BASEMENT ummoev m mcmm . _ As DETERMINED FROM WELL cm‘rmcs ' Thesis for the Degree ofMS,“ , " MICHIGAN STATE'UNNERSWY HARRY J. LAAKSONEN' 1971 ‘ - . . . ll 11; um; mzrwml L’" 11! R mm W" 1mg ll ! 77 ABSTRACT This study examines the cuttings from all of the fif- teen Precambrian basement tests in the Lower Peninsula of Michigan. The lithologies that are observed are in agree- ment with lith010gies for the various provinces that outcrop around the periphery of the Michigan Basin and can be rea- sonably extended under the Paleozoic cover using geophysical data. Magnetic susceptibility measurements made on the sam- ples cannot be conclusively related to magnetic data. but one case indicates a correlation with a high magnetic ano— maly. BASEMENT LITHOLOGY IN MICHIGAN AS DETERMINED FROM WELL CUTTINGS B? x“. ., 9‘ Harry JL Laaksonen A THESIS Submitted to Michigan State University in partial fulfillment of the requirement for the degree of MASTER OF SCIENCE Department of Geology 1971 ACKNOWLEDGHENTS The writer is deeply grateful to Dr. Harold B. Stonehouse under whose direction this study was carried out. Thanks is extended to Dr. William J. Hinze and to Dr. James R. Tron for their assistance as members of the advisory committee and for their examination of the manu- script. Thanks is also offered to Mr.G.D.Ells and to Mr. Irvin Kuehner of the Michigan Geological Survey for their assistance in obtaining samples and information used in this study. A special note of thanks is extended to the author's wife. Diane Laaksonen. for typing the manuscript and for her encouragement and patience while this paper was being prepared. TABLE OF CONTENTS Page INTRODUCTION................................... 1 HISTORY OF PREVIOUS INVESTIGATIONS............. 1 BASEMENT PROVINCES............................. 3 LITHOLOGIC RESULTS............................. 5 CONCLUSIONS.................................... 17 SUGGESTIONS FOR FURTHER INVESTIGATIONS.......... 18 BIBLIOGRAPHI................................... 19 APPENDIXOOOOOOOOOOOOOOOOOOOOOOOOOOOOOOOOOOOOOOO 21 Map or well locationSOOOOOOOOOOOO000...... 21 Table1.0.0.0000000000000OOOOOOOOOOOOOOOOO 22 Table 2....000......OOOOOOOOOOOOOOOOOOOOOO 24 "0111088......0....OOOOOOOOOOOOOOOOOOOOOO 26 Magnetic susceptibilities................. 32 Photograph8..........................ooa.. 35 INTRODUCTION There has been much discussion on the nature of the basement rocks of the Michigan Basin for a number of years. The rocks considered will be those crystalline and metamor- phic rocks covered by the Paleozoic sediments dipping toward the center of the Michigan Basin. Their lithology as en- countered in deep drilling through the Paleozoic sediments is related to the rock types typical of the exposed Precam- brian provinces surrounding the Michigan Basin. The rocks range in lithology from granite to meta-basalt (greenstone) and quartzite. The results of the magnetic susceptibility of the rocks as observed in this investigation are related to a magnetic survey of Michigan. HISTORY OF PREVIOUS INVESTIGATIONS Although there has been much curiosity about the base- ment rocks of the Michigan Basin for a good many years. most of the investigations have centered around geophysical in- terpretive techniques because very little is known from drill holes. The most recent work is that of Kellogg (1971) in his aeromagnetic study of the Lower Peninsula of Michigan. and a gravity and magnetic interpretation by Hinze and Mer- ritt (1969); both of these studies have interpreted broad 2 zones of lithology in the basement. Lidiak (1966) deter- mined lithology and age dates of samples for wells in Wash- tenaw and Monroe Counties. but the most comprehensive study of covered Precambrian basement rocks of Michigan was by Yettaw (1967). who worked on samples from rocks penetrated by the Security-Thalman #1 well in Berrien County, but with little attempt to tie in data from other wells. The only other significant source of information is the well IOgs that are available at the Michigan Geological Sur- vey. These logs have been written. for the most part. by drillers or petroleum geologists and put into the Survey's format without significant change. Some of the samples were looked at by Survey geologists. but not described in detail since they fall below any possible production of oil. and often only the top of the Precambrian was recorded. The first well to penetrate the basement was drilled in St. Clair County in the late 1920's. and several followed in the 1940's in the eastern part of the State. The Precambrian rock in most of these wells was described as a granite or granite gneiss with one in Hashtenaw County being described as a schist. There were some wells drilled in the 1950's into felsic rock in the eastern part of the State and on Beaver Island. In 1964 Consumers Power Company drilled a brine disposal well in St. Clair County which penetrated the Precambrian. and a core was taken. In 1962 the Security- Thallman #1 was drilled in the southwestern part of the State, the only basement test in this area. The Pan American 3 Drasey #1 was drilled in Presque Isle County in 1967. and the latest Precambrian well was completed in 1970 in Living- ston County by the Mobil Oil Corporation. There are a total of 17 basement tests in the Lower Peninsula of Michigan; samples are available for 15. including one core. Other wells drilled in the Michigan Basin penetrating the Precam- brian have been drilled in Ohio. Indiana. Wisconsin, and Ontario as well as in the eastern Upper Peninsula. BASEMENT PROVINCES It is generally considered that there are four provinces in the basement of the Michigan Basin. A province is defined as an area where the rocks are of similar type. age. and metamorphic grade. Other criteria include similarities in the magnetic and other geophysical characteristics. One of the provinces is the Penokean. which covers the Upper Penin- sula and the northern part of the Lower Peninsula.. It is described from Wisconsin (Dutton and Bradley (1970)), the western Upper Peninsula. and from Ontario north of Lake Hu- ron, The age dates range from 2.2 to 1.32 b.y. indicating a long range of activity. The rock types run the full range from acid to basic igneous, and there are many types of metamorphic rocks, particularly quartzites, associated with this province. The Central province covers the largest part of the southern Lower Peninsula and extends into Indiana from wes- tern Ohio and thence into Illinois. southern Wisconsin and Iowa. The ages obtained for the rocks of this area average u about 1.2 b.y. (Lidiak, et a1 (1967)). Rock types in this province range from felsic to basic with some metasediments. Perhaps the best defined province in the basement is the Grenville which occurs in the east and southeast parts of the State. The dates. .9 to 1.1 b.y.. obtained by Bass (1960)correlated with what he had found in central and eas- tern Ohio and into Ontario where the Grenville outcrops. The dates obtained in Michigan agree very well. Most of the Grenville rocks are metamorphic, although there has been some igneous activity. The Grenville in Ontario adjacent to Michigan is mostly metasediments and amphibolites with gneisses present. The fourth major rock type present in the Michigan Ba- sin is the Keewanawan. but it is not recognized by all geologists because there is no direct lithologic evidence or age dates. The Keewanawan is dated in its outcrop area in the Upper Peninsula and Wisconsin at 1.0 to 1.2 b.y.. and therefore is slightly older than the Grenville. Its presence in the Lower Peninsula is indicated only by the Mid-Michigan gravity high and the correlative magnetic ano- malies. These have been suspected for some time as being caused by extrusive or intrusive basic igneous rocks. and are continuous with Keewenawan basic extrusives in the type area. -It can be seen that the Mid-Michigan anomalies cut across the grain of the gravity and magnetic anomalies of the other provinces. and it can be reasonably said that the rocks causing the anomaly are younger. have higher density and higher magnetic polarization. 5 The dividing line between the Penokean and Central pro- vinces must fall somewhere across the Lower Peninsula. but on geophysical evidence is difficult to determine. In the north the magnetics show an east-west trend. and the ano- malies tend to be of short wavelengths. In the south the trends are similar but seem to curve slightly to the south- east. In the central part of the basin. the depth to the basement reduces the sharpness of any break. and the exact delineation of the two provinces with apparently similar geophysical properties becomes impossible. The Grenville province's magnetic “finger print“ is very clear in the eastern part of the State. The trends all fall into a northeast-southwest pattern that disappears Just about at the Livingston-Ingham County line. This trend can be traced down into Ohio and up across Lake Huron into On- tario where Grenville rocks outcrop. LITHOLOGIC RESULTS The Michigan Basin in the Upper Peninsula extends from eastern Dickinson County east to the end of the peninsula and then into Manitoulin Island in Lake Huron. In this area there are few basement tests. except for a series of holes around Escanaba. There is only one hole in the eastern part of the peninsula. on Neebish Island. The lithology that is reported for these wells is recorded at the offices of the Michigan Geological Survey at Lansing. The range of lithologies in this area is great. even where there is not a great deal of space between the wells. 6 (See Table 1). There is a good correlation of the reported iron formation and the large magnetic anomaly that is loca- ted Just to the west of Escanaba. The rest of the litholo- gies that are reported in the western part are granite. greenstone. and other metamorphic rocks such as talc schists. On Neebish Island the well is reported to have encoun- tered quartzite. There is quartzite outcropping on Manitou- lin Island. and it is entirely likely that these rocks are genetically related since Manitoulin is in such close prox- imity. The samples from the Upper Peninsula were not exa- mined. The Pan American-Drasey is a very interesting well in that it penetrated two distinct lithologies in the basement. The first is a very clean quartz rock. and the second is a greenstone of basaltic or diabasic origin. There has been some controversy about the origin of the quartz. Reed (1971) feels that the quartz is so clean that it has to be vein material. but there is only a very small chance that this is the case because it would require a di- rect hit on a nearly vertical vein to get the 210 feet en- countered. The geographical proximity of this well to the quartzites that are encountered in Neebish and Manitoulin Islands. as well as the shapes of some of the intergrowths and the graininess of the cuttings lead to the conclusion that this is a meta-sedimentary quartzite. It is entirely possible that the rock was originally a well washed sandstone with silica cement. Most of the old grain boundaries have been destroyed in recrystallization. (See photos 1 and 2.) 7 There has not been any controversy as to the origin of the greenstone. It was described in the log that was pub- lished by the Michigan Geological Survey as being of basal- tic or diabasic origin. This is confirmed. for when a thin section is examined. the plagioclase laths are clearly vis- ible (see photo #3). The other minerals that are seen are chlorite and other types which indicate low grade metamor- phism. There is some quartz. but this is a very minor con- stituent. The extremely fine grain nature of the rock makes further identification impossible. The other well in the Lower Peninsula that has pene- trated possible Penokean rock is located on Beaver Island. There are actually two wells on Beaver Island. both drilled by the McClure Oil Company. but no samples are available for the State Beaver Island #1.- The examination of the State Beaver Island #2 indicated a medium grained granite that could have gneissic texture. The magnetic examination shows the samples to fall into the broad range for granite. al- though at the lower end. This would indicate that there is a low magnetite content in the rock. The age date that is given for the rocks at Beaver Island is only 1.10 b.y. which would fall into the range that is given for the Keewanawan. although granitic rocks of Keewanawan age are uncommon in the outcrop area. There are several possible explanations for the Keewanawan age of this granitic rock. One theory is that the rocks are a product of magmatic differentiation of the more common basic rocks. The fact of the low magnetic 8 susceptibility can be used to support this theory. in that the magnetic minerals have been caught up in the basic rocks and depleted in the later stages of differentiation. (Bass (1964) states that there is an anomalously high amount of Rb in the samples. and he feels that this. along with some fluorite that he saw indicates to him that this.is a differ- entiation product.) Another explanation is that an older (Penokean) granite was metamorphosed by the Keewanawan ig- neous activity as indicated by the closeness of the gravity and magnetic anomalies. and redated. The Central province is postulated to run through the southern part of the Lower Peninsula of Michigan and Ohio. near the border with Indiana. west through Indiana. Illinois. Wisconsin. and Iowa. The best indication of this province extending into Michigan comes from the magnetic signature of this province in the southern Lower Peninsula. A study by Rudman and Blakely (1965) of an aeromagnetic anomaly in In- diana indicates that there is a great range of susceptibili- ties in the basement. The range that is published is from 66x10"6 e.m.u./ca for a rhyolite in Ohio to 7200x10'6e.m.u./ acpfor a basalt in Indiana. In general the values fall in- to the range of 250x10’6 to h00x10‘6 e.m.u./c.c.. This ac- counts for the relatively flat magnetic contours except where interrupted by basic rocks of much higher suscepti- bility. In Wisconsin Dutton and Bradley (1970) have compiled a list of age dates from south to north along the center of the State. There is a trend for the older dates to fall to the north, as would be expected. which indicates a Penokean 9 age for this part. The problem comes in the middle of the State where there is a mixture of dates. This seems to in- dicate a transition zone of Penokean crust that was intruded by Central province rocks. It is the feeling of Stonehouse (1971) that tectonic activity in Penokean time was early (2.2 to 1.8 b.y.). and the final phase (1.8 to 1.“ b.y.) was not so much orogenic as quiet igneous. Stonehouse (1969) draws the boundary line of the Central province through Mich- igan south of Saginaw Bay. based on the break in magnetic trends and age dates in Wisconsin to the west. Hinze and Merritt (1969) draw the line through southern Saginaw Bay and use the rationale that the trends and wave lengths of the magnetic anomalies are different. It is the feeling of this author that there is most likely a zone of transition that fills the space between the lines that have been drawn. The Security-Thalman #1 is an unusual well in that it penetrated 10h0 feet of Precambrian rocks. The samples were described by Yettaw (1967) as a medium grained granite that appeared gneissic in part and thus agrees with the lithology type of the Central province. Layton (1970) feels that this could be a zone of deep weathering and that the rock is ac- tually a granite wash; this is difficult to believe because of the great thickness. The main argument used to call the whole section a regolith is the speed at which the drill penetrated the rock. There is an explanation for this when one looks at the cuttings which are very fine and broken up. This condition could be caused by high bit pressure which would result in increased drilling rates. The nature of the 10 rock could be an asset here. too. because of the brittleness of a solid crystalline rock. The quartz in the rock could also act as an abrasive in cutting the softer minerals of the rock. The condition of the mineral grains is too fresh to indicate a regolith. This fact is further substantiated by the fact that good fresh sharp quartz and feldspar grains are found close to the top of the section (see photo ). There is some regolith present at the base of the Cambrian sandstone section. The Grenville rocks are the most drilled and therefore the best defined in the Lower Peninsula of Michigan. The first real proof that the Grenville did extend into Michi- gan was by Bass (1960) when he dated several wells in eas- tern Michigan. Along with the wells for which he had age dates in Ohio. Bass was able to set a minimum westward line for the Grenville front. Since then there have been new basement tests drilled.and these confirmed the earlier find- ings. Hinze and Merritt (1969) placed the Grenville front at about the Livingston-Oakland County line and north- northeastward to Saginaw Bay. on the basis of preliminary magnetic data. The work of Kellogg (1971) along with the lithologic data for the Mobil-Messmore #1 acquired in this study has brought the Grenville front west to the Ingham- Livingston County line. then trending northeast. The Gren- ville is marked by a magnetic lineation to the northeast that continues across Lake Huron and into Ontario into the rock outcrop area. In southeast Michigan the Grenville is 11 an area of broad magnetic lows with only a few highs. One high is in southern Wayne County and is penetrated by the Sturman-Chapman #1. as can be seen in Table 2. The magne- tic susceptibility is on the high side for a granite. There is another magnetic anomaly located on the western boundary of St. Clair County and one in the Howell area. which is the major anomaly of southeast Michigan. The general lithology that has been observed in the Grenville of Ontario is made up of calcareous and argilla- ceous metasediments. basic volcanics. granitic gneiss. and both basic and acid intrusives with the last predominating. In Ohio the basement lithology is typically a granite gneiss with some basic rocks. In southern Michigan the main lith- ology is also a granitic gneiss with some altered basic rocks. Samples from the St. Clair Oil and Gas-Hurst #1. the first basement well drilled in Michigan. were in very bad condition due to the rusting of contaminating steel. It is for this reason that the magnetic susceptibility was not run and that biotite was the only mineral that could be clearly identified. The Bernhardt-Puzzuoli #1 a few miles to the south is a more recent well. and therefore the samples were in better condition. The basement rock here is a gneiss with bands of quartz-rich rock. and others that run very high in bio- tite and plagioclase. Often the biotite bands were also rich in magnetite causing a sharp increase in suscepti- bility. This well is drilled on the edge of a magnetic gra- dient that appears to increase into Canada. The area to 12 the west of the well is magnetically very ”flat”. indicating a low susceptibility contrast between rocks in this area. Continuing to the south along the east boundary of Michigan the next well that is encountered is the Marathon- Woodhaven #1. drilled as a brine disposal well in 1967. This well is on the north flank of the magnetic anomaly that is located in southern Wayne and northern Monroe Counties. The rock is a granite gneiss. but the magnetic susceptibility is not particularly high; however. the anomaly could result from local rocks such as are sampled in the Sturman-Chapman #1 or something deeper. The Chapman well is interesting in that it has a very well developed regolith just above the basement rock. The percentage of minerals in the regolith interval is almost identical to that seen in the solid rock. the difference being in the weathering of the mineral grains. The feldspars are fractured and broken along cleavage planes. and the corners have been rounded and the surfaces clouded by weathering alteration. The quartz grains are rounded and slightly frosted. and many of the ferro-magnesian miner— als are rusted or entirely absent. The results can be seen in Table 2. It is unfortunate that only 1.5 feet of basement were penetrated for it would be interesting to see what ef— fect depth would have on composition and magnetic suscep- tibility. The Furgison and Garrison-Shimp #1 sample is best de- scribed as an intermediate gneiss because of both lithOIOgic and magnetic considerations. The lithologic examination 13 indicates several bands that are very rich in chlorite and therefore were probably mafic materials that were altered. while the quartz-feldspar bands were not altered. The feld- Spars appear to be at least 50 percent plagioclase. and probably more in the chlorite rich bands. Bass (1965) x-rayed the green minerals from this well and concluded that they were iron-rich chlorite mixed with biotite and muscovite. This study did not disclose any muscovite because of ex- tremely fine grain size. Beck-Sancrant #1 well has penetrated more basement than any in Michigan. over 1900 feet. There are no samples at all from the Middle Ordovician down to the top of the base- ment. and therefore the drillers t0p must be believed. There are good samples for several hundred feet into the basement. and then none for over 1500 feet. with a few samples from the bottom 50 feet which are contaminated. The rock is a granite gneiss that is rich in quartz. but some of the quartz as usual comes from up hole caving. as indicated by the very worn condition of the grains. The volume of the samples that were saved is so small that accurate measurement of the magnetic susceptibility was not attempted. Granite is encountered in the Eckert-Taylor #1 a few miles to the north. The percentages of minerals in this well are the closest to a “text book" granite that was encoun- tered. This perhaps means that this is a plutonic rock ra- ther than a metamorphic one. It is also possible that this rock was cut with less bit pressure. and therefore there was 14 less crushing and better retention of the feldspars in the samples. It is evident from the sample descriptions that rocks from the basement are rather uniform in appearance. and this is confirmed by the flat low magnetic character. Moving to the west. the rocks become more diverse. The Colvin-Meinzinger #1 samples again indicate a gra- nitic rock. This is one of the wells dated by Lidiak (1966) at 1.05 b.y. The samples in this well were badly contami- nated by drill steel and the susceptibility was not run. An interesting fact to be noted at this time is that all of these wells mentioned above fall between 0 and 250 gammas on the aeromagnetic map of the Lower Peninsula of Michigan. The wells that will be discussed from here on all fall above the 250 gamma contour although the suscep- tibilities of some of the samples are very low. reflecting that the rocks in the immediate vicinity of the well did not contribute significantly to the anomaly. The Chamness-Tory #1 and the Colvin-Voss #1 are only a few miles apart and bottom in similar types of rock. rich in biotite and chlorite. In the case of the Tory well there is considerable contamination from up hole. and previous work (Michigan Geologic Survey log and Lidiak) has described the rock as a granite (7). The Voss well has been dated at .95 b.y. It is possible that these rocks are related to the rocks that cause the Howell anomaly: however. they do resem- ble the rocks from the Shimp well. which is not close to a magnetic high. 15 The most recent well to penetrate the basement in Mich- igan is the Mobil-Messmore #1 that was drilled in Livingston County in 1970. The cuttings and stubs for this well were available. and therefore thin sections were prepared. The lithology from the cuttings appeared to be an intermediate gneiss because of the textures and minerals present. The magnetic susceptibility is unexpectedly low in this rock. averaging only 55.37x10"6 e.m.u./c.c. When the thin sec- tions were studied. it became apparent that the rock was made up of more than 80 percent plagioclase that was analysed by the twin angle method and shown to be oligoclase or ande- sine. The crystals are very small and very few are twinned except for some of the relict grains., There are difinite metamorphic structures seen in thin section as grains of opaque mineral flow around relict grains in response to stresses applied during the recrystallization. Turner and Weiss (1963) define this as a schistose texture. but since the whole rock cannot be seen. it will be considered a gneiss because of the lack of micaceous minerals. The opaque mineral is hematite rather than magnetite. and there is some leucoxene and some sphene present; quartz less than 5 per— cent in any sample and in most samples less than 2 percent. A few grains of pyroxene and some flakes of biotite occur. but all are minor when compared to the amounts of plagio- clase and hematite. The lack of magnetite and ferro- magnesian minerals tends to suggest oxidation before recrys- tallization. but this remains to be proved. An age date is being run at this time and is not yet available. 16 The only core taken in the Michigan Basin from the basement is from the Consumers Power Company-Brine disposal #1 in St. Clair County. It was loaned for the purpose of this study by the subsurface laboratory of the University of Michigan. The core chips were also studied. and it was found that they came from where the core was broken along joint planes and where alteration was heaviest. Within about B/h of an inch on either side of the break chlorite was predominant. The rock as a whole is a highly altered gneiss of intermediate to mafic composition. The most com- mon minerals are chlorite. biotite. and plagioclase with some potash feldspar. quartz. pyroxene. hematite. and leu- coxene. The core was washed and examined both wet and dry with a 10x hand lens and then 9 one-inch diameter cores were cut from the core as shown. to facilitate magnetic sus- ceptibility measurements; the magnetic susceptibility is even lower than that found in the Messmore well. Finally thin sections were prepared from six of the smaller cores. CONCLUSIONS 1) Lithologies consistent with those found in the out- crop area of the Penokean province are found in Presque Isle County and on Beaver Island. in the Lower Peninsula and all throughout the Upper Peninsula.. Age dates not consistent are attributed to Keewanawan intrusion. The southern pro- vince boundary may therefore occur on a line from Manistee to Tawas City as suggested by geophysical data. 2) Rock that is consistent with the lithologies found in the Central province occurs in Berrien County. 3) Rock types that agree with what is found in the out- crop area of the western Grenville province are found in southeast Michigan east and southeast of a line from the Ohio border. along the Ingham-Livingston County line and through Saginaw Bay City. 4) Nothing new can be said about possible Keewanawan rocks at this time. 17 SUGGESTIONS FOR FURTHER INVESTIGATION The best suggestion for further work is to have more basement tests drilled in areas of scientific interest. These could be best defined by geophysics. The strong anomalies of the Mid-Michigan gravity high would be an ideal place to start so that one could obtain both lithological and age date data. Other areas of strong interest include the transition area in the center of the basin. The depth to the top of the basement in this area makes any such test highly un- likely. however. The area of the Albion-Scipio trend is interesting in that it has been postulated that movement in the basement is the cause of the fracture related dolomite that is the oil trap. Just to have samples from any of these locations would add much to what we know. for the spacing of wells is now so wide that any correlation is im- possible. 18 BIBLIOGRAPHY Bass. M.N.. 1960. "Grenville boundary in Ohio". Jour.of Geol.. v. 68. pp. 673-677. . 1965-68. Personal communication to Wm. Mantek. Champion. B.L.. 1971. Personal communication. Dobrin. M.B.. 1960. Introduction to Geoghysical Prospecting. New York. McGraw Hill. Dutton. C.E. & Bradley. R.E.. 1970. Text accompanying U.S.G.S. Map #1-631. Ells. G.D.. 1971. Personal communication. Henderson. J.R. & Zeitz. I.. 1958. Inter retation of an aero- magnetic Survey of Indiana. (U.S.G.S. Prof. Paper 31 -B . Heinrich. E.W.. 1965. Microscopic Identification of Min- erals. New York. McGraw Hill. Hinze. W.J.. 1963. Gravit and Ma netic Anomal Ma s of the Southern Peninsula of Michigan. (Michigan Geol. Sur- vey. Report of investigation. #1). . 1971. Personal communication. . & Merritt. D.W.. Basement rocks of‘the Southegg Peninsula of Michigan. (Studies of the Precambrian of the Michigan Basin. Michigan Basin Geological Society). 1969. Kellogg. R .L.. An Aeromagnetic Study of the Lower Peninsula of Michigan. 1971. Ph. D. Thesis in preparation. Mich. State Univ.. Dept. of Geology. Kuehner. Irvin. 1971. Personal communication. Layton. F.L.. 1971. Personal communication. Lidiak. Marvin. Thomas. & Bass. 1966.‘Geochronology of the Mid-Congénent Region". Jour; of Geophys. Res.. v.71. Nov. 19 . McCromick. G.H.. 1961. Petrology of the Precambrian Rocks of Ohio. (Ohio Geological Survey. Report of Inv.. 41) Muehlberger. W.H.. et al. 1967.‘Basement Rocks in the Con- tinental Interior of the United States”. A.A.P.G. Bulletin. v. 78. 19 20 Reed. Robert. 1971. Personal communication. Rudman & Blakely. 1965. "Study of a basement anomaly in In- diana". Geophysics. Oct.. 1965. Rudman. A.J.. Summerson. C.H.. & Hinze. W.J.. 1965.‘Geology of the Basement in the Midwestern United States? A.A.P.G, Bulletin. v. 49. #7. July. 1965. Stonehouse. H.B.. 1969. Precambrian around and under the Michigan Basin. (Mich. Basin Geol. Soc.. Studies of the Precambrian of the Michigan Basin). . 1971. Personal communication. Summerson. C.H.. 1962. Precambrian in Ohio and Ad oini Areas. (Ohio Geol. Survey. Report of Inv.. #44) Turner. F.J.. & Weiss. L.E.. 1963. Structural Analysis of Metamorphic Tectonites. New York.McGraw-Hill. Yettaw. G.A.. 1967. Upper Cambrian and Older Rocks of the Security-Thalmann No.1 Well, Berrien CountyI Michigan. Unpublished Masters Thesis. Mich. State Univ.. Dept. of Geology. APPENDIX fir: 1.1%... \\ MICHIGAN DEPARTMENT OF CONSERVATION W MAP 1 LOCATION OF BASEMENT TESTS IN MICHIGAN 0/. !. 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Beaver Island #2 (6-37N-10W) Depth Rock Type Description 4720- Sandstone Quartz. clear-pink. frosted. rounded 4740 90$: slightly feldspathic in lower pt. 4740- Sandstone As above with increase of feldspar to 4745 20% 4745- Granite Quartz. clear.angular 25%: Feldspar. 4800 clean. fresh 60%; Some more mafics at base indicated by rust and magnetite grains. some Epidote present Pan American Oil Company Drasey #1 (29-35N-2E) 5600- Sandstone Quartz. rounded. frosted; Feldspar up 5720 to 10% in some intervals; show of Pyrite and some rust: some possible Chalcopyrite at 5680-90 5720- Quartzite Quartz. clear. angular cuttings some 5880 grainyness visible in larger peices. Bands with some pyrite alternating with bands without sulphides 5880- Quartzite As above with dark minerals and some 5910 Feldspar grains 5910- Greenstone Piagioclase lathes. Chlorite Visible 5940 Meta-Basalt Some Pyroxenes. Amphiboles possible Security 011 and Gas Company Thalmann #1 For detailed log refer to Yettaw (1967) Samples spot checked for aouracy and found to agree 27 St. Clair Oil and Gas Company Hurst #1 (26-5N-16E) Very poor samples due to rusting of contaminating drill steel. Biotite can be seen clearly but the other minerals are coated with a thick coat of rust. The ammount of Biotite indicates a Gneiss of a Schist. Grain size is also very fine due to the use of cable tools Bernhardt Puzzuoli #1 (3-2N-16E) 4142- Sandstone Quartz. rounded. frosted. some Biotite 4152 at base 4152- Quartz-Biotite Quartz 70+%. clear and angular 4188 Gneiss throughout interval with some bands as high as 85% quartz: Biotite most common accessory with bands of 20% biotite. very few Feld- spar grains seen. some of the samples have rusty clumps of grains where ident- ification is impossible Marathon Woodhaven #1 (22-48-103) 3650- Arkose About equal amounts of Quartz and Feld- 3660 spars with 20% Magnetite. Mggnetic susceptibility 26277.49110' emu/cc 3660- Arkose As above with dramatic decrease in 3670 Magnetite to less than 5% 3670- Sandstone Quartz. Medium to fine grained. round- 3710 ed. frosted very little Feldspar 3710- Granite Quartz. clear. angular 30%: Potash 3755 Feldspar. angular. fresh 50$; Mafics (Biotite. Magnetite. Amphiboles) 20$ Slight show of chlorite. Feldspars zoned at base of section 3299- Sandstone 3366 3366- 'Granite 3375 Nash” 3375- Granite 3376.5 28 Sturman Chapman #1 (29-53-103) Quartz. clear to frosted. rounded. slight show of feldspars Quartz. slightly rounded. Feldspars cleaved and surfaces cloudy with alter- ation. rounded; some Magnetite Quartz 70% (some from above); Feldspar and Mafics Furgison and Garrison 3626- Sandstone 3634 3634- Sandstone. 3642 Regolith. Granite 3642- Gneiss 3655 3655- Gneiss 3657 3657- Gneiss 3671 Shimp #1 (16-78-6E) Quartz. rounded. frosted. fine grained 90%; Some Biotite and Magnetite present Quartz. 90%. some fresh some as above: Chlorite 2%: some Feldspars and Biotite (Published log reports precambrian top at 3637) Quartz 70%; Chlorite 5-1523 small gar- nets possible at top of section; rest of sample is Feldspars Quartz. 60%: Chlorite; altered Feld- spars. some feldspar textures seen in the chlorite Quartz. 60$: Biotite.10 ; Chlorite.10% Feldspar and others 20 3 minor varia- tions. samples rusty at bottom with possible steel contamination 3595- ”Granite 3627 Wash" 3627- Granite 3395 Gneiss Beck Sancrant #1 (19-73-7E) Quartz and Feldspar. weathered. poss- ible Cambrian or Precambrian Quartz 50-90}: Feldspars. Chlorite. Biotite. and show of pyrite and “Jasper” Cuttings fine to very fine 29 Beck Sancrant #1 (coate) 3895- Gneiss As above with sericite 3900 3900- Gneiss As above without sericite. but with 4025 more Chlorite; some Magnetite. show of amphibole 4025- Granite Quartz; Potash Feldspar: Plagioclase; 4030 Gneiss Biotite; Amphibole; Magnetite: Coarse cuttings. slight foliation visible 4030- Granite As above. fine cuttings with mostly 4140 gneiss Quartz and very little other minerals 4140- No Samples 5335 5 85- Gneiss Samples coated with rust from Drill 5 95 steel. not able to obtain a good discription Eckett Taylor #1 (32-33-73) 3836- Sandstone Quartz. rounded. frosted 95% 3855 3855- Arkose or Quartz. as above 60% to 30% at base; 3875 “Granite Feldspar. cleaved. blocky. with rounded Wash“ corners. surface alteration 3875- Granite Quartz 30%; Feldspar 50%; Accessories 3900 20%; Drills finer than above and peices show breaking across mineral boundaries some possible weathering in top 4 feet Colvin and Associates Meinzinger #1 (lZ-ZS-7E) 5670- Sandstone Quartz. drills very fine 5673 5673- Granite Quartz. some from above 60% Potash 5692 Feldspars clearly visible 30 Chamness Tory Comm. #1 (27-13-7E) 5993- Sandstone Quartz. rounded. pink-white 6071 6071- Chlorite- Sample mostly Quartz from above. with Biotite Biotite the most common accessory; some Schist Feldspar and some Chlorite showing a1- teration in larger pieces Colvin Voss #1 (16-1S-7E) 6321- Sandstone Quartz. rounded. frosted 6368 6368- Chlorite- Sample mostly Quartz from above: Bio- 6410 Biotite tite; Chlorite. some larger pieces Schist showing slikensides?: show of Muscovite and Feldspar Mobil Messmore #1 (11-3N-5E) 7100- Sandstone Arkosic; Quartz and Feldspar. weathered 7140 7140- No Sample 7160 71(50- Granodiorite Plagioclase; Hematite; show Quartz; 7589 Diorite Pyroxene; Biotite; Leucoxene; Sphene Gneiss Called a gneiss because of textures seen in thin section Consumers Power Company Brine Disposal #1 (31-4N-15E) “615.5 Intermediate Mostly Plagioclase with Hornblende (4616.5 to Mafic needles. some injected material. broken Gneiss at 16.5 with 400 dip with slikensides and much alteration to chlorite 31 Consumers Power Company Brine Disposal #1 (cont.) 4616.5 Intermediate As above with more injected material 17.3 to Mafic 4617.3 18.0 4618.0 18.7 4618. 19. 7 8 4619.8 22.5 4622.5 24.0 o 6 4624. 24. 4624.6 25.5 4625.5 26.2 4626.2 27.0 4627.0 28.0 4628.0 29.3 4629.3 30.0 4630.0 34.0 Gneiss Very Fine Grained. broken along folia- tion at 45° Bands of potash rich Feldspars and bands of Biotite. Hornblende. and Plagioclase; bottom broken at 600 dip with alteration Chlorite Gneiss with 2.5'band of altered Biotite grading to gray. Minor Calcite vains perpendicular to foliation As above bottom broken at 45° As above broken at 90° to axis As above with slight increase in mafics foliation at 55° As above with band of diorite-pegmatite7 cutting across foliation(see photo) As above. core badly broken with no control Top broken at 50° dip and 80° rotation from previous breaks. strong alteration slikensides present Feldspars 70%: Mafics 20-30%: Quartz less than 10% As above. becoming more mafic at base Intermediate and mafic bands Biotite-Chlorite band. slight foliation homogeneous with minor Calcite and Quartz Fine grained dark rock. mostly Chlorite vains parallel to above foliation 32 Pan American Oil Company Drasey #1 Naonetic Susceptibility Depth (x10 U emu/cc) 5600-10 1373.20 10-20 616.54 20-30 420.37 30-40 252.22 40-50 364.31 50-60 224.20 60-70 532.46 70-80- 420.37 80-90 336.29 5690-5700 616.54 5700-10 364.31 10-20 224.20 Quartzite Section 20-30 140.12 30-40 182.16 40-50 112.10 50-60 392.34 60-70 $04.44 70-80 168.15 80-90 84.07 5790-5800 168.15 5800-10 84.07 10-20 448.39 20-30 196.17 30-40 560.49 40-50 588.51 50-60 280.24 60-70 504.44 70-80 392.34 80-90 896.78 5890-5900 672.59 5900-10 532.47 Greenstone Section 10-20 1457.27 20-30 2185.91 30-40 1933.69 5940 circ 30 2101.84 5940 circ 60 3390.96 33 Consumers Power Comoanv Brine Disposal #1 Depth Naonetic Susceptibility (x103 emu/cc) 4616.1 65.67 4617.5 32.13 4620.2 38.31 4624.3 43.78 4626.6 21.89 4627.3 49.26 4628.1 60.20 4629.8 65.67 4634.0 43.78 Bernhardt Puzzouli 51 4135-38 896.64 38-42 1092.78 42-48 1653.19 48-52 2381.70 precamhrian 52-58 1737.24 58-62 1737.24 62-66 1457.04 66-72 2605.86 72-79 1457.04 79-83 980.74 83-88 2437.74 Marathon Woodhaven #1 3670-80 812.71 80-90 1429.25 3690-3700 896.78 3700-10 476.42 Precambrian 10-15 700.16 15-20 1092.96 20-25 980.86 25-30 980.86 35-35 252.22 35-40 $32.47 40-45 $32.47 45-50 588.51 50-55 532.47 3299—3310 3310-15 15-23 23-30 30-42 42-55 55-66 66-75 75-76.5 34 Sturman Chaomanil 280.20 560.40 392.28 308.22 1457.04 840.60 560.40 1092.78 2521.80 Furgison & Garrison Shimp #1 3626-34 840.60 34-42 2241.60 (Transition, Basement 37) 42-45 560.40 45-55 Samole too small 55-57 756.54 57-62 1401.00 62-67.5 700.50 67.5-71 2745.96 (Poss. Steel contamination) Mobil Messmore #1 7360-70 56.05 70-80 28.02 80-90 70.06 7390-7400 28.02 7400-10 56.05 10-20 28.02 30-40 140.12 40-50 14.01 50-60 14.01 60-70 42.04 70-80 14.01 80-90 0.00 7490-7500 112.10 7500-10 42.04 10-20 84.07 20-30 28.02 30-40 112.10 40-50 56.05 50-60 14.01 ro-7n 98.09 70-80 56.05 80-89 126.11 Photo 1: Thin section of Quartzite from Pan American Oil Co.-Drasev #1. Plane polarized light v Photo 2: Thin section of Quartzite from Pan american Oil Co.-Drasev #1. Crossed Micols Photo 3: Polished section of Veta—Basalt fror the Pan Arerican—Drasev $1. Reflected Lijnt Photo 4:. Thin Section of fuartz and Kicrocline from the Securitv-Thalmannfll. Crossod Nicols (Overlv thick) 37 Photo 5: Nicrocline from the Security-Thalmann # . Crossed Nicols (faction too Thick) Photo 6: Alhite twins in a relect orain crom the rohil-vessmore #1. Crosced Ficols 38 o a, Photo 7: Thin section of rock from the Mobil- Nessmorefil showing flow structures around a relect grain. Crossed Nicols Photo 8: Polished section of same area as Photo 7 under reflected liqht. Photo 9: Polished section of rock from the Nohil- Messmore #1 showins larce “ass of Hematite with Feldspar drains. Reflected lioht. 3.1. Photo 10: Thin section frow the fiobil-Fessmore w showino cataclastic texture of the Feld- spar grains 40 fi -‘ h 7%: at, Photo 11: Biotite drain with other fero-majnesian mineral Grains from the Mobil-Kessmore #1. Photo 12: Se _— ction of core from the Consumers Power- ine L)isposal #1. Note hand of injected terial cutting across foliation 41 Photo 13; Section of core from the Consumers Power - “rine Disposal #1. Note heavv alteration along broken tace and how the angle of break is equal to the foliation Photo 14: Altered Biotite and Feldspar in reflected light from Consumers Power-Brine Disposal #1 Photo 15: Chlorite anleeldspar in the Consumers Power-Brine disposal #1. Reflpc+ca Lioht V\-r\—‘ Photo 16: An unusual yellow grain of Leucoxene fror the Lonsumers Power-Brine Disnosal #1. Reflected Light. 7 “7:11 11M @fluiyfljmmm tilifil "WI“ 74753