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Xerox University Microfilms 300 North Zeeb Road Ann Arbor, Michigan 48108 76-27,144 RIECK, Richard Louis, 1941THE GLACIAL GEOMORPHOLOGY OF AN INTERLOBATE AREA IN SOUTHEAST MICHIGAN RELATIONSHIPS BETWEEN L A N B F O R M S , SEDIMENTS, AND BEDROCK. Michigan State University, Ph.D., Physical Geography Xerox University Microfilms, Ann Arbor, Michigan 48106 1976 THE GLACIAL GEOMORPHOLOGY OF AN INTERLOBATE AREA IN SOUTHEAST MICHIGAN; RELATIONSHIPS BETWEEN LANDFORMS, SEDIMENTS, AND BEDROCK By Richard Louis Rieck A DISSERTATION Submitted to Michigan State University in partial fulfillment of the requirements for the degree of DOCTOR OF PHILOSOPHY Department of Geography 1976 ABSTRACT THE GLACIAL GEOMORPHOLOGY OF AN INTERLOBATE AREA IN SOUTHEAST MICHIGAN: RELATIONSHIPS BETWEEN LANDFORMS, SEDIMENTS, AND BEDROCK By Richard Louis Rieck This dissertation is concerned with the relationships between glacial landforms, glacial sediments, and the bedrock in and near an interlobate area in southeast Michigan. T h e ‘examination of well records provided a data base for mapping the bedrock surface and supplied infor­ mation on the area's glacial history. Analyses of the clay mineralogy of drift samples, using X-ray diffraction and other characteristics such as pebble lithology, color, fabric, and texture of tills, were made to identify lobe provenance. Investigations were made to determine the location of the surficial drift contact and the nature of deglaciation. Landform assemblages were identified by field investigation and study of topographic maps and air photos. The Kalamazoo Moraine of the Saginaw Lobe and the Mississinewa Mo­ raine of the Huron-Erie Lobe (possibly correlative with the Mississinewa Moraine of Indiana and Ohio) merge near the Washtenaw-Jackson county boundary. An Interlobate Moraine Tract is situated at the confluence of the moraines, and the Grass Lake outwash plain exists in the reentrant between them. Bedrock configuration influenced certain aspects of both the larger and smaller elements of the topography. A bedrock-surface map constructed from 1,482 data points shows that the two moraines are associated with the flanks of a subsurface bedrock tableland. Seven valleys, deeply burled by glacial drift and incised into the bedrock appear to be the result of fluvial erosion. Oxidized drift and organic Richard Louis Rieck material that underlie unoxidized till in these valleys indicate a non­ glacial episode of considerable length and provide evidence of multiple glaciation. Numerous linear lakes and streams are located on drift above the buried valleys and may be due to the ablation of buried stagnant-ice masses. Drifts of the Saginaw and Huron-Erie Lobes are so similar in the area it may be difficult, if not impossible, to identify the lobe prove­ nance of a till sample on the basis of such characteristics as color, pebble lithology, or texture. X-ray diffraction data of clay from forty-nine till samples and twelve glaciofluvial and glaciolacustrine samples indicate that lobe provenance may ordinarily be determined with a high degree of confidence. Magnesium-saturated, glycerol-solvated, basally oriented clays of all thirteen till samples studied from the Kalamazoo Moraine, areas proximal to it, and the associated portion of o o the Interlobate Morainic Tract had 7A/10A peak height ratios of 0.91 or more. Twenty-one of twenty-two till samples from the Mississinewa Mo­ raine, areas proximal to it, and the associated portion of the Intero o lobate Tract had 7A/10A peak height ratios of 0.90 or less. Saginaw Lobe drift produces higher ratios than Huron-Erie drift, probably due to the presence of larger relative amounts of kaolinite. On the basis of clay mineralogy the surflcial drift contact in the Interlobate Tract appears to be sharp, with little or no interdigitation of tills. Flow till is widely distributed in the Kalamazoo Moraine and ciated portion of the Interlobate Tract. Huron-Erie deposits as well. It is probably present in The presence of considerable amounts of flow till provides sedimentological evidence that ice stagnation was common during deglaciation. asso­ Richard Louis Rieck Both moraines appear to be accumulations of drift deposited pri­ marily in contact with stagnant, rather than active, ice. The Kalamazoo Moraine has a well-developed outwash apron which terminates at an icecontact slope as much as 150 feet (45 m) high. Latitudinal zonatlon in the moraine is marked by (1 ) linear depressions and ridges immediately proximal and parallel to the crest of the outwash apron, (2 ) a zone of lakes and bogs, and (3) a northern tract of linear depressions also oriented parallel with the crest. The Mississinewa Moraine is separated into two portions by the lowland of Mill Creek and conspicuous zonatlon is lacking. However, eskers and a smaller tract of linear depressions do exist. The Blue Ridge Esker trends across the Grass Lake Plain, and on the basis of sedimentary and morphologic evidence it apparently formed near the interlobate contact. Tributary eskers, physically connected with Blue Ridge and displaying a dendritic pattern, are associated with specific features in both moraines, indicating contemporaneous formation. The Grass Lake Plain is also directly related to the moraines. appears likely that, as the moraines were formed by meltwater streams at the inactive margins of the lobes, a superglacial outwash an englacial or subglacial esker Thus, it plain and system were formed distally to the moraines in contact with stagnant ice. Subsequent ablation of this stagnant ice caused superlmposltion of the glaciofluvial sediments on the subjacent material, including the esker system, to form a collapsed outwash plain. Ice-contact slopes at the confluence of the two moraines prove that their distal portions are time-correlative. A similar situation within the Interlobate Tract probably indicates that the medial or proximal portions of the moraines are also time-correlative. Two distinct landform assemblages are located In the Interlobate Moralnic Tract. Groups of linear depressions with uniform orientation, ice-contact outwash fans, and large ice-contact channel fillings are associated with the Saginaw Lobe portion of the tract; crevasse fillings and groups of linear depressions with dissimilar intergroup orientations are characteristic of the Huron-Erie portion. These assemblages are probably due to differing conditions in the stagnant ice of the two lobes. dent A line separating the two landform assemblages is almost coincio o with the boundary separating drift samples with 7A/10A peak height ratios of 0.91 or more and 0.90 or less. Thus, the evidence from two separate and distinct lines of investigation (sediments and landforms) indicates a similar location for the surficial interlobate contact. In addition, flow till, ice-contact slopes, and certain landforms indicate that stagnant-ice conditions prevailed during deglaciation. Of general interest is the finding that in certain areas the study of morphology may yield results at least as useful as those provided by investigation of sediment characteristics. Hence, those who are con­ cerned with the nature of glaciated areas may benefit from using morpho­ logical techniques as well as those that provide other meaningful in­ formation. To my loving wife Renate for her sacrifices and support ii ACKNOWLEDGEMENTS I wish to express my deepest and most sincere gratitude to my major pro­ fessor, Dr. H. A. Winters, for his patient guidance, advice, and con­ structive criticism at all stages of this study. I am indebted to the following faculty members- Dr. D. Brunnschweiler and Dr. J. R. Harman of the Department of Geography, and Dr. H. D. Foth and Dr. D. L. Mokma of the Department of Crop and Soil Sciences. They graciously served as members of my doctoral committee and gave freely of their time and counsel. I also wish to thank Dr. M. M. Mortland of the Departments of Crop and Soil Sciences and Geology for his advice and interest; the Department of Crop and Soil Sciences for laboratory space and equipment; the Department of Geography for funding the computer mapping and Mr. D. Batkins for programming assistance; Dr. C. E. Prouty and the Department of Geology for supplying well cuttings; Dr. W. A. Kneller, Department of Geology, University of Toledo, for discussions and maps; the United States Geological Survey for the loan of F. Leverett's field notebooks and maps; Dr. A. Dreimanis and Dr. R. M. Quigley of the University of Western Ontario for their discussions and interest; Mr. M. Fox of Napo­ leon, Mr. D. Lindemann of Dexter, and Mr. M. Meabon of Pinckney for well logs and information on buried organic matter; and Mr. D. P. Lusch and Mr. R. L. Dodson of the Department of Geography for their many hours of discussion both in the field and office. iii TABLE OF CONTENTS Page Chapter 1 Chapter 2 Chapter 3 INTRODUCTION Statement of Problem Definition, Concepts, and Techniques Rock Stratigraphy Morphostratigraphy Justification Study Area Literature Review Written Material- Study Area Written Material- Other Interlobate Areas Maps Summary THE BEDROCK AND ITS SURFACE CHARACTERISTICS Bedrock Maps Bedrock Characteristics of the Area Bedrock Geology Bedrock Surface Relationship of Bedrock Surface to Topography Major Buried Bedrock Valleys Location and Pattern of the Valley i Major Buried Bedrock Valleys and Associated Hydrographic Features Relationship Between Buried Bedrock Valleys and Hydrography CHARACTERISTICS, DISTRIBUTION, AND STRATIGRAPHIC SIGNIFICANCE OF THE GLACIAL SEDIMENTS Introduction Drift Thickness Subsurface Sediments Subsurface Sediments j.n the Area of the Kalamazoo Moraine Sediments Beneath the Mississinewa Moraine Sediments Beneath the Interlobate Morainic Tract Sediments Beneath the Grass Lake Plain Area Organic Matter and Oxidized Till(?) in the Subsurface Surficial Sediments Drift Associated With Kalamazoo Moraine and Related Portions of Interlobate Morainic Tract 1 1 1 3 6 7 •8 11 11 14 15 18 19 19 20 21 21 23 23 25 26 32 36 36 37 39 39 39 40 40 41 49 49 Page Drift Associated with Mississinewa Moraine and Related Portions of Interlobate Morainic Tract 86 Comparisons of Brill Lake and Chelsea Tills 99 Drift Associated with Grass Lake Plain and Related Areas 100 Chapter 4 Chapter 5 Chapter 6 GLACIAL LANDFORMS Introduction Relationship Between Bedrock Surface and the Kalamazoo Moraine Kalamazoo Moraine Crest Area Zone of Linear Depressions and Ridges Zone of Lakes and Bogs Northern Zone of Linear Depressions Portage River Lowland Relationship of Bedrock Surface and Mississinewa Moraine Mississinewa Moraine Southern Section of Mississinewa Moraine Northern Section of Mississinewa Moraine Relationship of Bedrock Surface and Interlobate Morainic Tract Interlobate Morainic Tract Relationship of Bedrock Surface and Grass Lake Plain and Associated Areas Grass Lake Plain and Associated Areas Features Located in More Than One Physiographic Section DEGLACIATION OF THE STUDY AREA Morphologic Factors Influencing Deglaciation Possible Changes in the Position of the Interlobate Contact Through Time Phases of Deglaciation Phase 1A— Formation of the Grass Lake Plain Phase IB— Formation of the Distal Flanks and Medial Portions of the Moraines and Leverett Hill Phase 2— Formation of the Proximal Flanks of the Moraines and Russell Hill Phase 3— Retreat of the Margins from the Moraines Phase 4— Completion of the Deglaciation Process Phase 5— Modification of the Landscape Since Deglaciation CONCLUSIONS AND IMPLICATIONS v 109 109 110 110 113 118 120 123 124 126 127 128 131 134 134 141 141 148 152 152 153 156 156 159 162 165 167 170 171 Page 177 Appendix A COMPILATION AND CONSTRUCTION OF BEDROCKSURFACE AND DRIFT THICKNESS MAPS Appendix B MINERALOGY OF CLAY-SIZED PARTICLES IN CERTAIN SAMPLES 181 Appendix C TILL COLOR 190 Appendix D TEXTURAL ANALYSIS 192 Appendix E LITHOLOGICAL CLASSIFICATION OF STONES 193 Appendix F TILL FABRIC 197 Appendix G LOCATIONS OF SELECTED FLOW-TILL SITES 209 LIST OF REFERENCES 210 vi LIST OF TABLES Title Page Average Drift Thickness in Study Area 38 Buried Organic Matter and Oxidized Sediments in Interlobate Morainic Tract and Vicinity 44 Buried Organic Matter and Oxidized Sediments in Grass Lake Plain Area 46 Buried Organic Matter and Oxidized Sediments Proximal to the Kalamazoo Moraine 48 5 Lithology of Surficial Boulders on Saginaw Drift 60 6 Lithology of Surficial Boulders on Huron-Erie Drift 93 7 Large Lakes and Their Neighboring Lakes 8 Locations of Landforms Situated in More Than One Morphologic Area 150 9 Well-Record-Data-Sources 173 10 Clay Mineralogy, Texture, & Color ofSelected Sediments 187 11 Color of Brill Lake and Chelsea Till Samples 190 12 Color of Grass Lake Till Samples 191 13 Pebble Lithology of Study Area Tills 194 14 Lithology of Surficial Boulders 195 15 Stone Lithology of Blue Ridge Esker 196 16 Till-Fabric Data for Site 74 200 17 Till-Fabric Data for Site 76 201 18 Till-Fabric Data for Site 78 202 19 Till-Fabric Daca for Site 79 203 3 4 vii 121 Table Title 20 Till-Fabric Data for Site 21 Till-Fabric Data for Site 81A 205 22 Till-Fabric Data for Site 206 23 Till-Fabric Data for Site 101 207 24 Till-Fabric Data for Site 104 208 25 81 Page 97 Locations of Selected Flow-Till Sites viii 204 209 LIST OF FIGURES Title Page Location of the Study Area 9 2 Study Area 10 3 Bedrock Lithology 22 4 Bedrock Surface 5 Major Buried Bedrock Valleys and Associated Hydrographic Features 24 Generalized Cross-Section of the Buried Bedrock ValleyHydrography Relationship 27 6 in pocket 7 Drift Thickness in pocket 8 Sediments and Relief in pocket 9 Sites and Ratios for X-Ray Diffraction Samples 52 10 Surficial Drift Contact in Interlobate Morainic Tract 54 11 Textures of Tills in and Proximal to Moraines 57 12 Pebble Lithology of Saginaw Drift in and hear Study Area 58 13 Boulder Distribution 61 14 Till Fabric 63 15 Stratigraphy at Brill Lake Pit 16 Exposure in East Wall of Brill Lake Pit 71 17 Close-Up of Massive Flow Till 71 18 Massive Flow Till 73 19 Stratified Flow Till 73 ix (Site 81) 69 Title Page Interfingering of Massive Flow Till and an Unbroken Outwash Sequence 76 21 Close-Up of Exposure in Figure 20 76 22 Flow Till in Morainic Areas 79 23 Lacustrine Sediments 82 24 Pebble Lithology of Huron-Erie Drift in and near Study Area 92 25 Section in a Deposit of Lacustrine Sediments 97 26 Surficial Drift Contact in Southwest Portion of Study Area 102 27 Textures of Tills on and near Grass Lake Plain 106 28 Local Relief 111 29 Maximum Altitudes 112 30 Diagram of a Portion of the Kalamazoo Moraine 114 31 Schematic Profiles of Kalamazoo Moraine Crest Area, East of Brill Lake 115 32 Selected Landforms 33 Diagram of a Portion of the Mississinewa Moraine 129 34 Diagram of Interlobate Morainic Tract 136 35 Diagram of Grass Lake Plain and Associated Areas 142 36 Possible Location of Saginaw and Huron-Erie Lobe Margins Prior to Cessation of Flow 155 Location of Saginaw and Huron-Erie Lobe Margins at Cessation of Flow 155 38 Phases 1A and IB 157 39 Simultaneous Formation of Superglacial Outwash Plain and Esker 160 40 Site of Figure 39 After Deglaciation 160 41 Phase 2 163 37 in pocket x Figure Title Page 42 Phase 3 166 43 Phase 4 168 44 X-Ray Diffractograms 184 xi Chapter 1 INTRODUCTION Statement of Problem This study is concerned with the nature and relationships of the glacial landforms and sediments at and near a segment of the Saginaw and Huron-Erie interlobate area in southeastern Michigan.^ The major objectives of this study are listed below: 1. To determine what relationship, if any, exists between the nature of the bedrock surface beneath the drift and the glacial landforms of the study area ; 2. to describe the characteristics, extent, and contact relationships of the surficial drifts associated with the Saginaw and Huron-Erie Lobes and to specify on what basis the drifts may be identified and delineated; 3. to determine the characteristics and assemblages of the various landforms in and near the interlobate area; 4. to determine, on the basis of landforms and sediments, the nature of deglaciation in the area and its effects upon the landscape. Definition, Concepts, and Techniques Chamberlin (1883A, p. 276) introduced the term "interlobate moraine" for a feature formed "by two glaciers pushing from opposite directions" and (1883B, p. 301) "by the joint action of two glacial lobes pushing their marginal moraines together, and producing a common ^"The study area is defined on page 8 and illustrated in Figures 1 and 2 . 1 one along the line of their contact." Modern definitions of interlobate moraines by T h o m b u r y (1969, p. 381) and Flint (1971, p. 200) do not emphasize quite as strongly the requirement that interlobate moraines be formed by lobes in contact with one another. Nevertheless, relatively.strict definitions such as these present problems in application. For example, if the lobes part slightly and are separated by an open valley when drift deposition takes place, is the feature formed an interlobate moraine? Alden (1918, p. 309) considered such a situation in the Kettle Interlobate Moraine of Wisconsin and stated that "no strictly interlobate deposition took place." Alden (1918, pp. 275, 308) also noted areas in the Kettle Moraine where one of the lobes continued to hold a stable marginal position and deposit drift after the margin of the other lobe had to retreat. begun Here the compound feature formed is not entirely inter­ lobate in origin as a portion of it was deposited after the lobes were no longer in contact. Black (1970, p. 37) hypothesizes that much of the Kettle Moraine was deposited not at the contact of two lobes but rather at the outer margins of the active ice which were separated by a zone of stagnant ice. Chamberlin (in Alden, 1918, p. 14) realized that interlobate areas may be complex and noted, "There are grades and degrees of interlobateness and corresponding degrees of interlobate moraines." Therefore, a narrow definition of the term "interlobate moraine" is of limited value especially in areas where the chronological details of deposition are not clear. Consequently, a more general definition of interlobate moraine will be used for this dissertation: a drift accumulation depo­ sited in or near the reentrant between (two) lobes of ice; it may have formed at a time when both glaciers were in contact or when the active ice margin(s) had retreated a distance of one to several miles (1.6 to several kilometers), exposing a narrow zone between them. In this study the geomorphic characteristics of a complex area are described and interpreted on the basis of the nature of the topography and characteristics of the underlying sediments. The related concepts of morphostratigraphic units and rock-stratigraphic units are also utilized in this investigation because they are concerned with the stratigraphic significance of form and sediment (Frye and Willman, 1962). Both concepts have been applied in studies in other areas (for example, see Willman and Frye, 1970) and have provided a workable basis for ex­ tensive investigations of glacial landforms and sediments. The nature of rock-stratigraphic and morphostratigraphic units is discussed below along with the techniques which provide the data used to identify such units. Rock Stratigraphy The American Commission on Stratigraphic Nomenclature Code (1961, p. 649) has defined a rock-stratigraphic unit as "a subdivision of the rocks in the earth's crust and delimited on the basis of lithologic characteristics. . . . Rock-stratigraphic units are recognized and de­ fined by observable physical features rather than by inferred geologic history." Willman and Frye (1970, p. 45) state that in reference to the Pleistocene the purpose of rock-stratigraphic classification is to "deal with the surficial deposits . . . on the basis of their physical char­ acteristics, to identify and map the different types of rock units, and to understand their variations and interrelations." Rock-stratigraphic units have been formally defined in such nearby states as Illinois, Indiana, and Ohio (for example, see Willman and Frye, 1970; Wayne, 1963; and Goldthwait and others, 1965). However, little work has been done on defining rock-stratigraphic units in Michigan. This study will provide at least a partial basis for the identification of two rock-strati­ graphic units that exist within the area investigated. One of the principal objectives of the rock-stratigraphic portion of this investigation is to locate the surficial drift contact of the Saginaw and Huron-Erie Lobes. Till is generally deposited at or very near the place it was released from glacial ice. 2 Therefore, if a surficial till body situated near the drift contact can be identified as to its provenance, it will provide evidence that ice from a particu­ lar lobe occupied that location or was very close by during final de­ glaciation of the area. With a sufficient number of such sites it may be possible to delineate the surficial contact between Saginaw and Huron-Erie drift. Till Texture Grain-size analysis has long been used as a basis for the descrip­ tion and differentiation of tills in the Midwest and other areas (see discussion by Drelmanis and Goldthwait, 1973, p. 75) and is one of the criteria that may be used to define rock-stratigraphic units. Textural analyses of surficial sediments from within the study area have been performed in conjunction with soil surveys and the investigation of glaciofluvial sediments, but to the author's knowledge none have been 2 An exception would be till that sloughed off an ice margin and moved downslope before final deposition. Such a till body would have moved only a short distance. Till transported by an iceberg in a water body deposited far from the point of calving from the glacier is an­ other exception. determined solely for the differentiation or correlation of tills. Therefore, one objective of this dissertation is to consider till differentiation by using textural analysis. Stone Lithology Identification of the lithology of sedimentary particles is a well-established technique that has been used to determine the prove­ nance of glacial till (Flint, 1971, pp. 174-75). Anderson (1957) did this for stones within Saginaw and Huron-Erie tills along two traverses which were located a considerable distance from the drift contact. This dissertation provides data on the lithology of certain coarse elastics from the area shown on Figure 2. Till Fabric The orientation of clastic particles within till is referred to as its fabric and may be useful to determine the former flow direction of glacial ice associated with the sediment. Very few fabric determi­ nations have been published for Michigan tills, and none of these are from the area considered in this investigation. This study utilizes a number of till— fabric determinations to provide a better understanding of the relationships between ice-flow directions and environment of till deposition in and near the Saginaw/Huron-Erie interlobate area in a portion of southeastern Michigan. X-Ray Diffraction of Clays X-ray diffraction techniques have been used in numerous studies to differentiate glacial sediments. For example, studies published by the Illinois Geological Survey have utilized clay-mineralogy data to differentiate drifts of differing ages and extent (see discussion by Frye, 1968). Also an interlobate contact between two surficial tills in Illinois has been located, partially through the use of clay mineral­ ogy (Castillon, 1972). The mineralogical characteristics of Michigan tills are not well known. The only detailed study (Mahjoory, 1971) of which the author is aware utilized X-ray diffraction to determine clay mineralogy in soil lithosequences and toposequences in areas of Michigan not shown on Figure 2. X-ray diffraction techniques are used in this dissertation to provide a basis for identification and differentiation of Saginaw and Huron-Erie tills in southeastern Michigan. Morphostratigraphy Frye and Willman (1962) have defined a morphostratigraphic unit as "a body of rock that is identified primarily from the surface form it displays; it may or may not transgress time throughout its extent." The use of morphostratigraphic units may provide Increased detail and under­ standing in Pleistocene studies and complement time, soil, and rockstratigraphic units. fined in Michigan. No formal morphostratigraphic units have been de­ This study will define the extent of two moraines that converge to form an interlobate area, and these may provide a basis for the future definition of morphostratigraphic units. Map and Air Photo Interpretation Topographic maps and air photos are useful tools for the glacial geomorphologist, and both have been utilized in this study. They pro­ vide insights into aspects of spatial and hypsometric relationships that are difficult to observe directly in the field. The largest-scale topo­ graphic maps available and 1:15,840 scale air photos (stereo coverage) were used in the investigation. 7 Justification Interlobate regions and their associated drift contacts are ex­ tensive and constitute a significant portion of the glaciated area in the Midwest. The landforms and their assemblages in these areas have received relatively little attention, and in the only extensive study on the topic in the Saginaw/Huron-Erie interlobate area of Michigan Kneller (1964) grouped at least seven separate landforms into one mapping unit. Problems related to the study area and the need for further research have been recognized previously. For example, in their study of the Ann Arbor quadrangle Russell and Leverett (1908, p. 5) stated, The features built along the line of retreat of the junction of the ice lobes are complicated and their study in detail will probably help to show the mode of development of interlobate moraines. Indeed, the portion of the interlobate tract that falls within the limits of this quadrangle not only well illustrates in its variety of topographic features the character of the great belt of which it forms a part, but serves as a fair sample of the usual diversity of interlobate areas in other places. In a review article on the Pleistocene of Michigan and Indiana Wayne and Zumberge (1965, p. 71) wrote, Interpretation of the history of deposition of the complex inter­ mingling of tills, outwash sediments, and lake deposits in the northern part of Indiana and in southern Michigan posed problems for Leverett, which have not been worked out adequately to this day. Typical tills from the three lobes can be distinguished without difficulty, but in the interlobate areas where they intertongue with each other, their identification becomes increasingly difficult. Kneller (1964, p. 26) called for work associated with the tills of the area by stating that "more detailed study of till lithologies is needed to define any stratigraphic relationships existing between Saginaw and Erie lobe deposits." This investigation utilizes several techniques to determine the relationships that exist between glacial topography and the underlying sediments. The results may provide information on the nature of de­ glaciation in the area, its effects on the landscape, and, in turn, how it may have been affected by the underlying bedrock. In addition, the findings may also add significantly to our knowledge of landforms, drifts, and drift contacts in and near interlobate areas and of certain relationships between the Saginaw and Huron-Erie Lobes. Study Area The study area is centered at the contact of Saginaw and HuronErie drift (Figure 1) and contains about 400 square miles (1,000 square 3 km). Two topographic trends, interpreted as moraines by early workers, converge at Leverett Hill 4 in northwest Washtenaw County (Figure 2). One of these trends northeast from the city of Jackson and has been named the Kalamazoo Moraine (Leverett and Taylor, 1915, p. 189) of the Saginaw Lobe. The other feature trends north-northeast from near Norvell and has been mapped by the same workers as a moraine of the Huron-Erie Lobe. Adjacent to Leverett Hill, their point of confluence, is a plexus of forms, interpreted by Russell and Leverett (1908, p. 5) as an interlobate morainic tract that extends northeast about 12 miles (20 km) to Pinckney in Livingston County. An outwash plain, the Grass Lake Plain, has been mapped in the reentrant between the morainal trends. 3 Approximate metric equivalents will be given throughout this report. 4 A feature unnamed on the Stockbridge quadrangle and located in portions of secs. 28, 32, and 33, T. 1 S . , R. 3 E. and sec. 5, T. 2 S., R. 3 E. This Informal designation of "Leverett Hill" is given only to facilitate identification and is not formally proposed as a geographic name. As shown on the Stockbridge quadrangle, Sugarloaf Hill is a knob on the west flank of Leverett Hill. 9 MORA1NIC S YSTEM S OF MICHIGAN Figure 1. Location of the Study Area 10 W 1ILUJIIIJ n * ‘ A WSBS * ' PINCKNEY W.T.E.P.I.P.BATE \4 M O R A IN I ft H+M• • • • •«* • * • m * m mmsm 0 : : : : : :-h-I JACKSON PLAIN W 0, n o r v e ll^ ^ ^ STUDY cm lW ^ M a n c h e s te r: :: : : : AREA MORAINE p* PORTAGE TILL a» HURON RIVER OUT WASH ** GRAND R IV ER E SKE R T R A N S I T I O N A L MORAINE BOUNDARY ** RIVER PLAIN ...... ri‘* V l'l RIVER RAISIN miles 10 kilometers SOURCES: F ig u r e 2. Study Area TH IS INVESTIGATION a MARTIN (1955) 11 Literature Review Written Material- Study Area In general, nineteenth-century works that treated the study area were concerned with reconnaissance mapping of surface formations at a statewide scale. Studies from the early part of the twentieth century which treated individual landforms were apparently based on a deglacia­ tion model which did not include several aspects of ice stagnation. The most recent works dealing with the area concentrated on sand and gravel characteristics or subsurface stratigraphy and treated landforms to a lesser degree. Only works that contributed significantly to the writer’s understanding of the area are cited in the following chronological re­ view of written material. In 1876-77 and 1883 Chamberlin presented short descriptions of the landforms in the area and in the latter publication (1883A) intro­ duced the term "interlobate moraine." Frank Leverett, who began field work in the area in 1887 and returned intermittently for over fifty years, compiled many field notes that are on file at the United States Geological Survey library in Denver. obtained on loan. A number of these notebooks were In addition, a limited number of his field notes have been transcribed and are in the library of the Michigan Geological Survey in Lansing. Alfred Lane noted the sandy nature of the moraines in the area and also the effect of ice-margin movement on interlobate reentrants (1899). Shortly after the turn of the century Frank Leverett, either alone or in collaboration with others, authored several publications treating the glacial landforms and geology of the study area. They include (1) the Ann Arbor Folio of the Geologic Atlas Series (Russell and 12 Leverett, 1908, and reprinted in a revised edition in 1915), which dealt with the Ann Arbor quadrangle (1:125,000) and included a part of the Interlobate Morainic Tract considered in this study; (2) a publica­ tion on surface geology and agricultural conditions in Michigan (1912, revised and reprinted in 1917), which referred to the moraine trending northeastward from Jackson as the Jackson Moraine; (3) and the most important, his monograph with Taylor, published in 1915, concerning in part the Pleistocene formations of Michigan. This is the only publica­ tion to provide a description and interpretation of the entire study area both in restricted and regional perspectives. In the monograph Leverett interpreted the north-northeast-trending moraine as part of the Mississinewa^Moraine of Ohio and Indiana, associated with the Huron-Erie Lobe and correlative with the Jackson Moraine of the Saginaw Lobe, which he renamed "Kalamazoo" (p. 189). Several features within the study area were investigated in the 1920s and 1930s. Scott's 1921 volume on the inland lakes of Michigan presented an interpretation of the origin and history of several lakes in the interlobate area. Newcombe and Lindberg (1935) suggested a possible relationship between bedrock features and surficial topography in southeastern Michigan. And a glacial history of streams in and near the study area was the topic of a paper by Bay (1938). New evidence bearing on the glacial history and geomorphology of southeastern Michigan and the study area was introduced in a 1960 ^Leverett and Taylor (1915) and Martin (1955) referred to this moraine as the Mississinewa. Later workers, Zumberge (1960) and Wayne and Zumberge (1965) , have deferred using this name until the question of correlation with the Mississinewa of Indiana and Ohio is answered. The term "Mississinewa Moraine" will be used in this investigation, but it should be noted that the problem recognized by Wayne and Zumberge has not been resolved. 13 article by Zumberge. He stated that some of Leverett's field notes In­ dicate that ice of the Erie Lobe overrode Saginaw drift in northeastern Indiana. Zumberge also reported that till of the Erie Lobe overlies Saginaw till at a place about 10 miles (16 km) south of Norvell in Lenawee County, Michigan. If Zumberge's interpretation is correct, it indicates that at one time the Saginaw Lobe held a position farther to the east than that indicated in Leverett and Taylor (1915). To explain this situation, Zumberge postulated a retreat of the Saginaw ice margin accompanied or follow&d by a westward advance of the Erie Lobe, resulting in the deposition of Erie till over the Saginaw drift. A review article by Wayne and Zumberge (1965) reiterated both this interpretation and Zumberge's belief that regional correlation of the Mississinewa with other Huron-Erie moraines to the southwest was impossible at that time due to the lack of field data from Branch, Hillsdale, and Lenawee Counties. Kneller (1964) investigated the sand and gravel deposits of Wash­ tenaw County and on the basis of pebble lithology was able to distin­ guish two lithologic groups which he interpreted as being Saginaw and Huron-Erie drifts. He concluded that exposures within a number of gravel pits in the eastern part of the county revealed Huron-Erie till overlying Saginaw gravel, in agreement with Zumberge's interpretation. Kneller did not discuss the Mississinewa Moraine, but did state (p. 35) that "Moraine-like ridges composed of stratified drift . . . formed . . . in the reentrant angle between the Saginaw and Huron-Erie lobes." These ridges are situated in T. 1 S., R. 3 E. and T. 3 S . , R. 3 E . , the townships in which the Mississinewa Moraine is located. He also stated (p. 36) that the pebble lithology in these ridges is intermediate 14 between the assemblages characteristic of both lobes. Written Material- Other Interlobate Areas Several studies from other portions of the Midwest provide valu­ able information on interlobate landform assemblages and deglaciation processes. Some of these also treat drift discrimination in interlobate areas. In 1918 Alden authored a comprehensive work describing the results of his reconnaissance of the Kettle Interlobate Moraine in Wisconsin. This remains one of the most notable works available on interlobate moraines of the Midwest and describes a number of landforms that exist in and near the former reentrant between the Green Bay and Lake Michigan Lobes. Black (1969) summarized many of Alden's previous findings regard­ ing the Kettle Interlobate Moraine and in the following year (1970) pre­ pared a field— trip guide on the Kettle Moraine, in which he postulated a sequence of events involving glacial thrust-faulting and the eventual formation of superglacial drift to explain the parallel moraines with medial lowland observed within the area of Kettle Moraine State Park. In a study detailing the glacial geomorphology of a quadrangle in the Lake Michigan-Saginaw interlobate area of southwestern Michigan, Folsom (1971) discovered abundant evidence of ice stagnation. He, as well as Black (1970), noted that an interlobate contact may be marked by two sets of hills bordering an intervening lowland. Concurrently Shah (1971) utilized relative proportions of lithologic types within glaciofluvial deposits to delineate the contact of Lake Michigan and Saginaw drifts. Folsom and Shah independently suggested a similar location for the interlobate contact within a certain area of south­ western Michigan. 15 Castillon (1972) investigated the relationship between till fabric and landforms in an interlobate area in east-central Illinois. He found that the till fabrics associated with two moraines converging at a low angle tend to be parallel with the long axes of the features rather than being perpendicular as one might expect. He was able to differentiate and delineate the surface drift contact by using X-ray diffraction to determine the clay mineralogy of the tills in the moraines. Maps Early landform maps of the study area were very generalized and were produced at a relatively small scale. Some of these maps by Cham­ berlin (1876-77 and 1883) and Taylor (1897) show a single Saginaw/ Huron-Erie interlobate moraine extending from Indiana to the vicinity of Lapeer, Michigan. The first glacial— landform map of the Lower Peninsula was pub­ lished at a scale of 1:2,000,000 and was included in an 1899 watersupply paper by Lane (Leverett, 1904, p. 107). Lane showed certain converging features in the study area in approximately the location of the major moraines as subsequently mapped, but the legend described them as the "overwash and interlobate gravels" of a "dissected sand and gravel plain." The first rather detailed surface— formation map (1:375,000) of the Lower Peninsula was by Nellist (1907) and shows converging landforms in southeastern Michigan in a pattern similar to that which appears on most later maps. moraines." The legend identifies such features as "gravelly or sandy In the following year, and also seven years later, the Ann Arbor Folio by Russell and Leverett (1908 and 1915) was published and contained a surface— formation map (1:125,000) showing a portion of the interlobate moraine extending northeast from Pinckney. The most 16 conspicuous landforms shown within this area are two moraines labeled "Interlobate Moraine, Saginaw Lobe" and "Interlobate Moraine, HuronErie Lobe," which are separated by the lowland of the Huron River. A map of the Lower Peninsula (1:1,000,000) by Leverett (1912) depicted the converging moraines in the study area as bordered by both outwash and till plains. Plate 32, accompanying Leverett and Taylor's 1915 monograph, is a map (1:2,000,000) that clearly identifies the con­ verging trends as the Kalamazoo and Mississinewa morainlc systems. A later surface— formation map by Leverett (1924), at a scale of 1:750,000, shows slight modification from the 1915 map, but the overall pattern remains essentially unchanged. A number of Leverett's field maps of differing dates are on file at the United States Geological Survey library in Denver. Three of the maps, at scales of 1:63,360, 1:85,000, and 1:178,200, showing portions of the study area, were obtained on loan. Some of Leverett's manuscript maps of the area are on file at the Mich­ igan Geological Survey in Lansing and in the Department of Geology at the University of Michigan In Ann Arbor. These are colored landform maps on topographic-map bases and have various dates associated with them. A Jackson County soil survey (Veatch, Trull, and Porter) was pub­ lished in 1930, although the map accompanying it is dated 1926.** A soil— survey map for Livingston County (Wheeting and Bergquist, 1928) has re­ cently been updated by a detailed soil survey (Engberg and Austin, 1974), although only advance sheets were available during the field-mapping and data-analysis phase of this investigation. The Washtenaw County soil map of 1930 (Veatch, Wheeting, and Bauer) has also been recently updated g A detailed survey of the county is in progress, but not enough has been completed to aid substantially in this investigation. 17 by a detailed soil survey. Here, too, advance sheets were utilized. Since the 1930s the Michigan Department of Natural Resources has produced hydrographic maps of many of the lakes in the study area. These maps may be useful in determining bottom trends and provide data indicative of minimum thickness for ice blocks which eventually melted to form lakes. Martin's (1955) 1:500,000 surface— formation map is probably the most-cited glacial map of the state at this time. This map shows a pattern in the study area similar to that first presented by Nellist in 1907. A chart on Martin's map correlates the Saginaw Lobe's Kalamazoo Moraine with the Mississinewa Moraine of the Erie Lobe. A number of Martin's manuscript maps (on topographic-map bases) are available for inspection at the Michigan Geological Survey. The converging moraines of the study area are clearly shown on a map by Zumberge dated 1960. On this map he identified the Kalamazoo Moraine of the Saginaw Lobe, but did not name the converging moraine of the Huron-Erie Lobe. In the same year Kunkle (1960) produced a surface— formation map of Washtenaw County showing, but not naming, this same Huron-Erie moraine. Kneller included a surface-formation map superimposed on a 1:62,500 topographic-map base in his 1964 investigation. Although recognizing the presence of kames, kame terraces, interlobate kame moraines, eskers, crevasse fillings, outwash fans, and outwash cones in the accompanying text, Kneller did not differentiate the features on his map but included them in a group labeled "ice contact deposits." Wayne and Zumberge (1965) provided a map which again shows two converging morainal trends within the study area. However, the moraine associated with the Huron-Erie Lobe was not named, and only the part of 18 the Kalamazoo Moraine associated with the Lake Michigan Lobe was labeled. Summary The pre-1900 works dealing with the study area provided a histor­ ical perspective on the subject of interlobate areas. Taylor's monograph Leverett and (1915) presented a synthesis of the deglaciation of the region at both local and regional scales. Leverett's field notes were especially helpful in providing information on exposures which are no longer available and for descriptions of areas which in the past were under cultivation but are now wooded, obscuring vision. In addi­ tion, his unpublished notes contained an interpretation of the driftcontact location in the Interlobate Morainic Tract. Recent studies treating other drift-contact areas were helpful in providing on differing interlobate situations. Recent works insights concerned with the study area provided quantitative data on the sediments and suggest a possible local history for late Wisconsinan events. Chapter 2 THE BEDROCK AND ITS SURFACE CHARACTERISTICS Bedrock Maps Maps of the bedrock and its surface were published for part or all of the study area by Russell and Leverett (1908 and 1915) and Leverett and Taylor (1915), but these were based on rather limited data. The two maps by Russell and Leverett, with approximate scales of 1:500,000 (1908) and 1:390,000 (1915), also show a number of spot altitudes on the bed­ rock surface. Leverett and Taylor's 1915 map is at a scale of 1:1,000,000 and depicts the bedrock surface with 100-foot (30.5-m) con­ tours. A "Bedrock Map of the Southern Peninsula" (1:500,000) by Martin, published in 1936, most probably represents an improvement over the earlier maps. It shows the lithology, age, and the general northeast- southwest trend of bedrock formations that are believed to exist beneath the drift within the study area. In the east and southeast portions of the area Martin mapped the uppermost preglacial bedrock as the Mississippian Coldwater Shale. Her map shows successively younger Missis- sippian formations toward the west— the Lower Marshall and Napoleon Sandstones and scattered bodies of the Michigan Formation and Bayport Limestone. Still farther west Martin mapped the Pennsylvanian Parma Sandstone and Saginaw Formation. An incomplete, unpublished manuscript map of the bedrock surface of Jackson and Calhoun Counties by Barwick (1958) is on file at the Geological Survey of Michigan in Lansing. On the basis of interviews with water-well drillers Barwick obtained infor­ mation on 363 wells in the Jackson County portion of the study area. He plotted well depth, bedrock lithology, and driller’s name at the 19 20 appropriate location on the 1:63,360 map. In 1959 Moore completed a thesis concerned with Livingston and Shiawassee Counties, including subcrop maps, contour maps of the bedrock surface, and drift isopach maps, all at a scale of 1:63,360. Kunkle (1960) constructed bedrock-lithology, bedrock-surface, and drift-thickness maps for all of Washtenaw County and a small portion of Livingston County. The portion of Kunkle's map showing the westernmost two ranges of townships in Washtenaw County (288 square m i l e s , or 745 sq km) was based on 11C well logs with seven additional logs from Livingston County. His subcrop map shows that the contact between Coldwater Shale and the Michigan—Marshall Formation is located approximately along the eastern boundary of Tps. 1-2 S., R. 3 E. Bedrock Characteristics of the Area County maps of the bedrock surface completed prior to this study were based on no more than a few hundred well records and interviews. Kunkle (1960) had data from 117 points in a portion of Livingston County and the western two ranges of townships of Washtenaw County. In the Livingston County portion of the study area Moore (1959) compiled data from 84 points. In addition to these 201 data points, appropriate well records and information on file at the Geological Survey of Michigan which dealt with the study area were investigated. Furthermore, pub­ lished and unpublished sources of information were consulted, and a limited number of interviews conducted. This resulted in a more than sevenfold increase (from 201 to 1,482) in the number of well logs avail­ able for map construction (see Appendix A for details of well-record data). 21 Bedrock Geology Figure 3 depicts the bedrock lithology of the area as determined by the data from 1,482 points. Due to the limited descriptions of water- well records, only lithologic units, not rock-stratigraphic units, are shown on the m a p . Bedrock Surface The bedrock surface of the region may be divided into three northeast-southwest-trending sections (Figures 3 and 4). These are (1) an area in the southeast, generally below the 850-foot (259.1-m) contour and underlain by the Coldwater Shale; (2) a higher (850 to 1,050 feet, or 259.1 to 320.0 m) surface underlain by sandstone within the central portion of the study area;^ and (3) a slightly lower tract in the north­ west with a surface altitude of 800 to 950 feet (243.8 to 289.6 m) underlain by shale, sandstone, and limestone. A number of buried bed­ rock valleys apparently begin on or near the sandstone tableland and trend southeast to the shale lowland. Russell and Leverett (1908, p. 3) stated that the sandstone table­ land has an east-facing escarpment with the top of the sandstone 100 to 200 feet (30 to 60 m) higher than the Coldwater Shale on the southeast. Details of Figure 4 indicate that the term "escarpment" may not be entirely appropriate because in most locations the contact between sandstone and shale is marked by a moderately sloping surface rather than a steep or abrupt slope as the term "escarpment" might indicate. "^Russell and Leverett (1908, pp. 2— 3) named this the "Marshall tableland," as it is a high area of relatively low relief underlain, at least in part, by the Marshall Sandstone. In this study the term "table­ land" will be used, but, because the Marshall Formation is not the only rock unit involved, it will be identified as the "sandstone tableland." 22 TIN R IE TIN Livingston C R3E R2E R4E TIS TIS T 2S T2S T3S T3S T4S T 4S o RIE R2E R3E BEDROCK 1 S H ALE 2 SANDSTONE 3 LIMESTONE R 4E LITHOLOGY milss 10 Km 4 PREDOMINANTLY SHALE (SOME SANDSTONE PRESENT) 5 PREDOMINANTLY SANDSTONE (SOME SHALE PRESENT) MAJOR llr *76 Figure 3. S0U R C ES: W E LL RECORDS, BARWICK (1958), MOORE (1959), KUNKLE, I9 6 0 ) Bedrock Lithology 23 However, there is little doubt stone that the surface is well over 100 feet (30 average altitude ofthe sand­ m) higher than thatof the lower area to the southeast underlain by shale. Relationship of Bedrock Surface to Topography The sandstone tableland, tour, outlined by the 900-foot (274.3-m) con­ is a blunt, wedge-shaped feature with its apex to the northeast. A comparison of Figures 4 and 8 shows that a strong relationship exists between this higher bedrock surface and the present landscape. From Jackson to Leverett Hill the distal flank of the Kalamazoo Moraine nearly coincides with the 900-foot (274.3-m) contour of the bedrock sur­ face. Although not as well defined as the distal side of the Kalamazoo Moraine, the outer flank of the Mississinewa Moraine is also very near the location of the 900-foot (274.3-m) bedrock contour. Thus, it may be concluded that the two moraines are situated on the north and east edges of the sandstone bedrock high and that the tableland itself underlies the Grass Lake Plain and associated areas of till plain. 2 Major Buried Bedrock Valleys A number of well-developed valleys, trending southeast, are assoc­ iated with the surface of the bedrock underlying the drift (Figures 4 and 5). The pattern of these buried valleys and their tributaries in­ dicates a fluvial origin. They were probably formed, for the most part, in preglacial time, though glacial modification and interglacial erosion may have taken place. The largest valley systems appear to originate within the sandstone, and, if this interpretation is correct, the 2 The relationship between bedrock features, the moraines, and the Grass Lake Plain will be described in greater detail in Chapter 4. 24 Livermore Cr. School L. I*-£ Honey Cr. G r e g o r y . C 2 ^ ^ IN C K N E m H s W 'msvillelS^^b^?^ ckn • Unadilla ^ el* .33 "Ztf&^Ha/fmoonL: Ellsworth L. Blind | L ^J^North L DEXTER V A L L E Y ^ S - / ^ Huron R. I Island L. ANN ARBOR CHANNELt;:* Portage L. I W: South L Clear L K a Pond Lily L. North Welch L B rill L .'.ji LIMA VALLEY Tims L. ? 2 ji\Grass L . ^ ^Gi/lefts L. Center L. \^iyndP.j^j:( J Dollar L. Oicott L. Wolf L. Little Wolf L. I BRIDGEWATER CHANNEL Ackerson Norvell River Raism Sa/ine N O R VELL/J ’VALLEY Brooklyn BROOKLYN VALLEY Mp. vineyard RIE I MAJOR BURIED B E D R O C K V A L L E Y S AND AS SOC IA TE D HYDROGRAPHIC FEATURES 25E SURFIC IA L TRACE OF BURIED BEDROCK V A LLEY miles Figure 5. Major Buried Bedrock Valleys and Associated Hydrographic Features streams that cut them flowed southeast to the lowland underlain by Coldwater Shale. Figure 4 reveals that at least two of the valleys have nearly right-angle turns along their courses and that many of the tribu­ tary valleys have trends normal to those of the main channels, giving the appearance of a somewhat angular drainage pattern. Location and Pattern of the Valleys Rhodehamel (1951) reported an angular pattern of bedrock valleys in the subsurface of the Saginaw Lowland of Michigan. He noted (p. 90) that Kelly had described a system of intersecting joints within Carbon­ iferous rocks at Grand Ledge with trends of about N. 50° E. and N. 50° W. buried bedrock valleys in the Saginaw Rhodehamel concluded that the area had trends similar to the joints described by Kelly. In those areas where Carboniferous rocks do not subcrop, but are covered by younger, possibly unjointed rocks, the bedrock valley pattern does not exhibit angular drainage (Rhodehamel, pp. 90-91). This suggested to Rhodehamel that joints controlled, or at least strongly affected, the development of the bedrock valleys. Ferris, Burt, Stramel, and Cros- thwaite (1954, p. 34) suggested that an angular drainage pattern may be present on the bedrock surface of Oakland County. Kunkle*s 1960 bedrock surface map for Washtenaw County displays well-developed northeastsouthwest and northwest-southeast angularity. Vanlier, Wood, and Bru- nett (1973) produced a bedrock-surface map for Eaton, Ingham and Clinton Counties, trends. which also shows an angular drainage pattern with similar If a fracture system exists in Jackson and Washtenaw Counties, it may have been an important factor in the development of the angular system of bedrock channels. The fracture pattern in the sandstone at Napoleon and research by Prouty (1975) support this interpretation, but 26 with the limited data available no definite conclusions can be drawn at this time. Ice flow from the Erie basin probably tended to parallel the trend of the bedrock valleys and may have resulted in a certain amount of widening and deepening in some places. However, the narrow, angular nature of some channels within areas of sandstone may indicate that the amount of glacial modification was minimal. Furthermore, organic matter and material interpreted as oxidized till are present at depth in certain buried valleys and suggest that at least sometimes deposition, not erosion, was dominant there during glaciation. 3 The age (or ages) of the bedrock valleys is not definitely known. If the interpretation that buried oxidized till exists in the valleys is correct, the valleys must predate that till and may therefore be pre­ glacial in age. It is also possible that they are, at least in part, Pleistocene in age and may have continued to develop or experience modi­ fication during Pleistocene time before (final) burial. Kunkle (1960, p. 72) noted that certain bedrock valleys in Washtenaw County are simi­ lar in size to the Teays and Mahomet Valleys of Indiana and Illinois. He considered (p. 122) the possibility that they may all be of approxi­ mately the same age, which is "thought to be Tertiary or early Quater­ nary." Major Buried Bedrock Valleys and Associated Hydrographic Features Seven major buried bedrock valleys are identified on Figures 4 and 5 and are named for their proximity to geographic features. In most parts of the study area the bedrock surface Is overlain by more than 50 3 The organic matter and oxidized till(?) are discussed in detail in Chapter 3. 27 feet (15 m) of drift. However, the bottoms of the valleys are often 150 feet (45 m) lower than the surface of neighboring bedrock, resulting in an overlying drift thickness of more than 200 feet (61 m) in some places. Nevertheless, these bedrock valleys buried beneath the drift appear to have had some influence on hydrographic features at the sur­ face. This is evidenced by a number of streams and lakes that are located directly above them (Figure 6). Descriptions of the valleys and their associated hydrographic relationships are given below. LAKE OR STREAM 5 0 feet D R IF T 200 D R IF T feet BEDROCK BEDROCK Figure 6. VALLEY BEDROCK Generalized Cross-Section of the Buried Bedrock ValleyHydrography Relationship Brooklyn Valley Brooklyn valley is located primarily in the southwest portion of T. 4 S., R. 2 E . , and originates near Brooklyn within the sandstone tableland (Figures 4 and 5). An apparent lack of headwater tributaries may be the result of an insufficient number of well records to define fully the drainage pattern. Near Brooklyn the bottom of the valley is more than 150 feet (45 m) lower than the surface of the adjacent 28 sandstone, but farther southeast it is only about 100 feet (30 m) lower than the surface of the Coldwater Shale. Although drift associated with the Brooklyn valley is more than 150 feet (45 m) thick in some places, Vineyard Lake and Brooklyn Mill Pond directly overlie the feature, and both lakes are elongated in the same direction as the bedrock channel (Figure 5). A segment of Goose Creek also coincides with the surficial trace of the buried bedrock valley. Norvell Valley The largest buried bedrock valley within the study area is the Norvell valley. The feature originates on the sandstone tableland and trends southeast past Norvell (Figures 4 and 5). In places it is more than one mile (1.6 km) wide and has been eroded more than 150 feet (45 m) below the surface of the adjacent bedrock. The maximum thickness of the overlying drift is more than 200 feet (60 m) in some places. Two angular changes in the course of the subsurface valley exist near Wolf Lake, and tributaries join the main channel at approximately right angles. As mapped, the valley trends southeast across the northeast c o m e r of T. 4 S., R. 2 E., although it is possible it may trend south across the center of T. 4 S., R. 2 E. to connect with Brooklyn valley. Sweezy Lake and almost all of River Raisin and its northern tribu­ taries in Jackson County are associated with unconsolidated sediments that overlie the lower course of the Norvell valley or its southern tributaries. A chain of lakes and streams that extend across the Grass Lake Plain also coincides with the surficial trace of the buried Norvell valley. These water bodies include Wolf and Little Wolf Lakes, Olcott and Little Olcott Lakes, Dollar Lake, Center Lake, and the stream 29 flowing west from Center Lake. This stream joins the Grand River near the eastern city limits of Jackson. From here the Grand River follows a course associated with the location of the Norvell valley for a distance of about two miles (3.2 km) to the western limit of Figures 4 and 5. Ackerson Lake and the stream flowing north from it, Gilletts Lake and the stream flowing south from it, and Brill Lake all have positions that coincide with the surficial traces of tributaries to the main channel that exists deep in the subsurface. Bridgewater Channel A well-defined southeastward-trending buried bedrock channel is located in T. 4 S . , R. 4 E . , Bridgewater Township, and T. 3 S . , R. 4 E . , of Washtenaw County. Kunkle (1960, p. 7 0 ) recognized this feature and named it the Bridgewater channel. The valley is 100 to 150 feet (30 to 45 m) deeper than the nearby bedrock surface, and the drift thickness associated with it is locally more than 200 feet (60 m ) . Two of the three valleys tributary to the Bridgewater channel begin on or near the sandstone tableland. The confluence of Norvell valley and Bridgewater channel is located in Sec. 6, T. 4 S . , R. 4 E. There is probably less surface expression of the Bridgewater channel than of any other major buried bedrock valley in the study area. Only the headwaters of the Saline River 4 and a small segment of the River Raisin near Manchester are located on the drift surface above the buried bedrock valley. Kunkle (1960, p. 71) previously noted this relationship. 30 Lima Valley The subsurface Lima valley trends eastward beneath T. 2 S., R. 4 E . , Lima Township, toward the Ann Arbor channel, which was identified b y Kunkle (I960). It is rather broad and shallow, although drift thick­ ness associated with it is more than 100 feet (30 m ) . Its tributaries follow the dominant regional pattern of northeast-southwest and northwestsoutheast trends. A southern tributary originates within the sandstone tableland and displays an angular course change near its confluence with the northern tributary. Most wells in T. 2 S . , R. 4 E. are developed in drift, so the exact course of this portion of the valley is not known with certainty. The limited data available suggest that it is very broad here and only slightly lower than the nearby bedrock surface. A portion of the North Fork of Mill Creek is situated directly above the buried Lima Valley. In addition, a considerable reach of Mill Creek trends parallel to the buried valley and is less than one mile (1.6 km) to the south of the poorly defined portion of the feature. Dexter Valley This valley trends southeastward beneath the northern portion of Washtenaw County and is named for Dexter Township, T. 1 S., R. 4 E. It may originate in Ingham County a short distance northwest of Stockbridge. Vanlier, Wood, and Brunett (1973) identify a bedrock valley that trends southeast near Stockbridge and extends to the southeast corner of Ingham County. Figures 4 and 5 show the Dexter valley trending generally south­ eastward from near the point common to Ingham, Livingston, Jackson, and Washtenaw Counties. Although the valleys on Vanlier, Wood, and Brunett's map and Figure 4 of this study do not appear to connect when the maps are juxtaposed, there seems little doubt they are related to each other 31 in some manner. The bottom of Dexter valley is approximately 100 feet (30 m) lower than the surface of the adjacent bedrock, and total drift thickness associated with the channel is more than 150 feet (45 m ) . Two angular course changes exist along the trend of the valley— one west of Unadilla and another just north of Island Lake. Dexter valley is prob­ ably a major headwater tributary to the Ann Arbor channel (see discussion in Kunkle, 1960, p. 70). South and Island"* Lakes and the unnamed stream connecting them are situated on drift that overlies the buried bedrock valley, as is North Lake.** In addition, Williamsville and Ellsworth Lakes and the stream connecting them also seem to be associated with the channel. Blind and Halfmoon Lakes may be associated with a northern tributary to the valley. Pinckney Channel A buried bedrock valley which originates beneath the town of Gre­ gory trends eastward. In secs. 28 and 29, T. I N , R. 4 E . , its exact course is unknown, although it may connect with a buried valley in sec. 22 trending east and southeast beneath the towns of Hell and Pinckney. Moore (1959, p. 22) labeled this the Pinckney channel. The bottom of the valley is more than 100 feet (30 m) below the surface of the nearby bedrock, and total drift thickness associated with the feature is more ^Kunkle (1960, p. 47) identified a "Lyndon tributary channel," and, as mapped by him, this bedrock feature trends southwest-northeast across the SH» T. 1 S., R. 3 E. The existence of the valley was not confirmed by this investigation; however, the two-mile (3.2 km)-long segment of Dexter valley beneath North and Island Lakes does correspond with a portion of Kneller's "Lyndon tributary channel." g The steep, subaerial slope in the sec. 13, T. 1 S . , R. 3 E. which is situated along a westward extension of the North Lake lowland, may also be associated with the Dexter valley. 32 than 150 feet (45 m ) . Pinckney channel is probably a headwater tributary to the Ann Arbor channel (see discussion in Kunkle, 1960, p. 70). Honey Creek from School Lake to a point east of Pinckney and a portion of Livermore Creek coincide with the surficial trace of the buried bedrock valley. Ann Arbor Channel Dexter valley and Pinckney channel apparently merge in the E%, T. I S . , R. 4 E. to form the Ann Arbor channel. Kunkle (1960, p. 70) named this bedrock valley and mapped it as trending southeast, extending past the city of Ann Arbor. His map indicates that the valley bottom is more than 160 feet (49 m) below the surface of the nearby bedrock in T. I S . , R. 4 E . , with the total thickness of drift overlying the valley bottom more than 200 feet (60 m).^ Without doubt it was one of the major streams of the area before burial. Kunkle (1960, p. 71) noted that the Huron River is located along the surficial trace of this buried bedrock valley. Relationship Between Buried Bedrock Valleys and Hydrography A number of buried bedrock valleys, interpreted to be of fluvial origin but possibly modified by glaciation, trend southeast beneath the drift of the study area. Despite burial these valleys appear to have influenced present hydrography because a number of lakes and streams are situated directly above their courses (Figures 5 and 6). Drift thickness in most of the area is 50 feet (15 m) or more. Bottoms of the valleys are often 150 feet (45 m) below the surface of ^In T. 2 S., R. 5 E., Kunkle shows the bottom of the buried valley to be more than 240 feet (73 m) below the nearby bedrock surface. 33 nearby bedrock, resulting in local drift thicknesses of more than 200 feet (60 m ) . At certain places both organic matter and material inter­ preted as oxidized till exist within the unconsolidated sediments overg lying the bedrock floors of the buried valleys. Surficial expression of the buried valleys is primarily limited to the presence of lakes and streams located along the traces of the subsurface channels. 9 The Wolf Lake-Center Lake-Grand River chain of fea­ tures associated with the Norvell valley (Figure 5) is probably the most striking example in the study area of the close relationship between the extent of buried bedrock valleys and certain hydrographic features. Conversely, there is little or no surface expression of segments of some channels, such as the northern tributaries of the Bridgewater channel. There is a tendency for hydrographic features associated with bed­ rock valleys to be best developed in those areas where the bottoms of the valleys are considerably lower than nearby bedrock surfaces. Where the buried valleys are incised less deeply in the bedrock, hydrographic features directly above the valleys are not as conspicuous. A satisfactory explanation of the genesis of the buried bedrock valley and hydrography relationship must therefore account for, at the least, two phenomena. First, the surficial expression of the buried bedrock valleys is not uniform and may vary from one reach of a valley 8See Chapter 3 for a discussion of the unconsolidated sediments associated with the buried bedrock valleys and also drift thickness in the study area, o In many portions of the area surficial streams trend across bed­ rock divides and seem unaffected by the bedrock surface. An example of such a situation is where Portage River flows across the trace of a bed­ rock divide in Tps. 1-2 S., R. 1 E. Newcombe and Lindberg (1935, p. 1181) discussed the relationship between lakes and the Marshall Sand­ stone but did not consider the relief on the bedrock surface. 34 to another. Second, a horizon in the drift of the buried valleys seems to mark a period of subaerial exposure. This suggests that a subsequent glacial advance buried the valleys and the sediments in them. Neverthe­ less, surficial expression of the valleys is present in the form of lakes and streams on the drift surface. Due to the buried oxidized till and organic matter, any explanation of the bedrock-hydrography relation­ ship would need to account for surficial expression of the bedrock val­ leys through at least two glacial episodes. One hypothesis which explains the bedrock valley-hydrography rela­ tionship involves buried ice that may have been associated with the channels during glaciation(s). Subsequent ablation would have lowered any sediments overlying the ice, thus predisposing these lineations to become drainage lines or lakes. This ice could have been buried in or over the bedrock valleys (1) by chance or (2) by subglacial expression of the valleys, permitting ice to be lodged in their deeper p o r t i o n s . ^ In the first situation depressions would be distributed in a random pattern after ablation, the individual features would be irregular in shape, and they would lack a preferred orientation. In the second case depressions would have preferred shapes, locations, and orientations re­ lated to the depth and trend of the related bedrock valleys. As some lakes of irregular shape and orientation are found overlying the buried bedrock channels, it seems possible that they may have formed by random burial of ice blocks; however, many streams and linear lakes are found directly above buried bedrock valleys and seem associated with them. ^ F e r r i s , Burt, Stramel, and Crosthwaite (1954, p. 31-34) suggested a third possibility— that masses of buried ice may be due to ponded pro­ glacial water bodies in preexisting drainage systems being overridden and frozen by the advancing glacier. 35 Hydrographic maps indicate apparent ice-contact slopes beneath the waters of Wolf, Patterson, South, Blind, and Halfmoon Lakes. These steep slopes are also parallel to the buried bedrock channels beneath the l a k e s . ^ In addition, Kunkle (1960, p. 72) noted that the Fort Wayne Moraine seems to extend westward a distance along the surficial trace of the Ann Arbor channel. He suggested that a valley may have ex­ isted in the drift overlying the bedrock channel, allowing ice of the last advance to flow in that linear feature and deposit the westward ex­ tension of the moraine near Dexter. Thus, many aspects of the bedrock valley-hydrography relationship may be explained if it is assumed that ice was buried in or above por­ tions of the subsurface channels. In general, related hydrographic features are situated over the deeper portions of the bedrock valleys. Apparently these locations were preferred sites for masses of stagnant ice. The orientation of linear lakes, their bottom trends, apparent ice-contact slopes, and streams are all generally parallel with under­ lying bedrock valleys and may be explained by ablation of ice blocks buried in the drift filling of the deeper portions of the valleys, pre­ disposing certain sites to become drainage lines or lakes. This process does not require unique conditions and probably was effective during more than one glacial episode, as is indicated by the buried organic matter and possible oxidized till found in the valleys. Ferris, Burt, Stramel, and Crosthwaite (1954, p. 31 and 34) noted similar steep slopes in some lakes of Oakland County and stated (p. 34) that such lakes "may be related to the bedrock surface of the area." Chapter 3 CHARACTERISTICS, DISTRIBUTION, AND STRATIGRAPHIC SIGNIFICANCE OF THE GLACIAL SEDIMENTS Introduction This chapter is concerned with the sedimentary characteristics of certain Quaternary deposits.'*' Drift thickness in the area varies from almost zero in a few places to over 200 feet (60 m) in others. Sub­ surface drift stratigraphy appears complex in terms of both sediment type and contact relationships. With the exception of loess all types of sediments commonly associated with glaciation were recognized at the surface in the study area. Till, including flow till, is common, and glaciofluvial sediments, some of which were deposited in contact with ice, underlie large portions of the area. Glaciolacustrine silts and clays exist within and near the Interlobate Morainic Tract. Different procedures and techniques were utilized to determine the characteristics of the surficial drift sheets recognized. These included the use of soil maps and the determination of till fabric, color, tex­ ture, and clast lithology. Certain aspects of the clay mineralogy of the sediments were analyzed to identify the different surficial drift sheets within the area. This identification was possible because till and some other deposits from both the Saginaw and Huron-Erie Lobes appear to have distinctive clay mineralogies that ordinarily permit recognition of the provenance of a drift sample. 2 ^See Appendices for field and laboratory procedures. 2 The drift contact suggested by morphology is very similar to that determined by clay mineralogy. This congruity of evidence provided by dissimilar methods of investigation is striking and lends credence to the results of both. 36 37 Drift Thickness Leverett and Taylor (1915, p. 199) noted that within the area glacial deposits thought to be associated with the Huron-Erie Lobe tend to be somewhat thicker than those of the Saginaw Lobe. Kunkle (1960) and Moore (1959) prepared drift-thickness maps for Washtenaw and Living­ ston Counties, respectively, with a total of 201 well records for the 363 survey sections (Figure 7) which are east of the Jackson County boundary. Figure 7, showing the east half of Jackson County plus por­ tions of Livingston and Washtenaw Counties, is based on these records and data from an additional 1,281 points (total=l,482). The map was compiled, then computer plotted, and finally manually modified in a manner similar to Figure 4. 3 It is apparent from Figure 7 that deposits proximal to the Kala­ mazoo Moraine are considerably thinner than the drift immediately to the east of the Mississinewa Moraine (Table 1). In f a c t , mean drift thick­ ness north of the Kalamazoo Moraine is about 80 feet (24.4 m) but aver­ ages approximately 180 feet (54.9 m) south and east of the Mississinewa Moraine.^ Mean drift thickness beneath the Kalamazoo Moraine west of Leverett Hill averages about 100 feet (30.4 m ) , and beneath the Mississinewa Moraine south of Leverett Hill it is approximately 115 feet (35.1 m ) . Drift thickness is therefore only slightly greater beneath the Kalamazoo Moraine than in the area proximal to it and is much greater proximal to the Mississinewa Moraine than it is underlying that feature. The west 3 As described in Appendix A. 4 These mean values are based on Figure 7 and were calculated by averaging the drift thickness at the center of each survey section. portion of the Interlobate Morainic Tract has a mean drift thickness of about 110 feet (33.5 m ) . Within the east part of the tract the thickness of the drift averages 145 feet (44.2 m ) . On the basis of these figures it is obvious that in those areas where Saginaw drift is at the surface the depth to bedrock tends to be less than in those with surficial Huron-Erie drift. Table 1. Average Drift Thickness in Study Area Kalamazoo Moraine Mississinewa Moraine Proximal to 80 feet (24.4 m) 180 feet (54.9 m) Beneath 100 feet (30.4 m) 115 feet (35.1 m) Interlobate Morainic Tract Areas with Surficial Saginaw Drift 110 feet (33.5 m) Areas With Surficial Huron-Erie Drift 145 feet (44.2 m) Grass Lake Plain Area Including Norvell Valley 80 feet (24.4 m) Not Including Norvell Valley 75 feet (22.5 m) In the Grass Lake Plain area^ the mean drift thickness is about 75 feet (22.9 m) if the effects of the Norvell bedrock valley are re­ moved. At least some of the trends of the major buried bedrock valleys are apparent on Figure 7, but are not as well defined as on Figure 4, "Bedrock Surface." ^This tract is located in the reentrant between the two moraines north of the T. 3 S.-T. 4 S. township line and east of Jackson. 39 Subsurface Sediments Study of more than 1,000 well records indicates the drift strati­ graphy of the area Is complex. The only fairly consistent subsurface relationship noted was that till immediately overlies the bedrock sur­ face in many places. An attempt was made to correlate subsurface sedi­ ments, but this effort was generally unsuccessful because most of these sediments seem to be of limited horizontal extent. Evidence for this is that records of very closely spaced wells are commonly quite different. Nevertheless, a few generalizations may be made on the sequence of sedi­ ments in the subsurface. Subsurface Sediments in the Area of the Kalamazoo Moraine Numerous well records indicate that till and glaciofluvial mater­ ials are present in approximately equal quantities both at and beneath the surface of the northern portions of the Kalamazoo Moraine. However, well records, existing road cuts, and scattered gravel pits indicate glaciofluvial materials to be predominant in the uppermost 30 to 50 feet (9.1 to 15.2 m) of the crest or southern portion of the moraine. Because of the nature of descriptions on many of the well records, it is often difficult to interpret the difference between till and shale (see Appendix A ) . Consequently it is not possible to state exactly with what frequency till is in contact with bedrock, but it is estimated that, in 60 to 70 percent of all wells which reach bedrock beneath the Kala­ mazoo M o r ain e , till is the basal glacial sediment. Sediments Beneath the Mississinewa Moraine Well records are not as numerous for the area of the Mississinewa Moraine, but those available indicate a greater abundance of till 40 present both at the surface and at depth beneath the northern portion of the moraine than beneath the Kalamazoo Moraine. sence of sand and gravel is more common. To the south the pre­ Possibly 80 to 85 percent of the records of wells which were drilled Into bedrock beneath the Missis­ sinewa Moraine indicate that till immediately overlies the bedrock sur­ face. Sediments Beneath the Interlobate Morainic Tract Both well records and soil maps indicate that the preponderance of surficial material in the Interlobate Morainic Tract is sand and gravel, although there are some areas underlain by till. Most well records note the presence of this sand and gravel to a depth of 20 to 40 feet (6.1 to 12.2 m ) . Below this level till is reported to be more common, and ap­ proximately 75 percent of the well records used in map construction of the Interlobate Morainic Tract indicate that till is in contact with the underlying bedrock. Sediments Beneath the Grass Lake Plain Area Soil maps and most well records indicate sandy or gravelly mater­ ial at, and near, the surface of much of the Grass Lake Plain area. However, significant amounts of till are recorded at depths of about 30 to 50 feet (9.1 to 15.2 m ) . This may represent basal till overlain by outwash sediments because kettles here are generally no deeper than 30 to 40 feet (9.1 to 12.2 m ) . Approximately 70 to 75 percent of the records of wells that penetrate bedrock beneath the Grass Lake Plain area indicate that till immediately overlies bedrock. 41 Organic Matter and Oxidized Till(?) in the Subsurface Organic deposits within glacial sediments in the subsurface do not appear to be common in southeastern Michigan although reports of such materials do exist. Sherzer (1917, p. 8) noted the presence of a buried soil at a depth of 85 feet (25.9 m) in Macomb County. Leverett and Taylor (1915, pp. 192, 290) reported buried soils in Eaton and St. Clair Counties and mentioned (p. 199) extensive swamp deposits at the base of Wisconsin(an)(?) till in Hillsdale County about 30 miles (48 km) south­ west of the study area. Russell and Leverett (1908, pp. 4-5) reported large quantities of pre-Wisconsin(an) till in the Ann Arbor quadrangle, but they knew of no soils burled in the subsurface there. Recently, additional evidence has become available primarily due to drilling operations. Both Chang (1968) and VanWyckhouse (1966) studied engineering test-boring samples from two sites in Detroit. They concluded that a number of tills were present in the subsurface and that a "Lower Drift" is either Illinoian or preclassical Wisconsin(an) in age. Kunkle (1960, p. 30) noted references to two or three buried tills on well records from sites in eastern Washtenaw County. He was able to separate an "upper Cary till" from a "lower pre-Cary till" on the basis of a number of criteria, two of which were the presence in the subsur­ face of "a red (oxidized?) clay or sand" and to hard clay" "a change from soft clay (pp. 31-32). A number of professional water-well drillers have developed wells in the area, and of the four interviewed three** indicated they had ^Personal communications, Messrs. Melvin Fox of Napoleon, December 30, 1974, Marshall Meabon of Pinckney, December 17, 1974, and Dale Lindemann of Dexter, December 17, 1974. 42 obtained wood from depths greater than 40 feet (12.2 m).^ On well re- g cords till is commonly described as clay or stony clay. Oxidized sedi­ ments apparently are most often described by drillers as red or brown, and unoxidized sediments as blue or gray in color. Wells with organic matter and red and brown clays and stony clays in the subsurface exist at a number of places within and very near the study area. Almost without exception these sites are associated with bedrock valleys or low areas on the bedrock surface. Organic matter or oxidized sediments found in the subsurface beneath unoxidized sediments interpreted as till imply a former weathering surface that has been buried by deposits from a subsequent glacial advance. 9 Interlobate Morainic Tract and Vicinity The strongest evidence for a paleo-drift surface is in the vicinity of Pinckney. Well records and interviews with drillers indicate that in this area red and brown clay and stony clay, wood, muck, peat, reeds, and even a snail shell have been recovered from beneath blue and gray clay ^These drillers do not ordinarily report organic matter on their records. g See discussion on well-record interpretation in Appendix A. 9 Because it has been stated that circulating ground water may cause subsurface chemical changes (Boulton, 1972, p. 389), well records with reports of red sands and gravels at depth were not considered as their relatively high permeability might permit large quantities of ground water to flow through them. Some red and brown clays at depth may be due to ground-water circulation, but the presence of organic matter associated with such sediments at depth seems to indicate that at least some are the result of subaerial, not ground-water, weathering. It is assumed that the red or brown color is due to secondary chemical changes after deposition and is not a primary characteristic. In addi­ tion, those records indicating organic matter and red and brown clays beneath sand and gravel were not considered because the uppermost ma­ terial may represent postglacial fluvial deposits. 43 and stony clay at depths ranging from 62 to 115 feet (18.9 to 35.1 m) (Table 2). Meabon and Llndemann i n d i c a t e ^ that wood is most common in the subsurface just east of the Huron River in T. 1 S., R. 5 E. and is also found in T. I N . , R. 4 E. and T. 1 N . , R. 5 E. recovered wood from a well in T. I S . , Lindemann also stated he R. 4 E. In this area the subsurface altitude of the top of the red and brown clay and organic matter varies from 785 to 850 feet (239.3 to 259.1 m ) , and the existing topographic surface averages about 900 feet (274.3 m ) . In five wells thickness of the buried and apparently oxi­ dized material was recorded as 6, 8, 11, 11, and 20 feet (1.8, 2.4, 3.3, 3.3, and 6.1 m ) . These should be considered minimum thicknesses because it cannot be determined to what degree subsequent glacial erosion may have removed material. The fact that paleosols are not common indicates that some erosion probably did take place. If the interpretation that these are subaerially oxidized zones is correct, they can be interpreted as representing a nonglacial episode of considerable length, because oxidation depths on the upper surface of Wisconsinan tills in the area averages about 20 feet (6.1 m ) . Grass Lake Plain Area There are reports of red and brown clay at depth near Wolf Lake, located about 15 miles (24 km) to the southwest of the Interlobate Morainic Tract (Table 3). Records from two wells located above the buried Norvell valley (secs. 20 and 21, T. 3 S., R. 2 E.) indicate that the top of 5 to 10 feet (1.5 to 3.0 m) of red and brown sandy and "^Personal communications, December 17, 1974. Table 2. Well Location Surface Altitude Ft. (m) Buried Organic Matter and Oxidized Sediments in Interlobate Morainic Tract and Vicinity Depth Ft. (m) Subsurface Altitude Ft. (m) Evidence Source and Driller T. 1 S., R. 5 E. SE^SE^SW^ sec. 10 900 (274.3) 62 (18.9) 838 (255.4) 8.ft. (2.5 m) red clay, with wood immediately above it in blue clay Record & Inter­ view, Lindemann #Secs. 11 and 12 900 (274.3) 50 (15.2) 850 (259.1) reeds beneath sand and gravel Interview Meabon SWWsNE** sec. 15 900 (274.3) 90 (27.4) 810 (246.9) 11 feet (3.3 m) red clay Record Lindemann S E^SEWi sec. 18 900 (274.3) 112 (34.1) 788 (240.2) wood and peat with H2S odor immediately beneath blue clay Record & inter­ view, Lindemann I. IN., R. 4 E. NEWsSW^s sec. 9 915 (278.9) 65 (19.8) 850 (259.1) 20 feet (6.1 m) brown gravelly clay Record Brown Bros. £EJ«NEW s sec. 14 930 (283.5) 92 (28.0) 838 (255.4) 11 feet (3.4 m) brown gravelly clay Record Fulmer SWWsS^s sec. 23 900 (274.3) 115 (35.1) 785 (239.3) 5 ft. (1.5 m) wood & bark with snail shell in sand, clay and stones Record Interview Meabon Table 2 (cont'd.) Well Location T, IN., R, 4 E. Surface Altitude Ft. (m) Depth Ft. (m) Subsurface Altitude Ft. (m) Evidence Source and Driller (cont'd) //NWWsNWis sec. 26 900 (274.3) 48 (14.6) 852 (259.7) 7 feet(2.1 m) of wood (pine?) beneath sand and gravel Interview Meabon mhStikSUk sec. 35 870 (265.2) 80 (24.4) 790 (240.8) 6 feet (1.8 m) brown clay and gravel Record Brown Bros. wood at ? depth Interview Lindemann T. 1 S., R. 4 E. NE^SW^SE*s sec. 12 // = beneath sand and gravel Table 3. Surface Altitude Ft. (m) Well Location Buried Organic Matter and Oxidized Sediments in Grass Lake Plain Area Depth Ft. (m) Subsurface Altitude Ft. (m) Evidence Source and Driller T. 4 S., R. 2 E. NEWsNE!* sec. 2<» 1,000 (304.8) 84 (25.6) 916 (279.2) 19 feet (5.8 m) of red clay Record, Brewer NE^SEJjSW^ sec. 21J 40 (12.2) 930 (283.5) 10 feet (3.0 m) of marl & sand, 4 feet (1.2 m) marl and gravel Record Sprunger 970 (295.7) T. 3 S., R. 2 E. NWisSWWs sec. 21) 960 (292.6) 55 (16.8) 905 (275.8) 10 feet (3.0 m) hard brown gravelly "shale11 Record Fox 2L 965 (294.1) 70 (21.3) 895 (272,8) 5 feet (1.5 m) brown sandy clay Record Fox NE*sNEW« sec. T. 3 S., R. 1 W. @N3{SEW{ sec. 1 960 (292.6) 20 (6.1) (§ = apparently beneath post-glacial deposit 940 (286.5) 8 feet (2.4 m) muck Record Washburn 47 gravelly clay beneath blue and gray gravelly clay is at an altitude of about 900 feet (274.3 ra) approximately 60 feet (18.3 m) below the surface. Another record from a well located along the surficial trace of the Brooklyn valley (sec. 28, T. 4 S., R. 2 E.) notes marl at a depth of 40 feet (12.2 m) beneath blue clay. Also, the record for a well located three miles (4.8 km) to the east (sec. 24, T. 4 S., R. 2 E.) in a tribu­ tary to the Norvell valley indicates that the top of 19 feet (5.8 m) of red clay is at a depth of 84 feet (25.6 m) beneath a body of blue clay. Area Proximal to the Kalamazoo Moraine Four wells with rather unusual R. 1 W. and Wig, T. 1 S., R. 1 E. records exist in the EJg, T. 1 S., (Table 4). All indicate what is appar­ ently the upper part of an oxidized till (red and brown clay) at depths from 48 to 83 feet (14.6 to 25.3 m ) , most with overlying blue or gray clay. However, thickness of the material interpreted to be oxidized till is great and varies from 27 to 44 feet (8.2 to 13.4 m ) . If this is sub- aerially oxidized material and was not affected by circulating ground water, it might represent a very long weathering interval. Just to wood has been the west of the study area in sec. 17, T. 1 S., R. 1 W. reported at a depth of 88 feet (26.8 m ) , overlain by sedi­ ment interpreted to be till. This is the only record observed from Jackson County which notes the presence of wood at depth. Significance of the Buried Organic Matter and Oxidized Sediments The widespread distribution of red and brown clays, peat, wood, and marl in the subsurface indicates the presence of at least one older drift sheet whose surface was exposed to the atmosphere for a period of time. These older sediments do not appear to form a continuous layer because Table 4. Buried Organic Matter and Oxidized Sediments Proximal to the Kalamazoo Moraine Surface Altitude Ft. (m) Depth Ft. (m) Subsurface Altitude Ft. (m) S E W s S W 3* sec. 1 930 (283.5) 83 (25.3) 847 (258.2) 31 feet (9.4 m) red clay Record Hart SW^SWWs sec. 17 950 (289.6) 88 (26.8) 862 (262.7) 2 feet (0.6 m) wood Record, Intrvw. Fox Well Location Evidence Source and Driller T. 1 S., R. 1 W. T. 1 S., R. 1 E. SE^SW^SE^ sec. 9 950 (289.6) 48 (14.6) 902 (274.9) 27 feet (8.2 m) hard brown clay Record Fox SWlsSW^SW^ sec. 17 955 (291.1) 83 (25.3) 872 (265.8) 34 feet (10.4 m) red clay Record Hart mkSEWk sec. 30 965 (294.1) 48 (14.6) 917 (279.5) 44 feet (13.4 m) red clay Record Hart //NE^SE^NE^ sec. 31 949 (289.3) 45 (13.7) 904 (275.5) 10 feet (3.0 m) muck and sand # = beneath sand and gravel Record, Oil well permit # 2631 49 they are found almost exclusively in the drift associated with bedrock valleys and low areas on the bedrock surface. Many well logs indicate a number of separate till layers at depth in the eastern portion of the study area, and Kunkle (1960) mapped the surface of a buried older drift sheet in eastern Washtenaw County but no well record studied showed con­ vincing evidence of more than one weathered zone. Surficial Sediments The bulk of the characteristics of certain surficial sediments— till color, clay mineralogy, texture, fabric, pebble and boulder lithology, and boulder distribution was determined by field observation, field sampling, and laboratory analyses. cussed in the appendices. Details of these procedures are dis­ The following discussion on the soils of the study area is based on available soil maps as modified by field observa­ tions . Drift Associated with Kalamazoo Moraine and Related Portions of Interlobate Morainic Tract Soils as an Indicator of Parent Material Soil maps were completed for Washtenaw, Livingston, and Jackson Counties in the 1920s and 1930s, and all seem to be based on similar mapping criteria. Recent and more detailed soil maps are also available for Washtenaw and Livingston Counties. By comparing the newer maps and older maps of these counties, it is possible to recognize what soil series are present in the older, more generalized mapping units. On this basis it is possible to identify those soil series which will prob­ ably appear on the new soil map for Jackson County'1'1 by using the older 11 Field work has begun on a detailed soil survey for Jackson 50 map as a base. The map accompanying the 1930 Jackson County Soil Survey (Veatch, Trull, and Porter) indicates that most of the soil in the north­ ern (proximal) two-thirds of the Kalamazoo Moraine is Hillsdale sandy loam, which is interpreted to have till as the parent material (Figure 8). The recent soil surveys from Washtenaw and Livingston Counties indicate that Fox, Spinks, and Boyer soils, interpreted to have glaciofluvial sediments as parent material, may also exist within areas that previously have been mapped as Hillsdale sandy loam. This is corroborated by per­ sonal field observation. Bellefontaine sandy loam soil vras associated with a series of gravelly knobs located along the highest (southern) part of the moraine on the 1930 soil map. It is also apparent that Boyer, Fox, Spinks-Oak- ville, and Boyer-Oshtemo soils may be expected to exist within areas formerly mapped as Bellefontaine. The parent material of all these soils is interpreted to be glaciofluvial sands and gravels. According to the 1930 soil survey, Plainfield loamy sand and Newton loam are scattered in small tracts throughout the moraine and are thought to be developed on glaciofluvial materials. Rifle peat and Greenwood peat have been mapped in certain poorly drained depressions. Spinks, Boyer, Oshtemo, Oakville, and Fox soils exist on the large area of glaciofluvial sediments on the Saginaw Lobe side of the Inter­ lobate Morainic Tract. Smaller areas of Miami and Kidder soils, which have till as parent material, exist primarily north of Patterson Lake. Sisson, Kibble, and Colwood soils formed on bodies of lacustrine clay and silt in the Interlobate Morainic Tract. These lake deposits may also County, but insufficient mapping has been completed to be of significant use in this investigation. 51 underlie areas more recently mapped as Miami. For example, at least a portion of the large tract mapped as Miami soil west of Patterson Lake la actually derived from a lacustrine deposit, and not till as shown on the recent soil map of Livingston County. Clay Mineralogy One of the basic techniques utilized in this investigation was Xray diffraction to determine certain aspects of clay mineralogy of samples from various locations in the area. A total of sixty-six samples was examined by this method (Figure 9 and Appendix B ) . Of these, sixty-one were obtained from glacial deposits and included forty-nine till, nine glaciofluvial, and three glaciolacustrine samples. Five samples of bed­ rock (three shale and two sandstone) were also analyzed. Samples of both basal and flow till were analyzed as was till from the crests of the Blue Ridge and Goose Lake Eskers. In addition, clay from glaciofluvial mate­ rials within these eskers and from beneath the surface of the Mississinewa Moraine was also X-rayed. were investigated, 12 Sediments from many parts of the study area and a number of samples from near the surficial Saginaw/Huron-Erie drift contact were collected and analyzed because the clay mineralogy of a drift sample proved to be a reliable indicator of its lobe provenance. In fact, of all the lithologic characteristics ex­ amined in this investigation, clay mineralogy was the most consistent and reliable property by which the provenance of a drift sample could be determined. The clay mineralogy of thirteen surficial till samples from the Kalamazoo Moraine, from associated portions of the Interlobate Morainic 12 Two samples (numbers 227 and 228) from the surface of the Fort Wayne and Outer Defiance Moraines were also studied. 52 0 .9 3 * ✓ * 0 .8 4 l-s !;| U9* P Jackson Co I 35« ,05* l.3h*v^' y L«i *or > *>#7 7 A * 0 .6 6 .50 A |.86 s t * •0.88 •0 .7 8 2.I6R 0 .9 3 o ' / 0.87 * f 0.84e * 0 .6 5 -t* 0 .8 3 _.•? •0.68 0 .8 7 e 0.59 s 1.30 _ • 0 .6 7 I.OOo • 0.76 0 96 • I0.7 h • 0 .6 9 0 .8 7 « 2 .50s l.83e SITES A N D RATIOS FOR X-RAY DIFFRACTION S A M P L E S KM KALAMAZOO M O R A IN E SAGINAW LOBE MM MISSISSINEWA MORAINEHURON-ERIE LOBE ILM T <<< INTERLOBATE TRACT MORAINIC ESKER SURFICIAL DRIFT CONTACT 7a / I 0 a RATIOS FOR SAMPLES OF-- 1.2 3 T IL L 1.23c GLACIOFLUVIAL I.2 3 l G LA C IO LA C U STR IN E I.2 3 r BEDROCK 1.23 I.2 3 g TILL N MATERIAL M A TERIA L STRATI GRAPHICALLY ABOVE GLACIOFLUVIAL M ATER IAL 0 5 miles Figure 9. Sites and Ratios for X-Ray Diffraction Samples 53 Tract, and from the area immediately to the north were analyzed according to the procedures described in Appendix B. Peak heights on the X-ray diffractograms were measured, and 7&/10& ratios calculated. All thirteen of these till samples yielded ratios of 0.91 or more and were collected from sites north and west of a line connecting Leverett Hill, Riley Hill, Stofer Hill, Russell Hill, ney 14 13 the east end of Patterson Lake and Pinck- (Figure 10). The range of the 7X 7 1 0 X. ratios for 13 sites is 1.12 with values varying between 2.03 at site 72 (NW^SW^NW^s sec. 24, T. 2 S., R. 1 W.) and 0.91 at site 129 (NW^sSE^SE^ sec. 10, T. 1 S., R. 1 E.). It is possi­ ble that the rather high value of 2.03 may be due to the influence of local bedrock overlain by relatively thin drift located just to the north of the sample site (Figure 7). Sandstone (probably from the Pennsylvan­ ian Saginaw Formation) is also reported both at the surface along the Grand River about one mile (1.6 km) to the west of site 72 (Leverett, field notebook 274, p. 86 and Martin and Straight, 1956, p. 235) and 1.5 miles (2.2 km) to the north in the bed of Portage River (Leverett, note­ book 275, p. 95). Analysis of a sample of the sandstone bedrock (number 229, NW^SW^sNW^s sec. 26, T. 2 S., R. 1 W.), probably from the Saginaw Formation (Martin and Straight, 1956, p. 235) and collected from a road cut along 1-94 about 1.5 miles (2.2 km) from site 72, indicates a very 13 A flat-topped hill located in sec. 1, T. 1 S., R. 3 E. which is unnamed on the Stockbridge quadrangle. The name "Russell Hill" is applied to this feature for identification purposes only and is not proposed as a formal geographic name. This hill has ice-contact slopes on three sides and is situated between Bruin and Blind Lakes. 14 This boundary line is also important morphologically and will be discussed in the following chapter. 54 R3E R4E TIN □ PINCKNEY 1 .0 5 * • 0 .7 7 1.19* 'Patterson Lake Livingston Co, Washtenaw Co. \^ /( 1.45 Prospect Hill " ell •0.86 R“S Hj„3el1 * 0 .6 4 l * 0 .7 3 • Heatley Hilt Shanahan H ill* '• 0 . 5 7 “ 1.05 TIS Hankard Hill* Stofer Riley H ill* 0.86 0.81 1.05* • 0 .7 4 SURFICIAL DRIFT C O N T A C T IN INTERLOBATE MORAINIC TRACT THIS INVESTIGATION 10 ✓ / I t ui z to < Ito >cc o Figure 12. oo ^ <8 to cm «\i ioD OS to * < X CO K- IQ D 1 0 0 UJ Ul t< z o OQ Z < o {£) z £ t o Q z < to DC UJ X o ^ o ° o : UJ to e1 in oo o ° '■ «:>. .«• .i i. T V- 1 » ^ V. ’ .••■>l-'.1 .TWii, »i? ,i . <.‘. . - , ’• '••V**'’f W W Figure 19. . ,;-,/?w \- ■ 74 On the basis of the preceding evidence, it seems likely that unit A is a massive flow till, not greatly modified by subaerial washing, that was deposited upon unit B. Unit B represents an earlier phase when glaciofluvial conditions predominated. The lower till, unit C, contains many sand lenses, sand partings, 30 and sandy horizons (some with bedding clearly visible). Most of the sandy horizons are subhorizontal and roughly parallel to the present topographic surface. unit A. The till is coarser and contains more pebbles than Kaye (1960, Figures 51 and 52) shows two tills with very similar appearance which he labeled "stratified till." He believed that these tills had moved downslope under the influence of gravity and were flow tills. It seems probable that unit C consists of a series of flow tills which had been exposed to meltwater before and after flow had taken place. The coarser texture and greater abundance of clasts is most likely due to meltwater removing the finer fractions of the till. Both Boulton (1968, p. 408) and Marcussen (1973, p. 222) have observed sediments. exposures which show interfingering of flow till and outwash They interpret this as flow till deposited simultaneously or penecontemporaneously with outwash. These authors have also described exposures revealing flow till conforming with, truncating, and grading into sediments with which they are in contact (Boulton, 1968, p. 400 and Marcussen, 1973, p. 221). all these relationships. The Brill Lake pit (site 81) has examples of An exposure along the north side of the pit re­ veals interfingered till and water-deposxted sands. One of the till bodies truncates the bedding in the lower portion of an outwash sequence (Figures 20 and 21). 30 Although the contact between till and outwash is Figure 19 shows similar till elsewhere in the pit. 75 SLUMP M A S S IV E FLOW P IC K T IL L MATTOCK OUTWASH SLUMP Figure 20. Interfingering of Massive Flow Till and an Unbroken Outwash Sequence. Till has been moistened to emphasize tonal difference be­ tween it and outwash. Till fabric 81 was measured at "X." Site of fabric 81A is just off picture to right. Pick-mattock is 18 inches (45.7 cm) long. Exposure in north wall of Brill Lake pit. July 25» 1974. OUTWASH M A S S IVE FLOW PICKMATTOCK TILL PEN C IL OUTWASH Figure 21. Close-up of Exposure in Figure 20. Bedding in outwash is truncated by till in lower part of photo but is conformal with it in upper p a r t . The outwash bedding appears to represent an unbroken depositional sequence. Note the stratification in the till near pencil. A portion of the till has been moistened to clarify the till/ outwash contact. July 25, 1974. Figure 20. Figure 21. 77 sharp and undeformed, the lower portion of the till displays stratifica­ tionlocally and in one location grades into underlying sediments. On the basis of the (1) sand lenses and horizons, dated nature," (3)vertical faces in exposures, position, (5) till fabrics, (2) "overconsoli­ (4) high stratigraphic (6 ) interfingering with outwash, and (7) proximity to an ice-contact slope (less than 100 yards or 91 m away), it is apparent that flow till is present in the pit. Prospect Hill "A" (S^SEifiSW^ sec. 2 and N^NW^ sec. 11, T. I S . , 3 E.) 31 is a large kame located just west of Russell Hill. R. Air photos and topographic maps show a 10- to 15-feet-deep (3.0 to 4.6 m) draw trending northeast down the flank of Prospect Hill "A." A portion of the gravel pit at site 183 (SW^sSE^SWij sec. 2, T. 1 S. , R. 3 E„) intersects the draw, and the resulting exposure reveals till up to 10 feet (3.0 m) thick on the side of the draw. The till is very sandy (loamy sand) and displays smooth vertical faces in the pit. The till spalls off the face in sheets and is generally massive and relatively stone-free, but those sandy horizons and striated pebbles present are parallel to the contact with the subjacent sand and gravel. Small drag structures in the sand and gravel indicate that the till moved obliquely downward toward the center of the draw. The preferred orientation of fifteen pebbles within the bottom part of the till was also transverse to the maximum slope of walls of the draw. On the basis of this evidence, it appears reasonable to conclude that flow till moved down the flanks of Prospect Hill"A" and flowed obliquely into a preexisting valley on the slopes of the feature. 31 A number of features named "Prospect Hill" are located in the study area. Those discussed in this dissertation will be identified by a letter; thus, this feature is Prospect Hill "A." 78 A somewhat similar situation exists at site 161 (N^SE^SE^s sec. 7, T. 2 S., R. 2 E.), where a vertical 25-foot-high (7.7 m) face in a gra­ vel pit exposes 10 feet (3.0 m) of till with smooth vertical faces, sub­ horizontal sandy lenses, and striated pebbles overlying 15 feet (4.6 m) of sand and gravel. A 4-foot-deep (1.2 m) channel at the top of the sand and gravel is filled with till. It appears that flow till comple­ tely filled the small channel and buried any of its surface characteristics. the sand and gravel, obscuring Marcussen (1973, pp. 222-23) noted a similar situation in Denmark. The maximum thickness of flow till observed in the study area was about 25 feet (7.6 m) at site 81 near Brill Lake. 391) reports a maximum thickness of 5 meters Boulton (1968, p. (16.4 ft) for flow till on Spitsbergen, and Marcussen (1973, p. 229) observed a deposit 7 meters (23 ft) thick in Denmark. Kaye (1960, p. 357) does not list the maximum thickness for flow till in his area of study but does include a photo­ graph of this material in an exposure which appears to be 15 to 20 feet (4.5 to 6 m) tions in height. Flow till is generally found on the higher por­ of the landscape in the study area, and in most exposures it is both uppermost and the last glacial sediment deposited, although in some cases 1 or 2 feet (0.3 or 0.6 m) of sand covers the till. 32 Flow till may be recognized quite easily in large exposures where both structure and stratigraphy are visible (Figure 22 and Appendix G ) . In small exposures it is generally not possible positively to identify flow till, although in some cases a probable recognition may be made. 32 33 Almost no exposures or excavations were found in the lower por­ tions of the landscape, so the presence or absence of flow till in such locations cannot be confirmed. 33 Positive identification does not appear possible from auger borings or well records. RIE Ingham Co. | Livingston Co. R4E 201 TIN 205# 183 / %''79 191 X TIS 189/ TIS 181 171 190 78 150 76 153 • 161 T2S 72 73 74 148 146 144 x ... X X T3S 138' 134 RIE Jackson C o .'r Washtenaw Co. FLOW TILL EXPOSURE - POSITIVE OF FLOW T I L L x SMALL EXPOSURE - P R OB AB L E OF FLOW T I L L « ID E N TI F IC AT IO N ID E N TI F IC AT IO N NUMBER — S U R F IC IA L •- R4E IN MORAINIC AREAS # LARGE 50 SITE T3S <43 X' D R IF T TRANSITIONAL KALAMAZOO MISSISSINEWA CONTACT MORAINE BOUNDARY MORAINE MORAINE N 0 ^ 5 miles 0 10 kilometers ilr'76 Figure 22. Flow Till in Morainic Areas 80 In the portion of the Kalamazoo Moraine and associated area of the Inter­ lobate Morainic Tract which extends from Jackson to Pinckney, twenty-one large exposures were studied during this investigation. Flow till was positively identified in nine of these exposures, and probable identification was made in four. 34 Thus, of the twenty-one large exposures suitable for study, flow till is thought to be present in thirteen, or 62% of the total. Data from soil maps and observations made in numerous road cuts also indicate the probability that flow till is widely distri­ buted in the Kalamazoo Moraine and associated portions of the Interlobate Morainic Tract. In summary, flow till appears to be a widespread sediment at the surface within the Kalamazoo Moraine and is very similar to that previ­ ously reported in the literature. fied types For example, both massive and strati­ of flow till were recognized in the area. In addition, most of the major characteristics of flow till were observed, such as (1) interfingering with glaciofluvial sediments, (2) orientation of striated pebbles parallel to the direction of movement, lenses and horizons, (4) sharp planar contacts with subjacent materials, (5) "overconsolidated" nature when dry, relatively fresh exposures, within the landscape, (3) presence of sandy (6) smooth vertical faces in (7) presence in higher topographic positions (8) association with ice-contact slopes, and (9) till fabric parallel to maximum surface slopes. The presence of this flow till in the Kalamazoo Moraine indicates that at least a portion of that feature was deposited in an environment in which ice stagnation was very common. 34 Considerable slumping at four of the sites precluded positive identification of flow till. 81 Lacustrine Sediments Deposits of pebbleless clays and silts exist at various places in the Saginaw Lobe portion of the Interlobate Morainic Tract and also within and north of the drainageway at Pinckney (Figure 23). Mechanical analysis of samples 83 (NEJiNW^SW^s sec. 30, T. 1 N., R. 4 E.) and 174 ( SW^sSWJfiNEijj sec. 9, T. 1 S., R. 3 E.) yielded textures of clay and silty clay, respectively. The sediments are generally massive, although bedding is visible locally. The bedding, fine texture, and scarcity of pebbles all indicate a lacustrine origin. Maximum thickness of the sediments was observed at site 83, where a road cut exposed 10 to 15 feet (3.0 to 4.5 m) of the material. 35 Sand often exists above and below the lacustrine sediments, and very fine sand partings are visible within the deposits at some places. In many exposures the sediment is massive, and at some locations bedding is vis­ ible but no rhythmites were observed. Not all visible bedding planes were horizontal; for example, steep dips and deformation may be observed at sites 174 and 194 (SW^SWJsNEis sec. 30, T. I N . , (SW^SWJ^NEJi sec. 30, T. I N . , R. 4 E.). At site 195 R. 4 E.) a 1.5-foot-thick (0.5 m) layer of lacustrine sediment is faulted with a 3-foot (1 m) vertical displacement. The silt and clay deposits are often near ice-contact slopes. Because these sediments were always observed in contact with sands and gravels, and never with adjacent or overlying till, it is reasonable to conclude that deformation is due to an ice-contact origin and is not the result of a readvance and overriding of the ice. This must be donsidered a minimum thickness because the sedi­ ments extend to an unknown depth below the road grade. 82 TIN PINCKNEYC 00 pat Livingston Co. | Washtenaw Co. re u s o n 95 36 | ___ 1 HALFM O O N L. 184 — CTO' 202 NORTH L. I 176 180 TIS R4E » R3E LACUSTRINE • D E P O S IT A L T IT U D E SEDIMENTS < 9 3 0 F E E T (2 8 3 .5 M), EXAM IN ED IN D E T A IL ▲ D E PO SIT A L T IT U D E ^ 9 3 0 F E E T ( 2 8 3 .5 M ), E X A M IN E D IN D E T A IL O D E PO SIT A L T IT U D E ^ 9 3 0 F E E T ( 2 8 3 .5 M ), L O C A TIO N FR O M S O IL M A P A D E P O S IT A L T IT U D E 5 5 9 3 0 F E E T ( 2 8 3 .5 M ), LO C A T IO N FR O M S O IL M AP OR L E V E R E T T F IE L D N O T E B O O K S U R F IC IA L D R IF T IN TE R LO B A TE 123 S IT E CO NTACT M O R A IN IC TRACT BO U N D A R Y NUM BER O____ [ MILE Figure 23. KM Lacustrine Sediments N 83 Clay mineralogy and geomorphic findings indicate that the Saginaw/ Huron-Erie drift contact is about 0.7 miles (1.1 km) east of site 83 and approximately 1.8 miles (2.9 km) east of site 174 (Figures 10 and 23). X-ray diffraction of samples from these sites yielded relatively high 7&/lo£ ratios (1.16 and 1.09, respectively), which are indicative of Saginaw Lobe provenance and imply that here there was little or no mix­ ing of sediment-laden meltwater from the two lobes during the time the lacustrine sediments were deposited. Had there been such extensive mix­ ing, one would expect the 7X/I 0 X ratios to be nearer the 0.91 value which separates Saginaw and Huron-Erie drift. Since this is not the case, the watersheds of the ice-contact lakes in which the sediments .were derived and deposited were most likely quite small. Recent soil maps show Sisson, Kibbie, or Colwood soils (lacustrine 36 parent materials) developed on several of the silt and clay deposits. As noted previously in this chapter (p. 50), some of the soils associ­ ated with the lacustrine sediments observed are also mapped as Miami (till parent material) on the modern soil surveys. In this study it was not feasible to determine the exact distri­ bution of the lacustrine sediments in and near the Interlobate Morainic Tract for the following reasons. 1. The number of exposures available for observation were limited. 2. Recent soil maps of the area are at too small a scale (1:15,840) to show many of the soils associated with lacustrine deposits, as they tend to be rather small. 36 Arkport soils are believed to have both lacustrine and outwash sediments as parent materials and are present in the interlobate area. This soil series is not shown on Figure 23 because none of the twentyseven silt and clay deposits observed were mapped as Arkport by recent soil surveys. 84 3.Some of the lacustrine deposits which are large enough to be shown on soil maps are classified as Miami soils which have till as parent material. 4. Some lacustrine deposits have a cover of sand which may exceed 5 feet (1.5 m) in thickness and therefore were probably not detected during soil mapping. Leverett wrote (notebook 275, melted north into T. I N . , p. 92) that when the ice margin R. 1 W . , an outwash apron with an altitude of about 930 feet (283.5 m) was deposited just north of Rives Junction in the Grand River valley, partially filling it. He believed that this apron acted as a threshold ponding the waters to the south at a level of 930 feet (283.5 m) 37 until it was trenched by river erosion and that the resulting lake covered a considerable area north of the Kalamazoo Mo38 raine. Furthermore, he considered the possibility that this ponding at 930 feet (283.5 m) may also have affected portions of the Interlobate Morainic Tract. Of the eighteen bodies of lacustrine sediment observed on the Saginaw Lobe side of the Interlobate Morainic Tract, four were at alti­ tudes higher than 930 feet (283.5 m) (Figure 23). This suggests that, if the ponding envisioned by Leverett did take place, not all, and possi­ bly none, of the lacustrine sediments are necessarily associated with it. Those silt and clay bodies with altitudes greater than 930 feet (283.5 m) appear to be associated with small ice-contact lakes with limited 37 Marginal notes in Leverett's hand on Rives Junction and Stockbridge topographic maps on file at the Geological Survey of Michigan. 38 A lake with dimensions of at least 2 miles (3.2 km) by 10 miles (16 km) could be expected to have formed beaches. Although a search was made for such features, especially on air photos, none were located. watersheds, and not the large lake Leverett hypothesized for the Grand and Portage River drainage areas. If this large lake did exist, some of the lacustrine sediments at or below 930 feet (283.5 m) may have been associated with small ice-contact ponds separated from the large lake by stagnant ice. X-ray diffraction data from sediments collected at alti­ tudes of less than 930 feet (283.5 m) may provide evidence of whether or not the lake existed and if sediment-laden meltwaters from both lobes flowed into it. Brill Lake Till— Characteristics and Type Section One of the most important sediments in the area is the flow till exposed at Brill Lake (hereafter referred to informally as the Brill Lake till) because it is believed representative of much of the surficial till of the Saginaw Lobe in the Kalamazoo Moraine and associated areas of the Interlobate Morainic Tract between Jackson and Pinckney. In most exposures of the study area this surficial Brill Lake till overlies, or is intercalated with, outwash of the Saginaw Lobe. The type section is in a pit at the north end of Brill Lake (site 81, SE^sSE^SWJs sec. 15, T. 2 S., R. 1 E.), where 12 feet (3.7 m) of massive flow till overlies 12 feet (3.7 m) of stratified flow till, which is underlain by at least 20 feet (6.1 m) of outwash sands. 39 Brill Lake till has only been recognized at, or very near, the surface, and the maximum observed thickness was 25 feet (7.5 m ) . Oxidized and unleached, it is a very pale brown (dry) or yellowish brown (moist). the till is variable but most commonly is sandy loam. 39 Texture of Sand lentils and Other representative sections are at site 183 (SWJaSEJjSW^ sec. 2, T. 1 S., R. 3 E.), site 191 (SE^SEljSWJi sec. 2, T. 1 S. , R. 3 E.), and site 161 (N*sSEi*SEJs sec. 7, T. 2 S., R. 2 E.). 86 sandy horizons are common. Orientation of certain elongate stones within Brill Lake till may be quite variable at some locations and generally re­ flect its flow-till origin. Glaciolacustrine sediments are found in con­ tact with outwash associated with the Brill Lake till. With the excep­ tions of a higher crystalline content and a lower shale content, pebble lithology of the till is quite similar to that of the till associated with the Mississinewa Moraine to the east and south (see description of Chelsea till in this chapter). X-ray diffraction of clays from the till matrix, and also of associated lacustrine clays, always yields a dis­ tinctive 7 X/I 0 X. peak height ratio of 0.91 or more which serves to iden­ tify its Saginaw Lobe provenance. Detailed information on the Brill Lake till and its distribution is presented in this chapter and Appendix B. Drift Associated with Mississinewa Moraine and Related Portions of Interlobate Morainic Tract Soils as an Indicator of Parent Material The soils in the higher, proximal portions of the Mississinewa Moraine (Boyer, Fox, Spinks, and Owosso) are developed largely on sands and gravels. On the lower, distal portions of the moraine, till parent materials are more common (Miami, Conover, Kidder, and Hillsdale soils). Soils of the Huron-Erie segment of the Interlobate Morainic Tract are in general coarse-textured, having glaciofluvial parent materials. However, finer-textured soils derived from till are slightly more common here than in the Saginaw Lobe sector. Along the surficial Huron-Erie/ Saginaw drift contact, soils associated with glaciofluvial materials are predominant (Boyer, Spinks, and Fox) although small soil bodies developed on till are present (Miami, Conover, Brookston, and Kidder). On the 87 eastern margin of the Interlobate Morainic Tract, soils associated with glaciofluvial materials (Boyer, Oshtemo, Fox, and Spinks-Oakville) are most common, but soils with till parent material (Miami, Kidder, Riddles) are more widespread than to the west near the interlobate drift contact. Clay Mineralogy 40 Twenty-two till samples from the Mississinewa Moraine, associated portions of the Interlobate Morainic Tract, and the area immediately to the east were analyzed according tr the procedures described in Appendix B. Twenty—one of the samples produced 7X/10& ratios or 0.90 or less, and all samples were from sites located east and south of a line connecting Leverett, Riley, Stofer, and Russell Hills, the east end of Patterson Lake, and Pinckney (Figures 9 and 10).^ The range of the 7&/10& ratios is 0.38, with the highest being 0.91 from site 225 (SEifiNEJsSE^ sec. 17, T. 2 S., R. 3 E.) and the lowest being 0.53 from site 146 (SWJfiSW^SWJz; sec. 12, T. 3 S . , R. 3 E.) . X-ray diffraction of clays extracted from four samples of glacio­ fluvial sediments from beneath the surficial till of the Mississinewa Moraine produced data quite similar to that of samples from surficial till. At site 234 (SW^SE^SW^s sec. 19, T. 2 S. , R. 4 E.), proximal to the moraine, the surficial till has a 7&/10& ratio of 0.79, and the clays removed from the underlying glaciofluvial sediments at a depth of 20 feet (6.1 m) have a value of 0.84. At site 146 the surficial till ratio was 0.53, and clays from the glaciofluvial material beneath at a depth 40 A total of twenty-four till, four bedrock, and four glaciofluvial 7&/10& ratios was determined for this portion of the study area. 41 All thirteen surficial till samples analyzed from sites proximal to, and in, the Kalamazoo Moraine and associated portions of the Inter­ lobate Morainic Tract had 7X/10& ratios of 0.91 or more. of more than 10 feet (3 m) yielded a ratio of 0.59. Till from a sample site on the crest of the Goose Lake Esker (site 148— NW^SE^SW^ sec. 329 T. 2 S., R. 3 E.) produced a ratio of 0.83, and clays from the underly­ ing glaciofluvial material, a ratio of 0.87. Site 143 (NW^NWifiNVft; sec. 22, T. 3 S., R. 3 E.) produced a surficial till ratio of 0.90, and clays from glaciofluvial materials 8 feet (2.4 m) below the surface, a ratio of 1.00. On the basis of this evidence, it seems reasonable to conclude that most of the buried glaciofluvial materials near the surface are of Huron-Erie provenance. If a planimetric outline of the Mississinewa Moraine is projected downward to the bedrock surface, it will encircle portions of the Upper Mississippian Michigan and Marshall Formations (primarily sandstones). A sample of Mississippian Napoleon Sandstone, a part of the Marshall Formation, was collected in a quarry in the town of Napoleon within a few hundred yards (m) of its type section. from this sample (number 230— The clay minerals removed SE*sSE*3jSW*s sec. 31, T. 3 S., R. 2 E.) gave a 7.&/10& ratio of 10.7 (scale factor 16). Two samples (numbers 227— 228— NW^sNW^SE^ sec. 3, T. 4 S., R. 5 E., and SW^SE^SWis sec. 12, T. 2 S., R. 6 E.) of surficial till from the Outer Defiance and Fort Wayne Moraines of the Huron-Erie Lobe, 15 miles (25 km) to the east of the Mississinewa Moraine, produced 7R/10& ratios of 0.87 and 0.86. If it is assumed that samples 227 and 228 are repre­ sentative of Huron-Erie till to the east, any incorporation of Napoleon Sandstone as the lobe moved westward would likely cause 7X/10& ratios to increase resulting in values of more than 0.90. If this reasoning is correct, it may be concluded that during deposition of the Mississinewa Moraine Huron-Erie ice was probably not generating drift from the 89 underlying sandstone. Another local bedrock unit was analyzed to determine what effect it might have on the Huron-Erie Lobe till. Lower Mississippian Coldwater Shale subcrops east of the Mississinewa Moraine, but is not known to be exposed anywhere in the study area. Three samples of the shale were ob­ tained from the well-cuttings library of the Michigan State University Department of Geology. The oil well from which the cuttings were derived is located in W^SE^SEh; sec. 22, T. 2 S., R. 3 E. (site 235, permit number 11655). The Coldwater Shale is 617 feet (188.1 m) thick here, and X-ray samples 235A, B, and C were taken 27 feet (8.2 m ) , 117 feet (35.7 m ) , and 457 feet (139.3 m) from the top of the shale on the assumption that be­ cause of the regional structural pattern sample 235A would be somewhat similar to shale subcropping just to the east of the moraine, that sample 235B might be representative of shale subcropping somewhat farther east, and that sample 235C is similar to shale subcropping about 15 miles (24 km) to the east (approximately beneath Ann Arbor). Clays from these samples produced 7&/loS. ratios of 2.16 (235A), 1.00 (235B), and 1.00 j2 (235C). The variation between clay samples from bedrock (7&/10& ratios of 1.00 or more) and surficial till (7&/10& ratios of 0.90 or less) may indicate that in this area Huron-Erie ice was not in contact with Cold- . water Shale during deposition of the surficial till of the Mississinewa Moraine. This would be possible if a subsurface drift sheet which pre­ dates surficial tills protected the bedrock from ice of the last advance. Leverett and Taylor (1915, p. 199), Russell and Leverett (1908, pp. 4-5), and Kunkle (1960, p. 29) discussed a hard till found at depth in Washtenaw ^2Chung (1973) determined that 7&/10& ratios decreased with depth in Coldwater Shale in the central part of Michigan also. County which they considered to be pre-Wisconsin(an) or early Wisconsin(an) in age. The presence of wood, peat, and apparent oxidized till in the subsurface in and near the study area, as discussed earlier in this chapter, also suggests the presence of an older drift sheet in the sub­ surface. Thus, the possibility exists that the characteristic 7&/10& ratio of surficial Huron-Erie drift in this part of the Mississinewa Moraine may be due to one or both of the following conditions: 1. An older subsurface drift sheet may have protected the Coldwater Shale and Mississippian sandstone from ice of the last advance pre­ venting incorporation into the till and a consequent increase in 7&/10& ratio. 2. The incorporation of a portion of this subsurface drift sheet may have caused surficial tills in the moraine to have 7^,/loS. ratios somewhat lower than those on the surface of the Fort Wayne and Outer Defiance Moraines. 43 Till Color The color of dry, oxidized, unleached till from the Mississinewa Moraine is very uniform, with twenty of the twenty-three samples investi­ gated having colors of 10YR 7/3 or 10YR 7/4 (very pale brown). Moist colors are also very similar, with eighteen of the samples 10YR 5/4 (yellowish brown) or 10YR 4/4 (dark yellowish brown) (Appendix C ) . Till Texture On the whole, unleached surficial tills associated with the Mississinewa Moraine are medium-textured (Figure 11). Mean texture of all till samples in and proximal to the Mississinewa is loam (sand 46%, Assuming this subsurface drift has a low 7&/10X ratio. 91 silt 30%, clay 24%). Mean texture of five samples from sites located proximal to the moraine is slightly coarser (sandy clay loam, sand 48%, silt 27%, clay 25%) than samples from seventeen sites within the moraine (loam, sand 45%, silt 30%, clay 25%). It should be noted these are mean figures and that individual samples may differ considerably from these values. Pebble Lithology The lithology of 100 pebbles collected from Huron-Erie till at each of the four sites where till fabric was determined within the Mississinewa Moraine is quite similar to that reported in previous studies by Anderson (1957) and Kneller (1964). Figure 24 shows that the greatest variation in results of the three studies was in the carbonate fraction: Anderson's data indicate a value of 64.3%, and data from this investigation indicate a value of 52.2%, or a difference of 12.1%. With this exception the vari­ ation between all other lithologic fractions was considerably less than 44 10%. 4 Shale exists in moderate amounts in the till and is most commonly dark brown in color. This contrasts markedly with samples of Coldwater Shale from well cuttings, which tend to be light to medium gray. Only rarely are fragments of coal found, and these are generally too small and fragile to excavate and measure. This observation agrees with Kneller's (1964) low value of 0.2% coal (Figure 24) for Huron-Erie drift.^ 44 Kneller's data (1964, Table 2) does not include 0.4% in his "others" and "armored mud balls and till clods" fractions. ^ M o r s e (1970, p. 19) stated that coal is an "indicator lithology" for Saginaw drift. Both Kneller's work and this study show that coal is also present in Huron-Erie drift but is less common than in Saginaw drift. 92 to V to 70 60 to 40 tz o 30 • I ANDERSON (1957) / / 0 KNELLER (1964) / / [ ] TH IS STUDY / 50 / e'­ en / 20 ✓ / * / 10 / t tu CO UJ z 15 z o en oc ac CJ Figure 24. ■■ / U> —; IO ~ ^ CM CM IO to to 3 ® ® CM CD a> n m IS. iiO .On UJ _J •I a: co UJ z o Jco Q z < CO tr UJ UJ ^ •U pH •H *"3 . pH CO X pH b iM i •H o fr-l t o pci a *—\ h a) a. V a) CO co 1-3 •pH pH pH 13 u01 cd u a) 0 o pH 00 c o PQiS o •H EH a> a O 4J CO H3 cd 4-1 cd a o -O J-4 a cd o co 632 630 618 10 2 2 - 1 0 0. 0 99.7 97.8 1.6 0.3 0.3 - Boulder Distribution The only major concentration of boulders in the Mississinewa Mo­ raine is south of Mill Creek (Figure 13). It is a linear tract of boul­ ders distal to the Sharon Short Hills and trends northeast-southwest across the northern half of T. 3 S . , R. 3 E. In places this line of boulders appears to be associated with meltwater channels that extend west on the flank of the moraine to the Grass Lake Plain. For the most part, the remaining boulders in the moraine are widely scattered. Till Fabric Till fabrics determined at three sites within Huron-Erie Lobe till show well-developed orientations IS., R. 4 E. , and 104— (sites 79, 101— NElfiNW^SEJs sec. 29, T. SWJsNE^SWJs sec. 33, T. 2 S. , R. 3 E.), and a fourth (97) has an irregular, multimodal pattern (Figure 14). The pri­ mary modes of fabrics 101 and 104 are oriented normal to the Mississinewa Moraine and associated areas of the Interlobate Morainic Tract. Pre­ ferred dips at these sites are to the east and southeast and may indicate flow from that quadrant. 94 Site 79 (NW^SW^SEiz; sec. 12, T. I S . , R. 3 E.) is located in a road cut near the crest of a linear feature trending N. 60° E. that is probably associated with final ice disintegration. In the exposure approximately 5 feet-(1.5 m) of till overlies at least 4 feet (1.2 m) of sand. Al­ though the well-developed till-fabric orientation with a preferred south­ east dip suggests that the till may be basal, the form and stratigraphy of the feature indicate the probability that it is flow till. The fabric at site 97 (NW^SWJsNW^ sec. 27, T. 1 N . , R. 4 E.), from a till exposure in a small ridge with ice-contact slopes trending N. 5 5 ° E . , is rather unusual. The till contains loamy sand and sandy loam lenses, and its fabric has similarities to the fabric at site 78 of the Saginaw Lobe, which is interpreted to be a flow till. Like the Saginaw Lobe site, the long axis of almost every clast in the fabric has a southerly dip, yet there is also a pronounced transverse mode directed to the southwest. Although the primary mode is nearly normal to nearby ice-contact slopes, it is also nearly parallel to fabrics 101 and 104 of the Huron-Erie Lobe, which are interpreted to be representative of basal till. Thus, the evidence is contradictory whether the sediment at the site is basal or flow till and whether the fabric is due directly to glacial deposition or the downslope movement of material induced by gravity. The absence of large exposures in the Huron-Erie portion of the Interlobate Morainic Tract or in the Mississinewa Moraine limits the possibility of recognizing the extent of flow till in the area (see discussion on pp. 78-80). three sites (Figure 22). Flow till is positively recognized at only From the limited evidence available, it appears that it may not be as common as in the Kalamazoo Moraine. Kneller (1964, 95 p. 30) concluded that much of the surficial till overlying sand and gravel in T. 2 S., R. 3 E. and T, 3 S., T. 3 E. is either flow till or ublatlon tl.11.. However, until more data are available, the character­ istics, extent, and distribution of flow till in the Mississinewa Moraine and associated areas of the Interlobate Morainic Tract will not be known. Lacustrine Sediments Deposits of almost stone-free silt and clay which are ordinarily of limited extent are scattered throughout the Huron-Erie side of the Interlobate Morainic Tract (Figure 23). They are located at, or within 2 miles (3.2 km) of, the surficial Saginaw/Huron-Erie drift contact, and most exposures of this clay and silt have maximum dimensions of less than 100 yards (m). On soil maps the deposits are most often associated with Kibble, Sisson, or Colwood soils. The maximum observed thickness was 8 feet (2.4 m) at site 95 (NW^NW^sNE^ sec. 32, T. 1 N. , R. 4 E.). However, the deposit could be thicker because an unknown amount also exists below the lower limit of the exposure. At every location where visible, the subjacent material is sand and gravel. In some places the deposits are overlain by a thin layer, generally 3 feet (0.9 m) or less, of sand. Hand-texturing of numerous samples in the field and .laboratory analysis of sample 202 all indicated fine textures (silty clay loam, sand 4.3%, silt 61.1%, clay 34.6%). Pebbles are very rare in these sediments, and no clasts larger than about 2 inches (5.1 cm) were ob­ served. Fine texture, the absence of large numbers of pebbles, and an occasional observation of bedding indicate a lacustrine origin. If this interpretation is correct, the pebbles may have been deposited from the melting of floating drift-laden ice in a lacustrine environment. 96 A sample of lacustrine sediment from site 202 ( S E ^ N E ^ E ^ sec. 7, T. 1 S., R. 4 E.), with an altitude of 935 feet (285.0 m) and located 1.5 miles (2.4 km) east of the surficial Saginaw/Huron-Erie drift contact, yielded a 7&/10& ratio of 0.64, well within the range of values associ­ ated with Huron-Erie drift (Figures 10 and 23). This may indicate that the watershed of the water body in which the sediments were deposited was of limited extent and probably did not receive sediment-laden meltwater from nearby Saginaw Lobe ice. At site 196 (SE*sSE%NWi£ sec. 29, T. I N . , R. 4 E.) (altitude 915 feet or 278.9 m) an exposure of massive silts and clays, at least 3.5 feet (1.1 m) thick and 50 feet (15.2 m) long, is juxtaposed with a 10foot-wide (3.0 m) body of fine sand which is in turn flanked by a 15foot-wide (4.5 m) body of sand and gravel (Figure 25). Contacts between the units are sharp, rather than gradational, and almost vertical, with a lack of distinct bedding in the sand and gravel. Considerable defor­ mation was also observed about 100 yards (m) to the southeast at site 200 (SW^fiSW^sNE^ sec. 29, T. I N . , R. 4 E.) (altitude 925 feet or 281.9 m) . Here massive lacustrine sediment is in contact with a body of fine sand. Where visible, beds in the sand have dips varying from horizontal to 80°, and an extension of the main body of lacustrine sediment protrudes about 3 feet (0.9 m) down into the sand as if faulted into position. On the basis of this evidence it seems likely the situation at site 196 is due to postdepositional faulting and subsidence of the sediments of a small ice-contact lake. 46 An ice-contact origin is also probable at site 200 because a numher of nearby depressions appear to mark the former 46 The sharp, vertical contacts between sand and gravel, fine sand, and lacustrine sediments give little support to an interpretation of the deposit representing a horizontal facies change. location of ice blocks. Similar relationships are visible in several other exposures in the area. SOUTH SHARP CONTACT S feet (1.5m) SAND a GRAVEL M ASSIVE a — SAND GRAVEL 2 5 feet (7. S m ) Figure 25. 3.5 feet LACU STR IN E SED IM EN TS FINE SAND 7 5 feet ( 2 3 m) Section in a Deposit of Lacustrine Sediments (Site 196) In 1921, when Leverett investigated the formations of the Stockbridge quadrangle, much of the land was in private ownership and under cultivation. He was able to observe (notebook 274, pp. 69-70) "clay" between Halfmoon and North Lakes associated with the tops and flanks of hills and also in intervening depressions. Elevations of the bottoms the depressions are from 920 to 930 feet (280.4 to 283.5 m ) . of He noted a knoll 30 feet (9.1 m) high (crest altitude 960 feet or 292.6 m) in the CE% sec. 12, T. 1 S., R. 3 E. that was covered with "clay" and a similar knoll in NE% sec. 13. One mile (1.6 km) to the east, near the south shore of Halfmoon Lake, a similar situation was discovered during the course of this investigation (site 202— 4 E.). SEhNEhiNEh sec. 7, T. I S . , R. A lengthy road cut on the flanks of a hill reveals 6 feet (1.8 m) of pebble-free silty clay loam (sand 4.3%, silt 61.1%, clay 34.6%) with the material extending below road grade. Near the crest of the hill the top of the deposit of fine sediment is at an altitude of about 940 feet (286.5 m ) , and at the base of the hill at about 910 feet (277.4 m ) . Although occasional fine sand partings are visible in the sediments, they are generally massive. lacustrine 98 In the Huron-Erie portion of the Interlobate Morainic Tract nine deposits of lacustrine sediments were studied during field work for this investigation. Of these nine sites five (95— 4 E., 176— CNE**NW% sec. 14, T. I S . , T. I S . , N^C sec. 32, T. I N . , R. 3 E . , 180— R. 3 E. , 184— CNW^s sec. 12, T. I S . , R. N^NW^SE^ sec. 14, R. 3 E. , and 202) were situated above 930 feet (283.5 m) and so cannot be directly related to Leverett’s hypothesized ponding of the Grand and Portage River lowlands (see pp. 8 4 - 8 5 ) . ^ The 7£/loX ratio at site 202 seems to indicate that the watersheds for these small ice-contact lakes were limited in area. Unfortunately, no 7X/I 0 X. ratios of lacustrine sediments are available for any sites at, or below, 930 feet (283.5 m ) . Therefore, it is not possible at this time to suggest if any mixing of sediments and meltwater from the Saginaw and Huron-Erie Lobes took place near the drift contact in the hypothesized ponded waters— if indeed the ponding extended that far east. Chelsea Till— Characteristics and Type Section The till exposed near Chelsea (hereafter informally referred to as the Chelsea till) is thought to be representative of the surficial till of the Huron-Erie Lobe in the Mississinewa Moraine and associated areas of the Interlobate Morainic Tract between Norvell and Pinckney. Chelsea till is often overlain by up to 5 feet (1.5 m) of outwash sediments. The type section is in a road cut 3 miles (4.8 km) northeast of Chelsea on the proximal side of the Huron-Erie portion of the Inter­ lobate Morainic Tract 47 (site 101— NEJ^NW^SEiz; sec. 29, T. I S . , R. 4 E.). Sites 180 and 184 are at altitudes of between 960 and 970 feet (292.6 and 295.7 m ) . 99 Here a thin layer of sand overlies 8 feet (2.5 m) of sediment interpreted to be lodgement till. in the area. surface. A flow till facies of Chelsea till is also present Chelsea till has only been recognized at or very near the When oxidized and unleached, it is, according to the Munsell notation, a very pale brown (dry) or yellowish brown (moist). the till is rather variable but is commonly loam. thickness was 14 feet (4.3 m ) . Texture of The maximum observed Fabrics in Chelsea lodgement till indi­ cate ice flow from the east and southeast. Pebble lithology of Chelsea till resembles that of Brill Lake till of the Saginaw Lobe (see descrip­ tion of Brill Lake till in this chapter), although the crystalline fraction is somewhat less and the shale content somewhat more in the Chelsea till. X-ray diffraction of clays from the till matrix, and also of associated lacustrine clays, yields a distinctive 7&/10& peak height ratio of venance. 0.90 or less, which serves to identify its Huron-Erie Lobe pro­ More detailed information on Chelsea till and its characteris­ tics in the study area is given in this chapter and Comparison of Brill Lake and Chelsea Table 10. Tills The color and boulder lithology of the Brill Lake and Chelsea tills are so similar it is not possible to identify the lobe provenance of till samples on the basis of these characteristics. Although Brill Lake till samples are often somewhat coarser than Chelsea till samples, it does not appear feasible positively to identify all, or even most, till samples on the basis of texture. A similar situation may hold if attempts are made to identify individual till samples on the basis of pebble lithology. The primary modes of fabrics determined in Brill Lake till are not ordinarily well developed, and clasts tend to he horizontal or have a apr* ■■■■ 100 predominant dovm-glacier dip. slope movement as flow till to be flow till. This is most likely the result of downand much of the Brill Lake till is believed Some till fabrics from deposits of Chelsea till have similar characteristics and may also represent flow till. However, other fabrics determined in Chelsea till have well-developed primary modes with a predominant up-glacier dip and are thought to represent lodgement till. Lodgement till is probably more common in Chelsea than in Brill Lake till. All thirteen samples of Brill Lake till and two samples of associ­ ated lacustrine sediment that were X-rayed had 7£/10& ratios of 0.91 or more. Of the twenty-two samples of Chelsea till and one sample of asso­ ciated lacustrine sediment that were analyzed, twenty-two had 7&/10& ratios of 0.90 or less. Thus, the clay mineralogies of the Brill Lake and Chelsea tills are distinctively different and provide a basis for identification in areas where drift thickness is at least 20 feet (6.1 m) or so. On the basis of the clay mineralogy a line may be drawn connect­ ing Leverett, Riley, Stofer, and Russell Hills, the east end of Patterson Lake, and Pinckney, which is interpreted to represent the surfical con­ tact between Saginaw and Huron-Erie drift. Topographic information is given in Chapter 4 which also indicates that the interlobate contact is located along this line. Drift Associated with Grass Lake Plain and Related Areas Soils as an Indicator of Parent Material A 1930 soil survey by Veatch, Trull, and Porter resulted in a map which shows most of the Grass Lake Plain as having Fox and Plainfield soils. Comparison of more recent soil surveys in Washtenaw and Living­ ston Counties with surveys completed in these counties at about the same 101 time as the 1930 Jackson survey indicates that Boyer, Oshtemo, and Spinks soils are also likely to be included in the old Fox mapping unit. On this basis it may be reasonable to conclude that sand and gravel is very common on the Grass Lake Plain, as all the soil series mentioned above have outwash as parent materials (Figure 8). The older Jackson County survey indicates that Hillsdale soils, interpreted to have till parent materials, exist primarily south of Wolf Lake. The limited work com­ pleted on a m o d e m survey indicates that Riddles soils, with till parent material, are also present in the area. Rifle peat is the most common organic soil on the Grass Lake Plain and is found in undrained depressions and along drainage lines. Clay Mineralogy Till is not common on the surface of the Grass Lake Plain north of Center Lake, but it is exposed over considerable areas in the south. Twelve till samples from the plain were X-rayed; seven have 7&/10& ratios greater than 0.91, and five have ratios less than 0.90. Of the samples with a ratio more than 0.91 one is from north of Wolf Lake (Figure 26), two are from the vicinity of Willow Creek, and two are from the crest of the Blue Ridge Esker. One of the samples with a 7&/loX ratio less than 0.90 is from a site north of Wolf Lake, two are from the vicinity of Willow Creek, and four are from locations on either side of the Blue Ridge Esker. Two samples, number 132 (SW^NW^sSW% sec. 12, T. 3 S., R. 1 E.) and 213 (SW^sNW^SE^ sec. 14, T. 3 S. , R. 1 E.), are from tills located north of Wolf Lake and produce 78/loS ratios of 1.17 and 0.88, respectively. This indicates that the drift contact is situated just north of Wolf Lake somewhere between these two samples. Topographic evidence, A R2E M C EN TER LAKE WOLF L ACKERSON STONY L. 77 U NAPOLEON NORVELL 0. 69^*7 SURFICIAL DRIFT CONTACT IN SOUTHWEST OF STUDY AREA 0.85 > > Hr '76 Figure 26. 7A/I0A RATIO OF TILL SAMPLE DRIFT CONTACT ESKER PORTION miles km Surficial Drift Contact in Southwest Portion of Study Area H o NJ 103 consisting of the slopes of the outwash surfaces associated with the Kalamazoo and Mississinewa Moraines, support this interpretation. Four till samples, numbers 218 (NE*sNElsSEJ£ sec. 3, T. 4 S., R. 1 W.), 223 (SE*£SEJsNE*s sec. 24, T. 3 S., R. 1 W.), 217 (NW^SW^SE^ sec. 32, T. 3 S., R. 1 E.) , and 133 (NE%SE^SE?s sec. 2, T. 4 S. , R. 1 E.), obtained from exposures near the Blue Ridge Esker, all produce 7&/10& ratios indi­ cating Huron-Erie provenance <0.75, 0.78, 0.66, and 0.69, respectively). This seems to indicate that the esker was deposited in Huron-Erie but close to the interlobate contact. ice However, two till samples from the crest of the esker, 219 (SW^SE^EJs sec. 27, T. 3 S. , R. 1 E.) and 220 (SEiiNE*^!)!^ sec. 6, T. 4 S., R. I E . ) , yield ratios of 1.96 and 1.50, respectively. provenance. These very high ratios appear to indicate Saginaw Lobe Thus, four till samples from sites north, northwest, west, and east of the esker indicate Huron-Erie provenance, and two till sam­ ples from the crest of the esker seem to indicate Saginaw provenance. It is not possible at this time to explain this seemingly anomalous situation. Any explanation must consider the fact that two till samples from the crest of the esker have very high 7&/10& ratios, suggesting Saginaw Lobe provenance, and four samples of till from either side of the esker have ratios of less than 0.90, indicating Huron-Erie provenance. In an attempt to determine the lobe provenance of the finer esker sediments clay was removed from five glaciofluvial samples collected at three sites along the trend of the esker (site 212— T. 3 S. , R. 2 E. , site 216A— site 220— SEJsNE^sNWiz; NE^sSE^SW^s sec. 17, N E ^ S E ^ E ^ sec. 28, T. 3 S. , R. I E . , sec. 6, T. 4 S., R. 1 E.). and X-ray diffraction data from these samples show 7R/I 0 X ratios of 1.22, 0.96, 1.86, 2.50, and 1.83 (Figure 9). These ratios appear to indicate a Saginaw provenance 104 for the clays in the glaciofluvial sediments. However, the ratios are so high it seems more likely that considerable kaolinite from sandstone boulders in the esker is dispersed in the sediments so as to preclude certainty about lobe provenance of the sediments on the basis of clay mineralogy. X-ray diffraction data were obtained from four samples of till exposed approximately 3 miles (4.8 km) north of Norvell (Figure 26). Peak height ratios indicate that two of these samples, 211 (NE^SW^NWis sec. 20, T. 3 S., R. 2 E.) and 226A (NEH;SE^SW^ sec. 14, T. 3 S., R. 2 E.) (0.76 and 0.82, respectively), are associated with deposition by the Huron-Erie Lobe. The remaining samples 231 (HEhiNEszNEh sec. 21, T. 3 S., R. 2 E.) and 226 (NW^SE^SWis sec. 14, T. 3 S. , R. 2 E.) yield ratios of 0.96 and 1.30, respectively. Saginaw Lobe provenance. These higher ratios seem to imply a However, two water-well records on file at the Geological Survey of Michigan and interviews conducted by Frank Leverett (notebook 166, p. 70) indicate that sandstone is within 5 feet of the surface nearby (Figure 7). The (1.5 m) proximity to Huron-Erie samples 211 and 226A and the slope of the outwash surfaces suggests that samples 226 and 231 may actually be Huron-Erie tills that have an unusually high kaolinite content because of the influence of local bedrock. Samples 226 and 231 seem to be the only till analyzed in which there is strong evidence of local bedrock altering the 7&/10& ratio of Huron-Erie Lobe till to resemble that of Saginaw Lobe till. 48 The northernmost till sample on the Grass Lake Plain has a 7.8/loX ratio indicative of a Saginaw Lobe origin, and most of the other tills on the plain have ratios suggesting Huron-Erie Lobe provenance. 48 Because of Such evidence is lacking for the till samples from the crest of the Blue Ridge Esker. 105 the scarcity of till on portions of the plain and the proximity of bed­ rock to the surface in some places, it does not seem possible to trace the drift contact across the entire Grass Lake Plain on the basis of the clay mineralogy of tills. However, on the basis of geomorphology it is probable that the drift contact in T. 3S. , R. I E . , is located between sites 132 and 213 (Figure 26). Till Color Eight of the twelve till samples from the Grass Lake Plain area have Munsell colors of 10YR 7/3 or 10YR 7/4 (very pale brown) when dry, and ten have colors of 10YR 5/4 (yellowish brown) and 10YR 4/4 (dark yellowish brown) when moist (Appendix C ) . As in the nearby moraines it is not possible on the Grass Lake Plain to differentiate Saginaw and Huron-Erie Lobe tills on the basis of color. Till Texture Figure 2 7 indicates that most of the till samples from the Grass Lake Plain have textures similar to those of the Huron-Erie Lobe in the Mississinewa Moraine (Figure 11). This is in general agreement with peak height ratios, which also indicate that most of the samples are of Huron-Erie provenance. Nevertheless, it is not possible positively to differentiate lobe provenance of surficial tills on the Grass Lake Plain on this basis. M e an texture 107 Boulder Distribution Boulders exist in moderate numbers in T. 4 S., R. I E . , southern portion of T. 3 S., R. 1 E. (Figure 13). and in the No obvious pattern to the distribution exists except that boulders are almost always associated with areas underlain by till. In his field notes Leverett (notebook 166, p. 69 and notebook 299, p. 38) reported a "boulder strip" south of Wolf Creek 49 trending eastward in S., R. 2 E. secs. 13, 14, 15, 16, 20, 22, and 23, T. 3 Although a careful search was made both in the field and on air photos, the presence of the concentration cannot be completely con­ firmed because boulders were observed in secs. 14, 15, and 16 only. Absence of Striations Sandstone bedrock is very near the surface at Napoleon, and although Leverett (notebook 32, p. 59) reported that the surface of the bedrock in the local quarries was smooth, as if glaciated, he did not observe any striations. During this investigation a search was made for striations in two quarries on the east side of Napoleon (SE^SE^SW^ sec 31, T. 3 S., R. 2 E. and site 230— NEH$E%NW% sec. 6, T. 4 S., R. 2 E.), but none were found. Till on Crests of Eskers At three sites(219— SEJ^NE^NW^ sec. R. I E . ) 6, T. 4 S., R. I E . ; and 221— on the Stony Lake Esker, E. ;220— SEJsSW**NW% sec. 6, T. 4 S. , on the Blue Ridge Esker and at one (214— 4 S., R. 1 E.) crests. SWJsSE^sNE^ sec. 27, T. 3 S. , R. 1 NW^NE^SW^; sec. 11, T. till was observed on the esker The till is generally massive and spalls off in sheets when struck, but not as readily as in the Brill Lake till type section. 49 Labeled "Willow Creek" on the Manchester quadrangle. The 108 long axis of many of the pebbles is subhorizontal, but few sandy horizons are visible. Structures that might be associated with ice shove are gen­ erally lacking in both the till and subjacent sand and gravel. Flint (1928, p. 411) has stated that till on the crests of eskers is not un­ common. Such till is generally thought to be from the ice overlying the eskers. Maximum observed thickness of the till was 7 feet (2.1 m) at site 2 2 0 . Rock-Stratigraphic Units Defining informal rock-stratigraphic units on the Grass Lake Plain is considerably more difficult than in the nearby moraines because expo­ sures of till north of Wolf Lake are limited in number and because south of Wolf Lake the proximity of sandstone to the surface appears to influ­ ence the clay mineralogy of some till deposits. However, it does seem possible to identify the lobe provenance of till on the plain with some degree of confidence by using analyses of clay mineralogy and landforms. Surficial till associated with the Saginaw Lobe exists only in the northern portion of the Grass Lake Plain and is hereafter informally re­ ferred to as the Grass Lake till-Saginaw Lobe. it is very similar to the Brill Lake till. Although slightly older, The surficial till of the Huron-Erie Lobe is located only in the southern portion of the plain and is hereafter referred to informally as the Grass Lake till-Huron-Erie Lobe. It is slightly older and has somewhat more variable characteristics than the Chelsea till, although these two tills are basically very simi­ lar . Chapter 4 GLACIAL LANDFORMS Introduction The study area may be divided Into four morphologic sections: (1) Kalamazoo Moraine, (2) Mississinewa Moraine, Tract, and (4) Grass Lake Plain area (Figure 2). (3) Interlobate Morainic Each of these sections and their distinctive surficial characteristics are described in this chapter, and a genesis suggested for many of the individual landform types. In his report accompanying the Glacial Map of Canada, Prest (1968, p. 8) used the term "kame moraine" to signify an ice-marginal complex including many kames, and a predominance of glaciofluvial deposits as compared to till. The term is applicable to some end moraines and many interlobate mo­ raines. . . . Such moraines cover large areas and probably due to infilling of depressions by glaciofluvial deposits may not look like moraine on air photos. Prest's definition is used in this dissertation and is applied to the portions of the Kalamazoo Moraine and Interlobate Morainic Tract in the study area.^ Flint (1971, p. 199) has defined a moraine as "an accumulation of drift deposited chiefly by direct glacial action, and possessing initial constructional form independent of the floor beneath it." It was shown in the previous chapter that the surficial sediments of the Kalamazoo Moraine consist largely of glaciofluvial sediments and flow till. Many declivities interpreted to be ice-contact slopes exist within the feature and appear to be associated with the deposition of drift in the presence of stagnant, not active, ice. Furthermore, the underlying bedrock has had a strong influence on the formation of the moraine. Thus, if Flint's definition is used, the linear feature trending northeast from Jackson to Leverett Hill cannot be considered a moraine at all. Similarly, Boulton (1972, p. 385) might consider the portion of the Kalamazoo Moraine under study to be an "inverted fluvio-lacustrine mold of an ice-cored moraine." 109 110 Relationship Between Bedrock Surface and the Kalamazoo Moraine Although it is reasonable to conclude that climatic conditions and general regimen were major factors influencing the Saginaw Lobe, the ex­ act postioning and configuration of this part of the Kalamazoo Moraine is believed to be closely associated with the nature of the underlying bedrock surface. It is evident from Figures 4 and 8 that the distal boundary of the moraine very nearly coincides with the trace of the 900foot (274.3 m) bedrock-surface contour. North of this contour the bed­ rock surface is generally at an altitude of less than 900 feet (274.3 m ) , and to the south, on the sandstone tableland, it is at an altitude of 900 to 1,000 feet (274.3 to 304.8 m ) . Thus, the planimetric outline of the moraine is located above the lower altitude bedrock and trends along the northern edge of the buried sandstone tableland, and the Grass Lake Plain is situated above the higher altitude bedrock. Kalamazoo Moraine The segment of the Kalamazoo Moraine which trends northeast from Jackson to Leverett Hill is about 15 miles (24 km) long and 3 to 5 miles (4.8 to 8.0 km) wide. Local relief 2 in this Saginaw Lobe moraine in­ creases from between 50 to 100 feet (15.2 to 30.5 m) in the west near Jackson to 230 feet (70.1 m) in the east near Leverett Hill (Figure 28). Maximum altitudes in the moraine also tend to increase eastward from about 1,020 (310.9 m) near Jackson to 1,164 feet (354.8 m) at Prospect Hill "B" (SW^SE** and SEkSW*£ sec. 1, T. 2 S. , R. 2 E.) (Figure 29). The amount of relief in a survey section as determined from topographic and hydrographic maps. PFTv 111 LOCAL RELIEF (R E L IE F / S E C T IO N ) SURVEY I— I 0 - 4 9 FEET (0 -I4 .9 M ) dZl 5 0 - 9 9 F E E T (I5.2-30.2M ) ES3 I 0 0 - I 4 9 FEET (3 0 .5 -4 5 .4 M ) I 5 0 - I 9 9 FEET (4 5 .7 - 6 0 .7 M) 2 0 0 - 2 4 9 FEET (6 I.0 -7 5 .9 M ) o ____ miles 10 kilometers 1 lr '7 6 Sources' U.S. Geol. Surv. topographic maps ft Mich. Dept. Natural Resources hydrographic maps Figure 28. Local Relief 112 R3E MAXIMUM R4E ALTITUDES □ 8 8 0 - 9 4 9 F E E T ( 2 6 8 . 2 - 2 8 9 . 3 M) EZ1 9 5 0 - 9 9 9 F E E T ( 2 8 9 . 6 - 3 0 4 .5 M) 1 ,0 0 0 -1 ,0 4 9 F E E T (30 4.8-31 9 .7 M) 1 ,05 0 - 1,099 FEET ( 3 2 0 .0 - 3 3 5 .0 M) 1,100-1,168 F E E T ( 3 3 5 .3 - 3 5 6 .0 M) o miles 10 kilometers Source: U.S. Geological Survey topographic maps '76 Figure 29. Maximum Altitudes 113 West of Brill Lake the surface of the moraine is rather irregular with little zonation of features apparent. East of the lake mazoo Moraine may be divided into four latitudinal zones: (2) zone of linear depressions and ridges, 3 the Kala­ (1) crest area, (3) zone of lakes and bogs, and (4) northern zone of linear depressions (Figure 30). A fifth zone, the Portage River lowland, is recognized north of the moraine. the zones has a distinctive landform assemblage. Each of In the following sec­ tions these zones will be described and an interpretation of their gen­ esis presented. Crest Area More than 60 percent of the survey sections along the crest, or southern portion, of the Kalamazoo Moraine have altitudes of 1,050 feet (320.0 m) or more and are thus well above the level of the adjacent Grass Lake Plain, which has an altitude of 1,000 to 1,030 feet (304.8 to 313.9 m). West of Brill Lake the crest is lower than 1,050 feet (320.0 m) , is not well defined, and is difficult to identify at some places because it tends to be only a few feet (m) higher than the general level of the Grass Lake Plain (Figure 29). East of Brill Lake the crest of the mo­ raine is higher, and well defined, and an apron-like surface underlain by sand and gravel slopes to the south, merging with the Grass Lake A Plain at an altitude of about 1,020 to 1,030 feet (310.9 to 313.9 m) . The crest is commonly bounded on the north by a very steep, east-west— trending, north-sloping declivity which may be well over 100 feet (30.5 3 The longitude of Brill Lake also marks the separation of other characteristics of the moraine which will be considered later in this chapter. 4 Steep-sided depressions may locally obscure this relationship. v5 HILLS e> BRILL L J OUTWASH FAN a ESKER SUGARLOAF ^W ELC H L CLEAR PROSPECT G /LLE TTS A \ LAKE \ A g ille tts ff'J HANGING CHANNEL l* eskerA POND A LILY A acrevasse FILLING A B N Kalamazoo Moraine Mississinewa Moraine C D E F CROOKED SACKRIDER HILL AGRASS LAKE AESKER A A FRANCISCO AESKER A GRASS LAKE PLAIN OUTWASH APRON ZONE OF LINEAR DEPRESSIONS AND RIDGES ZONE OF LAKES AND BOGS NORTHERN ZONE OF LINEAR DEPRESSIONS ■ PORTAGE RIVER LOWLAND CREST OF MORAINE MORAINE BOUNDARY LINEAR DEPRESSIONS AND RIDGES OUTWASH FAN Hr ‘76 Figure 30. Diagram of a Portion of the Kalamazoo Moraine miles kilometers approximate scale 114 CHANNEL FILLING 115 m) high (Figures 31 and 32). South North OUTWASH APRON CREST 1,050 F T (3 2 0 .0 M)' GRASS LAKE PLAIN RIDGE DEPRESSION 0 .2 5 -0 .5 MILE _____________ 0 .1 -0 .2 5 M IL E ___ (0.4-0.8K M ) —T (0.2-0.4K M ) FAN ON CREST 1,050 F T ___ (3 2 0 .0 M) Figure 31. Schematic Profiles of Kalamazoo Moraine Crest Area, East of Brill Lake On the basis of sediment, form, and regional relationships it seems clear that the sand-and-gravel surface which slopes south from the crest should be interpreted as an outwash apron formed by numerous streams depositing glaciofluvial materials as they flowed from the sur­ face of the glacier."* The crest and outwash apron are not conspicuous west of Brill Lake, where bedrock altitudes are generally less than 900 feet (274.3 m ) , but are well developed east of Brill Lake where the sub­ strate is at higher altitudes. See Thwaites (1963, p. 52) for a discussion on how the outwash apron associated with the moraine may be distinguished from the Grass Lake Plain. 116 The east-west-trending declivity which slopes to the north from the crest is ordinarily very steep and is inclined 27 to 29° from the horizontal at both Sackrider Hill and Prospect Hill "B." It is inter­ preted to be an ice-contact slope which marks the approximate location where glaciofluvial sediments were deposited against ice of the Saginaw Lobe. Only a few very shallow gullies, probably due to man-induced ero­ sion, are visible on the slope. Okko (1962, pp. 37-38) states that ice- contact slopes unmarked by fluvial erosion are evidence of deposition by subaerial streams because subglacial streams would likely erode channels on the proximal slopes. T h u s , it appears that the outwash apron was deposited an an alluvial fan at the ice margin. A number of gravelly knobs, such as Prospect Hill "B" and Sackrider Hill, are located along the crest (Figure 30) and form the highest points in the moraine with maximum altitudes of more than 1,050 feet (320.0 m ) . These asymmetric, cone-shaped features appear to mark the sites where especially large streams deposited sand and gravel at the margin and built outwash fans above the surface of the outwash apron.^ The steep northern slopes of the fans indicate an ice-contact origin. In most places there is little or no morphological evidence of these superglacial streams in the present landscape, but in the sec. 16, T. 2 S., R. 2 E . , a large, relatively flat feature trending south merges with such a fan. Flanked by steep, apparent ice-contact slopes with several angular bends along its course the feature is interpreted to be a large channel filling marking the course of a subaerial stream which supplied sediment to the fan. The county soil survey (Veatch, Trull, and Porter, 1930) indicates that a portion of the feature is covered with Hillsdale sandy loam, a 6 These fans are also discussed in the section of this chapter con­ cerned with the Grass Lake Plain. 117 soil interpreted to have till as parent material. This may be a cap of flow till, or, as the old Hillsdale mapping unit may include large amounts of glaciofluvial materials, it may mark bodies of flow till on the surface of the channel filling. Although glaciofluvial processes appear to have been predominant on the outwash apron of the Kalamazoo Moraine, Hillsdale soil with till parent material has been mapped (Veatch, Trull, Porter, 1930) in the sec. 17 and EJg sec. 18, T. 2 S. , R. 2 E. just west of Sackrider Hill. On air photos this lobe-shaped area contrasts with its surroundings due to lesser micro-relief. surface of the apron. It is the only known deposit of till on the There is no indication of a readvance of the ice which would permit deposition of basal till on the outwash apron, but there is abundant evidence of stagnant ice in the area. Because this till is on the crest of the moraine, it cannot represent a postglacial mass movement deposit from a higher area. The topographic position, smooth surface, and lobate form of this unit indicate that it is flow till which postdates accumulation of the outwash apron but predates the ablation of ice at the ice-contact slope proximal to the crest. Hester and DuMontelle (1971, pp. 367-82) discuss similar features associated with the Shelbyville Moraine in Illinois and state that they represent lobes of flow till deposited during deglaciation of the moraine. About 1 mile (1.6 km) west of Sackrider Hill a channel 30 to 40 feet (9.1 to 12.2 m) deep extends down the south-sloping sand and gravel apron into the SE^s sec. 19, T. 2 S., R. 2 E. The channel originates at the steep north-facing slope of the crest where its bottom is 40 feet (12.2 m) above a linear depression. Limited numbers of considerably smaller features are also visible along the crest of the moraine. One 118 of these, a 5-foot-deep (1.5 m) channel, trends southeast down the slope of Prospect Hill "B." the crest. All of these channels are well developed, even at This indicates that they were eroded by streams flowing off the Saginaw Lobe after most of the apron had been deposited but before deglaciation was complete. Zone of Linear Depressions and Ridges East of Brill Lake a number of linear depressions and ridges are located immediately to the north of the crest (Figure 31). tures are oriented parallel to the trend of the moraine. These fea­ Most commonly a sharp-crested sand-and-gravel ridge is separated from the crest by one of the linear depressions. A series of three or four additional sand- and-gravel ridges and linear depressions may be located to the north. Small lakes or bogs are often located in the depressions.^ These linear features are very striking in the field, on topographic maps, and espe­ cially on air photos. All the ridges and depressions form a zone which is approximately 0.5 miles (0.8 km) wide (Figure 30). The linear depressions are somewhat variable in size but average about 200 to 250 feet (61 to 76 m) in width and 1,000 to 1,300 feet (305 to 396 m) in length although a dimensions of the ridges few exceed 2,000 feet (610 m ) . also vary, but commonly they are 200 to 300 feet (61 to 93 m) wide and 1,200 to 1,300 feet (366 to 396 m) long, al­ though some are larger. feet (15.2 to 30.5 m) Bottoms of the depressions may be 50 to 100 lower than adjacent ridge tops with relief in­ creasing eastward toward Leverett Hill. Boulders may be visible on the flanks of ridges or in dry linear depressions, but no regular pattern is discernible. The 119 According to Charlesworth (1957, p. 415), steep-sided ridges and depressions with trends parallel to the kame moraines in which they are situated are common (see also Boulton, 1972; Bogacki, 1973; and Galon, 1973). Generally these moraines contain large amounts of sand and gravel, and the ridges and depressions are believed to be due to depo­ sition of glaciofluvial materials in contact with fractured, stagnant ice (Virkkala, 1963, p. 28; Fogelberg, 1970, p. 38; and Boulton, 1972, pp. 385-86). In the study area the ridges have steep slopes, sharp crests, relatively uniform dimensions, symmetrical form erosional channels on their slopes. and they lack Their presence in a linear zone 0.5 miles (0. 8 km) wide and 10 miles (16.0 km) long parallel to the crest of the moraine indicates that they were deposited by meltwater in a fracture zone in stagnant ice at the margin of the Saginaw Lobe. Adjacent linear depressions mark the former positions of ice blocks between the fractures. This zone of linear depressions and ridges is best developed east of Brill Lake, where nearby bedrock has altitudes of 900 feet (274.3 m) or more. The zone is either very poorly developed, or not present, west of the lake where bedrock altitudes are generally less than 900 feet (274.3 m). The causes of crevasse systems parallel to, or very near, the margins of ice sheets are not always clear although some are associated with the underlying bedrock surface. For instance, Fogelberg (1970, pp. 44, 65) cites numerous examples of linear ridges which are thought to have formed in crevasse systems at the edge of stagnant ice masses on high bedrock surfaces. Also Virkkala (1963, pp. 46-47, 70) notes that linear ridges of sand and gravel deposited in crevasses parallel to the ice margin are most common on the down-glacier sides of bedrock lows. 120 The zone of ridges and linear depressions In the Kalamazoo Moraine is also situated on the down-glacier side of a low-altitude bedrock area where the bedrock surface rises to a rather high altitude under the Grass Lake Plain. There is also evidence of the former presence of large blocks of stagnant ice on the Grass Lake Plain very near the Kala­ mazoo Moraine. Thus, it seems likely the bedrock surface was responsi­ ble, at least in part, for the crevasse system thought to have been pre­ sent at the stagnant margin of the Saginaw Lobe. The difference topography east and west of Brill Lake also seems to be related to the altitude of the bedrock surface. Fogelberg (1970, p. 78) made a similar observation about the Second Salpausselka of Finland when he stated that "deglaciation of the different marginal sections depended on vari­ ations in the topography of the substratum; this had important effects on the geomorphological activity of the ice margin and the meltwater." Zone of Lakes and Bogs Five lakes in the Kalamazoo Moraine between Jackson and Leverett Hill have surface areas greater than 110 acres (44.5 ha) (Table 7). g With the exception of Gilletts Lake all of the lakes are located about 0.5 miles (0.8 km) north of the crest of the moraine and form a zone about 1 mile (1.6 km) wide which has more lakes and bogs and fewer highrelief features than areas to the north or south (Figure 30). All five of the lakes have a neighboring lake to the north or south, either in the moraine or on the Grass Lake Plain. Relief in this zone is generally subdued, and most of the higher features which are present seem to be associated with the zones to the O Spelling of this name is variable— "Gilletts," "Gillett's," "Gillett," and "Gillette." "Gilletts" seems to be preferred locally. 121 south or north. Ice-contact slopes and flow till are common in this zone. Table 7. Large Lakes and Their Neighboring Lakes Neighboring Lake Large Lake In Kalamazoo Moraine In Grass Lake Plain Sugarloaf — Crooked Clear — Pond Lily Welch — Goose "A " 9 Brill Gilletts — Gilletts Brill — The presence of ice-contact slopes, flow till, and large lakes and the relatively low altitude (940 to 960 feet or 286.5 to 292.6 m) of much of this area indicate that a zone of stagnant ice was present during final deglaciation. Most of the lakes are 20 feet (6.1 m) or less in depth; and, according to hydrographic maps, at least three— Clear, and Welch— the water. Brill, seem to have ice-contact slopes below the surface of Although some of the lakes appear to have formed by ablation of buried ice associated with bedrock valleys (see Figure 5), some are situated over areas of high bedrock altitude. This may mean that their bottoms mark the approximate altitude of the base of the Saginaw Lobe during moraine deposition. On the basis of the few available exposures, the higher features in the zone seem to be k a m e s , for they consist primarily of ice-contact stratified drift deposited by meltwater flowing south or west. 9 Sec. 24, T. 2 S . , R. 1 E. Some of 122 these kames have flow till at the surface. Boulton (1968, p. 410) has stated that flow till may be formed when an ice margin is in compression due to (1 ) overriding of a bedrock obstacle, (2 ) stagnation of ice at the margin, and (3) decrease in the slope of the glacier bed. It has been shown (1) that the Kalamazoo Moraine is situated adjacent to a bedrock high; (2) that numerous ice- contact features, generally interpreted to be indicative of stagnant ice, are present at and near the crest of the moraine and in the zone of lakes and bogs; and (3) that the bedrock surface in the area tends to rise to the south— a gradient up which the Saginaw Lobe had to flow. Boulton indicates that any one of the three conditions is sufficient to permit flow-till formation, and it has been shown that all three prob­ ably existed in the study area during deposition of the Kalamazoo M o ­ raine. This helps to account for the widespread distribution of flow till believed present in the area (Figure 22). Asymmetric fan-shaped features of glaciofluvial materials with very steep slopes on their northern sides are located in this and sub­ sequent zones to the north and will be discussed in this section. The features resemble the high, fan-shaped hills along the crest of the moraine but are smaller. Three of these smaller fans have narrow ridges of sand and gravel trending into their steep northern slopes. All these features are interpreted to be outwash fans which were deposited in con­ tact with stagnant ice by meltwater streams. Their consistent southward slope indicates that the source of the meltwater was generally to the north. Those fans with associated ridges may mark the location of small esker streams and their deltas. Northern Zone of Linear Depressions North of the lake zone, on the proximal side of the moraine, is a tract about 1 mile (1.6 km) wide in which surficial till is more common than In the zone along the c r e s t . ^ Linear depressions with steep slopes are present here but tend to be smaller and not quite as well developed as in the zone near the crest. The orientation of these northern depres­ sions is generally parallel to the moraine. The linear depressions to the east, near the meridian of Leverett Hill, are quite obvious on air photos but are somewhat less conspicuous on topographic maps and are more difficult to observe in the field than are the larger depressions to the west or to the south in the zone near the crest. Accompanying high-relief ridges are rare, but an area north of Goose Lake "A" and west of Welch Lake contains a number which are up to 50 feet (15.2 m) in height. Although somewhat similar in appearance to the zone of linear de­ pressions and ridges near the crest, this zone differs from it in several ways: (1 ) ridges are not as pronounced; (2 ) although the linear depres­ sions are distributed in a zone parallel to the crest of the moraine, the individual depressions tend to be concentrated in four groups; well-developed outwash apron is not present; (3) a (4) flow till is more common here than in the crest area. Apparently the northern zone of linear depressions was formed in a manner somewhat similar to that of the zone of linear depressions and ridges to the south near the crest. However, the fractures in the ice ^ F i g u r e 8 is based on the 1930 soil survey map, which shows most of the zone as Hillsdale sandy loam (till parent material). As noted previously in Chapter 3, the old Hillsdale mapping unit contains consid­ erable amounts of sand and gravel. 124 may not have been as deep or deposition may have been less because the ridges between the depressions are not well developed. The bedrock sur­ face beneath this portion of the moraine is generally well below 900 feet (274.3 m) in altitude(Figure 4). However, a few outliers of the sandstone tableland are present in the subsurface. Three of the four groups of depressions that exist in the area are situated above these outliers and seem to be associated with them. It appears likely that these local bedrock highs caused the ice of the Saginaw Lobe to fracture, permitting the accumulation of sediments within crevasses. Although a well-developed outwash apron is not associated with the zone, two kame-like features consisting primarily of glaciofluvial sediments are located at the north end of Clear Lake and about 1.5 miles (2.4 km) west of Brill Lake. Both appear to have an ice-contact origin and are oriented parallel to the crest of the moraine. Flow till is more common at the surface here than in the vicinity of the crest. This indicates that till was present on the surface of stagnant blocks of ice in the area and perhaps that glaciofluvial depo­ sition was not predominant in this zone as it was in the zone of linear depressions and ridges to the south, where the ridges are larger, flow till is less common, and an outwash apron is present. Portage River Lowland The Portage River lowland is a tract 1 to 3 miles (1.6 to 4.8 km) wide and more than 15 miles (24 km) long north of the Kalamazoo Moraine (Figure 30). Its average altitude in the east is about 930 feet (283.5 m) and about 920 feet (280.4 m) in the west where the Portage River flows into the Grand River north of Jackson. Leverett referred to this feature as the "Portage Swamp" (Leverett and Taylor, 1915, p. 197). 125 The landforms situated on the lowland west of the longitude of Brill Lake are considerably different from those east of that line. A feature as much as 30 feet (9.1 m) high, 800 feet (245 m) wide, and 0.5 miles (0.8 km) long is located in sec. 8 , T. 2 S . , R. I E . , west of Brill Lake. It is underlain by till with numerous cobble-sized clasts on the surface and slopes to the north. Three channels, up to 12 feet (3.7 m) deep, trend down the north-sloping surface. in the feature expose large amounts of flow till. Ground silos Steep marginal slopes on the south indicate an ice-contact origin, and the morphology suggests that it is a deposit of flow till which moved downslope off a nearby block of stagnant ice. 11 The three channels appear to "hang" and suggest that meltwater flowed over the till feature from nearby stagnant ice after it was deposited. This is the only large landform in the study area thought to consist almost entirely of flow till. A number of hills of both high and low relief exist on the lowland east of Brill Lake. These features are aligned in a linear fashion nearly parallel to the Kalamazoo Moraine (Figures 2 and 30), and they appear to merge with the moraine in sec. 6 , T. 2 S., R. 2 E. According to the soils map (Veatch, Trull, and Porter, 1930), till is quite common on the surface of the hills. Linear depressions are almost totally lacking in the lowland, and the hills have fewer very steep slopes than in any of the zones to the south. East of the longitude of Brill Lake the landscape is more like the area to the north, near the Charlotte Moraine, than the topography west of Brill Lake or in the Kalamazoo Mo­ raine. Furthermore, if the line of hills is traced eastward, it merges ■^A small outwash fan and associated feeding esker are located immediately to the east and also indicate the presence of stagnant ice. with a spur of the Charlotte Moraine a few miles west of Pinckney. All of these factors suggest a different mode of deglaciation here than in the Kalamazoo Moraine, where stagnation seems to have prevailed. It appears that this zone marks a position held by an active ice margin for a relatively short time and which in its subsequent retreat may have left isolated blocks of stagnant ice. This margin seems to have been more active in the east than in the west, where there is evidence of stagnation. Relationship of Bedrock Surface and Mississinewa Moraine A comparison of Figures 4 and 8 shows that the Mississinewa Moraine is located along the south and east flanks of the buried sandstone table­ land. This correspondence in shape and location is so similar, even in certain details, that the relationship is almost certainly not coinci­ dental . The trace of the 900-foot (274.3 m) bedrock-surface contour is situated very close to the distal edge of the moraine. 12 One of the highest points on the buried tableland is in sec. 8 ., T. 3 S . , R. 3 E. and is within 1 mile (1.6 km) of the change in trend of the moraine near Mill Creek. In fact, this bedrock high probably deflected ice flow and, in conjunction with the regime of the Huron-Erie Lobe and the relatively steep eastern flank of the sandstone tableland, helped determine the location of the Mississinewa Moraine. The Mill Creek lowland also appears to be associated with the bed­ rock surface, for the surficial trace of the southern tributary of the 12 The distal edge of the Kalamazoo Moraine is also situated along the surficial trace of the 900— foot (274.3 m) bedrock contour. 127 burled Lima valley (Chapter 2) is situated along the lowland. 13 As mapped on Figures 2 and 8 , the southwestern terminus of the Mississinewa Moraine in the study area is located where the trend of the moraine intersects the surficial trace of the 900-foot (274.3 m) bedrock contour. The .difference in topography north and south of Mill Creek may be partially the result of differences in bedrock configuration beneath the two areas, just as the bedrock seems to have caused differences in mor­ phology east and west of Brill Lake in the Kalamazoo Moraine. The sand­ stone tableland beneath the southern part of the Mississinewa Moraine riser? more abruptly from the shale lowland than in the north, because it is 4 miles (6.4 km) or less between the 800- and 900-foot (243.8 and 274.3 m) bedrock contours in the south and almost twice that distance in the north. Furthermore, the 900-foot (274.3 m) bedrock contour trends northeast-southwest across T. 3 S., R. 3 E., and may have been oriented almost normal to Huron-Erie ice flow. In T. 2 S . , R. 3 E. the contour trends north-south and may only have been oriented obliquely to the ice flow. Mississinewa Moraine The portion of the Mississinewa Moraine within the study area is about 17 miles (27 km) long and trends north-northeast from a point near Norvell to the north-central portion of T. 3 S . , R. 3 E . , where it bears north toward Leverett Hill (Figure 2). The width of this Huron-Erie Lobe moraine varies from about 0.25 miles (0.4 km) to 4 miles (6.4 km), and local relief is from less than 50 feet (15.2 m) near Norvell to more than 180 feet (54.9 m) in the Sharon Short Hills (Figure 28). 13 Maximum Few well records are available in this area. The bedrock con­ tours in secs. 4, 5, and 6 , T. 3 S., R. 3 E . , are shown on Figure 4 ex­ actly as calculated by the computer and have not been hand-modified. 128 amounts of local relief tend to be located near the crest, which is situated along the proximal (east and southeast) side of the moraine. Maximum altitudes in the south near Norvell are about 960 feet (292.6 m ) , rise to a maximum of approximately 1,140 feet (347.5 m) in the Sharon Short Hills, and decrease to about 1,025 feet (312.4 m) near Lev­ erett Hill (Figure 29). Much of the moraine north of Mill Creek and also near Norvell is only slightly higher than the Grass Lake Plain, and a considerable portion of it is lower. The moraine merges with the Grass Lake Plain, commonly very gradually, at altitudes of 980 to 1,020 feet (298.7 to 310.9 m) in the south and approximately 1,020 feet (310.9 m) in the north. The Mississinewa Moraine may be divided into north and south sections, which are separated by Mill Creek (Figures 32 and 33). Southern Section of Mississinewa Moraine The highest point in this portion of the Mississinewa Moraine, with an altitude of 1,140 feet Sharon Short Hills (Figure 29). wash and till in secs. (347.5 m) , is along the crest in the This site is part of an apron of out­ 16, 17, 18, 19, and 20, T. 3 S., R. 3 E., which merges gradually with the Grass Lake Plain. Although the surficial till here has a lobelike shape, it is dissimilar to the till on the outwash apron of the Kalamazoo Moraine. feet or 12.2 m) in a quarter-section, numerous boulders, and meltwater channels which tend South of Mill sand and gravel are its trend. 14 14 Differences include greater relief (40 to converge to the west. Creek a number of linear depressions and ridges of proximal to the crest of the moraine and parallel to The ridges are sharp-crested, approximately 200 feet (61 These features resemble the linear depressions and ridges proxi­ mal to the crest of the Kalamazoo Moraine. 129 A ZONE OF LOW RELIEF SAND a GRAVEL FEATURES B ZONE OF LINEAR DEPRESIONS a RIDGES APRON OF OUTWASH a T IL L C D E LEVERETTj H IL L M IL L L. M ILL CREEK LOWLAND CREST OF NORTHERN SECTION LINEAR DEPRESSIONS a RIDGES ICE-CONTACT SLOPE 3 0 - 1 0 0 F E E T ( 9 - 3 0 M) HIGH MORAINE BOUNDARY TRANSITIONAL BOUNDARY □ A CEDAR CAVANAUGH LAKE BOULDERS DRY CHANNEL Chelsea M I LL L^. / ESKER V ✓ ✓ / Z O N E A OF I R R E G U L A R Francisco □ D E P R E S S I O N S GOOSE L .„ ESKER 't t GOOSE LAKE * ■** FRANCISCO A ESKER BLUE RIDGE ESKER /• •/ / ^ TUCKER L a •*. ESKER h ✓ X SHARON SHORT HILLS T IL L C Kalamazoo Moraine Mississinewa Moraine □ Norvell 2 miles d Kilometers approximate scale •llr'76 Figure 33. Diagram of a Portion of the Mississinewa Moraine frh7>ri«. 130 m) wide, and up to 1,500 feet (460 m) long, but average perhaps 800 to 1,000 feet (245 to 305 m ) . the ridges. Depressions are about as long and wide as Relief from the bottom of a depression to the crest of an adjacent ridge averages 50 feet (15.2 m) or less. The discontinuous zone of linear depressions and ridges is about 0.5 miles (0.8 km) wide. The form, materials, local relationships, and bedrock conditions associated with portions of the Kalamazoo Moraine and the Sharon Short Hills of the Mississinewa Moraine are so alike that they suggest similar origins. Landforms and sediments indicate that both were deposited in and near a fracture zone along an ice margin and that both have associ­ ated outwash aprons which grade into the Grass Lake Plain. However, there are enough differences to indicate that the details of deglaciation in both areas were somewhat different. This is evidenced by the absence of outwash fans along the crest of the Mississinewa Moraine. Also, the zone of linear depressions and ridges associated with this moraine is not as continuous nor as well developed as that in the Kalamazoo Moraine. Finally, since the linear ridges and depressions are located in a single zone, there appears to have been only one fracture zone in the HuronErie Lobe and three in the Saginaw Lobe during deposition of the moraines. Although not as widespread as in the Kalamazoo Moraine, there is evidence of stagnant ice in the Mississinewa Moraine. The crest of an esker-like ridge situated in a steep-walled depression in the E h sec. 8 , T. 3 S., R. 3 E . , is lower in altitude than the nearby surface of the outwash apron. Two meltwater channels on the apron east of the depres­ sion in sec. 9 appear to continue into sec. 8 on the west side of the depression. These channels apparently had no effect on the crest alti­ tude of the ridge. This suggests that the ridge formed beneath a mass 131 of stagnant Ice and that meltwater streams flowed across the top of the ice. In addition to this ridge and the zone of linear depressions and ridges proximal to the crest, there is additional evidence of stagnation in and near the Mississinewa Moraine. A steep-sided ridge of sand and gravel 40 feet high (12.2 m) trends completely through the moraine near Tucker Lake onto the Grass Lake Plain. It is almost 3 miles (4.8 km) long and may extend farther to the south of River Raisin. Too long and sinuous to be a crevasse filling, it is interpreted as an esker and will be referred to as the Tucker Lake Esker. West of the esker the evidence of ice stagnation, both in and distal to the moraine, is even more com­ mon and is in the form of steep, ice-contact slopes in glaciofluvial sediments. Northern Section of Mississinewa Moraine Variations in trend of the Mississinewa Moraine in T. 3 S., R. 3 E., give it a concave westward form (Figure 33). In fact, this concavity is so pronounced that the segment south of Mill Creek is oriented nearly normal to the segment north of Mill Creek. Mill Creek flows northeast in a lowland that extends northeastward from the Grass Lake Plain and bisects the moraine. The altitude of the lowland is approximately 1,000 feet (304.8 m) at the Grass Lake Plain-moraine contact and about 940 feet (286.5 m) at the proximal side of the moraine. It is 0.5 to 0.75 miles (0.8 to 1.2 km) wide, is under­ lain by much organic soil, and has a very steep and linear north flank which varies from 30 to 60 feet (9.1 to 18.3 m) in height. The south flank of the lowland is not as precipitous. ■^Both Willow Creek and the Blue Ridge Esker trend southwestward along the extension of the lowland onto the Grass Lake Plain. The Mill Creek lowland has characteristics of both a subglacial drainageway and a lowland associated with a buried bedrock valley. The eastward gradient of about 15 feet per mile (2.9 m per km), opposite to the flow direction of glacial meltwater, suggests that it does not have a subaerial origin. Linear sand-and-gravel ridges within the lowland that appear to be the head of the Blue Ridge Esker indicate a subglacial origin. However, the width of the feature, the pronounced ice-contact slope on the north, and the presence of the southern tributary of the buried Lima valley beneath the lowland (Figure 5) seem to indicate a collapse origin due to the ablation of buried ice. It may well be that it has a dual origin with both glaciofluvial erosion and collapse invol­ ved in its genesis. North of Mill Creek lowland the nature of deglaciation appears to have been considerably different than in the Sharon Short Hills to the south. For a distance of 4 miles (6.4 km) north of the creek the crest of the moraine is at an altitude of about 1,030 to 1,060 feet (313.9 to 323.1 m ) . Here, ice-contact slopes are visible on both the proximal and distal sides; few, if any, linear depressions exist; and no well-defined outwash apron is apparent. A tract 2 to 3 miles (3.2 to4.8 km) wide, with hills 30 to 50 feet (9.1to 15.2 m) higher than the numerous adja­ cent kettles, is located between the crest and the Grass Lake Plain. In fact, much of this portion of the moraine has an altitude from 20 to 80 feet (6.1 to 24.4 m) lower than the surface of the Grass Lake Plain. ^ L e v e r e t t (notebook 274, p. 75) mapped the Grass Lake PlainMississinewa Moraine boundary partially on the basis of the number of kettles present. He considered those areas with many depressions to be morainic and those with relatively few to be outwash plain. "^For a discussion of such situations see Thwaites (1963, p. 43). 17 ] 33 Tills suggests that deposition took place in contact with stagnant ice. With final ablation the ice blocks formed the kettles which are so common in this area and which may be as large as half a survey section. The western edge of this tract is indicated by a considerable decrease in the number of ice-contact depressions along a line trending north from Mill Creek along the county line to Francisco and thence northeast to the southeast flank of Leverett Hill. This line almost certainly marks the margin of the Huron-Erie Lobe when Leverett Hill was formed. Southwest of Chelsea a lowland, 0.25 miles (0.4 km) wide, breaches the crest of the moraine. It has a slope to the east of 15 feet per mile (2.9 m per km), and along its southwestward extension a 30 foot (9.1 m) high ridge of sand and gravel trends southwest past Goose Lake "B" 18 to within 0.5 miles (0.8 km) of the Blue Ridge Esker which trends west from the Mill Creek lowland. The lowland near Chelsea is interpre­ ted to have formed as a subglacial drainageway due to its eastward slope and the associated sand-and-gravel ridge which is believed to be an esker and is here named the Goose Lake Esker. The stream which deposited the esker may also have supplied meltwater and sediments to the Francisco Esker, as the two eskers seem to have been part of an integrated drain­ age system and may have had their confluence at the S^C sec. 31, T. 2 S . , R. 3 E. North of the lowland the crest of the moraine is less well defined and is in the form of several sand-and-gravel knobs with altitudes of 1,030 to 1,040 feet (313.9 to 317.0 m ) . A large sand-and-gravel ridge trends northwest past Cedar and Mill Lakes in secs. 4, 9, 15, and 16, T. 2 S., R. 3 E. Two relatively flat, delta-shaped features are situated 1Q S E h sec. 31, T. 2 S., R. 3 E. ppi'--/ 134 along its length. This feature is too long to be a crevasse filling and is interpreted to be an esker with two deltas or outwash fans along it. It will be referred to as the Mill Lake Esker. Relationship of Bedrock Surface and Interlobate Morainic Tract Almost all of the bedrock surface northwest of a line connecting Leverett Hill, Russell Hill, and Pinckney has an altitude of 800 feet (243.8 m) or more. Much of the bedrock surface southeast of this line is at an altitude of less than 800 feet (243.8 m) (Figures 4 and 32). Leverett Hill is situated in the angle between the Kalamazoo and Mississinewa Moraines. Its location within 0.5 miles (0.8 km) of the apex of the buried, wedge-shaped, sandstone tableland suggests that both bedrock configuration and altitude were important factors in determining the location of the interlobate contact in the study area. Interpreta­ tion of both drift and landform characteristics indicate that surficial phenomena associated with the Saginaw Lobe in the Interlobate Morainic Tract are generally situated over higher bedrock areas. The converse is true for surficial phenomena associated with the Huron-Erie Lobe. Interlobate Morainic Tract The Interlobate Morainic Tract is a rectangular-shaped area about 5 miles (8.0 km) wide and 12 miles (20 km) long which trends northeast from Leverett Hill to Pinckney. m) at Stofer Hill (Figure 28). m). Maximum local relief is 180 feet (54.9 Mean local relief is about 115 feet (35.1 Associated with this relatively high local relief are numerous steep slopes believed to be of ice-contact origin. The Interlobate Morainic Tract is bounded on three sides by low altitude, low relief areas about 1 mile (1.6 km) wide which are underlain by sand and gravel (Figure 8 ). 135 The highest altitudes In the tract tend to be located along_a series of hills which trends north and includes Leverett Hill— feet (341.1 m ) , Riley Hill— 1,040 feet (317.0 m ) , Stofer Hill— feet (335.3 m) , Heatley H i l l ^ — Hill— 970 feet (295.7 m) the tract into two areas— 1,120 1,100 1,020 feet (310.9 m) , and Russell (Figures 32 and 34). These features separate a northwest zone which is slightly more than 1 mile (1.6 km) in width and a southeast zone which is 3 to 4 miles (4.8 to 6.4 km) wide. About 1 mile (1.6 km) to the west of these hills is a second line of hills which trends northeast. It marks a continuation of the northern zone of linear depressions of theu Kalamazoo Moraine into the Interlobate Morainic Tract as a series of hills which includes Hankard Hill 20 — 1,086 feet (331.0 m) , Shanahan Hill— m) , and Prospect Hill "A"— 1,050 feet (320.0 m ) . 1,040 feet (317.0 This linear series of features trends toward the northwest flank of Russell Hill. The steep slopes and existence of several gravel pits in these features indicate they are ice-contact in origin and are kames. In addition, this section also contains several groups of linear depressions 21 with northeast- southwest orientation that strongly resemble similar features in the northern zone of linear depressions in the Kalamazoo Moraine. A high-altitude, relatively flat, linear hill north of Pinckney (SW^s sec. 14 and SE^ sec. 15, T. 1 N. , R. 4 E.) is composed of sand and 19 A steep-sided hill in SE^s sec. 11, T. 1 S. , R. 3 E. which is unnamed on the Stockbridge quadrangle. This name is applied for identi­ fication purposes only and is not formally proposed as a geographic name. 20 A steep-sided hill in S W % sec. 21, T. 1 S., R. 3 E. which is unnamed on the Stockbridge quadrangle. This name is applied for identi­ fication purposes only and is not formally proposed as a geographic name. 21 These depressions are located at or near the surficial trace of the 900-foot (274.3 m) bedrock contour where it indicates the presence of outliers of the sandstone tableland. P NCKNEY PA TTER SO N L B R U IN B U N D L. PROSPECT H I L L 't f / a , v #/ & y j| SHANAHAN HILL HILL /T/' ^ HANKARD b RUSSELL H ILL / |CV HEATLEY f ' ^ HILL / * ST0FER t^b ✓ RILEY H ILL LEVERETTj£fVK h ill \ % N K « m SAND a GRAVEL RIDGE ICE-CONTACT SLOPE 3 0 - i 50 FT (9 -4 6 M ) HIGH ■= LINEAR ?! DRY DEPRESSIONS KALAMAZOO M O R A IN E PERCHED CHANNEL M IS S IS S IN E W A M O R A IN E OUTWASH FAN — — INTERLOBATE 1lr '76 Ml Figure 34. APPR O XIM ATE CONTACT SCALE KM Diagram of Interlobate Morainic Tract 137 gravel, has very steep flanks and a number of linear depressions on its margins (Figure 34). Similar features are located to the southwest in secs. 20 and 21, T. 1 N . , R. 4 E. and secs. 29 and 30, T. 1 N . , R. 4 E. All three of these flat-topped features are about 0.2 miles (0.3 km) wide, trend approximately northeast-southwest, and are located in the northwest portion of the Interlobate Morainic Tract. The linear depres­ sions on the margins of these channel fillings are oriented parallel to the long axis of the larger features and probably mark the former sites of narrow, stagnant ice masses that were buried by glaciofluvial sedi­ ments. There is a possibility that these channel fillings may all have been deposited by the same southwest-flowing superglacial stream for they form a 6 -mile (9.6 km) long, discontinuous, southwest-sloping sur­ face as much as 1,000 feet (305 m) wide which is bounded by ice-contact slopes. Crest altitude at the north end near Pinckney is 1,000 to 1,010 feet (304.8 to 307.8 m ) , and at Patterson Lake it is about 970 feet (295.7 m ) . Two similar features are located in sec. 19, T. I N . , R. 4 E. and secs. 24 and 25, T. 1 N . , R. 3 E. and may mark the location of tributaries to the trunk stream which flowed almost exactly along the interlobate contact. Groups of linear depressions are located in both the northwest and southeast portions of the Interlobate Morainic Tract. Those in the northwest have northeast-southwest orientations and are associated with the extension of the northern zone of linear depressions into the tract. Linear depressions are distributed throughout the southeast portion of the tract. Here intragroup orientations are generally parallel to one another, but intergroup orientations are generally dissimilar. These depressions are most probably due to the burial of fractured, stagnant 138 ice by glaciofluvial sediments. The intragroup similarities and inter­ group dissimilarities in depression orientations suggest that the frac­ tures may have been determined by local conditions in the ice sheet. On the other hand, the tendency for the depressions to have northeastsouthwest or northwest-southeast orientations (Figures 32 and 34) may indicate some sort of regional structural control in the ice sheet. In any case, the exact cause of this situation is not clear and does not seem to be related to the underlying bedrock. Four fan-shaped features on the northwest side of the Interlobate Morainic Tract and five more to the north near Pinckney have steep northern slopes and relatively smooth surfaces dipping more gently to the south. These sand-and-gravel features resemble small outwash fans in the Kalamazoo Moraine described previously. Only one similar feature is thought to exist in the southeast portion of the tract, and it is located only 0.25 miles (0.4 km) east of Leverett Hill in SW^SWlsSWls sec 27, T. 1 S., R. 3 E. 22 to the east. wash fans. Here the gentle slope is to the west and the steep slope These features are interpreted as small ice-contact out­ With the exception of the single fan east of Leverett Hill, all slope south and indicate a Saginaw Lobe source of meltwater. Numerous narrow linear ridges are located in the Interlobate Morainic Tract. These features are ordinarily quite straight and any changes in trend are angular. Because of this, their steep flanks, and the presence of large amounts of sand and gravel in them, they are 22 Three sewage lagoons are now situated on what was the gently sloping surface; however, the steep slope is still present as is a feed­ ing esker trending into it from the east. Its unmodified form is clearly visible on air photos XT-3DD-6, -7, - 8 (Agricultural Stabilization and Conservation Service, October 1, 1963) which were exposed before the lagoons were excavated. 139 interpreted as crevasse fillings. There seem to be significant differences in the distribution of landforms in the Interlobate Morainic Tract. For example, the landform assemblage which includes the large channel fillings, small outwash fans, and linear depressions with a consistent northeast-southwest trend is located in the northwest portion of the tract. Another assemblage in­ cluding larger crevasse fillings and the groups of depressions with large amounts of intergroup orientation variability is located in the southeast. A number of features are located in a narrow zone that separates the northwestern landform assemblage from the southeastern. A consideration of these features may help to explain the distributional characteristics of the two assemblages. Riley, Stofer, and Heatley Hills are located along this boundary zone and appear to be composed primarily of sand and gravel. Their steep slopes and linear forms suggest they are ice-contact accumulations of glaciofluvial materials which were probably deposited in openings enlarged by melting along fractured zones or surfaces in stagnant ice. Leverett Hill is situated at the southwest end of this line of hills, and Russell Hill is at the northeast end. similarities between these two features. glaciofluvial sediments. sides. There are a number of striking (1) Both are underlain by (2) Both have ice-contact flanks on three (3) Both slope to the southwest indicating that the meltwater streams which formed them also flowed in that direction. (4) The zone of linear depressions and ridges along the crest of the Kalamazoo Moraine may be traced into the northwest flank of Leverett Hill and the HankardShanahan-Prospect Hill "A" series of features, and the extension of the northern zone of linear depressions of the Kalamazoo Moraine may be traced to the northwest flank of Russell Hill. On the basis of form, sediments, and regional trends, it is clear that Leverett Hill is a large outwash fan which marks the contact of the Saginaw and Huron-Erie Lobes during a phase of the deglaciation sequence. It is also clear that the northwest flank of Russell Hill is associated with a marginal position of the Saginaw Lobe. Furthermore, if the trend of the Mississinewa Moraine is extended north from Leverett Hill, it intersects the northeastern flank of Russell Hill. Thus, the similari­ ties in form, sediments, and geomorphic relationships indicate that Russell Hill is also an outwash fan that marks the contact of the Sagi­ naw and Huron-Erie Lobes for a period of time during deglaciation and that it postdates Leverett Hill. If this is correct, it is likely that the Riley-Stofer-Heatley series of hills between these two interlobate outwash fans probably formed in association with a stagnant-ice zone along, or very near, the interlobate contact. 23 Both Leverett (notebook 274, pp. 71-72) and Kneller (1964, p. 32) came to essentially the same conclusion (Figure 10). On the basis of this evidence, it may be concluded that landform assemblages in the Interlobate Morainic Tract were formed under varied conditions as a consequence of their association with ice of different lobes. The northwest assemblage, including channel fillings, small outwash fans, and linear depressions with similar orientations, was deposited in contact with Saginaw Lobe ice. The southeast assemblage, including crevasse fillings and groups of linear depressions with dis­ similar orientations, was formed in Huron-Erie Lobe ice. It should be noted that the surficial drift contact, as defined by 7S/10& ratios, is also situated along this line. 141 Relationship of Bedrock Surface and Grass Lake Plain and Associated Areas In general, the Grass Lake Plain and associated areas are under­ lain by the buried sandstone tableland, which has altitudes of 900 to slightly more than 1,000 feet (274.3 to 304.8 m ) . The relatively low amounts of surficial relief on much of the Grass Lake Plain is probably due, at least in part, to the subdued relief of the bedrock surface be­ neath it. A primary factor in the formation of the Center Lake-Wolf Lake chain of lakes is the buried Norvell valley, which is incised 100 to 150 feet (30.5 to 45.7 m) into the sandstone and trends southeast b e ­ neath the area from Jackson past Norvell (Chapter 2). Grass Lake Plain and Associated Areas The Grass Lake Plain and associated areas form a southwesterly sloping surface with an altitude of 1,050 to 1,100 feet (320.0 to 335.3 m) on Leverett Hill to approximately 950 feet (289.6 m) south of Jackson (Figures 29 and 35). A low-lying tract with an altitude of about 960 feet (292.6 m) trends northwest past Norvell to Jackson and contains a series of lakes— the Center Lake-Wolf Lake chain. The plain merges with the Mississinewa Moraine on the east and southeast (Figure 32) at altitudes of about 980 to 1,020 feet (298.7 to 310.9 m ) , and to the north the Kalamazoo Moraine outwash apron merges with the plain at altitudes of about 1,020 to 1,030 feet (310.9 to 313.9 m). The plain slopes to the south from the Kalamazoo Moraine and west and north from the Mississinewa Moraine. The surficial sediments on these aprons and the margins of the plain are rather coarse with con­ siderable amounts of gravel including large cobbles. However, with increasing distance from the moraines the surficial sediments become 142 Kalamazoo Moraine PROSPECT HILL"B" Mississinewa Moraine SACKRIDER HILL l\ / . FRANCISCON E S K E R f^ / A CREVASSE FILLING /G ILLETTS L. E S K E R 9 GOOSE L.yf ESKER^/ ^ » N ,-T COPPERNOLL GRASS L. ESKERA ACKERSON L Q RIDGE "7W OLF L ^TUCKER L. ESKER STONY □ Norvell >> >> STONY LAKE PP " m CP \l KM MM MCL U r '76 Figure 35. ESKER P IT T E D OUTWASH OUTWASH FAN PLAIN SHALLOW LINEAR DEPRESSIONS ICE-CONTACT SLOPE 3 0 -1 0 0 F E E T (9 -3 0 M ) HIGH CONTACT OF OUTWASH SURFACES FROM SAGINAW a H U R O N -ER IE LOBES COLLAPSED OUTWASH PLAIN DRY PERCHED CHANNEL DRY CHANNEL miles kilometers approximate scale KALAMAZOO MORAINE MISSISSINEWA MORAINE M ILL CREEK LOWLAND Diagram of Grass Lake Plain and Associated Areas 143 finer until little gravel is present. This indicates that the Grass Lake Plain is an outwash plain associated with both the Kalamazoo and Mississinewa Moraines. The contact of the two outwash surfaces which slope away from the moraines is interpreted to mark.the boundary between surficial drift of the Saginaw and Huron-Erie Lobes. It is situated approximately along a line bearing southwest from Leverett Hill to the center of T. 3 S. , R. 2 E. and then westward, separating the N^g and Sh, T. 3 S., R. 1 E. (Figures 9 and 35). Local relief on the plain (Figure 28) is generally less than 50 feet (15.2 m ) , but near the Center Lake-Wolf Lake chain of lakes it is somewhat greater, partially due to the depth of the lakes. 24 A tract about 1 mile (1.6 km) wide immediately distal to the Kalamazoo Moraine has 50 to 100 feet (15.2 to 30.5 m) of relief and steep-sided depressions which may be as large as a survey section. A similar zone is present distal to the Mississinewa Moraine, especially in the south near Norvell. This tract with numerous deep depressions on the outer margins of the plain shows abundant evidence of stagnant ice. Several crevasse fillings and eskers trend across the tract and will be discussed in detail below. Boulders are present in some of the depressions (Leverett notebook 32, p. 19) but are absent on the higher outwash surfaces. Till is visible in an exposure at the bottom of one of the depressions (NW^NEJsSW^ sec. 22, T. 2 S . , R. 2 E.). In addition, topographic profiles show that the higher outwash marks the remnants of a surface which slopes gently from the moraines. On the basis of this evidence, the marginal tract is According to the hydrographic map, Wolf Lake is as much as 45 feet (13.7 m) deep. JSPTT'-''--' ' 144 is interpreted as a pitted outwash plain. 25 Leverett Hill is a southwest-sloping sand-and-gravel feature approximately 2.5 miles (4.0 km) long, about 0.5 miles (0.8 km) wide, and more than 150 feet (45.7 m) high in places. It is situated in the narrow reentrant between the Kalamazoo and Mississinewa Moraines and has very steep slopes on its northwest, northeast, and southeast flanks. Leverett Hill is the highest point on the Grass Lake Plain, and its steep flanks indicate that it is an ice-contact feature (Figure 35). The southwest slope, sediments, and location at the northeast terminus of the Kalamazoo Moraine and the north end of the Mississinewa Moraine show that it is a large outwash fan deposited by meltwater in a former reentrant between the Saginaw and Huron-Erie Lobes. The meltwater which deposited it flowed to the southwest and onto the lower portion of the Grass Lake Plain. Several straight, steep-sided sand-and-gravel ridges at the west end of Goose Lake "A" are interpreted as crevasse fillings which were deposited in association with stagnant ice that existed on the distal side of the Kalamazoo Moraine. A nearby ridge trends south from sec. 26, T. 2 S . , R. 1 E. to Sec. 10, T. 3 S . , R. 1 E. This discontinuous feature, here named the Gilletts Lake Esker, has some of the character­ istics of a crevasse filling, but its somewhat sinuous nature and length indicate that it probably is an esker. The Grass Lake Esker (Keifenheim, 1974, p. 22), extended in this study, trends south near the town of Grass Lake. Air photos and hydrographic maps indicate that segments of the esker are also present on the bottoms of Grass and Tims. Lakes. See discussion in Thwaites, 1926, for a discussion of such features. P F T ■■■■■■ 145 Leverett (notebook 166, p. 63) examined an exposure in the ridge which revealed dipping beds that provide evidence that the esker stream flowed to the south. Another esker, here named the Francisco Esker, trends south along the Jackson-Washtenaw boundary at the distal margin of the Mississinewa Moraine. The Gilletts Lake, Grass Lake, and Francisco Eskers all originate distal to large outwash fans on the crests of the 26 Kalamazoo Moraine. It appears that superglacial streams deposited the outwash fans but that the continuation of the drainage became subglacial. The result was a number of streams that formed the eskers flowing south beneath stagnant ice. The deposition of the sediments was probably contemporaneous with the deposition of outwash on the upper surface of the stagnant ice. A fourth esker, here named the Coppernoll Esker, is rather short (secs. 3, 10, and 16, T. 3 S . , R. 2 E.) and does not appear to originate near the Kalamazoo Moraine. 27 The three easternmost eskers are all tributaries to the Blue Ridge Esker and tend to parallel that feature a short distance before merging with it. All the eskers associ­ ated with the Kalamazoo Moraine have adjacent low-lying tracts which are interpreted as esker troughs. The Goose Lake and Tucker Lake Eskers associated with the Mississinewa Moraine (pp. 131, 133) cannot be traced to a merger with the Blue Ridge, but their trends and proximity strongly suggest that they did supply meltwater and sediments to that feature. third esker associated with the Huron-Erie Lobe, the Stony Lake Esker ^ P r o s p e c t Hill "B," Sackrider Hill, and a large hill near Brill Lake. 27 Although portions of all these eskers are easily recognized in the field and on topographic maps, other parts are apparent only with close stereoscopic inspection of air photos. This may be due to more complete burial during superimposition of the superglacial outwash. A 146 (Keifenheim, 1974, p. 31), extended in this study, is physically connec­ ted with the Blue Ridge Esker (SE^NW^SW^z; sec. 6 , T. 4 S., R. I E . ) . This contact indicates that both features were deposited at the same time. Small depressions are present locally on the low-relief, central portion of the plain; and even on the flattest area (N*s, T. 3 S., R. 2 E.) groups of very shallow, parallel, linear depressions trending northwestsoutheast and northeast-southwest 35). are visible on air photos (Figure These patterns have little resemblance to erosional features and appear to have been caused by the deposition of outwash on stagnant, fractured ice. At least three eskers and associated troughs trend across the plain. wash It is apparent that the eskers were not formed prior to the out­ plain because the troughs would then have subsequently filled with outwash and would no longer be visible. associated troughs were formed and the outwash laid down on top Apparently the eskers and beneath a of the ice. thin sheet of stagnant ice Subsequent ablation of the stagnant ice resulted in the superimposition of the outwash upon the underlying materials. Thus, cn the basis of (1) the groups of linear depressions and (2 ) the presence of eskers and associated troughs, the low-relief portion of the Grass Lake Plain is interpreted as a collapsed outwash plain. Considering the plain, Leverett (Leverett and Taylor, 1915, p. 197) also concluded that "only a small portion of its surface is up to the plane of deposition." The sand-and-gravel ridges in the Mill Creek lowland (p. 132) ex­ tend southwest along the north side of Willow Creek as a series of short segments spaced at intervals of 1,000 feet (305 m) or more. West of sec. 11, T. 3 S . , R. 2 E. the ridge segments are wider and higher, may 147 be more than 0.5 miles (0.8 km) long, and are separated by only small gaps. The hydrographic map for Wolf Lake indicates that ridge segments are also present below the surface of the water. Immediately west of the lake a segment of the ridge is almost 0.5 miles has very steep slopes. (0.8 km) wide and It is not well defined in sec. 28, T. 3 S., R. 1 28 E., but from sec. 29, T. 3 S . , R. 1 E. it extends southwest as a con­ spicuous, steep-sided ridge more than 50 feet (15.2 m) high and is labeled "Blue Ridge" on topographic maps. Crest altitude near the Mill Creek lowland is about 1,000 feet (304.8 m ) , and at the southwest it is well over 1,050 feet (320.0 m ) . Blue Ridge is an esker which was deposited by a stream flowing west and southwest. 29 It may be considered the trunk esker in the area and received sediments and meltwater from at least four, and probably all seven, of the eskers shown on Figure 35. On the basis of pebble and cobble lithology, Keifenheim (1972, p. 42) concluded that the esker sediments are more closely associated with the Saginaw, rather than the Huron-Erie, Lobe. The lithology of 564 boulders in gravel pits along the esker was determined during this in­ vestigation and was found to be quite different than data on pebble lithology because 80% of the boulders and only 13% of the pebbles were 28 The 1930 soil survey indicates a narrow band of Bellefontaine sandy loam (sand and gravel parent material) in this section along the extension of the ridge. A gravel pit in this band (site 216— NE^SEisNE^ sec. 28, T. 3 S . , R. 1 E.) confirms the presence of sand and gravel. 29 In his monograph with Taylor (1915, p. 203) Leverett originally applied the name "Ackerson Esker" to this feature, but it is now commonly referred to as the "Blue Ridge Esker." He mapped it as far east as the west end of Wolf Lake. Later workers (Rieck, 1972, and Keifenheim, 1974) have mapped it extending 3 miles (4.8 km) east of the lake. As inter­ preted in this investigation, it originates in the Mill Creek lowland in SE% sec. 6 , T. 3 S., R. 3 E., 7 miles (11.2 km) east of the lake. 148 sandstone (Appendix E ) . Most of the sandstone resembled well-record descriptions of the local sandstone. 30 On the basis of morphology of the Grass Lake Plain and 7 8 /loX ratios of clays from near the esker (Figure 26), it seems likely that the section of the Blue Ridge Esker from west of the meridian of Norvell to Ackerson Lake formed very near the interlobate contact but in ice of the Huron-Erie Lobe. eskers" from Finland. There are numerous reports 31 on "interlobate However, the lobes between which these eskers formed were small, only 10 to 15 miles (16 to 24 km) wide or less and protruded just a short distance from the margin of the Scandinavian ice sheet. Buddington and Leonard (1962, p. 15) mapped an esker in the Adirondacks which was deposited between lobes which were somewhat larger. Wilson (1939, p. 124) and Stoelting (1970) described interlobate eskers which formed between major lobes in Canada and Wisconsin, respec­ tively, but reported none which had tributary eskers from both lobes merging with the trunk, interlobate, esker. Thus, the Blue Ridge seems to be a rather unusual esker because it was formed in close proximity to a significant interlobate contact and has connecting tributary eskers associated with both lobes. This indicates that stagnant ice from the Saginaw and Huron-Erie Lobes was present over a large portion of the Grass Lake Plain during deglaciation. Features Located in More Than One Physiographic Section Two distinct types of landforms are located in several portions of the study area. 30 31 One is a linear sand-and-gravel feature, often See also Dorr and Eschman, 1971, p. 156. Some of these include Repo, 1960, pp. 12-13; Aartolahti, 1972, p. 62; and Okko, 1962, p. 39. 149 flat-topped, with steep flanks and a dry channel or notch transverse to its long axis (Table 8 ). tely, others have not. 32 Some of the ridges have been breached compleExamples of these features are found in the Kalamazoo Moraine, Interlobate Tract, and the Grass Lake Plain. Due to their sediments and steep flanks, the breached and notched ridges pro­ bably represent crevasse or channel fillings with postdepositional glaciofluvial erosion. After the ridges were deposited and a portion of the adjacent stagnant ice had melted, superglacial streams probably flowed across the features, eroding some of the sediments. The depth of the eroded channels was determined by the length of time that the streams flowed in those locations. If the superglacial environment was rela­ tively stable, the streams may have flowed long enough to completely breach the ridge; if not, only a notch was eroded. The second type of landform is a high, relatively flat, sand-andgravel feature with steep flanks, which may have any shape from almost circular to irregular. to another. A dry channel may trend across it from one side This channel ends abruptly at an ice-contact slope and is not graded to the surrounding lowland. Such features are located on the Grass Lake Plain and in the Interlobate Morainic Tract. A variation is a high, flat feature with a dry depression on top and an associated dry channel which trends across the flat area toward lower ground. These features are also located in the Interlobate Morainic Tract and on the Grass Lake Plain. Genesis of the flat-topped features and their channels was probably similar to that of the breached and notched ridges except that deposition evidently 32 ridges. took place in some sort of perforation in the They resemble wind and water gaps which are found in bedrock 150 Table 8 . Locations of Landforms Situated in More Than One Morphologic Area Breached and Notched Ridges T. R. Morphologic Area 29 IN 4E Interlobate Morainic Tract 35 IS 2E Kalamazoo Moraine 10 IS 4E Interlobate Morainic Tract 9 IS 4E Interlobate Morainic Tract 16 IS 4E Interlobate Morainic Tract 16 2S IE Kalamazoo Moraine 27 2S IE Kalamazoo Moraine 33 2S IE Grass Lake Plain 3 2S 2E Kalamazoo Moraine Section Channeled Plateaus— Lacking Depressions 31 IN 4E Interlobate Morainic Tract 33 IN 4E Interlobate Morainic Tract 4 3S IE Channeled Plateaus— 24 IS Grass Lake Plain With Depressions 3E Interlobate Morainic Tract 19 & 30 IS 4E Interlobate Morainic Tract 28 2E 3S Grass Lake Plain ■ 151 ice rather than in a crevasse. The origin of the channels associated with the depressions is not as obvious. Perhaps the depressions mark the former locations of ice blocks which protruded above the sediments and the channels may have been eroded by the meltwater from the ice blocks. However, the depth of the channels, 20 feet (6.1 m) or more, seems to preclude this. There is a possibility that the depressions are the former locations of springs and mark the point of escape of sub­ glacial meltwater under hydrostatic pressure. The presence of the breached ridges and channeled plateaus in the Kalamazoo Moraine, in the Interlobate Morainic Tract, and on the pitted portion of the Grass Lake Plain indicates that large amounts of stagnant ice were present in these areas for a sufficient time to permit glacio­ fluvial erosion to take place after deposition of the sediments. The lack of such features in the Mississinewa Moraine indicates that stagnant ice was not as prevalent or did not remain for as long a time as in the other areas. Chapter 5 DEGLACIATION OF THE STUDY AREA Morphologic Factors Influencing Deglaciation The final deglaciation of southeastern Michigan is significantly associated with the characteristics of the underlying bedrock. face basins now occupied by Lakes Erie and Huron served as the axes flow for the Huron-Erie Lobe during late Wisconsinan time. The sur­ of Also, during the process of deglaciation active ice remained in these lower areas after the nearby higher tracts had been deglaciated. The "Thumb" of Michigan is underlain by bedrock with a surface of sufficiently high altitude to present an obstacle to the movement of glacial ice and de­ flect a portion of the Huron Lobe into the Saginaw Lowland, forming Saginaw Lobe (Figure 1) (Horberg, 1956, p. 105). the The former contact be­ tween the Saginaw and Huron-Erie Lobes is marked by an interlobate drift contact that is believed to be located approximately above this bedrock high of regional extent. The correspondence of the higher bedrock sur­ face and the drift contact of the different lobes indicates (1) that the surface configuration of the bedrock served to separate the ice into two lobes and (2) that its high altitude resulted in a comparatively thinner cover of overlying ice and consequently early deglaciation. Bedrock altitude influenced both the regional patterns of ice flow and the local deglaciation of the study area. The highest bedrock sur­ face in the area is associated with a buried sandstone tableland located along the southwest extension of the bedrock high in the Thumb. Evidence indicates that ice above the sandstone tableland thinned and eventually stagnated. At the same time the ice in nearby areas probably remained 152 153 active because of lower altitude of the subglacial surface and greater thickness of the glacier. Shearing of the active glaciers over the stagnant ice resulted in the deposition of sediments such as basal till, meltout till, flow till, and glaciofluvial materials in the areas where the Kalamazoo and Mississinewa Moraines and the Grass Lake Plain were in the process of formation. Possible Changes in the Position of the Interlobate Contact Through Time The exact positions of the margins of the Saginaw and Huron-Erie Lobes prior to the final deglaciation of the study area are not known. On the basis of previous works and findings in this study, it is not clear whether the interlobate contact always trended across the study area or was located elsewhere. Study of interlobate areas in Wisconsin (Black, 1969, p. 105) and Ontario (Westgate and Dreimanis, 1967, p. 1143) indicates that the loca­ tion of interlobate contacts may shift somewhat with time prior to de­ glaciation. Zumberge (1960, pp. 1182'83) and Wayne and Zumberge (1965, p. 72) state that clay-rich Huron-Erie till is stratigraphically above sandy till of the Saginaw Lobe in Lenawee County, Michigan, just a few miles (km) south of the study area. If this interpretation is correct,'*' it indicates that the Huron-Erie Lobe advanced into an area formerly covered by the Saginaw Lobe. Although indicating that his evidence "is not compelling," Kneller (1964, pp. 25-26, 35-36) interpreted many ■^The textures of both Saginaw and Huron-Erie Lobe tills in the study area tend to be rather variable (Figure 11), and identifying the lobe provenance of a till strictly on the basis of texture may not necessarily yield reliable results. Therefore, the possibility exists that the sediments described by Zumberge and Wayne may only represent coarse and fine facies of Huron-Erie Lobe till. gravel deposits in Washtenaw County, as far east as the Fort Wayne Mo­ raine, as exhibiting Saginaw Lobe pebble lithology and to be overlain by Huron-Erie Lobe till. As a test of this interpretation, samples of till and underlying outwash were obtained from two such sites (234— 2 S., R. 4 E.jand 146— SW^SW^SWls sec. 12, SW^SE^SW^s sec. 19, T. T. 3 S. , R. 3 E. ; Kneller's sites 22 and 18, respectively) and studied by X-ray diffraction. Clay­ sized particles from the till and outwash at site 234 produced 7X/10X peak height ratios of 0.79 and 0.84, respectively, indicating a HuronErie Lobe provenance for both sediments. Conversely, pebble-count data from the site "strongly suggests" (Kneller, 1964, Table 1) that the out­ wash deposit is of Saginaw provenance. The till and subjacent outwash at site 146 yielded 7 X/I 0 S ratios of 0.53 and 0.59, respectively, also clearly indicative of Huron-Erie Lobe provenance. Interpretation of the pebble lithology of this deposit is inconclusive and does not permit assigning a lobe provenance to the outwash (Kneller, 1964, Table 1). A third site (143— NWJjNW^NWis sec. 22, T. 3 S. , R. 3 E.) with till strati- graphically above outwash, and not studied by Kneller, produced 7&./10& ratios of 0.90 and 1.00, respectively. This suggests that the sediments are Huron-Erie till over Saginaw Lobe outwash. Thus, 78 ./IOX ratios at this site seem to indicate that the margins of the Saginaw and HuronErie Lobes were, for a time, located farther to the east near the Fort Wayne Moraine, possibly as shown on Figure 36. Peak height ratios at the other two sites support the interpretation that the margins were located as shown on Figure 37. Further investigation is needed to solve this problem and to determine whether the Saginaw and Huron-Erie margins changed position significantly before the ice along the final KM KM • MM —. LOBE M A R G IN MORAINE MM MISSIS SINE WA MORAINE FWM FT. KM K A L A M A Z O O 0 5 l= = = s a J mi Figure 36. — APPROXIMATE WAYNE M O R A IN E MORAINE BOUNDARY SCALE 9 19 I km I Possible Location of Saginaw and Huron-Erie Lobe Margins Prior to Cessation of Flow *6 ^ KM I KM KM MM LOBE MARGIN K A L A M A Z O O MORAINE M IS SI SS IN E W A 0 5 mi Figure 37. -- FWM ----- FT. WAYNE MOR AINE M O R A I N E BO UN DA RY M OR AI NE ? 0 APPROXIMATE SCALE 1 1 km "^ Km Location of Saginaw and Huron-Erie Lobe Margins at Cessation of Flow 156 interlobate contact stagnated and ablated. 2 Phases of Deglaciation The final events in the deglaciation of the study area took place in several phases beginning with the deglaciation of the terrain overlying the sandstone tableland. Subsequently the events moved north and east with the retreat of the margins of the Saginaw and Huron-Erie Lobes. The deglaciation process may be divided into five phases: IA. Formation of the Grass Lake Plain IB. Formation of the distal flanks of the moraines 2. Formation of the proximal flanks of the moraines 3. Retreat of the margins from the moraines 4. Completion of the deglaciation process 5. Postglacial modification of the landscape Phase 1A— 3 Formation of the Grass Lake Plain Topographic profiles show that the crest elevations of the higher hills on the Grass Lake Plain are successively lower to the south from the crest of the Kalamazoo Moraine and to the west and northwest from the Mississinewa Moraine. On this basis the hills are interpreted to represent remnants of a former surface of glaciofluvial deposition asso­ ciated with the two moraines (Figure 38). In addition, the average grain size of sediments associated with the plain tends to decrease with 2 Although the spatial relationships of the two lobes are not clear during this prelude to deglaciation, their relative positions can be delimited with much more confidence during several of the succeeding events. 3 Phases 1A and IB were essentially contemporaneous and are pre­ sented separately to simplify the description of the deglaciation sequence. 157 LEVERETT HI LL KM MM / I •' SOWP MM , _ / KM MM ±1 ------ KALAMAZOO M ORAINE M ISSISSINEW A MORAINE MORAINE B O U N D A R Y LO BE MARGIN O UTWASH A P R O N OUTWASH FAN LARGE SUPERGLACIAL MELTWATER STREAM • SOWP CREVASSES P E R F O R A T I O N IN ICE A L LO W IN G FORMATION OF A KAME S U P E R G LA C IA L PLAIN OUTWASH E S K E R S F O R M IN G S T A G N A N T ICE BRE S M A L L E R SUPERGLACIAL M ELTW ATER STREAM BLUE N RIDGE 0 fc= mi BENEATH ESKER 5 =l 10 km Figure 38. Phases 1A and IB =1 158 distance from the moraines. Both of these lines of evidence Indicate that the Grass Lake Plain is a complex outwash plain formed concomitantly with the Kalamazoo and Mississinewa Moraines. Evidence that masses of stagnant ice existed in the Grass Lake Plain area at the time the sediments were deposited is widespread and is illustrated by the following: 1. The Wolf Lake-Center Lake chain of lakes indicates that stagnant ice was associated with the Norvell bedrock valley. 2. Numerous depressions are present on the periphery of the Grass Lake Plain. 3. Ice-contact features such as breached and notched ridges and chan­ neled plateaus exist within the plain. 4. Shallow linear depressions exist even on the flattest portions of the plain, indicating that sand and gravel was deposited in contact with stagnant i c e . 5. Perhaps the strongest evidence for the existence of widespread stag­ nant ice is the presence of the Blue Ridge Esker and associated tributary eskers which form a dendritic pattern trending across the entire plain. 4 The areal pattern and the interrelated nature of the eskers indicate the presence of an integrated drainage system in and beneath stagnant ice of both the Saginaw and Huron-Erie L o b e s . The relationship of eskers and associated esker troughs to the Grass Lake Plain also indicates that it is not simply an outwash plain deposited in an area containing previously formed eskers. If such were the case, the esker troughs would have been filled by the subsequent 4 It is generally conceded that most eskers form in contact with stagnant, not active, ice (Embleton and King, 1968, p. 389). glaciofluvial deposition which formed the plain. Instead, the troughs, and other evidence for glacial stagnation discussed previously, indicate that glaciofluvial sediments from the moraines were deposited on a thin sheet of stagnant ice^ penecontemporaneously with the formation of the Blue Ridge Esker and its. tributary segments (Figures 38 and 39) . Sub­ sequent ablation of the ice superimposed the superglacial sediments onto the subjacent material and eskers, preserving the subglacial forms even thoughcovering them with a veneer of sediments (Figure 40). The abla­ tion of the ice and lowering of the superglacial sediments onto the sub­ jacent material also formed the Grass Lake Plain, which is probably best described as a collapsed outwash plain. Phase IB— Formation of the Distal Flanks Medial Portions of the Moraines and Leverett Hill and Contemporaneously with the formation of the superglacial outwash plain, numerous superglacial meltwater streams deposited the outwash apron of the Kalamazoo Moraine. In addition, several large superglacial meltwater streams formed the outwash fans which are built up above the general level of the apron (Figures 31 and 38). These larger streams then drained southward within and beneath the stagnant ice of the Grass Lake Plain and were associated with the formation of the Gilletts Lake, Grass Lake, and Francisco Eskers. Their configuration shows that each of these streams joined the trunk esker stream which formed the Blue Ridge Esker. The close association of the outwash fans and the eskers, and the location of the fans on the outwash apron, which in turn grades into the Grass Lake Plain, indicate that all of the features formed at ^Relations of the eskers and features in the moraines (discussed in Phase IB) indicate that the subglacial drainage which deposited the eskers was probably flowing at the same time the superglacial outwash plain was being deposited. SUPERGLACIAL OUTWASH PLAIN S T A GN A N T ESKER ESKER TROUGH BEDDED SAND ESKER GRAVEL SUBJACENT Figure 39. STREAM MATERIAL Simultaneous Formation of Superglacial Outwash Plain and Esker ESKER ESKER TROUGH COLLAPSED SU PE R G LA C IA L S E D IM E N TS BEDDED SAND GRAVEL SUBJACENT Figure 40. M A T E R IA L Site of Figure 39 After Deglaciation 161 approximately the same time. Simultaneously, fractures in the ice parallel to and near the Saginaw Lobe margin were enlarged, and glaciofluvial sediments were de­ posited within them. With deglaciation these crevasse fillings became ridges, and the adjacent masses of ice melted to form a zone of linear depressions and ridges proximal to the crest of the Kalamazoo Moraine. At this time a large tract of stagnant ice was situated to the north in an area that was to become the zone of lakes and bogs in the medial portion of the moraine. Glaciofluvial sediments deposited in scattered perforations in the ice eventually formed kames. Lakes and bogs mark the former location of larger ice masses which persisted long enough to prevent significant amounts of deposition. Along the contact between active and stagnant ice, probably located a short distance to the north, shearing of ice resulted in the formation of englacial debris bands. Subsequent ablation of the ice matrix permitted water-saturated meltout till to move downslope as flow till, which was then deposited on the kames after glaciofluvial deposition had slowed or ceased. Subaerial glaciofluvial processes were also important along the margin of the Huron-Erie Lobe, resulting in the deposition of large amounts of sand and gravel in contact with stagnant ice. In addition, subglacial streams deposited the Goose Lake, Tucker Lake, and Stony Lake tributary eskers and the Blue Ridge trunk esker. The upstream portion of the Blue Ridge Esker was probably formed at this time by subglacial meltwater flowing west out of the Mill Creek lowland. The intricate association of all the eskers with features in both the Kalamazoo and Mississinewa Moraines and the association of the outwash plain with the moraines clearly show that this assemblage of features was formed at : 162 about the same time and reflects different aspects of the subglacial and superglacial drainage systems of the two glaciers. The location of Leverett Hill at a reentrant site between the two lobes, its gradual slope to the southwest, and the steep ice-contact slopes on its northwest and southeast flanks indicate that the meltwater and sediments which formed it were supplied by both lobes. This is apparent because the continuous ice-contact slope near the crest of the Kalamazoo Moraine merges with a similar slope on the northwest flank of Leverett Hill. Also, the ice-contact slope on the southeast flank of Leverett Hill merges with the ice-contact slopes along the distal flank of the Mississinewa Moraine, proving those portions of the two moraines to be truly time-correlative.^ There is also evidence that a tract of stagnant ice was situated along the interlobate contact to the northeast of Leverett Hill and perforations in it were filled with glaciofluvial materials. When ex­ posed by ablation, these features resulted in kame-like forms now known as Riley, Stofer, and Heatley Hills. Phase 2— Formation of the Proximal Flanks of the Moraines and Russell Hill The northern zone of linear depressions in the Kalamazoo Moraine, Hankard and Shanahan Hills, Prospect Hill "A," and several sets of linear depressions in the Interlobate Morainic Tract form a zone which is aligned with, and in proximity to, the northwest flank of Russell Hill (Figure 41). If the crest of the Mississinewa Moraine is extended north into the Interlobate Morainic Tract, it is in line with the ^Farrand and Eschman (1974, p. 38) state that the Mississinewa and Kalamazoo Moraines were formed about 14,800 years ago. 163 LEVERETT * f H ILL • KM MM KM GRASS LAKE MM PLAIN KM KALAMAZOO MM — M ISSISSINEW A L O B E MA RG IN ■=-.... CREVASSES IN T E R L O B A T E MORAINIC TRACT BOUNDARY «*- M ORAINE MORAINE L A RG E S U P E R G L A C I A L MELTWATER STREAM * • KAME P E R F O R A T I O N IN ICE A L L O W IN G F O R M A T I O N OF A K A M E FRACTURE IN I C E ALLOWING FORMATION OF CHANNEL F IL L IN G - SMALLER SU PER G LA C IA L MELTWATER STREAM 0 5 b=======d ml 0 I, 10 - 1 ■ km Hr 76 Figure 41. Phase 2 I 164 northeast flank of Russell Hill. These spatial and morphologic rela­ tions, X-ray diffraction data on clay-sized particles, associated sedi­ ment type, southwest slope, and ice-contact flanks of Russell Hill closely resemble those of Leverett Hill and indicate a similar genesis for the two features. Thus, it is reasonable to conclude that Russell Hill was formed by meltwater deposition at a location between stagnant masses of ice associated with the Saginaw and Huron-Erie Lobes. Upstream from this reentrant sediment-laden meltwater flowed on stagnant ice in the zone of the interlobate contact, enlarging fractures and depositing the sediments that now form the chain of large channel fillings located between Pinckney and Russell Hill. 7 The two different landform assemblages in the Interlobate Tract— channel fillings and outwash fans in the Saginaw Lobe portion and cre­ vasse fillings and intragroup variability of linear depression orienta­ tion in the Huron-Erie portion— indicate that conditions were somewhat different on either side of the interlobate contact. However, conditions were not entirely dissimilar because both portions of the Interlobate Morainic Tract have (1) ice-contact glaciolacustrine sediments, (2) large amounts of ice-contact glaciofluvial sediments and (3) an abundance of ice-contact slopes, indicating the existence of a stagnant-ice environ­ ment. The dry perched channels and breached ridges in the area clearly indicate that stagnant ice supported superglacial streams capable of erosion after deposition of the sediments. 7 The corresponding landforms associated with Leverett Hill are kamelike, are considerably smaller, and include Riley, Stofer, and Heatley Hills. 165 Phase 3— Retreat of the Margins from the Moraines g During this phase of the deglaciation sequence, the outermost ice of the Saginaw Lobe was stagnant in the western portion of the study area but active in the east (Figure 42). West of Brill Lake numerous ice-contact slopes, an ice—contact feature comprised primarily of flow till, and an outwash fan appear to be indicative of deposition in associ­ ation with stagnant ice. East of Brill Lake, on the Portage River low­ land, a linear series of hills with large amounts of surficial till and a general lack of ice-contact slopes were probably formed by an active Saginaw Lobe margin. A somewhat similar situation may have existed in the Huron-Erie Lobe. The linear depressions and ridges in the Sharon Short Hills indi­ cate deposition in crevassed, stagnant ice. A bouldery tract trends 9 northeast-southwest across Tps. 2 and 3 S., R. 4 E . , and if extended, this tract intersects the Sharon Short Hills, which have a similar north­ east-southwest trend. Several hills and meltwater channels are also associated with the bouldery tract. Thus the margin of the Huron-Erie Lobe may have been stagnant near the Sharon Short Hills but active to the northeast. Russell and Leverett (1908, p. 6 ) made a somewhat °The contact between the Saginaw and Huron-Erie Lobes was not located in the study area in this phase and does not seem to be marked by converging, contiguous morphologic features (see Russell and Leverett, 1908, and Leverett notebook 188, p. 33). For this reason it is not pos­ sible to state with certainty whether the landforms associated with the two ice margins described below were deposited at exactly the same time. 9 Russell and Leverett (1908) also map this tract continuing north along the west bank of the Huron River to a point 3 miles (4.8 km) north­ west of Dexter. Although a search was made for boulders in this area, few were found. E. ^ T h e Lima Esker trends southeast-northwest across T. 2 S. , R. 4 Its orientation indicates former ice flow most probably to have been 166 V' KM MM f/ \ / \ LIMA ESKER V KM /? I GRASS LAKE PLAIN KM KALAMAZOO MORAINE MM MISSISSINEWA MORAINE SSH SHARON SHORT HILLS LOBE MARGIN « MORAINIC HILL “ CREVASSE • BOULDERS /// Z O N E OF STAGNANT ICE — MELTWATER CHANNELS 0 5 L—-___________- i mi 0 t Figure 42. Phase 3 10 — km « 167 similar interpretation and stated that the bouldery tract may mark a "brief halt" in the retreat of an active margin of the Huron-Erie Lobe. Phase 4— Completion of the Deglaciation Process There is evidence for at least two marginal positions of the Sagi­ naw Lobe in the area to the north of the Kalamazoo Moraine (Figure 43). Study of topographic maps and air photos, as well as field reconnais­ sance, indicates the presence of linear tracts of higher-relief topogra­ phy, which may be interpreted to be morainic in o r i g i n . ^ If this inter­ pretation is correct, it indicates that the margin of an active glacier may not have continuously retreated to a position marked by the Charlotte Moraine (the next Saginaw Lobe moraine to the north) but may have halted temporarily at least twice or even readvanced. Eskers, which are evi­ dence of stagnant ice, also exist in the area. This indicates that •* marginal stagnation took place after deposition of both the bouldery, undulating tracts and that the eskers were then formed in the stagnant ice masses. The exact position of the Huron-Erie Lobe margin during this phase is not known. With the exception of the bouldery tract near the Lima Esker described previously, there is little evidence of ice-marginal deposition in the territory between the Mississinewa Moraine and the adjacent moraine to the east (the Fort Wayne Moraine). southeast-northwest, but it also indicates the former presence of stag­ nant ice distal to the bouldery tract. It may be that a mass of stagnant ice was present from the proximal side of the Mississinewa Moraine to the bouldery tract which was deposited by an active ice margin. Retreat of this active margin with little stagnation probably took place until the position of the Fort Wayne Moraine was reached. ■^Leverett (notebooks 31, p. 84; 160, p. 98; 275, pp. 89,93) made a similar interpretation and also recorded the presence of numerous boulders in these tracts. SAGINAW LOBE ST O C K B R I D G E * KM MM KM MM KM MM — KALAMAZOO MORAINE M IS SISSINE W A MORAINE LOBE MARGIN < ESKER — LIN E OF DRAINAGE 00 M O R A I N I C H I L L S N 5 0 h- =d ml o 1= 10 =d km Figure 43. Phase 4 169 The ablation of buried ice took place during all of the four phases of deglaciation. It is known that the ablation rate of buried ice may be quite slow (Embleton and King, 1968, p. 394, and Flint, 1971, p. 213). Blind, Halfmoon, and South Lakes in the Interlobate Morainic Tract are all more than 80 feet (24.4 m) deep. If the masses of ice which melted to form these and other depressions were buried beneath drift, the abla­ tion process may have required a considerable time span before the melt­ ing of all the glacial ice was complete. Until all this buried ice melted, the glacial landscape was still in the process of formation, even though the margins of the glaciers may have retreated significant distances and were no longer altering the topography or directly deposit­ ing material in the area. As the margins of the Saginaw and Huron-Erie Lobes reached the positions now marked by the Charlotte and Fort Wayne Moraines, meltwater continued to drain through certain parts of the study area. Drainage from the interlobate contact, located to the northeast, flowed southwest along the present course of the Huron River and then west along the channel at Pinckney and the Portage River lowland to the Grand River. Meltwater from the Charlotte Moraine flowed south before merging with this line of drainage. Large amounts of meltwater which drained, in part, northwest along the lowland between Norvell and Jackson were associated with the deposition of surficial materials on the Fort Wayne Moraine. In addition, with final deglaciation and the removal of certain ice barriers, the direction of flow of several rivers, such as the Grand and Raisin, was reversed, and they began draining in the directions pre­ vailing today. 170 Phase 5— Modification of the Landscape Since Deglaciation Postglacial modification of the landscape since deglaciation has been relatively minor. The numerous lakes and swamps indicate that in­ tegration of drainage is not well developed. Entrenchment along the major streams of the area is generally limited to 30 feet (9.1 m) or less and may be partially the result of glaciofluvial erosion. Marl has formed in some of the lakes (Russell and Leverett, 1908, p. 13), and organic matter in the form of muck and peat has partially filled some of the poorly drained depressions. has Leaching of carbonates in the drift lowered the surface altitude a few feet (1 m) but it certainly has not significantly affected the landforms. Slope modification appears to have been minimal, and most ice-contact slopes are well defined and at, or near, the angle of repose. Chapter 6 CONCLUSIONS AND IMPLICATIONS This dissertation has four major objectives, set forth in Chapter 1. The conclusions of this investigation are presented below as they relate to these objectives. The first objective (p. 1) is "To determine what relationship, if any, exists between the nature of the bedrock surface beneath the drift and the glacial landforms of the study area." Findings of this study indicate that the character of the bedrock surface has had a significant effect on the glaciation of the area. The remarkable correspondence in shape and location of the moraines, even in certain details, with the north and east sides of the buried sandstone tableland is an illustration of the influence the bedrock surface has had on the larger geomorphic features of the area. The location, shape, and trend of certain streams and lakes above deeply buried bedrock valleys show that the bedrock surface has also influenced some of the smaller components of the exist­ ing topography to a considerable degree. It seems quite likely that in some locations masses of ice were buried within the confines of the bedrock valleys and later melted to influence the hydrography of the area. Apparently buried ice also protected organic matter and subaerially oxidized drift located in the lowest portions of the landscape which ex­ isted prior to the latest glaciation of the area. Therefore, not only did the configuration of the bedrock surface serve to influence the location of the two moraines and several hydrographic features, but it also was responsible for the preservation of certain sediments thus proving multiple glaciation of the area. 171 _ 172 The second purpose of this dissertation is "To determine the characteristics, extent, and contact relationships of the surficial drifts associated with the Saginaw and Huron-Erie Lobes and to specify on what basis the drifts may be identified and delineated." Most of the physical characteristics of drifts associated with the two lobes are so similar that it is very difficult or even impossible to identify and differentiate many samples of drift and their lobe provenance. However, this study has established that the clay mineral suites associated with the two lobes are sufficiently different that the lobe provenance of a drift sample may ordinarily be determined with a high degree of confi­ dence by means of X-ray diffraction. It was established that the 7X/I 0 X peak height ratio for Saginaw Lobe drift is 0.91 or greater and is 0.90 or less for Huron-Erie drift. This fact may prove to be very helpful at the Saginaw/Huron-Erie interlobate contact in other areas where morpho­ logic evidence for the location of the contact is obscure. Within the Interlobate Morainic Tract the drift contact may be delineated in a detailed fashion and apparently there is little or no interdigitation of the two drifts at the surface. Another objective of this thesis is "To determine the characteris­ tics, relationships, and assemblages of the various landforms in and near the interlobate area." Research has shown that one landform assemblage consisting of outwash apron, outwash fans, and linear depressions and ridges exists within the Kalamazoo Moraine. Outwash fans, large channel fillings and linear depressions trending northeast-southwest are char­ acteristic of the Saginaw Lobe portion of the Interlobate Morainic Tract. The Huron-Erie Lobe segment of the Interlobate Morainic Tract has cre­ vasse fillings and also linear depressions with large amounts of 173 intergroup orientation variability. Distinctive landforms in the Mis­ sissinewa Moraine include eskers, drainageways, numerous small dry channels, and limited numbers of linear depressions and ridges. The most conspicuous landform assemblage of the Grass Lake Plain is the complex system of trunk esker (Blue Ridge) joined by a number of tribu­ tary eskers extending from both moraines. Two landform. types are distri­ buted throughout much of the study area and may be described as breached and notched ridges and channeled plateaus. Areal relationships and characteristics of certain landforms in the area prove that the distal portions of the Kalamazoo and Mississinewa Moraines are time— correlative and strongly suggest that the medial or proximal portions of the moraines are also time-correlative. The final stated purpose of this dissertation is "To determine, on the basis of landforms and sediments, the nature of deglaciation in the area and its effects on the landscape." The distinctive landform assemblages in the area most likely are the result of differing condi­ tions in the Saginaw and Huron-Erie Lobes. The prevalence of ice- contact slopes indicates that stagnant ice was widespread during deglaci­ ation. Eskers located both north and south of the Mill Creek lowland and the Sharon Short Hills in the Mississinewa Moraine, kames, channel fillings, crevasse fillings and similar features in the Interlobate Morainic Tract are also evidence of stagnant ice. Furthermore, the Kalamazoo Moraine is not simply an end moraine formed by an active glacier. It is, at least for the most part, an accumulation of glacio­ fluvial sediments and flow till deposited in contact with stagnant ice. Southward-draining superglacial streams formed an outwash apron on the distal side of the moraine, and especially large streams deposited outwash fans that may be traced to the crest of the moraine. These streams and subglacial meltwater from the area of the Mississinewa Moraine flowed south and west and established a drainage system in and beneath stagnant ice of both lobes. The Blue Ridge Esker and its tributary eskers on the Grass Lake Plain are associated with features in both moraines and are the product of these streams. Conversely, active ice was probably responsible for the linear groups of hills and boulders in the area proximal to the moraines. Thus, although some secondary characteristics are due to active ice, the basic nature of the landscape was determined largely by the stagnant ice conditions which prevailed during the final deglaciation of the area. In recent years study of the rock-stratigraphy of glacial sediments has been given increasing attention and has resulted in significant find­ ings. Numerous separate and significant drift sheets have been identi­ fied in many areas and each may be associated with several moraines. At the same time, landforms may have become "less 'interesting*" (White, 1973, p. 26) to some as attention was concentrated more and more on rock-stratigraphy (White, 1973, pp. 26-27) in the belief that sedimentary characteristics provide more reliable results. Frye and Willman (1962) recognized the possible significance of landforms in the study of Pleis­ tocene stratigraphy with their proposal to formally recognize morphostratigraphic units within stratigraphic nomenclature. In fact, in situations where the rock-stratigraphy is similar or identical over extensive areas the details of deglaciation may be best revealed by the nature of topographic forms and their related sediments. This dissertation has clearly demonstrated that for an area in southeastern Michigan it is possible to map an interlobate contact by means of both morphology and rock-stratigraphy. In fact, the results obtained by (1 ) mapping of landforms and (2 ) analysis of clay minerals by X-ray diffraction are corroborative indicating that, in some areas at least, the careful study of surface form may be at least as revealing as the investigation of sediment characteristics. In addition it has been shown that certain topographic characteristics are also in­ dicative of the nature of deglaciation in the area. It is evident that several modes of investigation may provide more reliable results than one. Hence, those who are concerned with the nature of glaciated areas should consider use of all proven techniques which deal with morphology as well as those that provide meaningful information regarding sediments Suggestions For Further Research During the course of this investigation it became clear that cer­ tain topics merit additional consideration. (1) Radiocarbon dating of samples of the deeply buried organic matter may provide information on the aga of the weathering surface(s?) found in the bedrock valleys and supply additional information on the glacial chronology of the area. (2) Study of topographic maps suggests that several of the northeastsouthwest and northwest-southeast trending lakes and streams of southcentral Michigan, such as in Branch and Kalamazoo Counties, seem to have characteristics similar to the Wolf Lake-Center Lake chain of features in the study area. rock valleys. Thus, they may also be associated with buried bed­ Construction of bedrock maps for that and similar areas may reveal a bedrock valley-hydrography relationship and possibly the existence of buried oxidized drift and organic matter. (3) The use of 7&/10& peak height ratios appears to be a powerful tool for differenti­ ating Saginaw and Huron-Erie drift in Jackson and Washtenaw Counties. If this 7X/I 0 X relationship is applicable outside the study area, and limited evidence presented by Mahjoory (1971) and Ogunbadejo and Quigley (1974) seem to support this possibility, it may be possible to identify the Saginaw/Huron-Erie drift contact in other portions of the state where morphological evidence is not clear-cut, such as in Hillsdale and Branch Counties. (4) By applying the X-ray diffraction technique to the clay-sized particles in subsurface till in the study area, it may be possible to determine the relationships between the Saginaw and HuronErie Lobes during the time preceding final deglaciation of the area. (5) Sediments recognized in the study area and limited reconnaissance of the Saginaw/Huron-Erie interlobate area in eastern Livingston and western Oakland Counties indicate tities of flow till. the presence of considerable quan­ Mapping the distribution of this sediment will help to determine the nature of the deglaciation environment. (6) Large channel fillings, breached and notched ridges, channeled plateaus, crevasse fillings, and small outwash fans similar to those of the study area are evident on topographic maps of eastern Livingston and western Oakland Counties. Thus, the distribution of these landforms is not limited to the study area and further study and mapping of them are needed to determine if the characteristic assemblages are present elsewhere along the Saginaw/Huron-Erie drift contact. APPENDICES APPENDIX A COMPILATION AND CONSTRUCTION OF BEDROCKSURFACE AND DRIFT THICKNESS MAPS Map Compilation Figures 3, 4, and 7, showing bedrock lithology, bedrock surface, and drift thickness, respectively, are based on data from 1,482 points. Of these, 893, or 60 percent, represent well records on file at the Water and Environment Section of the Geological Survey of Michigan in Lansing. Most are water-well records dating from the late 1960s to the present, although some oil and gas wells are also included. Data from the remaining 589 points are from the several sources listed on Table 9. Data were obtained from three or four records per survey section within much of the area. In those sections where wells are numerous, one record from each quarter-section was selected, if possible. In areas where a major valley exists on the bedrock surface, as many as ten re­ cords per section were utilized, if available, to delineate better the nature and extent of the feature. Most of those who have developed water wells within the area have had little or no formal training in the technical interpretation of sediment type and characteristics, and as a result their well records may be difficult to interpret. For example, many records list "gravelly clayE" "sandy clay," "gravelly shale," "stony clay," or simply "clay" at the surface. By comparing these records with information from soil maps and personal observation, it is apparent that the sediment described with these terms is glacial till. Consequently, when drillers have re­ corded "gravelly shale," "stony clay," or a similar sediment, that unit is interpreted most likely to be till. 177 178 Table 9. U-l o 0) CO -Q 4-1 PU ,c i CO O (U 00 13 ca P3 s Pi =J ■H fl O O. i—I CO CO 4-1 4-1 O CO EH T3 > i— I S o o CU M o CM e CO CO id 00 in )-i -H (0 o > CJ ,C o >-* •H CO ed Well Record Data Sources OO m ON i— i § ■H > J-4 -l ON CO S w - - 1 2 - - - 2 - 2 1 10 - 40 36 47 2 2 4 — 637 363 9 7 86 CT> m On at o o o vO CT\ 4-1 M o ai e > 4-i 4-1 co 4 C O U N T Y 28 11 2 6 - - — 259 140 - 4 1 - 4 110 1,482 893 363 13 8 4 84 117 63 19 49 29 43 42 20 8 10 26 12 31 * only a portion of township mapped 3 1 1 8 6 22 179 Drillers commonly report "shale" in the subsurface underlain by considerable amounts of sand and gravel. Almost certainly this "shale" is a resistant till overlying glaciofluvial materials. In the interpretation of well records it is particularly difficult to identify a contact between till and shale. Some of the drillers in the area are aware of this problem but are probably not always success­ ful in differentiating drift and bedrock.^ A few of the oil-well re­ cords prepared by geologists examining cuttings indicate that they too experience occasional difficulty in identifying a till-shale contact. 2 Drillers do not ordinarily case water wells for more than a short distance following penetration of bedrock. Therefore, the casing length of a well was sometimes used as a guide to help differentiate till and shale. On this basis it is assumed that the stratum in which the casing is terminated is bedrock and that overlying units are drift, even though identified as various types of "shale" by the driller. This assumption is supported by the observation that water-well drillers' "gravelly shale" is most often till, and review of well records also indicates that such a term is usually applied to units in the cased portions of wells. Conversely, sandstone and limestone units are only rarely cased. Therefore, in certain circumstances the use of water-well-casing data seems to serve as a useful guide in differentiation of till and shale on well records where the contact between drift and bedrock is not obvious. The practice is not without limitations, however, because at least two ■^Personal communications, Messrs. Dale Lindemann, December 17, 1974, and Melvin Fox, December 30, 1974. 2 In Oakland County, Ferris, Burt, Stramel, and Crosthwaite (1954, p. 34) also remarked on the difficulty of recognizing the drift/bedrock contact in areas underlain by Coldwater Shale. 180 well records indicated the presence of wood in "shale" in uncased sec­ tions of wells. This suggests that at least in some circumstances re­ sistant tills may not be cased by water-well drillers and are identified as "shale" on the well record. Map Construction The geographic location of each well was determined to the nearest ten acres and then identified by arbitrary grid coordinates. Altitude of the well head was determined from the most recent U.S. Geological Survey topographic map, and subsequently bedrock-surface altitude was calculated. Grid coordinates, drift thickness, and bedrock-altitude data were punched on data cards and submitted to the Michigan State University Control Data Corporation 6500 Series computer. The General Purpose Contouring Program (GPCP), developed by California Computer Products (Calcomp), was used. This program generates gridded data from information distributed at arbitrary points (well locations) by con­ structing a smooth surface passing through every data point. Contours are generated on that surface at the mesh points of the regular grid constructed by the computer. A Calcomp 963 incremental pen plotter constructed the maps at a scale of 1:63,360. The maps were then manu­ ally modified on the assumption that karst development was not a signif­ icant process affecting the bedrock surface. It is estimated that the position of about 80 percent of the contour lengths on Figure 4 and 98 percent of those on Figure 7 are shown exactly as calculated and drawn by the computer. APPENDIX B MINERALOGY OF CLAY-SIZED PARTICLES IN CERTAIN SAMPLES The mineralogy of the sediments was examined by X-ray diffraction of oriented clay (less than 2 microns) samples from forty-nine till, nine glaciofluvial, three glaciolacustrine, three shale, and two sand­ stone specimens. Although the general procedures were the same for all specimens, the details of treatment varied slightly with sediment type. The major steps of the laboratory procedure (modified from Jackson, 1956) for till and glaciolacustrine sediments are described below in (1 ). Treatment of glaciofluvial sediments, sandstone, and shale is covered in (2), (3), and (4), respectively. (1) Oxidized, unleached (presence of carbonates was determined in the field by treatment with 10% H C 1 ) , air-dry till or glaciolacustrine samples were passed through a 2 mm sieve after gentle crushing. Soluble salts and carbonates were removed by adding IN sodium ace­ tate (buffered to pH 5 with acetic acid) and heating the suspension for thirty minutes. Organic matter was removed by treatment with hydrogen peroxide (30%) and heating the suspension for thirty minutes. Free iron oxides were removed by reacting the samples with sodium citrate-bicarbonate-dithionite at 80°C. The sample was then transferred to a sedimentation cylinder and distilled water added. After thorough agitation with a plunger, the sample was permitted to stand twenty-four hours. A siphon removed the less- than-2-micron portion of the suspension. was repeated once. This fractionation A porous porcelain plate was placed on a vacuum flask, vacuum applied, and treated clay suspension deposited on the 181 182 plate- The clay film was leached with 0.1N magnesium chloride glycerol by volume). (10% The film was then washed with 10% glycerol, air-dried, and stored overnight in a dessicator. The sample was then ready for analysis as a magnesium-saturated, glycerol-solvated basally-oriented film. (2) Clay was obtained from oxidized, unleached glaciofluvial samples by wet-sieving (#300 sieve) and collecting the wash water which contained the clay in suspension. filtered through #50 filter paper. The suspension was suctionThe solids trapped on the paper were then treated as outlined in (1 ). (3) Clay was obtained from sandstone by gently crushing bedrock samples The sediment was passed through a #300 sieve and then treated as outlined in (1 ). (4) Clay was obtained from shale by gently crushing well cuttings. The sediment was placed in water, disaggregated with a sonifier, and then treated as outlined in (1 ). The oriented samples were then placed in the X-ray diffractomator of the Department of Crop and Soil Sciences and exposed to nickel-fil­ tered copper radiation. Figure 44. The resulting diffractograms are reproduced in The 7%. and loX peak heights were determined and the 7 S./I08 . peak height ratios were calculated (Table 10). Kaolinite, chlorite, vermiculite, and illite are the predominant clay minerals in the samples. maining clays produce a Illite produces a loX peak, and the re­ peak. The intensity of the 7& peak is the result of the vermiculite, chlorite, and kaolinite either individually or in combination. Therefore, the 7&/10& ratio is not a complete rainer- alogical characterization but is only used to group the samples 183 investigated. Because the diffraction intensities are obtained from the same diffractogram and a ratio of the intensities is utilized, compari­ sons can be made between different diffractograms without the use of an internal standard. In their study of the clay minerals of the Neuse River estuary in North Carolina, Griffin and Ingram (1955, p. 199) used peak height ratios and stated, It is realized that the use of intensities of (001) lines as a measure of absolute clay mineral abundances is open to many un­ certainties ; but as all the samples were handled in the same manner and as only ratios of intensities were used, the results ...are considered to be significant. Till samples 122 (Huron-Erie Lobe) and 127 (Saginaw Lobe) received further treatment. They were potassium-saturated with IN potassium chloride, dried, and X-rayed (Figure 44 ). to 300°C and X-raying. This was followed by heating After heating to 550°C, the samples were allowed to cool and then X-rayed once again. After heating to 550°C, the 7& peak was very much reduced in intensity, indicating the presence of con­ siderable amounts of kaolinite in relation to illite. On the basis of samples 122 and 127 it appears likely that Saginaw Lobe till tends to have larger relative amounts of kaolinite than Huron-Erie Lobe till and consequently higher 7&/10& peak height ratios. The Student’s t test was applied to determine if there are two populations present in the surficial till samples from the two moraines, their proximal areas, and associated portions of the Interlobate rainic Tract. Mo- Test results indicate that two populations are present at a significance level of 0.0005. 1B4 TA B LE 10. CLAY MINERALOGY, TEXTU R E, a O F SELECTED SEDIMENTS COLOR « :S s in & S 3 COZ 54 71 72 *C5 £ e 1- fig S*< MOx: ^ « 2 a-t* C* o» o oc my— P x 2 5 H I 2 _ ° Z! £ (D# * u 5 • l~ i to NW NW 30 3S 3E T 27 33 0JB2 aandy loam >p 5s 53 SE SE 15 2S IE 093 2S IW 25 83 27 24 T T 31 2.03 loam sandy loam 42 68 T T 25 - 22 1.14 sandy loam - 59 - T 41 22 39 1.05 sandy loam 0 .7 3 sandy loam 53 S NW NW _ s '4= NW SW NW 74 76 NW SW NE 20 2S IE SW NW SE 10 2S 2E 78 SE NE SE 2S 79 SE SW 6 NW 12 1S 3E 3E T 8 1 SE SE SW 15 2S 1E T - 30 - 83 NE 30 1N 4E L 51 44 - to "8 s* o >. o ! I O O 3* I0YR 31 16 7 /3 5 /4 32 17 26 15 7/4 5 /4 7/S 5/6 28 - 13 - 7 /2 5/4 7 /4 5 /3 29 18 6 /4 5 /4 61 22 17 7/4 5 /4 sandy loam 7 1 21 8 7 /4 5/G 1.16 clay 3 26 71 silty clay - 85 SE NW SW NW SE 24 1N 3E T 43 4 1 1.05 89 SW SE NW 11 2S 2E T 32 26 91 SE SE SE 1 2S 2E T - - 1.23 sandy loam - 96 97 NW NW NW SE SW NW 14 27 IN 1N 4E 4E T T 27 23 32 30 0 .8 4 0 .7 7 100 101 102 NW NW 1S 4E T NW SE 20 33 35 NE SW NW 2 2 SE 2 9 41 28 104 SW 106 SE 118 NE 122 11 44 45 7 /3 5 /4 7 /3 5 /4 62 - 20 18 7 /3 4 /3 - - clay loam loam 33 41 30 34 . 37 25 7/3 5 /4 7/4 B/4 7 /4 5/4 0 .5 7 clay loam 43 28 7 /3 4 /4 loam 45 29 38 091 0 .7 4 29 26 loam clay loam 29 31 26 27 e/s 4 /4 0.68 45 42 7 /3 5 /4 45 21 33 22 7/4 5 /4 32 47 7 /3 5 /4 53 49 30 25 17 26 7 /4 5 /4 SW 3 1S 2S 4E 3E T T NE SW 33 23 3E T 19 28 SE SE 9 3S 3E T 29 34 0 .8 5 loam SW SW 15 2S 3E T 28 36 0.78 clay SE SE NE 17 33 4E T 32 48 0 .6 7 sandy loam 123 NE NE SW 14 2S 4E T 22 25 0.88 sdy. cl. loam 124 SW SW SW 22 IS 5E T 25 34 0.74 loam 46 29 7 /4 5 /6 2 5 . 6 /3 4 / 3 126 SE SW SE 1I 1N 3E T 25 27 0.93 51 30 19 127 SW NE 3 1S 2E T 74 55 1.35 5 30 . 25 7 /3 5 /4 7 /3 5 /4 129 NW NE SE loam loam SE 10 1S IE T 34 0.91 clay 25 29 46 6 /4 4 /4 132 133 SW NE NW SE SW 12 3S 2 4S 1E 1E T T 31 49 31 42 45 1.17 sandy loam 0 .6 9 clay 59 18 22 28 19 54 6 /6 4 / 4 7 /3 4 /4 443 A I4 3 B NW NW NW NW NW 22 3S 36 27 40 27 0.90 sdy.cl. loam 1.00 e7 25 7 /4 5 /4 3S T 0 48 22 3E 3E 20 17 38 29 0.53 sdy.cl. loam 0.59 58 20 22 7 /3 5 / 4 - - - 0 .8 3 NW SE I46A SW SW SW 12 3S 3E 1468 SW SW SW 12 3S 3E T 0 !4 8 NW SE SW 32 2S 3E T 29 35 148 A 174 181 NW SW SE 2S 1S 3E 3E 0 L 14 48 SW 1S 1S 3E 3E T T 36 182 SE SW 32 9 SW NE SW NE 2 6 NW NE II I6 44 42 50 43 loam ■ 0.87 1.09 s ilty clay 0 .8 6 sandy loam 0.86 silty clay 49 - 2 59 5 29 - 53 22 - 7 /3 6 /3 - - 6 /4 5 /4 - _ 26 45 13 7 /3 5 /4 7 /4 5 /4 44 51 7 /3 5 /4 185 TABLE 10. (confd.) £• o 2 g 8 CO ®e S o U3Z 5 IS E £ £ o a: o,*, Wh « )4 , Q- -C .» «^.S? 9 5 f- X S' ° Ite L O O P o W a •S <5? 1- >8 0s nP loamy eand sandy loam 81 13 6 7 /4 5 /6 "S 4- O i £ — CO O'* CJ o 3? O IO YR 183 SW SE SW 2 IS 3E T 42 29 1.45 189 NW SE NW 22 IS 3E T 41 39 1.06 67 20 13 191 SE SE SW 2 IS 3E T - - - sandy loam 56 38 6 7 /3 5 /4 43 32 1.31 sandy loam 73 12 15 7 /3 6 /6 35 7 /4 5 /4 201 NE NE SW 20 IN 4E T 202 SE NE NE 7 IS 4E L 27 42 0 .8 4 sty. cl. loam 4 61 7 /4 5 /4 208 SE NE SE 25 2S 2E T 19 29 0 .6 5 sandy loam 57 30 13 7 /4 4 /4 0 .7 6 211 NE SW NW 20 3S 2E T 38 50 212 NE SE SW 17 3S 2E 0 28 23 1.22 2 13 216 SW NW SE SE NE 14 3S 1E T 3 6 .5 41.5 0 .8 8 NE 28 3S IE 0 22 23 sandy loam 0 .9 6 217 NW SW SE 32 3S IE T 23 35 0 .6 6 clay loam 37 31 218 NE NE SE 3 4S IW T 30 40 0 .7 5 clay loam 28 35 loam sandy loam - 38 75 36 12 26 7 /4 - - - - - - - 219 SW SE NE 27 3S IE T 43 22 1.96 220 SE NE NW 6 4S 1E T 45 30 1.50 221A NW 6 4S IE O 26 14 1.86 clay loam - 35 31 34 7 /3 5 /4 '- - - - - 58 24 18 7 /6 5 /4 - - - - - 32 6 /4 5 /4 37 7 /3 5 /4 13 5 /4 5 /4 SE SW 2 2 IB SE SW NW 6 4S IE 0 60 24 2 .5 0 - 22IC SE SW NW 6 4S IE 0 33 18 1.83 - - - - 223 SE SE NE 24 3S IW T 36 46 0 .7 8 clay loam 4 1 26 33 7 /3 5 /4 68 19 13 7 /3 5 /4 7 /3 5 /4 224 SE SE NE 28 IN 3E T 37 31 1.19 sandy loam 2 25 SE NE SE 17 3E T 20 22 0.91 sandy loam 66 25 9 226 NW SE SW 14 2S 3S 2E T 43 33 1.30 sdy.cl. loam 49 26 25 7 /3 6 /3 6 /3 4 /4 226A NE SE SW 14 3S 2E T 41 50 0 .8 2 sdy. ct. loam 58 19 227 NW NW SE 3 4S 5E T 46 53 0 .8 7 clay loam 3 1 32 23 37 7 /4 228 SW SE SW 12 2S 6E T 30 35 0.86 29 30 41 7 /3 ’ 5^3 - - - - cl ay — 229 NW SW NW 26 2S IW SS 88* 1 3 * 6 .7 7 230 NE NE NW 6 4S 2E SS 43* 4* 231 NE NE NE 21 3S 2E T 46 48 0 .9 6 sandy loam 57 27 46 0 .8 7 loam 37 sandy loam - 10.7 2 33 NW SW SW 16 2S 3E T 40 2348 SW SE SW 19 2S 4E T 26 33 0 .7 9 2 34C SW SE SW 19 2S 4E 0 32 38 0 .8 4 - - 16 7 /4 6 /4 37 26 7 /3 5 /4 61 23 16 7 /4 5 /4 - - — - - - - - 235A SE SE 22 2S 3E SH 78 36 2.16 - - 2358 SE SE 22 2S 3E SH 34 34 to o - - 235C SE SE 22 2S 3E SH 43 43 1.00 - - ▲- S c a le Factor 8 * - Scale Factor 16 T - Till 0 - Outwash L - 6 laciolacuetrine S S - Sandstone 5 /3 - - S H - Shale - - EXPLANATION OF DATA IN FIGURE 44 Sixty-six of the seventy-two X-ray diffractograms shown in Figure 44 represent magnesium-saturated (Mg sat), glycerol-solvated, basallyoriented films. The remaining six diffractograms represent samples given additional potassium saturation (K sat) and heat treatment (300° and 550°C) and are labeled accordingly. Seventy of the seventy-two diffractograms were traced with a scale factor setting of 8 and the re­ maining two diffractograms had a setting of 16. marked with a ." These two samples are IOA I4A I8A 7A IOA 7A I4 A I8A IOA I4 A I8 A I4 3 A I4 6 A 104 U IOA 7A I4 A I8A F IG U R E 44. X -R A Y IOA I4 A I8 A D IF F R A C T O G R A M S IOA I4 A I8 A 219 226A V V ^ 220 2 2IA 227 228 \Va H | 22 IB 231 22 IC 233 234B 223 224 | >34C Ui L-z225H r i 226 I W * M S 235A e 7A IOA I4 A I8 A 7A F IG U R E 4 4 . IOA I4 A I8 A (C O N T 'D .) 7A o OA I4 A I8 A 7A IO A 3 .5 A 5A 7A IOA 14 A 18 A 3 .5 A 5A 7A IOA I4 A IS A !4A I8 A 23 5 B 122 Mg sat. 122 235C K sat 122 K sat. 300° 122 K sat. 550° 127 Mg sat. 127 K sat. 229* 127 K sat. 300° 230* 7A IOA I4 A I8A 127 K sat. 550° FIGURE 44 (CONT'D.) APPENDIX C TILL COLOR The color of till samples, both moist and dry, was determined using the Munsell system. It was necessary to air-dry several samples in the laborr'ory before a dry color determination could be made. Tables 11 and 12 present the results of the investigation of till color and are constructed as a page from the Munsell book. Table 10 lists the color of each till sample studied. Table 11. Color of Brill Lake and Chelsea Till Samples HUE CHROMA 7 2 1 I0 Y R 3 8 6 4 fO 5 T>> lO 1 v. O ui 6 => -i < 2 2 ------- 2 1 / > 5 1 4 1 / 10 / 1 Number o f samples of till (Saginaw Lobe) 15 3 / 3 Brill Lake Number o f samples o f Chelsea til! (Huron-Erie Lobe) to 'o I 191 Table 12. Color of Grass Lake Till Samples HU E CHROMA 2 7 Ul 3 < > 6 5 IOYR 3 4 5 3 1 1 1 1 1 I T »» Q ------- 7 m o 2 4 3 Number of samples of Grass Lake till 1 APPENDIX D TEXTURAL ANALYSIS The hydrometer method of textural analysis was utilized in this investigation. A textural-analysis subsample was gently crushed, passed through a 2 mm sieve, and two 40 gram samples removed. Sample A was weighed, dried overnight in a 105°C oven, and reweighed to determine moisture content. Sample B was transferred to a milkshake mixer con­ taining a 5% hexametaphosphate (Calgon) solution and distilled water. After soaking for ten minutes, the sample was mixed for five minutes, transferred to a sedimentation cylinder, and distilled water added. cylinder was transferred to a constant-temperature room. The After coming to temperature overnight, the solution was agitated with a plunger, the hydrometer inserted, and read after forty seconds. taken after two hours. Another reading was The results are presented in Table 10 and Fig­ ures 11 and 27. 192 APPENDIX E LITHOLOGICAL CLASSIFICATION OF STONES Pebbles The first 100 1.0-to-2.5 cm-long (0.4 to 1.0 in) pebbles located during till-fabric determination were bagged for laboratory analysis.'*' Any of these pebbles which were blade- or rod-shaped were also included in the till-fabric analysis. In the laboratory each pebble was broken, examined with a hand lens, and classified according to lithology (Table 13, Figures 12 and 24). Sedimentary pebbles were also tested for the presence of carbon­ ates with a 1 0 % hydrochloric acid solution. Boulders Wherever five or more boulders approximately 50 cm (18 in) or more in diameter were observed within 100 to 150 m (yds) of one another, the location was noted (Figure 13). were not included. Ornamental boulders near residences A total of 1,233 surficial boulders were identified and classified in terms of lithology at 19 sites (Table 14). A total of 564 boulders exposed during extraction operations in the Blue Ridge Esker were also identified and classified (Table 15). Anderson (1957, p. 1417) found this size fraction to be the most diverse and most suitable to determine the lobe provenance of till samples. 193 TABLE 13. PEBBLE STU D Y | f Z ® § „ CO -j= m b i co *1 o i- BRILL 81 SE SE SW 15 2S g) S’ C d ac l_ CO ® # c-0 B A s a> za. L IT H O L O G Y AREA s m O LAKE T IL L OF T IL L S I • « e •o *— m -P a o ■a== o5 *o c a t/» S2 3? 0s ii a> -c o II sI 3? o (SAGINAW LOBE) IE 100 28 53 6 8 3 74 NW SW NE 20 2S IE 76 SW NW SE 10 2S 2E 78 SE SE NE 6 2S 3E 100 23 55 3 7 4 2 5 100 27 47 3 16 5 1 100 100 20 32 60 54 7 7 7 5 5 1 2 9 .0 4.4 2 .2 127 SW SW NE 3 IS 2E Total pebbles or Mean % CHELSEA 79 NW SW SE 12 IS 97 NW SW NW 27 101 NE NW SE 29 IN 4E IS 4E 500 2 6 .0 TILL 3E 100 5 3 .8 - 3 .8 56 7 19 5 27 24 30 62 25 7 9 1 9 3 16 104 SW NE SW 33 2S 3E 100 Total pebbles or Mean % 4 0 0 1 9 7 61 15 2 5 2 .2 13.5 7.8 100 - 3 1 — — 0 .8 (HURON--ERIE LOBE) 12 100 o o o 1 - - - 3 - 4 2 - 5 .3 1.5 tr 195 TABLE 14. . a o 4“ o

CO *7 » c o c * o QC ON « c -1 < lO H _"5 o w ■£ >> H<5 BRILL LAKE T IL L 15 2S 2E 34 34 12 2S IE 39 39 13 2S IE 77 76 7 2S 2E 57 54 7 2S 2E 8 8 7 2S 2E 11 9 7 2S 2E 25 19 16 2S 2E 71 70 8 2S 2E 37 37 9 2S 2E 99 96 10 2S 2E 24 24 119 11 |2S 2E 119 TOTAL 601 585 % CHELSEA 100.0 & • 9 7 .3 TILL o • . to oOS x oliiidJ BOULDERS 0> o w c ■? I ■o 2 « O 1_ ♦»- > . or o (SAGINAW LOBE) 34 38 75 1 54 8 9 19 69 1 1 36 1 1 94 23 1 19 100 24 2 559 - - 1 3 - - 9 3 .0 4 .0 (HURON-ERIE 2 5 1 1 — 3 - - — — - 1 0 .3 15 23 <22 LOBE) 100 100 97 3 - 141 NE NW N E 19 3S 3E 110 110 109 I — NW 2 3S 3E 34 34 33 - SE 32 2S 3E 26 25 24 1 186 SW NW SE 3 2S 3E 106 105 105 - NE 16 3S 3E 83 83 82 2 0 7 NW NW SW 17 3S 3E 17 3 173 TOTAL 632 % — — 3E NW - a> — 3S 2 0 6 SE — — 19 SE - - NW NW SW 149 SE a o - — 55 145 NW S W o> c o « •o c a CO - 1 - - - - - - 1 — - 1 - 1 — - 168 5 — - - 630 618 10 2 - 2 100.0 99.7 97,8 A6 03 - 0.3 MS Oi CM ro 09 27 -4 Section CO £ £ £ £ in m m ni rn ro 09 ro 216 1100 MS O) 4S MS NE — m CO 1 ro m Range -4 Number of ciasts w CM % Crystalline ro — Oi OI > 1 100 3 3 1 26 1 28 38 I — % Carbonate CM ro 1 Site number % Sandstone ro i 4* 1 — ro ro % Shale i i 1 1 __ i — % Other Number of clasts cr 09 % Crystalline ^ — OI 4* % Sandstone % Carbonate ro i 1 t Cm CD CM 26 i & 48 42 40 i Cm a> ro — i Oi •ft o 001 100 33 2! 40 100 SS CM CM 66 600 i — OI i % Shale * o> % Other 961 u> TJ m CD CD m co ESKER % Carbonate RIDGE a> CD f" m ^ to rn ~n m z a: m 53 00 100 3 7 CD 40 100 CM o o 100 3 6 % Crystalline 29 100 5 0 £ 100 100 4 0 Number of clasts 1 38 *0 -» CO o -< 70 c: 3 4 36 29 •fe. ro a> 98 — 001 Oi CO CO BLUE 84 1 H z OF 67 I CD O <= r~ o m LITHOLOGY 80 *\» % Sandstone 45 1 600 80\ 1 001 CM ro Site number STONE 1 Township 15. 5 € TABLE 1 z 1/4 212 220 1 m 219 8 5 1 CO 127 1 1/4 SE z m 09 & 0) NE SE SE NE NW 1/4 section 481 NE SE NW SE Cb SE or Mean % ? z m i Total clasts cm z APPENDIX F TILL FABRIC The till-fabric methodology is basically that developed by Holmes (1941). The working face was on or near a hilltop in unleached till (as determined by 10% hydrochloric acid) at a depth of 1.2 m (4 ft) or more to minimize the effects of frost heave and mass movement (Harrison* 1957). A horizontal surface about 30 to 45 cm (12 to 18 in) square was cleared with a mattock, and pebbles were exposed by carefully scraping off thin layers of till with the blade of a spatula. shaped clasts (long [A1 axis to medium Blade-and rod­ 0*3 axis ratio of at least 3:2) have been shown to yield the most reliable results (Drake, 1974, p. 250) and were the only shapes considered in this study.^ Only stones with long axes of 1.0 to 10.0 cm (0.4 to 3.9 in) were used; stones touching one another were rejected. When a suitable clast was located which appeared to be of appropriate size and shape, an aluminum knitting needle was carefully aligned with the long axis of the clast. The pebble was then removed from the till matrix, measured with a vernier caliper to the nearest millimeter (0.04 in), and if the proper size and shape, its dimensions were recorded (Tables 16 to 24). Dip of the needle was then determined to the nearest degree and bearing to the nearest five degrees with a Brunton compass. At no time was it necessary to sample through a vertical distance of more than 0.3 m (1 ft). Seven fabrics were measured which consist of fifty pebbles; one fabric consists of thirty-one peb­ bles; and one fabric consists of twenty-five pebbles. ^It should be noted that this shape restriction may cause the mensuration procedure to be quite lengthy. At sites with tills that are not particularly stony, such as those in the study area, ten to fifteen hours may be required to measure a fifty-pebble fabric. 197 198 The lithology of the clasts was determined in the laboratory by the method outlined in Appendix E. Bearings of the long axes of clasts were plotted on rose diagrams in groups with fifteen-degree intervals (Figure 14). These diagrams show horizontal orientation and direction of dip of the long axes of the clasts. Dipping stones were plotted at full value, and horizontal stones were plotted at half values in opposite directions in the manner used by Wright, 1962. 199 EXPLANATION OF DATA IN TABLES 16 TO 24 Orientation of long (A) axis given in degrees. Bearings are in relation to true north based on 2 °W magnetic declination. Dimensions of pebbles’ A, B, and C axes given in millimeters. Dip of long (A) axis given in degrees. LAV— Long (A) axis vertical, therefore orientation data is for medium (B) axis. Table 16. Site 74 Till-Fabric Data for Site 74 Location NW^gSW^gNESg sec. 20. T. 2 S. , R. I E . Topography Kalamazoo Moraine Altitude 980 ft (298.7 m) Depth of Leaching 38 in (96 cm) Pebble Number Dimensions (roadcut) Orient. Dip 0 Analysis Depth 8 ft (2.4 m) Pebble Number Dimensions 26 12 8 4 N40W 2NW Orient. Dip 1 40 18 8 N60W 2 25 16 11 N60W 20NW 27 15 10 5 N55E 36 NE 3 28 16 10 N65W 25NW 28 22 10 7 N75E 15NE 4 33 22 12 S75E 12SE 29 11 6 5 S 7S 5 44 22 18 S80E 32SE 30 32 19 17 S55E 19SE 6 12 8 6 S70E 30SE 31 12 8 6 N50E 15 NE 7 18 7 7 N80E 8 NE 8 13 9 5 S40E 10SE 9 11 7 4 S45W 8 SW 10 10 4 4 N15W 5NW 11 13 7 4 N65E 5NE 12 20 9 9 N85E 23NE 13 19 13 4 N75W 0 14 15 10 7 N15W LAV 15 28 14 10 N80E 0 16 22 14 11 S25E 16 SE 17 14 9 5 S75E 37SE 18 18 11 7 S70E 18SE 19 62 26 34 S30E 4SE 20 82 54 30 S60E 4SE 21 20 10 7 N15W 0 22 19 12 9 S60E 23 18 12 7 N50W 24 26 15 r-i N20W 10NW 25 12 8 3 N20W 11NW 48SE 0 201 Table 17. Site 76 Till-Fabric Data for Site 76 Location StfhSiWhSEh sec. 10. T. 2 S. , R. 2 E. (roadcut) Altitude 970 ft (295.7 to) Depth of Leaching 50 in (1 .27 m) Pebble Number Dimensions Analysis Depth 5.5 ft (1.6 m) Orient. Dip Pebble Number Dimensions Orient. Dip 1 13 8 5 S5W 5SW 26 15 6 6 2 17 9 3 N5E 5NE 27 15 4 3 W 3 10 5 5 E 0 28 21 11 8 N5W 36NW 4 12 6 5 S5E 32 SE 29 13 9 5 S65W 37SW 5 10 6 5 S50W 30SW 30 10 5 3 S25E 5SE 6 20 11 8 S40W 24SW 31 10 6 5 N10E 0 7 13 8 6 N50W 22NW 32 13 9 3 S5W 4SW 8 12 7 4 N50W 28NW 33 19 11 9 E 16 E 9 27 5 3 N70W 2NW 34 11 5 4 N45E 0 10 21 12 8 N45W 3NW 35 13 6 4 S80W 3SW 11 13 7 5 N25W 0 36 20 9 6 S20W 43SW 12 12 6 5 S75W 10 SW 37 12 7 4 N25W LAV 13 13 4 3 S25W 31SW 38 12 7 5 N80W 7NW 14 13 7 5 S45E 56SE 39 12 5 3 N30W 2NW 15 12 7 4 N25W LAV 40 12 8 3 N25E 0 16 14 8 4 N20W 0 41 12 7 5 S35W 8 SW 17 14 9 6 S10W 39SW 42 12 8 6 S15W 5SW 18 20 11 5 N80E 46NE 43 11 4 3 N35E 2NE 19 16 6 5 N75E 28NE 44 11 7 3 S40E 55SE 20 18 12 8 N85W 5NW 45 15 10 5 N50W 15NW 21 14 6 4 S50W 17 SW 46 12 5 5 N15E 33NE 22 18 10 5 N35W 0 47 10 4 2 S25W 16 SW 23 25 12 6 N45E 3NE 48 10 7 4 S85W 48SW 24 12 8 4 N20W 0 49 11 7 4 S 8S 25 13 6 6 N80W 34NW 50 17 7 7 N45W 0 S25E 25 SE 5W 202 Table 18. Site 78 Till-Fabric Data for Site 78 Location SE^gSE^NE^ sec. 6 . T. 2 S., R. 3 E. Topography Kalamazoo Moraine Altitude 1000 ft (304.8 in) Depth of Leaching 36 in (0. 9 m) Pebble Number Dimensions Orient. (roadcufc) Dip Analysis Depth 59 in (1.5 tn) Pebble Number Dimensions Orient. Dip 1 15 9 8 S10E 30SE 26 13 7 8 S35E 45SE 2 11 6 5 S5E 22SE 27 23 14 12 S5W 65SW 3 20 10 9 S15E 14SE 28 21 12 6 S20E 30SE 4 17 11 3 N20E 29 11 7 5 S20E 54SE 5 29 17 8 S35E 15 SE 30 11 6 2 S55E USE 6 12 8 6 S20E 14SE 31 10 6 5 S35W 3SW 7 12 8 6 S75E 25SE 32 13 9 4 S40W 2SW 8 16 10 8 S25E 44SE 33 19 13 5 S15E 25SE 9 15 9 4 S50W 11SW 34 21 14 4 S5E 34SE 10 16 11 8 S5E 43SE 35 11 6 5 S35E 14SE 14 8 5 N10E 36 15 10 6 S25E 52SE 12 18 12 8 S5E 24SE 37 10 6 6 S35W 41SW 13 12 8 7 S 63S 38 13 6 5 S20E 47SE 14 18 9 7 S40E 21SE 39 10 5 5 N70W 17NW 15 20 13 11 S30E 44SE 40 24 16 8 S30E 26SE 16 11 6 4 S5W 4SW 41 15 10 8 S40E 28SE 17 20 13 10 S15E 45 SE 42 35 23 17 S60E 21SE 18 29 15 11 S10E 35 SE 43 13 7 6 S10E 36SE 19 12 7 5 S35E 28SE 44 12 8 6 S20E 31SE 20 18 9 9 S5E 34SE 45 19 13 12 S35E 62SE 21 15 10 9 S15W 45SW 46 28 17 11 N70W 6 NW 22 11 6 4 S20E 10SE 47 12 7 6 S25E 3SE 23 25 17 12 S10E 54SE 48 12 7 7 S50E 4SE 24 14 9 5 S15E 44SE 49 10 6 5 S5E 21SE 25 11 5 4 S5E 63SE 50 10 6 4 S40E 40SE 0 0 203 Table 19. Till-Fabric Data for Site 79 Location NWigSW^SE^ sec. 12, T. 1 S. , R. 3 E. Site 79 Altitude 940 ft (286.5 m) Topography Interlobate Morainic Tract Depth of Leaching 37 in (0.9 m) Pebble Number Dimensions Orient. Dip (roadcut) Analysis Depth 4 ft (1.2 m) Pebble Number Dimensions 26 20 12 8 N85E 43NE Orient. Dip 1 26 11 6 S55E 2 16 10 9 N35W 0 27 16 9 6 S45E 21SE 3 12 7 4 N80W 0 28 30 14 11 N20W 30NW 4 11 6 4 S30E 15 SE 29 21 14 7 S80E 32SE 5 16 10 3 S50E 213E 30 28 14 11 S65E 24SE 6 30 20 10 S50E 15SE 31 15 9 6 N25W 22 NW 7 11 7 5 N50W 5NW 32 15 11 8 N60E 12NE 8 25 16 10 N60W 26NW 33 14 9 6 S30E 30SE 9 29 15 11 S65E 54SE 34 10 6 3 N40W 2NW 10 28 15 9 N70E 35 14 8 6 N20E 2NE 11 18 11 8 N15E 23NE 36 14 7 2 N35W 0 12 20 10 10 S80E 40SE 37 18 12 8 N30E 13 26 15 12 S35E 21SE 38 13 8 5 N10E 14 13 7 5 S60E 28SE 39 36 23 18 S75E 38SE 15 22 10 9 N30W 0 40 19 10 10 S55E 23SE 16 24 15 13 N70W 8 NW 41 15 10 9 N75W 15 NW 17 18 12 8 S45E 42SE 42 18 12 4 N30W 15NW 18 12 6 4 N25W 0 43 13 8 8 S50E 44SE 19 17 9 7 S75E 5SE 44 28 15 8 S60E 10SE 20 15 7 5 S20E 35 SE 45 13 7 5 S85E 20SE 21 22 14 9 N75E 0 46 21 13 13 S55E 19SE 22 18 9 7 S55E 8 SE 47 15 9 6 S65E 37SE 23 31 18 11 S5W 9SW 48 11 7 5 S70E 37SE 24 20 13 11 N35W 25NW 49 23 14 13 N70W 25 24 12 7 S25E 28SE 50 16 10 10 N20W 28SE 0 54NE 0 0 14 NW 204 Table 20. Site 8T Till-Fabric Data for Site 81 Location SE*gSE?sSWh sec. 15, T. 2 S., R. 1 E. Topography Kalamazoo Moraine Altitude 960 ft (292.6 m) Depth of Leaching ? (topsoil removed) Pebble Number Dimensions Orient. (pit) Dip Analysis Depth about 6 ft (2 m) Pebble Number Dimensions Orient. Dip 1 10 7 4 N10W 40NW 26 10 4 3 S30E 4SE 2 10 5 4 N5W 27NW 27 12 7 5 S10E 6 SE 3 13 9 5 S80E 5SE 28 18 10 6 N70W 0 4 11 7 3 N85E 20NE 29 11 7 4 S15E 2SE 5 18 10 3 S10W 22 SW 30 17 11 5 S80E 28SE 6 30 11 4 N5E 1NE 31 15 10 7 N60W 0 7 25 13 7 N35W 15NW 32 16 8 7 S30W 6 SW 8 17 11 9 N20W 55NW 33 21 12 9 N35W 0 9 10 6 4 N30W 27NW 34 20 10 6 S15W 12SW 10 32 13 11 S80W 18SW 35 10 6 3 N85E 35NE 11 15 10 6 N 0 36 17 10 8 N30W 8 NW 12 17 10 6 N55E 2NE 37 13 5 4 N30E 5NE 13 15 10 4 N15E 5NE 38 17 9 6 14 26 17 8 S15W 3SW 39 24 16 5 15 15 9 6 N 2N 40 10 5 4 16 11 5 2 S5W 15 SW 41 27 18 11 17 10 6 u S40E 2SE 42 24 14 10 18 20 10 6 N15W 7NW 43 17 9 3 S20W 10SW 19 16 9 6 S40E 21SE 44 11 5 3 S5E 12 SE 20 15 7 1 N20W 5NW 45 13 7 7 N10W 17 NW 21 28 14 13 S40E 18SE 46 13 7 4 N30E 13NE 22 16 8 6 N75E 8 NE 47 17 6 4 N70W 0 23 11 5 2 N30W 0 48 12 8 4 N15W 4NW 24 23 11 8 S10W 11SW 49 25 14 4 N30W 0 25 15 8 6 S75E USE 50 13 7 6 N55W 24NW N N35E E S20E S 13N 17NE 5E 7SE 9S 205 Table 21. Site 81A Till-Fabric Data for Site 81A Location SE^SE^SW^ sec. 15. T. 2 S.. R. 1 E. (pit) Topography Kalamazoo Moraine Altitude 960 ft (292.6 m) Depth of Leaching ? (topsoil removed) Pebble Number Dimensions Orient. Dip 1 12 7 6 S15E 7SE 2 25 16 10 S10E 1SE 3 16 7 6 N25W 5NW 4 11 5 3 N20W 3NW 5 16 11 10 N35E 24NE 6 37 21 13 N10W 4NW 7 16 7 5 N35E 0 8 11 7 4 S25W 3SW 9 10 6 3 N 22N 10 18 12 7 S60E 9SE 11 18 12 8 S 8S 12 15 9 8 N5W 0 13 12 6 4 N15W 11NW 14 21 13 10 S15E 3SE 15 24 15 12 16 15 9 4 N35W 0 17 11 7 3 N10W 8NW 18 18 10 5 S15E 6 SE 19 18 11 10 S35W 2 SW 20 11 6 5 S5W 3SW 21 18 9 8 S 22 22 12 8 N15W 5NW 23 10 6 3 N5E 3NE 24 15 10 5 N15W 0 25 22 7 7 N10W 0 S 14S 4S Analysis Depth about 6 ft (2 m) Pebble Number Dimensions Orient. Dip 206 Table 22. Till— Fabric Data for Site 97 Location NW^gSW^NW^ sec. 27, T. I N . , Site 97 Pebble Number Dimensions (roadcut) Altitude 950 ft (289 .6 m) Topography Interlobate Morainic Tract Depth of Leaching 30 in (0.76 m) R. 4 E. Analysis ,1Depth 9 ft (2.7 m) Orient. Dip Pebble Number S 10 S 26 21 14 12 S65E 45 SE Dimensions Orient . Dip 1 15 10 6 2 14 9 6 S20W 16 SW 27 23 8 8 S40E 55SE 3 29 12 8 N30E LAV 28 28 19 11 S55E 41SE 4 21 14 9 S5E 34SE 29 20 12 5 S60E 4SE 5 12 8 5 S15W 3SW 30 17 9 7 S70E 56 SE 6 33 19 14 N85E 17NE 31 22 9 6 N50W 8 NW 7 15 10 7 S25W 6 SW 32 19 7 6 S15W 40 SW 8 14 8 7 S10W 36 SW 33 13 8 5 S75E 36 SE 9 12 7 5 S40E 41SE 34 12 8 4 S20E 8 SE 10 23 13 9 N5W 11NW 35 19 12 10 S45E 12SE 11 19 12 6 N65E 31NE 36 11 7 4 S40E 26SE 12 21 12 8 S55E 28SE 37 12 7 4 S10E 45 SE 13 29 11 5 N75W 40NW 38 18 12 8 S60E 58SE 14 20 13 4 S45W 27SW 39 12 7 6 S45E 17 SE 15 18 11 6 S30W 25 SW 40 28 14 5 N35W 19NW 16 13 9 5 N15W 13NW 41 25 16 13 S15W 49SW 17 11 4 3 S85E 44SE 42 20 13 10 S35E 41SE 18 17 9 7 N30E 46NE 43 23 12 8 N75E 20NE 19 16 11 7 S35E 35SE 44 27 17 13 S55W 34SW 20 18 12 5 S85E 33SE 45 15 9 6 S75E 38 SE 21 11 7 5 S20W 7SW 46 17 10 6 S65E 39SE 22 12 8 7 S70E 40SE 47 22 15 10 N80W 24NW 23 17 8 5 S80E 16 SE 48 14 9 9 S70E 3SE 24 17 10 9 S35W 32SW 49 13 7 7 S20E 44 SE 25 11 7 3 S60E 35SE 50 13 8 2 S85E 30SE 207 Table 23. Site 101 Till-Fabric Data for Site 101 Location NEigNW^SE^g aec. 29. T. 1 S., R. 4 E. Ooadcnt'l Topography Interlobate Morainic Tract Depth of Leaching 30 in (0.76 m) Pebble Number Dimensions Altitude 945 ft (288.0 m) Analysis Depth 6 ft (1.8 m) Pebble Number Dimensions 26 16 10 4 N80E 30NE 0 27 23 13 9 S70E 20SE 48E 28 13 8 6 N40W 35 NE 29 20 10 6 S85E 12SE 30 10 5 3 N75E 11NE 31 16 8 7 S85W 5SW Orient. Dip 18NW Orient. Dip 1 38 25 13 N55W 2 23 11 6 N85W 3 20 13 8 4 13 9 7 N60E 5 36 22 13 N85W 6 10 6 5 S55E 7 12 9 5 N65W 0 32 12 7 6 N55W 0 8 12 7 3 N65E 0 33 12 7 5 N55W 0 9 25 15 11 N80W 10 NW 34 13 7 4 S50E 10 15 9 4 S45E 28SE 35 12 8 5 N70W 0 11 15 9 7 N80E 28NE 36 12 8 5 N60W 0 12 23 12 10 0 37 11 7 7 S60E 15 SE 13 14 9 8 N50W 0 38 51 30 18 N75E 26NE 14 15 10 6 N80W 0 39 24 14 13 S60E 36SE 15 20 12 11 S55W 15 SW 40 25 13 12 N80E 37NE 16 12 7 3 N70E 15 NE 41 30 15 13 N45W 0 17 26 22 14 S55E 8 SE 42 13 7 4 N55W 2NW 18 13 8 6 N80E 9NE 43 11 7 4 N55W 0 19 14 8 8 N85W 0 44 14 8 4 N35W 0 20 15 9 8 10E 45 10 5 5 S45E 21 15 10 7 N70W 0 46 17 10 7 N80W 0 22 13 7 6 N80W 5NW 47 16 10 9 N50W 0 23 22 12 11 N75W 0 48 21 13 11 N70E 0 24 13 7 5 N45W 0 49 11 7 5 N75W 20NW 25 11 6 5 N60W 0 50 23 14 10 S40E 38SE E E E 0 30 SE 0 28SE 21SE 208 Table 24. Site 104 Till— Fabric Data for Site 104 Location SW^NE^SW^s sec. 33, T. 2 S. , R. 3 E. (roadcut) Altitude 990 ft (301. 8 m) Topography Mississinewa Moraine Analysis Depth 4 .5 ft (1. 6 m) Depth of Leaching 33 in (0.84 m) Pebble Number Dimensions Orient. Dip Pebble Number Dimensions Orient. Dip 1 10 6 5 S75W 8 SW 26 16 10 7 N55E 2 17 10 6 N80E 41NE 27 18 10 6 S80E 15 SE 3 30 20 5 N75E 46NE 28 18 10 6 S75E 14SE 4 26 15 5 N85E 41NE 29 28 17 12 S80E 35 SE 5 17 9 7 S60W 30 SW 30 16 8 6 S80E 15SE 6 17 10 4 S70E 45SE 31 18 12 7 N80E 23NE 7 11 5 4 S75E 35 SE 32 24 14 12 N85E 0 8 15 10 9 N55E 37NE 33 11 7 5 N85W 0 9 20 11 3 N60W LAV 34 70 45 25 10 18 12 8 N65E 5 ONE 35 25 14 13 S80E 35 SE 11 16 9 6 45E 36 20 11 7 S70E 16 SE 12 24 12 11 NSW 25NW 37 33 21 17 N75E 18NE 13 15 11 8 S85E 21SE 38 15 9 7 S70E 31SE 14 14 9 6 S75E 35SE 39 17 11 8 S65E 12SE 15 12 8 4 N50E 41NE 40 24 9 7 S60W 6 SW 16 41 28 15 N60E 38NE 41 48 28 21 N75E 15NE 17 19 6 4 N80E 22NE 42 16 7 7 N75E 18 12 7 3 S60E 20SE 43 12 8 5 N70E 33NE 19 27 12 10 S80E 14SE 44 20 13 8 N60E 36NE 20 57 28 11 N85E 8NE 45 64 43 31 N80E 30NE 21 14 9 7 N85E 28NE 46 18 10 6 S85E 10SE 22 12 6 4 17E 47 16 6 5 N75E 10NE 23 11 7 4 S65E 13SE 48 19 12 8 S70E 22SE 24 15 4 4 N75W 49 19 12 9 S80E 18SE 25 14 8 5 S70E 50 16 11 7 E E 0 55SE E E 0 29E 0 45E APPENDIX G LOCATIONS OF SELECTED FLOW-TILL SITES A positive or probable identification of flow till has been made at each of the sites listed below. Additional site locations are pre­ sented in Chapter 3 and Figure 22. Table 25. Locations of Selected Flow-Till Sites Site Number 51 NW^SESjjNWJfi sec. 17, T. 1 s., R. 4 E. 59 SEkpftJhSEhi sec. 73 NW^SW%NW k s e c . 24, T. 2 s • » R. 1 W. 12, T. 2 S. , R. 1 E. 88A m k S F k S E k sec. 10, T. 2 s . , R. 2 E. 134 m k S E k S E k sec. 25, T. 3 s • » R. 2 E. 138 SWJfiSWisSWJi sec. 16, T. 3 S., R. 3 E. 139 NW^SW%SW% s e c . 16, T. 3 s., R. 3 E. 144 NWJfiSWJsNW% sec. 14, T. 3 S., R. 3 E. 150 SWisNEifiNWJs sec. 10, T. 2 s., R. 3 E. 158 NE^SE^NW^s s e c . 171 NEJtSW^SWJs sec. 30, T. 1 s., R. 3 E. 190 NEJiNEi^NWiz; sec. 203 NE^SE*sNW*S sec. 17, T. 1 205 s w k s w k s w k sec. 7, T. 2 S • y R. 2 E. 1, T. 2 S. , R. 3 E. s *, R. 4 E. 35, T. 1 N., R. 4 E. 209 LIST OF REFERENCES LIST OF REFERENCES Aartolahti, T., 1972, On deglaciation in southern and western Finland: Fennia, v. 114, 84 p. Alden, W. C., 1918, The Quaternary geology of southeastern Wisconsin with a chapter on the older rock formations: U.S. Geol. Survey Prof. Paper 106, 356 p. American Commission on Stratigraphic Nomenclature, 1961, Code of stratigraphic nomenclature: Am. Assoc. Petroleum Geologists Bull., v. 45, p. 645-60. Anderson, R. C . , 1957, Pebble and sand llthology of the major Wisconsin glacial lobes of the Central Lowland: Geol. Soc. America Bull., v. 6 8 , p. 1415-1450. Barwick, J . , 1958, Bedrock topography and lithology of Jackson and Cal­ houn Counties, Michigan: Incomplete, unpublished map on file at the Michigan Geol. Survey, Lansing, scale 1:63,360. Bay, J. W . , 1938, Glacial history of streams of southeastern Michigan: Cranbrook Inst, of Sci. Bull., v. 12, 6 8 p. Black, R. F . , 1969, Glacial geology of Northern Kettle Moraine State Forest, Wisconsin: Wisconsin Acad. Sci., Arts, Letters Trans., v. 57, p. 99-119. 1970, Glacial geology of Northern Kettle Moraine State Forest, in Glacial geology of Two Creeks forest bed, Valderan type locality, and Northern Kettle Moraine State Forest: Wisconsin Geol. Survey Inf. Circ., v. 13, p. 33-38. Bogacki, M . , 1973, Geomorphological and geological analysis of the pro­ glacial area of Skeidararjokull, central western and eastern sec­ tions: Geographia Polonica, v. 7, p. 57-88. Boulton, G. S., 1968, Flow tills and related deposits on some Vestspitsbergen glaciers: Jour, of Glaciology, v. 7, p. 391-412. 210 211 Boulton, G. S., 1971, Till genesis and fabric in Svalbard, Spitsbergen, in Goldthwait, R . P ., e d . , Till: A symposium: Columbus, Ohio State Univ. Press, p. 41-72. 1972, Modern Arctic glaciers as depositional models for former ice sheets: Jour. Geol. Soc. London, v. 128, p. 361-393. Buddington, A. F . , and Leonard, B. F . , 1962, Regional geology of the St. Lawrence County magnetite district, northwest Adirondacks, New York: U.S. Geol. Survey Prof. Paper 376, 145 p. Castillon, D. A., 1972, The relationships between morphostratigraphy, rock stratigraphy, and aspects of till fabric in central Illinois (Ph.D. dissertation): East Lansing, Michigan State Univ., 149 p. Chamberlin, T. C . , 1876-7, On the extent and significance of the Wiscon­ sin kettle moraine: Wisconsin Acad. Sci., Arts, Letters Trans., v. 4, p. 201-234. 1883a, Geology of Wisconsin: Wisconsin Geol. Nat. Hist. Survey, v.l, p. 1-300. 1883b, Terminal moraine of the second glacial epoch: U.S. Geol. Survey Third Ann. Rept., p. 291-402. Chang, H. C . , 1968, X-ray diffraction studies of test boring samples from the glacial lake plain in Wayne County, Michigan (M.S. thesis) Detroit, Wayne State Univ., 89 p. Charlesworth, J. K . , 1957, The Quaternary Era with special reference to its glaciation: London, Edward Arnold, 2 v . , 1700 p. Chung, P. K . , 1973, Mississippian Coldwater Formation of the Michigan Basin (Ph.D. dissertation): East Lansing, Michigan State Univ. 159 p Dorr, J. A., Jr., and Eschman, D. F., 1970, Geology of Michigan: Ann Arbor, Univ. of Mich. Press, 476 p. Drake, L. D . , 1974, Till fabric control by clast shape: Geol. Soc. Amer­ ica Bull., v. 85, p. 247-250. Drelmanis, A., and Goldthwait, R. P., 1973, Wisconsin glaciation in the Huron, Erie, and Ontario Lobes, in Black, R. F . , and others, e d s ., The Wisconsinan Stage: Geol. Soc. America Mem. 136, p. 71-106. Embleton, C., and King, C. A. M . , 1968, Glacial and periglacial geo­ morphology: London, Edward Arnold, 608 p. Engberg, C. A., and Austin, F. R . , 1974, Soil survey of Livingston County, Michigan: U.S. Dept. Agriculture Soil Conservation Service and Michigan Agricultural Expt. S t a . , 92 p. 212 Farrand, W. R . , and Eschman, D. F . , 1974, Glaciation of the southern peninsula of Michigan: A review: Michigan Academician, v. 7, p. 31-56. Ferris, J. G . , Burt, E. M . , Stramel, G. J., and Crosthwaite, K. G . , 1954, Ground water resources of southeastern Oakland County, Michigan: Michigan Dept. Conserv., Geol. Survey Div. Prog. Rept. 16, 234 p. Flint, R. F., 1928, Eskers and crevasse fillings: Am. Jour. Sci., v. 15, p. 410-416. 1971, Glacial and Quaternary geology: New York, Wiley, 892 p. Fogelberg, P., 1970, Geomorphology and deglaciation at the second Salpausselka between Vaaksy and Vierumaki, southern Finland: Societas Scientiarum Fennica, Commentationes Physico-Mathematicae, v. 80A, 90 p. Folsom, M. McK., 1971, Glacial geomorphology of the Hastings quadrangle, Michigan (Ph.D. dissertation): East Lansing, Michigan State Univ., 166 p. Frye, J. C., 1968, Development of Pleistocene stratigraphy in Illinois, in The Quaternary of Illinois: Urbana, Univ. of Illinois, Coll. of Agriculture Spec. Pub. 14, p. 3-10. Frye, J. C., and Willman, H. B., 1962, Morphostratigraphic units in Pleistocene stratigraphy: Am. Assoc. Petroleum Geologists Bull., v. 46, p. 112-113. Galon, R . , 1973, Geomorphological and geological analysis of thepro­ glacial area of Skeidararjokull: Geographia Polonica, v. 26,p. 1556. Goldthwait, R. P., 1971, Introduction to till, today, in Goldthwait, R. P., e d . , Till: A symposium: Columbus, Ohio State Univ. Press, p. 3-26. Goldthwait, R. P., Dreimanis, A., Forsyth, J. L . , Karrow, P. F . , and White, G. W . , 1965, Pleistocene deposits of the Erie Lobe, in Wright, H. E., Jr., and Frey, D. G . , eds., The Quaternary of the United States: Princeton, N.J., Princeton Univ. Press, p. 85-97. Griffin, G. M . , and Ingram, R. L . , 1955, Clay minerals of the Neuse River estuary: Jour. Sed. Petrology, v. 25, p. 194-200. Harrison, W . , 1957, A clay till fabric; its character and origin: Jour. Geol., v. 65, p. 275-307. Hartshorn, J. H . , 1958, Flowtill in southeastern Massachusetts: Geol. Soc. America Bull., v. 69, p. 477-482. 213 Hester, N. C . , and DuMontelle, P. B. , 1971, Pleistocene mudflow along the Shelbyville Moraine front, Macon County, Illinois, in Gold­ thwait, R. P., e d . , Till: A symposium: Columbus, Ohio State Univ. Press, p. 367-382. Holmes, C. D. , 1941, Till fabric: Geol. Soc. America Bull., v. 52, p. 1299-1354. Horberg, L., 1956, Bedrock topography and Pleistocene glacial lobes in central United States: Jour. Geol., v. 64, p. 101-116. Jackson, M. L. , 1956, Soil chemical analysis- advanced course: Madison, Wisconsin, by the author, Univ. of Wisconsin, 894 p. Kaye, C. A., 1960, Surficial geology of the Kingston quadrangle, Rhode Island: U.S. Geol. Survey Bull. 1071-1, p. 341-396. Keifenheim, K. E . , 1974, A study of the morphology of the Blue Ridge Esker and certain related sedimentary characteristics (Master’s research paper, Dept, of Geography): East Lansing, Michigan State Univ., 49 p. Kneller, W. A., 1964, A geological and economic study of gravel deposits of Washtenaw County and vicinity, Michigan (Ph.D. dissertation): Ann Arbor, Univ. of Michigan, 190 p. Kunkle, G. R. , 1960, The groundwater geology and hydrology of Washtenaw County and the upper Huron River basin (Ph. D. dissertation): Ann Arbor, Univ. of Michigan, 247 p. Lane, A. C., 1899, Water resources of the lower peninsula of Michigan: U.S. Geol. Survey Water-Supply Paper 30, 97 p. Leverett, F . , various dates, Unpublished field notebooks and maps: on file at the U.S. Geol. Survey Library, Denver, Colorado. 1904, Review of the glacial geology of the southern peninsula of Michigan: Sixth Rept. Michigan Acad. Sci., p. 100-110. 1912, Surface geology and agricultural conditions of the southern peninsula of Michigan: Michigan Geol. Biol. Survey Pub. 9, Geol. Ser. 21, 144 p. Revised and reprinted as Pub. 25, Geol. Ser. 21, 1917. 1924, Map of the surface formations of the southern peninsula of Michigan: Michigan Dept. Conserv., Geol. Survey D i v . , scale 1:500,000. Leverett, F. , and Taylor, F. B . , 1915, The Pleistocene of Indiana and Michigan and the history of the Great Lakes: U.S. Geol. Survey Mon. 53, 529 p. 214 Lindsey, D. A., 1969, Glacial sedimentology of the Precambrian Gowganda Formation, Ontario, Canada: Geol. Soc. America Bull., v. 80, p. 1685-1702. Mahjoory, R . , 1971, Clay mineralogy of some litho- and toposequences of soils in Michigan (Ph.D. dissertation): East Lansing, Michigan State Univ., 138 p. Marcussen, I., 1973, Studies on flow till in Denmark: Boreas, v. 2, p. 213-231. 1975, Distinguishing between lodgement till and flow till in Weichselian deposits: Boreas, v. 4, 113-123. Martin, H. M . , 1936, The centennial geological map of the southern peninsula of Michigan: Michigan Dept. Conserv., Geol. Survey Div. Pub. 39, Geol. Ser. 33, scale 1:500,000. 1955, Map of the surface formations of the southern peninsula of Michigan: Michigan Dept. Conserv., Geol. Survey Div. Pub. 49, scale 1,500,000. Martin, H. M . , and Straight, M. T., 1956, An index of the geology of Michigan, 1823-1955: Michigan Dept. Conserv., Geol. Survey Div. Pub. 50, 461 p. Michigan Department of Natural Resources, various dates, Hydrographic maps of selected lakes, various scales. Moore, R. K . , 1959, Pre-Pleistocene topography, lithology and glacial drift thickness of Livingston and Shiawassee Counties, Michigan (M.S. thesis): East Lansing, Michigan State Univ., 39 p. Morse, E. W . , 1970, A study of subsurface Pleistocene drift at Saginaw, Michigan: Detroit, Wayne State Univ., 99 p. Nellist, J. F . , 1907, Surface (Pleistocene) Geology: Michigan Geol. Survey Ann. Rept., plate XII, scale 1:375,000. Newcombe, R. B., and Lindberg, G. D . , 1935, Glacial expression of structural features in Michigan: Am. Assoc. Petroleum Geologists Bull., v. 19, p. 1173-1191. Ogunbadejo, T. A., and Quigley, R. M . , 1974, Compaction of weathered clays near Sarnia, Ontario: Canadian Geotechnical J o u r . , v. 11, p. 642-647. Okko, M . , 1962, On the development of the first Salpausselka, west of Lahti: Comm. Geol. Finlande Bull. 202, 162 p. Prest, V. K . , 1958, Nomenclature of moraines and ice-flow features as applied to the glacial map of Canada: Geol. Survey Canada Paper 67-57, 32 p. 215 Prouty, C. E., 1975, An interpretation of major intrabasinal structuresMichigan Basin: Michigan Acad. Sci, Arts, Letters mimeographed abstract. Repo, R . , 1960, Jaamankangas-an ice-marginal feature in eastern Finland: Fennia, v. 84, 28 p. Rhodehamel, E. C . , 1951, An interpretation of the pre-Pleistocene geomorphology of a portion of the Saginaw Lowland (M.S. thesis): East Lansing, Michigan State Coll., 163 p. Rieck, R. L., 1972, Morphology, structure and formation of eskers with illustrations from Michigan and a bibliographical index to esker literature (M.A. thesis): Detroit, Wayne State Univ., 242 p. Russell, I. C . , and Leverett, F . , 1908 (revised and reprinted, 1915), Ann Arbor Folio, Michigan: U.S. Geol. Survey Geol. Atlaa, Folio 155, 15 p . Sherzer, W. H., 1917, Detroit Folio, Michigan: U.S. Geol. Survey Geol. Atlas, Folio 205, 22 p. Scott, I. D . , 1921, Inland lakes of Michigan: Michigan Geol. Biol. Survey Pub. 30, Geol. Ser. 25, 383 p. Shah, B. P., 1971, Evaluation of natural aggregates in Kalamazoo County and vicinity, Michigan (Ph.D. dissertation): East Lansing, Michigan State Univ., 192 p. Slawson, C. B., 1933, The jasper conglomerate, an index of drift dis­ persion: Jour. Geol., v. 41, p. 546-552. Soil Survey Staff, 1951, Soil survey manual: U.S. Dept. Agriculture Handbook 18. Stoelting, P. K. , 1970, A spatial analysis of the esker systems associ­ ated with the Kettle Moraine of southeastern Wisconsin (M.A. thesis): Milwaukee, Univ. of Wisconsin-Milwaukee, 220 p. Taylor, F. B., 1897, Moraines of recession and their significance in glacial theory: Jour. Geol., v. 5, p. 421-465. Thornbury, W. D., 1969, Principles of geomorphology (2nd ed.): New York, John Wiley & Sons, 594 p. Thwaites, F. T . , 1963, Outline of glacial geology: Ann Arbor, Edwards Bros., 143 p. Michigan, Vanlier, K. E . , Wood, W. W . , and Brunett, J . , 1973, Water-supply devel­ opment and management alternatives for Clinton, Eaton, and Ingham Counties, Michigan: U.S. Geol. Survey Water-Supply Paper 1969, 111 p. 216 VanWyckhouse, R. J . , 1966, A study of test borings from the Pleistocene of the southeastern Michigan glacial lake plain, Wayne County, Mich­ igan (M.S. thesis): Detroit, Wayne State Univ., 85 p. Veatch, J. 0., Trull, F. W . , and Porter, J. A., 1930, Soil survey of Jackson County, Michigan: U.S. Dept. Agriculture Soil Survey. Veatch, J. O, Wheeting, L. C., and Bauer, A., 1930, Soil survey of Washtenaw County, Michigan: U.S. Dept. Agriculture Soil Survey. Virkkala, K . , 1963, On ice-marginal features in southwestern Finland: Comm. Geol. Finlande Bull. 210, 76 p. Wayne, W. J . , 1963, Pleistocene formations in Indiana: Indiana Geol. Survey Bull. 25, 85 p. Wayne, W. J., and Zumberge, J. H . , 1965, Pleistocene geology of Indiana and Michigan, in Wright, H. E. Jr., and Frey, D. G., eds., The Quaternary of the United States: Princeton, N.J., Princeton Univ. Press, p. 63-84. Westgate, J. A., and Dreimanis, A., 1967, The Pleistocene sequence at Zorra, southwestern Ontario: Canadian Jour. Earth Sci., v. 4, p. 1127-1143. Wheeting, L. C., and Bergquist, S. G . , 1928, Soil Survey, Livingston County, Michigan: U.S. Dept. Agriculture Soil Survey. Willman, H. B . , and Frye, J. C., 1970, Pleistocene stratigraphy of Illinois: Illinois State Geol. Survey Bull. 94, 204 p. Wilson, J. T., 1939, Eskers north-east of Great Slave Lake: Royal Soc. Canada Trans., v. 33-4, p. 119-130. Wright, H. E., Jr., 1962, Role of the Wadena Lobe in the glaciation of Minnesota: Geol. Soc. America Bull., v. 73, p. 73-99. Zumberge, J. H . , 1960, Correlation of Wisconsin drifts in Illinois, Indiana, Michigan, and Ohio: Geol. Soc. America Bull., v. 71, p. 1177-1188. FIGURE 4. (ALTITUDES FEET METERS . 650 700 ,9 a I 213.4 — 750 80£ 22 8.6 2 4 3 .8 850 900 950 1000 1050 259.1 2 7 4 .3 2 8 9 .6 3 0 4 .8 3 2 0 .0 — BEDROC IN F E E T ABOVE M W ELL DATA SITE CONTOUR IN AREA W NUMEROUS W ELL CONTOUR IN AREA FEWER W E L L REC WEATHERED ZONES MATTER WITHIN D OVERLYING BEDRO CONTOUR INTERVAL 5 0 F o MILES K ILO M ETER S 4. BEDROCK SURFACE IS IN F E E t ABOVE MEAN SEA L E V E L) W ELL DATA SITE TIS ^CONTOUR IN AREA WITH NUMEROUS W E LL RECORDS T2S CONTOUR IN AREA WITH FEWER W E LL RECORDS T3S ^WEATHERED ZONES a ORGANIC M ATTER WITHIN DR IFT OVERLYING BEDROCK TOUR T4S RIE R2E zn CONTOURS MAY BE INTERVAL 5 0 F E E T (15.2 M) PARTIALLY ON RESISTANT T IL L 5 MILES 10 =1 SOURCES; SEE APPENDIX A a tlLO M E TE R S TABLES 2 ,3 ,4 . Hr • / • • I V / / ----------- N \ \ - \ \ \ X --N \ V V. ! i J . \ \ I • \ V J i i / * I v \ N 1 . I I \ I at "N • • / . r ^ / Vc*# r \ \ \ / • • r ?< y ----- - 8 5 0 - j s j \ / / \ ~y~ / /• . s \ \ A ■85o \ [ 7 \ / T ~ m / ' afra . LIVINGSTON 1 f v.800 \ § A3TTVA ^-•800 750 VALLEY L MA ^ __ .-800 - V 0 CD Q> / \ s \ / ■ ^ VV . \ / . s. X X ^ > ■ X * -* — •«- — 0^ s s V v v \ \ t \ 1 \ \ \ A 1 \ \ \ " \ \ A \ \ \ \ \ • J / / V ) \ \ / 1 1 i 1 1 / / £ 1 CD 1 \ \ / I / ( \ \ X > <" — -±1 ^ l / / / 9 ... ... r / / / W M v - / *. ■ / , ...... p / /: S r \ Vv \ s' / .- V X N V\\\ \\\ \ \\\ V \\ , \ o* ■■■ / / / ■ ■V ("~'”Oo§- ; \ r' / „ 1 / "k — \ a V Nw I I n - / / V / / I I 00 30 " “/ J ^ / A / / T3S / /-■•■ i v “T ~ \ I v / / / i / o ' m r~ \ / £ \ \ ^ \ s s Y ?5 q . / / ^ — — .L V \ -X N. N s s. / I I / A / \ ~7~ \ \ \ . \ / \ v' \ Jl / V 7 \ \ / / / I i / * / / R4E i ,£> & / / \ \ \ \ \ / • -T4S r-— \ Y t / Y I * s FIGURE 7 DRIF (IN F E E T l FE E T METERS 0 0 50 15.2 10 0 3 0 .5 150 4 5 .7 200 61.0 250 762 300 91.4 W E L L DATA SITE CONTOUR IN A R E A ! NUMEROUS W E LL CONTOUR IN AREA FEWER W E LL RE( W ELL W ITH BE DR 003 2 0 F E E T (6.1 M) 0 F | CONTOUR IN TER VA L 5 0 FI MILES o K IL O M E T E R S — J • / \ \ \ \ ✓N° < y l \ I f ( K* \ r 1 \ n ) \ \ MOO ' ' /■ ^ • N \ V \ A v - ✓ \ / V \ \ • 1 — ----- s ; .\0°"S v XUM 1 1 J L IV IN G S JACKSON CO. WASHT . •.V __ __ > • • /✓ \( Hoo— *S i \ \ • / vI \ / \ _ _ '. £ f • . . _Y f i\ i1• y • / 1 \ • \ •!• 1 1 \ J l ( \ \ \ • _- - v-s ‘— 150^ ! ' > / • / // «^206- x \1 \ \ \\.. / t XUM T IS s\ / * 1 . .. \ - I .. \• ft • \ \ // ■// • \ I i 1 / 1 1 1 \ \ 9 • L. . . . . \ s ( vk>w/ • \ \ \ i \I ; 1 • n I( I I- / V . ^ __ V Y s / . w J XUM wnx a C J 0 □ XUM XUM r R3E FIGURE 8. SEDIM Qsi PREDOMINANTLY GLACIOFLUVIAL SED [10 M] PER Q U A R TE R -S E C T IO N ) Qsh PREDOMINANTLY GLACIOFLUVIAL SEDI pO M] PER Q UAR TER -SECTIO N) Qti PREDOMINANTLY T IL L (BUT LOCALLY SEDIMENTS MAY BE PRESENT), L PER Q U A R TE R -S E C TIO N ) Qth PREDOMINANTLY T IL L (BUT LOCALLY SEDIMENTS MAY BE PRESENT), HI PER Q U A R TER -SEC TIO N ) Qp PALUDAL SEDIMENTS, FOR LOCATION PO STG LACIAL s LOW RELIEF OF GLACIOLACUSTRINE FLOODPLAIN SEDIMENT URE 8. SEDIMENTS AND RELIEF Y GLACIOFLUVIAL SEDIMENTS, LOW Q U A R TE R -S E C T IO N ) R E L IE F (LESS THAN Y GLACIOFLUVIAL SEDIM ENTS, HIGH R E L IE F (MORE T H A N Q UAR TER -SEC TIO N ) ABOUT 3 0 FEET ABOUT 3 0 F E E T T IL L (B U T LOCALLY CONSIDERABLE A M O U N TS OF G LA C IO FLU V IA L MAY BE PRESENT), LOW R E L IE F (LESS THAN ABOUT 3 0 F E E T [10 M] E R -S E C T IO N ) Y T IL L (B U T LO C A LLY CONSIDERABLE AMOUNTS OF G LA CIO FLU VIAL MAY BE PRESENT), HIGH RELIEF (MORE THAN ABOUT 3 0 F E E T [10 M] E R -S E C T IO N ) ENTS, LO W RELIEF OF GLACIOLACUSTRINE FLOODPLAIN SEDIMENTS SEDIM ENTS. NOT SHOWN SEE FIGURE 23 ABOUT ABOUT JLA C IO FLU V IA L BO F E E T [10 Mr] I l a c io f l u v ia l 10 F E E T [10 M] P3l Qsh Qth. Qsl jQsl Qtl Qsl Q sl Qsl Qsl * Q sl Qsl Q sl Qsh Qsl Qsl p \Q s h .Qsl Qth fls j Qth. / Qsh Qsh Q tl Qth m ‘Qsh Q sl Qsl Qsl Qsl Qsl Qsl Q sh\ QP Qth Qsh Qsh Qsh iSA Q tl Qp Qp Qsl Qsh Qsl Qsl Qsl Qsh Qsl Qsh Qs Qsh Qsh ^ iQsh Qtl Qsl Q tl Qsl Qsl Qsh Q th Qsl Qsl Qsh Qsl Q tl Qsh Qth Qs! Q tl Qsh Qth Qth Qsh West L. Qsl' Qsl Qth, Qsl Qsh Qsl Q tl Qsl; Qth Qsl .Qth Q tl Qsh Qsh V lIM Q tl d ^ M O R A IN E BOUNDARY T R A N S ITIO N A L MORAINE BOUNDARY i-1 . LINEAR DEPRESSIONS a RIDGES (INCLUDING BOUNDARY) Qsh Qsl- Qsl *V* Qsl Qsl Qp TIS L Qth SUR FICIAL DR IFT PROVENANCE CONTACT EXISTING LAKE INTERLOBATE MORAINIC XUM Center L XUM Qt! Qsl Qth .Qth Qsl Qsh Qsl Qsh Qsh Qsh Qsl Qth Q tl Qtl Qsh' Qsh Qsl Qshvptl Qsl Q tl Q sl Qsl Qsl. Qth Qtl, Cedar Qsl Qsl Qsl "Qsh [Qsh] Qsl Qth Qsh / Qtl Qsl Qsh Q tl Qsh Qsl Qsh Qsl Qsl Qtl Q tl Q tl /Qsl Qsh I Qsl Qsl Qth' Qsl ptr Qsl Qsl Qsh Qth Qsh Qsl Qth QsL /Qsl INTERLOBATE MORAINIC TRACT SAGINAW LOBE KALAMAZOO MORAINE _ HURON-ERIE LOBE GRASS LAKE PLAIN MISSISSINEWA MORAINE - Center L. iQsl Qsl * Qsh Q tl Qf I Qsh Qtfi) Qsl Qth] Qsh Qsl Qsh Qth Qsh, Qsl Qsh Qsl Qsl Qp R4E R3E FIGURE 32. SELEC MORAINE BOUNDARY — - TR A N SITIO N A L BOUNDARY * * * GEOMORPHIC CONTACT OF SAGINAW a H U R O N -E R IE LOBES O UT WASH FAN f T p C C HANNEL FILLING ITl m BREACHED OR NOTCHED RIDGE > > > ESKE CREV, OT CHAN WIT DEP HIGH DE RID BO K IL O Pleasant L 32. 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