THE CHARACTERIZATION AND INTERPRETATION. OF A COMPLEX SOIL LANDSCAPE IN SOUTH -'CENTRAL — MICHIGAN I Thesis for the Degree of MS. I MICHIGAN. STATE UNIVERSITY - TED M. ZOBECK ‘ ' 1976 WWWWWWW 3 1293 10376 1387 LIBRARY Michigan Scam: j: ummw ~ ABSTRACT THE CHARACTERIZATION AND INTERPRETATION OF A COMPLEX SOIL LANDSCAPE IN SOUTH-CENTRAL MICHIGAN BY Ted M. Zobeck The parent materials of most soils found in Michigan originate from depositional proceSses associated with the last glaciation. These processes are often quite complex and may result in what has been termed a complex soil landscape. This study characterizes the soils observed in a complex soil landscape and presents interpretations that suggest possible origins of this landscape. A discussion of the current concept of what soil classifiers map is followed by a review of the physio- graphic and lithologic considerations in Michigan. Gla- cial landforms similar to the research site have been inter- preted in several different ways. Several different theories are presented for comparison. The study area, a research facility operated by the Institute of Water Research, Michigan State University, is located in Section 6 of Alaiedon Township. Four hundred thirty observations to a depth of five feet yielded 66 soil series consisting of 30 different soil management groups and seven different parent material types. Two soil maps, one having medium intensity and another high intensity mapping units, were made for the research site. Series mapping units were found to be 28 and 47 percent homogeneous respectively for medium and high intensity mapping units. Soil management groups were 49 and 54.5 percent homogeneous and parent material types were 62.5 and 70.3 percent homogeneous respectively for medium and high intensity mapping units. Independent point- intercept transect observations were 15 and 12.5 percent in agreement respectively with medium and high intensity mapping units. These data fall within the range of homo- geneity found by Amos (1973) for an area one mile to the north. A 603 foot continuous line-transect excavation was ob- served and described. Thirteen soil series representing nine soil management groups and five parent material types were observed. Several interesting lithologic relationships were found in the excavation. Those present were: 1. An apparent inversion of topography having outwash at the crest of a hill and till in the adjacent swale. 2. Stratified-materials beneath a three foot mantle of till. 3. Stratification lines in 'till' material. 4. Outwash sands interfingering laterally with till. 5. Lacustrine clays overlying till. These sediments suggest that glacial ice stagnation and slow-downwasting were the major factors controlling parent materials deposition. The previous data and observations collectively formed a combination of characteristics of complex soil landscapes suggested as diagnostic criteria that may be used to predict their occurrence. Diagnostic features of complex soil landscapes resulting from stagnant ice areas, if they occur in combination, are as follows: 1. The area contains numerous closed depressions. 2. The area is often hummocky although subdued in ~ some areas. Slopes may vary from level to greater than 18 percent. 3. Inversions of topography are present having outwash derived soils on the uplands and till derived soils in the low- lands. 4. Tills may appear stratified. 5. Tills, lacustrine and outwash sediments may be interstratified. 6. Ice fracture fillings may be present. 7. All degrees of sorting may be present within very small areas and single map delineations. 8. Homogeneity of soil mapping units is quite low, often between 10 and 30 percent of the named soils. THE CHARACTERIZATION AND INTERPRETATION OF A COMPLEX SOIL LANDSCAPE IN SOUTH-CENTRAL MICHIGAN BY Ted M. Zobeck A THESIS Submitted to Michigan State University in partial fulfillment of the requirements . for the degree of MASTER OF SCIENCE Department of CrOp and Soil Sciences 1976 ACKNOWLEDGEMENTS The author wishes to express gratitude to Dr. E.P. Whiteside for his guidance and helpful suggestions as major advisor. Appreciation is also extended to Drs. D. L. Mokma, H. A. Winters, and C. Cress, for their helpful suggestions as members of my guidance committee. The author also wishes to thank Raymond Laurin for his help in many technical aspects of this study as well as W. Doucette, W. Warren, P. Denton, J. Flory, S. Brodnax and J. Pavlis for their supportive assistance in sampling and describing the study area. The author wishes to eXpress his sincere gratitude to the Institute of Water Research at Michigan State University for technical as well as financial support and to the Department of Crop and Soil Sciences for the assis- tantships that made this study possible. ii TABLE OF CONTENTS landscapes. ships Chapter I INTRODUCTION . . . . . . . . . II LITERATURE REVIEW . . . . . . . A. What soil classifiers map . . . . . B. Physiographic and lithologic considerations in Michigan . . . . C. Complexities in glacial 1. End moraines . . . 2. Overridden moraines 3. Stagnant ice areas D. Purpose of this study III. DESCRIPTION OF STUDY AREA . . . IV. METHODS OF STUDY AND PROCEDURES v. RESULTS . . . . . . . . . . . . VI. DISCUSSION . . . . . . . . . . A. Series mapping units . B. Soil management group mapping units . . . . . C. Parent material type mapping units . . . . . D. Transect data . . . . . E. Defining complex soil landscapes . F. Soil variability in a . continuous line-transect G. Soil lithologic relation in-& continuous line-transect . . . H. Local ice stagnation . I. Areal extent of ice stagnation . . J. Why the ice stagnated . K. Criteria for predicting the extent of a complex soil landscape . . . . VII. SUMMARY . . . . . . . . . . . . CONCLUSIONS . . . . . . . . . . iii Page 25 57 57 59 61 65 69 72 74 78 81 82 84 86 88 Chapter Page IX. LITERATURE CITED . . . . . . . . . . . . . . . 90 x. APPENDICES O O O O O O O O O O O O O O O O O O A Interrelationships of soil management groups . . . . . . . . . . . 95 B Soil series key for soils found on the I.W.R. Felton-Herron Creek wastewater project. . . . . . . . . . . 97 C Abbreviated legend for soils found on the medium and high intensity soil maps . . . . . . . . . . 99 D Description of soils analyzed for selected soil prOperties. . . . . . . .110 E Selected soil properties of five soils on the I.W.R. wastewater area . .117 F Supplementary point-intercept transect observations collected on the I.W.R. wastewater project. . . . . . . . . . .118 LIST OF TABLES Table. 1. 10. 11. Note-taking format used in sampling the I.W.R. spray irrigation area. . . . . . . . . . . . . . . Soil series observed on the Institute of Water Research spray irrigation area and their res- pective soil management group and parent material type in alphabetical order. . . . . . . . Series, percent homogeneity and percent of map area covered by each medium intensity soil mapping unit within irrigation area boundary . . . . . . . Series, percent homogeneity and percent of map area covered by each high intensity soil mapping unit 0 O O O O O O I O O O O O I O O O C O O O O 0 Summary of percent homogeneity of named series by Soil Management Group for medium intensity (A) and high intensity (B) soil mapping units. . . . . Summary of percent named parent material types for medium intensity (A) and high intensity (b) soil mapping units . . . . . . . . . . . . . . Homogeneity of three different kinds of mapping units for two mapping intensities. . . . . . . . . Comparison of point-intercept transect obser- vations with named soil series from high and medium intensity soil mapping units. . . . . . . . Comparison of point-intercept transect soil management group observations with soil manage- ment groups of named series from high and medium intensity soil mapping units. . . . . . . . Comparison of point-intercept transect parent material type observations with parent material types of named series from high and medium in- tensity soil mapping units . . . . . . . . . . . . Summary of percent agreement of point-intercept transect data with names of various kinds of landscape units. . . . . . . . . . . . . . . . . . Page . 21 Table ‘ Page 12 Length of line—transect excavation by soil series A. Summary of east-west excavation . . . 48 B. Summary of north-south excavation . . 48 13 Length of entire line-transect excavation by soil series . . . . . . . . . . . . . . . . 49 14 Summary of soil series observed by kinds of land- scape units in the 603 foot line-transect excavation . . . . . . . . . . . . . . . . . . 50 15 Summary of parent material types in the 603 foot line-transect excavation . . . . . . . . 50 16 Summary of soil management groups observed in the 603 foot line-transeCt excavation . . . 51 17 Summary of outwash parent material for medium and high intensity mapping units . . . 62 18 Relationships between parent material types and soil management groups among point- intercept transect observations from Tables 9 and 10 . . . . . . . . . . . . . . . 67 vi Figure 10 11 LIST OF FIGURES Location of study area in Alaiedon Township, Ingham County, Michigan . . . . . Distribution of spray irrigation lines on the Felton- Herron Creek watershed project of the Institute of Water Research, Michigan State University . . . . . . . . . . . . . Location of the 603 foot line-transect on the I.W.R. spray irrigation area . . . . Medium intensity soil map of the I.W.R. spray irrigation area (buffer strip included) . . . . . . . . . . . . . . . . . High intensity soil map of the I.W.R. spray irrigation area . . . . . . . . . . . Michigan Agricultural Experiment Station Map of I.W.R. spray irrigation area (buffer strip included) . . . . . . . . . . . . . . A portion of the continuous line-transect excavation having a relatively uniform sequence of horizons . . . . . . . . . . . . A portion of the continuous line-transect excavation having complex, discontinuous sequences of horizons . . . . . . . . . . . Section of the line-transect showing three profiles that illustrate an inversion of t0pography . . . . . . . . . . . . . . . Till overlying stratified materials . . . . An area where till interfingers laterally with outwash . . . . . . . . . . . . . . . . vii Page 16 19 23 31 33 35 52 53 55 56 56 I . INTRODUCTION One of the most important jobs of a soil classifier is the characterization of the soil maps that he or she makes. Soil maps made in different areas may not be char- acterized similarly. The factors important in the formation of soils (organisms, climate, parent material, relief and time) may be different for each area and in fact for each different soil. These soil formation factors will affect the make-up of soil mapping units. To adequately characterize a soil map the soil classifier must have an appreciation of the processes associated with the formation of the soils in the region mapped. In characterizing a soil map the soil classifier des- cribes the soils making up individual mapping units. Map- ping units will normally contain many inclusions of soils not in the name. The inclusions found in map units may be related to soil classifiers themselves, or they may be inherent in the system used in soil classification (Amos, 1973). If the mapping legend does not adequately define the allowable number of inclusions found in mapping units, incorrect map units will result. As recently as 25 years ago soil map units were assumed to be quite uniform with only minor inclusions of other soils in them (Soil Survey Staff, 1951). Only recently have soil scientists begun to accept the idea that soil map units are usually more complex and commonly contain only 50 to 60 percent of the soil in the name (Amos, 1973; Whiteside, 1975; also see Soil Survey Staff, 1967). Have we gone far enough? Could some soil landscapes be found to be even less homogeneous? Certainly many areas may be even less homogeneous than suggested above. Amos (1973) notes an area that is quite variable. When soil maps of the area are compared to independent observations less than 30 percent agreement with named series was found. These kinds of areas may be called complex soil land- scapes. The purpose of this study was to characterize a com- plex soil landscape and describe the processes involved in its formation. Two soil Imuxs were made of the landscape, one having medium intensity and the other high inten- sity mapping units. These maps were compared by various landscape mapping units such as series, soil management quup and parent material type. In addition independent soil observations were compared to the two soil maps as well as to a map completed under the direction of the Michigan Agricultural Experiment Station in 1965. The complexity of this soils landscape is the resulgmi of certain specific soil forming and geologic processes. These processes were investigated by observation of a con- tinuous line-transect excavation made on the study site. The soils and depositional sequences observed are described and interpretations suggest the processes that were res- ponsible for this complex soil landscape. In addition diagnostic features are suggested to assist soil classi- fiers in recognizing these complex soil landscapes. II . LITERATURE REVIEW A. What soil classifiers map. "The scientist who makes a soil survey examines the soils in a field, classifies them, and sketches their boun- daries on an aerial photograph” (Overton, et 21., 1959). This succinct description of the process of making a soil survey and map encapsulates a lengthy and technical task in- volving aspects of geology, geophysics, chemistry, carto- graphy, and geography, in addition to soil science. A soil map has a number of uses such as providing soils information for use in regional planning and zoning, planning for septic tanks and other sewage disposal sys- tems, agricultural planning, planning for highways, management of recreation and wildlife areas, and tax ad- justments (Robinson, et 31., 1955; Olson, 1966). In order to distinguish one soil from another it is necessary to classify soils in some way. Many methods have been applied to classify soils. These methods may be di— vided into two major groups. One uses broad simplification through application of a single property or a small group of definite properties. A second method bases the classi- fication system on consideration of all properties of the soil body collectively. The former system is considered artificial and the latter a natural genetic classification system (Kubiena, 1958). Kubiena points out that both sys— tems are possible in classifying soils. Others prefer the analytical (artificial) approach (Leeper, 1956). Earlier concepts of soil classification are discussed by Simonson (1952). In classifying soils we implicitly assume that a "soil individual" exists. The ultimate soil individual is the pedon (Cline, 1949). A pedon is a three-dimensional body the same thickness as the genetic soil profile (or the depth of observation) with horizontal dimensions just large enough for observation and sampling. A pedon is the smallest volume that can be called "a soil" (Soil Survey Staff, 1960). The soil individuals that form units in the taxonomic system developed in the United States for classiu fying soils are called polypedons (Buol, gt gt., 1973). The polypedon usually conSists of a number of contiguous pedons, all falling within the defined range of a single soil series (Johnson, 1963). A single naturally occurring soil individual or soil body may be best described by the polypedon. —These soil individuals are bodies whose boun- daries can be recognized in the field (Cline, 1963). Do soil sdientists actually map these kinds of bodies in the field? 3 The collection of soil bodies of a specific kind that are identified and mapped by soil scientists in the field is a soil map unit. The existence of defined soil map units is a prerequisite to the mapping of soils in detail (Marbut, 1921). The need to adequately define and under- stand soil map units is great. The soil scientist must be able to form a mental construct of a soil map unit in his or her mind. It is impossible to delineate a body without some idea of the nature of that body. A soil map unit does not consist of one pedon or even of one polypedon. The soil map unit is commonly a variable unit made up of many different soil individuals. The variability of soil map units has been described by many workers (Waynick, 1918; Bushnell, 1928; Wilding, 1965; Mahjoory and Whiteside, 1975; McCormack and Wilding, 1969; Beery and Whiteside, 1970). A soil map unit, or more pre- cisely, a soil landscape unit is a spacial aggregate of soil individuals (Knox, 1965). The lateral boundaries of this unit are determined by the geographic pattern of variation in soil characteristics. It is not assumed that all indivi- dual pedons are alike. The main assumption is that natural soil units occur in certain positions in the landscape. When these landscape positions have been influenced by the same soil formation processes the same soil landscape units will occur. Physiographic conceptions are a great aid in recognizing significant relationships between the topo- graphic forms and related soil landscape units. As long ago as 1928, soil mapping was possible only because a person could examine a profile at one point and successfully predict its occurrence at another point where surface indications were similar (Bushnell, 1928). B. Physiographic and Lithologic Considerations in Michigan In order to understand the types of soil landscape units expected in Michigan one must have a thorough know- ledge of glacial processes. WCurrent soil formation in south-central Michigan began after the retreat of the re- gion's most recent glacial advance, approximately 13,500— l6,000 years B.P. (Dorr and Eschman, 1970). Sediments de- posited by glacial activity make up the parent material as well as the associated landforms or topography. Due to the relatively short time since soil formation began, the type of sediment deposited by the glacier is often a controlling factor in soil genesis and classification. An understanding of the glacial processes involved in parent material deposition will lead to a better understanding of the distribution and formation of the soils in Michigan. Glacial processes account for much of the variability observed in soil map units in Michigan. This variability has been shown to be quite large. Recent studies in Michi- gan have shown that medium intensity soil mapping units are composed 32764 percent of the named series (Mahjoory and Whiteside, 1975; Beery and Whiteside, 1970). One study found units of even greater complexity having composi- tions 0-78 percent of the named series (Amos, 1973). The 'map units in most of the counties studied in Michigan average 50-60 percent of the named series (Whiteside, 1975). These data indicate that in some glacial areas inde- pendent observation correlated quite well with the mapping unit name. Yet in other areas independent observations show very poor correlation. It is recognized that soil classifiers do differ in their ability to correctly delineate soil mapping units (Amos, 1973). Accurate soil identification is needed to understand soil properties (Kellogg, 1966). Much of the variability in soil mapping units cited earlier is more related to complexities in the soils present than to pro- ficiency of soil classifiers, per se. Guidelines established for naming series and mapping units and the amount of inclusions,of other soils that may be present in them, were made with the hope of delineating all possible soil types. In an older system as much as 15 percent of a soil type or phase as mapped could be inclu- sions of other soils (Soil Survey Staff, 1951). The newest revision is more liberal and sets the limit at 25 percent for closely similar series before they are recog- nized in the name (Soil Survey Staff, 1967). A unit with more than one series each making up at least 25 percent of the unit is termed a 'complex.' A maximum of three soil components may be combined in forming names of complexes. In many areas these guidelines are not adequate to define the mapping units observed (Amos, 1973). It would be helpful if areas that strongly deviate from the suggested allowable mapping unit inclusions could be identified prior to mapping. Often these complex areas are not identified due to incomplete or nonexistent transect data. If transect data does become available it does so after the area has already been mapped. If some criteria could be established to help recognize unusually complex areas it might be possi- ble to invoke a modified set of mapping unit guidelines (as yet to be devised). The inadequacy of the present guidelines in describing some soils landscapes points out the necessity for some kind of change. C. Complexities in Glacial Landscapes. As previously noted, the sediments in Michigan are mainly derived from processes associated with the most re- cent glaciation. Many different landforms are made up of two general types of glacial deposits, till and outwash (Dorr, and Eschman, 1970). Till is that material deposited directly by the glacier. Outwash is material deposited by meltwater from7upon, or within, the receding ice mass. There are a great number of landforms associated with both types of deposits as well as with combinations of the two together. This study is concerned with processes that may be responsible for the formation of complex soil landscapes. The type of soil landscape of special concern are hummocky areas where both outwash and till deposits occur together and separately within short distances. Similar landscape types may develop in several different ways. 1. Bad moraines End moraines vary from smooth gently undulating surfaces to sharply irregular surfaces marked by knolls, hummocks 10 and closed depressions (Flint, 1955; Flint, 1971). T111 and outwash are often intermingled in these deposits. The lower part of the moraine may be eroded by glaciofluvio meltwater activity or partially buried by meltwater depo- sits (Henderson, 1959; Embleton and King, 1968). End moraines often display a lobate form and are associated with kames and eskers (Henderson, 1959). 2. Overridden moraines Overridden moraines may also have a similar appearance. Overridden moraines studied by Totten (1969) have a subdued or drowned appearance and appear in many places only as a chain of knolls. These areas were formerly mapped as' ground moraines. The surficial deposits consist of till units and associated silt, sand and gravel. Quite often soft laminated sediments such as lake clays will be highly faulted and distorted after being overridden by a later glacial advance (Huddart, 1971). Some structures such as kames may be flattened and their outwash sediments mixed with the till from the ice sheet (Sangrey, 1970). Totten (1969) suggested criteria for tracing overridden end mOraines in north-central Ohio using such information as hummocky topography, mottled pattern as seen on an aerial photo- graph, green overprint on U.S.C.S. quadrangle maps (indi- cating woodlots), and rectangular drained patterns. In describing overridden end moraines in north-eastern Ohio, White (1962) noted that much of the volume of material in 11 the moraines studied were derived from an earlier glacia- tion. The latest till layer found ranged from two to ten feet thick. 3. Stagnant ice areas A final type of landformrthat closely correlated with 2” a complex soil landscape originated from processes asso- ciated with stagnant or nearly stagnant glacial ice. According to Flint (1929), dead or stagnant ice resulted from total loss of forward motion of an ice sheet while at its maximum extent. Nunataks, mountain peaks protruding through the ice-sheet, may have shaded large areas and caused dif- ferential ice melt. These shaded areas may have preserved fields of stagnant ice for long periods of time after the recession of the rest Of the ice-sheet (Flint, 1929). Higher eleva- tions far from the ice source tend to produce stagnant ice areas. As the ice thinned, it became unable to surmount relief barriers (Stalker, 1960; Holmssen, 1963). Areas near the marginal zones of large ice-sheets were probably never as vigorous as those near the source. Consequently, even relatively low hills far from the ice source may have caused stagnation. Seismic exploration beneath stagnating ice on the present day Malaspina Glacier indicate that the ground surface rises several hundred feet toward the terminus (Embleton and King, 1968). Eskers form in several ways and are often associated ‘with stagnant ice areas (Embleton and King, 1968; Flint, 1971). The origin of eskers as subglacial stfiém deposits 9 12 was suggested as long ago as 1884 (Shaler, 1884). A bit later Hershey (1897) noted that eskers must have formed as the ice rapidly backwasted since they were not destroyed by active ice movement. Some eskers may terminate in proglacial lakes or ponds and exhibit deltaic formations along their length (Shaler, 1884; Hershey, 1897). Other eskers have been interpreted as forming in englacial tunnels (Alden, 1924) or superglacial stream valleys (Sproule,l939). Areal extent of ice stagnation may not necessarily be large if the glacier is rapidly backwasting. The main por- tion of an ice mass may be active except for a narrow ter- minal zone. Deadfice moraines and related landforms have been described by many workers (Tarr, 1909; Flint, 1955; Gravenor and Kupsch, 1959; Kay, 1960; Winters, 1961; Clayton, 1967; Parizek, 1969; Flint, 1971). Dead-ice moraines go by many names. The term 'ablation moraine' was first proposed by Tarr (1909). He applied the term to moraines in initial superglacial position as well as the same moraine after‘the underlying ice melted out. The term is now more closely assOciated with the former defini- tion. Collapsed-superglacial-till topography, stagnation moraine, disintegration moraine, hummocky disintegration moraine, hummocky moraine, collapse moraine or ablation moraine have all been coined to describe dead-ice moraines. Dead-ice moraines vary in relief from apronounced_nelief 13 of several hundred feet to a subdued relief of five to ten feet. Inversions of topography are common. Depending upon the influence of past live ice the resulting topography may or may not appear to be ordered (Gravenor and Kupsch, 1959). Perched lacustrine sediments may be present due to past super-glacial lakes (Winters, 1961). Wastage of the stagnant ice proceeds from both the base and the surface (Kaye, 1960; Florin and Wright, 1969) leading to the formation of Tlow tills . Deposits become incorporated in the ice when in/the active phase/gs the ice thrusts upward under compressive flow. Nye (1952) des- cribed factors responsible for compressive flow. As inter- stitial ice melts the sediments uncovered become saturated and start to flow. The 'flow tills' exhibited some crude sorting (Harrison, 1957). Flow tills may overlie fluvial sands and gravels or become interstratified with them (Hartshorn, 1958). Modern day analogues to these processes have been ob- served for many years. An esker currently forming near the snout of the Boverbreen Glacier in Norway has been de- scribed by Lewis (1949). This esker emerges from beneath a rapidly retreating ice front. Stokes (1958) described an esker-like feature extending out from the retreating Svartisen ice-cap in north Norway. This esker extends onto adjacent dry land in front of the ice. Ice in the vicinity is almost stagnant. Tarr and Martin (1914) de— scribed 1ow-partly forested morainic hills on the Malaspina l4 Glacier in southern Alaska. A narrow 450 foot belt of flow till on the Barnes ice cap has been described. As the ice receded the till insulated the underlying ice and a trough developed behind it. It is believed that by this process it will eventually become isolated from more active ice (Goldthwait, 1959). Areas on the Malaspina and Bering glaciers have stagnant terminal zones a few miles in width that show sediment dragged up from the base along thrust planes. Drift thicknesses on the Martin River Glacier is ten to twenty feet thick (Clayton, 1967). Addi- tional description of flow tills on stagnant ice have been reported on the Vestspitsbergen and Svalbard glaciers (Boulton, 1968; Boulton, 1970). D. Purpose of This Study The apparent heterogeneity of soils in Michigan has been described. It was suggested that the glacial deposi— tional processes may account for the heterogeneity observed. Several types of similar landscapes that may produce a variety of sediment types have been suggested. A soil inventory, conducted on Michigan State University property presently managed by the Institute of Water Research, re- sulted in the observations of a wide variety of soils. This study characterizes the soils in this complex soil landscape and presents evidence and suggests interpretations that help account for the observed variability. Field criteria to facilitate the recognition of these types of areas prior to soil mapping are suggested. III. DESCRIPTION OF STUDY AREA The study area is located on a 60 hectare (150 acre) tract in Alaiedon Township, Ingham County (8 172, Sec. 6, T.3.N. - R.1.W.) (Figure l). The area is currently owned by M.S.U. and under the management of the Institute of Water Research at M.S.U. The Institute has designated the area as a spray irrigation area for its Felton-Herron Creek Pilot Watershed Study (I.W.R., 1974). The data col- lected for this thesis were, in part, the results of a soil inventory designed to characterize, sample and map the soils preSent on the irrigation site. The site is composed of two dominant types of vege- tation, trees and oldfield herbaceous species. In the past, the oldfield areas were cleared and utilized as cropped fields or pastures. These abandoned fields are currently dominated by herbaceous species, principally cool-season grasses and warm-season perennial dicots such as Aster and Solidagg (aster and goldenrod, respectively) (I.W.R., 1974).. The forest land, Allen and Lott woodlots, consist of sugar maple, beech, elm, red maple and basswood (I.W.R., 1974). The landscape is hummocky, which might account for the presence of the woodlot. Slopes range from zero to nineteen percent and are often short and steep or 15 ‘ I k ‘7‘, L” If: .‘1. Figure 1. Location of study area in Alaiedon Township, Ingham County, Michigan. 17 irregular in cross section. Maximum local relief is appro- ximately fifty feet. Numerous closed depressions are present. This landform was originally mapped by Leverett (1917) as a till plain or ground moraine. This map unit was shown as a ground moraine when remapped by Helen Martin (1955) (Figure 1). A ground moraine consists of glacial till deposited in sheets over the landscape without the formation of conspicuous ridges (Thornbury, 1960). The depth of the till may be quite deep, often over 100 feet. The depth of till near the research site is appro- ximately 80 feet as indicated by well-log data (Michigan Department of Natural Resources, 1976). IV. METHODS OF STUDY AND PROCEDURES A total of 430 soil profiles were observed,using a bucket auger,to a depth of five feet. Ninety-five of the observations used to characterize the area were collected by Dr. Delbert Mokma* for other research purposes. To facilitate accurate estimates of observation location, sample sites were located in reference to irrigation sprink- ler heads located on the site (Figure 2). At each observa- tion location the following data was collected: 1. Number of observation 2. Location Example: 10 A 5 refers to valve 10, irrigation line A, sprinkler head number 5. 3. Natural drainage 4. Horizons observed 5. Depth in inches for each horizon 6. Samples collected (S) 7. Texture 8. Classification according to the Soil Taxonomy, 1973 9. Regional slope (general slope) *Assistant Professor, Department of Crop and Soil Sciences, Michigan State University 18 I; O..- 3-: .‘Q.! . I. .‘I ‘. -_-----------4 r--— .— 7:3 I “7 .14 av" )Isnlooot. A LEI. memcnm m. Uumnnwvcnuop om mpnmw hmnwmmneos prnm on n50 mmHnoplmonnoo nnmmrn canonmrmd uncumnn on «so Humnuncnm on canon ”bananas. zunrwmm: mnmno caucou mmwe poocmm whalmq x omuov NU HH . mm mmon .mmm usmnam a x oanmm Ho we macaw .m mchm smao go x mmuHH pmm mxmsmz mmgumm msflsmcou meow am Halm md 224m manpsHmmm gamma coflumowmamwmau m\a us on a x mno ma a: ma on men mmuoz muguxme xm Amococflv :onuom mmmcflmno cowumooq .oz Hmcoflumopd Symon .monm cofiummflnuw mzH man ocflamamm CH poms quHOM mewxmulmuoz .H mange 22 a depth of five feet. Four hundred three feet occurred in an east-west direction in a variable outwash unit. A 200 foot length, located in a more homogeneous unit, formed a T-leg to the south of the E-W excavation (Figure 3). The soils observed were classified according to the Soil Taxonomy and the series were recorded along the entire length of the trench. Selected soils observed in the trench were sampled and analyzed for bulk density, saturated hydraulic conductivity, permeability, and percent total pore space. Bulk density measurements were determined by the core method described by Blake (1965). Saturated hydraulic conductivity followed the constant-head method prescribed by Klute (1965). The conversion from saturated hydraulic conductivity to permea— bility was made by the use of the equation: k = Kn/pg where K is the saturated hydraulic conductivity, n the coefficient Of ViSCOSitY: P the density of water and 9 the force of gravity (Klute, 1965). Total porosity was calculated by averaging the values determined by the difference method and the bulk density/particle density methods (Vomocil, 1965). Ten samples were averaged for the A and upper B hori- zons of each profile. Six samples were averaged for the lower B and C horizons of each profile. Thornburn and Larsen (1959) illustrated that five soil samples will show statistically significant differences in soil physical pro- perties. Ten were allowed in the upper three feet or so Valve 4 Valve 6 _l——r—'J _ L—E—J .A B C D 1 0 Sprinkler Head :::::: Line - transect %‘ 120 M 4‘4 Figure 3. Location of the 603 foot line - transect on the I.W.R. spray irrigation area. 24 to reduce any extreme variation that might have been due to soil fauna or flora activity. V . RESULTS Sixty-six soil series consisting of thirty different soil management groups and seven different parent material types were observed on the entire research site (Table 2). A total of three different soil groupings were studied; soil series, soil management groups and parent material types. "A soil series is a group of soils having soil horizons similar in differentiating characteristics and arrangement in the soil profile, except for the texture of the surface soil, and developed from a particular type of parent material." (Soil Survey Staff, 1951). Soil manage- ment groups are composed of soil series that have similar dominant profile textures and natural drainage classes (Appendix A) (Mokma, gt gl.,1974). A parent material type is a group of soil series consisting of materials of simi- lar origin and mode of deposition. Since each series can be classified as some specific soil management group and parent material type2transfer from the series to these more general groups is quite simple although the reverse may not be true. The two mapping intensities studied were referred to as medium and high intensities. A medium mapping intensity was used to construct a map similar to those made currently by the National C00perative Soil Survey in Michigan. Only soils and map units recognized in the current Ingham County muagpoammm Danae .ofimme .pmxfiE .>EmoHumcflm mmamonammm ofimaa .owmmE .pwxflE .mEmoHlmcwm mumfinmmmflpmz Gamma .owmoE .owsm mmaosvounoo owned .owmme .poxfie .wpcmm nm>o .xEmoHumcfim mmamosammm oflmwe .ofimmE .Umxwe .mfimoHlmmumoo mmampSHmmm vammh .owwmfi .voxfiE .>Emoalmcwm meMpSHmmm Danae .oflme .pwxfle .mEmOHnmcwm mHHonwmammm onxB .oaon .poxfle .AUCMm mHHogvadmm ofldme .owme .poxfle .>Emofiummnmoo muaopoammm oflmxa .oflmmE .pwxfle .mpamm um>o wsmoflnwcflm mmampsammm oflamfi .oflmmfi .pmxfie .mfimoHummumoo mmampsammm owmme .oflmofi .pwaE .mEmoHlmmumoo muauuonouusm gamma .pmxwe .mpcmw nw>o amxmao Aoflmmev .mmamsgmucoo Owned .oflwwE .pmxHE .wemolecwu mHHoomemmm oflmhe .ofime .ooxfie .mfimoHlmmumoo mmamowmncoo UHHHopD .onwE .pwxflfi .mfimoHumcfim mHHogvmammm cammh .oflwmfi .wmxflfi .afimoHnmcfim munmEHMmmeu camad .OAmmE .pmxfle maaongHmmm owucosvm>sHm .owwme .pmxfle .SEonImmuwoo mmappgammm oaggd .oflmma .pmxflfi .wcwm 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.oflme .pmxfle .wsonnomumoo mwampsammm gamma .oflmmE .pwxwe .MEmolecHw mmampsammm cacwud .owmmE .pmwa .mEmoa muamggmucoo UMHHOUD .OAmmE .pwxflfi .mEmoHnmcfiu mmamsgmucoo owaaoos .oamme poxfiE .mpcmm um>o >EmoHImcfim mmampcammm owuonowmoHo .oflmwe .pmxwe .hEmoHumcflm mwammuamwm oflamomwm .oflmmE .pmxfie .mHMOalmcflw mMHMpuHmmm owaflonw4 .ofimwfi .pwaE .wfimoHnmcflm muawggmamwm ofiumm .owmofi .pwomcoc .pmxwe .>Emofiuomumoo mmamvsHQmm camxe .owmme .pmxfie .mEmoanwcfim mmagpsammm owmxe .owme .pwxflfi .>EmoH|mcwm mmagpnammm uwaaouw4 .Uflmme .pwxflfi .meOHIOCAm . uwflummmfipmz Uwucmsvw>sam .OAmoE .owso mmawpnammm meha .oflmmE .pmxwfi .hEmoHlmc«w Nansen Hgom mgwuumgomn Hmw>saad Hafluuuw>o cmwzuso cmm3ugo mcwuumsomq Haas Haas Haas nmmsuso Haw» umpo cwmzugo Haflu uw>o cmm3uso nmmsuso nmmsuso nmmzuso cmmsuso Haws Haw» uo>o cmm3uso Hawu nw>o cmmzuno cmmzuso Hawa Haflu no>o Smwsuso Hflae mcwuumgomq Hawa HHfiB Haws Hmw>sHH4 Haw» um>o nmozuno .B.Z.m muum.~ ONIQ nm\v om\m mm.H om.~ nm.m Mm.N av am\m m~\m as mm.~ mm mIEm mm.~ mm\v n~\m nm\m om.N n~\m am mnom nm.N Mm.N Dm.N 02nd um\m .U.2.m +c0mmwm mamonm mmugumnmm mzmnmw gawHHwbmwahmm *«ucMAum> om .mmflwnflm «eucmaum> omkm mmauowm +mmaunum cannon +0mm030 amkmuu +ofimunmo swaxuo mHHH>xmo monflx dawns MOUOE +muoumumz +couumxumz +wuumflumx nuoomx mxuoq +c0mumq usagum> anew “moans Hmvvwm +mgnnnm aoumumm mHHwbaamvcmM mowumm Hwow pongwugou .N manna .mnma .pcmmmq >m>ngm HHOm wucsoo EmcmcH may cw pmuwcmoomn me0m + .mnma .hnmncmn .cmmwcowz cw poms mmfiuwm Hwom mo cofiumowmwmmmao can ca mow>uom c0wum>nwmnoo aflom gnu an wmumua non mmwnmm «a .cmmflzowz aw m>w4omcw maucmuuno mmflnwm « mHHonwmfimnm oflmma .owmme .poxfls .mEmoHlmcflm mmampsammm 0am>9 .oflmme .poxHE .hEmoHIOCAM m wammm ownaougm .ofime .pmxHE .xEmoHlmmnmoo mmwmuammm oeun6flwmfifimmm .owmmd .pwxflfi .xpcmm mmaMpuHQmm cauwm .oflmmfi .powa .%EmoH|wch mmampusmm owucmufimmm .oflmmfi .pmxHE .xpcmm ”Hoswmflmmm owucwswm>gam .oflme .pmxfiE .xEmoHnmcflw mmamsgmunoo Owned oflmmE .pwwa .>Em0aumcwm HwEmh Hwom mezuoo nmmzugo um>o gage nmm3ugo nmmzuso onwuumsomg nmmzugo HmH>SHH4 zmmzuso .pmsgaucou Ucmgummz «mxmzmz “momma +UHOmumnB maoomsa +mxgwmm +Cm0Hw «afiummam mmflumm Hfiom .N magma 29 soil survey legend were delineated. Areas no smaller than three acres are shown. Ordinarily at this intensity obser- vations are made about every five to ten acres. These ob- servations along with observations of lepe, erosion, vege- tation, geologic formation, and land use enable the soil classifier to construct a medium intensity soil map (Figure 4). A high intensity map was also prepared. This map shows areas as small as one and one-third acres in size. All soil series observed and their usual mapping subdivi- sions were permitted in this legend (Figure 5). A map constructed by Michigan Agricultural Experiment Station personnel in 1965 is included for comparison (Figure 6). A soil series key by parent material and natural drainage, as well as series descriptions are located in Appendix B and Appendix C, respectively. The names, percent homogeneity of series and percent area of medium and high intensity soil map units may be found in Tables 3 and 4, respectively. Tables 5 and 6 summarize the percent homogeneity of named soils by soil management groups and parent material tYpes, respectively, for both medium and high intensity soil mapping units. Homogeneity is defined as the percentage of all observations within a mapping unit that are of the named kind (series, soil management group, or parent material type). 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Hnnwmmnwop mum». Tmm image: .28 wocaaoQ m mm mp _ b W032: mood Rood Phillips Sworwom: wonwocwncnow mapmnwambn mnmnwoa Sup bemoan 39m MKBUOH 3mm Gown zmam 3mm MKBUOH 3am dawn zmam H >.w wHooxmno: Hows m v.w gonna Homaw mono m w.o . szBH Homa Ho wowmn mmpow Home w 0.0 sz3H mmpmw Homa HH w.n mpwpwm HomBK mmsm A v.w nogoHmm m.w. .zlJIleIHpanBHnwmgd mwnmmg mwmcnm o. Kunrummb >mNananan mxoonnaogn mnmnHog zap 0m H.€.w. «anew Hnnwmmnuo: anon Accmmon manuv wgnwcaoav. m._.>._.m Ii< .mm \3/ 5m s> mm as + CIVOU SdI'I'IIHd 9201:... _ nope z - I 36 Table 3. Series, percent homogeneity and percent of map area covered by each medium intensity soil mapping unit within irrigation area boundary. ’Seers in *Map TESHomogeneity $‘5f‘MEE—_ Soil Map Units Symbol of Series (Observed) ‘ Covered Marlette 33 B 43.2 24.7 Marlette 33 C 51.2 15.9 Capac 18 A 0 7.7 Colwood complex 17 A 0 3.2 Sebewa 37 A 19.6 6.8 Boyer 12 B 6.4 4.1 Boyer 12 C 0 2.1 Owosso-Marlette 36 B 44 6.2 Riddles-Hillsdale 25 B 0 6.9 Riddles-Hillsdale 25 C 12.5 5.0 Lamson-Colwood 44 A 53.8 3.6 Matherton 29 A 57.1 1.9 Gilford 23 A 5.3 7.6 Sisson 39 B 66.7 1.4 Teasdale 50 B 0 2.6 Boyer-Spinks 11 C 0 ’11 Metamora-Capac , 30 B 0 .11 15 units . Average 28.1 100.02 37 Table 4. Series, percent homogeneity and percent of map'area covered by each high intensity mapping unit. SeriesSIn Map % Homogeneity 8 of Map Soil Map Units Symtgl of Series (Observed) Covered Brookston 1.Av 46.7 5.5 Miami-Marlette 213 47.6 22.0 Miami-Marlette 2C2 53.1 20.0 Conover 3 A 51.9 4.6 Fox 4 B 43.8 3.0 Granby 5 B 37.5 1.1 Barry 5 A 100 1.8 Barry 5 B 31.2 4.4 Corunna 7.A 50.0 0.6 Westland 8 A 44.4 1.1 Kalamazoo .9CI 21.4 3.0 Owosso 10 B 52.4 5.2 Owosso 10C: 66.7 0.4 Metea 11(2 100 1.8 Matherton 13.A 57.1 1.7 Hillsdale-Dryden 14 B 50.0 4.3 Hillsdale-Dryden 14(2 40.0 7.1 Lamson. 15 A 66.7 1.2 Sisson 16‘B 100 0.6 Kidder 17 B 38.9 1.5 Sebewa 18.A 46.1 2.6 Colwood 19.A 10 5.0 Spinks _122\ 33.3 1.6 23 units Average 47.3 100.2 38 Table 5. Summary of percent homogeneity of named series by Soil Management Group for medium intensity (A) and high intensity (B) soil mapping units. A. Medium Intensity Soil Mapping Units Soil Management Group Homogeneity by % of Map of Named Series Soil-Management Group _§gyered 2.5a 61.6 42.0 2.5b 46.9 7.7 2.5c-s 75.0 3.2 3b 18.2 2.6 4a 16.7 6.2 4c ' 5.3 7.6 2.5a - 3/2a 43.9 6.2 2.5c-s- 3c-s 61.5 3.6 3/5b ‘57.1 1.9 3/5c 19.6 6.8 11 units Average 49.1 Total 99.8 B. High Intensity Soil Mapping Units “‘— —-— _-—-—' Soil Management Group Homogeneity by % of Map of Named Series Soil Management Group Covered 2.5a 62.9 44.0 2.5b 55.6 4.6 2.5c 50.0 11.7 3a 43.9 11.4 Be 31.7 7.3 4a 33.3 1.6 So 37.5 1.1 3/2a 54.2 5.7 3/2c 50.0 0.6 3/5a 46.7 5.9 3/5b 57.1 1.7 3/5c 46.1 2.6 4égg__ 100 1.9 13 units Average 54.5 Total 100. 39 Table 6. Summary of percent homogeneity of names’series by Parent V Material Type for medium intensity (A) and high intensity (B) soil mapping units. A. Medium Intensity Mapping Units % Homogeneity by % of Map Parent Material Type1 Parent Material Type Covered Till 65.1 60.3 Outwash ' 60.9 25.0 Outwash over Till _84 6.2 Lacustrine 34.8 8.2 4 units Average 62.5 Total 99.7 B. High Intensity Mapping Units % Homogeneity by % of Map Parent Material Type 'Parent Material Type Covered Till 68.5 71.2 Outwash 90.8 14.0 Outwash over Till 81.6 8.1 Lacustrine 34.5 6.7 4 units Average 70.3 Total 100.0 . lLacustrine over till, till over outwash observations on organic and alluvial parent material were not numerous enough to be mappable units. 40 Table 7 summarizes the homogeneity of the three different kinds of landscape units for medium and high intensity soil mapping units. Table 7. Homogeneity of three different kinds of mapping units for two mapping intensities. Homogeneity for Homogeneity for ‘Kind of Medium Intensity High Intensity Mapping Units Mapping Units Mapping Units Series 28.1 47.3 Soil Management Groups 49.1 ‘ 54.5 Parent Material Types 62.5 70.3 A total of forty point-intercept transect observations were also recorded. Table 8 compares the named soil series to the observed soil series for both medium and high inten- sities map units. Soil management groups and parent material types are compared in a similar fashion in Tables 9 and 10, respectively. Transect data are summaried in Table 11. Percent agreement of natural drainage was found by the use of Table 9. The soil series observed in the line-transect excava- tion are listed in Tables 12 and 13. Soils that have the same soil management group as the named soil unit are considered similar to the soil by the same name. A summary of the soil groups observed in the line-transect appears in Table 14. 41 pMOHwa pHOMwa unemaflw om pHOMHHu pHOMHHU noppwx .o.m.m mm “whom xom MBGQmm mm ouumaumz muuwHHMZIwEoHS mHHfl>nmm om w3mpom mzopwm coumxoonm mm muumanmz mono: mundane: mm noxom xom MHOEmumz «m wuumaumz ovumauszfi86flz moappflm .o.m.m mm wuuwaumsIOmmozo owmozo >pmnm mm enemseo ampsuoumemsmsanm mzmnmm Hm pnowaflw >Qcmuw mappmmme om mamsmaeemImmHsch cmcmuoImHmumHHnm xom as wuuwanmz muumauszwEowz mampmaawm ma muumHnms muumauszwEowz wuumHnmz 5H compo UMQMUInm>ocoo omomo ma muumaumz muuoauszwsmfiz maae>mwasmm ma wuumanmz mxcflmm coumxoonm 8H muumHnmz ovumauszwEowz mxcfldm ma onmEOU poozaoo coumxooum muuwaumz NH muuoHnmz ouuoHszIfiEsz mflcoH Ha omamu . um>ocoo wHHH>moa>mm OH omdmu muumauozIfiEmfiz cmon m mnumanmz muumauszfismez 032.6 m mpumauws muuwHHMEIwEMHE muumHnmz o muumsumz amcsuaumnmomeeflm emceumsmm a mepmHHHmImmepflm copwuoImHmpmHHHm couumnumz m counmnumz counmcumz ucwpgm>pam v ummom xom couumnums m Howom nwppflm cuomam m muuoanmz opumHHMSIHEmaz oodmu H mm: NuflmcwucH Epflpm: an: wuwmpmucH nmwm mowumm HHOm nmpepz Eoum pmuoomxm mmwumm Haom Eonm pmuomaxw moanmm Hwom pw>ummno uommcmne .muwcp anemone HMOm Hufimgoucw Epwpwe can now: Eoum mmfluom pmewc HHom cufl3 mcowum>ummno wommcmnu udwououcqusfloa mo comflnmafioo .m prme 42 ma Epflpmr m.~H seem ucmemuod unwoumm >uflmcmucH mcfimmmz “>HMEESm m3mpwm . pcmaumma HHosgmHmnd ow mzmnwm . magnum 0mm030 mm mupmanmz muuwHHmZIHEMHS mfiumaupz mm muuoHHmz muumHMMZIMEowz compo om medEoo poo3Hoo goumxoonm 6x636: mm muuoHHmz muumaumz compo mm compo omdmqum>ocoo .coumxoonm vm muuwanmz ovumanmzlfleowz 0mm030 mm mappmHHHmImmepHm cmpwnonHmpmHHHm wuuwaumz mm mappmHHHmImOprwm pmpmuonHmpmHHflm wHHfl>wHHmm Hm popcwucoo .m magma 43 Table 9. Comparison of point-intercept transect soil manage- ment group observations with soil management groups of named soil series from high and medium intensity soil mapping units. Transect Observed Expected S.M.G. Expected S.M.G. Number S.M.G. High Intensity, Medium Intensity l 2.5b 2.5a 2.5a 2 2.5b 2.5a 4a 3 3/5b 3/5a 4a 4 L-Zc 3/5b 3/5b 5 2.5b 3a 2.5a - 3a 6 4/2b 3a 2.5a 7 2.5a 2.5a 2.5a 8 3/2a 2.5a 2.5a 9 L-Zc 2.5a" 2.5b 10 1.5a 2.5b 2.5b 11 3/5a 2.5a 2.5a 12 2.5a 2.5c 2.5c-s 13 4a 2.5a 2.5a l4 2.5c 4a 2.5a 15 1.5a 2.5a 2.5a l6 2.5b 2.5b 2.5b 17 2.5a 2.5a 2.5a 18 3a 2.5a 2.5a 19 3/5a 3a 2.5a - 3a 20 3b 5c 4c 21 3/5c 3a 4c 22 4b 3/2a 3a - 2.5a 23 2.5b 2.5a 2.5a 24 3/2b 3/5a 4a 25 2.5a 4/2a 2.5a 26 2.5c 3/5c 3/5c 27 3/2c 2.5a 2.5a 28 3/5c 3/5a 4a 29 2.5b 4c 4c 30 4c 4c 4c 31 4/2c-' 3a 2.5a - 3a 32 2.5a 3a 2.5a - 3a 33. 3/2a 2.5a 2.5a 34 2.5c 2.5b 2.5b 35 2.5c 2.5a 2.5a 36 2/4a 2.5c 2.5c-s 37 2.5b 2.5a 2.5a 38 2.5a 2.5a 2.5a 39 3/2a 5c 3/5c 40 3/2b 2.5c 3/Sc 44 Table 9. Continued Summary: % Agreement Mapping Intensity of S.M.G. High 12.5 Medium 17.5 45 cmm3upo HHHu nmmzupo HHHu cmm3upo HHHu HHHu nm>o cmm3uso no HHHu cmmzupo ammBupo HHHu HHHu HHHu HHHu HHHH HHHH HHHu mcHnumpomH. Han» Has» Has“ HHHu Heep HHHu HHHu nmm3upo sm03upo nmmzupo HHHu NUHmcmucH EpHpmz 92m pmuomdxm cmMSupo HHHu nmw3upo HHHu um>o smozupo cmm3upo HHHu HHHu Hm>o :mm3uso HHHu nmmzupo HHHU HHHu HHHu HHHu HHHU :wm3upo HHHu HHHu HHHu HHHu HHH» HHHu HHHu HHHU HHHU cmm3upo smwzupo HHHu HHHu Nmecmuce stm. and pmuuwdxm nmm3ugo HHHu nm>o nmm3u=o HHHu HHHu HHHu nm>o smm3upo HHHu smm3upo zmm3upo cmmzuso nmm3uso HHHu Hana Hess H..—”H..... HO>O OCHHUMSOMH Hana nmmzupo HHH» :mm3upo HHHH HO>O OCHHUMDOMH HmH>sHHm HHHu Hm>o nmm3upo HHHu HHHu Hm>o ammzupo nwmzupo HmH>sHHm smmzupo nmm3upo HHHu .802.“ pm>nomno mm hm mm mm gm mm mm Hm ON mH wH NH wH mH vH MH NH HH I-INMQ‘IDWFQO‘ HmQEpz nommgmua .muHCp mpHmamE HHOm SUHmsmucH EsHpmfi ppm 20H: Scum mmHumm memc mo mommy HMHumuoE ucmnmm SUHz mgoHum>nom Ino dawn HMHnmumE uponmm uoomgmuu umwououcHIusHom mo comHuomEoo .OH OanB 46 m.hv EDHUOE oa smHm ucwEmoumd w HuHmcmucH mCHQsz ”wumfiapm nmm3uoo nmm3ugo HHHu Hm>o cmm3upo ow numBupo nmm3upo HHHH Hm>o nmp3uso mm HHHu HHHu HHHu mm HHHu HHHL Hews am wcHuumpomH HHHu amazuso no>o HHHu pm HHHu HHHu HHHu mm HHHu HHHu HHHO am HHHu HHHu HHHu um>o smaguso mm HHHu HHHu. HHH» mm Has» HHH» HHHu um>o smmzuso Hm Smm3u90 £mfl3fi50 £mfl3u50 . o m smmzuso smmzuno HHHu mm pongucoo .oH mHQMB 47 Table 11. Summary of percent agreement of point-intercept transect data with names of various kinds of soil landscape units. % Agreement to % Agreement to High Mapping Medium Mapping Soil Landscape Unit Intensity Units Intensity Units Series 12.5 15.0 Soil Management Group 12.5 17.5 Parent Material Type 40.0 47.5 Natural Drainage 37.5 40.0 Illllll‘lll“!llllli lyillllll 48 Table 12. Length of line-transect excavation by soil series. A. 'Summary of East-West Excavation - 397 Feet Total Length of Series Series in Feet % of 397' Capac 26 6.5 Metamora 6 1.5 Celina 3.5 0.9 Teasdale 4.5 1.1 Owosso 20 5.0 Miami-Marlette 18 4.5 Wawaka ' 83 20.9 Spinks 11 2.8* Oshtemo-Spinks 15 3.8* Riddles ' 78 19.6 Riddles, sandy-substratum phase 14.5 3.7 33.4 Riddles, fine variant 40 10.1 Owosso, sandy substratum phase 11 2.8 Hillsdale 57.5 14.5 Oshtemo 9 2.3 ' Total 397 100% *Considered similar to the soil found in the name. B. Summary of North-South Excavation - 206 Feet Total Length of Series Series in Feet % of 206' Riddles, , sandy substratum phase 18 8.74 Riddles, ‘ fine variant 8.5 4.13 24.03* Riddles 23 11.16 Saylesville 114.5 55.58 Miami 14 6.80* Owosso 28 13.59 Total 206 100.00% *Considered similar to the soil found in the name Illlll ll Ill-‘I‘l I [I ‘II N IIIIIIIIHI‘HIIII' I.Il I‘ll. (Ii I III. rile. 1‘ .IIIIII.I..IIII. III 11 I'll 49 Table 13. Length of entire line-transect excavation by soil series. Total Length of % of Entire Series Series in Feet Excavation Capac 26 4.3 Metamora 6 1.0 Celina 3.5 0.6 Teasdale 4.5 0.7 Owosso 48 8.0 I -908 Owosso, sandy substratum phase 11 1.8 Miami—Marlette 18 3. -5.3 Miami 14 2.3 Wawaka 83 13.8 Spinks 11 1.8 Oshtemo-spinks 15 2.5 Oshtemo 9 1.5 Riddles 101 16.7“ Riddles, sandy substratum phase 32.5 5.4 -30.1 Riddles, fine variant 48.5 8.0‘ Hillsdale ' 57.5 9.5 Saylesville . 114.5 19.0 . Total 603.0 feet 99.9% 50 Table 14. Summary of soil series observed by kinds of land- scape units in the 603 foot line-transect excavation. Number of Different Landscape Unit Landscape Units Observed Series 13 Soil Management Groups 9 Parent Material Types 5 A breakdown of the different kinds of parent material types observed in the trench appears in Table 15. Close examination of this particular soil grouping will aid in the interpretation of the depositional environment of the area. Table 15.. Summary of parent material types in the 603 foot line-transect excavation. Parent Material Type - % of Total Trench Length Till 46.9 Lacustrine overlying till 19.0 Till overlying outwash 19.2 Outwash overlying till 10.8 Outwash, 4:0 . Total 99.9 Soil management groups observed in the line-transect can be summaried in a similar manner (Table 16). 51 Table 16. Summary of soil management groups observed in the 603 foot line-transect excavation. S.M.G; % of Total Trench Length 1.5a 19.0 2.5a 36.1 2.5b 4.3 3a 9.5 3b 0.8 4a 5.8 3/2a 9.8 3/2b 1.0 2/4a 13.8 'Total 100.1 The five soils sampled in the line-transect included a wide range cf profile textures (see Appendix D). Satur- ated hydraulic conductivity, bulk density, percent total pore space and permeability are listed in Appendix E. Field descriptiOns of these five soils were made using the stan- dard conventions described in the Soil Survey Manual (1951). ' The sediments observed in the trench were quite variable as one might suspect from reviewing the previous data. The lateral extent of horizons and textures varied from relatively uni- form sequences (Figure 7) to complex, discontinuous se- quences (Figure 8). Several interesting lithologic rela- tionshiops were also observed in the line—transect exca- vation as follows: 1. An apparent inversion of topography having outwash at the crest of a hill and till in the adjacent swale. An 52 5n Figure 7. A portion of the continuous line - transect excavation having a relatively uniform sequence of horizons. SL Sandy Loam L Loam CL Clay Loam e Effervescent with dilute HCL MS Medium Sand C III] ‘. 53 .II 4_ .m ... 8 " ///////////// //////////// /////////// . 4 /////////// ///////////WI 2 sumac: //////////////////////// mm £?E,_ , //////////// /////////// ,ufi. #55:: IIIIIIIIIIIIIIIIII I.......... ...... / / / / / / / / / / '60" L Loam CL Clay Loam SCL Sandy Clay Loam SL Sandy Loam A portion of the continuous line - transect excavation having complex, discontinuous sequences of horizons. Effervescent with dilute HCL MS Medium Sand e FS Fine Sand LS Loamy Sand .Figure 8. 54 intermediate soil consisting of till overlying outwash lies between the two (Figure 9) 2. Stratified silts, sands, gravels and loams be- neath a 3' mantle of till (Figure 10). 3. Stratification lines in 'till' material. 4. Glacial till interfingering laterally with outwash deposits (Figure 11). 5. Lacustrine clayey materials overlying till. Figure 9. AA. Section of the continuous line - transect showing three profiles that illustrate an inversion of topography. A. Outwash profile on crest of hill, 8. Till overlying outwash on slope, C. Till profile in the swale. Tape measurements are in feet. Till overlying stratified materials. Figure 10. An area where till interfingers laterally with outwash. Figure 11. VI . DISCUSSION The complexity of this research area is indicated by the great diversity of soil series, soil management groups, and parent materials observed. Comparison of the soil homogeneity for three different kinds of mapping units (series, soil management groups and parent material types) at two mapping intensities along with independent tran- sect data illustrate the variability and complexity of this soil landscape in more quantitative terms. A. Series Mapping Units By careful consideration of the names of the units and compositions of medium and high intensity soil series map- ping units judged by all the profiles observed during map- ping (Tables 3 and 4, respectively), it was possible to identify some of the factors responsible for the low average homogeneity. The values of-28 and 47 percent homogeneity for medium and high intensity mapping units, Tables 3 and 4, may be similar to a soil classifers concept of the map homo- geneity in that these figures were made up of soil observations that actually go into the delineations made. For example, when the medium intensity mapping units were delineated, on 57 58 an average, 28 percent of the soils observed were actually found in the name. These observations are the basis of the mapper's concept of the mapping unit. Perhaps an even better indication of mapping unit com- position and homogeneity would be to collect independent soil observations. We recall that the average percent homo- geneity for medium intensity soil mapping units in most coun- ties in Michigan was 50 to 60 percent (Whiteside, 1975), based on point-intercept transect observations following mapping. When similar criteria are applied to these map units, Table 11, the homogeneities are 12.5 and 15.0% respectively. In the construction of the medium intensity map only the soils recognized in the Ingham County soil survey legend were delineated. Some areas were composed of soils currently not recognized in Ingham County. These areas were mapped as the soil on the legend that moSt closely resembled the soil actually present. For this reason some soils mapped on the medium intensity soil map in fact have zero observations of the series in the name. Part of the increased homogeneity of high intensity mapping units is due to map design. Since only 0.6 hectares (1.5 acres) of a soil is needed to be delineated, some areas of as few as three contiguous observations of a series were delineated. These areas were composed of 100 percent of the series in the name. To reduce this bias as much as possible the average homogeneities were always computed by weighing 59 the percent homogeneity of each mapping unit according to its areal extent on the soil map. The data indicate that many of the mapping units do follow the guidelines established by the Soil Conservation Service (Soil Survey Staff, 1967). Many of the mapping units, however, do not even approach the guidelines. Two- thirds of the medium intensity and one-half of the soil series of the high intensity mapping units contain less than fifty percent of the series in the name. The range is all in- clusive, 0 to 100 percent. B. Soil Management Group Mapping Units Soil management groups are composed of soil series with similar drainage and dominant profile texture. In this manner similar series were assembled into groups that would react in a similar way to similar management practices. It might be assumed that since many series may possibly be grouped together, soil management groups would tend to be more homogeneous. This assumption was verified when sum- maries of the soil management groups delineated as medium and high intensity soil mapping units were examined (Table 5). Compared to the soil series mapping units the total num- ber of mapping units identified were fewer: 11 vs. 15 for medium intensity mapping units and 13 vs. 22 for high in- tensity mapping units. A greater percentage of the units identified.were greater than fifty percent of the named S.M.G. and total average homogeneity is increased. The con- version to soil management groups also reduced the variation 60 in medium intensity mapping units. A relatively low average homogeneity indicates that a large portion of the soils present in many mapping units were not similar in profile texture and/or natural drainage class. The conversion from series to soil management groups did not greatly increase the average homogeneity of the high intensity map units. The seven percent increase is attributed to the diluting effect of averaging some previously highly homogeneous units with units lower in homogeneity. The greatest increase in percent homogeneity occurred when series units were converted to soil management groups on the medium intensity soil map. A 57 percent increase in homogeneity from 28 to 49 percent, may be considered important from a land use aspect. The data indicates that grouping soils as soil management groups on this landscape at a medium mapping intensity, will substantially increase the homogeneity of the units delineated. The value of a soil map is largely in its use as a management tool. Since soil management groups combine soils into groups that have similar properties important in their use and management, it may be more sensible to map soils as soil management groups.in the types of landscapes under study. A decrease in the number of units delineated (possibly taking less time) coupled with an increase in homogeneity make this type of mapping very favorable for many uses on this type of landscape. Although the homogeneity is increased when soil manage- ment groups are used, still many inclusions of other soil 61 management groups are obvious. These inclusions indicate that soils of different textures are present. These differ- ences may be associated with differences in parent material types. C. Parent Material Type Mapping Units Soils similar in mode of deposition, as indicated by textures and stratification of materials are grouped. Any effects of natural drainage were minimized by grouping together all drainage classes. Several soil management groups and series may be consolidated. The soil management groups do no always differentiate between different parent material types. Some soils may be of the same soil management group and yet have different depositional histories. Spinks soils are a 4a soil management group but may form in sandy till or sandy outwash. Also, different series having different parent material types may have the same soil management group. Sleeth soils are considered outwash and papac soils are usually composed of till yet each soil has a soil management group of 2.5b. The effect of this grouping was to again reduce the number of units identified, to 4 from 11 and 13 for medium and high intensity map units, respectively. In addition to this grouping it greatly reduced the range in percent homogeneity of the units and increased the average percent homogeneity for both medium (49 to 62%) and high intensity (54 to 70%) soil mapping units (Tables 5 and 6). 62 By grouping the soil observations into 4 parent material types much of the mapping intensity differences in homo— geneity were removed. The individual parent material types for both mapping intensities have similar homogen- eities. An outstanding exception is noted in the outwash parent materials. A fifty percent increase in homogeneity occurred when mapping at the higher intensity (61 vs. 91%). A closer look at the data obtained for outwash parent materials for mapping units or both high and medium intensity helps explain the discrepancv (Table 17). Table 17. Summary of outwash parent material for medium and high intensity mapping units. A. Medium Intensity Mapping Units. WSoil % Homogeneity % of Outwash Mapping Unit of Mapping Units Units Covered Boyer B-slope 74 18.4 Boyer C-slope 64 9.3 Gilford A-slope 37 33.7 Matherton A-slope 71 8.3 Sebewa A-slope 71 30.4 B. High Intensity Mapping Units. Soil % Homogeneity % of Outwash Mapping Unit - of Mapping Units Units Covered Fox Baslope - 100 21.0 Granby B-slope 75 8.1 Kalamazoo C-slope 86 21.1 Matherton A-slope 71 12.0 Sebewa A-slope 100 18.8 Spinks A-slope 100 11.3 Westland A-slope 78 7.7 63 The Gilford medium intensity mapping unit has a very low homogenity (37%). The geographic location of this unit may be found in Figure 3. The unit surrounds the northern portion of Felton Drain. This same area is mapped as Col- wood and Barry soils on the high intensity soil map (Figure 4). These soils are developed in lacustrine and till parent materials. The omission of this area from the outwash areas considered in the high intensity map- ping units accounts for the difference in percent of the map covered by outwash in Table 6. The inclusion of this large area in averaging the homogeneities of medium inten- sity mapping units contributed substantially to the observed reduction in weighted average homogeneity. Another factor also contributed to the observed dif- ference in outwash homogeneity. The Spinks unit recognized in the high intensity map (Figure 5) was not mapped as an outwash unit but is mapped as Marlette, a till unit, on the Inedium intensity map (Figure 4). This unit covered over twelve percent of all the area mapped as outwash and contained only outwash observations (Table 17). This area was not recognized as a Spinks mapping unit when mapped at a medium mapping intensity. Increasing the mapping intensity made the observation and identification of this unit possible. A final point illustrated in Table 17 pertains to the mapping units actually mapped as outwash. Only two 'units, Sebewa and Matherton, occurred in both medium and high .intensity soil maps. The high intensity Sebewa unit is 100 64 percent homogenous according to the observed soils. Yet, on the medium intensity mapISebewa is 71 percent homo- genous. The homogeneity is increased by dividing one of the Sebewa mapping units into 4 other different smaller map- ping units. This manipulation also occurred in other map- ping units and may have been a significant homogenizing factor. The problems associated in the identification of medium intensity outwash deposits did not appear in the till, lacustrine and outwash over till parent material types. Mapping intensity made no differenceiJIthe homo- geneity of these parent material types. Grouping soils by parent material types did increase average unit homogeneity from that obtained using soil management groups. The fact is that the average homogeneity of parent material types, the broadest units studiedq‘was still only 62 to 70 percent. The range in homogeneity varied from 34.5 to 90.8 percent. Although characterizing soil landscapes by parent material types does increase the percent agreement to named units the value of«the information obtained is questionable. Parent material types do help in interpreting the deposi— tional history of an area, but properties important in soil use and management are not considered. Similar parent material types will be composed of soils having signifi- cantly different properties. The relatively low mapping unit homogeneity indicate that within a general depositional environment many minor types of deposition will occur. 65 D. Transect Data The previous data analyzed individual map units and calculated an average homogeneity by weighing all observations in each unit. Independent point-intercept transect obser- ‘vations taken over the area also related the same sort of information. In this procedure observations were taken systematically throughout the area at 60 pace intervals on traverses normal to the irrigation line system. All obser- vations are compared in Tables 8,‘9 and 10. A summary of initial transect data lists the percent agree- ment of the transect observations to both the high and medium intensity soil maps (Table 11). The data indicate that the entire map was less homogeneous than that found by all 430 soil observations made during mapping. This result might be due to random variation in this extremely variable landscape. Map units mapped by five soil classifiers of 'varying experience in an area onEmile north of the current study area were analyzed by Amos((1973). Similar agreement of independent observations with map units was reported. Series ‘were found to be 10.4 to 26.1 percent the same as the names of the map units. Soil management groups were found to be 10.9 to 33.5 percent in agreement. These values compare favorably with the transect data in Table 11. Both series and soil management group data fall within the range found by .Amos. Subsequent transect data show similar trends and indicate that the medium intensity map may indeed be the best (Appendix F). 66 Parent material type units more than doubled the per- cent agreement over soil management groups, Table 11. Similar results were obtained when natural drainage homo- geneity (see Table 11) was compared. Similarities of the per- cent agreement of observations with natural drainage and parent material types indicate that at least part of the differences between soil management groups and parent material types reflect the irregularities in the topography of the landscape studied. The relatively low agreement of observed natural drainage to the named drainage reflects the varia- bility of sediments that commonly occur in the same posi- tions in the landscape. Small micro—variations in slope landscape irregularities, account for much of this varia- bility. Table 18 illustrates the relationships between ob- served soil management groups, grouped as parent material types, and expected parent material types from the medium intensity soil map. In this transect, the till derived soils, 40% of the observations, were 81.2% in agreement with the medium intensity soil map units. All drainage classes are represented and all but one soil had the same profile texture. Outwash transect observations, representing 27.5% of the transect, were only 54.5% in agreement with the medium intensity soil map. In this case twice as many different profile textures were found compared to the till transect observations. Again all drainage classes were recognized. This example illustrates the statement made earlier that Table 18 67 Relationships between parent material types and soil management groups among point-intercept transect observations, from Tables 9 and 10. Till Transect Observation Number Soil Manage- ment Group Expected Parent Material From Medium Intensity Soil Map 16/4 1 7 12 14 16 17 18 23 25 26 29 32 34 35 37 38 2.5b 2.5a 2.5a 2.5c 2.5b 2.5a 3a‘ 2.5b 2.5a 2.SC' 2.5b 2.5a 2.5c 2.5c 2.5b 2.5a till till lacustrine till till till till till till outwash outwash till till till till till = 81.2% agreement Outwash Transect Observation Number Soil Manage- ment Group Expected Parent Material From Medium Intensity Soil Map 11/40“ 2.5b 3/5b 2.5b 3/5a 4a 3/5a 3b 3/5c 4b 3/5c 4c outwash outwash till till till till outwash outwash outwash over till outwash outwash 54.5% agreement Table 18. Continued 68 Outwash over Till Observation Number 5 8 24 27 31 33 39 59 8/40 = 20% Soil Manage- ment Group 4/2b 3/2a 3/2b 3/2b 4/2c 3/2a 3/2a 3/2a E Me xpected Parent Material From dium Intensity Soil Map 0/8 till till outwash till till till outwash outwash = 0% agreement Lacustrine over Till Transect Observation Number 10 1; 2/40 = 5% Soil Manage- ment Group Expected Parent Me Material From dium Intensity Soil Map 0/2 till till = 0% agreement Alluvial'Transect Soil Manage- Expected Parent Material From Observation Number ment Group Medium Intensity Soil Map 4 L-2c outwash _2 L-2c till 2/4 = 5% . 0/2 = 0% agreement Till Over Expected Parent Outwash Transect Observation Number 39 1/40 = 2.5% Soil Manage- ment Group 2/4a Material From Medium Intensity Soil Mgpi O/l lacustrine = 0% agreement Average 47.5% agreement with medium intensity soil mapping units. 69 i different parent material types will be composed of dif- ferent soil management groups. In this case, both texture and hatural drainage combine to create the observed variability. Outwash over till observations were fairly homogeneous with respect to texture having only 2 different types. Again all drainage classes'were observed. Lacus- trine over till, alluvial and till over outwash observa- tions had the same profile textures, drainages, and soil management group within respective parent material type. More observations are needed to generalize with any certainty about the last three units. The data for parent material types illustrates the great variability of soils found within a particular parent material type due to the many different textures and natural drainage classes allowed within this grouping. Variability is also attributed to the occurrence of soils of different parent material, and hence different deposi- tional environment, within a mapping unit of a particular parent material type. The former condition is recognized by soil management groups although the latter may not. E. Defining Complex Soil Landscapes. Data presented to this point illustrates the great variability in soil distribution and homogeneity of many types of soil groupings on the research site. Broader groupings did increase the percent agreement in all cases. Within these broader groupings, however, great variability still remained. 70 Increasing mapping intensity did not greatly increase mapping agreement in all cases. As the soil groupings got broader, the effects of mapping intensity diminished. Unusual variability occurred at all levels and at all inten— sities. In the previous section transect data from the re- search site was compared to data obtained from a similar area nearby. The comparison indicated that the two areas were quite similar. The transect data. however. was only a sample and did not cover the entire research area. Tables 3, 4, 5, and 6 were not developed from transect data, but from all observations made in the mapping, and indicate somewhat of an increase in homogeneity.‘ The reported homo- geneity can be compared to that expected from simi- lar intensity soil maps made by the National Cooperative Soil Survey personnel. One may assume that the soil maps of the irrigation area are more accurate than those normally made by the National Cooperative Soil Survey. More observations were made and a detailed topographic mapwused to more accurately place soil boundaries for the research site.‘ The net effect of this procedure was to increase the mapping accuracy and resulted in somewhat more homogeneous soil mapping units. The determination of the percent agreement of soil ob- servations to named mapping unit delineations by the two methods described makes it possible to confidently place limits on the expected homogeneity of soil map units 71 delineated by the National Cooperative Soil Survey. These limits would apply to similar soil landscapes only. The homogeneity of maps made by the National Cooperative Soil Survey on similar areas, at similar intensities, ought to fall within the designated range of map unit homogeneity. The homogeneity of the study area maps as determined by the weighted average of all mapping units was considered an upper limit of homogeneity for each mapping intensity. The observed agreement of transect observations of the study site to the named unit enclosing the observation would make the lower limit of soil units' homogeneity for each map- ping intensity. The type of soil landscape on sites defined by the limits in homogeneity thus established was unusual if not unique even for glacial materials. It is suggested that soil landscapes of similar variability be designated as complex soil landscapes. Such areas may be recognized by low map unit homo- geneity when compared to independent observations. Per- cent agreement to named series should fall within the range of 12 to 28 percent and 15 to 47 percent for medium and high intensity maps respectively. Many types of complex soil landscapes may exist. Each type may form by different processes and exhibit different landforms. The remainder of this study is devoted to describing the possible process responsible for the type of complex soil landscape described for the research site. Criteria for predicting similar soil landscapes are suggested. If 71 delineated by the National Cooperative Soil Survey. These limits would apply to similar soil landscapes only. The homogeneity of maps made by the National Cooperative Soil Survey on similar areas, at similar intensities, ought to fall within the designated range of map unit homogeneity. The homogeneity of the study area maps as determined by the weighted average of all mapping units was considered an ’3: - \ upper limit of homogeneity for each mapping intensity. observed agreement of transect observations of the stud? ate site to the named unit enclosing the observation would n A. ‘~ the lower limit of soil units' homogeneity for eachzmh ping intensity. ‘ - "- ‘ ‘ The type of soil landscape on sites defineiffi . “- ‘ o“ limits in homogeneity thus established wasz1;£::l«» unique even for glacial materials. It is sauxseee ~* ‘ ‘ ‘ — T‘ o " o - - § ‘ ‘ ‘- soil landscapes of similar variability be fieszr‘ complex soil landscapes. Such areas may be recognized by 135: :33 geneity whnbcompared to independent :55 1' a s ' to named series shcxli 55-- H- cer' nd 15 to 4 9311-7? 53’ spectively. k- mplex Soi- -erii'sks .- -.. a. ‘ ‘ g -‘H . ~ - .. y , 4t” ferent pro:.=.=ss>° 5- hinder of...- "" ’34s- 72 F. Soil Variability in a Continuous Line Transect Characterizing an area using point-intercept transect observations enables one to determine the relative com- plexity of the area but often the processes associated with the observed variability are uncertain. An understanding of the processes involved in the formation of complex soil landscapes is essential if intelligent predictions of their composition, extent, and associated features are to be made. An excavation, 603 feet long, previously described was studied with the hope of obtaining some idea of the processes associated with the formation of the soils present. This line transect was divided into two sections, one part being in an area mapped as outwash and another mapped as till. This position was chosen for two reasons. First, the range of textures between these units was quite large indicating sig- nificant differences in depositional environment. And second, the position of the transect across two significantly dif- ferent units made a study of the transition zone between the two different types of facies possible. The transition zone between such units is one of the best places to study the relationships of the units to one another. A summary of the series observed in the east-west sec- tion, north-south section, and both sections together ap- jpears in Tables 12 and 13 respectively. Data with asterisks following the numbers indicate soils that were considered similar to the soil found in the name. These soils will 73 be in the same soil management group as the named unit transected by the excavation. A few soils are noted as variants and phases. A soil variant is a taxonomic unit closely related to another taxonomic unit, a soil series in this case, but departing from it in at least one differentiating charac- teristic at the series level. Variants may actually be considered different soil series but are too small in ex- tent to be established as new series. Soil phases are sub- divisions of a taxonomic unit made on the basis of any char- acteristic or combinations of characteristics potentially significant to man's use or management of the soils (Soil Survey Staff, 1951). The Riddles Fine Variant soil may be described as a Riddles with a twenty inch surface of lacustrine clays. This soil grades into the Saylesville. The sandy substratum phases are soils that were classified as particular series but had a sandy outwash below the depth considered in Soil Taxonomy. A summary of the soils observed in the east-west con- tinuous line transect (Table 12A) again illustrates the extreme variability in this complex soil landscape. No fewer.than 13 soil series were identified. These series may be placed into nine different soil management groups and five different parent material types. In other words, within a two hundred foot radius five different modes of deposition of parent materials were observed. The difference in the number of different soil management groups and 74 parent material types was related to differences in natural drainage within a single parent material type (see Tables 15 and 16). Even a cursory study of the lateral distribution of soils in this line-transect (Figure 7 and 8) lends some credibility to the large range in homogeneity observed for individual map units. Fairly uniform soil horizon sequences are represented as well as very complex, discontinuous sequences. A soil classifier, or different soil classi- fiers, may map the landscape in a number of different ways depending upon exactly where the soil observation is made (Figure 6). G. ’Soil Lithologic Relationships in a Continuous Line- Transect. Several interesting lithologic relationships present in the line-transect excavation indicated the possible origin of the parent materials. Glacial ice stagnation and its attendant processes are suggested. One such relationship illustrated in Figure 9, shows an inversion of topography. The observed sediments occurred in positions in the land- scape opposite to what might be expected. In this example outwash material occupied the crest of a hill and till sedi- ments occupied the low area in the landscape. A transition of till overlying outwash occurred in an intermediate posi- tion. Normally water worked deposits are associated with lower positions in the landscape. Till is unconsolidated sediment and easily eroded by running water. An hypothesis 75 to explain this inverse relationship assumes the stagna- tion of an ice block followed by slow downwasting. To envision this process imagine an ice block or higher ice hill at position C of Figure 7. In position A water is flowing and outwash is being deposited. As the ice slowly melted the rate of water flow slowly reduced and sands settled out. Eventually the ice melted enough so that englacial till was exposed. This till becomes saturated with water and flows onto the immediately adjacent outwash deposits. The ice continued to melt but at a slow enough rate that little water working occurred. The sediments left where the ice once existed were the sediments incorporated in the ice when it was active. The ice did not contain enough material in this case to leave as much sediment as the earlier fluvio-glacial activity. As a result of this lack of debris a topographic low composed of till lies immediately adjacent to a higher outwash deposit. Similar deposits in southeastern Massachusetts have been described and interpreted in a similar manner (Harthsorn, 1958). The outwash deposit adjacent to the lower till seemed to end quite abruptly. The outwash first appeared at a depth.of five feet in the profile, thirty feet from the westward origin of the line-transect. A deep boring at.the beginning of the line-transect, in the swale, was observed for comparison. Excepting a ten inch section from 7'6" to 8'4" composed of fine sand, the boring to a depth of 9 feet was composed of till. The outwash observed in the deep 76 boring was gray and may or may not be connected to the outwash at the bottom of the excavation. The real difference in the elevation of outwash sediments between the two points was approximately 11.5 feet. The bottom of the trench 30 feet to the east lay approximately four feet above ground level in the swale. It is believed that the gray outwash observed at depth is related to an earlier ice retreat and the present till is related to a later readvance. The interpretation of the sediments associated with the stagnation of at least a portion of the ice sheet is based in part on evidence that till actually flowed in a quasi—liquid state as flow till. Observations from other parts of the line-transect excavation support this assumption. A portion of the north-south line-transect was composed of till overlying stratified outwash materials. This stratified outwash was much more sorted and stratified than previously noted. This was readily apparent by com- paring Figure 9a and 93 with Figure 10. The stratified material in Figure 10 contains till bands as well as sands, silts and gravel. A similar sequence was described by Boulton (1968) for flow tills currently forming on some Vestspitsbergen glaciers in Greenland. Even more convincing evidence of flow till occurred in the east-west line- transect. Much of the eastern-most 100 feet consisted 77 of alternating units of Riddles and Hillsdale. Both soils were developed from sandy loam till parent materials. Hills~ dale has a coarser solum than Riddles, the former being in the coarse-loamy family and the latter in the fine-loamy family according to the Soil Taxonomy. These 'till' derived soils showed incipient stratification bands in their pro- files. This banding did not appear to be pedogenic in nature. The banding was interpreted as evidence of quasi- liquid till flowage, flow till. The presence of flow till suggests that the ice down- wasted in place. Active glacier movement would be expected to destroy the incipient stratification observed in the till. Other observations in the line-transect excavation more strongly suggested ice stagnation and slow downwasting. As indicated in Table 16, a large portion of the line-tran- sect appeared to be lacustrine clays overlying the till. This soil, Saylesville silty clay loam, is described in Appendix D. The textural difference between the clays and the underlying sandy loam was quite large. Pebbles were absent from the upper lacustrine material but quite abundant in the underlying sandy loam till. There were no apparent varves in the clays. Quite often lacustrine sediments will exhibit a banding that corresponds to seasonal deposition. The clay sediments observed in the Saylesville silty clay loam would seem to indicate that water ponded on the surface of a non—moving 78 ice mass. The clays were the last sediments to settle out of the standing water and thus do not contain coarse sediments. In time the ice mass melted out. It is possible that in the process of ice melting out the varves that may have been formed were destroyed by mass flow. The line- transect trench bottom was not level but had a 2-3% 510pe. A final observation of a portion of the line-transect excavation suggests that the observed soil materials were deposited contemporaneously. A small portion of the transect was composed of till interfingering laterally with sandy out- wash deposits (Figure 11). This observation occurs in the transition zone between the till swale and the outwash upland. As the outwash was being deposited the flow till buried part of the outwash. Water continued to flow at least for a short time, and subsequently buried some of the till. The final collapSe of the ice block to form the swale must post—date the outwash deposits; otherwise, the lowland created by the melt out would have collected the outwash deposits. H. Local Ice Stagnation From the lithologic relationships described in the line-transect excavation it seems reasonable to suggest that depositional processes associated with local ice stag- nation and slow downwasting account for the parent ma- terial and soil variability observed on the research site. The inversion of topography, depositional sequences of till over outwash, incipient till stratification and lacustrine 79 clays overlying till were previously recognized in the context of an ice stagnation environment. Their occurrence together on the research site strongly support the hypothesis of ice stagnation. ‘Diagnostic features that suggest an area is derived from processes associated with ablation of an ice-supported moraine have been listed by Kaye (1960). Diagnostic fea- tures of an ablation moraine, if they occur together are as follows: 1. All degrees of sorting will be found 2. Tills may appear stratified. 3. Tills, lacustrine, and fluviatile sediments may be interstratified. 4. Large scale plastic deformation by contorted folding may occur. 5. Ice-fracture fillings may be present. 6. Hummocky topography, with superficial beds paral- lel to the surface is common. Most of these features were present on the research site. The first three features listed above were well re- presented in the line-transect excavation as previously described. The research site was too small to show the relationship described in number four. The last two criteria, similar to number foury:might not be well represented on the research site, oerere subdued in nature, but have been observed nearby. An apparent crevasse filling occurs within two miles of the research site. 80 The exact location of this feature is SEk, NE%, SE%, Section 30, T.4N., R.1W. The landform may be described as a 200 meter long linear ridge having a relief in excess of 20 feet, over the surrounding lowland, with slopes greater than 25%. This ridge is composed of loam and sandy loam, till parent materials. Two observations taken on top of the ridge to a depth of five feet, 120 paces apart were both composed of till. In addition, a thirty five pound granitic boulder was observed on the top of the ridge indi- cating till deposition. An active glacier would not be expected to leave linear till ridges. This ridge may have formed as till filled into cracks on the top or at the bottom of the glacier. The important point is that an active glacier would close the cracks and destroy any till-crevasse fillings. The last criteria suggested by Kaye for use in identifying dead-ice moraines, hummocky topography, have also been identified on and near the re- search site. Hummocky topography will naturally range from relief of several hundred feet to a subdued relief of five to ten feet (Gravenor and Kupsch, 1959). The study area had numerous closed-depressions indicated on the two foot contour interval topographic map. Amos (1973) noted numerous closed depressions in his study area one mile to the north. This area was previously shown to be of similar complexity to the research site. The re- lief on the research site can be classified as subdued with maximum relief of approximately fifty feet. 81 The research site did meet most diagnostic criteria (five out of six) for classification as an ablation moraine (dead-ice moraine). Alone each feature may or may not be readily attributed to depositonal processes other than stagnating gliéial ice. At least one interpretation of each feature, however, would suggest this hypothesis. Together these features presented a strong argument that the processes associated with the downwasting of stagnant glacial ice are indeed the correct interpretation as to the origin of the complex soil landscape studied. I. Areal Extent of Ice Stagnation The prediction of the areal extent of ice-stagnation would be of great help to the soil classifier in predicting the occurrence of complex soil landscapes. Eskers have been associated with ice stagnation in the past and may indicate in some instances areal extent of stagnating ice. Numerous eskers may be observed in Figure l as linear hatch markings trending north-south. These eskers occur in association with many end moraines. Since end moraines are associated with the retreat of an active ice front it may be argued that in this region the presence of eskers are not necessarily associated with stagnating ice. Al- though the prediction of regional ice stagnation is beyond the scope ofthis study, local ice-stagnation and the resultant complex soil landscape appeared to extend at least four miles in width north-south. Not enough data was avail- able to predict the east-west extent. The northern-most 82 boundary extended at least to Mount Hope Road as indicated by the presence of the crevasse filling previously des- cribed. The southern most boundary extended at least a half mile past Willoughby Road, two miles to the south of the study site. Soil sequences very similar to the study site have been observed in SE%, NW%, Section 13, T.3N., R.2W. The sediments observed were found in a thirty square foot, five foot deep excavation. The sequences observed included till over outwash grading to outwash, and incipient stratification lines in a till profile. The till contained an apparent random distribution of clasts more typical of ablation till. In places this flow till occurred over a more compact till. More exact delineation of the complex soil landscape boundary would require a more detailed treatment than provided in this study. J. Why the Ice Stagnated. If one suggests a mechanism such as ice-stagnation to account for observed landscape characteristics it seems only reasonable to suggest possible reasons why the ice stagnated. Again, solving such a complex problem was beyond the scape of this study, but this did not preclude the possibility of some speculation. One of the regions most outstanding ass- emblage of landforms may be observed in Figure 1 as crescentic dark bands trending east-west. It is generally agreed that these bands represent end moraines and recessionsl moraines (Leverett, 1917). 83 An unusual feature of the moraines in this area is the con- spicuous lack of outwash normally associated with end moraines (Henderson, 1959). Is it possible that some of the end moraines are in fact dead ice moraines? Probably some of the landforms mapped as end moraines are in fact end moraines (or recessional moraines). It is impossible from the landform map to tell exactly how the glacier receded. It may have melted back straight to its source or, more probably, it may have melted back, re- advanced a bit, melted back more,‘readvanced again, etc. Each minor readvance may be shown as a morainic feature. The presence of the gray fine sand at a depth of 7'6" found in the swale may be interpreted as outwash associated with a minor oscillation in the ice front. Three separate se- quences of till over outwash were observed at the intersection of College Road and I-96. These detailed borings to a depth of over thirty feet are currently on microfilm at the Michigan State Highway Department. These sequences suggest the possibility of oscillations in the ice front._ The question as to which glaciation they re- present has yet to-be answered. The regional bedrock in- creases in elevation over 750 feet from north to south in Ingham County (Vanlier, et al., 1973). This in- crease in bedrock relief may have been enough to cause stagnation of the ice sheet in the final stages of de- glaciation. The increase in bedrock relief appears to be of the same order found by Sharp (1949) in stagnating areas of the Malaspina Glacier. 84 A simple explggation to account for the complex soil landscape may be that this area is a subdued end moraine. The area did not show evidence that the subdued appearance is due to overriding. The stratification lines observed in the line-transect were not distorted as is often the case in overridden end moraines (Totten, 1969). If the area studied did in fact show an arcuate appearance in its east-west extent some workers might suggest the area is an end moraine (Totten, 1969). The evidence strongly suggests ice-stagnation, however, and a more descriptive term would be dead-ice moraine in this case. K. Criteria for Predicting the Extent of a Complex Soil Landscape. Although the precise reasons for ice-stagnation may be uncertain the complex soil landscape associated with it does exist. Accurate prediction of the occurrence of such complex areas in soil mapping will be of great help in trying to decipher soil patterns. If these areas are of great enough extent some radically different mapping unit criteria may be necessary to more adequately describe the units found therein. The following diagnostic features modified from Totten (1969), are suggested as guidelines to be used in identify- ing complex soil landscapes: l. The area contains numerous closed depressions. 2. The area is often hummocky although subdued in some cases. Slopes vary from level to greater than 18 per- cent. 85 3. Inversions of topography are present having outwash derived soils on the uplands and till derived soils in the lowlands. 4. Tills may appear stratified. 5. Tills, lacustrine and outwash sediments may be interstratified. 6. Ice fracture fillings may be present. 7. All degrees of sorting may be present within very small areas and single map delineations. 8. Homogeneity of soil mapping units is quite low, often between 10 and 30 percent of the named soils. The moréiiisted diagnostic features that an area displays the stronger is the evidence that it is a complex soil landscape. VII . SUMMARY This study discusses soil classification systems and attempts to relate soil classification to the soil mapping units delineated by soil classifiers. The physiographic and lithologic properties of soil in this area are associated with their parent material origin as glacial depositional materials. The relationship of soil variability in glacial landscapes is discussed. Many landscape types are associated with glaciation in Michigan. The origin of hummocky areas that have both till and outwash material present is of special interest. Several landforms with similar characteristics are reviewed. Fea- tures associated with stagnant ice are described. Areas currently undergoing processes associated with ice stagnation are cited. Physiographic and biological features are noted. Four-hundred thirty soil observations of the study site were used to construct two maps of differing intensity. These two maps, having high and medium intensity soil map- ping units, were compared for four types of soil groupings; soil series, soil management groups, parent material types 86 87 and natural drainage class. Point-intercept transects are discussed and compared to the previous data which indicate that the study area is unusually complex. This idea is deve10ped in detail and a definition of complex soil landscapes is suggested. The processes involved in the formation of this com- plex soil landscape were studied in a 603 foot line-tran- sect excavation. The soils present and their extent are compared for soil series, soil management groups and parent material types. Interpretations of the soil sediment deposi- tional sequences are suggested. The processes suggested as responsible for the soil complexity are associated with ice stagnation. The possible cause of ice stagnation is discussed and diagnostic features to delineate areas formed by ice stagnation processes are suggested. VIII. CONCLUSIONS This study indicates that the soils present on the Institute of Water Research irrigation area are extremely variable. Soil mapping units delineated for the area are heterogeneous, often containing strongly contrasting soils within their boundaries. The processes responsible for the observed complexity are associated with the depositional processes involved in the slow melting of stagnant glacier ice. The soil land- scape formed through these processes has been referred to as a 'complex soil landscape.' A complex soil landscape can be identified when the following diagnostic features are present: I l. The area contains numerous closed depressions. 2. The area is often hummocky although subdued in some cases. Slopes will vary from nearly level to greater than 18%. 3. Inversions of topography are common. Outwash soils may be present on the upland and till derived soils in the swales. 4. Till, lacustrine and fluviatile sediments may be interstratified. 5. Tills may be stratified. 88 89 6. Ice fracture fillings may be evident. 7. All degrees of sorting may be present within a small area or in single mapping units. 8. Homogeneity of soil mapping units is quite low. Between 10 and 30 percent of the named unit can be ob- served. LITERATURE CITED LITERATURE CITED Alden, W.C. 1924. The physical features of central Massa- chusetts. U.S. Geol. Survey Bull. No. 760. pp. 13-105. Amos, D.F. 1973. Soil Surveys: A Critical Evaluation with Emphasis on Use in Urbanizing Areas. Ph.D. Thesis, Michigan State University. Beery, M. and B.P. Whiteside. 1970. Mapping Unit Com- position Summary: Washtenaw County, Michigan. 1968-1969. Mimeographed. Blake, G.R. 1965. Bulk density. In C.A. Black (ed.) Methods of _S__o_il Analysis, Part I. Agronomy 9: 374-390. Amer. Soc. of Agron., Madison, Wis. Buol, S.W., Hole, F.D. and R.J. McCracken. 1973. Soil Genesis and Classification. Iowa State Univ. Press, Ames, Iowa. Boulton, G.S. 1968. Flow tills and related deposits on some Vestspitsbergen glaciers. Jour. of Glac. Vol. 7:391-412. . 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A“Af\“ APPENDICES APPENDIX A 0m cm wh.m >.m ucwEdon>0o Hwom lean on no mauuwa\3 pcmm on em em.m m.m unmeuoem>me Hwomesm HmEHcfiE\3 teem ov\2 0m nm mm m unmeaon>mo Hwomncm HMSfixME\3 pcmm om nm\m m~\m ~\m smeo on snoH um>o ..oe low .ocmm mecca ou ccmm _TIIIIII 0v be we v teem hamon o~\¢ nw\v m~\w «\v Emoa hmao auawm on EmoH Hm>o .eoeuou .ncmmquMm mason 0H\v na\v ma\< H\v mean Hm>o .govlvH .UcmmIUGMm mason omxm nmxm am\m m\m Hm>mum can seem Hm>o .eovlom .EmoH accmm oz om\z am am mm m Enos enema o~\m n~\m mm\m ~\m EmoH unflo wuawm on seed Hm>o .sovlom .EdoH aecmm 5 made Hm>o 9 oH\m nH\m H\m H\m ..oeneH .smoH mecmm 0m.~ am.~ em.~ m.~ Emoa pawn can Econ om.H pm.H em.H m.H smoH mean madam ecu EmoH hmao 0H.z 0H DH MA A “wowloev hmao no no go o .mow Hw>ov >MHU «can u o o n a mHonemm mews» x0fi£u omcwmuo Umcwmua cmcwmun Hamz =4m ue>o I hauoom >Hm> hauoom hamumumooz mucuxwe emcwmuo use hauoom uwnsmeom use Hamz mawmoum ucmcweon hauoom huw> sz mawom owcmmuo meom Hmuwcwz mommmHU ommcwmuo Hmucumz « mmDOMU BZHZWQ£Z¢Z AHOm m0 MQHEmZOHfidflmmmHBZH fl xHDmem4 96 e _mdon emenm u o macaw m+mm n macaw wmmume u m meoem weum u m odoam wmanma n a macaw wmlo u e ”mommmHo macaw .muflcs ucmfimmmcme Haom mum menace macaw omega mHOQE>m enema ucmEmwmcmE Hflom on» on cocoa mum muwuuwa mmmHo macaw mcH3OHH0m one cmnz he oE\z 8 Hum: oenq oeuq wens ens seemm owns omuq mmiq mus >5moH 02nd A mmmud encased no Hmw>saad o 0 o n m maonENm APPENDIX B 97 meee>xmo mEoHou QOmqu moses unomxud wncmuw vacuumne mxcflmm unemaflw flammmz canned umwom nmm3uso puOmaww >pmum cemcoum OEmunmo umeom msmemm couumcumz wacoH xom cousmwo oonEmme ecmHemmz summem smexoo mzmuuo mHHH>mHHmm cwwuumm .m.m momEu< mmeeeeemm mmemz see» maceuou mHOEmumz 0mm030 uw>o mHHw>uwm counmm amm3uso nEoomz maafl>amccmx meee>mmemwm Heep um>o mcfluumsomq comqu ooozaou mfleefim waoomoe c0mmwm oceuumsomq . mxmemz smm3usouum>onaafle muuwm wxooq cmomuo Hoppflm .m.m Hoppwx muumm mampmmma mamoEHm wamomaaflm weapoflm .o.m mwaooflm .m.m mamoEHm mwaocflm HmEom couaawuo HHHB omdmu muumaumz coumxooum um>ocoo mcwamu flame: boom Room Hams . Hamz umnzweom hamumumcoz Hmwumumz weaned mewauo Hmusumz BUMhomm mme<3mam<3 xmmmu zommmmIZOBAmh .m.3.H NEE ZO OZDOh mAHOm mom wmx mMHmmm AHOm m anzmmmd Hmom mo cflmwuo 98 cmon smuoocou mHflom c0pmumm mamosm Hmw>sHH¢ pwcflmuolwwuoom cmcflmuo hwuoom umssmeom counmsom . mafiom deflnp< owcmmuo Auaooc m xHozmmm< omcwmuo wauoom Nuw> APPENDIX C APPENDIX C ABBREVIATED LEGEND FOR SOILS FOUND ON THE MEDIUM AND HIGH INTENSITY SOIL MAPS MEDIUM INTENSITY MAP - ABBREVIATED LEGEND SOIL SYMBOLS. Each area on the Medium Intensity Map is iden- tified by a symbol composed of one or two parts. The first digits stand for the soil series name, the capital letter of each symbol indicates the dominant slope in that area. These map units are also on the current soil survey of In- gham Co., Michigan. The lay of land or slope gradient is expressed in the percent slope of the surface. The percent slope is equal to the number of feet rise or fall of the land surface for each 100 feet of horizontal distance. The soil scientist uses an Abney level in the field to determine percent of slope. The following legend applies to the slope classes. A - 0 to 2 percent slopes (level to nearly level) B - 2 to 6 percent slopes (undulating or gently sloping) C - 6 to 12 percent slopes (rolling or moderately sloping) D.- 12 to 18 percent slopes (hilly or strongly sloping) In interpreting or drawing conclusions from the soil maps, it is important to understand that every area (mapping unit) includes a range of properties. The lines of demarca- tion between soil symbols vary from definite sharp lines to areas where the mapping units grade from one another so 99 100 gradually that precise boundaries are not to be expected. Small areas of other soils may also be included within each delineated mapping unit. The symbol on the map must be un- derstood to represent the dominant and characteristic kind of soil and not always a soil which is uniform in every respect. Within the outlined mapping units, distinct inclusions of other soils too small to be shown on the soil map frequently occur. The final correlation of the soil series names in the Ingham County has not been made; con- sequently, some changes in nomenclature may be necessary. .mawwumume Hafiu EmoH pawn 0cm em.m EmoH co Ummoam>m© mHHom omcwmno hauoom uwn3meom occaocw mwfiuwm ommmu EmoH cameo .medEoo one mo ucmoumd ma pecan as wme 0cm mHHocx 0cm mmmpwu 30H so one .pmcflmup >Hu00d mmma mun mHMOm omega .mHAOm muoemumz can .mwenwx .ommwu no names Hanan mum mcflmmme cw Hwom menu nuw3 UmocaocH .pcmm wcwm mnwb pcm madam mcomumoamo mo mumwmcoo Ecumuumnsm one .mzmswmmcwmno one mmmum Hmcowwmmummc cw maHOm Hm>ma m:0m.m aaummc .pmcwmuo wauoom >um> use hanoom mo mumwwcoo wamEoo Hwom mace medEoo ©003HOU .mmwcxownu cw mesocw oa cmnu mme we coNfiuoc m Hmucuxmu EmoH amao modem .6de can Hm>mum msomumoamo mcwmaum>o .xowcu mwsocfl me on em .mHMHHmumE pawn hamoa ou Emoa mvcmm co Ummon>mU mHAOm omcfimuolaamB menace“ meom uwwom Emoa hunch ammom 101 we .mawmoum ecu uso Inmsounu m.m can» kummum mm cuw3 modem hEmoH 6cm mocmm co Ummonbwo mmawom mxcfidm one .Ucmm can Hm>mum mcomumoamo mcwmaum>o mamwuwume been AEMOH ou EmoH mpcmm co pmmon>m© wagon Homom one .mcfimmme cw Ewan mumummwm ou Hmoauomum was we ufl use» cwDMwUOmmm wawumofinucw on one maflom omega .xmadeoo one unocmsoncu mum mHAOm mxcflmm can Homom one .mHHocx new mwmoau 30H .mmmnm Umoun mo mHHOm mcaumaso seine use use Hm>ma Manama .pmcamup Ham3 mo mumamcoo medEoo Haom mace modem mecca mxcammlumwom .mcoNfluoc Home: on» cw ommOQEoowp HHmE ma camp mace .mamwumume wmomm mcounwm Scum Ummon>w© mHHOm Decemuo meme mwsaocfl mHHOm cousmcom oz x058 coucmsom abomw mmmufi AHOm BZflSflUdZdE AHOm ma ha NH HH Homzwm 102 om\v nm.mlnm\m nm\m oniom.~ oe .HHHu moan on seed mcoouooamo mcweauo>o maownouoe econ ocem esooH Ho econ >6oo~ .ocom mo monocw we on ma co codoHo>oo mawom nonwouo Haos nonsense mofiuom mouoz ocom meooa mono: .usonmsounu EmoH hoao can Eooa we oomoo ooouon3 EmoH uo>o Ewen meson mo oucuxou HwOmnsm women no o>on mHflOm oucEwuoz NHHMOAQhe .mcflmmoe cw Eonu ououomom ou Hoe Ifiuooum no: we we umnu oouowOOmmo maouooeuuce On one meOm omone .ouwm cw mouoo ooa conu once on m Eonm omcmu one omonm aw Hoasmouufl one moons Hocoe>wonH .mcoflmmoumop 3OHHonm ca one mmo3omocflouo ocean .maaocn one momowu 30H .mmouo mcfima 30H omoun :0 me0m mcflumacocc one Ho>oH mauooc .oocflouo mHHOOQ ponzoeom mo mumwmcoo onmEoo Hwom mane meooa meson commonmuoEmuoz .moomuuou one ocean» onHo> .mcflmaa noosuso no one mHfiOm omone .ccom mHHoboum no ocom an cfioanocs mnemomoo maao>onm oonsuxou Esflooe one omuooo haououoooe ca ooEHom mHfiOm mcwumasocc one Ho>oH hauooc .oocwouo MHHOOQ pon3oEOm mo mumflmcoo mowuom mane EMOH xenon couuonuoz .moapowm conu uomuooo .HeOmnsm EooH meson o mcfl>on ca moaopflm Eoum nommwo mHHOm oaocmaaam one .waououodom Eon» awe ou Hoowuooum #0: me He won» poxfie maouoo Iwnucfi On one mHHom omone .moceouofi one mcfimHm Hawu no Hana Hmwomam monomoH hamooo oousuxou omunoo eaoumuoooe no Esfipoe ca ooEMOM uonu wawow MHHwn ou wcwuoasocc oocfiouo Hams mo umwmcoo vac: mnemmoe mane anon macaw mememHHeeummeeeem .ocom mEooH m we momma ooomusm one .xownu monocw ca con» mmoH we EooH hone hogan .connon m Honsuxou one .ocmm one Ho>oum msoonwoaoo mnemano>o .xOAnu monocw mm on em .mameuouoe econ waned ou EooH xenon co oomoHo>o© meOm pocwouc eanoom owsHoce mawom Unemafiw Ewen ewcmm pHOMHwo Hm om mm mm mm 103 wlem.N o mxm mm.~-m~\m we em.N .EeoH wonem onHm mH onnuxou noheH 30Hm .muHHm one onem onHm >no> ooHMHuenum no oodoHo>oo mHHOo oonHeno HHo3 oonHonH mHHOm nOmmHm EeoH nOmmHm .noHnu mononH 0H nenu noueonm mH noNHnon m Henouxou EeoH heHo monem one .Ho>enm one monem mnooneoHeo no>o .xOHnu mononH ov on em .mHeHnoueE EeoH one EeoH eonem no oomoHo>oo mHHOm oonHeno anoom oonHonH moHnom e3onom EeOH e3onom .mnHmmeE nH Bonn onenedom on HeoHnoenm non mH UH nenu ooueHoomme >HoueoHnunH on one mHHOm omone .mHo>Huoodmon onmEoo onu mo unoonom om on mm one we on ov an oxen one onmEoo onu usonmnonnu one mHHOm ouuoHnez one 0mmo3o one .mHHonx one momoHn 30H .meone oeonn no on50m mH ann mnHmmeE mHne .HHOmnnm oonnuxou nonHm one ounH mnomnHmnounH mooemnnm unnm EeoH monem num3 HHHu HeHoeHm uHHm no .EeoH uHHm .EeoH nH oomoH uo>oo mHHOm oonHeno HHo3 oonHonH oHHom ouuoHnez .EeoH >eHo eonem >HHenwn mH oHHmonm on» mo unem none: one nH HHOmnnm one .EeoH eeHo on EeoH onHmHno>o mHeHnoueE EeoH eonem mo mononH me on mH no oomoH Io>oo mHHom oonHeno HHo3 hHouenoooE on HHo3 moonHonH moHnom Gomozo mEeoH monem ouuoHneZIOmmo3o .mmononnu nH mononH OH nenu mon mH noNHnon m Heneu Ixou EeoH ero monem one .Ho>enm no .monem mEeoH .onem Henunon no mnooneoHeo mnHMHno>o onnn mononH mm on me .mHeHnoueE EeoH >onem ou onem >EeoH no oomoHo>oo mHHOm oonHenolHHoz oonHonH mHHom OEounmo EeoH eonem OEounmo .HHOmnnm oonnuxou nonHm on» ounH mnomnnmnounH.mooemnnmn9m EeoH eonem one uenu nH HeeHz Eonm mnoMMHo ouuoHnez .EeoH on EeoH eonem mH onnuxou noeeH onm .HHHu HeHoeHm uHHm no EeoH uHHm .EeoH nH oodoHo>oo mHHom oonHeno HHo3 oonHonH mHHOm ouuoHnez one HEeHz mamon onuonnez Annenzv mm hm mm mm illl 104 .mononH we nenu noueonm enumoo ue mnooneuHeo mH noHn3 HHHu neoH eonem no oomoHoboo mHHOm oonHeno mHn00d.uen3oEom oonHonH moHnom oHeomeoe nm EeOH eonem oHeomeoe .eHouenemom Eonu men on HeOHuoenm non mH uH uenu ooxHE mHoueoHnunH one HHeEm On one mHHOm omonu mo meone HenoH>HonH .mHHOm nomEeH on» nenu nomeH ooemnnm nonOHnu e one HHOmnnm onu nH heHo onoe o>en mHHOm ooozHou one .munoEHoom oonnuxou EnHooE on owneoo mo mnomeH manennouHe nuHs muHmomoo ooHMHpenum nH ooEnom mHHOm omone .meex omenHeno HeHoeHm oHo nH one .meone Henonmonmoo nH mHHOm Ho>oH mHneon oonHeno eHnoom >no> one oonHeno eHnoom mo mumHmnoo ondEoo HHOm mHne elem onmeou ooo3HooIn0mEeH .mononH me one em noosuon nnooo eonen onem meeoH ane .oHHmonm onu unonmnonnu m.m nenu noueonm mm nuH3 monem aneoH one monem no oomoHo>oo mHHOm oonHenouHHoz oonHonH mHHom mnanm ee onem mEeOH mxnnnm om «v Hv HIGH INTENSITY MAP - ABBREVIATED LEGEND SOIL SYMBOLS. Each area on the High Intensity Map is iden- tified by a symbol composed of one or two parts. The first digits stand for the soil series name, the capital letter of each symbol indicates the dominant slope in that area. The lay of land or slope gradient is expressed in the 'percent slope of the surface. The percent slope is equal to the number of feet rise or fall of the land surface for each 100 feet of horizontal distance. The soil scientist uses an Abney level in the field to determine percent of slope. The following legend applies to the slope classes. A - 0 to 2 percent $10pes (level to nearly level) B - 2 to 6 percent lepes (undulating or gently sloping) C - 6 to 12 percent slopes (rolling or moderately $10ping) In interpreting or drawing conclusions from the soil maps, it is important to understand that every area (mapping unit) includes a range of properties. The lines of demarca- tion between soil symbols vary from definite sharp lines to areas where the mapping units grade from one another so gra- dually that precise boundaries are not to be expected. Small areas of other soils may also be included within each de- lineated mapping unit. The symbol on the map must be 105 106 understood to represent the dominant and characteristic kind of soil and not always a soil which is uniform in every respect. Within the outlined mapping units, distinct inclu- sions of other soils too small to be shown on the soil map frequently occur. 107 .EeoH monem e mH noeeH 3on one .unomonm hHHenmn mH noNHnon m Hennnxou EeoH meHo honem n .EeoH eeHo >UHHw on EeoH mnHano>o .noHnu mononH we on mH .mHeHnoueE EeoH eonem onHm on onem onHm eneoH nH oomoHo>oo mHHOm oonHeno thoom oonHonH mHHOm ennnnou 0m\m ennnnoo e .EeoH eonem e mH noeeH 30Hm one .HHHu EeoH wonem mnooneoHeo no ooQoHo>oo mHHOm oonHeno eHnoom oonHonH mHHom mnnem 0m ennem w .onnnonn we» nH nnoEdoHo>oo Hennuxon neonuH3 monem onHHenHe eHoHHE on Hennnon .mooo no oomoHo>oo mHHom oonHeno mHnoom oonHonH moHnom mnnenw 0m ennenw m .mmonnoHnu nH mononH 0H nenu noueonm mH noNHnon m Hennuxou.EeoH meHo on EeoH >eHo honem .Ho>enm one monem mnooneo IHeo .ooHMHuenum mnHmHno>o .noHnn mononH me on em .mHeHnoueE EeoH on EeoH eonem no oomoHo>oo mHHom oonHeno HHo3 oonHonH mHHom xom emxm . , xoe e .mHeHnopeE HHHn EeoH uHHm one EeoH no oomoHo>oo mHHom oonHeno mHnoom uen3oEOm oonHonH moHnom no>onoo nm.~ ereU I no>onou m .HHHu HeHoeHo uHHm no EeoH uHHm .EeoH nH oodoHo>oo mHHOm oonHeno HHo3 oonHonH mHHOm onuoHnez one HEeHz em.m onuoHneS one HEeHS m .mHeHnoueE HHHu EeoH uHHm no EeoH mnooneo IHeo no oomoHo>oo mHHOm oonHeno mHnoom oonHonH moHnom noumnoonm 0m.m . noumnoonm H mmoomo mmmee HHOm Homzem ezm2m6¢z¢z me: HHOm 108 em nm\m ev eN\e em\m em\m Um.~ .mmnoen we seen noueonm mnumoo ue monenonneo oonm nnH3 HHHu EeoH monem mnooneoHeo mHuanHm no oomoHo>oo mHHOm oonHeno HHo3 oonHonH moHnom oHeomHHHm emenne can onmemnnnm .noHnn mononH 0H nenu once mH EeoH weHo no EeoH meHo eonem mo noNHnon m Hennuxon one .monem one Ho>enm mnooneoHeo mnHeHno>o .onnu mononH we on em .mHeHnoueE EeoH one EeoH monem no ooQoHo>oo mHHOm oonHeno mHnoom uenBoEom oonHonH mHHOm nounonnez nonnonuez .mononH me one em noozuon nnooo monen onem >EeoH ane .oHHwonm onu unonmnonnu m.m nenu noneonm mm nqu monem >EeoH one monem no ooQoHo>oo mHHOm oonHeno HHo3 oonHonH mHHom mnnHmm mnnHQm .HHHu >eHo on EeoH mnoo IneoHeo mnHeHno>o mHeHnoueE onem onHm useoH no onem >EeoH onem mo mononH va mH no oomoHo>oo mHHOm oonHeno HHoB moonHonH moHnom eonoz eonoz .EeoH meHo monem >HHenmn mH oHHmonm one we uned none: on» nH HHomnnm one .EeoH meHo on EeoH mnHmHno>o mHeHnoueE EeoH monem mo mononH me on mH no oomoHo> Ioo mHHow oonHeno HHo3 >Houenoooe on HHo3 moonHonH moHnom ommo3o . Ommo3o .mononH me nenu noueonm mH Ho> Ienw one onem mnooneOHeo on numoo one .numoo nqu oHoe mmoH mnHEoo Ion .mHo>enm one monem .monem >EeoH en nHeHnoonn mHeHnoneE EeoH on EeoH monem no oomoHo>oo mHHOm.oonHeno HHo3 oonHonH mHHom ooNeEeHeM ooNeEeHeM .onew one Ho>enm mnooneoweo .ooHMHu Ienum mnHeHno>o .noHnu mononH we on we .mHeHnoueE nmezuno EeoH one EeoH uHHm no oomoHo>oo mHHom oonHeno eHnoom oonHonH moHnom oneHumo3 onennmoz «H mH NH HH 0H muom.~ 0m\m Om.N muem.m .onem onHm mnob one mnHHm mnooneOHeo mo mumHmnoo Enuennwnnm one .meezomenHeno one meone Henonmondoo nH ooQoHo>oo mHHom Ho>oH aneon oonHeno eHnoom oonHonH mHHOm oOOBHOU ooozHou . .onnn mononH m nenn noueonm mH nONHnon m Hennuxou EeoH eeHo monem one .Ho>enm one monew moooneoHeo no>o .onnu mononH ov on em .mHeHnoueE EeoH one EeoH monem no oomoHo>oo mHHom oonHeno mHnoom oonHonH moHnom e3onom e3onom .nnnn nanomnm neon monem wHHo>enm mnHmHno>o EnHOm EeoH >eHo eonem one EeoH eeHo e o>en mHHOm omonu .eHHeOHuee .mnHeHm HHHu one .mnHHEnno .monHenOE mooum on Ho>oH mHneon no oodoHo>oo mHHom oonHeno HHo3 oonHonH wHHOm noooHM noooHM .mUHHm one onem onHm mno> ooHMHuenum no oomoHo>oo mHHom oonHeno HHo3 oonHonH mHHom nemmHm nemmHm .mnHeHm nmezuno one mnHeHa oneH no one mHHom omone .munoEHoom oonnuxou nnHooE on omneoo mo mnomeH mnHuennouHe nUH3 muHmomoo ooHMHuenum nH ooEnou uenu mHHOm Ho>oH >Hneon .oonHeno mHnoom >no> one thoom mo mumHmnoo moHnom mHne nOmEeH mH wH 5H mH mH 60I APPENDIX D APPENDIX D DESCRIPTIONS OF SOILS ANALYZED FOR SELECTED SOIL PROPERTIES The following soils were all located in NW%, SE%, SW# of section 6, T.3N., R.1W. The dominant vegetation was mixed cool-season grasses and warm-season perennial dicots. CAPAC LOAM Parent material: glacial till Drainage: somewhat poor Classification: Aquic Hapludalf; fine-loamy, ' mixed, mesic Horizon Depth (cm) Description Ap 0-25 Very pale brown (10YR7/3 dry) to yellowish brown (10YR5/4 moist): fine sandy loam: moderate, fine, granular structure: friable; medium acid (pH 6.0); abrupt, smooth boundary. B21t 25-53 Strong brown (7.5YR5/6);c1ay loam: many medium distinct light gray (10YR7/l) and few, fine, distinct gray (10YR6/l) mot- - tles; moderate, medium,subangular blocky structure: firm; medium acid (pH 6.0); gradual, wavy boundary. Light gray (10YR7/l),sandy loam coatings, greater than 2 mm wide, on ped faces. B22t 53-94 Strong brown (7.5YR5/6);clay loam; many - medium distinct gray (10YR6/1) and few fine gray (10YR5/1),mottles; moderate, medium subangular blocky structure; firm: neutral (pH 7.0); gradual wavy boundary. 110 111 C 94-150 Yellowish brown (10YR5/4) loam; many medium distinct gray (10YR6/1) and few medium distinct strong brown (7.5YR5/6) mottles: structureless massive structure; friable; moderately alkaline (pH 8.0): calcareous Additional notes: 1. Light gray (10YR7/l) sandy loam coatings on ped faces that were greater than 2mm in width in B21t. APPENDIX E 112 HILLSDALE LOAM Parent Material: Drainage: Classificaton: Horizon Depth (cm) Ap 0-23 A2&B2t 23-107 1183 107-130 IIC 130-150 glacial till well Typic Hapludalf; coarse-loamy, mixed, mesic Description Pale brown (10YR6/3,dry) to dark yellowish brown (10YR5/4,moist) loam; weak fine granular structure: friable; strongly acid (pH 5.5); clear wavy boundary. Yellowish brown (10YR5/6);loamy sand; common medium faint light yellowish brown (10YR6/4) mottling; structure- less single grain; loose; medium acid (pH 6.0);and brown (7.5YR5/4);sandy loam; weak medium subangular blocky struc- ture; very friable; slightly acid (pH 6.5); clear wavy boundary. Dark brown or brown (7.5YR4/4);loam; weak coarse subangular blocky struc- ture; friable; moderately alkaline (pH 8.0): gradual wavy boundary. Yellowish brown (lOYRS/4);loam; moderate fine subangular blocky struc- ture: friable; moderately alkaline (pH 8.0). 113 MARLETTE SANDY LOAM Parent material: Drainage: Classification: Horizon Depth (cm) Ap 0-18 A2 18-30 B & A 30-53 B2t 53-81 B3 81-99 C 99-150 This profile sampled Glacial till well Glossoboric Hapludalf; fine- loamy, mixed, mesic Description Pale brown (10YR6/3.dry) to dark brown (10YR3/3p moist); sandy loam; moderate medium subangular blocky structure; friable; medium acid (pH 6.0); clear smooth boundary. Brown (10YR5/3);loamy sand; weak, fine, platy structure; friable; medium acid (pH 6.0); clear distinct boundary. Dark brown to brown (7.5YR4/4);loam; very pale brown (10YR7/3) coatings on ped surfaces; strong, medium subangular structure; firm; medium acid (pH 6.0); clear, smooth boundary. Dark brown to brown (7.5YR4/4);clay loam; strong, coarse angular blocky structure; very firm; slightly acid (pH 5.5); clear, smooth boundary. Dark brown to brown (10YR4/3):loam; dark brown to brown (7.5YR4/4) coatings on ped surfaces; strong, coarse subangu- lar blocky structure; very firm; neutral (pH 7.0); clear, smooth, boundary. Brown (10YR5/3);loam; moderate, medium subangular blocky structure; very firm; moderately alkaline (pH 8.0); cal- careous. and described by Raymond Laurin. Parent Material: 114 SAYLESVILLE SILTY CLAY LOAM Drainage: Classification: Horizon Depth (cm) AP Bl B21 B22 IICl IIIC2 0-18 18-36 36-63 63-86 86-112 112-150 lacustrine clays over till well Typic Hapludalf; fine, mixed, mesic Description Yellowish brown (10YR5.5/4,dry) to dark yellowish brown (10YR3/4,moist); loam; strong, coarse granular structure; firm; clear, smooth boundary. Yellowish brown (10YR5/4);silty clay loam; strong, coarse, subangular blocky structure; firm; gradual, wavy boundary. Dark brown to brown (10YR4/3);silty clay; strong, coarse, angular blocky structure; very firm; gradual wavy boundary. Brown (10YR5/3);silty clay; strong, very coarse, angular blocky structure; very firm; clear, wavy boundary. Dark brown to brown (10YR4/3);clay loam; strong, coarse, subangular blocky structure; firm; abrupt smooth boundary. Dark yellowish brown (10YR4/4);sandy loam; strong, medium, subangular blocky structure; friable. 115 SP INKS SANDY LOAM Parent Material: sandy outwash Drainage: well Classification: Psammentic Hapludalf; sandy, mixed, mesic Horizon Depth (cm) Description Ap 0-25 Light gray (lOYR7/2,dry) to brown (10YR5/3,moist) sandy loam; moderate, coarse subangular blocky structure; friable; strongly acid (pH 5.5); clear wavy boundary. A2&BZt 25-114 Yellowish brown (lOYR5/6);sand; struc- tureless, single grain; loose; slightly acid (pH 6.5); and dark brown to brown (7.5YR4/4);loamy sand; weak, medium subangular blocky structure; very friable; strongly acid (pH 5.5); clear wavy boundary. Cl 114-132 Pale brown (lOYR6/3);fine sand; struc- tureless single grain; loose; slightly acid (pH 6.5); gradual wavy boundary. IIC2 132-142 Dark, yellowish brown (lOYR4/4);loam; moderate, fine, subangular blocky structure; friable; moderately alka- line (pH 8.0); abrupt wavy boundary; calcareous. r IIIC3 142-150 Very pale brown (10YR7/3);fine sand; structureless single grain; loose; moderately alkaline (pH 8.0); calcareous. Additional notes: A2 bands average 10 cm in thickness. Bt2 bands overage 6 cm in thickness. Some A2 bands are fine sand. ‘ Parent Material: Drainage: Classification: Horizon Depth (cm) AP B2t+A2 Bth B22t IIA2 + IIBZt IIICl IVC2 Additional Notes: thickness, total thickness being 8 cm. evident. 0-15 15-41 41-56 56-79 79-125 125-130 130-150 116 WAWAKA LOAM Glacial till over sandy outwash well Typic Hapludalf; fine loamy over sandy, mixed, mesic Description Very pale brown (10YR7/3,dry) to yellowish brown (10YR5/4,moist); loam; weak, medium granular structure; friable; slightly acid (pH 6.5); clear smooth boundary. Brown (7.5YR5/4);clay loam; moderate, medium, subangular blocky structure; firm; medium acid (pH 6.0); and pale brown (10YR6/3);sandy loam on ped faces; very friable; slightly acid (pH 6.5); gradual wavy boundary. Pale brown (7.5YR5/4):c1ay loam; mo- derate, medium, subangular blocky structure; firm; medium acid (pH 6.0); gradual wavy boundary. Dark brown to brown (7.5YR4/4):clay loam; strong, coarse, subangular blocky structure; very firm; medium acid (pH 6.0); abrupt wavy boundary. Brownish yellow (10YR6/6);fine sand; structureless, single grain; loose; neutral (pH 7.0); and strong brown (7.5YR5/6);loamy fine sand; structure- less massive; very friable; medium acid (pH 6.0); abrupt wavy boundary. Brown (10YR5/3);silt loam; weak; fine, subangular blocky structure; friable; moderately alkaline (pH 8.0); cal- careous. Light yellowish brown (10YR6/4) fine sand; structureless, single grain; loose; moderately alkaline (pH 8.0); calcareous. IIBZt bands range from 1.25 to 5 cm in A + B interfingering IIICl and IVC2 interfinger horizontally. 117 ouenoooz mIOme~.H mm.Hv mm.H mIOHXm~.H be.H UHHH 3on OHIOerv.e mv.ov em.H mIOHme.e HIOmeo.H ummHH+~dHH 30Hm >no> HHIOmem.m mm.vm we.H mIOmem.m NIOmem.H ummm 3on >Houenoooz mIOHxvm.H om.mm me.H vIOonmH HIOmem.N Nn+u~m 30Hm NHHouenoooz mIOmeo.w ew.mm oe.H eIOHme.m HIOHxvo.e an eneBez ouenoooz mIOmeH.H mo.Hv em.H mIOHxMH.H Nw.H HUHH 3on eHouenoooz mIOmee.v mo.mm mw.H «IOone.v HIOere.m m+< 3on eHouenoooz mIOmeo.~ He.mm mm.H vIOHxHo.N HIOmem.~ m4 mnnHmm 30Hm OHIOHxvo.¢ mm.mm em.H mIOwam.m HIOmeN.H HUHH 3on >no> HHIOHxHo.m om.m¢ om.H wIOmea.m mIOHxvm.v ummm onem mIOHxNe.m mm.mv vm.H mIOmem.m m~.m uHNm ouenoooz mIOerm.H om.mv mm.H mIOHxvm.H mm.m an oHHH>moH>em 3on OHIOerm.v mH.Hm om.H mIOmem.v HIOHxNv.H UHH Bon eHonenoooz mIOHxvm.v Hm.om mo.H vIOme~.v HIonmH.e m+n ennmm enonmnmeoz mIonxmm.~ ~m.oe ne.H muonxem.~ em.m. on oneemnnnm BOHm mno> oHIOHva.m mv.Hm em.H mIOHxOH.N NIOmeo.m U 30Hm OHIOerv.v mH.mm ve.H mIOmem.e NIOonm.o ummm 30Hm OHIOme~.m mm.mm we.H mIOerH.m NIOHxvm.m nHmm ouenoooz eIOerm.H mv.Hv mm.H mIOmem.H vm.H an ereo NnHHHneoEnom . ~20 ooemm Nmenoa onooom nom noon noNHnom moHnom HHOm euHHHneoEnom onom anm nouoEHunoo nom mononH Hence . nnn>nnoseeoo w UHHnenoxm oouennuem , m xHQmem4 BUMbomm mme<3mem¢3 .m.3.H mme ZO BZMmMmm mHHOm m>Hh m0 mmHemmmomm HHOm DMBUMHmm APPENDIX F 118 Appendix F Supplementary Point-Intercept transect observations collected on the I.W.R. Wastewater Project. Transect Number Observed Soil Series Wasepi Matherton Metamora Riddles PD Matherton Westland Metamora Locke Ionia Sleeth Thetford Riddles Riddles SWPD Riddles Riddles PD Owosso Ockley Matherton Selfridge Sebewa ’Brookston Capac Capac Riddles SWPD Gilford Lamson Sebewa Metamora Teasdale Riddles Capac Brookston Spinks Brookston Wawaka Riddles Owosso Spinks Marlette Capac Thetford Capac Morley Kalamazoo Brookston Miami Miami Marlette Riddles SWPD Lamson Soilhenmmment Gang; 4b 3/33 3/23 2.3: 3/33 2.&: 318’s {<88 H8 6 m 8 893 NDNNNW Iwa m\- Q N819 9’ W hJN HE wPPPPPerPs HEEWHWEH Panxmlkuerhfl. OOHOHHHHOOOOOHHHHOOOHOOOHOOO >1 >1 >1 >1 '8 8300-3668 c>e ee 119 Transect Soil Series Ebcpected Fran Soil Management Parent Material Nmber ‘ Medium IntensitLMap Group ' ‘ Type 1 Gilford 4c 0 2 Gilford 4c 0 3 Riddles-Hillsdale 2.5a-3a T 4 Teasdale 3b T 5 Teasdale 3b T 6 Iamson—Colwood 3c-s-2 . 5c-s L 7 Lanson r‘olwood 3c-s-2.5c-s L 8 Riddles-Hillsdale 2.5a-3a T 9 Riddles-Hillsdale 2.5a-3a T 10 Gilford 4c 0 11 Riddles-Hillsdale 2.5a-3a T 12 Riddles-Hillsdale 2.5a-3a T 13 Riddles-Hillsdale 2.5a-3a T 14 Riddles-Hillsdale 2.5a-3a T 15 Lamson-Colwood 3c-s-2 . Sc-s L 16 Capac 2.5b T 17 Marlette 2.5a T 18 Capac 2.5b T 19 Capac 2.5b T 20 Sebewa 3 5c 0 21 Sebewa 3/5c 0 22 Marlette 2.5a T 23 Marlette 2.5a T 24 Capac 2.5b T 25 Sebewa 3/5c 0 26 Sebewa 3/5c 0 27 Sebewa 3/5c 0 28 Sebewa 3/5c 0 29 Sebewa 3/5c 0 3o Sebewa 3/5c 0 31 Capac 2.5b T 32 Marlette 2.5a T 33 Marlette 2.5a T 34 Colwood Canplex 2.5c-s L 35 Marlette 2.5a T 36 Farlette-Omsso 2.5a T 37 Marlette 2.5a-3/2a T 38 Marlette 2.5a T 39 Marlette 2.5a T 40 mrkette 2.5a T 41 Capac 2.5b T 42 'Capac 2.5b T 43 Marlette 2.5a T 44 Marlette 2.5a T 45 Colwood Couplex 2.5c-s L 46 Marlette 2.5a T 47 Marlette 2.5a T 48 Marlette 2.5a T 49 Colwood Complex 2.5c-s L 50 Colwood Canplex 2.5c-s L arcent in Name 28 LA) on U'l N \omxlmmthI-a ET rt ercent in Name Soil Series Expected From High Intensity Map Colwood Colwood Hillsdale-Dryden Spinks Spinks Brookston Spinks Hillsdale-Dryden Hillsdale-Dryden Colwood Hillsdale-Dryden Hillsdale-Dryden Matheron Hillsdale-Dryden Lamson Conover-Capac Conover-Capac Kalamazoo Canover-Capac Westland Westland Corunna Miami-Marlette Conover-Capac Barry Barry Granby Miami-Marlette Granby Corunna Conover-Capac Miami-Marlette Miami-Marlette Brookston Spinks Miami-Marl ette Miami-Marlette Miami-Marlette Miami-Marlette Mmemnam Canover-Capac Mimi-Marlette Miami-Marlette Spinks Brookston Miami-Marlette Miami-Marlette Miami-Marlette Brookston Brookston 14 Soil Managerent ' Group 2.5c-s 2.5c-s 3a 4a 4a 2.5c 4a 3a 3a 2.5c—s 3a 3a 3/5b 3a 3c-s _ 2.5b 2.5b 3/5a 2.5b 2.5c 2.5c 3/2c 2.5a 2.5b 2.5a esnsnnennnss S‘X'B’I‘ES'X' HEB-"8‘8 N uh Paralt Mataial HHHHHO—JOHBHHHHHQOHHHBSOF—JOHHQHSHOO—JOBH?‘D-JOt-BHL'H-ll-lol-Joot-Jt‘t‘ 5 L11 0 5% \OCDNO‘U'I-waH HEJPJ uric: :cent in Name soiléknieslbqecuxifrom 121 LymanChuHQ{th,Nbes Itodmton Cbnmmr Neeea Cbnmmr Cbnmmm Commmr Cbnmmm Omrwer maxe Buxfisfixl Comwer bktea Cbmmmr Mflmu Conmmm Nuami Mfimd Cbnmmm Cbnmmm ankquI BuxksUXI Burkstml Cbnmmm cemmmm Cenmmm Cbnmmm (humor bflami . . “FTT' M' . Bfiami Mumu Buxksfinl lfiami M' . Dfiami . . fgaml anflmmon anmsuMl Meme. Mfimd thu anmsuxl Mfimd Nfiami . . igaml anflstml l6 Soilfiemxfiment Gnmqg 2.3: 2.33 4/2a 2.5b 2.39 2.53 8888888588888888883888888888888888888 NNNNNNNNNNNNNNNNNNNNNNNNNNNNNNNNNNNNN O N on rananxmnnnnu BGHHGHHBHHHHHHBHHBHBHHHH6680-386HHBHHHQHSHHSHHHHHSHH 5 U1 N HICHIGRN STRTE UNIV. LIBRQRIES 31293103761387