965, showing that in northwestern Ohio there is no indi- cation of a Findlay Arch during Black River time, and only a hint of thinning over a positive feature during Trenton time. Calvert states that pre- vious interpretations of a prominent Findlay Arch during Trenton time had erroneously included within the Trenton theoverlying Cynthiana Formation, which consists of a series of reefs in northwestern Ohio. There is general agreement that the Algonquin Arch has been a pos- itive feature throughout the Paleozoic. Associated with this is the Chatham Sag which, although originally thought to be a breach in the old Findlay- Algonquin Arch formed by subsidence of the Michigan and Appalachian Basins adjacent to it (Lockett, 1947, and Fettke, 1948), is more likely a faulted basement block which acted as a fulcrum about which the Findlay Arch moved upward (Sanford, 1961). 11 MIDDLE ORDOVICIAN HISTORY OF THE MICHIGAN BASIN The present study lends support to several of the previously stated ideas. A study of the isopach maps and of the general cross-sections, Figures 3 and 4, suggests embryonic basinal subsidence in the Lower Middle Ordovician. The Glenwood isopach, Plate 1, shows an elongate thickening in the area of the "thumb" of the Lower Peninsula. Interest- ingly, the elongation of this thickening is approximately parallel to the major northwest-southeast structural trend of folds and faults in the Michigan Basin. Another anomalous Glenwood thickening occurs in the ex- treme northern part of the Lower Peninsula. This is also elongated approximately parallel to the major structural trend in the basin. In both cases, the basins could be partially due to the vertical reflection of movement along basement faults. There is some evidence to justify the existance of basement fault patterns in the Michigan BaSin. Through a gravity and magnetics study, Hinze and Merritt (1969) concluded that the dominent northwesterly structural trend in the basin reflects lines of weakness in the basement. These Glenwood anomalies, then, may be due to reactivation of these basement faults during Lower Ordovician time. The concept of basement lines of weakness was first stated by Pirtle (1932). Figure 5 shows this lineation in features in the Paleozoic of the Michigan Basin. Thomas (1974) has recognized similar features in the Williston-Blood Creek Basin, and suggests that the basement is broken up by basement weakness zones into blocks. Regional horizontal compression would produce lateral adjustment in these basement weakness zones, resulting in a shear couple being applied to the sediments above. This basement block movement is illustrated in Figure 6. llA 5:009:90 3&2 .n 2:2“. 2.3 330m 4. 33:60 $323: .8 ads. 0» ~08 debto:l°8 . A 52.. 20(40 Km); x016 52¢ . 52¢ 1 53¢ . .85» I .¢m>.¢ 20440 20:65 2922: 29sz , 29.2mm» . 2922: “ AIv. NI O.Illv I2 fl I A..IIQ 3 w I Jm . 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Initial cardboard model: dashed lines are precut weakness zones; solid lines are di5placement indi- cators. llD Representative experiment; compression from south of the bisectrix (after Thomas, I97h). 12 The Black River fOrmation represents an embayment of the Middle Ordovician sea. It thickens locally into Lake Huron, but is Open toward the southeast. In the southeast corner of the state there is an anoma- lous thin, which is open toward the area of the Chatham Sag. This type of thinning could be due to erosion of a subsequently positive area, or a lesser rate of subsidence of the area during deposition. Each expla- nation has support: there is some indication of an unconformity at the top of the Black River in this area; on the other hand, this area appears throughout the Middle Ordovician to have been somewhat more stable than surrounding parts of the basin. More well control is needed in order to resolve this problem. It should be noted that the northern end of the Basin was quiet during this interval. Also, there is no indication of a Findlay Arch to the southeast during Black River time. It is clear that during Trenton time a locally closed basin began to develop about a depositional center in southern Lake Huron. The Trenton isopach map, Plate 3, lends support to the statement by Green (1957) that the Michigan Basin was formed by basin subsidence, rather than by marginal uplift. There is no abrupt thickening off of a struc- ture to the south, but rather a very gradual thickening, on the order of 25 feet per mile, into the basin. The Trenton basin is noticably elon- gate toward the east and west. This is particularly apparent when viewed in conjunction with isopach data from southwest Ontario, as shown in Figure 7. However, in view of the pattern and rate of thickening of the Trenton, the elongate shape of the basin is most likely due to stability, rather than uplift, of the marginal areas with respect to basinal subsi- dence. IZA Figure 7. Trenton thickness in Michigan and Southwestern Ontario. Contour interval is 100 feet, except 20 feet where indi- cated (Southwestern Ontario after Sanford, l96l). 13 The northern part of the basin appears to have been active during the Trenton. During this period, there appears to have been wrench faulting, with the northeastern block moving right laterally. Figure 8 illuatrates the type of movement proposed; the general location of this fault is shown in red on Figure 5. Figure 9 is a cross-section of this area (note-~the Trenton has been subdivided in this area, and the cross- section indicated that movement began during Middle Trenton time). If such movement did occur during deposition fo the Trenton sediments, there would be local thinning on the two truncated anticlines thus formed in the simplest case. This is, in fact, what is observed. Deposition concur- rent with movement would produce thinning on the uplifted areas, and thick- ening in the troughs. Lateral movement need only have been on the order of a few hundred yards. It must be realized, however, that the structure is likely to be much more complex. Thus, en echelon fOlding and complex fracturing, as well as multiple lateral faulting is likely. A similar origin has been proposed by Harding (1974) for the Albion- Scipio trend, in the southern Lower Peninsula. In the case of the Albion-Scipio trend, the wrenching was opposite to that proposed for the norhtern Michigan fault, being left lateral. In the Albion—Scipio trend, the wrenching was interpreted as being somewhat divergent, in order to produce the sag which occurs in the dolomitized zone of the trend. The movement was probably Upper Devonian (Fisher, personal comm., 1974); the proposed movement for the northern Michigan fault of this study was Middle Ordovician Trenton. Wilcox, Harding, and Seely (1973) present an excellent primer on basic wrench tectonics. If this type of tectonic activity did take place in the Albion- Scipio trend, and in the norhtern Lower Peninsula, then it seems reason- l3A Figure 8. Diagram of the prOposed type of wrench fault. 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