I N F O R M A T IO N T O USERS This d isserta tio n was p roduced from a m icrofilm co p y o f the original d o cu m ent. While th e m o st advanced technological m eans to p h o to g ra p h and re p ro d u c e this d o c u m e n t have been used, th e quality is heavily d e p e n d e n t u p o n th e quality of th e original s u b m itte d . The follow ing explan atio n o f Techniques is provided to help you u n d erstan d m arkings o r p a tte rn s which may ap p ear on this reprod uction . 1. T he sign o r " ta rg e t" for pages ap p a re n tly lacking from th e d o cu m en t p h o to g ra p h e d is "Missing Page(s)''. If it was possible to o b ta in the missing page(s) or section, th ey are spliced into th e film along with a d ja c e n t pages. This may have necessitated cutting th ru an image and d up licatin g adjacent pages to insure y o u co m p lete co n tin u ity . 2. W hen m ark, copy image. 3. W hen a map, drawing or chart, etc., was part of the m aterial being p h o t o g r a p h e d th e p h o to g ra p h er follow ed a definite m e th o d in " se c tio n in g " th e material. It is cu sto m ary to begin p h o to in g a t the u p p e r left hand corner of a large sheet a n d t o co n tin u e p h o to in g from left to right in equal sections with a small overlap. If necessary, s ection ing is co n tin u ed again — beginning below th e first ro w and c o n tin u in g on until com plete. 4. T h e m ajority of users indicate th a t th e textual co n te n t is o f greatest value, however, a som ew hat higher quality rep ro d u ctio n could be from "p h o to g ra p h s" if essential to th e und erstand ing of the d isserta tio n . Silver prints o f " p h o to g ra p h s " may be o rd ered at a d d itio n al charge by writing th e O rder D epartm en t, giving th e catalog n u m b er, title, au th o r and specific pages y o u wish rep ro du ced. an image on th e film is o b lite ra te d w ith a large ro u n d black it is an indication th a t th e p h o to g ra p h er suspected t h a t th e may have m oved during ex p o su re an d th u s cause a blurred You will find a go o d image of th e page in th e ad jacen t frame. U n iv ersity M icrofilm s 300 N orth Z e o b R o a d Ann Arbor, M ichigan 48106 A Xerox E d u c a ti o n C o m p a n y J I 72-22,287 SHAH, Balkumar Prataprai, 1939EVALUATION OF NATURAL AGGREGATES IN KALAMAZOO COUNTY AND VICINITY MICHIGAN. Michigan State University, Ph.D., 1972 Geology U niversity Microfilms, A XEROX C om pany , A nn A rbor, M ichigan Copyright © by BALKUttAR PRATAPRAI SHAH 1972 All Rights Reserved EVALUATION OF NATURAL AGGREGATES IN KALAMAZOO COUNTY AND VICINITY MICHIGAN By Balkumar Prataprai Shah A THESIS Submitted to Michigan State University partial fulfillment of the requirement for the degree of DOCTOR OF PHILOSOPHY Department of Geology 1971 PLEASE Some NOTE: pages may indistinct Filmed University as Microfilms, have print. received. A Xerox Education Company ABSTRACT EVALUATION OF NATURAL AGGREGATES IN KALAMAZOO COUNTY AND VICINITY MICHIGAN By Balkumar Prataprai Shah The surface geology of Kalamazoo County was remapped with the help of Frank Leverett's manuscript field maps (available at the Michigan Geological Survey) and extensive field checks. The drift samples from the county were collected using the channel and pebble volume sampling methods. The petrographic analyses of gravel samples were carried out, and the data are correlated with the similar data from the surrounding nine counties in southwestern Michigan. Kalamazoo County lies in a reentrant district of the Lake Michigan lobe and the Saginaw lobe of the middle Wisconsinan glacial age. On the basis of provenance, observed lithologic distribution, and field evidences, a viable glacial history of the area has been pictured in seven figures. It is suggested that the Lake Michigan lobe and the Saginaw lobe were out-of-phase with each other. The Saginaw lobe sediments being laid down first Balkumar Prataprai Shah in the county and then pushed and overlain by the eastward advancing Lake Michigan lobe sediments. Characteristics of glacial, glacio-fluvial, aeolian, and other features and their associated elastics are described in detail. This information should help in future exploration of aggregate sources in Kalamazoo County. It is desirable, however, to incorporate the in­ formation regarding the nature and structure of local bedrock, thickness of glacial drift, and soils and their relation to the parent material, to complete the total picture of the area under investigation. Using available surface and subsurface information, attempts are made to present the total picture with the help of maps, cross sections, diagrams, and tables. The lithologic data are presented by a series of maps on which the percentages of each major lithologic group is entered, and isopleths are drawn. The resulting distribution patterns are clearly indicative of two pre­ dominant source areas in relation to sediment dispersal, and of glacial processes of two quite separate lobes. On the basis of above lithologic distribution patterns and geomorphology, the interlobate line is proposed The engineering properties, (Plate I). such as physical strength and chemical reactivity, show direct correlation with the lithologic composition of the drift in Kalamazoo County. Balkumar Prataprai Shah With the aid of petrographic analyses and the glacial geology, a map "Gravel Resources of Southwestern Michigan" is prepared. This map is a guide for giving preferences to the areas for prospecting future sand and gravel deposits. DEDICATION To My Family ii ACKNOWLEDGMENTS The writer wishes to express his deepest and most sincere gratitude to his major professor Dr. James W. Trow of the Department of Geology, Mi chigan State University for his patient guidance, advice, and constructive criti­ cism throughout this study. The writer is indebted to the following professors of the Michigan State University, who graciously served as members of his doctoral committee. Dr. Maynard M. Miller of the Department of Geology for providing intellectual stimulation for glacial inter­ pretation of the study area and his critical review of the manuscript. Dr. Chilton E. Prouty of the Department of Geology for his considerable professional aid and constant en­ couragement in the course of the graduate study and especially the doctoral work. Dr. Eugene P. Whiteside of the Department of Crop and Soil Science for his innumerable suggestions and helpful criticism concerning the soils and other aspects of the study. Thanks are due to Dr. William J. Hinze of the Department of Geology for his interest in the welfare and progress of the writer. The research was carried out under the auspices of the Research Laboratory Section of the Michigan Depart­ ment of State Highways as a Highway Planning and Research Project. The writer wishes to thank the entire laboratory staff, many of whom contributed materially with partial participation from time to time. It is not possible to cite every contributor to the project; however, Mr. M. G. Brown and Dr. N . E. Wingard require special mention for getting the project approval of the Research Laboratory Section and discussing the initial stages of the project. Recognition is also made of the efforts of the personnel of Graphic Presentation Unit and Photo Laboratory, who assisted in preparing the illustrations. Thanks are expressed to the personnel of the Michigan Geological Survey for furnishing well logs and other geological information. iv TABLE OF CONTENTS Chapter Page PART I I. INTRODUCTION ............................... Aims and Purposes of the Study Previous W o r k ................ II. 1 . . . 1 3 PHYSICAL SETTING..................... 6 Location........................... 6 A r e a ........................... Cultural Geography. . . . . . 6 . 6 Geomorphological Ch a r a c t e r ....... 9 Relief........................... D r a i n a g e ........................ 9 10 C l i m a t e ........................... 11 PART II III. FIELD INVESTIGATIONS ..................... 13 Surface M a p p i n g ................... .... Field Sampling..................... 13 Large Samples— Channel Sampling M e t h o d ........................ Small Samples— Spot Sampling Method . Auger S a m p l i n g ................... .... Sampling Problems .................... IV. GLACIAL HISTORY AND STRATIGRAPHY 17 18 19 19 . . . Pre-Wisconsinan Glaciation....... Wisconsinan Glaciation ................. v 15 21 22 25 Chapter V. Page Time-Stratigraphic Relations . . . . ................. Distribution of Drift 26 30 Lake Michigan L o b e .................... Saginaw L o b e ........................... The Lake M i c h i g a n —Saginaw Inter— lobate A r e a ........................ 32 34 CHARACTER OF SURFACE G E O L O G Y .............. 58 Glacial F e a t u r e s ........................... Terminal and Lateral Moraines. . . 36 58 . 60 The Kalamazoo Morainic System . . . The Tekonsha Moraine ................. Other Small Moraines in Kalamazoo C o u n t y ............................... 60 64 Till P l a i n s ............................... Dr uml i n s .................................. 71 73 Glacio-fluvial Features ................. Outwash Plains. .............. Lacustrine Plains and. Drainage Ways. . Clay and Silt Capping on Fluvial Plains Aeolian F e a t u r e s ........................... Sand Dunes and Loess Sediments Other Features . . . 67 74 74 79 80 81 81 .............. 82 Undefined Transitional Zones . . . . The Question of K a r n e s ................. 82 83 Types and Associated elastics . . . . Boulders and C o b b l e s .................... Gravel and Sand . ................. Silt and Clay . vi 84 84 86 86 Chapter VI. VII. VIII. Page BEDROCK G E O L O G Y ............................... 88 The Lithologic S equence.................... 89 Coldwater S h a l e ........................... Lower Marshall Sandstone................. 89 93 Bedrock Configuration and Pre—glacial D r a i n a g e ................................. S t r u c t u r e s .................................. 93 98 .............. 100 Isopach Map of Kalamazoo County . . . . Cross Sections.............................. Correlations of Bedrock and Drift Thickness................................. 100 103 107 SOILS OF THE A R E A ........................... 109 DRIFT THICKNESS AND STRUCTURE Soil Series.................................. Relation to Parent Material and Surface G e o l o g y .................................. Use bf Soils in Surface Mapping . . . . Ill 114 116 PART III IX. LABORATORY ANALYSIS OF SAMPLES .............. 119 Mechanical Analysis . . . . . . . . Petrographic Analysis . Lithologic Terms and Classification. . . Coarse Aggregates ....................... 120 120 121 123 Five-Size Fraction .................... Pebble V o l u m e ........................... 123 12 5 Fine Aggregates........................... 128 One-Size Fraction .................... 128 Heavy M i n e r a l s ........................... 129 Comparison of Channel and Pebble Volume T e c h n i q u e s .................... Determination of Engineering Quality . vii . 129 130 Chapter X. Page LITHOLOGIC DISTRIBUTION OF AGGREGATES . . Lithologic Map Interpretation and Provenance............................ . Igneous Rock C o n t e n t .................... Metamorphic Rock Content ............. Crystalline Rock Content ............. Chert C o n t e n t .............................. Carbonate and Chert Content . . . . Sandstone Content ........................ Siltstone and Shale Content . . . . Clay Ironstone Concretion Content . . Clastic Rock C o n t e n t .................... XI. ECONOMIC CONSIDERATIONS.................... 133 136 138 138 142 142 145 147 149 151 153 Sand and Gravel E c o n o m i c s ................. 154 Industry and C o s t ........................ Benef iciation.............................. 154 155 Potential Building Aggregates . . . . Gravel Pit Locations . . . . . . Highways, Population, and Gravel Pit Density Relations.................... Ground Water in Kalamazoo County . . . Environmental Application ................. XII. 132 157 158 158 159 161 AGGREGATE SUITABILITY FOR ENGINEERING USAGE. . Properties and Performance of Aggregates Physical Strength and Chemical R e a c t i v i t y .............................. Deleterious Aggregates and Their Desirability in Concrete . . . . CONCLUSIONS, ACADEMIC AND ECONOMIC ................. SUGGESTIONS FOR FURTHER RESEARCH . REFERENCES . . . ........................................ 165 165 166 169 174 176 G L O S S A R Y ............................................ A P P E N D I X ............................................... viii 185 188 LIST OF TABLES Table 1. Page Classification of Soil Series in Kalamazoo County in Old and New Classification Systems with Their Associated Natural Drainage, Parent Materials, and Glacial F e a t u r e s ..................................... 112 2. Lithologic Terminology and Classification. . 122 3. Gravel Lithology of Kalamazoo County, M i c h i g a n ..................................... 188 4. Mechanical Analysis 189 5. Gravel Lithology of Supplementary Study Area, Southwestern Michigan ................. 190 Sand Analysis from Kalamazoo County, M i c h i g a n ..................................... 191 6. ........................... LIST OF FIGURES Figure Page 1. Primary study A r e a ........................... 7 2. Location Map Noting Primary and Supple­ mentary Study A r e a s ....................... 8 3. 4. 5. 6. 7. 8. 9. 10. 11. 12. Modified Stratigraphic Classification of the Wisconsinan Deposits in Illinois . . 29 Map of Wisconsinan Age Moraines, North­ eastern Illinois, Northern Indiana, Southern Michigan, and Northwestern Ohio (after J. H. Zumberge, 1 9 6 0 ) ............. 31 Designated Morainic Systems of Michigan and Northern Indiana (after Leverett and Taylor, 1915) 33 Surface Geology of Kalamazoo County, Michigan. . . . . . . . . . . 38 First Regime Trend in the Lake Michigan— Saginaw Interlobate Glaciation . . . . 44 Second regime trend in the Lake Michigan— Saginaw Interlobate Glaciation . . . . 45 Third Regime Trend in the Lake MichiganSaginaw Interlobate Glaciation . . . . 46 Fourth Regime Trend in the Lake MichiganSaginaw Interlobate Glaciation . . . . 47 Fifth Regime Trend in the Lake MichiganSaginaw Interlobate Glaciation . . . . 48 Sixth Regime Trend in the Lake MichiganSaginaw Interlobate Glaciation . . . . 49 x . Figure 13. 14. 15. 16. 17. 18. Page Seventh Regime Trend in the Lake MichiganSaginaw Interlobate Glaciation . . . . 50 Hypothetical Cross Section Showing Inter­ relationship and Sequence of Formation of Glacial, Glacio-fluvial, and Glaciolacustrine Depositional Features by a Retreating and Downwasting Ice Front . . 59 Boulders and Cobbles in a Cultivated Field on the Kalamazoo Moraine, Alamo Township, Kalamazoo County ........................... 63 Ablation Till Overlying Stratified Outwash, Tekonsha Moraine, Charleston Township, Kalamazoo C o u n t y ........................... 63 Current Bedding in a Valley Train Deposit, American Aggregate Co. Pit, Cooper Township, Kalamazoo County. ................. Large Pocket of Locally Deposited Lake Clay, American Aggregate Co. Pit, Cooper Township, Kalamazoo County . . . 78 78 19. Bedrock Geology of Southwestern Michigan. . 90 20. Generalized Stratigraphic Sections of the Lower Marshall Sandstone and Coldwater Shale in Southwestern Michigan Showing Unique Identifiable Characteristics. . . 91 21. 22. 23. 24. 25. Bedrock Topography of Southwestern M i c h i g a n ..................................... 94 Bedrock Topographic Map of Kalamazoo County (after Ibrahim, 1970) 96 Generalized Drift Isopach Map of Kalamazoo County, Dashed Lines Show Cross Section T r a n s e c t s ................................. 101 Map Showing Surface Geology, Cross Section Transects, and Bedrock Valleys . . . . 104 South-North Cross Sections AA', B B ', and C C 1 in Kalamazoo C o u n t y .................... 105 xi Figure 26. 27. Page West-East Cross Sections D D *, EE', and F F ' in Kalamazoo County . Relationship Between Material Sizes and Lithologic Distribution....................... 28. Sample Locations in Southwestern Michigan 29. Igneous Rock Content in Southwestern M ichigan.................................... 30. 31. 1 . 135 137 Metamorphic Rock Content in Southwestern M ichigan........................................ Crystalline Rock Content in Southwestern M i c h ig an..................................... . Chert Content in Southwestern Michigan 33. Carbonate and Chert Content in Southwestern Michigan........................................ 34. Sandstone Content in Southwestern Michigan 35. Siltstone and Shale Content in Southwestern M i c h ig an..................................... 139 140 32. 36. 126 . . 143 144 146 148 Clay Ironstone Concretion Content in Southwestern Michigan ....................... 150 37. Clastic Rock Content in Southwestern Michigan. . 38. Gravel Resources of Southwestern Michigan . 156 39. Geologic Environment for Solid Waste Disposal in Kalamazoo County, Michigan. . 162 40. 41. Percent Distribution of Physically Strong Particles in Near Surface Drift of Kalamazoo County, M i c h i g a n .................... 167 Percent Distribution of Chemically N o n­ reactive Particles in Near Surface Drift of Kalamazoo County, M i c h i g a n ................ 167 xii LIST OF PLATES Plate I. II. Page Surface Geology of Southwestern Michigan . . 192 Soil Map of Kalamazoo County, Michigan. . . 193 xiii PART CHAPTER I INTRODUCTION This investigation was undertaken initially at the request of the Research Laboratory Section of the Michigan Department of State Highways, and subsequently has been developed as a dissertation for the doctoral degree. As such it forms an expanded phase of the statewide investi­ gation of the availability and quality of sand and gravel deposits of glacial origin, and provides an opportunity for a contribution to the glacial history of southwestern Michigan. On the practical side it is hoped that the study will have value in meeting the increasing demand of suit­ able natural aggregates for future highway programs in this state, as well as some fresh insights into the aca­ demic view of these practical matters. Aims and Purposes of the Study For the purpose of this investigation, it was decided to study one area, preferably as large as a county, to be geologically and geographically representative for the systematic evaluation of sand and gravel deposits in 1 2 Michigan. The first aim is, of course, use in planning by the State Highway Department. Kalamazoo County was selected for the study because of a shortage of known aggregates for highway construction in that region. To determine the origin and quality of material in the Kalamazoo area, a systematic geological study is essen­ tial. The glacial sediments in this region have been deposited by glacial and glaciofluvial processes of two separate glacial lobes of the Wisconsinan glaciation, i.e., the Lake Michigan lobe and the Saginaw lobe affect­ ing the area with repeated invasions of ice. This has produced what will be referred to as an interlobate "reentrant district," defined as an area in which mater­ ials from two different sources have become intermixed. Because, this situation makes field interpretations often quite difficult, the writer has mapped and sampled a large number of surficial deposits in the study area, and using field and laboratory interpretive techniques, attempts to clarify Pleistocene stratigraphy of these complex surface deposits. By applying time—stratigraphic, rock-stratigraphic, soil-stratigraphic, and morphostratigraphic analyses to the sequence, a glacial history of the area is evolved. Although some important questions remain unanswered, it is hoped that the new information here presented will be helpful in future exploration of such aggregates and in the interpretation of geologically 3 significant interlobate areas elsewhere in this state and in other regions where glacial, glacio-fluvialf and glacio-lacustrine processes have been dominant. The originally stated specific aims of this investigation, both for the Highway Department and for the dissertation were: 1. To prepare a detailed surface geologic map of the study area, and describe the geology and the glacial history of the area. 2. To point out sand and gravel deposits of the area with economic potential. 3. To determine the lithologic distribution of aggregates in the glacial drift by petrographic and other applicable methods. 4. To determine if the deposits of two different glacial lobes can be traced on the basis of their composition and engineering properties. Previous Work Previous work which bears on this subject, con­ sists of some small scale areal mapping and the descrip­ tion of surface features in this area. Taylor Leverett and (1915, the Pleistocene of Indiana and Michigan, U.S.G.S. monograph 53) and Leverett (1924, Map of the Surface Formations of the Southern Peninsula of Michigan) are broad reconnaissance studies of the glacial geology. 4 These do not show the details necessary to characterize effectively the glacial aggregate sources. Helen Martin (1955) compiled a map of the Surface Formations of the Southern Peninsula of Michigan, which also depicts the general distribution of the surface features. She also reported informally on the glacial history of Kalamazoo County (1957). Detailed glacial mapping on a one—county basis was done by Terwilliger (1954) in Van Buren County as part of a state groundwater resources survey. (1964) Kneller studied the gravel sources of Washtenaw County and prepared a gravel resources map. Ibrahim (197 0) made wide use of the gravity method to delineate buried bedrock valleys in Kalamazoo County, and prepared a bedrock topographic map of the county. Folsom (1971) did his doctoral thesis on the Hastings Quadrangle area in Barry County, Michigan, and worked on the interlobate problem between the Lake Michigan lobe and the Saginaw lobe; but the area of his concentration was too restricted to give much understanding of the situation pertaining to the whole reentrant district. Wingard (1969) carried out a study of glacial gravels in Michigan, also under the auspices of the Research Laboratory Section of the Michigan Department of State Highways. His work also concerned a broad region in a reconnaissance fashion to determine the engineering properties and lithologic compositions of 5 glacier-related aggregates, and their provenance and d i s ­ persal throughout the southern peninsula of Michigan. The present investigation was originated as a continuing and more detailed phase of the program intro­ duced by Wingard, therefore, some specific references will be made to his research. Though the present study is mainly concentrated on the interlobate problem, it concerns itself as well with aspects of the bedrock geology, bedrock topography, drift thickness, and soils of the area. These aspects are covered in Part II. In Part III lithologic distribution, economic considerations, and engineering usage of aggregates are considered. CHAPTER II PHYSICAL SETTING Location Area Kalamazoo County lies in the southwestern part of the southern peninsula of Michigan (Fig. 1). The area is nearly square in shape and has sixteen full civil town­ ships. The total area covered by this county is approxi­ mately 562 square miles. counties: it is surrounded by seven other Allegan, Barry, Calhoun, Branch, St. Joseph, Cass, and VanBuren. Selective supplementary studies, equally significant to this investigation in southwestern Michigan (Fig. 2) have also been conducted in these sur­ rounding seven counties and in Berrien and Eaton counties. Geologically, Kalamazoo County is located on the we&tenTfedge of an interlobate reentrant district between the Lake Michigan lobe and the Saginaw lobe of the Wisconsinan glacial age. The position of the reentrant is shown on Plate I . Cultural Geography Kalamazoo County was organized as a Civil Unit in July, 1829, the earliest settlers having come chiefly from 6 7 a T*CE 7. I CILHOUN 1 ■vA» ftuftCn s KALAM AZOO MICHIGAN COUNTY S T A T E H IG H W A Y C O M M I S S I O N DEMMTWEHT Of STATE HIGHWAYS H ’A HIGHWAY I^ « K M T M N t or wftin Figure 1. Primary study area. >*M> PLA NN IN G SURVEY T m w > W IW T * * iJN HWimyMTictl 8 ** mud I !nittMAvAiNAt c UIIIWUI ; ««C0«TA Q C I A N A 4|A|ILLA UONTCALU S R A T I O T C U N ION i N t H A M 'VAN IUNKN « A « N t t N AW] KAiAUAIOQl- e A L H O U M 'C A | l : •t jo » (N h : ] : » a a n c n PRIMARY STUDY AREA i trtlM N T W n il l NDACN SUPPLEM ENTARY STUDY AREA Figure 2* Location map noting Primary and Supplementary study areas. 9 New York State. 13,179, The population by 1850 had risen to and by 1860 it had about doubled. The 1970 cen­ sus reports a population of 201,550 for the entire county, and 85,550 for the city of Kalamazoo. The area is easily accessible by federal and state highways, county roads, and township roads. The main across— state highways serving the county are 1— 96, U S — 131, M-43, M — 89, and M-96. All county and township roads, which usually parallel the section lines, are well surfaced. The county is further served by the Grand Trunk, New York C e n ­ tral, and Pennsylvania railroads. The industry of the area involves manufacture of diversified products, among the most important being paper and allied products, pharmaceuticals, portation equipment, chemicals, trans­ and various types of machinery. Mineral industries in the county produce processed sand and gravel, marl, and some peat. The county also yields a variety of specialized and general farm products, exports being celery, the most important agricultural blueberries, cherries, and grapes. Geomorphological Character Relief The present geomorphic features of Kalamazoo County area were formed during the Cary stage of the Wisconsinan glacial age, and thus are largely in a y o ut h ­ ful stage of geomorphic development. The highest elevation 10 in Kalamazoo County is in Oshtemo Township, the elevation being 1,040 feet above sea level. The general relief of the county is 50 to 27 5 feet above the bed of the Kalamazoo River. Surface relief in the northwestern and west- central parts of the county, however, higher due to marginal features. is appreciably The rest of the area below about 900-foot elevation is generally flat, and consists of glacio-fluvial sediments, with a maximum re­ lief of 80 to 100 feet. Most of the flat area is breached by the Kalamazoo River and is dissected by several small tributaries. Some remnants of the outwash plain in the northeastern part of the county lie at elevations as much as 960 feet above sea level. The elevation is 800 feet where the Kalamazoo River enters the county, and 734 feet where it leaves the county. Drainage The Kalamazoo River, the principal drainage way of the county, flows in a westerly direction as far as the city of Kalamazoo, and then in a northerly direction, leaving the county in a northwesterly direction. In general, the northern half of the county is in the Kalamazoo River drainage basin, and most of the tribu­ taries flow into the Kalamazoo River. The rest of the county lies in the drainage system of the St. Joseph River, only a few tributaries of which reach the county. The northwestern corner of the county is drained by the 11 Paw Paw River basin. All the drainage from Kalamazoo County eventually reaches Lake Michigan. There are numerous lakes in the county, several of which are interconnected. Gull Lake is the largest of all, the next largest being Austin Lake. Chains of lakes abound in the upper reaches of the main streams. In general, most of these lakes were formed during deglaciation, and lie in the reentrant district between the two glacial lobes noted above. In general, drainage in the county is marked by irregular stream courses, swamps, ponds, and lakes, and it can be described as a "deranged pattern" in geomorphic terms (Thornbury, 1962). Climate Weather-wise, Kalamazoo County experiences short and warm summers and long winters which are not unusually severe. In winter the temperatures may fall to 15° to 20°F or more below zero, for a week or so, but not for prolonged periods. from 34°F to 100°F. around 50°F, in summer the temperatures may range The mean annual temperature is Lake Michigan greatly affects the weather in the county, as the prevailing westerly winds are warmed in winter and cooled in the summer while passing over the lake, thus giving the region a slightly "mari­ time" aspect. 12 The annual precipitation in this area averages about 3 5 inches a year, with precipitation being heaviest in spring and summer. The driest month is February, in which the average precipitation is only about 2 inches, Kalamazoo County lies on the eastern edge of the snow belt, which is induced by moisture and warmth picked up by the westerly winds crossing Lake Michigan. Conse­ quently, the average annual snowfall in the county is 10 to 15 inches greater than in the central and eastern parts of southern lower Michigan. In the last decade, the snowfall has averaged about 55 inches annually, though the secular climatic trend, at present involves a gradual winter cooling of several degrees since the 1940's. Nevertheless, the climatic conditions are essentially temperate. PART CHAPTER III FIELD INVESTIGATIONS Keeping the initial scope and objectives in mind, systematic and detailed field investigations were carried out. Objectives of the field investigations were divided into the following phases: (1) to prepare a detailed surface geologic map and work out the glacial history of Kalamazoo County, so that it can be used to locate and evaluate natural aggregates of glacial origin; and (2) to locate suitable exposures for sampling and collection of representative glacial drift for petrological analysis, so that evaluation can be made of its potential for use in construction projects in southwestern Michigan. Surface Mapping Originally the surface geology of Kalamazoo County was mapped by Frank Leverett and published by Leverett and Taylor (1915) in U.S. Geological Survey Monograph 53. Later, Leverett, who was largely responsible for the field work in this area, published (1924) a slightly revised map of the surface formations of the southern peninsula of Michigan. Helen M. Martin in 1955 published another large 13 14 scale map of the surface formations of the southern penin­ sula of Michigan, in which very few changes were made from Leverett1s maps. The above mentioned maps cover large areas and are very general in their applicability to a small area like a county. To answer the need for more detailed studies, the writer decided to remap Kalamazoo County from field obser­ vations, using additional available surface and sub­ surface information which has recently come to light. The surface mapping was carried out by obser­ vations along roads, with occasional foot traverses off the roads of course, often with the permission of property owners. The county has a very good network of section- line roads, and is covered by topographic quadrangles. The U.S. Geological Survey topographic quadrangle maps, the Michigan Department of State Highways county roads map (1 inch = 1 mile), and copies of L e v e r e t t 's original manuscript maps were essentially used as field guides. All possible exposures were visited and auger holes drilled at a number of places for evaluation of the parent material of glacial origin. Additional infor­ mation from highway borings has also proved useful. Study of aerial photographs has aided the mapping in the field as well as in the laboratory. The indi­ vidual photographs used are at a scale of approximately 1:20,000. The composite index photo map for the whole 15 county has also been useful, at a smaller scale, detailed study of regional glacial features, for a and to locate any gravel and borrow pits not listed in the Mic hi ga n Department of State Highways' Gravel Pit Inventory. soil map prepared by the Bureau of Soils (1922) A has also helped in the mapping of glacial features and the assess­ ment of parent material uncovered at given locations. Subsurface information regarding the nature of the material and its association with glacial features was obtained from waterlogs and oil and gas well logs a v a i l ­ able at the Michigan Geological Survey. Also, infor­ mation from various ground-water investigations was referred to, and at times conversations with well drillers and local people were carried out. After gathering the above information in 1968, a detailed map of the surface geology of Kalamazoo County was prepared (Fig. 6). Later on part of the studies were extended into neighboring counties, so it has become neces­ sary to compile from all available information a m a p of the surface geology of southwestern Michigan (Plate I). Field Sampling The sampling of glacial material was carried out simultaneously with the surface mapping. Over 90 large and small gravel pits were visited throughout Kalamazoo County to determine their suitability for sampling. of these, 18 pits were initially sampled, using the Out 16 channel sampling method. Samples were collected for the petrographic and mechanical analysis of the glacial material. Later on, it was found necessary to gather additional petrographic data in the county, with 23 more locations being sampled by the spot sampling method. 100 locations (including the above) Over were sampled for petrographic and mechanical analysis of sand, using channel, spot, and auger sampling methods. The locations to be sampled were based on the following characteristics: (1) freshness of exposure, though in several old gravel pits, fresh exposures were unavailable because of extensive slumping and the growth of vegetation, which made it difficult to obtain repre­ sentative samples in some cases; (2) type of deposit and the nature of its glacial origin; the material; (3) size and texture of (4) the associated glacial lobe and its former direction of ice flow; and (5) sampling density. Many gravel pits were not sampled because of lack of fresh and suitable exposures. It was desirable to take a commercial or e n g i ­ neering type of sample, as this study is concerned with evaluating the gravel deposits, as a whole, desirability as concrete aggregates. for their Suitable sampling methods and procedures for an engineering type of sample were decided from the outcome of earlier similar studies conducted in the Research Laboratory, Michigan Department of State Highways {Wingard, 1969). 17 Large Samples— Channel Sampling Method Channel sampling method was used for the first 18 samples obtained in Kalamazoo County, obtained by Wingard samples were large and samples 19-22 (see Table 3 in the A p p e n d i x ) . (weighing 600-1200 pounds) These and were used for laboratory petrographic and mechanical analyses. Channel samples were always taken normal to the bedding of the deposit. First, all materials that had slumped over the face of an exposure or a pit were shovelled away in order to prepare a more or less vertical face. about 20 feet of face Usually (excluding the overlying soil p r o ­ file) was cleared to obtain a wide range of the material to be analyzed. Precautions were taken to remove weathered and out-of-place material from the face. Then a channel about 9-12 inches wide and 5-6 inches deep was dug in the wall. The depth of the channel was more than the diameter of the largest pebble in the sampling zone. The entire vertical column was sampled by using a two liter laboratory scoop and a p i c k - m a t t o c k . was discarded. Any excess of caved-in material In order to obtain a representative and properly weighted sample, the material was sampled from each bed in proportion to its thickness. Occasionally sample transects were offset in order to obtain complete vertical sections. In each gravel pit anywhere from one to four channel samples were taken, depending on the amount of fresh exposure. 18 Small Samples--Spot Sampling Method An isolated sample taken at a particular point on the exposure is termed a spot sample. But, here the con­ cept of a spot sample is used in a slightly different way. These types of samples were taken from gravel pits, small borrow pits, and other small man-made exposures. The sample consisted of an integrated composite of a zone, or selected random samples taken in a small vertical channel in coarse sedimentary strata only. using a laboratory scoop, only coarse material was taken and the 1/2-inch to 1— inch pebble fraction was separated by hand sieving through square mesh screens. Approximately 10 pounds of material were bagged for further pebble volume analysis (see Chapter I X ) . This method of sampling and analysis has been successfully used in earlier work by the Research Labora­ tory Division, Michigan Department of State Highways, and has been proved by Wingard (1969) to be very economical and reasonably accurate for determining lithologic compo­ sition of drift materials. The writer, therefore, decided to use it, to compare his data with similar data acquired by previous investigations of the Research Laboratory, Michigan Department of State Highways in the vicinity of Kalamazoo County. Analysis of the first 18 samples suggested that additional lithologic data were needed to make more 19 precise glacial interpretations. Thus, an additional 23 locations were sampled by using the above described sampling method and related volume pebble analysis. Auger Sampling In Kalamazoo County, wherever surface and sub­ surface information was insufficient for interpreting the geology of the area, auger holes were drilled and samples collected. In all 13 holes were drilled throughout the county, the depths varying between 4 2 feet and 72 feet. A truck-mounted six-inch uncased power auger was used, provided by the Soils Division, District #7, Michigan Department of State Highways. Subsurface information was recorded at every five-foot vertical interval and, as noted above, samples were collected for further analyses. Occasionally a six-foot hand auger was used in the field for mapping purposes and for collecting small samples, especially for sand analysis. Samples from a large truck-mounted auger were also used for sand a n al y­ sis, but none of the auger samples could be used for petrographic analysis of coarse size (+3/16-inch) material, because of the inability of the auger to bring many large rocks to the surface. Sampling Problems A few problems are associated with these sampling methods. Caving or slumping was found to be the largest 20 problem encountered in the channel sampling method. Every so often during sample collections material would cave in or slumping would occur to upset the procedure. Almost always there was at least some slight disturbance in the middle of sampling. Thus the channel sampling method proved to be quite a time consuming process— more so than the spot sampling method, but it provided more information than the other technique. Also, when the water-table was higher than the lower limit of a dug channel, problems of caving-in were experienced. serious Just as caving- in introduces complexities into the sampling picture, induration further complicates the sampling. Generally induration in sand and gravel deposits is the result of carbonate or silica cementation. (hardpan) Such indurated material is very difficult to scoop out or break loose, and can offset the sampling continuity. CHAPTER IV GLACIAL HISTORY AND STRATIGRAPHY The Pleistocene Glacial Epoch in the geologic history of Kalamazoo County and vicinity is the most significant with respect to yields of commercial sand and gravel, and to important resources of ground water for the area. The rather comprehensive earlier studies of the Pleistocene geology of this area, were done by Leverett (Leverett and Taylor, 1915) and subsequently by several others including water resources investigations g e r , 1954; Travis, 1964). (Terwilli- Earlier workers suggested several probable invasions of continental Laurentide glacial ice in southwestern Michigan, but the problem of recognizing and dating the various invasions and ice fluctuations remains inconclusive in most sectors because of insufficient surface evidence. Also, glacial sediments of earlier ice advances and retreats have either been destroyed, covered, or modified by erosive and deposi­ tions! effects of younger ice. Thus the recognition of earlier ice age deposits in Kalamazoo County must be made primarily from well records, which, because of improper 21 22 and incomplete recording becomes a frustrating and diffi­ cult procedure. In fact, the nature and composition of subsurface materials is too often inadequately indicated in well records, and if noted at all, usually cannot be extended areally for any particular horizon owing to the absence of records from adjacent sites, or because of in­ consistencies on the part of drillers in their descriptions and use of terminology. Pre-Wisconsinan Glaciation It is a sufficiently established fact that all of the surficial sediments of Kalamazoo County are related to the Wisconsinan Glacial age except recent (Holocene) alluvial sediments along presently existing rivers and streams. On the basis of morainal sequences in Ohio and Indiana to the south, we know that pre-Wisconsinan ice once covered Kalamazoo County and presumably unloaded some of its material in the form of glacial and glaciofluvial deposits. The writer has observed what he be ­ lieves to be oxidized early Wisconsinan or pre-Wisconsinan drift in the neighboring Parma area of Jackson County, Michigan (see the Glossary). Also, others have reported presumed pre-Wisconsinan material at the base of the Wisconsinan drift in the Devils Lake sector south of the Irish Hills in Michigan (Miller, personal communications, 1971) and in the Grand Rapids area (Zumberge, 1964). Also, one's attention can be drawn to the Glacial Map of 23 the United States East of the Rocky Mountains (Geological Society of America,. 1959), on which a clearly delineated zone of Illinoian and earlier drift is shown extending across southern Illinois, southern Indiana, and southern Ohio, well covering the region adjacent to and south of the study area. It follows that Kalamazoo County lies on a direct path of pre-Wisconsinan Laurentide ice, the provenance of which was in the source area of the Lake Michigan and Saginaw (Huron) lobes to the north. Whether Nebraskan and Kansan glaciation actively affected Kalamazoo County is not indicated by any identifiable older drift, though a detailed study of well records also suggests that Illinoian glaciation probably left its mark in this area. It is fair to state that the uncertainty which surrounds the extent and nature of pre-Wisconsinan drift in Kalama­ zoo County stems simply from a lack of sufficient infor­ mation. What pre-Wisconsinan drift does occur is most likely of Illinoian age, this drift or correlated erosional topography of which seem to underlie much of the Wisconsinan drift in this sector of Michigan's southern peninsula. It should further be noted that Leverett and Taylor (1915) reported pre-Wisconsinan till farther east, especially in the southeastern and eastern parts of Michigan (U.S.G.S. Monograph 53). This till is generally 24 unoxidized darker blue-gray material, quite distinct from the newer drift. This older material is also described as more stony, and considerably indurated. Sometimes this older till is referred to as "hardpan" by well drillers and in places is overlain by dark colored Sangamonian soil profiles or deeply weathered zones marked by brown color­ ation from oxidation. In the Leverett and Taylor examples the supposedly Illinoian deposits appear to be largely sand and gravel or loose (non-compacted) textured material, in which case they cannot easily be separated from W i s ­ consinan deposits, except on the basis of rockstratigraphic and weathering differences. It is suspected by the writer that Illinoian deposits do, in fact, occur in Kalamazoo County as p r e­ glacial valley fillings and in thin patchy zones over buried bedrock surfaces. Some of this postulated Illinoian drift could have been reworded and redeposited by Wisconsinan glacial ice, in which cases the evidence of earlier glacial effects would be largely destroyed. The basis for this suggestion is that several deep well records in Kalamazoo County reveal the presence of hard stoney and bouldery clay, "hardpan,” blue-gray clay balls, and silt-clay just a few feet above bedrock. In several areas above layers of hard blue clay there are thin (10-15 feet) zones of brown silty clay and brown sandy and gravelly clay, a situation which somewhat fits the 25 Leverett and Taylor description of Illinoian till in southeastern Michigan. In addition to the above, Abdelwahid Ibrahim (1970) reports from Kalamazoo County finding references in driller's logs to buried soil profiles containing tree logs, brush stems, and muck and peat beds. He found references to a sufficient number of places to reinforce the belief that glacial sediments in Kalamazoo County were indeed, deposited during more than one glacial age. This writer has also found two d r il l er ’s logs reporting soil profiles at considerable depth near bedrock in Kalamazoo County. The presence of highly weathered boulders found in a number of gravel pits in the county may also relate to older presumably re-worked Illinoian drift fragments. Wisconsinan Glaciation It has been well documented in the glacial geological literature that the Wisconsinan ice spread completely over the state of Michigan and about twothirds of Indiana and large adjoining areas of Illinois and Ohio. As the present area of study is in south­ western Michigan, it is well within these borders, and hence the surficial drift deposits throughout this area are of the Wisconsinan age. The pattern of known ice- sheet limits indicates a considerably more lobated form at the time of its different stages than that of the 26 Illinoian and earlier ice-sheets. Present, landforms in Kalamazoo County and immediate vicinity were essentially the result of Wisconsinan ice pulsations, s t i l l - st an d s, and withdrawals, during downwasting being characterized by repeated small readvances producing myriads of oscil­ lation moraines and much varied relief. The ice was believed to be enormous in thickness compared to presentday temperate icefields around the globe, with the e x ­ ception of the continental to subcontinental polar ice sheets in Antarctica and Greenland which are considered at least morphologically comparable. For this reason, studies of such existing ice masses can improve one's understanding of conditions in Michigan during W i s ­ consinan time. Time-Stratigraphic Relations The stratigraphy of the Wisconsinan age has been rather descriptively treated by earlier workers because of its complex nature, and the lack of sufficient direct glacialogical experience in regions of existing glaciers. Leverett and Taylor cene geologists, (1915), who were well-trained Pleisto­ in their U.S. Geological Survey Monograph 53 worked out in broad outline the approximate time re­ lations of these ice lobes and morainic s y s t e m s , empha­ sizing the Wisconsinan glaciation in Indiana and southern Michigan, Because of the large number and intricately combined nature of these m o r a i n e s , Leverett and Taylor 27 considered them in groups, rather than correlating each individual moraine across the whole region. They right­ fully considered that this method simplified questionable correlations of individual moraines, and of course it served its purpose by providing a fine general framework. But they left many details untouched. Since about 1950, the stratigraphy of Wisconsinan age deposits has been reexamined in more detail. A criti­ cal study of newly available road cuts, gravel pits, building foundations, streambank exposures, and other types of outcrops has provided a new basis for major improvements in and alterations of the earlier concepts. Classification of the Wisconsinan age has been reviewed recently by Leighton and Willman (1960), and Wright cent studies by Wayne (1958, 1959, 1960), Frye (1964); also in some re­ (1963) and Gooding (1963). In 19 58 the Illinois State Geological Survey issued a report on its official classification policy Frye, (Willman, Swann, and 1958), and in 1961 the American Commission on Stratigraphic Nomenclature (A.C.S.N.) stratigraphic code for North America issued its proposed (A.C.S.N., 1961). From these two publications, the principles of classifi­ cation are reviewed and modified in detail into a recent report, "Pleistocene Stratigraphy of Illinois,” by Willman and Frye (1970). 28 In most of the papers, it is difficult to determine what type of classification is being used. form is based on time-stratigraphy. The most common The Illinois State Geological Survey recognizes several independent categories of stratigraphic classification, out of which the follow­ ing four are formally used in the report by Willman and Frye (1970): Time Rock Soil Morpho - stratigraphic stratigraphic stratigraphic stratigraphic For the purposes of the present paper, reference is made primarily to the most recent and commonly applied time-stratigxaphic classification. The evolutionary his­ tory of the Wisconsinan age is shown diagrammatically in Figure 3. According to the A.C.S.N. Code of 1961, "A time-stratigraphic unit is a subdivision of rocks con­ sidered solely as a record of a specific interval of geologic time." More detailed description of a time- stratigraphic classification need not be repeated as it is given in the A.C.S.N. Code (1961, p. 657). With re­ spect to the sequences in Figure 3, the Leighton chrono­ logy appears to be more applicable to the present study because it is in more detail than the chronology found to apply in Illinois alone. 29 R A D IO CARBON YRS B F> o - HOLOCENE RECENT f 1U « O w V ALD ER S G L A C IA L T W O C R E E K IN T - / r/ // / VALDERAN STAGE LATE 5 ,0 0 0 — MODIFIED A F T E R F R Y E AND W ILLM AN 1970 M O D IF IE D A F T E R L E IG H T O N I 9 6 0 TW OCREEKAN STAGE M ANKATO G L A C IA L in Y * C A R Y G L A C IA L S T C H A R L E S IN T b o w m a n v il l e GARDENA 2 0 ,0 0 0 UJ IO W A N IN T G L A C IA L o < 2 5 ,0 0 0 - < z W O O D F O R D IA N ST A G E G L A C IA L UJ _i Q a FARM C R E E K I N T R A G L A C IA L 5 z o 3 0 ,0 0 0 - u to 3 5 .0 0 0 4 5 .0 0 0 - FARM D A L E G L A C IA L 5 5 .0 0 0 - EARLY $ AGE TAZEW ELL WISCONSINAN 1 5 ,0 0 0 - F A R M D A L IA N STAGE A L T O N IA N STAGE 6 5 .0 0 0 7ft AAA SANGAMON AGE S A N G A M O N IAN AGE F ig u r e 3 . M o d ifie d S t r a tig r a p h ic C la s s ific a tio n o f the W is c o n s in a n d e p o s its in Illin o is . 30 Dist.ribut.ion of Drift The entire Kalamazoo County and vicinity was covered by two lobes of the Wisconsinan age continental glacier, the Lake Michigan lobe which advanced from the northwest, and the Saginaw lobe from the northeast. These two lobes, along with the Erie lobe to the east, extended southward into northern Illinois, northern Indiana, and northern Ohio. The maximum advance of these three lobes is considered to be the Minooka moraine of the Lake Michigan lobe, the Iroquois-Packerton Moraines of the Saginaw lobe, and the Union City moraine of the Erie lobe (Fig. 4). Zumberge (1960) considers that these moraines mark the Cary drift border in Illinois, Indiana, and Ohio. Retreat of the ice margin of all these lobes formed the present surface features in northeastern Illinois, northern Indiana, northern Ohio, and southern lower Michigan. Therefore, the present surface geology of Kalamazoo County and vicinity came into existence because of the major withdrawal of ice in middle Wis­ consinan time (Fig. 3), with minor readvances of the Lake Michigan lobe and the Saginaw lobe of the Cary stage of the Wisconsinan age. It is probable that the thickness of glacier ice in these two lobes, within a few miles of its border, was more than one mile, which effected the huge bold morainic patterns found. Advances and retreats of both the Lake Michigan and the Saginaw lobes were presumably controlled by glacio-climatic liTOa l_ _ K £ M /C H IG A N sr jomm Figure 4. Map of Wisconsinan age moraines, Northeastern Illinois, Northern Indiana, Southern Michigan, and Northwestern Ohio (after J. H. Zumberge, 1960). 32 changes in the net accumulation in nourishment zones (Nev€ ar ea s ) « or inner areas f i.e., the interior icesheet. Lake Michigan L o b e .— In terms of the Wisconsinan glacial history, the Lake Michigan lobe continued to fluctuate in marginal position and volume during all of the time between the deposition of the Minooka moraine in northeastern Illinois and the readvances of Valders ice in the late Wisconsinan time. The Lake Michigan lobe fed by ice flow from one or more ice centers located around and probably somewhat southwest of the Hudson's Bay area. This lobe (along with the Green Bay lobe) flowed south­ ward into the Lake Michigan lowland along preglacial river valleys, with glacial erosion taking place on rocks of Middle and Lower Paleozoic age. The major ice limits of all weak stages and main Wisconsinan moraines were first worked out by Leverett (1902), using topographic and morphologic methods. ing to Leverett and Taylor Accord­ (1915), after the development of the Bloomington morainic system there seems to have been rapid recession along the junction (Fig. 5) of the Lake Michigan and Huron-Erie lobes across the Kankakee basin and on northeastward into southern Michigan as far as the Kalamazoo area. Late retreatal history of the Lake Michigan lobe is intimately related to the history of Lake Chicago and associated low-water stages 1951, 1955; Hough, 1955, 1958; (Bretz, Zumberge and Potzer, 1956). *w 33 F ig u r e 5 . D e s ig n a te d m o r a in ic s y s te m s o f M ic h ig a n and N o r th e rn In d ia n a (a fte r L e v e r e tt and T a y lo r , 1915)* 34 Horberg and Anderson (1956) believe that the Lake Michigan and Green Bay lobes were deflected southwestward by ice streams from the east which deposited huge piles of drift east of the interlobate area at the time of the Tazewell stage. They support this interpretation on the basis of drift lithologies patterns (rock-stratigraphy) and moraine (morpho-stratigraphy), which in effect involves a litho-morphostratigraphic interpretation. This concept of a westward shifting of the axis of the Lake Michigan lobe was described by Leverett vey Monograph 53. (1915) in U.S. Geological Sur­ The eastern side of the Lake Michigan lobe had thus less freedom for deployment than the western edge, w i th the ice tending to hold its position on the east while advancing on the west. The present glacial features of the Lake Michigan lobe and the Saginaw lobe in Kalamazoo County were formed during this eastern orientation of the axis, followed by the downwasting and retreatal phases of the Cary stage (Fig. 5). Saginaw L o b e .— At the time of the Cary stage, the Saginaw lobe of Laurentide ice moved southwestward through and beyond the Lake Huron— Saginaw Bay area into Michigan and northwestern Indiana. Iroquois-Packerton moraines in northern Indiana represent the maximum advance of the Saginaw lobe at the time of Cary glaciation. Anderson Horberg and (1956) placed the boundary of the outer Cary at the Iroquois moraine. This is 1 ithologically distinct 35 from the Lake Michigan lobe Cary moraines, but it is similar to the Tazewell moraines found farther southwest. Leverett studied moraines and deposits of all three lobes (Leverett and Taylor, 1915, p. 123) and concluded the following: A study of the moraines of northern Indiana and southern Michigan has shown that the portion of the ice sheet which moved southwestward from the Saginaw basin into Indiana melted back and disappeared from northern Indiana while the Lake Michigan and HuronErie lobes still extended into that state. This perhaps is not surprising, for the path of the Sagi­ naw lobe, especially the part beyond the immediate basin of Saginaw Bay, was across more elevated country than the path of the bordering lobes. Its thickness must have been correspondingly less and its movement correspondingly weaker, and these differences would become more noticeable with the waning of glaciation and decrease in the bulk of the ice sheet. It is of interest that this description connotes strong out-of—phase fluctuations of major proportion in these two main lobes. Further evidence of this and its consequences will be considered later with respect to specific features in this study. On the same page Leverett also explains the strong moraines in southern Michigan formed by the Saginaw lobe, in spite of its degenerative regime compared with the Michigan lobe at that time. He suggested that simul­ taneous convergence of the three lobes might have caused an excessive loading with drift material in the part of the ice sheet which subsequently became differentiated into the Saginaw lobe. Further, Leverett thinks that 36 this excessive loading may have been even more influential than the comparative thinness of the ice in bringing about the reduction in flow. With the further recession of the Saginaw lobe into southern Michigan, reentrant angles developed between it and the Lake Michigan lobe in southwestern Michigan, and between it and the Huron-Erie lobe in southeastern Michigan. This was the simplest possible explanation given by Leverett <1915). He suggested that the actual history may have been much more complicated. The border of these lobes, for instance, may have readvanced instead of merely halting at the moraines formed during recession. Due to a lack of more detailed evidence, however, Leverett did not go into a complicated interpretation. From the last quarter of a century's studies of existing glaciers around the globe, it is a well-documented fact that major ice retreats from vigorous advance positions are usually associated with minor readvances and vice-versa. These pulsations are related to many factors in the general systems nature of ice sheets as quite sensitive responders to climatic perturbations. The Lake Michigan-Saginaw Interlobate A r e a .— An interlobate area is defined as an area between bold end moraine systems from different glacial lobes and also along the line of junction of two adjacent glacier lobes. In this definition southwestern Michigan is a classic 37 interlobate area frequently referred to as a reentrant district (Leverett1s term). The reentrant angle is the angle at the junction of two end morainic systems formed by two quite separate glacier lobes. Most of Kalamazoo County and vicinity lies within such a reentrant district, situated between the bold Kalamazoo morainic system of the Lake Michigan lobe to the northwest and the bold moraines of the Saginaw lobe to the northeast (Fig. 6 and Plate I ) . During the for­ mation of the Kalamazoo morainic system, the interlobate junction was in Barry County, a few miles southwest of Hastings and immediately north of Kalamazoo County (Plate I). From this location, the interlobate tract runs northward in a zigzag course toward southern W e x­ ford and Missaukee counties, which lie in the upper middle center of the western "hand" of Michigan (Fig. 5). In this interlobate tract are the most prominent moraines developed anywhere in the southern peninsula. From the axis of this interlobate tract, there is a general west­ ward topographic descent toward the Lake Michigan basin, and a general eastward descent toward the Saginaw basin. At the interlobate junction southwest of Hastings in Barry County, the Kalamazoo morainic system is,charac­ terized by larger lakes than are commonly found else­ where along the interlobate tract. Also the tract includes several small gravel plains developed as an outwash from 38 - ;V’« -r'J-ifi . - i t ■•, F ig u re 6 . S u rfa c e geology o f K alam azo o 38 L EGEND cm TILL R jLlN OUT m a n plain □ T « W * r T e M A L BOUNMUT, THIN TILL «JW O l/T W W t OTTAILT N M M D 9V MAMA* P S U R F A C E GE O L O G Y OF K A L A M A Z O O C;O U N T Y M I C H I G A N KE4.I, iivil eology of Kalam azoo County, M ichigan. 39 one or both of the ice lobes. (1915), According to Leverett these outwash plains are in places characterized by small in-filled basins of sediments at the border b e ­ tween the gravel plains and the associated moraines. He thought that the slopes of the outwash plains and the distribution of these basins indicated the source of the outwash, which in some places appeared to be the product either of one or both lobes. Leverett (1915) further pointed out the relation and trends of the moraines of both lobes in the reentrant angle. Moraines of the Lake Michigan lobe lead up to the line of junction from southwest or south, and those of the Saginaw lobe lead up to the junction line from the southeast. At this junction much outwash is found. Leverett (1915, p. 186) thought that both lobes for a while retreated from south to north along the line of junction up to the southwestern part of Mecosta County. He thought that probably both lobes thinned and shrunk away toward the Lake Michigan lowland to the west and the Sag in a w lowland to the east, leaving a massive moraine system extending northward from southwestern Mecosta Coun ty to Cadillac. This interpretation may be correct, but it is quite different from L e v e r e t t 1s interpretation regarding the earlier disappearance of the Saginaw ice from northern Indiana while the Lake Michigan and HuronErie lobes still extended into that state. The present 40 writer suggests that Leverett's second interpretation is probably more realistic in the interlobate area between the Lake Michigan lobe and the Saginaw lobe. Broad scale correlative studies of all three, the Lake Michigan, Saginaw, and Huron-Erie lobes, have been carried out by investigators such as Leverett and Taylor (1915), Wayne and Thornbury and Anderson (1956), Anderson Wayne and Zumberge and Michigan. (1951, 1955), Horberg (1957), Zumberge (1960), (196 5) and several others in Indiana Most of the studies, however, are focused on the regional relationship between terminal moraines of all three lobes in northern Illinois, northern Indiana, and northern Ohio. Very few detailed correlative studies have been done along the border between Michigan and Indiana, and particularly the present area of study. Leverett (1915) has described individual glacial features and deposits in the Kalamazoo area, but he posed problems for interpretation of the history of deposition of the complex intermingling of various kinds of tills, outwash sediments, and lake deposits, both here and in the northern part of Indiana, These problems have not yet been adequately solved. This writer's interpretations are based on field examinations, laboratory analysis of surficial gravels and sands, and study of other literature some relating to the area of Kalamazoo County and vicinity. The 41 interpretations given in the following pages may, of course, be subject to change in the future when additional data may become available from future road cuts and exca­ vations. The present chapter presents a brief glacial history of the reentrant district, with detailed descrip­ tion of individual glacial features in Kalamazoo County covered in the succeeding chapter. Anderson (1957) determined pebble and sand lith- ologies of the major Wisconsinan glacial lobes of the central lowland in this country, and he interpreted distri­ bution of lithologic types in terms of provenance, ologic properties, and glacial processes. lith- It appeared difficult for him to differentiate glacial lobes on the basis of a single "indicator" lithology. Only the Saginaw lobe contained the always identifiable Precambrian (Huronian Gowganda) tillite and the well-recognized jasper conglomerate from the Lorraine formation (also of Huronian age) which are not found in the Lake Michigan and other lobes. The present writer considers that these two indicator rocks (index erratics) are ideal for differ­ entiating deposits of the two different lobes in this study area, on the basis that the Saginaw lobe only con­ tains these indicator rocks with a provenance in Ontario. Anderson's investigation suggests that the relative proportion of lithologic types is the most fruitful method for the differentiation of glacial lobes. Lithologic 42 composition of a particular drift must be dependent upon the sources of the ice and the composition of the bedrock floor over which it passed. Comparison of the lithologies of the drift deposited by ice lobes moving over different bedrock lithologies should, therefore, show differences intimately related to the former directions of flow. A detailed petrographic analysis of gravels from several locations in Kalamazoo County was carried out by the writer, and the data (see Tables 3 and 5 in the Appen­ dix) are correlated with similar types of data from sur­ rounding counties. It is clear that pebble—sized fractions show significant differences between the Lake Michigan lobe deposits and the Saginaw lobe deposits. More d e ­ tailed interpretation of various proportions of lithologies associated with each lobe is given in Chapter X, under the heading "Lithologic Distribution of Aggregates." Anderson*s (1957) As in investigation, this writer finds that the correlation of the relative proportions of certain types of groups of lithologies— i.e., rock-stratigraphy— provides the most useful method for differentiating deposits of these two lobes. Considering all available information, it is suggested what Leverett had apparently unwillingly hinted, that, the terminal behavior of the Lake Michigan lobe and the Saginaw lobe in middle Wisconsinan time were quite out—of-phase with each other. A sequence of regional 43 trends within the glacial borders of both lobes in the Kalamazoo reentrant district are illustrated in Figures 7-13. Arrows in these figures only indicate shift in position of ice margins due to downwasting and not the direction of actual ice flows. First, the Saginaw lobe ice (Fig. 7) was extended through most of Kalamazoo County, all the way, passing southward across the Michigan-Indiana border. At this time the Lake Michigan lobe ice margin was farther west and northwest (Figs, 3 and 4, and Plate I) and well con­ tained in the Lake Michigan basin. When the ice margin of the Saginaw lobe started retreating with associated small ice advances, its terminus shifted towards the Saginaw basin leaving in its way a series of relatively bold maraines, till plains, outwash plains (valley trains in narrow linear areas), and recessional moraines; the Lake Michigan lobe in contrast appears to have started advancing again towards the southeast and east in the area of southwestern Michigan. Presumably this represented a difference in the dominant storm track pattern affecting the different source areas, or n£v£s, of these ice systems, as has been well demonstrated in comprehensive studies of smaller icefield systems of present glaciation in the middle latitudes (Miller, 1963, 1972). The retreating Saginaw lobe the Sturgis moraine (Fig. 8) resulted in (Figs. 4 and 5; Plate I) in St. Joseph County, part of the Alamo moraine in the northern part of MICHIGAN SA3INAW LOB STAGNATION AND READ1fANCE RECESSION STAGNATION L A M U N t W Note. Arrows only indicate shift in position of ice margins due to regime changes and not the direction of actual ice flows. Figure 7. F irst regim e trend in the Lake Michigan-Saginaw interlobate glaciation. 1 ! f A L G E L 0/ O)/' N A 1 . R A R Y b E A T 0 N \) \/ m i ::h i g a iM L O B E ICE LAK e ; *'B i/' ? ^* s A / S \ GINAi V L O E »E ICI > 1 1---- f > J k W v v \/" V A N B U * T A G N jTION ANI AOVAf C E R V V ' K A L A M E y Vy A 2 C 0 s /'* c !*■ y /C/ r ( ■p 1U . - 0 N U r p c s K ‘N AND ^ S T AGNAT O N 0 >0 ) ’ "N\ y ? \ H i tf/ — \ i --- y - , , a z r C A s s \M --- Figure 8. *' ^ ^ ( / 0 S E P S Tv <* _ s - < /■*> * B H R A N C H ■;> 1— Second regim e trend in the Lake Michigan-Saginaw interlobate glaciation. ( : m ic HIGAfv SA SINAW LOB STAGNATION A U N STAGNATION AND LIGHT Ai 'VANCE Figure 9. Third regim e trend in the Lake Michigan-Saginaw interlobate glaciation. N 4ki MICHIGAN A SAGINAW LO X N U r e A dvak SHORT PERIOD flEADV OVER .AMAZOO ORAINE i TEKOIMSHA MORAINE TCTTIV' Figure 10. Fourth regim e trend in the Lake Michigan-Saginaw interlobate glaciation. N : MICHIGAN SAGINAW f c LOBE ICO FAST CESSION < z . L A M H 0 RECESSION i Figure I I. Fifth regim e trend in the Lake Michigan-Saginaw interlobate glaciation. U N LAKI: MIC HIGAIS SAGINAW LOBE S 3 IB y A -OW iS S IO RCCESSI AND AGNAi A N /U N co 1 Figure 12. Sixth regim e trend in the Lake Michigan-Saginaw interlobate glaciation. iic h k 1 LOB e L ‘ ;A N 1 ; ic i: G IN A \| ! v; I . S -s . A / V A N L L E G N A B A If W' A 'cc 'M m RVR ' 1^1 )-< : Ut \ \f sue RECES SION ANl ! TAGW TION 1 B U R fj. l V y k LOE e T 0 N ECESS ON k J fF AND ATION E A % • a LAM ic e : c x\ v 1 E 1 t *1 c A Z 0 0 A L H 0 . u "* —1 ^ N i \ --- , V $ i _ : --------- ---------- — — — ----- ------ . K> K ' -------- C ^ 1 V A\ >s s S T J 0 S E P H B R A N C Figure 13. Seventh regim e trend in the Lake Michigan-Saginaw interlobate glaciation. H 51 Alamo Township of Kalamazoo County; and possibly the Kendall moraine {Fig. 5) in northeastern Van Buren County, which is believed (Leverett and Taylor, 1915) to be a possible westward extension of the Alamo moraine. This may also be the earlier phase of the Kalamazoo moraine in Van Buren, Kalamazoo, and Barry counties, which is considered to be the outermost bold moraine of the Lake Michigan lobe in this area. Field evidence indicates that at this time the previously stagnant and retreating Lake Michigan ice border advanced again into the western part of Kalamazoo County and overrode previously deposited Kendall and Alamo moraines of the earlier Saginaw lobe. The ice then stagnated near the present main axis of the northeasterly and southwesterly striking Kalamazoo moraine. Greater relief and boldness of this moraine indicates a vigorous ice push, followed by a rapid retreat from this moraine, and then continuing stagnation, as a still-stand phase, characterized by minor fluctuations, as shown by the existence of many lesser moraines. Overriding of the Lake Michigan lobate front over the Alamo and Kendall moraines is suggested on the basis of two lines of evidences: analysis Firstly, the petrographic (Figs. 28-37) of samples taken from the Alamo and Kendall moraines area have lithologic composition quite similar to the rest of the known Saginaw lobe samples. Leverett (1915, p. 183) described the Kendall 52 moraine, at least its northern half of which is very hummoky and bouldery, and he suggested the possible correlation between this m o r a i n e and the Alamo moraine in Kalamazoo County. Leverett also pointed out that in the northern half of the Kendall moraine there were many huge boulders, some up to 8 or 10 feet in diameter. Amongst these boulders he reported conglomerates of various kinds, including the red jasper conglomerate from Ontario which has been previously regarded as an indicater rock of the Sag i na w lobe. He also reported a few pieces of gypsum, and numerous limestone fragments from M ississippian formations to the north. Such e v i ­ dence shows strong correlation of these two morainic ridges with the Saginaw lobe moraine system. Secondly, the strike of the Alamo m o r a i n e and northern half of the Kendall moraine, Buren County north of the village of Kendall in Van (Plate I ) , is east-west. This strike is parallel to m o s t of the m o r a i n e s of the Saginaw lobe. Suggesting further that these two moraines were formed by ice earlier from the Saginaw lobe. F r o m the glaciological studies of Miller 1970) (1964, and others of the existing glaciers of today in Alaska and elsewhere in the world, we know that glaciers retreat and advance and thin and thicken due to climatological changes, and changes in other physical p a r a m ­ eters controlling individual glaciers. Recent studies 53 of Taku glacier and adjoining Norris Glacier 1950; Eagan, 1971) (Lawrence, of the Juneau icefield in Alaska show that Taku Glacier since the 1890's has been advancing abnormally fast, while the Norris Glacier since the 1910's has been slowly downwasting and retreating. The former advancing phase of the Norris Glacier ice once overrode but did not destroy earlier terminal moraines formed by the Taku Galcier in its previous advance and retreat 200 years ago (Miller, Egan, and Yates, 1964). This modern small scale example can be applied to large scale continental glacier lobes, where the terminal ice was probably of comparable thickness, at least suffici­ ently thin in its terminal zone to override moraines like the Alamo and Kendall without disturbing them. After formation of the Sturgis moraine, lobe the Saginaw (Fig. 9) continued to retreat more rapidly, forming a series of till plains (Plate I) and outwash plains up to the Tekonsha moraines (Figs. 4, 5, and 6), where it then experienced a stillstand and allowed establishment of the Tekonsha moraine as a strong recessional feature. The Lake Michigan lobe was more or less at a standstill too, with smaller advances which built the western end of the Sturgis moraine (Plate I) in Cass County and the outer part of the Kalamazoo moraine north of Kalamazoo River in Kalamazoo and Barry counties. This part of the Kalamazoo moraine in the Hastings quadrangle in Barry 54 County is described by Folsom (197 0) as an interlobate moraine. The Saginaw lobe (Fig. 10) readvanced slightly for a short time as far as the outer limit of the drumlin field (Plate I) lying southeast of Kalamazoo County. This readvance is indicated by drumlins and thin ablation till (Fig. 16) on the top of the northwest-southeast trending Tekonsha moraine. At the same time the Lake Michigan ice readvanced over the Kalamazoo moraine up to the Saginaw ice border in the southeastern part of Kalamazoo County, a situation shown in Figure 10. This readvance of the Lake Michigan lobe appears to have pushed the surface material east of the Kalamazoo moraine, previously d e ­ posited by Saginaw ice. Pushed material was thus re­ deposited in the form of weak morainic ridges marking the outermost advance of the Lake Michigan lobe in Kalamazoo County. North-south trending ridges (Plate I ) , which are also allied to the Tekonsha moraine system of the Lake Michigan lobe in eastern Kalamazoo County, are correlated by Leverett naw lobe. (1915) with the Takonsha moraine of the Sagi­ There are a couple of other weak ridges, one in Comstock Township (Fig. 6) and another just northeast of the city of Kalamazoo. These two ridges were probably also formed as push moraines at the same time. The writer suggests that material was pushed eastward by this re­ advance. The evidence here is that the lithologic 55 composition of samples taken to the east (Figs. 28-37) of the Kalamazoo moraine of the Lake Michigan lobe shows strong correlation wi t h the samples of the Saginaw lobe towards the n o r t h e a s t . Yet the geomorphic character of glacial features shows stronger ties with those of the Lake Michigan lobe. In this sector, readvance of the Lake Michigan ice is also marked by sandy ablation till on the top of the Kalamazoo moraine. On the basis of the above interpretation, interlobate boundary line an (Plate I) is drawn through these weak ridges formed by the max im u m advance of the Lake M ichigan ice in Kalamazoo County. This interlobate line passes farther north through the interlobate m o r a in e described by Folsom Similarly, (197 0), in southwestern B arry County. the interlobate line to the south of Kalamazoo County is considered to pass through weak m o raines per­ pendicular to the Sturgis mora in e of the Saginaw lobe in the western part of St. Joseph County. It is suspected that this line may pass through farther northwest part of St. Joseph County. A sample taken from the Sturgis moraine in St. Joseph County falls into the S a g i na w lobe lithology class, and the sample taken from the Sturgis moraine in Cass County falls into the Lake M i c h i g a n lobe lithology class (Figs. 28-37). Figure 11 indicates how the Saginaw lobe ice retreated rapidly, shifting its front back to the line of the Tekonsha moraine and forming drumlins on the top of 56 till plains. In contrast, the Lake Michigan lobe retreated slowly to the Kalamazoo moraine position, and produced a few north-south trending weak ridges in consequence of its minor marginal fluctuations. mapped These weak ridges are (Pig. 6) as thin linear moraines in the southeast Prairie Ronde, northeast Portage, and northwest Cooper townships of Kalamazoo County. After forming these small ridges, the Lake Michigan lobe ice retreated (Fig. 12) rather rapidly to the present Kalamazoo moraine position. Such an accelerated recession is explained by the presence of a thin till capping (Fig. 6) outwash deposits in Cooper and Prairie Ronde townships of Kalamazoo County. In contrast, at this time the Saginaw lobe experienced a slow retreat, forming series of parallel and quite subdued moraines northeast of the outermost main Tekonsha ridge. Some of these ridges of the Tekonsha morainic system show a plexal relationship, indicating again that small readvances characterized the retreat of Saginaw ice. Figure 13 shows the last significant event or trend in the glaciological regime when ice from both lobes retreated to their respective positions of the present Kalamazoo morainic system. Here a major still- stand occurred for a long period but again with minor fluctuations resulting in the strikingly irregular scenes of superimposed small ridges on the massive structure of 57 the main bold moraines in southern lower Michigan. The behavior of both lobes during the main retreatal phase that followed, i.e., through the rest of Wisconsinan time— have been generally described in the Leverett and Taylor monograph (1915). The integration of all factors supporting this interpretation is given in the Conclusions, Part III, pages 170-71. CHAPTER V CHARACTER OF SURFACE GEOLOGY The surface geology of Kalamazoo County is made up of unconsolidated materials, origin. predominantly of glacial The near-surface materials have been deposited directly by the Wisconsinan ice, or indirectly by meltwaters from the retreating glaciers, along with a very few aeolian deposits of post-Cary age. classified, Surface features are in four major categories: g l ac i o- fl uv ia l, (3) aeolian, and (1) glacial, (4) others. (2) The c h a r a c ­ ter of each m ajor feature and associated elastics is described, with the idealized interrelationship and sequence of formation of these features illustrated diagrammatically in Figure 14. Glacial Features Glacial features in Kalamazoo County include terminal or end moraines, lateral moraines, ground moraines or till plains, and drumlins. These features are mostly comprised of tills containing local lenses of stratified sand and gravel. 58 RETREATING ICE o fr DOWNWASTING ICE GLACIAL OUTWASH PLAIN FINE COARSE SANDY g ravelly OUTWASH OUTWASH BOLD 't e r m i n a l ' MORAINE DRIFT SHEET GROUND MORAINE RECESSIONAL OR GROUND S T IL L MORAINE STAND MORAINE OUTWASH PLAIN OR VALLEY TRAIN COARSE GRAVELLY OUTWASH .i f I . LOCAL OUTWASH GLACIAL LAKE SEDIMENTS KETTLE POND A S&TILUr -B E D R O C K Figure 14. Hypothetical cross section showing interrelationship and sequence of formation of glacial, glacio-fluvial, and glacio-lacustrine depositional features by a retreating and downwasting ice front. 60 Terminal and Lateral Moraines Moraines of Kalamazoo County are associated with the activities of the Lake Michigan lobe and Saginaw lobe of the Wisconsinan ice sheets. Evidences for assigning the following moraines to a particular lobe are also considered in the previous chapter and Chapter X. The Kalamazoo Morainic System.— This moraine system of the Lake Michigan lobe occupies the northwestern part of Kalamazoo County (Figs. 5 and 6). It includes mostly all of Oshtemo Township and parts of A l a m o , C o op er , Texas, and Prairie Ronde townships. Leverett (1915, p. 174) described this system in southern Michigan as having two well-defined ridges and inner ridges) gravel plain. (outer separated by a narrow nearly continuous In Kalamazoo County, however, this system does not have this configuration. More often it appears with the outer and inner ridges merging to form one large, bold moraine (Fig. 6). Disconnected shallow patches of local outwash commonly occur along the moraine axis. The highest elevation of the Kalamazoo moraine in this county is 1,040 feet in sections 9 and 10 of Oshtemo Township. The moraine's average elevation is around 950 feet, and the average width, outwash, 4 to 5 miles. including the patches of The maximum width along an east- west direction is about 7 miles, and is found in Alamo and Cooper townships. 61 The outer m a r g i n of the moraine shows slight relief above the onlapping outwash plai n to the east which in some places extends outward from the moraine. Patchy outwash between the outer and inner margins of this moraine is found close to the average elevation of the moraine itself. The inner or western marg in drops steeply to a n a r ro w outwash plain or valley train associated with a glacial drainage c h a n n e l . T he Kalamazoo mor ai ne exhibits strong knob and kettle topography. Several knobs are developed 50 to 7 5 feet above the neighboring kettle holes, 50 feet ab ove the bordering outwash apron but only 25 to (Fig, 6). Below this a number of kettle-like basins have depths of 2 5 feet or more. F e w of the kettles are occupied by water, but where small lakes occur they are called kettle ponds (Fig. 14). Many kettle ponds have become d r y and show d e p o si ts of stratified material near the bottom. High Ridge in the northeast cor ne r of Cooper T o w n ­ ship and the northwest corner of Richland Township, is a north-eastward continuation of the Kalamazoo moraine beyond the Kalamazoo River valley. It is this sector which reaches in altitude of 1,040 feet above sea level, in Section 1 of Cooper and Section 6 of Richland t o w n ­ ships. T h e bold topography and high relief resembles that of the interlobate moraine in southern Barry County (Folsom, 1971) which is, in fact, the northeastward continuation of this ridge in Kalamazoo County. 62 The Kalamazoo moraine is composed of assorted material of various grades of coarseness. Most of the drift is sandy and gravelly and in general thick beds of sand and gravel are found interbedded with clay till (Figs. 25 and 26) right down to bedrock. are also reported in some wells. Layers of silt The layers of sand and gravel are considered to be the result of deposition by large amount of meltwater associated with the final dis­ appearance of large stagnant ice masses. More or less throughout the moraine, near-surface material is either loose-textured stony clay or sandy drift with entrained cobbles and boulders. boulders, (Leverett, 1915), Such cobbles and along with sandy or clayey material, are often seen in cultivated fields (Fig. 15). In general, near­ surface sand seems to predominate over loose-textured clay. The inhomogeneous character of the unstratified sand and the loose texture of the clay, containing some gravel and cobbles, indicate that ablation till covers large surface areas in the Kalamazoo moraine. Below this sandy ablation till, thicknesses of which vary from place to place, brown discontinuous clay layers of varying thickness also are present depth, (Figs. 25 and 26). At greater in well logs, clay layers are described to be blue or gray in color, with some exceptions of brown or yellow clay. The Kalamazoo moraine in the sector north of the Kalamazoo River, in the northeast corner of Cooper Figure 15. Boulders and cobbles in a cultivated field on the Kalamazoo moraine, Alamo Township, Kalamazoo County. Figure 16. Ablation till overlying stratified outwash, Tekonsha moraine, Charleston Township, Kalamazoo County. 64 T o w n s h i p , also has m u c h sandy till at the surface with many large boulders similar to those found in both the Lake Michigan and Saginaw lobes. This relationship helps the interpretation of an interlobate moraine (Plate I). The Tekonsha M o r a i n e .— In Kalamazoo County this moraine was also formed by the interplay of glacial activities in the Lake Michigan and Saginaw lobes 5 and 6, Plate I ) . (Figs. The Tekonsha m o r ai ne of the Saginaw lobe, however, is stronger than that of the Lake Michigan lobe, and comes into Kalamazoo C o u n t y from Quincy, M ichigan in a northwesterly direction, Calhoun County. passing through The Tekonsha moraine of the Saginaw lobe also forms a reentrant angle with the Tekonsha of the Lake Michigan lobe, just west of the Kalamazoo-Calhoun County line and south of the Kalamazoo River valley in Charleston Township (Fig. 6). This part of the moraine trends northward from the reentrant area which forms a couple of isolated spurs in Ross T ownship north of the Kalamazoo valley. The reentrant area between the Tekonsha moraine segments of both lobes extends s o u t h ­ ward (Plate I) beyond the boundaries of Kalamazoo County and into neighboring c o u n t i e s . The Tekonsha moraine, like the Kalamazoo, has a general width of 4 to 5 miles east of Kalamazoo County but is in places much narrower. T h e width reduces to 2 to 3 miles and becomes very narr ow in Pavillion and es Brady townships toward the southwest (Fig- 6). The writer believes that this weaker and narrower northeast-southwest trending moraine was formed as a push moraine by the Lake Michigan ice. Leverett in his Michigan Geological Survey manuscript field maps# refers to this moraine as the eastern limit of Lake Michigan ice. Topography of the Tekonsha moraine is character­ ized by small knobs and kettles and is subdued compared to the bold Kalamazoo moraine segments. The moraine also is dissected by valley-like gaps in Brady Township where glacial drainage (Leverett# 1915) seems to have been forced across it while it was in contact with stagnating and downwasting ice in Kalamazoo County. The maximum altitude reached by this moraine is about 1#000 feet above sea level# and this occurs at the moraine junction south of Fort Custer Military Reservation in Charleston Town­ ship (Fig. 6 and Plate I ) . The greater ^ art the of moraine south of the Kalamazoo River, is a bit lower, reaching elevations between 92 5 and 97 5 feet. The morainal spurs north of the Kalamazoo River are slightly lower reaching an average of 900 feet elevation. The relief towards the outer margin of the Tekonsha moraine is very gentle except for a few large knobs and groups of knobs having 100 feet or so of relief. The inner margin has slightly greater relief than the outer margin. Width, relief, and elevation 66 decrease considerably towards the southwest, in Pavilion and Brady townships. North of Climax village this moraine is known locally as "Tobys Hill." There are very few lakes near the head of this reentrant district compared with the head of the reentrant area between the Kalamazoo moraines {Fig. 6}. The Tekonsha spurs north of the Kalamazoo valley, however, have large depressions below the border­ ing gravel plains, and surficial stratified materials reveal much slumping, which suggests that stagnant ice conditions may have persisted here during the building of outwash from the Kalamazoo moraine. The Tekonsha moraine in Kalamazoo County is c om ­ posed of loose-textured sand and gravel and isolated areas of finer clayey material. Sand predominantes. Leverett (1915) believed that this excessive sand was derived from neighboring sandstone formations to the northeast, as well as from the removal of finer material during deposition. From a few well records (Figs. 25 and 26) it seems that there are some thick layers of clay till 50 to 80 feet below the surface, and near-surface sandy material is oxidized to yellow to brownish-red color. Diversity of structure even in small areas suggests too that ice borders of both lobes must have been very active in this inter­ lobate area. The writer observed 6 to 8 feet of ablation till overlying stratified outwash sediments at sample site number 16 (Figs. 16 and 28 and Plate I ) . on the southern 67 margin of the Michigan-Saginaw ice junction, in the southwestern part of Section 22, Charleston Township X on Plate I ) . (see This till connotes a significant readvance of the Saginaw lobe towards the southwest. It is of interest that similar type of till is not found on top of the outermost northeast-southwesterly trending Tekonsha moraine of the Lake Michigan lobe. Also, boulders and cobbles are numerous at the interlobate junction area south of the Kalamazoo River valley. Other Small Moraines in Kalamazoo C o u n t y .— There is a norrow east-west trending ridge south of Marrow Lake which connects the main Tekonsha Moraine of the Lake Michigan lobe in Sections 24 and 2 5 of Comstock Township (Fig. 6 and Plate I). maps Leverett, in his manuscript field (Michigan Geological Survey), named this as the Battle Creek Moraine of the Lake Michigan lobe and showed a connection with the western part of the morainal spur in Ross Township. On the basis of morphology and litho- logic distribution of sediment, this writer disagrees with this interpretation, believing instead, that this narrow ridge marks the maximum advance of the Lake Michigan lobe and was formed at the same time as the northeast-southwest trending Tekonsha moraine Also, (Figs. 5 and 6, and Plate I). this narrow east-west trending moraine may have connected with the weak and disconnected almost north-south 68 trending moraine in northwest Comstock and southwest Richland townships (Fig. 6 and Plate I). The east-west trending Tekonsha moraine in Comstock Township has very low relief and is mostly composed of loose-textured sandy material. According to this writer's interpretation of interlobate line (Plate I) in the last c h a p t e r , the nearly north-south trending moraine, in northwest Comstock and southwest Richland townships, also marks the latest maximum advance of the Lake Michigan lobe against the Saginaw lobe. (Mich, Geol. According to L e v e r e t t 1s S u r . manuscript maps) interpretation, he con­ sidered this as a pre-Kalamazoo moraine, but the writer suggests that this moraine was formed between Lake Michigan ice and Saginaw ice (Fig. 10), when the Lake M i chigan lobe ice overrode the bold Kalamazoo moraine. The rationale here is that this moraine also has loose-textured sandy material mixed with clay in some areas, but at a dep th of more than 50 to 60 feet thick clay till layers are present according to well log data. In other words, this moraine * seems to show connection to the north with the bold inter­ lobate moraine (Folsom, 1971) formed in the northeast part of Cooper and northwest part of Richland to w ns hi ps . In case the reader questions the validity of small linear moraines representing the outer limit of Lake M i c h ig an ice, he is reminded that the regional trend of these moraines is aligned with the well-established Lake Michigan ice moraines to the w e s t . 69 A narrow north-south trending morainal ridge about 3 to 4 miles long exists in Sections 17, 20, 29, 31, and 32 in Brady Township (Fig. 6). dissected by Portage Creek. Its southern end is This ridge, too, has very low relief and its width is about one-third mile. Surface material is again loose-textured and sandy looking similar to the above described two small moraines which are sug­ gested as marking the limit of the Lake Michigan lobe in Kalamazoo County. There are also two small, elongated, spur-like ridges present in this county (Fig. 6). One is a north- south trending ridge mostly in Sections 2 and 11 of Port­ age Township, port. southwest of the Kalamazoo Municipal A ir ­ Detailed characteristics of this spur are not known except in one gravel pit where sample 17 was collected. In this gravel pit materials vary from clay to boulder size. Some coarse gravel is crudely stratified and sand and clay near the surface are not laminated. and cobbles are scattered all over the pit. Boulders Thin clay till is present on top of the loose-textured sand and clay. A second northwest-southeast trending spur-like ridge is present 2 miles north of Cooper Center in Sections 4, 5, 8, and 9 of Cooper Township. Here, too, there is little information available about this narrow ridge due to lack of exposures and very few wells drilled in the area. 70 A small moraine (Plate I) in Sections 26, 34, and 35 of Prairie Ronde Township is believed (Leverett, 1915, p. 147) to be the northward extension of the massive Sturgis moraine lying to the south in Cass and St. Joseph counties. We should recall the Sturgis moraine which lies on the interlobate tract between the Lake Michigan and Saginaw lobes (Plate I ) . Topography of this moraine in Cass and St. Joseph counties is similar to that of the interlobate moraine in southwestern Barry County. The high knobs of this moraine are among the most prominent in southwestern Michigan. In this connection, Leverett (Leverett and Taylor, 1915, p. 149) suggested a possible overriding by the Lake Michigan lobe on deposits of the Saginaw lobe. Here the writer agrees with Leverett1s interpretation, based on analysis of petrographic data. Further discussion of this point is given in Chapter X. The northward extension of the Sturgis moraine in northern Flowerfield Township, St. Joseph County and Prairie Ronde Township of Kalamazoo County, was mainly formed by the retreating Lake Michigan lobe ice. and kettle topography is conspicuous. Knob The altitude reached by this moraine in Prairie Ronde Township is between 850 to 900 feet. The average width of its north-south trending ridge is 2 miles, narrowing to half a mile in Sections 26 and 36 of Prairie Ronde Township. Here the surface material is not as sandy as that of the Kalamazoo moraine, but it differs by the presence 71 of numerous boulders and cobbles and loose-textured clayey till near the surface. This writer has drilled a few drill holes up to the depth of 72 feet to the west of this moraine, which revealed the presence of tight clay till at depths between 40 and 60 feet. More detailed infor­ mation of the deeper part of this moraine is not available because of the lack of deeper wells in the area. Till Plains There are three gently undulating till plains which are important in the glacial history of Kalamazoo County and vicinity (Fig. 6 and Plate I ) . The major till plain of Climax, Wakeshma, Brady, and Pavillion townships in southeastern Kalamazoo County (Fig. 6) was formed during the main north-eastward retreat of Saginaw ice, accompanied by minor readvances of the Saginaw ice, accompanied by minor readvances of the Sagi­ naw lobe. This till is traversed by a group of drumlins, and later has been dissected by meltwater channels flowing towards the southwest during retreat of the Saginaw lobe ice. This till plain was formed at the same time and in the same way that other till plains formed in neighboring Calhoun, Branch, and northeastern St. Joseph counties. In southeastern Kalamazoo County and immediate vicinity this till plain is composed of clayey till and has a gently undulating surface with numerous 10 to 4 0 feet high knolls. Some of these have drumlin shape. Boulders and 72 cobbles are plentiful in the area as one m a y see along the sides of the roads and in fields. 1957) It is believed (Martin, that some of the sandy and gravelly outwash from the Tekonsha moraine in reentrant area covered the ground moraine or this till plain by forming an outwash capping over it (see Fig. 14 as an e x a m p l e ) - Th ere is very little information regarding the detailed subsurface structure of this till plain. Till plain in Cooper Township (Fig. 6) has also characteristic undulating topography resulting from the westward retreat of Lake Michigan ice. This till plain is composed of about 2 to 8 feet of boulder and cobbly clay till overlying earlier formed valley train deposits, just the opposite of the above described case in south­ eastern Kalamazoo County. This till plain, however, i£ discontinuous at some places where the underlying outwash is exposed at the surface. Good exposures can be seen in the American Aggregate C o m p a n y ’s gravel pit northeast of Cooper Center. Such a till capping over valley train deposits reveals readvance of the Lake M i c h i g a n lobe overriding the earlier Kalamazoo moraine and outwash. A similar but smaller till plain overlying an outwash plain is present in Prairie Ronde Township w e s t of the Sturgis moraine. (Fig. 6), This one indicates a seemingly rapid retreat of Lake Michigan ice up to the Lake Michigan Kalamazoo moraine, in that stagnant ice would produce m or e irregular terrain. 73 Drumlins Most of the drumlins in this area are formed over till plains, except for a few surrounded by glacial drain­ age, in southeastern Kalamazoo County. The "ideal” stream­ lined drumlin usually looks like an inverted halfellipsoidal bowl or spoon, but drumlins in Kalamazoo County vary much from this ideal shape. narrow elliptical hills; Some are long some have sharply pointed ends pointing in both upstream and downstream directions, and some are lacking systematic form. Their long axes, how­ ever, generally parallel the direction of flow of the Saginaw lobe ice. The presence of drumlins in this county (Plate I) connotes short readvance of the Saginaw lobe, also in neighboring Calhoun, Branch, and St. Joseph cou nt i es . Due to the lack of sufficient exposures and sub­ surface information, the internal structure or composition of these drumlins is not known. From the study of surfi- cial deposits and soil types and a few well logs, it seems that they are composed of clay till. These unusually streamlined features are presumed to be the result of very actively flowing ice of the Saginaw lobe just before for­ mation of the massive Kalamazoo moraine where complex and rugged morphology was subsequently modified by stagnating and dead ice conditions. 74 Glacio-fluvial Features Glacio-fluvial features in the study area consist of a group of stratified sediments and a group of icecontact stratified sediments. In Kalamazoo County, most of the glacio-fluvial features are proglacial, indicating outwash plains, lacustrine plains, drainage ways, and clay and silt capping on fluvial plains. Major ice-contact features like kames and eskers have not been found in Kalamazoo County. The question of their presence is d i s­ cussed in a later part of this chapter. Outwash Plains Outwash plains of Kalamazoo County and vicinity were built during the shrinkage of the Saginaw and Lake Michigan lobes respectively. Whatever outwash was built by pre—Cary ice was overridden and destroyed or buried before the two lobes reached their maxima in Kalamazoo County. Kalamazoo County has two-thirds of its area covered by outwash plains developed waters from both ice lobes. (Plate I) by the melt- The vigorous line of fluvial discharge in the reentrant district produced an outwash plain wh ich descends southward continuously from the reentrant angle between the two lobes to across the Kalamazoo River valley up to St. Joseph River valley. places this outwash plain is more in the form of a tributary valley train situation. As a unit, however, In it constitutes most of the outwash in Kalamazoo County. The width of the outwash (Fig. 6) is about 12 to 15 miles, and the elevation lies between 1,000 feet near the head of the reentrant and 9 50 feet within a few miles to the south. The elevation is nearly 9 50 feet along much of the outer margin of the Kalamazoo moraine in the western part of Kalamazoo County, and remains above 900 feet in the south­ western part of the county. The surface elevation drops 60 to 8 0 feet near the center of Kalamazoo County where meltwaters from the west and northeast joined together and flowed southward towards the Kankakee Torrent (Fig. 4). Outwash to the north of the Kalamazoo River in the northeastern part of Kalamazoo County and all the way up to the head of the reentrant area is coarse with numerous pits. Some of these pits are very large and indicate that huge detached masses of ice remained when the Saginaw ice retreated back to form the Kalamazoo morainic system. Time was insufficient to melt these detached masses be­ fore they become surrounded by outwash, and also the cli­ mate might have been cooled a little to preserve these masses, while the filling of outwash around them from the downwasting Kalamazoo moraine system was completed. Eventually, of course, the detached ice masses melted away, leaving large pits, as inverted topographic forms. Taking into consideration the general slope, the writer interprets the lithologic composition as is similar to 76 that found elsewhere derived from the Saginaw lobe. Thus the outwash north of the Kalamazoo River is considered as carrying meltwaters of the Saginaw lobe. similar factors, Considering the outwash to the south of the Kalamazoo River and to the west of the Tekonsha moraine of the Lake Michigan lobe was formed by earlier retreating Saginaw ice and later overridden by the Lake Michigan ice. outwash east of the Kalamazoo moraine lobe segment) age (Fig. Thus the {the Lake Michigan up to the line of southward flowing d r ai n­ 6) was formed by meltwaters from the Lake M ichigan lobe. The outwash in the reentrant angle between the Tekonsha moraines of both lobes slopes from northeast to southwest. The elevation is 990 feet at the northeast edge and drops to 912 feet at Scotts station in the south­ eastern part of the county. It is very coarse in the northeast, but becomes sandy toward the southwest. South of Climax this outwash seems to be spread over the n orth­ ern part of a till plain which was built earlier. A long narrow body of outwash (Fig. 6) covered by a thin till plain in Cooper Township east of the Kalamazoo moraine, is a classic valley-train deposit. This valley- train form of outwash indicates that active deposition m us t have taken place by braided meltwater streams in a n arro w valley, with water derived from the ice of both lobes. Thus it seems that the Kalamazoo River valley was 77 blocked by advancing Lake Michigan ice. current beddings Presence of (Pig. 17), slumped outwash, channel fillings, varying dip directions indicating rapid fluctu­ ations of streams, terracing, locally deposited lake clay interbedded with sand and gravel (Fig. 18) and so forth reveals the complexities of this depositional history. About 60 per cent of the material is sandy and quite a few cobbles are seen embedded in coarse gravel beds (Fig. 17). There is other outwash covering small areas in the western part of the county. A small outwash plain formed south of the Alamo moraine slopes south indicating meltwater direction from north. Small areas of patchy out­ wash along the axis of the Kalamazoo moraine also repre­ sent shallow local deposits, underlain by till and probably filling large kettle holes in this major moraine system (Fig. 14). In general along the border next to the moraines the outwash material is much coarser than it is at a d i s ­ tance (Fig. 14). Cobbles and coarse gravels are common for about half a mile from the moraine, but average grain size diminishes downstream away from moraine, whereas roundness of particles increases, as does the sorting in a classic fashion. 78 Figure 17. Current bedding in a valley train deposit, American Aggregate Co. pit, Cooper Township, Kalamazoo County. Figure 18. Large pocket of locally deposited lake clay, American Aggregate Co. pit, Cooper Township, Kalamazoo County. 79 Lacustrine Plains and Drainage Way? Retreating Lake Michigan lobe ice made a halt, at the west end of the Alamo moraine, forming proglacial Lake Dowagiac to the north and proglacial Lake Alamo to the south of the Alamo moraine (Fig. 6), When the ice retreated farther west into Van Buren County, Lake Alamo was con­ nected to Lake Dowagiac which later drained through a southwestward outlet west of the Kalamazoo moraine system. Then Lake Michigan ice retreated after forming narrow moraine of the Kalamazoo moraine system in northwestern Oshtemo and southeastern Alamo townships. The Alamo lacustrine plain is made up of sandy reworked outwash with very few pebbles, whereas the Dowagiac lacustrine plain consists of clayey, silty, and sandy material with boulders and cobbles in some areas. These plains are 2 to 3 miles wide with quite a flat surface and they are parallel to the Alamo moraine. The main glacial drainage in central Kalamazoo County was southward, originating at the reentrant between the Kalamazoo moraine systems of the Lake Michigan and Saginaw lobes in southern Barry County. The drainage flowed directly across the present course of the Kalamazoo River east of Kalamazoo. When the northward trending Kalamazoo River valley was blocked by the Lake Michigan ice the Kalamazoo River flowed southward the Austin Lake area. (Fig. 6) via Then most of the meltwaters from 80 the reentrant drained through this outlet and joined the main trunk line drainage southward to eventually join the Kankakee Torrent (Fig. 4). Earlier meltwaters from the reentrant of Tekonsha moraines drained through two southwestwardly flowing drainage channels in the southeastern part of Kalamazoo County. One channel divides the till plain in half, and another channel in Brady Township lies west of the till plain between Glacier and the Tekonsha moraine. This one cuts the terrace and cliffs along the western margin of the Tekonsha moraine. Both of these drainage channels flowed southwestward through m ai n trunk drainage in St. Joseph County. After the ice had withdrawn from the Kalamazoo River valley north of Kalamazoo, meltwaters from the re­ entrant between the two lobes in northeastern Allegan County drained southward along the Run River vall ey to the Kalamazoo River valley and finally southward through the low channel west of the Kalamazoo moraine system in the vicinity of Paw Paw (Plate I) . Clay and Silt Capping on Fluvial Plains As the meltwaters from retreating glaciers drained southward through these fine stratified flat lowlands, fluvial plains of outwash sediments were built in some areas (Fig. 6) especially south of the Kalamazoo River. Above these sandy fluvial plains can be found about 1 to 4 feet of lake clay and silt layers. It is probable that this 81 clay and silt capping on fluvial plains was due to shallow local ponding of waters. Major sites of this type in Kalamazoo County are found in Schoolcraft and Prairie Ronde townships, along with two small areas north of Long Lake and south of Marrow Lake. Development of prairie soil made these areas fertile. Aeolian Features Wind-blown sediments are also present over some of the glacial sediments in Kalamazoo County. The aeolian features are few in number, however, and cover too small an area to draw any inferences as to climatic conditions or their direct relation to glacial activity in this area. Sand Dunes and Loess Sediments Inactive sand dunes or wind-blown sand deposits in Kalamazoo County were probably originally built by reworked glacial and glacio-fluvial drift. They have been recog­ nized in Alamo, Texas, Portage, and Pavillion townships (Fig. €). Sand dunes are difficult to recognize in the field, because of the sandy nature of the surface drift throughout the county. covered with vegetation. Also, some of them have become Some sand dunes plotted in Portage Township by Leverett on his manuscript field maps, have been covered by recent construction. Where found, they are very thin wind-blown deposits and vary much in shape. Longitudinal dune patterns on both sides of 82 Austin Lake and U-shaped dune patterns west of Pickerel Lake indicate that some dunes were formed by eastward blowing winds in a climate appearing rather dry, at least locally. Loess deposits in Kalamazoo County are not very well recognized, but it is just a guess that silt associ­ ated with clay capping over an outwash (Fig. 6) may be wind-blown in nature. Other Features Besides the features described above, other lesser features deserving mention, there are as they are useful in locating sand and gravel deposits. Undefined Transitional Zones In the field it is often difficult to recognize an exact line separating morainal deposits from outwash deposits, due to lack of exposures and difficulty of access to the area. The dashed lines on the map (Fig. 6) represent such undefined transitional boundaries or zones between two recognized and well-mapped features. Such zones are usually about one-fourth to one-half mile wide in which materials show gradation from coarse to fine or vice-versa. For example, as noted in Figure 14, the outwash in this zone is thin and coarse and usually u n d e r ­ lain by till at shallow depth. This transitional zone is ideal for prospecting for coarse aggregates. down slope, As one goes the outwash generally becomes finer. 83 The Question of Kames Karnes are usually known to be ice-contact features formed either by accumulation of water-worked detritus on the surface or inside stagnant ice, or else in the form of delta or outwash cones built in front of the ice by vigor­ ous meltwater stream action. Usually a kame is a jumble of conical knolls and hollows and is formed of stratified gravel, till. sand, and silt which may contain local pockets of The possibility of kames is usually higher in inter- lobate areas, but due to practical difficulties in proper identification in Kalamazoo County, they were not shown on the map (Fig. 6). If kames are present at all in this county, they would be mixed with the knob and kettle topography in the complex moraines. Folsom (1970, p. 110) reported kamic-type land­ scapes which cover about seven square miles of area in the central part of Hastings quadrangle, Barry County. Ex­ cepting this area, there are no other kames reported or observed in the reentrant districts. guess of this writer, It is purely a that there were very large and numerous kames built in the Saginaw-Huron-Erie interlobate area in southeastern Michigan due to smaller re­ entrant angles than that between the Lake Michigan and the Saginaw lobes. In addition to the reentrant angle factor, other factors like longer periods of stagnation of ice, thickness of ice, and intensity of meltwater activities 84 may be responsible for building large kames. The subject needs further study beyond present purposes of this in­ vestigation . Types and Associated elastics The most common clastic sediments of glacial origin in Kalamazoo County can be divided into three major groups: (1) boulders and cobbles, (2) gravel and sand, and (3) silt and clay. Boulders and Cobbles Free boulders and large cobbles in Kalamazoo County are mostly associated with terminal and lateral moraines and till plains, where they can be seen in the fields or along the road sides. Boulders and cobbles are found in moderate number on the surface of the Kalamazoo, Tekonsha, and other small subterminal moraine zones of the main Lake Michigan lateral moraine system. Also, they are found in substantial number on the till plain of the southeastern part of the county. Most of the boulders and cobbles are no longer evident in densely populated areas, having been used in foundations and building purposes. Originally most of these were of crystalline rocks of different sizes and shapes, and some show exfoliation on the surface. These boulders and cobbles do not show any particular system of patterns in Kalamazoo County, except that they are most prevalent on interlobate moraines in northeastern Cooper Township and southwestern Barry County. 85 The majority of boulders and cobbles associated with Saginaw ice are granite, granite gneiss, and pink and white quartzites, but m an y are of other rock types. Among these are index erratics such as the red jasper conglomer­ ate derived from Huronian ledges north of Bruce Mines, Ontario, and a Precambrian tillite Gowganda from Ontario) (quite certainly containing pink granite pebbles. The writer observed large— sized cobbles and boulders of jasper conglomerate and the Pre-Cambrian tillite in four localities in Kalamazoo County. Specifically, these are: (1) in fields associated with the till plain in Wakeshma Township; (2) in a gravel pit associated wi t h the morainal spur in Ross Township, where sample 4 4 was taken; (3) associated with valley train deposits in a gravel pit in Cooper Township where sample 2 was taken; and (4) in a gravel pit associated with the Kalamazoo moraine of the Lake Michigan lobe in Prairie Ronde Township, where sample 1'8 was t a k e n . Boulders and cobbles associated with Lake Michigan ice are granite, granite gneiss, some purple quartzites, and ma n y dark crystalline rocks. But, the Lake Michigan lobe material does not contain any peculiar or exotic rock type such as the Gowganda, which can be used as an index rock for this lobe. The foregoing information was taken into consideration in interpreting the glacial history of the a r e a . 86 Gravel and Sand In Kalamazoo County and vicinity, gravel and sand are easily accessible in many parts of the area. Gravel is less widely distributed than sand, which makes up about 60 per cent of the surface material. Most of the gravel and sand deposits of the county are associated with o u t ­ wash plains and small outwash deposits; and they are better sorted and stratified than in other areas. Some of the outwash is rather poorly sorted and difficult to d i s t i n ­ guish from adjacent till. As shown in Figure 14, generally coarse gravelly material is present showing crude stratifi­ cation associated with the transitional zone between moraines and outwash. In general, the grain size decreases and the quality of stratification improves with increasing distance downstream from the source. At several places gravel and sand deposits are interbedded with numerous lenses of fine sand, salt, and clay. Gravel and sand deposits associated wi t h other glacial, g l a c i o - f l u v i a l , gla ci o- la cu st ri n e, and aeolian features are described under each heading in this chapter and so need not be repeated again. Silt and Clay Silt and clay deposits associated with tills of this county are, in most places, sandy material, whereas, dominantly fine sand, too full of stony and lake bottom deposits are p r e ­ silt, and clays. The most recent 87 drainage channel deposits, however, are locally inter­ bedded with lake-deposited silt and clay and are mantled by silt deposits of the modern rivers in this county. Clay and silt capping on the fluvial plains (Fig. 6) south of the Kalamazoo River is described previously in this chapter. The silt deposits mixed in with clay in this area may have partially been laid down by wind in locally ponded waters or it could have been brought by southward flowing meltwaters. In general, silt and clay deposits near the surface have been observed to overlie the glacio-fluvial sediments which cover such large areas in Kalamazoo County. CHAPTER VI BEDROCK GEOLOGY Consolidated sediments beneath the unconsolidated glacial sediments of Kalamazoo County are all of Paleozoic age. Owing to the total absence of rock outcrops and the limited number of deep wells in the county knowledge of the subsurface geology in this region is restricted in scope. A few widely scattered oil and gas wells penetrate the bedrock formations, and some water wells reach the bed­ rock surface; but many of the well logs lack adequate descriptions of the rock penetrated. Hence, the follow­ ing discussion pertaining to the lithology, extent, con­ figuration, and structure of bedrock is based on rather limited data obtained from wells within the county and from available outcrops examined. adequacy, In spite of this in­ some knowledge of the bedrock formations, how­ ever, is essential to the interpretation of the source and presence of local lithologies in the surficial deposits of glacial origin. 88 89 The Lithologic Sequence The bedrock geology m a p of southwestern Michigan (Fig. 19) and available well logs reaching bedrock in Kalamazoo County reveal that the glacial drift is u n d e r ­ lain primarily by Colwater shales and Lower Marshall s and­ stones of lower Mississippian age. as indicated by deep borings, Below these fo r m a t i o n s , the stratigraphy is r e p re ­ sented by older Paleozoic sediments of Devonian and Silurian age. These older strata in turn m a y be un der­ lain by still older Paleozoics resting upon crystalline rocks of Precambrian age. The Coldwater shale forms about 95 per cent of the bedrock surface in Kalamazoo County. The remaining 5 per cent is formed by the Lower Marshall sandstone. Both of these formations in Kalamazoo County are briefly described as follows, and their stratigraphic sections are pictured in Figure 20. Coldwater Shale The Coldwater shale is the main bedrock lithology in Kalamazoo County, running beneath the drift as a broad belt about 2 5 miles wide trending northwest-southeast across the county. the northwest, This shale further extends toward southwest, neighboring counties. and southeast well into the Cohee (1965) suggested that this shale was deposited during early Mississippian time, and its source was supposedly from the western side of the MXll CD O BEDROCK GEOLOGY OF SOUTHWESTERN MICHIGAN Figure 19. Bedrock geology of Southwestern Michigan. 91 .\ V v v V • V y ’y y.y V V V .V V ' y - I SHALE DOLOMITE LIM ESTONE I S 3 O O LITIC E CLAY IRONSTONE C O N C R ETIO N S !•*-*« J M EGAFOSSILS I D CHERTS i MICACEOUS F ig u r e 2 0 . G e n e r a liz e d s t r a t ig r a p h ic s e c tio n s o f the L o w e r M a r s h a ll s a n d s to n e and C o ld w a te r s h a le in S o u th w e s te rn M ic h ig a n s h o w in g u r iq u e id e n tifia b le c h a r a c t e r is t ic s . 92 Michigan Basin as a result of uplift and erosion in the Wisconsin highlands (Fig. 19), The Coldwater formation was first described in 1895 by Lane. In the southwestern part of Michigan it is dominantly a blue to gray and occasionally greenish shale or sandy shale becoming more micaceous and arenaceous up­ ward, and gradually passing into overlying Lower Marshall sandstone. These shales seem to be more blue than gray towards the northeastern part of Kalamazoo County. There are thin interspersed beds of limestone and dolomite (Fig. 20) which are discontinuous over large areas. These are more common in the western and southwestern parts of the county. In the northeastern part of the county, near the top, interbedded sandstones and shales are reported in oil and gas logs. Hard brownish zones of shale, also revealed by logs, are present toward the southeastern part of the county. These shales are known to contain thin zones of cherty limestone, oolitic limestone, dolomitic limestone, fossiliferous limestone, and clay iron­ stone concretions. The writer visited the type locality and several other outcrops of Coldwater shale in Branch and Calhoun counties, where he observed a number of zones of clay ironstone concretions and ferruginous bands in shale. Also he came across septarian-like structures with secondary mineralization of calcite. in these outcrops, One can also see, fossiliferous zones containing mainly 93 varieties of brachiopods and other less common fossils. Near the base of several oil and gas logs, a reddish or purplish rock (called "Red Rock") has also been recorded. This is variable in composition, and may not be used as a direct horizon marker. The average thickness of the Cold- water formation in Kalamazoo County is approximately 650 feet. Lower Marshall Sandstone The presence of Lower Marshall sandstone in the northeastern part of Kalamazoo County is indicated by a very few well logs. Its contact line with the underlying Coldwater shales (Fig. 19) is a matter of debate. Winchell (1861) first described this sandstone as white, gray, green, and red in color, locally very micaceous and fossiliferous (Fig. 20). Again clay ironstone con­ cretions are present in blue-gray sandy shale lenses. Streaks and pockets of coal and coaly vegetation impres­ sions are reported. Data pertaining to the occurrence of this sandstone in Kalamazoo County are mostly lacking, and so it is not described more completely. Bedrock Configuration and Pre-glacial Drainage Configuration of the bedrock surface in southwestern Michigan is complex. (Fig. 21) Its character sug­ gests that different processes were active during a series of geomorphic cycles. The present bedrock wf v i Cllv * w o o * DO [All cm***} o. M\ '** € ' W. II ■— UflJ BEDROCK TOPOGRARHY SOUTHWESTERN MCHK3AN rnnmm.mmi _L_\ Figure 21. Bedrock topography of Southwestern Michigan. 95 topography in the study area was sh ap e d by preglacial c rustal d ef or ma ti on ac co m pa ni ed by fluvial erosion, glacial and g l a c i o — fluvial erosion, fluvial modification. then and then p os t—g l a c i o - Inter p re ta ti on of the p r i n c i p a l drainage lines has b e e n attempted by several previous workers on the basis of its general structure, i.e., topography, bedrock and the di f f e r e n t i a l h a r d n e s s of bedrock, whether shales, and A n d e r s o n (1956) sandstones, or carbonates. H o r be r g and several o t h er earlier w o rk er s believed that the p r e —glacial d r a i n a g e flowed toward the Lake M i c h i g a n lowland w h i c h further empt i ed e astward into the St. La wrence River. Bedrock d r a i n a g e patterns o b s e r v e d on the m ap s in F i g u re s 21 and 22, s u g ge st that b e d r o c k channels dip toward the Lake M i c h i g a n lowland, and a r e g e n e r a l l y parallel to the strike of the underlying b e d ­ r ock . On a broad scale, bedrock t o p o g r a p h y also is known to influence the p a t t e r n of ice mo vement, especially w he n we take into c on s i d e r a t i o n the d o m i n a n t importance of the angle of surface slope in the f l o w - l a w of ice 197 0). Therefore, (Miller, it seems possible that the gen er al slope of the bed r oc k surface in s o u t h we st er n M i c h i g a n toward the Lake M i c h i g a n lowland c o ul d have promoted a d ­ vance of the Lake M i c h i g a n lobe toward the east and s o u t h ­ east, w i t h the result being mu c h g l a c i a l plucking a n d erosional m o d i f i c a t i o n of the p r e - g l ac ia l bedrock surface. 96 F ig u re 2 2 . B e d ro c k to p o g ra p h ic m a p o f K a la m a z o o C ounty (a fte r Ib r a h im , 1 9 7 0 ). 97 Similarly, the bedrock highland in the southeastern part of the area (Fig. 21) of study m a y have reduced the erosive effectiveness of the Saginaw ice. This bedrock high is assumed to be the result of the greater hardness of lithologies in this sector, as well as some control exercised by structure (Fig. 21). Ibrahim (1970) mapped in detail the bedrock topo­ graphy (Figs. 2 2 and 24) and buried pre-glacial bedrock drainage channels of Kalamazoo County, using available well log data and gravity surveys. His purpose was an analysis of the p r e —glacial and glacier marginal drainage and groundwater potential of the county. In this he also attempted to reconstruct the drainage pattern before and during glaciation. Figure 24 shows the distribution of bedrock channels and surface geology in Kalamazoo County. It is apparent that present surface drainage is westward, is the buried bedrock drainage, coincide with each other. as but they do not exactly In general, however, the sur­ face channels of Kalamazoo County exist more or less in the same areas where underlying bedrock channels exist, except where bedrock channels are blocked by great thick­ nesses of drift. In fact, some of the surface channels coincide very closely with the buried bedrock channels, although in a broader sense the correlation between surface topography, drift thickness, and the bedrock configuration is inversed in Kalamazoo County. To 98 explain this, while the pre-existing bedrock surface generally slopes downward to the west in this county, the present surface topography, as well as the average thick­ ness of the drift is highest at the western side of the county, and 26). i.e., it slopes and thins to the east (Figs. 25 The situation appears to be just opposite in the eastern part of the county. This situation is considered in the next chapter, and is illustrated by the crosssectional diagrams in Figures 25 and 26. Structures The formations of lower Mississippian age, which make up the bedrock in Kalamazoo County, are part of the bowl-shaped structure of the Michigan Basin. The pre­ dominantly Paleozoic formations of this basin outcrop in more or less concentric bands, the youngest being at the surface in the central part of the structure and the o l d ­ est at the surface around the perimeter. Kalamazoo County and vicinity lies in the southwestern part of the Michigan Basin. The Coldwater shale and Lower Marshall sandstone (Fig. 19) gently dip northeastward toward the center of the basin and strike northwestward. Here, it is note­ worthy that in the Kalamazoo County area the Lake Michigan lobe ice eroded the bedrock formations along their strike, whereas the Saginaw lobe eroded some formations perpendicu­ lar to their strike. 99 In the southeastern part of the study area shown in Figure 21, the major upland, which strikes northeast, conforms very closely to the bedrock lithology and is possibly a residual structure of an earlier age. This lithology is predominantly the durable Lower Marshall sandstone with the exception of some hard facies of C o l d water shale. This upland is named the Marshall Upland (Horberg and Anderson, 19 56) , and it follows the strike line of the sandstone. Apparently this upland to some extent, impeded the advance of the Lake Michigan and Huron-Erie lobes, a fact which is borne out by the morainal pattern in southern lower Michigan. bedrock structure, if present, Residual could in part at least reflect the physiographic expression of the Marshall upland. CHAPTER VII DRIFT THICKNESS AND STRUCTURE Most of the Kalamazoo County landscape is developed on unconsolidated glacial deposits, overlying bedrock of varying configuration. These galcial sediments are parent materials for Kalamazoo County soils, as well as being important sources of building aggregates, and of ground water. Thus they deeply affect land use, mining, c on ­ struction, and water drilling operations in the county. Also, they must be removed or penetrated in any oil and gas drilling operations that go into the bedrock. For these reasons a description of the thickness and struc­ tural character of the unconsolidated deposits in Kalamazoo County is significant, and the more detailed the infor­ mation the greater its potential in regional and local site-evaluation problems. Isopach Map of Kalamazoo County A generalized drift isopach map of Kalamazoo County (Fig. 23) is compiled from deep well records, drift thickness map of 1938 (Mich. Geol. 100 Surv., Pub. the 101 N BARRY CO. R.IOW. R.9W. B* A L LE G A N COR .I2 W . R .II W. A' T .1 S . H y CO. / T .3 S . ST JO SEPH CALHOUN f CO o i 2 3 4 IS O P A C H IN T E R V A L 5 0 FEET MILES C R O SS SECTIO N TRA N SECTS F ig u r e 2 3 . G e n e r a liz e d d r i f t isopach m a p o f K a la m a z o o C o u n ty . lin e s s h o w c r o s s s e c tio n t r a n s e c t s . D ashed 102 3528), and known differences in land surface elevations and the depth of bedrock (Figs. 2 5 and 26) in selected areas. On this isopach map, glacial drift in Kalamazoo County is seen to range in thickness from less than 50 feet to above 500 feet. The thickest drift occurs over major valleys cut into bedrock. Regionally, est in the northwestern part of the county. drift it is thick­ The thinnest (less than 100 feet) occurs over a sector of south­ eastern Kalamazoo County. Additional regional details on the drift thickness may be obtained from deep driller's logs available in the files of Michigan Geological Survey. The isopach pattern shown in Figure 23 reflects irregu­ larities at the base of the drift or at the top of the drift, or both. course, The surface irregularities were, of fashioned mostly by Wisconsinan glaciers and subsequent Holocene erosion. Although the drift is very thin in the southeastern part of the county, it becomes even thinner in neighboring Calhoun and Branch counties, a region where bedrock is widely exposed. These areas may be of special interest to industry, especially those which require quarried shale and sandstone, as well as to highway engineers for planning. Such isopach maps can also be useful for ground water studies and for the petroleum industry in exploration drilling. 103 Cross Sections Six structural cross sections are presented here (Figs. 24, 25, and 26) representing Kalamazoo County. Of these, three trend approximately north-south, and the other three trend approximately east-west. Bedrock elevations are taken from the bedrock topographic map of Kalamazoo County (Ibrahim, 1970), and the present land surface ele­ vations are taken from existing U.S. Geological Survey topographic maps. Subsurface stratigraphic information is generalized from available water well logs and oil and gas logs in the county. These cross sections show the general character and thickness of drift to vary from place to place. They also indicate that unconsolidated materials are relatively young and are terrigenic, as opposed to the consolidated layered marinogenic bedrock underlying the drift. Drift material generally consists of boulders, gravel, sand, silt, and clay, most of it being sand and gravel with lenses of clay. Most of the clay can be defined as clay till, since it contains some sand and gravel and has no stratification. brown In general clay near the surface is (light) colored and near the bedrock blue-gray (dark) colored, though there are some exceptions. The source of the blue-gray clay is very well like that of the Coldwater shale. Sand and gravel deposits are also present on the buried bedrock surface and these are 4 A .LCGA* Tih^MAi w a i n □ CD n □ Oi/'^Sn AlA'A LMf hi D »iiU HAT W OA 7 PRAIRIE R O NO E (T 4ft, 0 R i *w 20 IT T E M A S < T 3f t , R r 2* l 1 2ft DftHTlMOa2S,Rl2WJ C R O S S S E C T I O N A L A U O (Tift R | £ W ) B'B* 1000 too •00 ax TOO TOO ?WO •00 M O 400 4« MO see3* 21 10 S C H O O L C R A F T < T 4f t , R l l W > C O M S T O C K t T 2S , R l O W ) P O R T A G E (Tift, R l lW l 20 IT K l C M L A N O CTtS, R l Q W l S£C 9 300 CROSS S E C T I O N C ’C 1000 •00 K A L A M A Z O O RIVER 700 W O M O 500 SEC U M 27 2ft 25 BB RR AA DD YY II TT 4SS ,. RR II OO WW JJ C U M A X < T 3ft, R f t W ) ^ ( T * f t ( R B R j 1" * * 4* 400 CHARLESTON(T2ft, A* C H A R L E S T O N (Tift, RftW) R O f t f t ( T il ff t t, , f tt * * WW l l SOUTH *- NORTH l e g e n d E ^ l CAAYCL □ G « U C L A N O SANO Figure 25. SAND | C L A Y A N D SILT lff3 L O W E R M A R S H A L L S A N D S T O N E j uNOlFfEREnTiatEO GLACIAL DRIFT c o l d w a t e r s h a l e B A S E D A T U M IS W E A N S t A L E V E L South-North cr o ss section s A A \ B B \ and CC’ in Kalamazoo County. C R O S S 1000 S E C T O * D - D 1 wo ^ 7M TOO |100 w “HQ •00 MO- ICC ” "TT < I 1* ALAMO (T U , ||* W ) COOPCR | 22 M ZJ 24 2? 20 3N 21 •ICHLANO fTU, mow) TIi. «IIW) C R O S S S E CT I O N E - C >000 •00 •00 h too TOO TOO $ *00 •00 500 400 aoo SCCII 21 23 22 2* KALAMAZOO{T2$,III*! OSHTCMO |T 2 1 Ml2 1 ] 21 27 23 COMSTOCK fT 2 S , ftiO w) C R O S S S E C T I O N 20 o Cl 300 27 SEC 25 CHARLESTON (2 5 , OfW> F - F 1000 •00 •00 PORTAGE RIVE* GOURONECK CREEK TOO 400' 400 300- I—“ T— - — 21 27 2* T E U S (T3V *I2») PORTAGE (TJ% RMWj SCHOOLCRAFT |T4% ftM « | ORAOT(T4%RIOW) 20 21 22 23 SCC 25 MAKESHMA (74% K fw j WEST EAST LE&ENO fc j- .'j SRAVEL ETH [' GRAVEL A M ) SAND Figure 26. j SAND I CLAV AMO JILT £23 I UNDIFFERENTIATED GLACIAL DRIFT LOWER MARSHALL SANDSTONE COLDWATER SHALE BASE DATUM IS MEAN SEA LEVEL W est-E ast cro ss section s D D \ EE', and FF' in Kalamazoo County. 107 possibly of pre-Cary age. The cross sections show that the bedrock has great gross relief and that the drift mantle has somewhat lessened the control of the older topographic configuration, as far as the subaerial surface of today is concerned. Correlations of Bedrock and Drift Thickness A complicated erosion surface with valleys and uplands was developed on the uppermost Coldwater shale and Lower Marshall sandstone before and during glaciation. This resulted in deposition of unconsolidated drift on a very uneven floor. The glacial and glacio-fluvial pro­ cesses, however, have been mostly responsible for fashion­ ing the major landforms that make the upper surface of the uneven drift. Holocene fluvial erosion in some areas has produced further minor irregularities. in this chapter The cross sections (Figs. 25 and 26) and a comparison of Figure 23 and Figure 24 show the tendency for drift to be thicker in large bedrock valley areas and thinner in the bedrock upland areas. For example, where the main Kalama­ zoo moraine either crosses or is aligned with bedrock valleys, the drift is further thickened. Therefore, drift thickness and the alignment of isopach lines essentially reflect the bedrock configuration. may, The bedrock topography therefore, have been a major controlling factor in the thickening and thinning of terminal ice in the 108 interlobate zone, as well as exercising a direct control on the relief and depth of the glacial drift. CHAPTER VIII SOILS OF THE AREA Soil is the collection of natural bodies in the upper portion of the earth's crust that has been altered in situ by natural processes into layers or horizons whose physical, chemical, and biological properties differ from each other and the underlying unaltered parent rock materials from which they were formed. In Kalamazoo County such materials are originally of glacial origin and have been altered at various times since by weathering, action of water, air, and organisms. The soil processes, of course, began after glaciers r e ­ treated, depositing unconsolidated glacial drift with diverse textures and lithologies exposed to weathering. Such soils are usually classified into more complex classifications, than merely as glacial soils, depending on the physical, chemical, and biological properties of the individual layers, or on soil profile characteristics and their interpretations. In some places several grades of soil on a single glacial feature have been described because of differences in their properties. 109 110 Interpretation of soil morphology, soil genesis and soil classification are related to the following soil formation factors, which deserve mention here: 1. Parent rock material— texture, structure, or fabric and mineralogical or chemical composition. 2. Soil climate— soil moisture, soil temperature, and soil air. 3. Topography— shape of the soil body in relation to the e arth’s center of gravity, water table, and s u n 's r a y s . 4. Organisms— plants or animals or man. 5. Time or age— for which land surface is exposed to above factors. A genetic soil classification is based on the above soil formation factors, and a morphological soil classification is based on observed properties of soils. But, the best classification is a combination of both. The new soil classification system adopted by the National Cooperative Soil Survey on January 1, 196 5, is more realistic as well as more comprehensive than any ever developed in the United States. Because of the aim of this investigation, the simplest approach is desired, hence hereafter terms from the classification used prior to 1965 are used. Ill Soil Series The first detailed report on the soil survey of Kalamazoo County was by S. O. Perkins and James Tyson, published by the U.S. Department of Agriculture in 1928, in cooperation with the Michigan Agricultural Experiment Station. This report has a colored soil map (Plate II) of the county prepared by the Bureau of Soils in 1922. It describes all soils in detail and shows distribution of the soil series and their types in the county. After 1928 no new detailed and revised soil survey report or soil map of Kalamazoo County has been published. The Kalamazoo County Soil Conservation District has made more detailed soil maps of scattered farms for planning pur­ poses. The writer makes primary reference to the 1922 soil map and uses soil series names which precede the new classification. In Table 1 an attempt is made to correlate soil series names from the older classification with that of the new classification. Also in the table, the associ­ ated natural drainage, parent material, and glacial fea­ tures are briefly described. series, County In all, 13 mineral soil and organic soils have been reported in Kalamazoo (Plate II). Out of these, the Beliefontaine series is now a part of the Fox series and the Griffin series is described as the Shoals series. et al. According to Whiteside (1963), most of the better drained local soils TABLE 1 CLASSIFICATION OF SOIL SERIES IN KALAMAZOO COUNTY I N OLD AND NEW CLASSIFICATION SYSTEMS WITH THEIR ASSOCIATED NATURAL DRAINAGE, PARENT MATERIALS, AND GLACIAL FEATURES Sol] Series Ntmes used In U.S.D. A. Soli Survey Report 192 8 ' New Equivalent Series fielletontaine Fax Brtdy Colomn New Classification Family Name (After 1941] Floe-loamy over sand or sandy-skeletal, mixed, mealc, Typic Hapludalfs Order New Classification (Order Old Classification) Alfisol (Zonal Soil) Spinks Sandy, mixed, mealc, Paammentlc Hapludalfs Alfisol (Zonal Soil) Fine-loamy mixed, mealc, Udolllc Ochraqualfs Alfisol (Zonal Soil) CTosby ~ Fine-loamy mixed, mealc. Aerie Ochraqualfs Alfisol (Zonal Soil) Fox ... Griffin Shoals Maumee — Newton - Fine-loamy over sand or sandy-skeletal, mixed mesic, Typlc Hapludalfs Fine-loamy, mixed mesic. Aerie Fluvaquenta (non-acid) Sandy, mixed, non-acid, mesic, Typic Haplaquoll* (non-calcareous) Sandy, mixed, acid mesic, Typic Humaquepts - Coarse - loamy mixed, mealc, Typic Hapludalfs Well drained U. story: Sandy loam to slit loam. 2O”-40" L story: Gravel and Send. (Two-storied) Moraines and Eskers ;(some Drumllnes and .high relief Outwanh) Imperfectly or somewhat poorly drained L\ story: Loamy sand to sandy loam. 20"-40" L. story: Gravel and Sand, Outwash plains (Two-storied) Well drained Loamy sands or sands with textural bands. (One-storied) Moraines Imperfectly or somewhat poorly drained loam or silt loam (One-storied) Till pis ins and Lake plains Imperfectly o r somewhat poorly drained Loam or silt loam, (One-storled| Till plains U. story: Sandy loan, to silt loam. 20"-40" L.story: Grsvel and sand. (Two-storied) OUfwaah plains and Glacial drainage un­ derlain by sand t grsvel Imperfectly o r somewhat poorly drained Loam to slit loam (Stratified) Alluvial deposits Poorly or very poorly drained Sand to loamy n n d (One or two storied) Outwash plains (Bandy) Poorly or very poorly drained Sand (One-storied) Outwash plains (Sandy) Alfisol Well drained (Zonal Soil) Entlao) (Azonal Soil) Mollisol (Intrazonal Soil) Incept iaol (htraxooal Soil) Oshtemo Associated Glacial Feature (Zonal Solly Coarse-loamy, mixed, mealc, Aquollic Hapludalfs -- Associated Parent Material and Texture Alfisol — Conover Associated Natural Drainage Alfisol Well drained (Zonal Soil) Plainfield -Rodman Warsaw - Muck (Organic Soil) ~ Sandy, mixed, add mealc, Typic Udlpsammenta Sandy-skeletal, carbonatic, mixed, mesic, Typic Hapludolls Fine-loamy over sandy or sandy skeletal, mixed, mealc, Typic Argludolle -- U. story: Loamy sand to sandy loam. 20"-40" L. story; Gravel and sand. Outwash plains (Two-storied) (Sandy) Entinol Well drained (Azonal Soil) Mollisol Outwash plains (Sandy) Well drained U .story; Gravelly sandy loam to loam. L story; Gravel and sand, (Two-storied) Cobbly, gravelly and sandy narrow Outwash, and Eskers Well drained LI.story: Sandy loam to silt loam. 20"-4£T L story: Gravel and sand. (Two-storied) Prairie over Outwash and Glacial drainage. (Intrazonal Soli) Mollisol (Zonal Soil) Hist isol (Intrazonal Soil) Sand (One-storied; Very poorly drained - - 113 belonged to the Gray-Brown Podzolic soil group in the former classification, or Alfisols in the new classifi­ cation. Principal subgroups are classified according to the degree and type of soil profile development, texture, the nature of parent material, and natural drainage development. In the column under new classification names the family name is given. This includes the name of each of the higher categories in the complete classification of that series in the new system. The new names connote the major properties of the kind of soils included in each class, and the names also indicate how they are related to each higher category. Each family, for example, coarse-loamy, mixed, mesic, also indicates how it differs within the higher categories. For more detailed infor­ mation regarding the new classification, one may refer to "Pedological-Lectures on Soil Classification" by Guy D. Smith (1965), published by the Belgian Soil Science Society, and "Soil Taxonomy" by the U.S. Department of Agriculture (1971, in press). Among the 13 mineral soils, five have one-storied parent material, six l.ave two-storied parent material, the Maumee series can have either one- or two-storied parent material, and the Griffin series include Holocene stratified alluvial deposits along the banks of rivers and streams. Seven soils are well drained, four soils 114 are imperfectly or somewhat poorly drained, and the r e ­ maining two soils and organic soils (muck) are poorly or very poorly drained. Relation to Parent Material and Surface Geology The texture, fabric, and mineralogical composition of glacial sediments in Kalamazoo County vary greatly, these varied sediments, of course, being the parent materials of the soils. The texture of such parent material varies from very coarse gravel boulders and cobbles) (with a few to sands to silts to clays, all of which have relic t affect on the soil profile. The fabric or structure of the materials varies from relatively porous layered glacial outwash and fluvial deposits to unconsolidated sandy till to compact clay till of varied composition texturally. The geologist is commonly more interested in the mineralogical or lithological composition of the parent materials and its relation to soils, than in textures and fabrics of glacial sediments. For this reason, in this study some petrographic analyses of surficial sediments and a study of soils have been made in Kalamazoo County. The data are shown in Figures 28 to 37. These interpre­ tations reveal local variations in composition, but in general, coarse parent material contains about 60 per cent carbonates, and about 30 per cent crystalline rocks, with the remaining 10 per cent comprised of other lithologies. 115 From this it is clear that parent materials in Kalamazoo County contain much free lime, with most of the soils here being less acidic than in other areas in Michigan where there is less limey parent material or the deposits are of older age. In southeastern and the ex­ treme northwestern part of Kalamazoo County, the per­ centage of carbonates is somewhat less than 60, and the proportion of crystalline rocks rises to 40 per cent. Here we find more acidic (pH less than 5.5) soils such as the Newton and Plainfield types, other series. in association with This example reveals that the composition of parent material is a most important factor in soil formation. Because of many abrupt horizontal changes in tex­ ture, structure, and composition of parent material of glacial origin, the soils of Kalamazoo County are very complex, and their distribution essentially parallels that of the distribution of parent material and natural drainage conditions. The soils are geologically young, as the surficial drift was deposited less than 20,000 years ago. Though topography and drainage of the county were initially induced by the latest glaciation, they are in a geomorphologically youthful state. Neither weather­ ing nor geologic erosion is extensive, and the initial undrained depressions are commonly filled with reducing environment organic soils (mostly m u c k s ) . 116 The depth of weathering varies from 3 to 5 feet, and in the southeastern part of the county it is little over 6 feet (indicated by the newly named Hillsdale series developed over till p l a i n ) . Following the leaching of calcium carbonate the development of an argillic horizon (a horizon with illuvial c l a y s ) , with downward migration of clays, is characteristic mineral soil profiles in Kalamazoo County. The majority of soils in this county show development of each of the A, B, and C horizons, with distinct argillic Bt horizons. This argillic horizon is a distinct characteristic of the humid region Alfisols Brown Podzolic) of southern Michigan. (Gray- In Kalamazoo County, the best example of illuvial migration of clays can be seen in the American Aggregate Company's gravel pit (location of sample no. 2) in Cooper Township. Here stratified sandy and gravelly materials of valley train deposits are overlain by a thin veneer of clay till. Illuviil clays from above lying till are migrating d o w n ­ ward into sand in irregular bands which are not n e c es ­ sarily parallel to the bedding plains of the sand. developed in this area is mapped as Fox loam Soil (Plate I I ) . Use of Soils in Surface Mapping Soil maps and soil descriptions are very useful tools in mapping surface geology, especially the glacial geology in Kalamazoo Coun ty and elsewhere in the state of Michigan. In Table 1, the first and last columns show the 117 relationship between soil types and associated glacial features in this county. These soils are largely the direct product of weathering of the parent materials whose properties are so directly related to former glacial processes in the area. In fact in Kalamazoo County there isr in some areas, quite good agreement between the soil map and the glacial geology map. The writer has made considerable use of the 1922 soil map to trace the surface geology of Kalamazoo County, especially in areas where drift exposures are lacking and the nature of the material is unknown. careful, however, One has to be very in using soil maps, because soil series boundaries do vary in consequence of human error. The Bellefontaine series, which is now called Fox, is usually associated with morainal deposits in Kalamazoo County, but it is also associated with drumlin crests and high level outwash plains, as well as pitted outwash. So one has to recognize and delineate the limitations of soil maps before surface mapping of formerly glaciated areas may begin. Field recognition of soils has proved to be very useful in locating sand and gravel deposits of the area. For example, knowing two-storied soil which has twostoried parent material, can greatly aid in locating some slightly buried sands and gravels. The upper story of the Fox series, as a case in point, usually consists of two 118 to three feet of sandy loam or silt loam, whereas the lower story is composed of sandy and gravelly material. Beneath the lower story one may find coarse 3and and gravel deposits, which shows that soil is a reflection of underlying materials. A geologist should certainly use soils information wherever available, but similarly knowledge of the geology of such an area can also aid the soil scientist when preparing soil maps. PART III CHAPTER IX LABORATORY ANALYSIS OF SAMPLES Large channel s a m p l e s , small spot samples, and auger samples were collected during the field work and brought into the Michigan Department of State H i g h w a y s 1 Research Laboratory for analysis. Mechanical and petro- graphic analyses were made of coarse (-3/16 inch) fractions, (+3/16 inch) and fine to determine the size frequency distribution and lithologic distribution of glacial drift aggregates. Other physical and chemical characteristics such as texture, roundness, sphericity, surface coating, and so forth were not determined, since many of these have been delineated by Wingard in a study conducted to (1969) evaluate gravel resources of southern lower Michigan. W i n g a r d 's study, In he concluded that such additional proper­ ties of individual gravel particles show generally low but consistent correlations, and are only useful for local or detailed assessment of individual gravel deposits. the present investigation, three key properties, In litho­ logic composition, physical strength, and chemical r e ­ activity of aggregates, were determined in detail, 119 since 120 they play the major role in the durability of con­ crete . Mechanical Analysis A n initial 18 channel samples of bank-run sand and gravel material were split using a Jones sample splitter until final split portions weighed about 75-100 pounds. Using a Gilson sieve shaker, particle si 2e distribution of coarse fraction (gravel) of each sample was determined. Sieving time was 10 minutes. following sizes: 1/2-3/8, +2, 3/8-3/16, Samples were sieved into the 2-1-1/2, 1 - 1 / 2 - 1 , 1-3/4, -3/16 inches. 3/4-1/2, Material less than 3/16 inch size was considered as a fine fraction (sand). Such fine fractions were quartered to about 500 grams and sieved by using the following U.S. Standard 10 (2000u), 18 230 (ASTM number) Sieves: (1 0 0 0 m ), 35 (5 0 0 m ), 60 (2 5 0 m ), 120 (1 2 5 m ), (62p), and pan (-230). Fine fractions from the first 18 channel samples and other spot and auger samples were used for mechanical analysis. Complete mecaanical analysis of corase and fine aggregates is given in Tables 4 and 6 (in the A p p e n d i x ) . Fetrographic Analysis The petrographic analysis consisted of basic lithologic identification of each particle of coarse and fine fractions of glacial materials, and determination of the physical strength and chemical reactivity of indi­ vidual particles in the coarse fractions only. Particle 121 counts are commonly made as a basis of discrimination b e ­ tween drift sheets of different glacial epochs. study, however, In this the purpose of the petrographic analysis was to determine relative percentages of specific rock types associated with the two different ice lobes laying down deposits of relatively the same age. time, At the same the information regarding their mineral composition and physical and chemical characteristics can be extremely useful for engineering applications of the materials. The petrographic examination was carried out mainly with the help of a binocular microscope. Lithologic identification of the pebble fractions was made by breaking each with a hammer. Occasionally thin-sections were made and examined for identification of a particular rock. Lithologic Terms and Classification Lithologic terminology and classification was standardized for this study (Table 2). The writer's earlier experience w ith the Highway Department in p e t r o ­ g raphic analysis of glacial gravels associated with the Lake Michigan lobe and the Saginaw lobe, helped to simplify the lithologic terminology and classification for this study. In Table 2, an initial classification I was established for a coarse fraction, w h i ch included the 18 lithologic categories expected in the gravels of this area. Later on a more simplified but yet meaningful new classification II was adopted for faster and more TABLE 2 LITHOLOGIC TERMINOLOGY AND CLASSIFICATION COARSE FRACTION Classification I (Initial) Phaneritic Acid Igneous Phaneritic Intermediate Igneous Phaneritic Basic Igneous Micro-Phaneritic Igneous Aphanitic Acid Igneous Aphanitic Basic Igneous Foliated Metamorphic Non-Foliated Metamorphic Dolomite Dolomitic Limestone Limestone Sandstone Siltstone Shale Clay Ironstone Concretions Porous Chert Dense Chert Others* FINE FRACTION Classification II (Simplified) Acid Igneous Basic Igneous Foliated Metamorphic Non-Foliated Metamorphic Carbonate Sandstone Siltstone and Shale Clay Ironstone Concretions Porous Chert Dense Chert Others* Classification III Acid Igneous Basic Igneous Metamorphic Carbonate Chert Clastic Feldspar Quartz Others* *This refers to any rock which was extremely difficult to identify because of extensive weathering or could not be placed in any of the above lithologic categories due to its rarity. 123 efficient identification of lithologies. only 11 lithologic categories. This included In this study, more specific lithologic terms, used in the earlier studies of Wingard (1969), were eliminated to avoid complicating certain glacial interpretations in the area. Classification III was designed for petrographic analysis of the fine fractions (sand s i z e ) , and in this classification only nine lithologic categories were used on the basis of expected rocks and minerals in this fra ct i on . Description of the standard lithologic terms is not given here, since they can be found described in any petrology or petrographic text or reference book or in any geological glossary. Coarse Aggregates For petrographic analysis of coarse aggregates, two types of samples, channel samples, and spot samples, were used. A detailed five-size fraction analysis was used for channel samples 1 through 18, and a pebble volume analysis was used for the rest of the spot samples. Five-Size F r a c t i o n .— Coarse material used for the mechanical analysis was also taken for petrographic analysis. The following five-size fractions were selected for petrographic analysis: 124 Size 1 + 1 inch Size 2 1 - 3/4 inch Size 3 3/4 - 1/2 inch Size 4 1/2 - 3/8 inch Size 5 3/8 - 3/16 inch The above size fractions were quartered, whenever possible, to 200 pebbles each. All five-size fractions of 18 channel samples yielded 200 pebbles each, with the exception of greater than 1 inch (Size 1) fractions of 3 samples, which yielded a few less than 200 pebbles; for the sake of uni­ formity of the data these were still used for the analysis. A total of about 1,000 pebbles were analyzed per sample. This brings the total figure to 17,860 pebbles analyzed for 18 channel samples. Lithologic classification I (Table 2) was used for this five-size fraction analysis of 18 gravel samples. Data were recorded in code numbers to speed up the pro­ cedure. Percentages of each lithology present in each fraction were calculated. Then these data were regrouped into the following 11 lithologic categories: others, igneous and foliated metamorphic, non-foliated metamorphic, dolomite, dolomitic limestone, limestone, sandstone, siltstone and shale, clay ironstone concretions, porous chert, and dense chert. This breakdown was made to study the lithologic distribution according to variations in size of the material. Using the whole data of 18 channel 125 samples, mean percentages of each lithology samples) in each size were claculated. (mean of 18 These are repre­ sented graphically in Figure 27. From a plot in Figure 27, it can be said in general that all lithologies except clay ironstone concretions, porous chert, and dense chert, show more or less similar distribution in all five sizes. Petrographic analysis of sizes 2 and 3 can give average value of lithologic distri­ bution in a particular deposit. Clay ironstone concretions seem to decrease in number with the decrease in size of the material and this could be due to the weak physical nature of these concretions. The number of porous and dense cherts seems to increase with the decrease in the size of the material- This may be due to the deleterious nature of chert, which can expedite mechanical breakdown compared to other rocks. Limestones show slight increase in number with decreases in particle size. This could be also due to mechanical breakdown. The petrographic data for 18 channel samples were averaged for the whole sample and again regrouped into classification XI sample data. (Table 2) for correlating with spot These data are given in Table 3 (in the A p pendix). Pebble V o l u m e .— A pebble volume analysis was used for 23 spot samples (No. 23 to 45) of coarse material collected in Kalamazoo County. This method has been MEA N - PERCENT IGNEOUS & OTHERS Figure 27. FOLIATED ME TAMORPHIC Relationship between material sizes and lithologic distribution. 2 NON-FOLIATED METAMORPHIC DOLOMITE — DOLOMITIC LIMESTONE LIMESTONE — SANDSTONE — O o SILTSTONE 1 SHALE CLAY IRONSTONE CONCRETIONS POROUS CHERT DENSE CHERT 9ZT 127 stressed by Ehrlich and David (1968) in their study of glacio-fluvial sediments, and is also described and used by Wingard (1969) in the study of drift materials carried out in the Research Laboratory, Michigan Department of State Highways. This method gives lithologic percentage by volume rather than by number of pebbles. The pebble volume procedure needs to be briefly described here. Gravel samples in 1/2 to 1 inch sizes were collected in the field and washed to free them from clay or fine material in the samples. Then they were quartered until approximately a 2 liter fraction remained. Pebbles were packed by agitating in a 2 liter waxed strong cardboard cylinder mold to obtain the approximate initial volume. Pebbles from a 2 liter volume were petrographically analyzed into 11 different lithologic categories of classi­ fication II (Table 2). Then the volume of each lithologic fraction was determined by weighing, in each category, in grams, all pebbles in air and then in water. ence between the two weights volume in cubic centimeters. (in grams) The d i ff er ­ is equal to the From this volume percentage by volume for each lithology was determined. Approximately 12,000 pebbles were analyzed using this method. Lithologic data collected using 1/2 to 1 inch sized fractions are believed to be representative of all size grades of coarse aggregate. by Figure 27. This fact is revealed This assumption is supported by Figure 27 128 in which volumes of sizes 2 and 3 Cl/2 to 1 inch) are shown as an average of all five sizes. Anderson (1957) believed that the 1/2 to 1 inch size grade contains the greatest variety of rock types, and hence he also used this size for pebble counts. Fine Aggregates In Kalamazoo County, more than 100 samples were collected for the sand analysis using the channel, and auger sampling methods. spot, Of these, 88 samples were subjected to petrographic and mechanical analyses. One-Size Fra ct io n .— The sand fraction of 1 to 2 mm. (ASTM No. 18-10) investigated. size from each sample was petrographically This size grade was chosen because of the large variety of lithologies, which with the aid of tweezers can be rather accurately identified under a binocular microscope. The fractions were coned and quartered until reduced to about 350 grains. grains were examined. Only 300 Sand grains were classified into nine different lithologic and mineralogic categories. These are listed in Table 2 under Classification III. A total of about 27,000 sand grains were analyzed and the data are tabulated in Table 6 (in the Appendix). The sand analysis was carried out to abet the interpretations of glacial history, but because of hetero­ geneity this did not provide as much information as did the coarse fraction. 129 Heavy Minerals The heavy mineral analysis can be used as an additional tool for differentiating various drift sheets. It is well established that the heavy minerals in sand fractions are m o s t l y concentrated in its finer grades, and that they can be separated from the lighter minerals by using heavy liquids of different density, and then identified under a petrographic microscope. A pilot study of heavy minerals was therefore made from a -27 0 mesh fraction of channel samples numbered 1 to 18. separated using acetylene tetrabromide 2 .96 at 20®C). These were (specific gravity The results show that 1 to 5 per cent heavy minerals by weights are present in -270 mesh fractions of all samples. Comparison of Channel and Pebble Volume Techniques Both channel and pebble volume methods were used, the channel technique for engineering types of samples and pebble volumes for lithologic samples. Each technique has its advantages and disadvantages, as noted below. The channel sample subjected to mechanical analy­ sis gives more detailed engineering type of information, especially regarding the particle size distribution in the deposit. The pebble volume sample cannot provide this valuable information because of its small volume and single size grade. The petrographic data on channel samples give a more detailed lithologic distribution 130 within each size grade, whereas the pebble volume sample data are derived from one size grade only, and so does not represent an average of the whole deposit. Similarly, other engineering information such as physical strength and chemical reactivity can be obtained for the whole deposit from a channel sample, whereas these character­ istics can be defined only for the 1/2 to 1 inch size fraction of the whole deposit from a pebble volume sample. The channel sample technique is more lengthy and more expensive, and most of the time it requires new or fresh exposure to cut the cost of operation. In contrast the pebble volume technique is quick and less expensive, and it does not require many efforts to obtain a fresh sample. Lastly, the channel sample method gives more detailed information and the pebble volume technique gives more general information. Determination of Engineering Quality The two most important properties affecting the engineering quality of glacial materials are physical strength and chemical reactivity. Glacial aggregates are usually used in concrete for construction purposes, so determination of these two properties, along with petro­ graphic analysis of coarse aggregates, is most desirable. Economic effects of these properties are discussed in Chapter XII. 131 The physical strength was determined by estimating how strong the blow of a hammer was required to break a rock particle. used: Two categories of physical strength were i.e., simply either strong or weak. Extensive weathering affects the physical strength of some rocks; also, these rocks may have lower density and rough surface texture or smooth clayey texture. Some of the weathered or altered mineral products may be chemically reactive with cement, causing a premature failure of concrete. The chemical reactivity of each particle was determined after its lithological composition was defined, the latter, of course, being directly related to the chemistry of each mineral present. react Rocks with free silica (alkali-silica reaction) with hydrating alkali cement. Also some dolomitic limestones or calcareous dolomites are known to create alkali-carbonate reactions, causing failures in concrete. Therefore, the reactive and non-reactive rocks were identified and recorded for further analysis. These two key properties were determined in samples number 1 to 18 in Kalamazoo County. discussed in Chapter XII. The resulting data are CHAPTER X LITHOLOGIC DISTRIBUTION OF AGGREGATES What started as an apparently simple study to evaluate gravel deposits.in Kalamazoo County with respect to their suitability for concrete aggregates soon became revealed as a very complex problem. This complexity has been revealed by the recognition of out-of—phase fluctu­ ations! relationships between the Lake Michigan lobe and the Saginaw lobe (see Chapter IV) , and by the detailed picture of the distribution of gravel lithologies in southwestern Michigan shown by isopleth maps (Figs. 29-37) . Initial data gathered just from Kalamazoo County are insufficient to dr a w any firm conclusions from regard­ ing provenance and lithologic distribution of glacial materials in the county. The main reason for this in­ adequacy is that sample locations in the county are not properly distributed throughout the county. This is directly related to the lack of good exposures Chapter III), some of which, of course, are more dense in certain areas attempts, (see (Fig, 28). After several inconclusive the writer decided to compare petrographic data from Kalamazoo County with similar types of data from 132 133 surrounding counties in southwestern Michigan. The data from surrounding counties are cited in the earlier pilot study by Wingard (1971), of aggregate sources in Michigan. Usable parts of these data are rearranged and 5 in the Appendix) (see Tables 3 to match the w r i t e r ’s data from Kalamazoo County. Lithologic Map Interpretation and Provenance Petrographic data from 130 sample locations <45 in Kalrmazoo County and 8 5 in surrounding counties) are utilized for this interpretation. Each sample location is indicated by a symbol depicting associated glacial feature. The majority of locations lie on moraines, out- wash plains, and moraine-outwash contacts. Bedrock o u t ­ crop locations and their lithologies are also shown on the map. The map in Figure 2 8 shows only gravel sample locations and their numbers, as given in Tables 3 and 5 (in the A p p e n d i x ) . All petrographic data are regrouped into the following nine broad lithologic categories, each c o n s i d e r ­ ing common occurrence, source area, local bedrock lith— ology, bedrock configuration, and glacial lobe movements. Minor amounts of rare lithologies as a group are e l i mi ­ nated. For more details one may refer to Tables 3 and 5 (in the A p p e n d i x ) . 134 Igneous (Acid + Basic) Metamorphics (Foliated + N o n — foliated) Crystallines (Igneous + Metamorphics) Cherts Carbonates and Cherts Sandstones Siltstones and Shales Clay Ironstone Concretions elastics (Sandstone + Siltstone + Shale + C .I . C o n c r e ti on s) Precambrian Fraction (Possible S o u r c e : Canadian Shield Area) Paleozoic Fraction > (Possible S o u r c e : Michigan Basin Area) / Igneous and metamorphics are grouped together into broader and more general categories of crystallines, for the purpose of observing the reflection of gross lithology from the same source areas. grouped together, Carbonates and cherts are since cherts are usually associated with carbonates, which means that they have the same source. Siltstones and shales are grouped together, as they are present in minor amounts and seem to have the same source. Sandstones, siltstones, shales, and clay ironstone c o n ­ cretions are grouped into the general category of elastics, because in certain areas, they represent local bedrock lithologies and seem to show increased amounts of mixing and dilution of other lithologies due to increased erosion and the glacial plucking of bedrock. For a simple and clearer interpretation, percent lithologies for each lithologic group are plotted on nine different maps (Figs. develop a pattern. 29-37) , and isopleths are drawn to These patterns show glacial and LCGCHC i M P U h M A r m AM O M U A ttO GUICttL f U T t f t l • T*U T»« - Tvl p^mhcq*r*ct ■ Q V T ^P * CflHWCl Q T U M H -m tlD C il * 0UT«U» H.MM-kJHt lift A M L 'T H O L W r T -- + 135 11* -4 GRAVEL SAMPLE LOCATIONS SOUTHWESTERN MICHIGAN k iwautwvnitoii% ■ 4<* » » i « it « * i « nr • IT * a n * nil# h 14w «uw m i ail* a 10 Figure 29. Igneous rock content in Southwestern Michigan. 137 > *mw^ii 138 Chapter IV. The Lake Michigan lobe deposits in general show less than 20 per cent igneous rock content, w ith some exceptions. An isopleth of 15 per cent in Calhoun and Eaton counties can be explained by the increased influx of local bedrock lithologies. Metamorphic Rock Content The metamorphic rock content pattern also, (Fig. 30) in general shows higher percentages in the eastern part of the study area. The 10 per cent isopleth passing through the western part of Kalamazoo County seems to be the arbitrary line separating deposits of the two lobes. The Lake Michigan lobe deposits in general contains less than 10 per cent metamorphic rocks, except at a very few locations where they are higher than 10 per cent but less than 15 per cent. According to Anderson (1957), the metamorphic rock content of the Saginaw lobe is higher than the Lake Michigan lobe due to an influx of quartzite pebbles. This fact was also corroborated by the writer in his petrographic analysis. Crystalline Rock Content In the study area (Fig. 31), the Saginaw lobe deposits generally contain more than 30 per cent crystal­ line rocks, and in certain areas it is higher than 40 per cent. hand, The Lake Michigan lobe deposits, on the other show crystalline rock content to be less than 3 0 L E GE * © tM ^ L E L K A T m « • A U K U H B GLACIAL flA T U M A iflMf 8 Kl. PLAM f ftrlwu* n.«* 6 0 fc , ”■ * - Tn A.WCCMTM1 -(utwimm cmuci - l w u « d m m m h u c c n u t contact EJ t n m w - l u h m b o« owowtfi m m 1 !0 -A. Z 9 QuTmtofLwiyWE a(B m mmmt*w i CC"T«T J/ 11T,li *I '”■'1 nf*l tin / W '/ w it 1 TT.H" i’; _ _ u i „ _____i H i d >4*0 / t l 139 GRAVEL LITHOLOGY OF SOUTHWESTERN MICHIGAN METAMORRWC ROCK CONTENT f FDLlATEIMtfM- FOL lA ftO l I M K I T H H fllttW L A X Figure 30, Metamorphic rock content in Southwestern Michigan, L E GC N O f t M r f l t LOCATION V MOOCMTC 0 G U C M . O A T U M I TU. ftJMi • WW h*w A U M IW IV O W IM IM ) D MOMMt-TILL Tl*H C W W l O « W t - OgTMMh.Mt CONTACT A now*-lw< *»o* eewwci contact B T IL • O U T W M N W - A I W - L N U t o a* PN**nrt P I t o 00 m u i a f i t W I W l R l |« l l | « ■ |T W «>•« IIS* n *49 * !»« R if* * " « m o w M W t i f t N T * NftW ft * W Bj M .N > ^-^-tdlfer'iHa' if ViU >J j^M-L A' ■V.rMM' ' Figure 33. Carbonate and Chert content in Southwestern Michigan. mplitm mnwi. *% 145 the carbonate and chert content of the Lake Michigan lobe sediments is above 6 0 per cent, and in some areas, p r e ­ sumably near the Devonian carbonate source above 7 0 per cent. (Fig. 19), is Values below 60 per cent could be b e ­ cause of the dilution from the increased amount of elastics (Fig. 37). The carbonate and chert content of the Saginaw lobe sediments is in general less than 60 per cent, and in some areas it is below 50 per cent for the same reason given in the case of the Lake M ichigan lobe (Plate X) . Values above 60 per cent, northeast of Kalamazoo County are probably due to bedrock erosion of cherty Bayport limestone of upper Mississippian age, and some carbonates of Pennsylvanian age. The writer has observed slightly higher dolomite content in the Lake Michigan lobe s e d i ­ ments than the Saginaw lobe sediments. Dolomite m a y have come from cherty dolomitic lenses in the Coldwater shale; or from any other source in the Lake Michigan basin. The 60 per cent isopleth passing through western Kalamazoo County seems to be the arbitrary lithologic interlobate line. Increased values in the southeastern part of Branch County may again be due to the contamination from the Erie lobe sediments. Sandstone Content The sandstone content map (Fig. 34) does not show any clear pattern distinguishing the Lake Michigan lobe sediments from the Saginaw lobe sediments. In general a HA1 t IN ■Kfl* 'iffl (I)w 146 1* 4 1* GRAVEL LITHOLOGY SOUTHWESTERN MICHIGAN Figure 34. Sandstone content in Southwestern Michigan. 147 high concentration of sandstone is clearly observed near sandstone outcrops and thin drift areas. Lower Missis- sippian and Pennsylvanian sandstone formations are mainly responsible for the sandstone content of this area. The pattern in Eaton and Calhoun counties shows a clear relationship between the source area and dispersal by the glacial flow. Siltstone and Shale Content Siltstones and shales (Fig. 35) are more uni­ formly distributed in the Saginaw lobe sediments. These show spotty distribution in the Lake Michigan lobe sedi­ ments/ with very high values in isolated areas. The pattern showing high values in the Calhoun County area more or less matches with that of the chert content (Fig. 32) in the same area indicating local provenance and similar dispersal by glacial flow from the northeast. Most siltstones and shales of the Saginaw lobe are pre­ sumably derived from the underlying Coldwater formation. Extremely high values in southwestern Kalamazoo County can be explained by local influx of siltstone and shale derived from the Coldwater formation, by glacial plucking of pre-glacial valley floors in Van Buren County, i.e., by Lake Michigan ice. Glacial plucking can be sus­ pected because of the isolated and disconnected bedrock lows in this area (Fig. 21). High siltstone and shale content in Berrien and Cass counties may be due to the *r mi m 148 'a GRAVEL LfTHOLOGY SOUTHWESTERN MICHIGAN SILTSTONE AND SHALE CONTENT o", •• • * 4— Ham ill* Mi U.LL ttit* R14V Figure 35, »ifW Siltstone and Shale content in Southwestern Michigan, 149 erosion and glacial plucking of the Ellsworth-Antrim shales by Lake Michigan ice, A 2 per cent isopleth in western Kalamazoo County seems to indicate the arbitrary lithologic interlobate line. Clay Ironstone Concretion Content The map in Figure 36 shows mostly less than a 2 per cent clay ironstone concretion content in the Saginaw lobe sediments, while values of clay ironstone concretions in the Lake Michigan lobe sediments show extremely high concentrations in isolated areas such as southwestern Kalamazoo County. This again can be explained by glacial plucking and abrasion of the source rock. It is sug — gested that most of these concretions are derived from the Coldwater formation, with some from the Lower Marshall formation, and a few from other formations. Antrim shales are known to contain these concretions, but low values in Berrien County do not seem to correlate with the high values of siltstone and shale content same county. (Fig. 35) in the The 2 per cent isopleth passing through Kalamazoo County seems to indicate, once more, the arbitrary lithologic interlobate line. Once again it is brought to the attention of the reader that, the 1.8 per cent clay ironstone content of a sample, from the north­ ern part of the Kendall moraine in the extreme northeastern corner of Van Buren County, correlates with the Saginaw lobe sediments. £ ICCCftC im # l i io c a TO n A U o c u m « la cm l f ia t u u c i * |0M« ft fill fut* ft oinift** a.j« 6 L*KHfrCft0»W*a*fl □ H P * * * - Till *CM* C«T*tT 0 IfltoM ' O u T m f H A*AM CA*t«CT 4 «M4 • im{ HP m P>*^ ni m contact 0 TL i •L a w - u w I KO C* t* * m Q l com cT 4 gutwuHfvwi'Viwi m h giwuiet w s ttxTKi i ijTm / i( \\V1>ai-^#l S?*| i t 150 GRAVEL LITHOLOGY OF SOUTHWESTERN MICHIGAN e a A ', s (. CLAY IRONSTONE CONCRETION CONTENT ' * 4 »£1W V Figure 36. Clay Ironstone Concretion content in Southwestern Michigan. IMflfTH MTU** t\ m « t M M O U T H M T llfM L i % Figure 37. C lastic rock content in Southwestern Michigan, CHAPTER XI ECONOMIC CONSIDERATIONS The role of the geologist is a very essential one in the sand and gravel industry, which is considered the largest (tonnage-wise) mining industry in the world. The sand and gravel industry is expanding as a n e w highway program and other construction projects are increased. In 1969, Michigan alone produced 58,092,000 short tons of sand and gravel valued at $58,968,000, nationally in production. thus ranking second Most of this tonnage was mined in areas adjacent to the larger metropolitan areas of the state. About 1.6 per cent of the total sand and gravel output was processed in Kalamazoo County. In 1969 this county produced 941,000 short tons worth about $1,163,000. As sand and gravel production in Mi chigan increases every year, it is a fact that presently known gravel sources are depleting rapidly. There is a need for locating additional sand and gravel resources for servic­ ing future highway construction and planning future building construction. 153 154 Sand and Gravel Economics In recent: years, depletion of material and the new zoning laws which have been involved because of increasing environmental concerns, has made the industry ask the geologist for help in locating suitable new sand and gravel resources. The average layman thinks that sand and gravel deposits of glacial origin are everywhere in Michigan and that the supply is unlimited. But he is not aware of the fact that these deposits have to m e e t certain specifications in terms of gradation and composition. In fact, an economically feasible sand and gravel deposit must meet specific physical and chemical characteristics. the deposit does not meet these requirements, If the quality of that deposit can be upgraded to the required standard by using different beneficiation methods. Note is made of all these concerns in this chapter. Industry and Cost In 1969 there were eight sand and gravel producers operating in Kalamazoo County. Among these, the American Aggregate Corporation was the principal producer. American Aggregate Corporation's sand and gravel pit is the largest in the county. It is located in Cooper Township along the west bank of the Kalamazoo River, about one mile east of Cooper Center. Al though sand and gravel can be produced throughout the county, the low value and high transpor­ tation cost have demanded that the production be 155 concentrated near the city of Kalamazoo and major highways (Fig. 38). Presently, processed gravel in Kalamazoo County costs slightly more than a dollar per short ton on the average. This cost may increase in the near future when all useable sand and gravel sources near the m e t ro ­ politan area and major highways are depleted. Then it will become necessary to transport aggregates from the rural and suburban areas into metropolitan centers. Benef iciation In recent years, has rapidly increased, the demand for premium aggregates because of the rigid standards of quality control and increasing technology in the field of concrete mixing. Deposits of inferior material can be upgraded by several beneficiation methods. Detailed d i s ­ cussion of specific beneficiation methods is, of course, beyond the scope of the present study. directed, Wingard however, to Lenhart (1969) (1962), The reader is Kneller (1964), and for a more comprehensive discussion of the sand and gravel beneficiation methods, problems of pro­ cessing specific rock types, and specification standards set by different agencies for concrete aggregates. Lenhart discussed the Heavy Media Separation (HMS) method in detail along with general discussion of the sand and gravel industry. Kneller describes the following six commonly used beneficiation methods: washing, and crushing; (2) jigging; (1) screening, (3) elastic O0(D[E[E@00 W* (f TIN TIN aM m or w n M o m « l ll« TI» T tl 156 // T I I ■NIBlJ"A it a il*T«V J ’** 4f* GRAVEL RESOURCES SOUTHWESTERN MICHGAN t.. *-i t /( m T il [ Figure 38. Gravel resou rces of Southwestern Michigan. 157 fractionation grators; (bounce m o d ul us )? (4) cage mill disinte­ (5) heavy media separation (HMS); and (6) the one-two-punch system which combines the elastic fraction­ ation and the heavy media separation methods. Wingard has very briefly discussed the HMS process and problems of upgrading some deleterious gravels in some areas specifi­ cally in southern lower Michigan. The Heavy Media Separation (HMS) or the so-called "Sink-Float" process, using heavy media of specific gravity between 2.50 and 2.60, usually produces the premium aggre­ gates required by the Michigan Department of State High­ ways. The disadvantage of the HMS method is that it will not eliminate high-gravity deleterious (undesirable) material such as clay ironstone concretions. It is an expensive method but certainly the most suitable process for production of superior quality material. Potential Building Aggregates With increasing needs of the large sand and gravel industry, it has become necessary for a geologist to out­ line areas of potential building aggregates. To do this, it is necessary to study the locations of abandoned and presently operating sand and gravel pits. approach used in the present study area. made on the map (Fig. 38), This is the Attempts are "Gravel Resources of South­ western Michigan," to outline the probable areas of future gravel resources. These areas are outlined, taking into 158 consideration the gravel pit location pattern and assuming that coarse gravel (required for the highway construction) can most likely be found near the transitional boundary between moraine and outwash deposits. This map is just a guide for prospecting for future sand and gravel deposits. It should be used with great caution and, of course, also with a detailed geologic study of the location. It may prove to be unsatisfactory in some areas. Gravel Pit Locations Gravel pit locations w h i ch are shown on the gravel resources map are taken from the Michigan Department of State Highways 'gravel pit inventory (1966). These include all abandoned and operating pits from which the MDSH p u r ­ chased aggregates through the end of 1966. County, In Kalamazoo some additional pits are shown which vere d i s ­ covered and sampled at the time of field work for this study. Highways, Population, and Gravel Pit Density Relations The gravel resources m a p shows in general that the density of gravel pit locations is higher near the p o p u ­ lation centers (cities and towns) creases away from them. and highways, and d e ­ This relationship exists because of one or both of the following factors: (1) low values and high hauling costs demanded that production be c o n ­ centrated near the major population centers and highways; 159 and (2) unfavorable and unidentifiable glacio-morphological conditions (e.g., transitional zones) which usually pro­ duce gravel reserves but not easily found to date. With rapid depletion of sand and gravel reserves and stockpiles near cities, towns, and present highway systems, it will become necessary to explore these potential areas more fully for sand and gravel, even though the costs will become higher Ground Water in Kalamazoo County The major supplies of ground water in Kalamazoo County comes from aquifers in the glacial drift. Minor supplies come from wells penetrating the Marshall sand­ stone (Fig. 19) in the northeastern part of the county. The Coldwater shale which underlies the glacial sediments throughout the county, and other Paleozoic rocks that underlie the Coldwater formation, have little or no potential for future ground water development. Glacial sediments are the source of water in most of the wells in the county, and these have considerable potential for future d e v e l o p m e n t . Ibrahim (1970) pointed out that the water-saturated glacial sediment thickness is small where the drift thick­ ness is low and hence in such situations the possibility of developing suitable aquifers is minimal. He also noted that areas of large thickness in glacial sediments are more favorable for locating aquifers of appreciable thickness 160 and suitable yield. Further, Ibrahim points out that bedrock channels are especially favorable for locating ground water aquifers, also discussing more specific areas, including bedrock channels, possible quite suitable for high yields of ground w a t e r . It has also been noted by Deutsch, Vanlier, and Grioux (1960) that permeable outwash and channel deposits are good sources of water for wells of large capacity. Higher permeability sand and gra ve l beds between lower permeability till in moraines locally yield larger supplies of fresh water. This situation sometimes develops more than one aquifer. lower) 1956; are reported Ibrahim, county, In general, two aquifers (upper and (Deutsch et al^. , 1960; Reed et a l . , 1970; Allen, 1972} in some areas of the especially in the city of Kalamazoo and vicinity. The thickness of these two aquifers varies from place to place, and they are separated by about 3 0 to 4 0 feet of less permeable material. In this area, several water wells are located along or near the Kalamazoo River and other s t r e a m s , so that pumping of wells in such an area will induce the migration of wa ter Allen, 1972) (Travis, 1966, and from the stream toward the wells. In this case, polluted rivers and streams can pollute the ground water in this area. The water s of the Kalamazoo River, whi ch is the largest surface drainage in Kalamazoo County, and the Portage Creek are alre ad y polluted, so there is 161 urgent: need to clean up these rivers and creeks and stop discharging industrial and other wastes into them. Subsurface and ground w a t e r information must be considered before excavating for future sand an d gravel deposits to be used in planning for future highways. It is already clear that much care mu s t be taken not to dis tu r b natural aquifer conditions existing in the glacial sed intents. Environmental Application A map (Fig. 39) of the geologic environment for solid waste disposal in Kalamazoo County was prepared by using the surface and subsurface this study. information ga thered for Mo s t of the subsurface information comes from water well logs and oil and gas logs. About 230 well logs were used, and their locations are plotted on the map. Three types of areas are outlined: satisfactory, less satisfactory, and unsatisfactory for solid waste disposal and for planning other land uses. An explanation for the delineated areas is g iven on the map, w h i c h should be consulted before locating sanitary landfill sites. The present guidelines developed by the Illinois S tate G e o ­ logical Survey, and followed by the Michigan Geological Survey in cooperation with the Department of Public Health, require a minimum of 25 to 30 feet of clay or relatively impermeable material between the base of a landfill and the shallowest underlying w a t e r —yielding aquifer. With mWACTQty hfah*4m« b a tx «ait 4 P H M . «lt*' Ik « I • M p t l M * . C l M l f l p*Pd t a w lfa r t w a i n vf tim f c a tta d i * 4 arri p a.» 1 wiih m ----- A f M » l K ^ tl*p > T i l l . U h I I ^ ■ » ! » ! w l n i (p m k afayba * « p a d i« id » > c l» rf iiiiii< h !y M w p d i itw cfcy *d>Ja cwd'FiW* ------ * 1 ^1 iJ li ■ ■ j | Iir’l I* ‘ j Aii^iilBpfr C t n d i t w t a t Ifca M T i t l r i f a ia i m n Q l y l a n p i m M . E3 * □' LEM S A llg A C T Q K Y h * t* r i« c 4 » a l ^ k t w ^ . 1 fa r m 4 U mmtm d ^ a i L vflfclacaf «>«*ptfaw. G w w alfy la * r i m 2$ fact a# •* pam aabfa d a y o w l y i n ( lh* wafai arf4a, and infam ii^ lad wffh feyan 9# fUt, w d , dnd y e v a l. G lacial * i f r nfaarlaJ if cM plM m i m iw □ J-f' •* ' *.\' "T '..>’ li £ r * ■\ •■- f CH «U . » t « | r~ f ^z in a n d M r w c lu n l * a * a f l y w * d l l m m tla a H y , A dafailad m h ^ w im w if a f ia n « f H y+ a^ ofagic candiriafit ■m ' ha catriad aut far a n la a rta n of th* »i**. All y H U p m a i * fidra M n t e a w f la avoid # o u n d * ie r eaw iafaatiaii, i • 5 □ yr L N S A T B fA C T O tY w b u H a c a p a l a t e • m i i a w t t t m m l * w f a dafaaali * 1 * fatal • ■ y f o i a , ‘T i m a l l j » i ‘i iti i n i a i a^ d fw ■ft p a a ta , p a n a ^ l i , aad kftatilfad m 4 and p a**l «f glacial ant* m * w ^ draina^ c h m b . Lacolly **n Im of faa y m g U * cfay and tilt mm inimtadriad r»iriv wall p a v a L T h n t glacial o u t m * *ifar< I location, W k a tf a law rtm> 23 f m a* clay a m 1 facatfan, indiaafaa m tr iy a ta ttf lad p a * n fa 162 E 4 1 • ■Ad' "■■...£.v ■FTTQ^JVTai tp GEOLOGIC ENVIRONMENT FOR SOLID WASTE DISPOSAL S. .... O IN K A L A MA Z O O A.±&6:-LA.— + ■ < ■ *! »T J0«c*t MICH IGA N Figure 39. Geologic environment for solid w aste disposal in Kalamazoo County, Michigan. C O U N T Y 163 this criterion kept in mind, the m a p in Figure 39 was prepared. This map also is but a guide for giving preferences to different areas for quick location of a proper landfill site. CHAPTER XII AGGREGATE SUITABILITY FOR ENGINEERING USAGE Variations in lithologic composition and distri­ bution of glacial materials, which are direct products of the geologic history of the area, are discussed in Chapter X. Their economic considerations are noted in Chapter XI. Discussion in the present chapter is brief, and relevant to the few important properties of aggregates determined in this study affecting their performance in concrete. Several other factors relating to aggregate suita­ bility and the engineering test results are discussed by Wingard (196 9) in his work, carried out in the Research Laboratory Division of the Michigan Department of State Highways prior to the present study. The reader is directed to Wingard*s work for more details. There are several other good sources of information regarding the application of petrography and other geologic information in the evaluation, selection, processing, and use of aggregates in concrete and elsewhere. 164 A few of these 165 are listed, along with other related references, in the reference section at the end of this paper. Properties and Performance of Aggregates In the world of today, Portland cement concrete is still a construction material of fundamental importance and unique versatility. The design and control of concrete many times depends on the physical, chemical, logical properties of the materials used. and litho- Aggregates generally occupy 60 to 8 0 per cent of the volume of c o n ­ crete, and also influence mix proportions and economy. They must conform to certain requirements for certain types of jobs. There are many causes of inferior quality or failure of concrete, of which two are given special attention in this study and discussed briefly as follows. Physical Strength and Chemical Reactivity Physically weak and chemically reactive particles can lead to the deterioration or failure of concrete, whereas an increased number of physically sound and chemically nonreactive rocks can strengthen the concrete. The effects of these properties are also discussed by Wingard. Methods for determining these two properties are outlined in Chapter IX of the present report. Total percentages of the physically strong and chemically nonreactive particles for each channel sample (1 through 18) in Kalamazoo County were determined. 166 Values for each sample location are shown in Figures 40 and 41. The average mean value for all 18 samples was determined as shown in these figures and an arbitrary line separating the above-average from the below-average values has been drawn. It is obvious from these figures that the arbitrary lines coincide in general with arbitrary lithologic interlobate lines on the lithologic maps discussed in Chapter X, i.e., note the maps in Figures 29 to 37. In both of the Figures 40 and 41, the values which are aboveaverage appear to correlate with the Saginaw lobe s edi­ ments, presumably because of the comparatively high crystalline rock content in that lobe. Values which are below-average appear to correlate with the Michigan lobe sediments, presumably because of the comparatively high clastic rock content in that lobe. This observation reveals that even engineering properties of aggregates are directly related to the lithologic distribution (because of different provenance) of course, also their provenance. exploration purposes, of drift materials and For planning and attention is, of course, drawn to the solid lines in these figures and their positions w ith respect to the township borders for the purpose of explicit location. Deleterious Aggregates and Their Desirability In Concrete Physically unsound and/or chemically reactive particles are considered deleterious (undesirable) in N ! ! ALLEGAN CO RII_W. _ R _ 1 2 W ___ RIOW. BAPRY CO. R.9. W. COOPER ALLEGAN CO R. 12 W, R. II W. BARRY CO RIOW. R.9W, r aosst COOPER I ROSS •84.5 •8 8 7 TIS TIS. 76.4» 799«> 868* _______\ _ 3 _?U)8_ 3fc5 _ 4 ___________ 89^83 •6 9 4 88.2* |*87 T2S. 847 I •89.1 T2S. •8 5 7 OSKTEMO_______ ,KA(._AUZOO_ ' A •8 4 9 CHARLESTON •89.1 OSHTEUO j COUSTOCK_ _jCHARLESTON KALAMAZOO 83 5 AGE I^'^erage) T3S. I T.4S. co »6Q7 oi I PRAIRIE RONDC t u a s SCHOOLCRAFT * |RRAOV _ CALHOUN UI . PAVILION 8 z u T.4S. %| (D Z < _ ___ j_PORTACE_______ I___^_PAV]L1 ON i CLIMAX CO. pEXAS__ / ■83.3 I I I > IPRAIRIE RQNOE A / |SCHOOLCRAFT y i i IRRAOV iWAAESHMA ST. JOSEPH CO. ST. JOSEPH CO. (Above-iverage values relate to the Saginaw lobe sediments and below-average values relate to the Lake Michigan lobe sediments. Average value: 83.4). (Above-average value* relate to the Saginaw lobe sediments and below-average values relate to the Lake Michigan lobe sediments. Average value: 89.0). Figure 40. Percent distribution of Physically Strong particles in near surface drift of Kalamazoo County, Michigan. Figure 41. Percent distribution of Chemically Non­ reactive particles in near surface drift of Kalamazoo County, Michigan. CALHOUN T.3S. 168 concrete. Usually weak, friable, or weathered and lami­ nated aggregate particles are physically unsound, and hence not desirable. stones, Especially friable sandstone, silt- shales, clay ironstone concretions, weathered cherts, leached limestones, and highly weathered crystal­ lines are physically unsound; rocks with free amorphous silica and iron oxide, like porous cherts, cherty or siliceous limestones, siliceous shales, phyllites, and other minor rock varieties are chemically reactive. All above listed rocks should be avoided as much as possible if one is to assure the best quality of c o n ­ crete . CONCLUSIONS, ACADEMIC AND ECONOMIC 1. Detailed glacial mapping of an area, preferably as large as a county, is essential for the systematic evaluation of sand and gravel deposits and for future highway planning. Also, it helps a great deal in the groundwater studies. 2. T h e channel sampling method, even though more lengthy and tedious, gives a representative sample of glacial sediments and reveals more valuable information. The pebble volume is quick and more economical, but its applications are limited, and it can be only used for a broad scale reconnais­ sance study of the large areas. 3. On the basis of r o c k - s t ra ti gr ap hy , morpho-stratigraphy, time—s t r a t i gr ap hy , and soil— stratigraphy a viable glacial history of the area is worked out. It is suggested that at the Cary time, the terminal behaviors of the Lake Michigan lobe and the Saginaw lobe were out-of—phase with each other. 169 170 4. Field evidences and gravel lithologies indicate that the Saginaw lobe ice covered Kalamazoo County first, and after it started retreating, Michigan lobe ice advanced, the Lake pushing the material eastward and overriding its own bold Kalamazoo moraine along with the Kendall and the Alamo moraines built earlier by the Saginaw ice. This eastward pushing produced several weak and parallel moraines including the Tekonsha in eastern Kalamazoo County. On the basis of morpho-stratigraphy and rock-stratigraphy a somewhat arbitrary interlobate line is suggested {Plate I ) . Following weak line of evidences put to­ gether strongly supports the interpretation of overriding and the placement of an interlobate line. A. These evidences are briefly reiterated: Presence of what appears to be an example of ablation till over the Kalamazoo moraine of the Lake Michigan lobe. B. Lithology of the Alamo and Kendall moraines is similar to that of the Saginaw lobe sed im en ts . C. Presence of the Precambrian jasper conglomerate and tillite lobe) (index erratics of the Saginaw in the Kalamazoo and Kendall moraines. 171 D. Presence of thin till plains over outwash plains in Cooper and Prairie Ronde townships of Kalamazoo County. E. Fluctuation of lithologic interlobate line within 4 to 6 mile zone east of the Kalamazoo moraine (see Figs. F. 29-37). Presence of weak push moraines east of the Kalamazoo moraine, and they are parallel to the moraines of the Lake Michigan lobe. They may indicate glacial surges or usually strong pulsations in the Lake Michigan lobe in conse­ quence of differing of flow-lags. G. Axes of elongated lakes in Kalamazoo County are parallel to the moraines of both lobes. H. The heads of glacial drainage, the originating point in the Tekonsha reentrant district mark the related ice margin and provide the clue as to the direction of the former ice flow. 5. In a broader sense, the correlation between sur­ face topography, drift thickness, and bedrock configuration is inversed in Kalamazoo County. This observation is illustrated by the geologic cross sections of the county. 6. In Kalamazoo County, there is a general agree­ ment between the lithologic composition of parent materials, and properties of some soil types. 172 7. Significant lithologic differences exist among the Lake Michigan lobe and the Saginaw lobe sedi­ ments; and an investigation of the relative p r o ­ portion of lithologic types appears to be the most fruitful method for exploration and evaluation of gravel resources of these two l o b e s . 8. The Precambrian lithologies play a valuable role in differentiating the Lake Michigan lobe sediments from the Saginaw lobe sediments. In general, the Precambrian lithologic content of the Saginaw lobe is higher than the Lake Mi chigan lobe in southwestern Michigan. 9. Local Paleozoic clastic lithologies display greater variations between the two lobes. fore, There­ sometimes local elastics content alone can not be used very successfully in differentiating between two lobes in southwestern Michigan. A relatively high amount of elastics in isolated areas indicates extensive bedrock erosion and plucking by the glacier ice. It also indicates a relatively close source area. 10. Regional knowledge of the glacial geology and petrographic analyses provides the basis for p r e ­ dicting regional trends of aggregate quality and potential areas of their sources. 173 11. Variations in gross lithology within each lobe in Kalamazoo County are also reflected by the regional variations in the engineering properties, such as physical strength and chemical reactivity. 12. The gross deleterious rock content of sand and gravel deposits of the Saginaw lobe is slightly less than that of the Lake Michigan lobe in south­ western Michigan. It is strongly recommended that all the deposits investigated must be beneficiated in varying degrees to meet the specifications set by the Michigan Department of State Highways and other agencies for use in concrete. The isopleth maps in Figures 28 through 37 help an investigator to recommend what beneficiation process is needed to upgrade a given deposit. SUGGESTIONS FOR FURTHER RESEARCH The writer believes that there is a place and a need for future studies of this type in the fields of highway planning and research, sand and gravel industry, ready—mixed concrete industry, asphaltic concrete industry, soil surveys, ground-water surveys, and economic resource surveys for the state and federal agencies. It is hoped that the geological approach in this research, will serve as a basic model for future detailed studies of this kind. Further information in the following areas will be helpful for future evaluation of natural aggregate sources in the state of Michigan and elsewhere. 1. This type of study is more essential in glaciated interlobate areas in Michigan or elsewhere for determining the distribution of natural aggregates. 2. Studies of the performance of deleterious aggre­ gates in concrete subjected to severe weather conditions should be carried out with varying size and composition of natural aggregates. 3. An updated and a detailed bedrock configuration map of Michigan is essential for a glacial, a 174 subsurface, an engineer. and a petroleum geologist, and for This type of m a p can be usef ul in various phases of their work. Detailed petrographic p h y s ic al and chemical properties of various r o c k s outcropping in the state should be determined to know about their possible use for highways and other construction. Closer relationships should be established between the composition of surface aggregates and engineering properties of soils. Clay content and minerology of shales and tills in the drift may be helpful to determine possible sources of clays. REFERENCES REFERENCES Allen, C. W. , 1948. Influence of mineral aggregates on the strength and durability of concrete: Symposium on Mineral Aggregate; Amer. S o c . T e s t ­ ing Mats., Spl. Tech. P u b l ., No. 83, pp. 152-59. Allen, W. B . , et a l ,, 1972. Av ailability of Water in Kalamazoo County, Southwestern Michigan; U.S. Geol. S u r v ., Water Supply paper. No. 1973 (in press). American Society for Testing Materials, 1966. Significance of tests and properties of concrete and concretemaking materials: Special Tech. Publ. 169-A. 197 0. Concrete and Mineral Aggregates: Annual Book of ASTM Standards, Part 10; Philadelphia, 62 O p p . Anderson, R. c., 1 9 5 5 . Pebble lithology of the Marselles till sheet in Northeastern Illinois: Jour. Geology, V. 63, pp. 228-243. Pebble and sand lithology of the major Wisconsin glacial lobes of the central lowland: Geol. Soc. Ame ri ca Bull., V. 68, No. 11, pp. 1415-1450. 1957. Bergquist, S. G. and MacLachlan, D. C., 19 51. Pleisto­ cene features of the Huron-Saginaw ice lobes in Michigan: Geol. Soc. America Guidebook, Detroit Meeting, Glacial field trip, 36 pp. Blanks, R. F ., 1952. Good concrete depends on good aggregate: Civil Engineering, V. 122, No. 9, pp. 6 51-55. Chamberlin, T. C., 1895. glacial deposits: 277. The classification of American Jour. Geology, V. 3, pp. 270- 176 177 Cohee, G. V., 1965. Geologic history of the Michigan Basin: Jour. Washington Acad, of Sci., V. 55, pp. 211-223. Connally, G. G., 1964. The Almond moraine of the western Finger Lakes Region, New York: Ph.D. thesis, Dept, of Geology, Michigan State University. Deutsch, M., Vanlier, K. E., and Giroux, P. R., 1960. Ground-water hydrology and glacial geology of the Kalamazoo area, Michigan: Mich. Geol. S u r v * Progress Report 23, 122pp. Egan, C. P., 1971. Contribution to the Late Neoglacial history of the Lynn Canal and Taku Valley sector of the Alaskan boundary range: Ph.D. thesis, Dept, of Geology, Michigan State University. Ehrlich, R . , and Davies, D. K., 1968. Sedimentological indices of transport direction, distance, and process intensity in glacio-fluvial sediments: Jour. sed. Petrology, V. 38, No. 4, pp. 1166-1170. Ekblaw, G. E., and Athy, L. F., 1925. Glacial Kankakee Torrent in northeastern Illionis: Geol. Soc. America Bull., V. 36, pp. 417-428. Embleton, C., and King, C. A. M., 1968. Glacial and Periglacial Geomorphology: St. Martin's Press, New York, 608pp. Flint, R. F., 1971. Glacial and Quaternary Geology: John Wiley and Sons, Inc., New York, London, 892pp. ________ , et al., 1959. Glacial map of the United States east of the Rocky Mountains: Geol. Soc. America, Scale 1:1,750,000. Folk, R. L., and Weaver, C. E., 1952. A study of the texture and composition of chert:A m e r . Jour. Sci., V. 250, pp. 498-510. Frye, J. C., and Willman, H. B., 1960. Classification of the Wisconsinan stage in the Lake Michigan glacial lobe: 111. State Geol. Surv., Circular 285, 16pp. Giroux, P. R., et a l . , 1964. Water resources of Van Buren County, Michigan: Geol. Surv., Water Investi­ gation 3, 144pp. 178 H a n e s „ F. E . , and Wyman, R. A., 1962. The application of heavy media separation to concrete aggregates: Canadian Min. and Met. Bull., V. 55, No. 603, pp. 489-96, Highway Geology Symposium, 1950. Geology as applied to Highway Engineering: Sponsored by the Dept, of Highways, Richmond, Virginia. Highway Research Board, 1966. A gg regate characteristics and Examination: Publication 1361. 1958. Chemical reactions of aggregates in concrete: Special Report 31, NAS-NRC, P u b l . 54 9. Horberg, L ., and Anderson, R. C., 1956. Bedrock topography and Pleistocene glacial lobes in central United States: Jour. Geology, V. 64, No. 2, pp. 101-115. Hough, J. L. , 1958. Geology of the Great Lakes: of Illinois Press, Urbana, 313pp. Univ. Ibrahim, Abdelwahid, 197 0. The application of the gravity method to mapping bedrock topography in Kalamazoo County, Michigan: Ph.D. thesis, Dept, of Geology, Michigan State University. Johnstone, J. G., et a l . , 1953. A manual on the airphoto interpretation of soils and rocks for engineering purposes: School of Civil Eng. and Eng. Mechanics, Purdue University. Kelley, R. W . , and Farrand, W. R., 1967. The glacial lakes around Michigan: Mich. Geol. Surv. Bull. 4, pp. 23. Klasner, J. S., 1964. A study of buried bedrock valleys near South Haven, Michigan by the gravity method: M.S. thesis. Dept, of Geology, Michigan State University. Klyce, D. F., and Bishop, R. J., 1971. Mineral industry of Michigan, 1969: U.S. Bureau of Mines, Ann. Statistical Summary, No. 13, pp. 18. Kneller, W. A., 1964. A geological and economic study of gravel deposits of Washtenaw County and Vicinity, Michigan: Ph.D. thesis, Dept, of Geology, U n i ­ versity of Michigan. 17 9 Krumbein, w. C . f 1 9 3 3 . Lithological variations in glacial tills: Jour. Geology, V. 41, pp. 382-408. _________ , and Pettijohn, F. J . , 1938. Manual of Sedi­ mentary Petrography: Appleton-C entury-C ro f t s , Inc., New York, 549pp. Krynine, P. D., 1957. The megascopic study and field classification of sedimentary rocks: Mineral and Exp. Sta. Tech. Paper 130, College of Mineral Inds., Pennsylvania State University. _________ , and Judd, W. R . , 1957. Principles of Engineer­ ing Geology and Geotechnics: McGraw-Hill Book Co., Inc., 730pp. Kuehner, I. V., 1956. A geologic study of the soundness of limestone for use as concrete aggregates: M.S. thesis. Dept, of Geology, Michigan State University. Kunkle, G. R . , 1960. The groundwater geology and hydrology of Washtenaw County and Upp j.r Huron River basin: Ph.D. thesis. Dept, of Geology, Univ. of Michigan. Kurk, E. H., 1941. sediments: The problem of sampling heterogeneous M.S. thesis, Univ. of Chicago. Lane, A. C., 1895. The geology of Lower Michigan with reference to keep borings: Mich. Geol. Surv., p u b l . 5, Part 2. _________ , 1907. Summary of the surface geology of Michigan: Mich. Geol. Surv. Report 1907. Lawrence, D. B . , 1950. Glacier fluctuations for six centuries in S. E. Alaska and the relation in solar activity: Geographic Review, V. 40, No. pp. 191-223. Legg, F. F., Jr., and Vogler, R. H., 1964. Alkalicarbonate rock reactions in Michigan: Highway Research Records, No. 45, H R B , NAS-NRC, publ. 1167 . Leighton, M. M., 1960. The classification of the W i s ­ consin glacial stage of Northcentral United States: Jour. Geology, V. 68, pp. 529-552. 2, L e n h a r t , W, B ., 1961. Sand and gravel: in Industrial Minerals and Rocks; Amer. Inst. Min. Met. Eng,, pp. 733-58. _________ , 1962. Sand and gravel: Reviews of Engineering Geology, V. I., F l u h r , T. and Legget, R. F., editors: Geol. Soc. America, pp. 187-96. LeRoy, L . W . , 1950. Subsurface geologic methods, 2nd edition, Colorado School of Mines, Golden, Colorado. Leverett, Frank, 1912. Surface geology and agricultural conditions of the southern peninsula of M i c h i g a n : Mich. Geol. Surv., publ. 9. _________ , 1915. Specific reference is made to chapters written by Leverett alone in the U.S. Geol. Survey Monograph 53 (Leverett and Taylor, 1915). _________ , 1917. Surface geology and agricultural c o n ­ ditions of Michigan: Mich. Geol. Surv., Publ. 25. _________ , 1905-1920. Field Notes: L e v e r e t t 1s Notebook, Nos. 202, 269, and 275, available at Mich. Geol. Surv. Library, Lansing, Michigan _________ , 1924. Map of the Surface Formations of the Southern Peninsula of Michigan: Mich. Geol. Survey. _________ , 1929. Moraines and shore lines of the Lake Superior Region: U.S. Geol. Surv., Prof. Paper 154- A , 7 2p p . _________ , and Taylor, F. B., 1915. The Pleistocene of Indiana and Michigan and the history of the Great Lakes: U.S. Geol. Surv., Mo nograph 53, 529pp. Litehiser, R. R., 1938. The effect of deleterious materials in aggregate for concrete: National Sand and Gravel Association, Circular 16, 8pp. Martin, H. M . , 1936. The centennial geological map of the Southern Peninsula of Michigan: Mich. Geol. Surv., Publ. 39. _________ , 1955. M ap of the surface formations of the Southern Peninsula of Michigan: Mich. Geol. Surv. Publ. 49. 131 Martin, H. M., 1957. Outline of the geologic history of Kalamazoo County, Mich, Geol. Surv., Misc. Report Mather, K . , and Mather, B., 1950. Method of petrographic examination of aggregates for concrete: Proc. Amer. Soc. of Testing Mats, V. 50, pp. 1288-1312. Mazola, A. J., 1954, A survey of groundwater resources in Oakland County, Michigan: Mich. Geol. Surv., Publ. 48, Part 2, pp. 101-34 8, Michaels, E. L. , et a_l. , 1965. The properties of chert aggregates in relation to their deleterious effect in concrete: Inst. Min. Res., Mich. Tech. Univ. and Mich. State Highway Dept. Joint Study. Mielenz, R. C., 1962. Petrography applied to Portland cement concrete: Reviews in Engineering Geology, V. I, Fluhr, T. and Legget, R. F., editors: Geol. Soc. America, pp. 1-3 8. Miller, M. M., 1963. Taku glacier evaluation study: State of Alaska, Dept, of Highways and U.S. Dept, of Commerce, Bureau of Public Roads, 2 00 pp. (with figures) . _________ , 1964. Inventory of terminal position changes in Alaskan coastal glaciers since the 1750's: Proc. Amer. Philosophical Soc., V. 108, No. 3, pp. 257-273. _________ , 1970. Gl aciers and glaciology: McGraw-Hill, Encyclopedia of Science and Technology, 197 0 rev is i on . _________ , 1972. The Alaskan glacier commemorating project, Phase III (include details of the concept and significance of storm track shifts): National Geographic Soc. Research Reports (1966 Projects), 35 pp. (in press). _________ , Eagan, C. P., and Yates, W. C., 1964. A drumlinoid feature at the terminus of Norris Glacier, Juneau Icefield, Alaska: Mimeographed paper. Appendix C, Juneau Icefield Research Program, Glaciological Inst., Juneau, Alaska. Mineral Producers, Annual: Mich. Geol. Surv., Ann. Statistical S u m m a r y , Lansing, Michigan. Moorehouse, W. W . , 1959. The study of Rocks in Thin Section: Harper and Brothers, New York. 182 Newcombe, R. B. , and L i n d b e r g , G. D . # 1935. Glacial expression of structural features in Michigan: Preliminary study: Amer. Assoc. Petroleum Geologists, Bull. V. 19, No. 8, pp. 1173-1191. Otto, G. H . , 1938. The sedimentation unit and its use in field sampling: Jour. Geology, V. 46, pp. 569-582 Perkins, S. O , , 1928. Soil survey of Kalamazoo County, Michigan; U.S. Dept. Agriculture Soil Survey Report. Pettijohn, F. J . , 1957. Sedimentary Rocks: Harper and Brothers, N e w York. 2nd edition, Piskin, K . , and Bergstrom, R. E., 1967. Glacial drift in Illinois: Thickness and character: 111. State Geol. Surv., Circular 416, 33pp. Reed, J. E., et a l ., 1966. Induced recharge of an artisian glacial-drift aquifer at Kalamazoo, Michigan: U.S. Geol. Surv., Water Supply Paper 1594—D , 62pp. Riggs, C. H., 1938. Geology of Allegan County, Michigan: Mich. Geol. Surv. Prog. Report 4. Schneider, I. F., Johnson, R. W., and Whiteside, E. P., 1968. Tentative placements of Michigan soil series in the new classification system: M i m eo ­ graphed Manuscripts, Soil Science Department, M i c h ig an State University and U.S. Dept, of Agriculture. Shah, B. p., 1971. Geology and geologic environment for solid waste disposal in Independence Township, Oakland County, Michigan: Student Water Publi­ cation, Michigan State University. Slawson, C. B . , 1933. The jasper conglomerate, of drift dispersion: Jour. Geology, V. 546-552. an index 41, pp. Swenson, E. G., and Chaly, V., 1956. Basis for classify­ ing deleterious characteristics of concrete aggregate materials: The Crushed Stone Jour. June-Sept., pp. 17-2 6? Jour. Amer. Concrete Inst., V. 27, No. 9, May, Proceedings, V. 52. Tarbell, E . , 1941. Antrim-Ellsworth-Coldwater shale formations in Michigan: Amer. Assoc. Petroleum Geologists Bull., V. 25, No. 4, pp. 724-733. 183 Terwilliger, F. W . , 1954. The glacial geology and g r o u n d ­ water resources of V a n Buren County, Michigan: Mich. Geol. Surv. Publ. 48, Part I, 95pp. Thomas, W. A., 1930. A study of the Marshall formation in Michigan: Mich. Acad. Sci., Arts, and Letters, Papers, V. 14, pp. 487-98. Thornbury, W. D., 1962. Principles of Geomorphology: John Wiley and Sons, Inc., N ew York, 618pp. Thwaites, F. T . , 1957, Outline of glacial geology: Published privately, available through Mrs. F. T. Thwaites, 41 Roby Road, Madison, Wisconsin. Travis, P. A. A., 1966. An analysis of Pleistocene sedi­ ments in an aquifer recharge area, Kalamazoo, Michigan: Ph.D. thesis. Dept, of Geology, Michigan State University. Vanlier, K. E., 1966. Ground-water resources of the Battle Creek Area, Michigan: Mich. Geol. Surv., Water Investigation 4, 52pp. Wayne, W. J., 1956. Thickness of drift and bedrock physiography of Indiana north of the Wisconsin glacial boundary: Report of Progress, No. 7, Indiana Geol. Surv. and Dept, of Conservation. _________ , and Zumberge, J. H . , 1965. Pleistocene geology of Indiana and Michigan: in The Quaternary of the United States, Princeton Univ. Press, Princeton, N e w Jersey, pp. 63-83. Webb, W, M., and Smith, R . , 1961. The bedrock geology of Lake Michigan (abst.): Univ. of Michigan, Great Lakes Res. Div., Fourth C o n f ., Great Lakes Res. Proc., publ. 7, 14 6pp. Whiteside, E. P., Schneider, I. F., and E n g e b e r g , C. A., 1955. Taxonomic classification of Michigan soils: Mimeographed Manuscript, U.S.D.A. Soil C o n se r­ vation Services, 313pp. Willman, M. B . , and Frye, J. C., 1970. Pleistocene Strati­ graphy of Illinois: Illinois Geol. Surv. Bull., No. 94. Wilson, L. M., 1955. Surficial glacial deposits of the Michigan-Saginaw lobes in Grand Rapids area, Michigan: A study of relationships: M.S. thesis. Dept, of Geology, Michigan State University. 184 Wingard N. E., 1969. Economic and petrographic evalu­ ation of gravel resources in southern Michigan: Ph.D. thesis. Dept, of Geology, Michigan State University. 1971. Evaluation of aggregate sources of glacial origin (same study as above): Mich. Dept, of State Highways, Research Report, No. R — 7 4 6. The Coldwater formation in the area Wooten , M. J . , 1951. of the type locality: M.S. thesis. Dept, of Geology, Wayne State University. Wright, H. E., and Frey, D. G., editors, 1965. The Quaternary of the United States: Princeton Univ. Press, Princeton, N ew Jersey, 922pp. Zumberge, J. H . , 1960. Correlation of Wisconsin drifts in Illinois, Indiana, Michigan, and Ohio: Geol. Soc. Amer. Bull., V. 71, pp. 1177-1188. GLOSSARY GLOSSARY The following t e r m s , as used in this dissertation are explained for purposes of consistency in the text. These definitions are also deemed adviseable for readers not fully familiar with the language of glacial geology, and as well to insure clarity because of some ambiguity in the use of these and alternative nomenclature in the literature. Ablation t i l l : Till deposited during downwasting (ablation) and recession of a glacier. Such till is fre­ quently more sandy than basal or linear moraine tills, and is found directly at the surface of the ground and often overlies more clayey lodgement till. Agei Any major period of time in the history of the earth or the material universe marked by special phases of physical conditions or organic development. In this dissertation this term is specifically applied to the Wisconsinan glaciation, because in the literature age is commonly used for reference to the deposits of earlier glaciations of the Pleisto­ cene, e.g., Illinoian age deposits. Flow-lag: The lag in years whereby the effect of signifi­ cant changes in the neve are expressed by ad­ vances, stillstands, or retreats in the terminal area of a glacier. Holocene: The term which is generally used for reference to the time interval since retreat of the last major ice advance of the Wisconsinan age, i.e., usually this represents the last 10,000 years. Interlobate l i n e : An interpretive line drawn between deposits and geomorphic features from two adja­ cent glacial lobes. Such an interlobate line in this dissertation (see Plate I) is drawn from evidences given by the lithologic distribution 185 186 (see Figs. 29-37) and the geomorphology of an area. It is not always a sharp line, but rather a zone, in some cases 4 to 6 m iles wide, in w hich weak and parallel moraines are found. Isopleth: A line of equal abundance or magnitude, in this dissertation used to show changes in average lithological composition of glacial gravels. Neve a r e a : Accumulation area or nourishment zone in the upper part of glaciers (in the broadest sense, the ice centers of continental g l a c i a t i o n ) . A nev€ is composed of consolidated granular snow "not yet changed to glacier ice," called firn. Parma t i l l : An early Wisconsinan or Illinoian (?) basal tTll, which is characterized by considerable induration, hence actually a tillite. This tillite was exposed in May, 1971 by sewer tr eat­ ment excavations and subsequently buried. The writer observed the outcrop southeast of the Parma, Jackson County, Michigan near a series of turf farms. The till is composed of angular frag­ ments of Bayport-type (?) limestone and what appear to be rounded pre-Cambrian pebbles. It overlies Parma sandstone and lies at shallow d e p t h below muck (turf) and bogs in this region. The tillite has been weathered substantially, w i t h a surface gossan which separates easily into a limonitestained powder. Pleistocene; The Pleistocene is the latest epoch of the Tertiary Period (Cenozoic E r a ) . This epoch is subdivided into four m a j o r glacial ages, the Nebraskan, Kansan, Illinoian, and Wisconsinan, taken in order from oldest to youngest. Plexal z o n e : An area in which a differential forward m ovement of ice has created contrasting relations between older and newer geomorphic features of the same lobe and p r o v e n a n c e . Thus making the chrono­ logical interpretation difficult. This single lobate sequence equates to the complexities of an interlobate sequence. Provenance: S t ag e : Origin or source. A time-stratigraphic unit, used as a time term for major glaciations of the Pleistocene epoch. In this dissertation it refers to subdivisions of the Wisconsinan age, because the term age is applied to subdivisions of the Pleistocene epoch. 187 Till; An unsorted mixture of boulders, cobbles, pebbles, sand, silt, and clay— deposited by the advance and retreat of glaciers. Valley t r a i n ; A long narrow body of outwash confined within a valley. W i s c o n s i n a n : Latest major glacial age of the Pleistocene epoch. APPENDIX 4 .0 0 4 . SO 7 .6 0 C hannel 0 ,4 0 3 .3 0 6 .5 ft 5 50 11- 12 U 90 SO. 40 4 7 .0 9 4 2 .4 0 3 -6 4 4 .1 0 C oop er C oop er C hannel C hannel 0 .8 2 0 ,3 0 4 .7 6 f t .00 7. SI 7. SO 1 1 .4 3 7 .0 0 4 1 .4 4 4 0 .2 0 4 .3 5 3 .0 0 0 .4 0 *23 ft. 40 1 0 .6 0 1 .0 0 0 .6 0 4 4 -5 0 4 3 .5 1 3 .7 0 6 . 33 3 .0 8 TOWNSHIP RANGE 38 1 A lam o C h ann el NW IT 1 C oopt f ft NW mr 12 11 NE 0 1 12 A lam o 6 7 sw sw NW aw 31 33 1 1 11 11 t a. O f,: a 0*70 1 0 0 .0 0 1000 1 0 0 .0 0 1000 32 40 5 1 ,1 0 5 0 .3 0 7 .3 0 7 .6 0 1 5 -1 0 1 ,7 0 9 .6 0 3 .3 0 Z .3 0 1 .0 0 1000 W 20 H .O D 1 7 .3 0 1 8 .9 0 Lake M ich igan 3 -0 ) S . 20 3 .6 0 2 .7 0 4 ,0 ft 7 .B 0 3.-QI 4 ,7 0 2 ,0 6 1 .2 0 1 0 0 .0 0 10 0 .0 1 1 0 0 .0 0 962 1000 3 3 25 3 2 -1 0 5 4 ,1 5 5 4 .7 0 1 0 .5 0 1 2 .0 0 1 3 ,9 2 2 0 .2 0 Lake M ic h .-S a g . In terlob ate 4 . 57 4 ,5 0 0 . ftfl 9 ,7 ft 4 .4 0 4 .9 0 2 ,9 4 4 ,0 0 1. 31 2 .3 0 1 0 0 .0 0 ftift 1000 5 4 ,1 9 5 7 .0 0 ft.ftO 1 2 .4 0 1 8 ,2 6 1 1 .7 0 L ake M ich igan 6 . BO 1 1 .7 5 5 6 .1 0 7 .7 0 1 3 .6 0 1.B 4 2 .2 0 1 .7 4 3 4 -5 1 2 8 .3 0 3 5 -4 0 3 1 .5 6 5ft. 55 7 .4 4 1 9 .6 2 Lake M i c h .’ S ag E r te r lo U te Lake M ich , -flag- In ter lo b a te NE 8E NW BE 34 13 1 1 11 11 C oop er JC alam aioo C hannel 1 .0 0 C h ann el 1 .4 0 SW NW 18 1 14 C om atock C h ann el S .3 0 7 .2 0 6 .8 0 1 1 .3 0 4 6 .0 0 4 .0 0 3 .7 0 0. 50 11 IS BE W l/1 SE NW ft 1 11 K a la m a zo o 11 5 .0 0 ft.ftO 1 0 .1 0 6 .1 0 2 .9 0 3 .9 0 13 14 NW NW SE SE 16 31 1 2 11 10 K i ln m u o o K alam azoo 5 ,6 0 4 .3 0 3 . 90 1 0 .0 0 7 .4 0 4 6 .0 0 8 Channel Channel Channel 8 .4 0 0 .1 0 1 0 .1 0 7 .9 0 1 1 ,6 0 1 4 .0 0 43. 20 4 .3 0 6 .4 0 3 .W IS NW SW 8 1 0 C h a rlesto n C h a m t) C hanel 6 .4 0 6 .5 0 1 2 .1 0 0 .3 0 0 .3 0 1 3 .1 0 3 6 ,7 0 5 ,6 0 10 IT 18 aw BE NE sw sw SE 11 I ft 2 a 4 0 11 C h a r le s to n fb r ta ft Channel Channel 8 .4 0 04 10 7 .0 0 6 .3 0 1 0 .2 0 1 0 .1 0 » . 20 3 1 .2 0 18 SO SW SE SW sw 4 T Z 2 12 0 P r a ir ie R o e * C h arleatn n C h a r le s to n C h arn el Channel Channel 0 ,0 0 9 ,W 464 1 .0 0 1 0 .2 3 <4 SO 1 .2 3 S . 34 3. 70 3 .3 3 1 .5 6 4 .6 0 1 4 .0 0 1 0 .0 7 3 6 .1 0 4 0 .0 0 3 3 .5 6 11 Sw SE IT Z 10 C om * tack C lu nteL 7 ,3 4 4 .4 7 1 .3 3 n NE SW NE SE t ia I 11 12 K alam azoo 13 Channel Spot 3 .M 3 .4 7 M 30 SE SW SE SW 8 4 12 P r a ir ie flon d e P r a ir ie Rood* 4 4 12 P r a ir ie R aod e T U S ?; K -IS S u u ^ a 6 .2 0 6 .5 0 9 ft H ttS S 6 .«0 6 ,0 0 10 C om a to e k A SSO C IA TED GLACIAL LOBECS) 7 . SO NE Is 3 :* C L A ST IC 5 -5 0 BE 0 .3 0 PERCENT GROUP LITHOLOGY CRYSTALLINE i .. 1 CARBO NATE ; AND C H E R T ft-90 C hannel 8 .3 0 9, 00 0 . 40 j TOTAL 0 .6 0 7 ,8 0 C hannel j OTHERS 2 .1 0 2 . ZO CIUMl ! D E N SE | CHERT SIL T ST O N E AND S H A L E 4 ,8 0 A la m o C oo par S z PO R O U S CHERT SA N D STO N E 4 . ftO 12 11 P o C A RBO N A TE 3 8 .3 0 4 6 .1 0 1 1 SAMPLE NON- FOLIATED M ETAM ORPHIC 1 9 ,9 0 1 2 .8 0 R 10 Iff B A SIC IG N E O U S 30 6 .8 0 T O W N S H IP NAM E ft BE BE 3 4 FOLIATED METAM ORPHIC TYPE OF SA M PI W. 4 .0 0 S .4 0 8W NE 1 1 3 CLAY IRONSTONE 1 C O N C R E T IO N PERCENT LITHOLOGY U i S E C T IO N S. NUM BER LOCATION TOTAL PE B B L E COUNTS OR VOLUME TABLE 3 GRAVEL LITHOLOGY OF KALAMAZOO COUNTY, MICHIGAN n.n 4 0 .9 0 lft,3 0 Lake M ic h .-S a g , U a r k f a a t e L ake M ic h .-fla g . In ter!ob aie Lake M ic h .-S a g . (n te r lo b tte Lake M ich . -S a g im er io b n ie 2 .6 0 0 .8 0 1 .4 3 1 0 0 .0 0 1 0 0 .0 0 1000 97ft 7 ,5 0 4 .2 ft 3 ,6 0 1 ,1 0 1 0 0 .0 0 1000 3 4 ,6 0 5 6 .1 0 8 .2 0 1 5 .3 0 Lake M ich . - t e g . In ter lo b a te 2 .9 0 1 1 .2 0 9 .6 0 6 .9 0 3 .6 0 1 .4 0 0 .4 0 0, 70 1 0 0 .0 0 1000 30. 90 1000 25 40 5 9 .2 0 5 3 -3 0 9 ,5 0 2 0 -6 0 19- B0 1 0 0 .0 0 2 6 -0 0 Lake M ic h .-S a g , u te r lo b a te L ake M ic h .-fla g . UnerLohata 5 .4 0 7 .1 0 i.ftO 2 .4 0 0 ,1 0 0 .0 0 1 0 0 .0 0 1 0 0 .0 0 1000 1000 33. 30 1 2 .5 0 3 8 -5 0 5 6 ,4 0 5 2 .7 0 ft.ftO 1. 30 1 .3 0 0 .6 0 8 ,3 6 1 1 .4 0 L ake M ic h .-f la g , im e r la b a w Lnke-M lrh. -flag- In ter lo b a te 2 .5 0 1 .2 0 0 .4 0 3 .5 0 1 .4 0 1 0 0 .0 0 1000 4170 4 7 .6 0 9 .3 0 1 5 .6 0 S agin aw 4 ,9 0 2 .9 0 3 .0 0 4 .4 0 6 .8 0 9 .3 0 7 .0 0 1 1 .3 0 L .90 0 .9 0 1 .4 0 0 .6 0 1 0 0 .0 0 1 0 0 .0 0 1000 1000 4 6 ,9 0 4 9 ,4 0 1 5 .5 P 1560 2 0 .3 0 2 4 .9 0 S agin aw 1 .4 0 14. 90 2 .4 4 1 0 0 .0 0 1 0 0 .0 9 1004 3 -1 1 4 ,6 0 0 .6 0 1 7 .7 0 6 ,1 0 S . 11 4 .4 4 450 3 1 .5 6 4 1 ,3 0 5 7 78 3 3 ,3 0 9 ,1 1 3 7 .1 0 2 1 .7 8 Lake M ichigan flaglnew I . 44 1 7 .1 0 0 . Bf 0, M 3 4 .2 0 3 4 -4 0 1 0 .3 0 0 .2 2 100-02 450 35, 80 5 7 ,1 2 4 .6 * 2 6 .0 0 S agin aw 3 7 .7 0 4 . 8ft 3 .7 * 4 0 .0 9 5 5 .7 5 3 .5 6 0 .7 3 3 .5 6 ft. 7ft 5 7 .1 7 1 .1 3 5 4 .7 7 4 5 .0 0 4 9 ,1 0 6 . 70 Z. 81 15. U 1 .0 0 0 ,1 9 1 1 .3 1 8 .0 0 1 .3 9 2 .3 * 3 ,5 1 3 .7 * Spot 4 . 2ft 1 3 .5 0 3 .3 7 3 .1 2 S pot Spot 4 .6 4 I l.I -i 3 .0 0 1 . 10 S pot 1 .9 2 3 .9 7 1 3 .1 3 9 .4 3 2 .4 2 2 .6 5 1 ,4 2 1 .8 2 4 ,2 ft 1 1 .8 7 5 6 .5 0 3 2 .4 3 4 .0 0 1 .3 3 1 0 0 .4 5 f t .39 7 .5 6 9 .8 2 3 .1 0 2 0 .0 1 0 . 33 1 0 1 .5 8 9 9 .9 9 450 2 lit e r s 2 0 .0 8 5 .9 0 4. 03 4 -7 5 C« 0 .9 7 1 0 0 .0 0 2 . 70 0 -6 1 3 -6 3 1 .1 9 3 ,5 4 9 9 .9 * 2 5 -2 7 24. 36 6 2 .7 6 1 .0 ft 2 liter * 2 lite r * S 2. 75 O .ftl 6 . 34 9 ,9 6 2 ,4 5 1. 01 7 .2 7 9 9 .9 9 2 lite r * 2 0 .7 0 5 6 .2 1 3 7 .9 6 0 .3 3 0 .4 1 8 .0 3 2 6 .2 5 0 .5 9 L ,2 t 2 lite r * 2 lite r * 2 0 , 8ft 1 5 .5 5 4 .5 2 1 .9 2 9 9- 99 4 .3 0 1 .4 2 1 .9 0 1 7 .8 7 3 9 ,9 7 6 0 .0 5 1 .7 3 0 .4 8 1 .6 5 0 .1 5 3 .1 4 1 0 .8 1 J. 47 1 .9 0 0 ,0 0 1 0 0 .0 0 6 3 ,1 7 9 9 .9 9 2 lite r * 2 lite r * 2 8 .8 2 5 ,7 4 4 8 .6 7 4 * . 08 6 ,1 1 2 .3 4 0 .6 4 0 .5 7 M NW NW 4 4 12 P r a ir ie Ronde IT SW 31 3 11 10 NE SW NW 4 4 13 T ea** P r a ir ie R ood e n SW SE « 4 11 S ch ool c r a ft 1 0 .7 3 NW NW 30 4 10 B rad y Spot Spot 0 .1 0 30 1 7 .4 4 1 7 .5 3 5 .6 2 1 .0 1 31 NE NW 14 4 11 S c h o o lc r a ft Spot 1 0 .6 4 1 3 .2 0 2 .0 8 5 .0 0 5 0 .4 0 1 -3 6 2 .3 2 31 33 34 NW NE NW NW SE NW 14 38 ft 4 2 3 11 10 9 S c h o o lc r a ft C o m * to e It Spot Spot 9 .3 2 8 .6 0 1 0 .2 2 1 3 .4 0 6 .4 6 2 .2 1 9 .3 2 0 .1 7 36. 10 3 3 .5 0 2 -4 5 5 -0 0 ft 3 9 l2 ,ftS 19. 31 3 .6 1 4 .4 2 2. 05 SW 7 .4 3 1 0 .1 4 4 9 .2 2 SW Spot Spot 0 .2 0 30 C lim ax C lim ax 1 .1 4 2 .3 7 1 .0 7 6 .4 4 3 5 .0 0 5 .4 7 2 .4 9 5 6 .9 1 2 .7 3 1 .2 1 0 .2 2 2 .6 7 2 3 ,5 6 79 100 00 450 2 8 .6 7 23. 33 L ik e M ic h ,‘ flag. M e r lo b a tr 6 1 .5 6 8 .B 9 2 7 .7 * Lake M ich . -flag- In terlob ate 4 8 .4 5 6 7 -6 7 ft. 79 1 3 .7 9 2 3 .1 0 Lake M ichigan 1 1 .9 1 1 1 ,0 4 1 2 .4 * 1 5 .3 0 1 4 -9 0 Lake M ich igan Lake M ichigan 1 5 .* 1 1 8 .7 6 L ake M ich igan 3 4 -6 1 2 0 .2 8 3 6 .2 9 2 2 .9 ft Lake M ichigan ft.ftO 1 7 .6 8 L ake M ic h .-S a g . b te .-]o h * te 6 0 -2 8 Lake M ichigan Lake M krhlfan Lake M ich, ‘ Sag, In terlob ate H .04 4 .5 6 0. 64 1 0 0 .0 0 2 lit e r s 3 1 .4 4 6 3 .6 0 4 .3 2 1 6 .1 6 la k e M ich. -flag. In terlob ate 1 7 .2 5 2 0 ,2 6 4 .6 6 2 .9 4 0 ,4 9 0 ,1 6 2 lit e r s 2 lit e r s 3 5 .3 2 3 2 .3 6 6 0 .0 1 5 6 .7 0 4 .1 6 1 0 .7 8 2 .4 6 2 .5 7 1 .5 5 0 .0 0 3 1 .9 9 4 0 .3 1 6 1 .3 6 5 0 .4 4 5 .0 9 9 .2 5 Lake M ich. .fla g . In terlob ate L ake M ich. -S a g . In terlob ate Lake M ich. -S a g . In terlob ate 1 0 0 .0 0 2 lit e r s 2 lite r * 2 3 .6 2 2 8 .1 6 1 5 .1 6 1 .2 9 9 .6 9 1 2 .0 7 9 9 .9 8 1 0 0 .0 0 1 0 0 .0 0 Id . 42 Lake M ich. - Sag. In terlob ate 2 .6 1 l.ftT 38 NW NW aa I 9 C h a r le s to n Spot 7. SO 1 7 .6 0 3-ftO 12- 31 2 9 .2 6 1 1 .7 4 1 .0 6 2 ,3 6 1 2 .2 2 1 .4 7 O.ftN 1 0 0 .0 0 2 lit e r s 4 0 .0 1 4 2 .9 5 1 5 .1 6 1 7 .1 1 Saginaw 3T 38 BE SW 23 1 0 C hirL eattm 3 .3 4 7 .7 2 4 4 . 19 3 .6 6 2. 71 2 ,2 3 1 1 -7 8 2 .0 7 1G .79 Saginaw 10 2 ,4 3 9 .7 9 3 1 .2 1 9 ,7 1 2 ,7 8 1 .0 9 1 9 /4 3 .2 6 1 3 .5 6 25. *5 Lake M ich- -S a g . In terlob ate SW NW a 1 0 0 .0 0 3 4 .6 3 8 -6 1 4 .6 9 Lnkr M ich. -S a g . In terlob ate 0 .9 0 5 4 .2 2 5 9 .3 8 2 1 .0 4 1 -5 5 2 titer* 2 lite r * 3 4 ,7 7 1. 55 1 5 ,5 2 1 7 ,4 6 1 0 0 .0 0 2 .0 6 2 -7 6 0 .4 9 0 ,4 0 1 4 0 .0 0 4 0 .3 7 0 ,6 ft 0 6 .0 0 1 2 .9 7 3 .7 4 SE 1 6 ,0 0 9 .7 9 2 .3 ft sw Spot S pot 10, 24 40 14 12 2.11 5 3 -2 1 3* 28 1 2 .3 0 3 2 .0 0 3 1 .8 8 6 .6 0 2 9 9 ,0 9 9 9 .9 9 5 8 ,0 4 2ft L, 35 1 .3 4 2 liter * NE 0 .4 0 7 .2 0 1 2 ,2 6 SW S pot Spot 2 1 .0 5 Lake M ich. -S a g . In terlob ate 41 41 NE SW SE SE 0 1ft i 1 13 A la m o C oop er Spot 1 0 .3 4 6 ,8 9 1 .9 2 0 .0 8 9 9 -9 9 2 lite r * 8 1 , 38 5 5 ,7 7 5 -2 0 16. 74 1 7 .1 9 Lake M .ch. -S a g . In terlob ate 9 9 Ho h H «a S pot Spot 3 1 .9 8 2 7 .6 2 6 2 -5 8 5 9 .5 7 4ft SE SE 2 1 10 R ich land Sp« 4 .0 6 9ft, 99 100. 00 1 0 0 .0 0 9 9 . 98 3 3 .3 3 3 8 .8 2 1 1 1 -2 9 1 04 % lite r * 27 21 5 .3 3 6 ,ft7 0 .4 0 SW NE 3 .6 3 1 .6 0 2 ,3 3 4 7 .0 4 4 1 .9 7 NW SW 1170 6 .2 ft 4 .3 4 1 0 .1 2 1 3 .6 2 1 8 .0 0 2 ,4 6 Spot 43 44 3 9 ,2 7 5 4 .5 0 • U C o m tto r k C o m eto c k A la m o 1 0 .'4 1 7 .4 0 1 8 .0 1 1 0 .0 0 1 .6 3 2 .0 0 0 .5 6 1 .8 4 4 .2 4 5 4 .2 5 4 ft. 92 1 .5 3 2 .0 0 5 .7 4 2 .9 9 1 .5 2 4 .9 1 0. 40 1. 38 1. 33 1 2 .4 2 1 2 ,5 1 7 -2 9 7, 49 6 .2 1 4ft. 2 .5 5 1. 27 L. 51 4 .7 9 2 -1 6 0 .6 4 0 .5 6 0 .0 3 0 ,1 6 T tila n l u * m a y t a b l|h « r i f u r id d ttk iB o d O w r p h y i i c i l l y m t u d c h e m ic iilly r c i c t l v c r o c k * , w hlcti ran s o t b e • e p t r t t e d In dividu ally In th is ta b le . 2 lite r s 2 li t e m 2 lite r * 2 lite r * 4 .0 2 4 -8 * ftfl 11. 5 . 33 1 1 .2 1 15, A f t ft, 20 Lake M ich. -S a g . In terlob ate S aginaw Saginaw S agin aw TABLE 4 MECHANICAL ANALYSIS Sample Number Grade Size D iam eter mm. 1 2 3 4 5 6 7 9 8 10 11 12 13 14 15 16 17 18 Weight Percent Frequency 2-in, 50.80 4.15 -- 8.96 1.26 0.97 2.41 1.43 0.70 — 3.51 1.74 3.17 1.63 2.66 1.85 6.15 1 -1 /2 -in. 38.10 1.61 3.22 3.16 2.63 3.26 0.97 2.49 2.11 1,60 2,47 1.04 4.37 1.88 2.46 2.09 4.36 2.59 9.72 1-in. 25.40 2.54 3.98 6.21 5.06 5.10 2.02 3.26 4.10 2.01 3.37 0.56 4.79 5.58 4.06 3.17 5.55 5.83 11.83 3/4-in. 19.00 3.28 3.35 5.53 4.72 4.96 1.97 5.61 4.86 2.74 4.03 1.11 5.98 5.14 3.45 4.48 4.66 5.51 9.85 1/2- in. 12. 70 10.12 6.99 6.43 6.96 5.99 3.73 5.77 4.07 5.43 7.03 2.31 6.70 7.52 7.39 7.43 5.74 6.22 11.74 3 /8 - in. 9.51 7.97 4.75 4.29 6.21 5.10 2.94 3.90 3.40 4.10 5.72 1.92 4.67 6.08 5.91 5.27 4.00 4.86 7.16 3/16-in. 4.76 24.45 13.00 10.73 16.46 17.02 9.73 9.31 20.35 12.58 17.05 6.80 12.56 18.67 18.86 15.93 10.51 12.12 12.73 ASTM No. 10 2.00 16.80 17.22 9.73 12.41 24.07 13. 38 9.00 26.33 16.59 13.57 10.65 13.04 20.33 19.65 27.97 12.04 12.89 8.78 ASTM No. 18 1.00 11.80 14.64 9.30 9.12 13.48 12.24 8.05 12.92 18.02 10.85 13.01 10.44 16.53 11-54 19.54 10.32 9.74 5.47 ASTM No. 35 0.50 8.00 15.74 15.31 11.45 7,48 18.85 15.14 9.36 14.87 15.28 24.67 14.08 6.93 11.09 7.23 14.87 13.39 6.40 ASTM No. 60 0.25 5.75 12.38 15.86 11.10 6.39 25.91 27.14 6.46 14.87 12.15 26.78 15.58 4.55 8.50 3. 76 15.81 17.92 7.29 ASTM No. 120 0.125 1.80 3.61 3.23 10.03 5.24 4.64 8,05 2.41 5.65 3.58 8.36 3.69 2.19 2.54 0.72 4.36 5.72 2.23 ASTM No. 230 0.062 0.83 0.52 0.82 1.87 0.50 0.53 0.61 1.27 1.00 0.62 0.76 0.46 0.48 0.88 0.24 0.94 1.51 0.73 ASTM No. -230 - 0.062 0.83 0.45 0.42 0.57 0.4S 0.45 0.27 1.63 0.43 0.68 0.33 0.40 0.48 0.99 0.29 0.59 1.63 0.92 99.99 99.85 100.01 99.77 100.03 99.97 99.90 99.97 99.92 99.93 99,97 Total f t r cent 99.90 99.85 99.91 100.04 99.93 99.99 99.98 5.12 190 TABLE 5 GRAVEL LITHOLOGY OF S U P P L E M E N T A R Y STUDY AREA, S O U T H W E S T E R N MICHIGAN PE R C E N T Q A O U P LITHOLOGY P E R C E N T LITHOLOGY l o c a t io n a o 1*1 * Z J in H h 1*1 104 109 IM in 14 I* *T J« 19 T .4 N . . T -4 N -, T. 4N . * T 4N - , T -4 N . , R .6 W , B OWR . *W . R- Ik W . H . 1 LW- E ito w B a rn 1 fta rrr B a rry A l la g a a IS . 90 2 5 .1 0 1 4 ,9 0 * 1 . 11 1« 9 0 3 . 50 1 ,5 0 1 .9 0 2 . 44 1 .0 0 9. 0. 0, B. 0. 90 00 TO 0O 90 51 9 0 0 0 . 90 9 3 . 10 I I I ) 5 7 . SO 141. 10. T. 9. ■ put *PPt Spot C hannel Boot IB . 30 19. 30 3 1 -4 0 1 1 . ■* 1 9 . TO 2 .1 0 0 90 1 TO 0. « I . 10 5. 40 7 . 70 9 -9 0 0 . 17 « . 90 9 7 .0 0 0 1 .1 0 3 1 .1 0 9 4 -9 0 9 1 .5 0 2 . 10 1 .1 1 1 .1 0 S . TO 2 ,0 7 4. 411. fl. 14. >0 00 30 10 22 70 90 SO 13 10 I . TO -1. 30 0 . 99 5 .6 0 0. 1. 4. 0. 40 OO 09 50 0 .47 2 .3 0 3 . 00 a. 00 ) 40 1 5 . 10 3- 4 0 *. 1. 4. I. i, 3. 2. 41. 4. 10 TO 30 74 » 5. 5. «. 0. S. 9 5 -4 0 4 * . 2a 9 0 . TO 9 2 . 50 4 0 , 30 2 . 70 1 2 -3 9 13, 10 13. *0 5 ,4 4 5 . BO 4- 44 3 .0 0 5 . 30 1. 1 I 4 «0 T T T. T. T 4N JN . 3N . .IN . JN , . . , , . AA. ft. Hft 11W 14* 13W . J 3W . 13*. A lla g a n A lla p n A l le g a n A l la g a n A lla g a n 111 lit 113 114 Hi 99 9 90 0 IS T T. TT. T. JN IN . JN . 3N 3N . T * t , . A in k . H . 1 1W R. U V . R , lO W . R .tW . A l la g a n A lla g a a A ll a g a a B a rry B a rry 3 (rt C haanal Sf-M flo a t C hannel 10. 50 14. 9 4 10. * 0 14*0 1 1 . T* III 1IT US U l m 10 10 IT 14 3 T. T T. T. T- 3N . 3N . 3N , JN . IN - . , . , , R .B W . R .T W . R 04*. H 1W R .3 W , B a rry B a rry CnUM E a t4 > E a to n Spot Spot Bpot rh a n a n J C haanal 1 0 .0 0 1 7 .0 0 1 0 .0 0 14. IP 1 0 ,4 3 1. 4 0 3. TO 140 2. 0O 1. 5 4 11- 10 9 .3 0 13. M 15. 5 0 ID 0 0 4 » . 0O 99 50 4 1 . lO 4 4 .0 1 3 0 .0 0 15, 12. 1 11 3. 7. 90 10 50 33 33 m its 1*9 124 III 19 I* 14 15 1 T -3 N , T. I N ., T 2 N -. T I N .. T. 9N . . R , JW A. 4W . R AW . f t .O W . J8. f W . E a to n £ |k > E a te n E a te n B arry C hannel C lU M U l C haanal I T . Mi 11. 0 0 I I , *9 *4. *0 9 4 . 73 1- TB I . 44 00 J , 30 1. 34 II. 13, 10. 10. 11. 30. 34 37. S4. 40. »« 00 11 30 iO ill III III II* 1*0 SO IT « 21 3 T .tN T IN T IN T .2 N T tN . . , * .. * 1 0 W I IIV ft. l l W , R . |1 W R . I4 W . B arry A ll* g a n A lla g a n A lta g a a A lla g a n c tu u l l& .M I B .9 0 in , 3 ^ 1 3 . '01 2 -4 0 1. 5. 1 0. 9. 00 50 M 00 >0 S . 10 3 .3 f S 40 * 0O « , 70 111 131 13* 1M I® 5 94 SO 0 I T. T. T T T- I N .4 I N .. IN -. IN . . IN . R . I4 W . R . la w . R . 1 IW . R .tW ft-tW A lle g a n A l la g a a A ll e g a n B a rry B a rry SfHK C hannel flo at Spot Spo* 1 4. TO 1 4 .0 0 17 4 0 3 1 B0 1 * . TO 4 . 30 » .0 t 0. 70 >. 0 0 &. 9 0 LMI lf no in 140 31 * 5 15 33 T -IN . , T I N ., T . IN , T IS . T, lg .. A 6* H . TW , R JW R .T W . R . SW B a rry B a rry E a to n C a lh o u n C a lh o u n Soot SpDI C*hanne1 C h a ra ie l C hannel > 1 .3 0 1 0 . 30 2 1 . 70 I S . 77 IS 07 2. 5. 1. Z. 1 141 i 42 143 144 145 9 34 39 4 1« T IS . . T IS - . T IB . T 33. . T, IS . , ft. H W ft- 1 JW . R AW R . TW . V an B u rc n V an f t i r r * V an (h r* « C a lh o u n C a lh o u n flw * C hannel rh an ael 3» 23. 33 11. 13 0 0. I 1. 1 140 147 140 140 1*0 *7 14 3) 31 IT T T T T T H OW. R . 5W R SW R .4 W . ft SW C a lh o u n C a lh o u h C a lh o u n C a lh o u n C a lh o u n C hannel t hum el C hunel C hannel C h a b ie l 191 192 199 ' 194 199 33 13 11 37 39 TT TT. 38. . M .. 3S- . 3 fl. . T.n. . R. R. R. R. A V u ftu re n V u B u r* n v a n B u rcn B e rrie n B e rrie n flooi 3(101 Spot 194 1ST 191 IS* 190 19 19 4 13 34 T SS T 59 T .99, T .iS T -0 3 , . , , , R .4 W A 6W , R . AW, R .W W f t. i a w B ra n c h B ra n c h B ra n c h S i. J o a c p h S t. J o n e a h *pot r^ ia a ri f 9(M3t Spot Spot 2 2 -* « i t . SS 31 9 0 10. 00 3 0. 00 3, 00 l.T N * .7 4 0 .9 0 4 .9 0 1*1 i«* 103 1*4 1*9 21 10 II 1N 8 T. 1. T. TT. 53. 53. 5SOS. M- , , , , , R. H. ft R. R 1 9W . 18W . 1«W . I« W . IT W . 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ASTM iiiii NO 39 5 = S Stt EBBSB 0 4*49 siiii 000*0 0 0-90 0 0 u . 0 £ S 0 0 ! 53883 u— a— 0 0 0 — u * 4 9 V 0 0 — O *O— H —— 0 * 0 *4 4U O9 *9 s : 1B i S ; 5 1 S £3831 4O * 0 440 0 9 OM O4 O* O 4.40. 00 a0 •9 O0 i t s i s 9 0 ssgiss i i t i t E8SS3 * *118 ssiti 33383 *9*90 0 0 •0 0 80 S80 H ASTM NO. 10 ~..... H^ .H 83388 9 4 P-* * * * a * — ..... — » M * - iiisi ooots 0 0 0 a0 A U A It(I 0 p M p U M • 9 * H H p*0 M 0 BES.S i s i i i 35*58 ***** 00000 2 TOTAL S 1 3 11 go S S B ASTM NO 60 ASTM NO 120 ASTM NO. 2 M PAN (-NO 230) TOTAL PERCENT n s £ K > 9 Z m fn * Z ► a l-H o > % > I N z nIB Gi Ci 1 j- * - I N T E R leg en d TERMINAL MORAINE V ,1 I t n J *1 GROUW) MORAINE OR TILL PLAIN OUTW ASH PLAIN LAKE BEDS AND DRAINAGE WAVS CLAV CAPPING ON OUT WASH »z ~W , ’I zV = T } -- 'v SAND DUNES deltas THIN T IL L O N OU T WASH 1 oQ* ip8 P&cS ft 2 0 W & ai4 c d w N .r o m o w c o u n t y w r a m K x u > I I I H n « a a or S t « t c M iS K W w i G * * C l P it NuTNtONT* R 10 W R 17 W R 10 W n is w n 12 W N II w 192 JTERLOBATE LI NE r^fr i i w 1//1 *#**»*’ *< t * : . ’. v . i v w , * ' ■/ « SOURCES O f INFORMATION *. *.*.■»*■■■ •> S 1, L o v a r a tt, F ra n k , P rior to 1915, M o n u c c fip t mop* G w l . S u rv e y to p o g ra p h ic trap * a n d M i c h . S ta to C o u n ty m o p b o r a , fi«W not** a n d U . S . G m I* S m o n o g ra p h 5 3 (1915), 5 2 9 p p . 2. T * r * il l ig o r , F . W # fli, 1954, M a p o f th o g l o c ta f o f V o n b u ro n C o u n ty , M ic h ig a n , G o a l* S u r . DI« M i c h . D o p t, o f C o n M rv o tio n , p u b l ic a ti o n 4 0 , 9* 3, M a r t in , H a lo n M ., 1955, M a p o f tb o s u r f a c e fori o f th o S o u th e rn P e n in su la o l M ic h ig a n a n d " o n u * m ap * , G e o l , S u r , D i v ., M ic h ig a n O o p t. o f Con* t i o n , p u b l ic a ti o n 4 9 . 4. S h a h , f a ih u M H P . , I9 6 0 , M o p o f th a S u r fa c e O* o f K o f a m a to o C o u n ty , M ic h ig a n , R e s e a rc h Labor M i c h . O o p t. o f S toto H i g h w a y . iijVtYAv.v. si oo* jgfe TIN T IN <‘V«Vv *»** / :**;*!»*> < » ♦ • K ».*•«*.tl.l R 3W w, KEY TO COUNTCS *65 SURFACE GEOLOGY OF SOUTHWESTERN MICHIGAN COWP4.EO 0* BALKUMAA R SHAH MCMQAN OCRARTMENT OF STATl HttHWWS I*TO R 10W Raw PLATE I U. S. D E P A R T M E N T O F A G R I C U L T U R E B U R E A U OF SOILS !N CO O PERA TIO N W I T H T H E MICHIGAN A GRICULTURAL E X P E R IM E N T STATION MICHIGAN K A L A M A Z O O C O U N T Y 193 S H T E T ftp lltf ilitn in e w n d r liu fu ■ a n ti; lim m b**l kefon'aine I'HIJI N ew tn n ( . I i ll lo a m y w u i l till; i*Ih> NMini C u lo tllt O ftlllf'llH l title tutiLij K tllJy lo« |kI O .lo n m llJHDL (H lilt-m o luwm Ilmji'iAii ufHNetly miriity in H LK'k ti r i l t i i ) f*MT w in ) lu»rii Manure siItj c la y (lain Hmlloa|iliaw j ” Vvr m a r l i>r i m h H t c l a y C O N V EN TIO N A L S IG N S I I S o il* a u rv a y o d b y S . O . P o r k in s o f t h o U. S O a p * rlm « n t A ^ricuiw ro, «r» c l i i f n , a n d Ja m # * T y so n , o f t h a V ic f c ig a n A g ric u ltu ra l E x p o r i m o n t S ta t io n , SAFF U S MAP C F oL O G lC A l. FROM SURVEY SHEETS CONVEN TIO N AL 5 IG N S itw