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Rwism SEE [1me fHESlb This is to certify that the thesis entitled Dolomitization in the North Adams Oil Field, Aren%r%se° n‘t’éfir‘bfl Ronald Glenn R 1 bhey has been accepted towards fulfillment of the requirements for _M.n.S_n.__ degree in m MEI/L 5/ Major professor Date q/é’r/ffl 0-7639 lllllllllllllllllM 0V FIRES: 25¢ per W per rim RETQRNDS LIBRARY MTERIAL§: Planat bookretum tovemo chargefm circulation records APP 2 9 ms V /W%’ In 2,9019% . ‘_ 1 DOLOMITIZATION IN THh NORTH ADAMS OIL FIELD, ARENAC COUNTY MICHIGAN By Ronald Glenn Richey A THESIS Submitted to Michigan State University in partial fulfillment of the requirements for the degree of MASTER OF SCIENCE Department of Geology 1980 ABSTRACT Dolomitization in the North Adams Oil Field appears to be mainly epigenetic and is the result of fluids moving up through fractures into the Dundee. This is shown by the generally high degree of dolomitization between 80 and 160 feet below the tOp of the formation. This coin- cides with natural rock porosity as shown by well logs. Dolomite also seems to be concentrated along the length of the main field which is interpreted to be a fault, and also along the smaller field interpreted to be an anti- cline. Finally, there appears to be a small amount of dolomite associated with the overlying Bell Shale which may have been a source of both Mg2+ and Fe2+. This dolo- mite occurs just below the top of the Dundee formation. ACKNOWLEDGMENTS I wish to express my gratitude to Dr. C. E. Prouty, Committee Chairman for his advice and time, given in this study. I wish also to thank Dr. D. F. Sibley and Dr. J. W. Trow for their review of the thesis text. Also, I would like to thank my mother, Ethel Richey and my aunt, Eleanor LaVean for their help in typing this work. ii TABLE OF CONTENTS LIST OF FIGURLS . . . . . . . INTRODUCTION . . . . . . . General Statement - Previous Work . - . . . . STRATIGRAEHIC FRAMEWLRK STRUCTURAL FRAMEWORK - . . . . THE NORTH ADAMS OIL FIELD Location and Extent - . - History and Development ° ° Structure Top of Dundee ° ° Structure Top of Traverse ' Isopach . . . .. . . . Production vs Structure ' ° LIMESTONE AND DULCMITE ANALYSES - Experimental Method 0 . . Source of Samples 0 . . Sample Selection . . . Sample Preparation . . X-Ray Diffraction Procedure Calibration Curve . . . Isodolic Maps . . - . Vertical Dolomitization Variation Petrogenetic Analyses- - - Core 0 o o o o o 0 Well Cuttings - ° ° 0 Model of Dolomitization - O O O O I“ Summary of Dolomitization Wo k Done Conclusions ' ° ° ° ° Appendices ° ° ° ° ° I List of Wells Used ' II Dolomite Percentages in This Page Area III List of Wells Used in Vertical Analysis BIBLIOGRAPHY ' O o 0 o o o 0 iii iv \OO\(=‘l—‘l—‘ 11. 12. 13. 14. 15. 16. 17. 18. LIST OF FIGURES Stratigraphic Succession Michigan . . . . . Michigan Region Tectonic Map . . . . . . . Structural Trends in the Michigan Basin . . . Location of North Adams Oil Field in Michigan . Faults and Folds of a Wrench Deformation Model . Structure Map on the Top of the Dundee Limestone Structure Map on the Top of the Traverse Limestone Traverse Group Isopach Map . . . . . . . Dolomite Ratio Map-~O-20 Feet Below the Top of the Dundee Limestone . . . . . . . . . . Dolomite Ratio Map--20-h0 Feet Below the Top of the Dundee Limestone . . . . . . . . . . Dolomite Ratio Map--hO-6O Feet Below the Top of the Dundee Limestone . . . . . . . . . . Dolomite Ratio Map--60-80 Feet Below the Top of the Dundee Limestone . . . . . . . . . . Dolomite Ratio Map-~80-100 Feet Below the Top of the Dundee Limestone . . . . . . . . . . Dolomite Ratio Map-—lOO-120 Feet Below the Top of the Dundee Limestone . . . . . . . . . . Dolomite Ratio Map--120-1h0 Feet Below the Top of the Dundee Limestone . . . . . . . . . . Dolomite Ratio Map-~lhO-160 Feet Below the TOp of the Dundee Limestone . . . . . . . . . . Vertical Dolomite Variation I . . . . . . Vertical Dolomite Variation II . . . . . . iv page 10 11‘ 14 21 15 16 17 31 33 35 37 39 41 43 45 w as INTRODUCTION The Dundee (Devonian) is one of the major sources of oil in Michigan. Production appears associated with at least some type of dolomitization. Attention has been called to the diagenetic origin of dolomite in various areas (Prouty, 1948, Cohee and Landes, 1958; Adams and Rhodes, 1960: Deffeyes, Lucia and Weyd, 1965; Illing, Wells and Taylor, 1965: Bathurst, 1971). hEach of the studies has certain special conditions under which dolomite is formed. Some studies have indicated certain dolomites in the Michigan Basin as diagenetic in origin (Lasemi. Y. 1969: Newhart, R.E.. 1976: Dastanpour, M., 1977; Syrjamaki, R.M.. 1977). In other studies within the Basin where dolomite is shown to be epigenetic in origin (Landes. 1946: Powell, 1950; Jodry, 1954; Egleston, 1957; Tinklepaugh, 1958: Paris, 1977; Dastanpour, 1977; Hamrick, 1978; TenHave, 1979, Hyde. 1979) there is the question as to the source and movement of the dolomitizing fluids. The diagenesis of shales produces water, Fe and Mg (Boles and Franks, 1979), during illitization. The Bell shale which overlies the Dundee may have served as a source of Ferroan dolomite. Another likely source is from 2 fluids which have picked up Mg from the dissolution of more deeply buried dolomites. Syrjamaki (1977) has shown that this dissolution has happened in the Lower Ordovician in the area of the Albion-Scipio oil field. Probably this dolomite would be less iron rich. It is the principal purpose of this study to investigate the distribution and characteristics of any dolomite present to possibly determine the origin(s) of the dolomite in the North Adams field. That there is dolomite in this Field has been shown by Landes (1946) and Jackson (1958), both using simple acid tests to show a general presence or absence of dolomite. With x-ray diffraction analysis. it is possible to do a much more detailed study and show vertical and lateral variations in the dolomite. Structural maps are to be used to compare the dolomitization to structural changes. Petrographic analysis of grains stained for ferroan dolomite was done to indicate the possible source of the dolomitizing fluids. The North Adams field (Figure 4) was chosen for the following reasons: (1) Reconnaissant work by Landes (1946) and Jackson (1958) shows that dolomite is present; (2) The field shows a different orientation than those done in the past, most other fields showing general NW-SE orientations 3 instead of NE-SW; (3) Samples are available. along with at least a short section of core: and (4) This field is midway between West Branch (TenHave. 1979) and the Kawkawlin (Hyde. 1979) fields and should either reinforce or else change con- clusions found in these fields. It is hoped that the results found in this study will be helpful in finding and developing other lineartype fields and also in developing general conclusions about this type of dolomitization. 4 Previous Work In a study of the relationship between porosity and secondary dolomite. Landes (1946) looked Specifically at the dolomitization in the Adams oil field. The study related dolomitization to oil occurrence. Jackson (1958) tried to relate structure to dolomitization by looking two dimension- ally at the structure of the top of the Dundee and dolomitiza- tion. Jackson differentiated dolomite from limestone using a simple acid test. In all three fields Jackson studied, including the North Adams, structure and dolomitization were related. Several studies using Dolomite/Calcite ratios have been done to determine local variations in d010mitization. Powell (1950) used a wet chemical method in testing the Pinconning field, a field having about the same orientation, but smaller than. the North Adams. Jodry (1954) used the titration method in testing the fields in Mecosta County, specifically looking at secondary dolomitization. Tinklepaugh (1957) also used the titration method, looking at Dundee dolomitization along fold axes in structures in the central Michigan Basin. She found correlation between structure and dolomitization. Dastanpour (1977) started the current trend of using x-ray diffraction to find Dolomite-Calcite ratios in his study of the Dundee and Traverse formations in the Reynolds's Oil 5 Field, and concluded that the Dundee dolomite was of both early (diagenetic) and later (epigenetic) origin. whereas the Traverse was of epigenetic origin. Finally Hamrick (1978). Walker Field, TenHave (1979), West Branch Field, and Hyde (1979), the Kawkawlin Field. were all recent studies of the Middle Devonian, using the x-ray diffraction method. TenHave and Hyde's works both showed good correlation between struct- ure and dolomite. Hamricks also showed this, but also showed a trend of diagnetic dolomite to the west end of the field. Regional semi-quantitative dolomitization studies were made in the Middle Ordovician by Newhart (1976), Lower Ordovician by Syrjamaki (1977), and on the Traverse by Runyan (1976). These studies show the presence of early diagenetic dolomite to the west. A regional depositional and strati- graphic study of the Middle Devonian was made by Gardener (1974). STRATIGRAPHIC FRAMEWORK The Dundee studied in this field is overlain by the Traverse Group and underlain by the Detroit River Group (Figure 1). These three make up the Middle Devonian in Michigan. The Traverse Group as described by Cohee and Underwood (1945) lies conformably on tOp of the Dundee. The Traverse Group is divided into three units, the Traverse Formation at the top, the Middle Traverse limestone, and the Bell Shale at the base. Cohee (1947) described the Traverse in eastern Michigan as interbedded argillaceous limestones and shales with a little pure limestone. The general trend is for the Traverse to become more calcareous to the west. The Dundee as used in this paper includes everything from the base of the Bell Shale down to the top of the Detroit River. Ehlers and Radabough (1939) on the basis of surface work divided the formation into the Dundee at the base and Rogers City above. These divisions are based on faunal differences and they are almost indistinguishable lithogically. Any subsurface work must either treat them as one unit or divide them arbitrarily. According to Cohee (1948). 6 STRATIGRAPHIC SUCCESSION IN MICHIGAN «a mum-nor. T] E. 8 i CENOlO MVMV NIGMAl YEIMS $.00, 'OIMAVION hunt-lot...» u—v——.-..~ “It“ "nu-”dw-Mn— “MW mu ~—_l 5—...___-——- Figure l ‘ 8 the Rogers City-Dundee is typically a dark brownish-buff dolomitic limestone to dolomite. Tinklepaugh (1957) showed that dolomitization is the locallized result of replacement of marine limestone. The Detroit River Group is mainly limestone with some anhydrite, becoming dolomitic, and more anhydritic in western Michigan (Tinklepaugh 1957). STRUCTURAL FRAMEWORK The North Adams field lies nearly in the center of the Michigan Basin, with the true center directly to the west. Arches rim the basin, the Wisconsin Arch to the West, Kankakee Arch to the Southwest, the Findlay to the South- east and the Algonquin Arch to the east (Figure 2). The problem of the origin of the Michigan Basin has been addressed by many workers whose conclusions vary appre- ciably as to both time and mechanics of development. Newcomb (1933) and Pirtle (1932) proposed that the Basin formed in the Precambrian-Keweenawan disturbance. Kirkham (1937) attributed settling to the movement of magma in the crust. Lockett (1947) believed that the Basin settled because of the load of sediments produced from Precambrian mountains that surrounded the Basin. Cohee and Landes (1958) believed that the Basin came into being in the late Silurian. continuing on and off into the late Mississippian. Hinze and Merritt (1969) using gravity and magnetic measurements believed the Basin was the result of a Precambrian rift zone (Keweenawan). Paleozoic intrabasinal structures (Figure 3) are 9 AM I|CAN Figure 2. A ... , g - .. ~ .g- ., .g. .—--.---—- up. --_-—.-..- u H- . : p.."..“..—o—f.. ‘76:"... zu- w\.~~‘wv . woe-o_ ‘9‘: 09m .— - . \?J; $Y; .u. 11.. “(3‘ ITWES~o~MQ§"' -9’VV'Z’?mrflsg* Cr“ "Ms ”“7 T\:EZ~\ ( d \A“\« 4 0‘- /.-:w ---- b 081‘. “'3' “no: o‘u .. Z’;'u'io'ivo"“l.-", 1 I : \> "" I ' . .fl' I’. If: I \ m;..fi.a:"/ ll, 7W‘“.l’ ”flaunt“ /-”" . § (”0.000. -n. --- _. C:/ /c} t 0"...“ Gun. —u ".”'II -0 0- 3.“ «II- . /‘.’ I; III ‘ .' ./ '55:- :2 /'/ i‘ / ./n f , h OMAV 'IDCI wat- . ./ | no" unmu --- X .353. “é: )5.” ”nil/I". 7413““: ._.... .4 " ‘ Mia-4’4?» Mm ~. ° / ' \ \ I A ./ | ,3) z "“7 l / . j | “i , 3 ’c‘u‘n amt/'2”; um ""—’¢F‘oph .7;- F‘ ,4” 1' ' MI 'I/7"' i - \ / . ‘I .II . ‘ E..'/’ . '\O\ . \‘\ u “gill! Icéi'l-"Jé'I/T-w :Kfig‘i'VT W“ """“' \A... I / / ' ,/‘/' . /—-" L,.._...‘-—----"" -. f I It a I A u A o n . a 7/1 I x I . -_ I ~/ . .\ . ). //!,43//’/'/ {I g ! /)Yl/ ! \ /.LL / ’7 .L/ ’ ’L_. Figure 3. Major Structural Trends in the Michigan Basin (compiled by C. 3., Prouty, 1971) 12 generally thought to be the result of movement of Precambrian basement rocks producing near-vertical faults. Prouty (19763. 1976b)believes lineaments taken from LANDSAT imagery repre— sent shear faults with lateral movement, and whose azimuths define a wrenching model responding to stresses directed from the east-southeast: further, it is considered that most basinal folds (other than saltfilled and possible radial folds) are genetically related to the mechanics of the wrench— ing tectonics (Figure 3). THE NORTH ADAMS OIL FIELD Location: The field is located in the eastern part of the Arenac County, sections 11.14.15.22,23,24,25.26.27 of Adams Town- ship (T 19N, 3E). The field can be divided into two separate fields: one to the northwest following a probably fault zone, about 3 miles long and up to 1/2 mile wide and referred to herein as the Main Field: southeast following an anticline about 3/4 mile in diameter, referred to herein as the South- east Field (Figure 8). Developmental History: The first discovery well in the southeast field, the Shearer #1, was drilled in section 26, in May 1938. into the Traverse. Initial Production was 68 Bbls, increased to 83 Bbls with acidation. The first well in the Main Field, the Yenior #1 section 22, completed July 1940, produced 500 Bbls, 2,500 Bbls after acidation. At first both fields were called "Adams", but as it became obvious that they were two separate fields. the Main Field was designated to be North Adams. Because almost all the production came from the North Adams, present day reports put the Adams production into the North 13 0-» travail ": ‘2‘ . I L, '- Lu i.- till“ .‘I I I 'i- i I ' ' It 31.331.- ‘L’JJ'TL'U; '70"? ‘ stream ‘ I :II ' I . . - r2 . . x . 5......4:£°9._+ i. z ' “not I ;_ I o r— 1.. I! «use . (1!! (ll! - nun-u ,0 0 4+. - Cl. ‘0 Q‘V. JCI‘DI ' 090.3. ¢ . . h d—u "can“ Figure ‘3 , r 1107: o (397 1,5102 105m 0 L" (,1 244:4 0 1 4 3 2 13533 14434 25970 O f“ 0 11249 148.57 0 13655 12695 18810 13856 L o O L 9 IO 11 12 12219 zazr 19970 O O o 12022 11343 , c 12970 2142 1:19 C 0 11685 1 38 11318 . é‘ J 11036 1 115 0 10.11 11353» 10765 o O 16 15 14 13 1C '02 1. 54 (8 . 74GB 1068? , . . y 4 1 :114 1088 $16 6 C1 «111 1 L 8301 1217.2 515 5955 was ‘15” o 11 c o 1'880 9-.94 67 4 ‘ t f asap “2‘. ‘8’“ o 3180 NO‘ 3.90 '67“, 7924 “.591 c1 0 C L ~ 130 (24 9§21 5043 8067 7116‘ ‘6” 1:351 W, (. U o o o o o 0 85m) 8461 82.51) . o 0 2| 23 24 8383 7. says . 33/36 3300 8‘ a ‘7, 8654 1293 91139 9093 9207 83-” 7909 743 8,555 c o o o o o g 0 o 9864 . , 5430 10671 5949 B713 9003 9 56 , 819( 0 o o o 6 0 o .5 5 7537 a 74 was 75 4 04 b 49 5 4a . ‘5 . ti 5 21117 9102 54.55 7906 1?” 52% 9102 3‘59 0 o 0 o .1901 4718 15729 “313 . [‘61 §23 . . b 5468 560 1 36 O s 13 . 98m 9&5 o 1 35 4 71 18538 F845 4&55 $366 4‘ a O 27 26 25 . . 12620 4508 4387 8911 r 1 a North Adams Oll Fle'd O . g y 4810 4.350 g4 . 9637 - 3701 Adams Townshlp. Arenac Co. 0 15448 0 Michi an .830 . 23496 Well Locanon Map N o 1 4496 P82 .5 . Oroyy Well 20124 95‘“ -Produc1ng W211 o C 1/4 1/2m1. 18 Adams figures and call the field collectively, the North Adams. Most of the drilling was completed by 1942. with a final 50 producing wells and 510 proven acres. To the end of 1977 when 18 wells were still pumping. a total of 9.385.156 Bbls of oil and 1.280 mcf gas had been produced. for an 18.402 Bbls recovery per drilled acre (National Oil Scouts and Landmen's Association Year Book. 1939.42.77). For most wells. pay was in the top 2-10 feet of the Dundee. although at the edges of the field pay was down to 90 feet below the top. Structure: Structure maps are based on formation t0ps as given on driller logs. Any logs that were incomplete or otherwise questionable were not used. Logs were verified where possi- ble by comparing formation top designations with actual cut- tings. Wells used are located on the base map (Figure 6). Driller's designations are tabulated in Appendix I. To fully interpret structure and timing of structural events. three maps have been constructed: the structure on top of Dundee and top of the Traverse; and an isopach map of the Traverse. The Dundee structure map (Figure‘?) shows both parts of the field. the Southeast Field (sections 23.26) and the Main Field (sections 11.14.22). The Main Field is very complex with alternating highs and lows. The Southeast Field on the 19 other hand. is very simple with the least closure to the E-SE. covering sections l3-lS.22-27. The orientation is basically W-NW. E-SE. nearly right angles to the Main Field. The Traverse structure map (Figure 8a) although similar to the Dundee does have several faults that do not show up in the Dundee structure. These faults are similar in orienta— tion to the Southeast Field. or nearly perpendicular to the Main Field. They are all parallel to each other and divide the main structure into cross-blocks. each of which appears to have moved in the left-lateral sense with some indication also of some vertical component. Isopach: The is0pach of the Traverse was constructed in order to determine when faulting and folding occurred. It would appear very unlikely that the Southeast Field structure had been formed or was forming during Traverse time. as there is a lack of thinning over the structure. In fact there are several highs. The isopach map of the Main Field is much less conclusive. as there is thickening and thinning along its length. This may be due to differential compaction with the faulting occurring after deposition of the Traverse. It would appear much more plausible that all the tectonism occurred at the same time rather than separately. for each of these closely-related structures. 20 Deformation Model: Moody (1973) developed a model (Figure 5) based on re- gional fault orientation studies which can be applied to ex- plain structures formed in the Michigan Basin (Prouty. 1970. 1976a). To produce these structures. forces probably came from a general eastward direction reactivating shear faults in the basement complex and creating the faults and related shear folds in the Paleozoic rocks. (Figure 3). Harding (1974) showed. using a clay model. that en echelon faults with related fold deformation structures are produced with wrench-type forces. This may show why there is a thickening in the Traverse isopach over some of the structures. They may be produced by deformation rather than sedimentation. They also may have been produced by differential solution or by dolomitization shrinkage. Hydrocarbon production vs structure: Dundee production in the southeast field follows the high very closely. with original pay thickness about 9 feet at the center of the anticline. decreasing towards the edges. The pay in the Traverse was much less with most wells deepened to the Dundee. Production along the Main Field is much less typical. As wells in the center of the structure had pay at the tOp of . Figure 5;--rau1ts and Folds of a wrench Deformation Mode] (constructed by J. D. Moody. 1973) 22 the Dundee but were not drilled through the pay. and because two wells on the edge of the field had oil cut water at 90 feet below the top of the Dundee. the pay was interpreted to be 90 feet thick (National Oil Scots and Landmens Association Year Book. 1942). More drilling in the southern most part of the field showed production that was very complex. with pay found at more than one level. or at least at levels other than the Dundee top. X-RAY ANALYSIS X—ray Diffraction: The x—ray diffraction technique was developed in the late 1950's (Tenet and Berge. 1956). and has been used in such studies of carbonate rocks as Weber (1967): Gunatilaka and Till (1971): Badiozamani (1973): Folk and Land (1975): and Supka (1977). This method has many advantages over other methods. Chemical methods are based on the amount of Ca and Mg. and can be influenced by the presence of other carbonate minerals. Thin section point counts can be very accurate but accuracy depends on the number of points counted. For example: with a mixture of 10% of one component and 90% of another. 400 points much be counted to achieve an accuracy of + or - 3%. or 900 points to achieve + or - 2% (Pettyjohn. Potter. and Siever. 1972). Lumsden (1979) has shown that an accuracy of + or - 3% or better. can result using x-ray diffraction. Samples used in this study were analyzed several times and found to vary from the mean by less than 3%. The accuracy of this method is limited by several factors: (1) The background is not constant over the range of values measured. (2) The peaks 23 24 are not totally centered over one point and using the area under the curve might improve accuracy but would be very time consuming. (3) Probably the greatest source of error is the fact that there is a range of crystal sizes. It is assumed when using this method that all crystals are the same size. This is never true. What compounds the error is the fact that there can be a bimodal distribution of grain sizes be- tween calcite and dolomite. Also. there may be a difference between the sample crystal size and the crystal size in the standard (Jenkins and Devries. 1968). (4) There are other errors associated with the equipment but these are probably insignificant. Method: The method used consisted of measurement and comparison of the peaks of calcite and dolomite. By finding their rel- ative height and comparing the ratios against a series of samples of known composition. the composition of the sample of unknown composition can be found (Tenet. 1956). As has been stated above. a source of error is introduced in this method because of nonuniformity of the peaks. Samples that are poorly packed. allowing more randomness in the grain orientation will tend to have broader. flatter peaks. To overcome this somewhat. there was an attempt to make packing uniformly tight for all samples. 25 Samples: Well cuttings from 38 wells. nearly all of which were cable tool samples. were chosen. The choice of wells was based mainly on getting the best distribution without using wells that were poorly sampled and/or contaminated. Cable tool wells were chosen over rotary wells because of the better quality of cable tool cuttings. with less caving and better depth control. Samples were then separated into 20-foot intervals. with 4 grams weighed per sample. Samples were crushed. using mechanical grinding for 10 minutes per sample. X—Ray Procedure: Samples were packed into a sample holder and placed into the goniometer. Equipment used was a G.E. x-ray diffraction goniometer. X-rays were produced using the Copper K alpha radiation with a nickle filter. at 50 KV and 10 MA. The cal- cite peak at 30.9602 theta and the dolomite peak at 29.400 were found. counted for 100 seconds and recorded. Because of small errors introduced in poor orientation of the sample holder. etc. the true peaks in most cases varied a little from their predicted angle. There was an attempt in each case to take readings on the true peak by manually setting the angle at maximum peak height. Background readings were 26 taken at 28.00. Each sample was x-rayed twice. at two dif- ferent spots on the sample. and the results were averaged. Calibration Curve: A calibration curve was constructed using standard sam- ples already prepared (Dastanpour. 1977). The curve when plotted. showed that the peak height ratio virtually matched the true dolomite/calcite ratio. with no corrections being indicated. ISODOLIC MAPS Dolomite maps are based on percentages as calculated by ratios. With the exception of the three samples noted in the appendix all values are based on 20 foot intervals. The three samples noted are based on samples less than 20 feet and are used only because of lack of good data in the center of the field. These values are meant only to show minimum dolomite values. All plots use a 5%1isodolic contour interval which is based on the accuracy of the data. Well logs men- tioned in the following are Gamma Ray-Neutron logs. and are listed in the Appendix. Lateral Variation: 0-60 Feet below top of Dundee (Figure 9-11): All well logs show that these intervals have little porosity. with a single exception. a log next to the field which shows some porosity from 0-20 feet. Dolomitization only can be seen to occur along the main structure. particularly in the producing zone. Even in wells that were not analyzed for dolomite be- cause of lack of cuttings or because they just penetrated into the Dundee. the Dundee was called dolomite in driller 27 28 logs. Where dolomite is found there are some very high val- ues but laterally dolomitization is rather restricted. 60—80 Feet below the top of the Dundee (Figure 12): All mechanical logs show this zone to be tight. No wells penetrated this deep in the center of the Main Field. In spite of this there has been some dolomitization. Two wells over the Southeast Field show the first indication of dolo- mitization in this structure. 80-100 Feet below tOp of Dundee (Figure 13): In this zone there is a transition from the tight. impermiable lith- ology above. into a very porous zone. as indicated by logs. In the Southeast Field there are 5 wells with 10% or greater dolomite. This is the first interval with a high dolomite value. 70%. which may indicate a small crossfault. It ap- pears that dolomitization continues on to the north of the Main Field. 100-120 feet below top of the Dundee (Figure 14): All mechanical logs show this zone to be very porous. Dolomiti- zation is laternally the most continuous of any levels studied. with at least a 15% isodol around both fields. Well #13655 has only 1%.dolomite showing. Although dolomitization is continuous on-structure. off-structure there has been little or no dolomitization. It appears dolomitization continues both to the North and South of the Main Field. 29 120—160 Feet below top of Dundee (Figure 15.16): Well logs show that porosity decreases from that in the above level. although it still exists. Control is less for these maps but they were included to show the high levels of dolo- mitization. (up to 75%). not necessarily right on structure. but adjacent to it. possibly indicating cross faults. Dolo- mitization on the southeast structure is decreasing with 7% dolomite. the high value at 140-160 foot level. Figure 9 Map of Dolomite Percentages 0-20 Feet Below top of the Dundee 5% Contour Interval 4 3 2 I 9 IO l1 I? 16 I5 I4 IE 0 0 El 23 24 O 28 27 26 25 o O I North Adams Oil Field Adams Township,Arenoc Co. ic igon Dolomite Ratio Map 020 feevbe1ow1he10p ofthe Dundee Formahon tDry We1l :Producmq wen 1/4 1/2m1 Figure 10 Map of Dolomite Percentages 20-40 Feet Below Top of the Dundee 5% Contour Interval 0 C1 1 O 10 11 12 16 15 14 13 (r, 21 23 24 O Q I C O I O as 27 25 25 O I North Adams Oil Field Adams Township,Arenac Co. Michigan Dolomite Ratio Map N 20» 4o leelbelow lop oi me Dundee Formation =Dry 1911 :Producmg Well 0 1/4 1/2m1. Figure 11 Map of Dolomite Percentages 40-60 Feet Below Top of the Dundee 5% Contour Interval 0 4 3 2 ' 9 10 || 12 16 15 I4 13 (j o 0 2| 22 23 24 o (1 o o I O 28 27 26 25 O North Adams Oil Field Adams Township,Arenac Co. Michigan Dolomite Ratio Ma 40760 1691 below lopaflhe Dundee Formahon :Dvy Well =Produc1ng Wel1 1/4 1/2m Figure 12 Map of Dolomite Percentages 60-80 Feet Below Tap of the Dundee 5% Contour Interval North Adams Oil Field Adams Township.Arenac Co, Michigan Dolomite Ratio Ma 60-80 feet below lopof Dundee Formohon 0:131, Well I:Produc1ng We11 1 1/2mi Figure 13 Map of Dolomite Percentages 80-100 Feet Below Top of the Dundee 5% Contour Interval Norlh Adams Oil Field Adams Township,Aren . Michigan Dolomite Ratio Map 50400 «99.1 new lop at Dundee Format1 O=Dry Well .=Praduc1ng Well c [/4 1/2m1. Figure 14 Map of Dolomite Percentages 100-120 Feet Below Top of the Dundee 5% Contour Interval North Adams Oil Field Adams Township,Arenac Ca. Michigan Dolomite Ratio Map N 100'120 feet below lopot the Dundee Farmahon O=Dry Well .tpioduclng Well 1/4 1/Zmi. *4 Figure 15 Map of Dolomite Percentages 120-140 Feet Below Top of the Dundee 5% Contour Interval 1 // é/ / Figure 16 Map of Dolomite Percentages 140-160 Feet Below Top of the Dundee 5% Contour Interval O 3 2 | (3 9 10 11 12 15 13 2' 24 g o O \ 5 23 25 O I O 0 North Adams Oil Field Adams Township,Arenac Co. is gan Dolomite Ratio Ma N 140 '1601eetbelowtop oi Dundee Formahon O=DvyWe11 tprooucmg Well 1/4 1/zm1. §.__. VERTICAL DOLOMITIZATION VARIATION In order to determine what effect the structures had on vertical dolomitization. two groups of wells were chosen and averaged. Ten wells that are on or adjacent to the Main Field. and eight wells over the center of the anticline were used. Also a single well that was well off both structures were used to show dolomitization in an off-structure position (Appendix III). The resulting graphs (Figures 17.18). show that vertical dolomitization was affected by the structures. The well off- structure has a high of 3.9% dolomite over the 120 feet that the well penetrated. The average of all wells shows that overall. dolomitization follows porosity. as shown by mechan- ical well logs. The logs show the upper 80-90 feet to have a low porosity. with much higher porosity below this. The average of all wells shows that the top 80 feet never averages more than 5%.dolomite per interval. while the lower 80 feet never averages less than 10%0 Dolomitization on the structures is very similar between the two fields. except for the fact that at every interval dolomitization in the Main Field is greater than that on the Southeast Field. Finally. it can 46 % Dolomite 0 5 10 15 20 20 - 40 ~ so - so - 100 - 120 - 140 - 160 - Du ndee A_verage of all- Wells of top 1 % Dolomite“ bel ow 20 4o 60 / so 100 120 Depth Well nu 13655 Figure 17 below top of Dundce Depth “Duo-it: 20 40 60 3. ‘f’ _l 100 * 120 [ - 3 J no I ' 160 Avalage Value: to: 10 We”: fh‘main fiel&’ ‘ fibula-it: o s 10 is ' iv FT— 2o ‘ no so so 100 120 140 160 Avatago Value: For 8 Well: Dvor Altlcline . AL ,1 - -...1 . _._,,, 4 Figure 18 49 be seen that the average top 20 feet has nearly twice as much dolomite as either of the next two intervals (20-60 feet). PETROGRAPHY Core: There was one core that was available for study. This core. from the Bolger and Rose State Adams #1 in section 14. (permit #10572). was from 96 1/2 to 99 feet below the top of the Dundee. This well. although not a producer. was very close to the fault. Of the 2 1/2 feet. 8 slides were pre- pared and stained. The thin sections show that the original sediment was almost entirely a wackestone. with a fine micritic matrix. Interbedded are a few thin. grainstone beds with longitudi- nally-oriented fossils showing current flow. The types of fossils preserved are crinoids. brachiopods. ostracods. corals. and bryzoans. indicating an Open marine environment. Pellets were also found in both thin sections and grain mounts. In the thin sections the cement is nonferroan calcite which. because of is blocky rather than elongate crystal habit. is interpreted to be fresh water-deposited. low-magnesium calcite (Longman. 1980). Stylolites are very common and tend to occur in swarms. They are mainly of the sutured type. Much 50 51 of the original fabric of the rock has been recrystallized as can be seen by the large amounts of neomorphic spar. This Spar can be seen to be preferentially recrystallizing some beds over others. There has been a degree of dolomitization which varies in amount throughout the slides. The occurrence of dolomite can be divided into three different associations. stylolites. in the matrix. and in the pore space. The greatest concen- tration of dolomite occurs along stylolites where it appears to either have crystallized from solution moving along the stylolite or from selective dissolution of calcite along the stylolite. The crystals are slightly larger than those found in the matrix. and are euhedral. This problem will In dis- cussed later. The dolomite in the matrix is evenly distri- buted. Dolomite grain size is very small. and crystals tend also to be euhedral. By far the largest dolomite crystals occur in the larger pores. These crystals are grown together and are euhedral. When stained for iron these crystals are the only ones that can be seen here to be even slightly ferroan. Those that did stain have a faint. rather thick zone. that has some iron. The faintness of this zone indicates that there is only a little iron compared to the ferroan dolomite discussed later. These crystals have clear rims and cloudy centers. 52 Well cuttings: The well cuttings used in this study were prepared as grain mounts and stained. Two wells. one with high dolomite and one off-structure were divided into 20 foot intervals as they were for x-ray analysis. Cuttings from four producing wells. from within the producing zones were also prepared. Well #8045 contained the highest percent dolomite of any interval in any well. with 85%.between 140-160 feet. In this interval none of the dolomite is ferroan. Dolomite'changes going upward become almost totally ferroan at the top. In the top 20 feet there is even a little ferroan calcite. Well #4203 shows the same thing. Also there is one instance where ferroan dolomite. in the tOp 20 feet. fills an unbroken ostracod. Unlike the West Branch field. these wells have virtually no chert (Ten Have. 1979). Those grain mounts prepared from cuttings in the pro- ducing zones are all very high in ferroan dolomite. There are a few crystals that show zoning with high iron at the edges. These crystals are euhedral and probably grew in open pore space. Nearly all the original rock has been either dis- solved or recrystallized with the rare exception of a few Spots of micritic matrix. These cuttings all have a lot of opaque material. most of which is organic. but in reflected light. some can be seen to be pyrite. There is one piece of 53 shale that contains “inclusions" of ferroan dolomite. MODEL OF DOLOMITIZATION All dolomitization models depend on chemical. pressure. or temperature regimes that differ from those in the typical environment of carbonate deposition. In determining whether or not the dolomite found in this area is early diagnetic. only chemical changes need to be considered. Differences in temperature and pressure at the near surface are not known to be important. In order for dolomite to be produced there must be a mechanism whereby it will replace calcite. Several possible models have been proposed. based mainly on observations of dolomitization in modern sediments. Most of these models depend on a high Mg/Ca ratio. This has been found in several places where dolomite is now forming. and seems to always be associated with hypersaline waters. In the sabka-type environment (Illing et a1. 1965) it can be seen that high degrees of evaporation of sea water produce evaporites. particularly anhydrite and gypsum. As both of these minerals incorporate Ca into their structure. there is a loss of Ca from the fluids. raising the Mg/Ca ratio. When 54 55 the ratio becomes high enough dolomite replaces the calcite. There are other variations such as dolomitization by seepage reflux (Adams and Rhodes. 1960). or by a density gradient (Deffeyes. 1965). but both of those depend only on evapor- ation. and hypersaline waters. Another type of model depends on the mixing of marine water with phreatic water (Badiozamani. 1973; Land. 1973; Folk and Land. 1975). This mixing produces a fluid which is supersaturated with reSpect to dolomite. but understaurated for calcite. This model depends on the presence of both sea and fresh water in the sediment for a length of time long enough for dolomitization to occur. Badiozamani (1973) showed that dolomite can be produced with a mixture of 5-30% sea water with fresh water. There needs to be a great deal of mixing in order to replenish the Mg in solution when it is being re- moved by dolomitization. All the above models depend on an emergence of the land above sea level. In the western part of Michigan there are interbedded evaporites in the Dundee showing that there may have been a sabka type of environment in that area (Dastanpour. 1976). Howeven,evaporites are not found in the Dundee of central or eastern Michigan. There is a blocky calcite cement from which one might infer a fresh water origin (Bathurst. 56 1971). Given that the rock was originally deposited in marine water and later there was fresh water indicates that probably at some time in between there was a mixing of the two. Assuming this to be the case. it would be expected that the mixing would have come before the deposition of the Bell shale as this would probably stop descending fresh water. As was shown by the iSOpach of the Traverse (FigureEb). it appears the structures in both fields were not in existence in Dundee time. In order for most of the dolomite to have been formed by the mixing of fresh and sea water. the pattern of dolomitization would not have followed the structures. As it did follow the structures it is doubtful that it was the result of the Dorag model (Badiozamani. 1973). There is another possibility that. as in the Bahamas. there was dolomitization by hypersaline brines. but with a loss of evaporites. This is shown. as above. to be unlikely because the dolomite follows the structure too closely. If the dolomite is not early then it would have to be later epigenetic. probably at the same time the structures formed. There are two main possible sources for the dolomit- izing fluids. either from below. or from the shales above. It has been shown (Boles and Franks. 1979) that the diagenesis of shales at about 100°C causes Smectite and K+to change to Illite: 57 + . + . 3 93K 1 57 KNaCaZMg4Fe4A114Si180100(OH)2 O+H20 Produces K M F A1 S (OH)2 0+1 57 N 2++ 3 14 2+ 2+ 5.5 92 c1.5 22 1350100 . a . Ca +4.38 Mg+ 4.78 Fe2++ 24.66 Si2++ 570 2++ 11.4 (OH)- + 15.7 H O 2 + K + Smectite + Water + Illite + Na2++ Ca2+ Mgz++ Fe2++ Si2++ 02++ OH + Water This reaction depends on the presence of potassium and Smectite. The original amounts of these two components will affect how much of the products are produced. The iron pro- duced is reduced iron. Fe2+. Potassium Ferrocyanide. the stain used in this study. specifically stains for this re- duced iron (Evamy. 1963). It has been shown (Evamy. 1969). that reducing conditions are required for the substitution of Fe for Ca in calcite; under oxidizing conditions. the re- duced iron is not available. As iron content in the dolomite found in this study increases to its maximum at the top of the formation. it would appear that the bulk of dolomitization at the tOp of the formation occurred under reducing conditions. There are still a few problems with this model. Bower and others (1975) showed that the shale tends to act as a closed system for Illite. Mg. Fe. and Si. Yeh and Savin (1976) showed using 02+ isotopes that SiO definately appears to 2 stay in the shale. Little or no silica was found in this 58 study. However Fe and Mg were found. Boles and Franks (1979) pointed out that although bulk chemical analyses show little change in Fe. Mg or Si with depth. significant amounts can be released from the shales without apparent change in bulk chemistry. There is evidence that there is slightly more total dolomite in the top 20 feet of the Dundee compared to the amount of dolomite found from 20 to 60 feet. The difference is small. about 4% at the top. to about 2% below. but is very consistent. This tends to show that any fluids produced from the shales either were not able to do much dolomitizing. or else they were lost quickly down the fault and other frac- tures where they mixed with other fluids. The latter seems more likely as seen by the ferroan gradient in dolomite in wells along the fault. The fact that dolomitization is greater with depth. and also the lack of ferroan dolomite at depth would tend to show that not all dolomite was the result of shale diagenesis. In well #8043 the interval from 140 to 160 feet had no trace of ferroan dolomite. with a total of 84%.dolomite. None of the dolomite found in the core. with the exception of that found in large pore Openings. was ferroan either. This would seem to mean that the main dolomitizing fluids were nonferroan and probably came from below. 59 Syrjamaki (1977) showed that approximately 350-500 feet of the Prairie du Chien dolomite has been lost in one place in south-central Michigan. presumably by dissolution. It is conceivable that deeply buried dolomite could become dis- solved. and the solution could then move upward and re- precipitate the dolomite. If this were the case the dolomite should be greatest where there was the greatest movement of solutions. mainly in areas of high permeability. There are many ways to get good permeability in lime- stone. Hyde (1979) stated after studying a core from the Kawkawlin field. that much porosity seemed to be related to dissolution of both fossils and matrix. There is also por- osity produced by faulting and resulting breccia. Jackson (1957) indicates brecciation in core from the Dundee in the Pinconning field. When folding occurs. as in this field. there are usually joints formed. Dolomitization itself may form porosity. In this field there are some very good avenues for the movement of dolomitizing fluids. particularly along the faults. As shown in (Figure13). the greatest degree of dolomitization occurs along the main structure. The highest values found anywhere were in the pay zone (Appendix II). Also there appears to have been lateral movement along highly porous beds. as shown by well logs. resulting in high average dolomite 60 values from 80-160 feet below the top. with much lower values from 0-80 feet. Finally there has been dolomitization along the anticline. Possible the solutions were hotter or other- wise less dense than the surrounding original fluids causing them to move into the highest permeable zone that they could. This might explain why only the axis of the anticline was dolomitized: also the anticline is likely fault related with fracture porosity and permeability present. Finally there is the problem of the dolomite found along stylolites. There are several possible interpretations. One is the concentration of dolomite because of dissolution of calcite but not of the dolomite. The fact that the dolomite grains are larger than those found in the matrix might be ex- plained by dissolution of very small dolomite grains and re- precipitation of the larger grains. The stylolite might act as a local pathway for these fluids. Another interpretation could be that later solutions moving through the rock would flow along stylolite surfaces because of the clay. and the dolomite could then be deposited. Another possibility is that solutions moved along stylolite surfaces at the time the stylolite was forming. There is no way to prove or disprove any of the above possibilities. given what has been observed in this field. SUMMARY OF DOLOMITIZATION WORK DONE IN THIS AREA (1) Early diagenetic dolomite: This type of dolomite was found almost entirely in the west part of the state. Newhart (1976) has shown in his regional study of the Middle Ordovician that. at least during Middle Ordovician time. the Wisconsin arch was emerging and the resulting uplift in west Michigan allowed subareal ex- posure of the carbonates and resulted in dolomitization. Runyon (1976) showed that in the Traverse. clastics in the carbonates increased to the west. In Hamrick's (1976) study of the walker Field. it was shown that in the west end of the field dolomite increased greatly and did not follow structure. indicating that there is a diagenetic dolomite. Dastanpour (1977) showed that there was diagenetic and epigenetic dolomite in the Reynolds field in the Dundee but only epigenetic in the Traverse. The Dundee dolomite in this field was associated with anhydrite. Generally this type of dolomitization results in much greater degree of dolomitization. Sections with 60 to 100% dolomite are most common. This dolomite tends to follow large. broad areas and is not influenced by local small structures. 61 62 (2) Structurally controlled. epigenetic dolomite: This type of dolomite is associated with the faults and folds that occur throughout the Michigan Basin. Landes (1946). looking at the North Adams field. and Jackson (1957) looking at the North Adams. Pinconning and Deep River fields. were able to determine that dolomitization directly on top of Dundee structures was greatest with little or no dolomite off structure. Later with x-ray techniques. it became possible to show in more detail along which paths the dolomitization occurred. Hyde (1979) was able to show. using petrographic studies of core. that dolomite followed natural porosity laterally. presumably along bedding. TenHave (1979) showed the same thing using porosity as given by Gamma-ray Neutron logs. Dastanpour (1977) was able to show that although the Dundee below. showed diagenetic dolomite. the Traverse dolo- mite still appeared to be epigenetic. These studies all showed that dolomitizing fluids appeared to follow vertical permiability. produced by their reSpective structures. Be- cause of the distribution of the dolomite. greater lower in the Dundee. the source of fluids is generally assumed to be from a more deeply buried formation. possibly the Prairie du Chien as was stated earlier. Possibly some type of trace element distribution work could be done to solve this problem. The degree of dolomitization of this type is generally 63 much less than diagenetic dolomite. Where there has been found to be good porosity. values most commonly range from 10 to 30% dolomite over 20 foot intervals. although in a few instances they ranged much higher. Probably the thing that is the most different about this type of dolomite over the other two types is the lack of lateral continuity. Away from structures this type of dolomite does not occur. All fields of this type appear to fit the Moody (1973) wrench deformation model. In eastern Michigan there is a re- markable similarity in the field orientations. The West Branch. Deep River. and Kawkawlin fields all have a WNW-ESE orientation. All are broad anticlines with wrenching causing them to curve slightly south on their east ends. The North Adams and Pinconning fields are oriented NNE-SSW. and are virtually parallel in their orientation. (3) Dolomite resulting from the diagenesis of shales: The diagnesis of shales produces the least degree of dolomitization. with generally less than 5% found over the 20 foot interval next to the shale. This study was the first to specifically mention this type of dolomite although data in other studies show its presence. Tinklepaugh (1957). using chemical methods observed that total iron content in the area she studied was greater in the 5 feet next to the Bell Shale than in the 20 feet next to the shale. Iron concentration 64 did not appear to follow the structure. TenHave (1979) used luminesence and observed that there was more iron in the in- terval from 0 to 20 feet from the Bell Shale than in any in- terval from 20 to 170 feet below the base of the shale. Young (1955) in his study of the Stony Lake oil field found) no relationship between dolomite and structure. but found that there was more dolomite from 0-3 feet than from 0-10 feet from the top of the Traverse Limestone. Both Hamrick (1978) and Dastanpour (1976) showed the same for the Traverse. with slightly higher dolomite percent averages at the tOp and bottom of the limestone. where it was in contact with the Antrim and Bell Shales respectively. Both TenHave (1979) and Hyde (1979) observed this for the Dundee capped by the Bell Shale. Possibly some of the "damming effect" observed may be the result of this kind of dolomitization. From concluded: (1) (2) (3) (4) (S) (6) (7) GENERAL CONCLUSIONS the preceding analysis the following can be Dolomitization appears to be mostly epigenetic. There are two potential sources of dolomitizing fluids. the Bell shale. and from fluids derived from lower formations. In the top 160 feet of the Dundee. overall dolo- mitization decreases upwards showing the Bell shale was probably not the main source of fluids. Dolomitization is highest on the main structure and in crossfaults. Dolomitization highs on the Southeast Field follow anticlinal highs. Laterally moving fluids follow pre-existing planes of permeability as shown by Gamma-Ray Neutron logs. There is dolomite associated with stylolites which may have formed in one of several ways. 65 LIST OF WELLS USED IN STUDY, ARENAC COUNTY Permit No. Section 1. 11073 12879 13533 25979 Section 2. 4205 10628 14484 24424 Section 3. 25102 Section 9. 8666 Section 10. 13655 Section 11. 11249 11343 11819 11820 12022 Adams Township. T19N. R3E -1288 -1304 -1287 -1313 -1312 -1289 -1311 -1322 -1327 -l314 -1308 -l306 -1322 -1319 -l323 APPENDIX I Traverse Group TOp 66 Traverse Group Thickness 790 802 800 782 810 816 800 815 792 758 804 806 784 803 788 Dundee Top -2078 -2106 -2101 -2087 -2097 -2122 -2105 -2111 -2137 -2119 -2072 -2119 -2112 -2116 -2123 -2111 67 Permit Traverse Group Traverse Group Dundee No. Top Thickness Top Section 11. 12142 -1320 796 -2116 12219 -l316 788 -2104 12327 -l316 788 -2104 12328 -1320 781 -2101 12695 --- --- -2119 12702 -1306 819 -2125 18810 -1321 800 -2121 Section 12. 14837 -1271 831 -2102 19070 -1276 840 -2116 Section 13. 9711 -1274 812 -2086 Section 14. 7880 -1322 790 -2112 10198 —1316 784 -2100 10572 -l3l7 804 -2121 10622 -1308 790 -2098 10702 -1315 786 -2101 10774 -1318 776 -2094 10765 -ll96 896 -2092 10821 -1322 792 -2114 10855 -1311 794 -2105 10932 -1320 775 -2095 10987 -1313 792 -2105 11036 -1309 797 -2106 11115 -l321 788 -2109 11304 -1298 790 -2088 11318 -1280 818 -2098 11685 -1292 806 -2098 11837 -l332 790 -2122 Section 15. 7872 -1298 794 -2092 8181 -1310 785 -2095 8301 -1284 795 -2089 68 Permit Traverse Group Traverse Group Dundee No. Top Thickness Top Section 15. 8988 ~1300 793 -2093 9158 -1245 838 -2083 10497 -1250 843 -2093 12408 -1312 790 -2102 20352 -1296 784 -2080 Section 17. 7943 -l364 792 -2163 8784 -1196 812 -2008 14579 -1220 798 -2018 Section 20. 4507 --- --— --- Section 21. 8383 -1315 782 -2097 19862 -l303 789 -2092 20164 -1309 787 -2096 Section 22. 7463 -1306 775 -2081 7895 -1306 785 -2091 7905 -1302 775 -2097 7907 -1307 798 -2105 7908 -1309 771 -2080 7961 -1335 756 -2091 8043 -1314 780 -2094 8044 -1311 777 -2088 8087 -1309 784 -2093 8180 -1320 775 -2095 8230 -1297 754 -2051 8300 -1313 764 -2077 8345 -1315 772 ~2087 8382 -1306 780 -2086 8436 -1311 782 -2093 8461 ~1310 794 -2104 8472 -l313 773 ~2086 8560 -1315 786 -2101 69 Permit Traverse Group Traverse Group Dundee No. TOp Thickness TOp Section 22. 8575 8667 8773 8880 8949 9008 9009 9207 9821 9169 9289 9290 9294 9821 10548 10549 10671 11293 Section 23. 7462 7809 7837 7875 7876 7901 7924 8192 8215 8334 8480 8574 9214 9291 13966 Section 24. 4804 8654 8346 -1311 -1229 -1305 -1339 -1312 —l313 -1310 -1304 -1301 -1305 -1301 -1305 -1312 -1301 -1302 -1308 -1308 -1299 -1261 —1270 -1261 -1293 -1269 -1299 -1277 -1270 -1268 -1176 -1308 -1272 -1294 -1269 -1251 -1247 -1247 -1269 776 856 765 747 770 766 765 774 785 783 781 790 790 785 772 787 783 793 785 792 803 793 797 800 795 884 774 794 805 797 875 815 786 794 -2097 -2085 -2070 -2086 -2082 -2079 -2075 -2078 -2086 -2088 -2082 -2095 -2102 -2086 -2074 -2095 -2091 -2092 -2055 -2062 -2096 -2062 -2096 -2077 -2063 -2060 -2082 -2066 -2099 -2066 -2126 -2062 -2060 -2063 Permit No. Section 24. 8365 8576 16855 Section 25. 4365 4571 4755 5117 8335 9501 9606 9637 13824 16010 18538 20031 23496 Section 26. 4190 4387 4496 4508 4610 4718 4785 4855 4901 5160 5523 6465 7461 7906 8246 8911 9102 9468 9865 13122 Traverse Top -1252 -1271 -1279 -1252 -l245 -1270 —1273 -1268 -1271 -1264 -1270 -1222 -1262 ~1273 -1270 -1266 -1272 -1254 -1275 -1284 -1268 -1262 -1259 -1192 -1264 -1260 -1264 -1181 -1264 -1268 -1265 -1183 -1264 ~1270 -1280 -1200 Traverse Group Thickness 796 815 Dundee Top 71 Permit Traverse Group Traverse Group Dundee No. Top Thickness TOp Section 26. 13373 15236 15448 15729 20124 20213 44966 Section 27. 8045 9377 9701 9702 9844 10547 12625 17314 26705 Section 28. 10390 11258 -1255 -1275 -1264 -1269 -1286 -1293 -1256 -1307 -1219 -1307 -1313 -1304 -1276 -1310 ~1336 ~1297 -1356 -1404 929 890 800 782 778 824 787 810 789 807 771 -2236 -2109 -2107 -2095 -2082 -2100 -2097 -2046 ~2086 -2163 -2175 Wells in Pay zone: Permit Number 9377 8230 9290 72 Feet Below Dundee TOp 0-9 43-45 1-3 Percent Dolomite 92.6 99.1 90.4 APPENDIX II DOLOMITE PERCENTAGES Permit 0-20 2-40 40-60 60-80 80-100 100-120 120-140 140-160 Number 14.7 3.5 11.7 20.2 10.9 1.3 3.3 1.8 1.1 4203 4.6 19.1 15.1 2.4 2.0 8.7 4.4 1.6 1.0 3.0 1.2 4496 8.0 --- 7.5 4.4 1.4 4901 7.2 -"‘- 8.6 12.8 3.5 1.7 1.6 3.4 1.3 7461 12.3 9.4 9.6 8.9 5.4 15.3 1.2 7872 8.6 25.5 3.1 4.2 2.6 1.4 1.5 2.0 1.7 7875 6.9 18.2 5.4 14.7 22.5 1.3 7901 7961 8043 8045 13.9 3.6 9.7 4.7 1.5 1.3 84.6 31.5 14.7 18.8 3.8 2.8 2.6 1.3 3.1 5.8 1.4 6.2 . 7.9 8.3 7.0 22.9 17.6 2.1 1.9 8181 8301 7.4 7.0 10.4 --- 18.7 5.2 2.4 3.2 3.8 3.7 8334 8335 5.2 3.2 14.2 17.1 10.9 1.3 7.5 10.8 22.4 24.1 1.9 2.4 8346 8382 9.1 12.0 16.2 2.6 2.4 1.0 4.3 1.6 3.3 60.5 15.9 13.6 1.2 .9 8383 13.3 12.9 2.2 1.1 1.3 8575 7.0 2.1 5.9 6.7 13.9 70.4 .9 2.8 1.6 8576 77.2 15.5 2.6 1.4 2.6 10.1 9008 9169 9291 9390 9468 9501 9637 2.6 1.8 20.7 .5 4.0 2.7 2.4 9.0 7.1 10.9 7.0 4.7 3.2 1.4 2.8 1.4 4.2 3.1 13.0 4.6 14.1 3.4 4.5 4.4 2.9 6.0 17.1 4.4 2.1 2.0 14.2 3.2 4.8 1.3 2.2 1.4 1.8 4.4 1.4 6.1 3.6 3.2 3.1 20.9 7.3 6.1 7.7 8.9 20.8 20.2 34.1 9701 9844 10390 9.8 29.6 21.3 5.3 6.2 --"" 2.3 7.3 1.6 10549 10671 10855 10.8 2.4 1.2 15.3 6.8 7.8 1.0 2.9 2.0 2.0 73 74 Permit 0-20 2-40 40-60 60-80 80-100 100-120 120-140 140-160 Number 11318 1.1 1.4 3.6 20.0 18.7 12.5 9.8 10.7 12879 4.5 1.5 .5 1.9 25.4 22.4 3.5 ---- 13122 --- 1.2 1.2 2.6 .9 22.6 8.3 ---- 13655 1.2 .7 2.9 3.9 1.9 1.1 --- -—-- 14484 1.9 1.4 .9 2.9 1.7 29.6 13.1 ---- APPENDIX III List of Wells Used in Dolomite Averages Iain Field: Anticline: 7875 4901 7901 7461 7961 8334 8043 8335 8181 8346 8382 8576 9008 9291 9169 13122 10549 11318 BI BLI 0G RA PHY Adams, J. E., and Rhodes. M. L., 1960, Dolomitization by Seepage Refluxion: Am. Assoc. Petroleum Geologists Bullo' V. 44' pp. 1912-1940. Badiozamani, K.. 1973, The Dorag Dolomitization Model- Application to the Middle Ordovician of Wisconsin: Jour. of Sed. Petrology, v. 43, pp 965-984. Bathurst, R. G. C. (ed.) 1971, Carbonate Sediments and Their Diagenesis: Developments in Sedimentology, v. 12, Elsevier, Amsterdam, 620 p. Berry. L. G. (ed.) 1974, Selected Powder Diffraction Data for Minerals: Joint Committee on Powder Diffraction Standards, lst Edition, 833 p. Bloomer, A. T., 1969, A Regional Study of the Middle Devon- ian-Dundee Dolomite in the Michigan Basin, unpublished Masters Thesis, M.S.U. Boles, J. R.: and Franks, S. G., 1979, Diagenesis in Wilcox Sandstones of Southwest Texas: Implications of Smectite Diagnesis on Sandstone Cementation. Journal of Sed. Pet.. vol 49, No. 1, pp 55-70. Cohee, G. V.. 1944, Thickness and Character of the Traverse Group and Dundee Formation in Southwestern Michigan, U.S. Geol. Survey Oil and Gas Inv. Prelim. Chart 4. , 1947, Lithology and Thickness of the Traverse Group in the Michigan Basin: U.S. Geolo. Survey Oil and Gas Inv. Prelim. Chart 28. , and Underwood, L. B.. 1945. Lithology and Thickness of the Dundee Formation and the Rogers City Limestone in the Michigan Basin: U.S. Geol. Survey Oil and Gas Inv. Prelim. Map 38. Dastanpour, M., 1977, An Investigation of the Carbonate Rocks in the Reynolds Oil Field, Montcalm County, Michigan: Unpublished Master's Thesis. Michigan State University. 75 76 Deffeyes, K. S., Lucia, F. J., and wey1, P. K., 1865, Dolo- mitication of Recent and Plio-Pleistocene Sediments by Marine Evaporite Waters on Bonaire, Netherlands Antilles: Soc. of Econ. Paleontologists and Mineralogists, Spec. Publ. No. 13. pp. 71-88. Egleston, D. C., 1958, Relationship of the Magnesium/Calcium Ratio to the Structure of the Reynolds and Winfield Oil Fields, Montcalm County, Michigan: Unpublished Master's Thesis, Michigan State University. Ells, G. D., 1969, Architecture of the Michigan Basis: Mich. Basis Geol. Soc. Ann. Field Excursion, pp. 60-88. Evamy, B. D.. 1963, The Application of a chemical Staining Technique to a Study of Dedolomitization. Sedimento- logy, vol 2, pp 164-170. , 1969, The Precipitational Environment and Correlation of some Calcite Cements deduced from.Artificial Staining. Journal of Sed. Pet., vol 39, pp. 787-793. Fisher, J. C., 1969, The Distribution and Character of the Traverse Formation of Michigan: Unpublished Master's Thesis, Michigan State University. Folk, R. L., 1974, The Natural History of Crystalline Calcium Carbonate: Effects of Magnesium Content and Salinity, Journal or Sed. Pet., Vol. 44, No. 1, pp. 40-53. , and Land, L. S., 1975, Mg/Ca Ratio and Salinity: Two Controls over Crystallization of Dolomite: Am. Assoc. Petroleum Geologists Bull., v. 59, pp. 60-68. Gardener, W. C., 1974 Middle Devonian Stratigraphy and Depositional Environment in the Michigan Basis: Mich. Basin Geol. Soc. Spec. Papers, No. 1, pp. 43-48. Goodrich, R. E., 1957, Geology of the Reynolds Oil Field in Montcalm and Mecosta Counties, Michigan: Unpublished Master's Thesis, Michigan State University. Gunatilak, H. A., and Till, R., 1971, A Precise and Accurate Method for the Quantitative Determination of Carbonate Minerals by x-Ray Diffraction Using a Spiking Technique: Mineralogical Magazine, v. 38, pp. 481-487. 77 Hamrick, R. S., 1978, Dolomitization Patterns in the Walker Oil Field, Kent and Ottawa Counties, Michigan, University. Hanshaw, B. 8., Back, W., and Kieke, R. G., 1971, A Geochem- ical Hypothesis for Dolomitization by Groundwater: Econ. Geoll, v. 66, pp. 710-724. Hardin, T. P., 1974, Petroleum Traps Associated with Wrench Faults: Am. Assoc. Petroleum Geologists Bull., v. 58, pp. 1290-1304. Hinze, W. J., and Merrit, D. W., 1969, Basement Rocks of the Southern Peninsula of Michigan: Mich. Basin Geol. Soc. Ann. Field Excursion, pp. 28-59. Hower, J., Eslinger, E. V., Hower, M. E., Perry, E. A., 1976, Mechanism of Burial Metamorphism of Argillaceous Sedi- ment: 1. Mineralogical and Chemical Evidence. Geol. Soc. America Bull. vol. 87, pp. 725-737. Hyde, M. K., 1979, A Study of the Dolomite/Calcite Ratios Relative to the Structures and Producing Zones of the Kawkawlin Oil Field, Bay County, Michigan. Unpublished Masters Thesis, Michigan State University. Illing, L. V., Wells, A. J., and Taylor, J. C. M. 1965, Pene- contemporaneous Dolomite in the Persian Gulf: Soc. of Econ. Paleontologists and Mineralogists, Spec. Publ. No. 13. pp. 89-111. Jackson, R. P., 1958, Dolomitization and Structural Relations of the Deep River, North Adams, and Pinconning Oi1 Fields, Michigan: Unpublished Master's Thesis, Michigan State University. Jenkins, R., and DeVries, J. L., 1968, Practical X-ray Spectrometry: Springer-Verlag, New York, pp. 105-120. Jodry, R. L., 1954, A Rapid Method for Determining the Magnesium/Calcium Ratio of Well Samples and Its Use as an Aid in Predicting Porosity in Calcereous Formations: Unpublished Master's Thesis, Michigan State University. Krumbein, W. C., and Sloss, L. L., 1963, Stratigraphy and Sedimentation: Freeman and Co., San Francisco, 2nd Edition, pp. 71-74. 78 Kutsykovich, M. B., 1971, Roentgen-Diffractometric Method of Determination of Carbonates, Quartz, and Other Minerals in Sediments: Lithology and Mineral Resources, v. 6, pp. 513-514. Land, L. S., 1973, Contemporaneous Dolomitization of Middle Pleistocene Reefs by Meteoric Water, North Jamaica: Bull. of Marine Science, v. 23, pp. 64—92. , L. S., Salem, M. R., I., and Morrow, D. W., 1975, Paleohydrology of Ancient Dolomites: Geochemical Evidence: Am. Association Petroleum Geologists Bull., v. 59. pp. 1602-1625. Landes, K. K., 1946, Porosity Through Dolomitization: Am. Assoc. Petroleum Geologists Bull., v. 30, pp. 305-318. Lasemi, Y. 1969, Subsurface Geology and Stratigraphic Analysis of the Bayport Formation in the Michigan Basin, Unpublished Master's Thesis, Michigan State University. Lockett, J. R., 1947, Development of Structures in Basin Areas of Northeastern United States: Am. Assoc. Pet- roleum Geologists Bull., v. 31, pp. 429-446. Longman, N. W., 1980, Carbonate Diagenetic Textures from Nearsurface Environments, Amer. Assoc., Pet. Geol. Bull., vol. 64, No. 4, pp.461-487. Lumsden, D. N., 1979, Discrepancy Between Thin Section and X-ray Estimates of Dolomite in Limestone, Journal of Sedimentary Petrology, Vol. 49, No. 2., pp. 429-435. Michigan Geological Survey, 1964, Stratigraphic Succession in Michigan: Mich. Geol. Survey, Chart 1. Moody, J. D., 1973, Petroleum EXploration Aspects of Wrench- Fault Tectonies, AAPG, Vol. 57, No. 3, pp. 449-476. National Oil Scouts and Landmens Association Year Book, 1939, Volume 9. , 1942, volume 12. , 1978, volume 46. 79 Newhart, R. B., 1976, Carbonate Facies of the Middle Ordo- vician of the Michigan Basin: Unpublished Master's Thesis, Michigan State University. Paris, R.M., 1977, Developmental History of the Howell Anti- cline: Unpublished Master's Thesis, Michigan State University. Pettijohn, Potter, and Siever; 1973, Sands and Sandstone, Springer-Verlag, New York. Pirtle, G. W., 1932, Michigan Structural Basin and Its Re- lationship to Surrounding Areas: Am. Assoc. Petroleum Geologists Bull, v. 16, 145-152. Powell, L. W., 1950, Calcium Carbonate/Magnesium Ratios in the Rogers City and Dundee Formations of the Pinconning Field: Unpublished Master's Thesis, Michigan State University. Prouty, C. E., 1948, Trenton and Sub-Trenton Stratigraphy of Northwest Belts of Virginia and Tennessee: Am. Assoc. Petroleum Geologist Bull., v. 32, pp. 1596-1626. , 1970, Michigan Basin-Paleozoic Evolutionary Develop- ment: Geol. Soc. of Amer. Abst. with Programs, v. 2, No. 7, pp. 657-658. , l976d. Michigan Basin-A Wrenching Deformation Model? Geol. Soc. of Amer. Abst. with Programs, v. 8, no. 4, pp. 505. , l976b, Implications of Imagery Studies to Time and Origin of Michigan Basin Linear Structures: Abst., Am. Assoc. Petroleum Geologists 6lst Ann. Meeting, pp. 102. Runyon, S. L., 1976, A Stratigraphic Analysis of the Traverse Group of Michigan: unpublished Master's Thesis, Michi- gan State university. Supko, P. R., 1977, Subsurface Dolomites, San Salvador, Bahamas: Jour. of Sed. Petrology, v. 43, no. 3, pp. Syrjamaki, R., 1977, Stratigraphy of the Prairie du Chien Group of the Michigan Basin: Unpublished Master's Thesis, Michigan State University. 80 Tennant, C. B.. and Berger, R. W., 1956, X-ray Determination of Dolomite-Calcite Ratio of a Carbonate Rock: Am. Mineralogist, v. 42, pp. 23-29. TenHaven, L. E., 1979, Relationship of Dolomite/Limestone Ratios to the Structure and Producing Zones of the West Branch Oil Field, Ogemaw County, Michigan, Uh- published Master's Thesis, Michigan State University. Tinklepaugh, B. M., 1957, A Chemical, Statistical, and Structural Analysis of Secondary Dolomitization in the Rogers City-Dundee Formation of Central Michigan Basin: Unpublished Ph.D., Thesis Michigan State University. Wanless, J. R., 1979, Limstone ReSponse to Stress: Measure Solution and Dolomitization, Journal of Sed. Petrology, Vol. 49, no. 2, pp. 437-462. Yeh, H. W., and Savin, S. M., 1977, Mechanism of Burial Meta- morphism of Argillaceous Sediment: 3.9-Isotope Evidence. Geol. Soc. America Bull. vol. 88, pp. 1321-1330. Young, R. T., 1955, Relationship of the Magnesium/Calcium Ratio as Related to Structure in the Stony Lake Field, Michigan: Unpublished Master's Thesis, Michigan State University. // C < w North Adams on Field Adams T0wnship,ArenocCo. Michigan Structure top of the Dundee Formation Contour Interval 10H. O-Dry WeH O’Producmq Watt 0 v4 Wm‘t. w / 3 9 NW§ /\ [6 a 21 \§ £3 /\r\) 0 North Adams Oil Field Adams Township,Arenac Co. Michigan Structure top of the Traverse Formation Contour Interval 10 lt.anrl 50 ft. O'DWW’M .iFtaductnq Well l/4 l/2ml, N