ISGS CONTRACT/GRANT REPORT 1990-1 557.09773 IL6cr 1990-1 HYDROGEOLOGY OF SHALLOW GROUNDWATER RESOURCES, KANE COUNTY, ILLINOIS Illinois State Geological Survey Department of Energy and Natural Resources ILLINOIS STATE GEOLOGICAL SURVEY ■Ifl 1990 HYDROGEOLOGY OF SHALLOW GROUNDWATER RESOURCES, KANE COUNTY, ILLINOIS B. Brandon Curry Paul R. Seaber ISGS CONTRACT/GRANT REPORT 1990-1 ILLINOIS STATE GEOLOGICAL SURVEY Morris W. Leighton, Chief Natural Resources Building 615 East Peabody Drive Champaign, Illinois 61820 Digitized by the Internet Archive in 2012 with funding from University of Illinois Urbana-Champaign http://archive.org/details/hydrogeologyofsh19901curr CONTENTS EXECUTIVE SUMMARY 1 OVERVIEW 1 METHODS 1 FINDINGS OF THE INVESTIGATION 2 Location of Water-Bearing Deposits 2 ACKNOWLEDGMENTS 4 HYDROGEOLOGY OF SHALLOW GROUNDWATER RESOURCES 5 INTRODUCTION 6 Framework 6 Hydrogeologic Setting 6 METHODS OF THE HYDROGEOLOGICAL INVESTIGATION 7 Water Well Records 9 Surficial Geophysical Methods 9 Seismic Refraction 9 Electrical Earth Resistivity 10 Test Drilling 11 GEOLOGY 11 Stratigraphy 13 Paleozoic 13 Cenozoic 13 Buried Bedrock Topography 19 Buried Bedrock Valleys 19 St. Charles bedrock valley 19 Aurora bedrock valley 19 Other buried bedrock valleys 19 Drift Thickness 21 HYDROGEOLGOGY 21 Definitions of Aquifers 21 Hydrostratigraphy 23 Upper Bedrock Aquigroup 23 Prairie Aquigroup 24 St. Charles aquifer 24 Marengo aquitard 27 Pingree Grove aquiformation 27 Bloomington aquifer 27 Elburn aquiformation 27 Valparaiso aquifer 27 SUMMARY OF FINDINGS OF THE INVESTIGATION 27 REFERENCES 29 APPENDIX 34 FIGURES 1 Topographic and geologic features of Kane County 2 2 Major aquifers of the Prairie Aquigroup in Kane County 3 3 Generalized distribution and well locations in relation to Kane County 6 communities 4 Location of seismic refraction survey lines 8 5 Profile of bedrock topography as interpreted by seismic refraction methods 10 and demonstrated agreement from drilled wells 6 Stratigraphy of rocks underlying Kane County 12 7 Paleozoic rock units outcropping at the bedrock surface 14 8 Surficial drift map and stratigraphy of glacial drift (Prairie Aquigroup) 16 underlying Kane County 9 Environments of glacial deposition 18 10 Buried bedrock topography underlying Kane County 20 11a Schematic diagram showing relations of hydrostratigraphic units identified 22 in this report 11b Schematic diagram showing relations of glacial drift units 22 12 Cross sections of the Aurora bedrock valley 24 13 Cross sections of the St. Charles bedrock valley 25 14 Cross sections showing the Marengo aquitard in relation to the 26 Bloomington aquifer PLATE 1 Aquifers with potential for development of public water supplies: Prairie Aquigroup in Kane County, Illinois TABLES 1 Informal classifications of drift aquifers compared with hydrostratigraphic units 21 2 Hydrostratigraphic hierarchy in Kane County 23 APPENDIX A1 Water quality summary from wells in Prairie Aquigroup in Kane County 34 A2 Water quality summary from wells in Upper Bedrock Aquifer in Kane County 35 A3 Water quality summary from wells in Midwest Bedrock Aquigroup in Kane County 35 A4 Summary of principal aquifer hydraulic properties from aquifer tests and 36 specific capacity analyses A5 Mean and sample standard deviation of water quality data from the Prairie 37 Aquigroup, Upper Bedrock Aquigroup, and Midwest Bedrock Aquigroup Printed by authority of the State of Illinois/1990/250 EXECUTIVE SUMMARY OVERVIEW Kane County and its many communities just west of Chicago have depended on public water supplied from sandstone bedrock aquifers 1,100 to 2,000 feet below ground surface. The demand for water from a growing population has resulted in overpumping, and thus lowered groundwater levels. Water levels have dropped more than 900 feet in the deep sandstone aquifers, known as the Midwest and Basal Bedrock Aquigroups, lying deep below the Fox River Valley (Sasman et al., 1982). Water quality is also a concern: concentrations of barium and radium in water pumped from these aquifers are higher than recommended by the U.S. Environmental Protection Agency (1975) (Gilkeson et al., 1983, 1984). Pumping from deep aquifers or transporting water from Lake Michigan is costly. Obtaining local groundwater sources from aquifer materials at shallower depths would be more cost effective if water quality and yield were satisfactory. Several communities along the Fox River in Kane County and the Kane County Develop- ment Department contracted with the Illinois State Geological Survey and the Illinois State Water Survey in the mid-1980s to determine the potential for groundwater resources in (1) the Prairie Aquigroup, surficial materials or glacial drift deposited on bedrock during the Pleistocene Epoch from about 165,000 to about 10,000 years ago; and (2) the Upper Bedrock Aquigroup, fractured bedrock underlying the glacial drift. Drift consists of till (diamicton), sand and gravel, and stratified silt and clay more than 350 feet thick in places. Drift is thickest under the moraines left by glaciers and in "buried bedrock valleys" (fig. 1). These buried bedrock valleys became the focus of a search for shallow groundwater resources. The Surveys divided the responsibility for this cooperative investigation, and the results are being published separately. The main goals of the Geological Survey's investigation were • to locate and map the distribution and thickness of potentially water-bearing sand and gravel deposits, or aquifers, lying at relatively shallow depths in the glacial drift under Kane County. Both aquifers and nonaquifers of the Prairie Aquigroup and the Upper Bedrock Group have been described within a hydrostratigraphic framework that aids prediction and exploration. The fractured bedrock directly underlying the Prairie Aquigroup has been described briefly. The investigators proposed to demonstrate the effectiveness of surficial geophysical methods (seismic refraction and electrical earth resistivity) in prospecting for groundwater. The main goals of the Water Survey's investigation were • to evaluate the water chemistry, water-yielding properties, and long-term potential yields of sand and gravel deposits underlying Kane County, given the hydrostratigraphic framework developed by the Geological Survey. METHODS Geological mapping and surface geophysics were used to site test borings and production wells. Cross sections of the drift-filled buried bedrock valleys were constructed on the basis of well records, with both surface and borehole geophysics used for correlation. These cross sections aided in the design and interpretation of aquifer tests. Buried bedrock valleys, which were expected to contain major groundwater resources, were the focus of the investigations: 1. Preliminary maps of the buried bedrock surface were plotted using outcrop elevations, existing records from water wells, and test borings with verified well locations. 2. Locations of buried bedrock valleys were refined using seismic refraction techniques. Figure 1 Topographic and geologic features of Kane County 3. Prospecting for sand and gravel aquifers in bedrock valleys utilized electrical earth resistivity surveys. 4. Thickness and distribution of sand and gravel units (aquifers) within the bedrock valley fill were determined from test drilling and existing well data. 5. Data from piezometers and pump tests defined aquifer properties and boundaries. This was necessary for design and interpretation of the tests, which were complicated by the complex geology and geometry of the aquifers. Aquifer tests must be custom-designed to fit these factors if hydraulic characteristics are to be quantitatively assessed. Well location, design, and aquifer test duration must be adapted to site-specific criteria to test various models of aquifer properties. 6. Aquifer tests, conducted in three different buried bedrock-valley settings, provided data on water chemistry and well and aquifer yields. Each of the steps outlined above is necessary to efficiently develop the shallow groundwater resource. The investigation of aquifer distribution concentrated on the sand and gravel deposits that are greater than 50 feet thick and fill buried valleys, which are generally less than 3,000 feet wide. The buried bedrock topography map of Kane County helps to define the location of valley deposits. The map is based on more verified datum points than is any other map of its kind in Illinois. FINDINGS OF THE INVESTIGATION Conditions are favorable for development of shallow groundwater resources for public water supplies. Tests show that aquifers in buried bedrock valleys underlying Kane County have specific capacities (pumping rate per foot of drawdown) that range from less than 10 gallons per minute per foot (gpm/ft) to more than 250 gpm/ft; these aquifers provide the necessary transmissivity (as much as 270,000 gpd/ft) for municipal well production, and an adequate volume of water for sustained long-term yields (Visocky, 1987a, 1987b). The areas with the best potential for groundwater development in the glacial drift are shown in figure 2 and plate 1. Location of Water-Bearing Deposits The Illinois State Geological Survey defined and described units within the Prairie Aquigroup, a hydrostratigraphic grouping. Focus was on the aquifers within the buried bedrock valleys, R6E R7E R8E St. Charles aquifer Valparaiso aquifer Kaneville aquifer member of the Elburn aquiformation 1 Bloomington aquifer A A' cross section A 10 mi. |\J Figure 2 Major aquifers of the Prairie Aquigroup in Kane County. Figures 5 and 12-14 show the three-dimensional relationships on cross sections A— A', B — B', C — C', D — D', E — E', F — F\ and G— G', for example, the St. Charles aquifer (fig. 2, plate 1). This is because the deposits within and over these valleys are generally thick and include sediments that usually store and yield large amounts of water. As much as 120 feet thick, the St. Charles aquifer generally maintains a thickness of at least 50 feet spanning the bedrock valleys, which may be up to 3,000 feet wide. The continuity of water-bearing deposits may be interrupted by deposits that do not yield any significant amount of water. The St. Charles aquifer was the main focus of this study. Geological mapping suggests that the distribution and thickness of other significant aquifers within the Prairie Aquigroup need further characterization. "How much groundwater is available?" is a reasonable question frequently raised by local officials charged with the task of managing groundwater resources (Illinois Technical Advisory Committee on Water Resources, 1967). The resource lends itself to quantitative assessment (U.S. Water Resources Council, 1973). However, groundwater reservoirs are dynamic in nature; their withdrawal rates and patterns of extraction can be managed. Therefore, the development of the resource is subject to alternative plans, which may differ in their effects on yield potential, longevity of the supply, cost of recovery, impacts on other groundwater reservoirs or interconnection with surface water, and water quality. The Illinois State Water Survey discusses aquifer yields and water quality in a separate publication. The appendix in this report contains a summary of the principal aquifer hydraulic properties from aquifer tests and specific capacity analyses, and a summary of the quality of water in Kane County wells. Data for the appendix were furnished by the Water Survey; interpretations of the data are presented in their report on the shallow groundwater resources of Kane County. ACKNOWLEDGMENTS We are grateful for the support of the Kane Country Development Department and the people representing municipalities in Kane County. Richard Young, Director of the Kane County Environmental Department, was particularly helpful in coordinating county and community interests. Partial funding was provided by the cities of Aurora, Batavia, Carpentersville, Elgin, Geneva, North Aurora, and St. Charles; and the villages of East Dundee, Elburn, Hampshire, Montgomery, South Elgin, Sugar Grove, and West Dundee. Many of the Illinois State Geological Survey staff were involved with various stages of this project. Robert H. Gilkeson, currently with Roy F. Weston, Inc., Albuquerque, New Mexico, was the principal investigator for the Geological Survey during the early stages of the study. He was replaced as principal investigator by Stephen S. McFadden, now with Applied Engineering and Science in Atlanta, Georgia. Database creation, entry, and processing of well, seismic, and resistivity data were completed by Douglas Cantwell, Paul Heigold, Mary Holden, Douglas Laymon, George Lin, Joseph McGinnis, Robert McGuinness, Cynthia Morgan, Faith Stanke, and Cheryl Wegscheid. Geophysical field work and well location verification were performed by Douglas Cantwell, Craig Gendron, David Heidlauf, Paul Heigold, Douglas Laymon, Joseph McGinnis, Walter Morse, Phillip Orozco, Steven Padovani, Vickie Poole, John Skinner, Faith Stanke, Charles Tindell and Cheryl Wegscheid. Robert Vaiden compiled the bedrock topography map and assisted in the aquifer mapping. Richard Berg prepared the surficial drift map. Other professional expertise was provided by Ross Brower, Ardith Hensel, Phillip Reed, and Robert Vaiden. Keros Cartwright, Robert Gilkeson, Beverly Herzog, John Kempton, Stephen McFadden, and Nicholas Schneider reviewed the manuscript. The production editor was Ellen Wolf, text editor was Richard Davis, and graphic artists were Barbara Stiff and Pamella Foster. HYDROGEOLOGY OF SHALLOW GROUNDWATER RESOURCES OF KANE COUNTY INTRODUCTION Public groundwater supplies in Kane County, Illinois, have been obtained principally from sandstone bedrock aquifers of Cambrian and Ordovician age. Overdevelopment of these deep sandstone aquifers has resulted in water-level drawdowns of more than 900 feet. Water quality is also a concern (Sasman et al., 1982) because these waters contain concentrations of naturally occurring radium and barium in excess of standards set by the U.S. Environmental Protection Agency (1975) (Gilkeson et al., 1983, 1984). In the mid-1980s, the Kane County Development Department and several Kane County communities contracted with the Illinois State Geological Survey and Illinois State Water Survey to assess the potential of other aquifers, including sand and gravel in the glacial drift (Prairie Aquigroup) and fractured bedrock below the glacial drift (Upper Bedrock Aquigroup). These two rock units, referred to as shallow groundwater aquifers, are underutilized and represent potential major sources of water for the county (Gilkeson et al., 1987). Framework Evaluating the groundwater resources of the Upper Bedrock and Prairie Aquigroups begins with the description of the age, sequence, and composition of the geologic materials in addition to their capacity to store and transmit groundwater. The descriptions constitute a stratigraphic framework used to predict, among other things, the characteristics and distri- bution of rocks between datum points. This is accomplished by first describing independent stratigraphic categories of units: (1) lithostratigraphy, which delineates and distinguishes rocks on the basis of composition (lithic characteristics) and sequence (stratigraphic position) and composition; (2) chronostratigraphy, which defines the age of the rocks of this composition (lithology); and (3) hydrostratigraphy, which describes the hydrogeology within the rocks. These categories depend on descriptions at a reference section, a locality chosen for study. Away from the reference section, identical or similar material properties are matched and correlated. The results are depicted on geologic maps. For the most part, chronostratigraphic and lithostratigraphic units correspond. Until recently, these have been the primary mapping units in the bedrock and glacial drift in Illinois (Lineback, 1979). Hydrogeology involves the occurrence, direction of flow, and storage of groundwater below the surface of the earth. In this report, the hydrogeology of the rock units is described in terms of hydrostratigraphy, which is similar to lithostratigraphy in that the composition and sequence of the rock units are described. In addition, hydrostratigraphy describes the porosity of the rock and its ability to transmit water (permeability). Hydrostratigraphic units are primarily distinguished and characterized on the basis of porosity and permeability. Hydrostratigraphy involves the study and mapping of not only the solid rock material but also the character and nature of the pores and fractures (interstices) in the rock (Seaber, 1988). For this investigation, a hydrostratigraphic framework was developed describing the occurrence, location, extent, and thickness of the water-yielding and non-water-yielding deposits of glacial drift and the bedrock immediately underlying the drift. This framework will be used by the Illinois State Water Survey in their discussion of the water quality and yields of the aquifers underlying Kane County. Hydrogeologlc Setting The shallow bedrock in Kane County consists of the Kankakee and Elwood Formations, Silurian in age and composed mostly of dolomite, and the Maquoketa Group, Ordovician in age and composed of shale and argillaceous dolomite (Graese et al., 1988). The bedrock has been referred to as the "shallow dolomite aquifer" (Schicht et al., 1976; Sasman et al., 1982) and is known formally as the Upper Bedrock Aquigroup (Visocky, Sherrill, and Cartwright, 1985). R6E R7E R8E HAMPSHIRE M MAPLE PARK * -U U . *v '.. p ELBURN >MS v>~ I ELGIN SOUTH ELGIN * ' i \ CARPENTERSVILLE EAST DUNDEE WEST DUNDEE SLEEPY HOLLOW VALLEY VIEW ST CHARLES GENEVA BATAVIA NORTH AURORA AURORA SUGAR GROVE MONTGOMERY A j° mi - N Figure 3 Generalized distribution and well locations in relation to Kane County communities (screened areas). Dots indicate verified well locations. The bedrock surface, buried by Pleistocene glacial deposits, resembles modern topography featuring hills and valleys. Buried bedrock valleys generally contain the thickest deposits and the greatest volume of sands and gravels of glacial-fluvial origin. Geological reasoning points to the bedrock valley systems as having the greatest potential for containing predictable and high-yielding aquifers. Bedrock valley aquifers can be recharged not only from overlying drift, but by groundwater stored in fractures in weathered bedrock in the valley walls and immediately below the glacial drift. Valley-fill deposits not only consist of fluvial sands and gravels that are excellent aquifer materials, but also contain fine-grained diamicton (glacial till or debris flows) and lacustrine (lake bed) deposits that are poor aquifer materials, or aquitards. The ability to predict the location of aquifers and the water yield from these aquifers will improve as the bedrock-valley sediments continue to be explored and sedimentological models are developed to explain the genesis of the deposits. The Prairie Aquigroup (glacial or surficial deposits above the bedrock) has been informally divided into aquiformations, such as aquifers (water-yielding deposits) and aquitards (non- water-yielding deposits). Maps and cross sections show the distribution and thickness of aquiformations in the glacial drift in Kane County. How they were constructed and how they should be used to prospect for groundwater resources will be discussed under methods of investigation. The maps and cross sections depict the distribution and thickness of the various hydrostratigraphic units, including the St. Charles, Valparaiso, Bloomington, and Kaneville aquifers; the Pingree Grove and Elburn aquiformations; and the Marengo aquitard. An important hydrostratigraphic unit in the Prairie Aquigroup is the St. Charles aquifer consisting of sand and gravel that fills several buried bedrock valleys. This aquifer was the focus of testing by the Illinois State Geological and Water Surveys. The maps in this report are regional in scope, intended only for countywide planning. Areas have been mapped and units correlated by interpreting geologic information from drillers' logs or core samples. As in any geologic mapping, interpretations have been made between datum points, and the resulting maps and cross sections are considered to be the best present interpretations of the available data. This information is a reference for exploring, developing, and managing the groundwater resources of Kane County. METHODS OF THE HYDROGEOLOGICAL INVESTIGATION Geological mapping and surface geophysics were used to guide location and siting of test borings and production wells. Cross sections of the drift-filled buried bedrock valleys, prepared using well records and surface and borehole geophysics for correlation, aided in the design and interpretation of aquifer tests. Buried bedrock valleys, which were expected to contain major groundwater resources, were the focus of the investigations: 1. Preliminary maps of the buried bedrock surface were plotted using elevations of outcrops and records from water wells and test borings with verified locations as datum points (fig. 3). 2. Locations of buried bedrock valleys between datum points were interpreted using seismic refraction techniques (fig. 4). 3. Prospecting for sand and gravel deposits in bedrock valleys utilized electrical earth resistivity surveys. 4. Thickness and extent of sand and gravel bodies within the bedrock valley fill were determined by test drilling. In addition to existing sources of data, several new sources were used to construct maps and cross sections. These include seismic refraction studies conducted for the communities R6E R7E R8E T , i •i 1 42 N 7" l"* i ' *". T i 41 N I ~ i * * * *■■ ■■ i . ; I i i ■ftn, ' / I T 40 / - _-- -^ / • *''* N ^ s d|f 1 "iv. x y*- . '1. Lf r — T 39 N < 1 ■ / i -r ■| V; _ , - . « * 1 ' v v. — • • T {- -- !■ A 38 N 1 • . ^ .A' /I "*■ • -V*- * * ' . * .• (0-350) .•.•'••*.:y.r:± silt and loess peat and muck sand and gravel ■ ■*!■! T*...i?»irJ diamicton (clay, silt, sand, gravel, and 5S5S*SSS boulders = commonly till) Joliet-Kankakee (0-50) Elwood (0-30) Wilhelmi (0-"20T (0-210) dolomite, fine-grained, cherty shale, argillaceous dolomite and limestone (155-185) 7~7 \ 1 X F K rJ^=* dolomite, some limestone, fine- to medium- grained, slightly cherty (140-150) h-:—i-—i *&: Glenwood-St. Peter (60-520) ML.. ' ,-6. ' VUI ' $ '. \ l lj '. *** !'.. * ". '. sandstone, white, fine- to medium-grained, sandy o-.:.s.v.-v QL O (0-400) Eminence (20-150) Potosi (90-225) Franconia (75-150) dolomite, sandstone dolomite, fine to medium grained, sandy dolomite, fine grained, trace sand and glauconite sandstone, fine-grained, glauoonitic; green and red shale Ironton-Galesville (155-220) sandstone, fine- to medium-grained, dolomitic 53?*=S Eau Claire (350-450) sandstone, fine grained, glauoonitic; siltstone, shale, and dolomite Mt. Simon (1400-2600) sandstone, white, coarse grained, poorly sorted PRECAMBRIAN (13,000+) granite Figure 6 Stratigraphy of rocks underlying Kane County. 12 Stratigraphy Paleozoic The Galena, Maquoketa, Kankakee, and Elwood Formations are the most widespread units beneath the bedrock surface (fig. 7). Distribution of the geologic units is determined by the structure of the bedrock, thickness of the units, and most importantly on a local scale, the topography of the bedrock surface. Ordoviclan • Galena Group Composed of nearly pure medium- to fine-grained carbonates, both dolomite and limestone, the Galena also contains chert nodules and shaly zones, but these are not as common as in the underlying Platteville. The average thickness of the Galena is about 180 feet beneath Kane County (Graese et al., 1988). The Galena is present at the buried bedrock surface only where the dominant St. Charles bedrock valley exits Kane County on the southwest. • Maquoketa Group Composed of shale, argillaceous dolomite and limestone, and interbeds of shale and dolomite, the Maquoketa is as much as 210 feet thick in the northwest where it is overlain by the Kankakee Formation. The Maquoketa is not present, however, in the southwestern portion of Kane County in the bottom of the St. Charles bedrock valley. The regionally important formations of the Maquoketa include, in ascending order, the Scales Shale, Ft. Atkinson Limestone, Brainard Formation, and Neda Formation (Kolata and Graese, 1983); but these cannot be readily differentiated in Kane County (Graese, 1988; Graese et al., 1988). Instead, the Maquoketa consists of two sequences composed of basal shales that become increasingly carbonate rich. Figure 7 shows the distribution of lithologies dominated either by shale or dolomite. Silurian The Elwood and Kankakee Formations are composed of thin to medium-thick beds of dolomite; the Kankakee also contains abundant nodules and interbeds of chert. Because the lithology of these units is similar, they are not differentiated on figure 7. The thickness of the two units is more than 100 feet on the southeast of Kane County, where the Joliet Formation may be present as well. The Joliet is also composed of dolomite; and in the subsurface, it is difficult to distinguish from the underlying Kankakee. The Wilhelmi Formation may be present in places where the top of the Maquoketa is deeply eroded (Graese et al., 1988, p. 17); it is composed of argillaceous dolomite and domomitic shale (Willman et al., 1975, p. 26). The distribution of Silurian dolomite, as depicted in figure 7, is determined chiefly by the buried bedrock topography. The Silurian subcrop corresponds, in large part, to the bedrock valleys (fig. 10). The thickness of Silurian dolomite beneath the outliers in R.6.E. of Kane County is generally less than about 30 feet. Cenozolc Quaternary: Pleistocene The lithology of the Pleistocene glacial drift (fig. 8) has more diversity than that of the bedrock units (fig. 6). The distribution of the surficial drift units is shown on figure 8b. The bulk of the drift is composed of matrix-supported loam to clay diamicton (till), well-sorted to poorly sorted sand and gravel (outwash), subordinate stratified silt and clay (lacustrine deposits), and organic-rich, pedogenically altered sediment (buried soils). Many differences in the lithology of the glacial sediments can be explained in terms of the sedimentology (Eyles, 1983; Ashley, Shaw, and Smith, 1985). Predicting the occurrence of aquifers depends upon understanding the sedimentology of the glacial drift, which is important for understanding the resulting hydrostratigraphy because of the numerous unconformities and abrupt facies changes in drift sequences (Anderson, 1989). A glacial setting is dynamic, especially along the front of the ice sheet. The glacial front advances and retreats, and through time, covers or removes earlier deposits. The results are 13 R6E R7E R8E Kankakee and Elwood Fms dolomites S/n! Maquoketa shale/dolomite Galena carbonates A 10 mi [\J Figure 7 Paleozoic rock units outcropping at the buried bedrock surface (modified from Graese et al. 1988). 14 the fades changes previously mentioned (fig. 9). Sand and gravel deposits fill much of the buried bedrock valleys and occur as sheet deposits elsewhere in the county. In the St. Charles bedrock valley, these deposits are late Wisconsinan (about 25,000 years old), but in the Aurora bedrock valley, the deposits are lllinoian (more than 130,000 years old). Figure 9 shows several environments of glacial deposition. The stratigraphic framework (fig. 8) is helpful for understanding the sequence of events, and in some cases, for determining the continuity of sand and gravel bodies. The general history of continental glaciation in Kane County includes two major periods of glaciation, the lllinoian and late Wisconsinan, that were separated by a long, warmer, soil-forming interval (interglacial) during the Sangamonian and early to middle Wisconsinan (Curry, 1989). Pre-lllinoian glaciations probably affected Kane County, but deposits of this age have not been identified. The position of fluctuating glacial margins during the late Wisconsinan are marked by various landforms, including end moraines and outwash fans, but older deposits now covered have no surface expression. • lllinoian The oldest glacial drift identified in Kane County is lllinoian and may correlate to the Glasford Formation near Rockford in Boone and Winnebago Counties (Berg et al., 1985). Richmond and Fullerton (1986) suggest that the lllinoian spans from about 245,000 to 130,000 years ago. • Sangamonian and Early to Middle Wisconsinan lllinoian deposits are covered by Sangamonian and early to middle Wisconsinan colluvium composed of organic carbon-rich silty deposits that have been modified by soil formation; these include Berry Clay and Robein Silt (fig. 8). The soils were developed from about 130,000 to about 25,000 years ago (Curry, 1989). These sediments may be as much as 25 feet thick in Kane County, but are more commonly thin or absent. • Late Wisconsinan The late Wisconsinan Wedron Formation, Henry Formation, and related formations (Willman and Frye, 1970) cover the Robein Silt. Wedron Formation The bulk of the late Wisconsinan deposits belong to the Wedron Formation; its representative members in Kane County in ascending order are the Tiskilwa, Maiden, Yorkville, and Haegar Till Members (fig. 8). The till members can be separated on the basis of particle-size distribution, semiquantitative mineralogy of the less than 2-micron fraction, color, and stratigraphic position. Wickham, Johnson, and Glass (1988) and Graese et al. (1988) summarize these properties. Henry Formation The Henry Formation consists of sand and gravel; its distribution and thickness are relatively well known because of its importance as an aggregate resource (Masters, 1978). The Henry is subdivided into three members based on association with landforms (Willman and Frye, 1970), including the Mackinaw Member (valley trains), Wasco Member (kames and eskers), and the Batavia Member (fans and deltas). Equality Formation The Equality Formation is composed of stratified to massive sand, silt, and clay associated with sedimentation in lakes. The Dolton Member is composed of well-sorted fine- to medium-grained sand deposited along shorelines and spits; it is only locally present in large lake deposits in northern Kane County (Leighton et al., 1931; Wickham, Johnson, and Glass, 1988). The Carmi Member is composed of chiefly stratified or laminated silt, clay, and subordinate sand; it is a common surficial deposit across Kane County (Graese et al., 1988). Generally, it is less than 20 feet thick, but may be as much as 45 feet thick. 15 Genetic Interpretation of Materials and Description Alluvium — sand, silt, and clay deposited by streams Peat and muck, often interbedded with silt and clay Lake deposits — stratified silty clay and sand Outwash — sand and gravel Till — yellowish brown loam; extensive, thick basal sand and gravel yellowish brown to gray silty clay loam Till — yellowish brown to brownish gray loam to clay; extensive basal sand and gravel west of the Fox River* Till — pinkish brown to grayish brown clay loam* Buried soil developed into alluvium, colluvium or bog deposits — organic rich silt, sand and clay Accretion-gley — colluvium Outwash — sand and gravel Till — gray silty loam Till — pink sandy loam; extensive basal sand and gravel disturbed (quarries, sand and gravel pits) till interbedded with sand and gravel Figure 8a Stratigraphy of glacial drift (Prairie Aquigroup) underlying Kane County. Figure 8b Surficial drift map of Kane County (modified from Graese et al., 1988). 16 R6E R7E R8E esker esker delta facies contact supraglacial flow tills glacier proximal outwash facies distal outwash facies medial outwash facies basal till proximal '.•;.;■ .» :*£$D Bl Wm *y;« : '"ia '!»£?£. b 25 20 20 S3 gravel sand silt/clay Figure 9 Environments of glacial deposition (from Anderson, 1989). Dotted lines indicate facies contacts. 18 • Post-late Wlsconslnan and Holocene deposits Post-late Wisconsinan glacial deposits are thin and mantle the ground surface. Cahokia Alluvium (floodplain deposits) and Grayslake Peat are mapped on figure 8b. Richland Loess and Peoria Loess are generally less than 2 feet thick and have not been included on the maps for this report. Buried Bedrock Topography The bedrock surface has been mapped statewide by Horberg (1950) and in Kane County by Gilkeson and Westerman (1976), Wickham (1979), Wickham and Johnson (1981), and Wickham, Johnson, and Glass (1988). The bedrock topography map has been updated as a result of seismic refraction studies (Heigold, personal communication) and the test drilling for the proposed site for the Superconducting Super Collider in Illinois (Kempton et al., 1987a, 1987b; Curry et al., 1988; Vaiden et al., 1988). Additional data came from logs on open file at the Illinois State Geological and Water Surveys. The map in this report (fig. 10) is similar to the bedrock topography map in Graese et al. (1988). The elevation of the bedrock surface is less than 500 feet above mean sea level (msl) at the bottom of the St. Charles bedrock valley on the southwest of Kane County, and more than 825 feet above msl on the uplands to the northwest (fig. 10). The surface is dissected by several troughs that resemble modern valleys; the genesis of the bedrock valleys was probably similar to that of a modern valley system, but the possibility remains that some reaches were modified by glacial erosion during the Quaternary Period. The age of the valley fill varies, indicating that the history of the drainage network is complex. Burled Bedrock Valleys The individual buried bedrock valleys described below are indicated (by a stippled pattern) on the bedrock topography map (fig. 10). St. Charles bedrock valley The major bedrock valley under Kane County, the St. Charles bedrock valley, heads east near Elgin and parallels the Fox River on the north, diverging from and crossing beneath the Fox River just south of St. Charles. The St. Charles bedrock valley lies just west of Batavia and Geneva and trends southwest to pass beneath State Route 47 north of Sugar Grove and eventually exits Kane County on the extreme southwest. The St. Charles bedrock valley was once thought to extend south from Aurora to near the village of Newark in Kendall County, but new data suggest a westward route west of Kane County and eventual confluence with the Paw Paw bedrock valley in Lee County. The Paw Paw is a tributary to the ancient, buried channel of the Mississippi River (Horberg, 1950). Therefore, the bedrock valley formerly called "Newark" has been renamed the St. Charles bedrock valley. Aurora bedrock valley A major tributary of the St. Charles bedrock valley, the Aurora bedrock valley is a narrow, sinuous feature trending approximately east-west across the southern part of Kane County. The valley begins in western Du Page County east of Montgomery and passes beneath the Fox River in southern Aurora, trending west where it joins the St. Charles in southeastern Kane County (Graese et al., 1988). Other buried bedrock valleys Other tributaries to the St. Charles bedrock valley occur in Kane County. Prime targets for aquifer development include the Elgin bedrock valley that heads northwest of Elgin and joins the St. Charles bedrock valley west of St. Charles. Another prominent tributary is the Elburn bedrock valley that merges with the St. Charles about 2 miles south of Elburn. Other smaller, unnamed valleys are evident in figure 10 (although they are not marked by a pattern), including a valley that apparently trends toward Lake Michigan and may have joined ancient drainage to Hudson Bay or the St. Lawrence 19 R6E R7E R8E Elgin bedrock valley St. Charles bedrock valley Aurora bedrock valley A 10 mi. |\j Figure 10 Buried bedrock topography underlying Kane County. A stippled pattern indicates the major bedrock valleys. 20 River. Small valleys on the west of Kane County, including one near Maple Park, join the Troy bedrock valley in De Kalb County. These relations imply that the central part of Kane County was part of a preglacial drainage divide. Cross-valley topographic profiles of modern ground surface and the bedrock surface across the St. Charles and Aurora bedrock valleys and the modern Fox River Valley show similar relief of about 150 feet. The buried valley width varies from less than 2,000 feet to more than 3,000 feet. The steepest documented valley slope is about 13°, and the gradient of the St. Charles valley channel bottom is about 0.0006 feet per mile. Drift Thickness Glacial drift is more than 350 feet thick beneath the Marengo moraine and more than 200 feet thick above reaches of the St. Charles bedrock valley. Bedrock is locally exposed along the Fox River and a few tributaries. Drift is thickest beneath moraines and other positive glacial landforms such as kames, or above bedrock valleys, especially on the northern half of Kane County. Drift is thinnest in the southern part of Kane County along major drainageways and above outliers of Silurian dolomite. A drift thickness map (the result of subtracting the elevation of the bedrock surface from U.S. Geological Survey 7.5-minute topographic maps) will soon be available for Kane County (ISGS, 1990). It can be used with aquifer maps to give a crude indication of the level of natural protection afforded the aquifers described in this report. HYDROGEOLOGY Definitions of Aquifers The term aquifer has been used in Illinois in different ways (Seaber, 1989). Aquifers in geologic mapping have been defined as (1) relating groundwater to the classical geological (lithostratigraphic) framework without detailed regard for hydraulic continuity, (2) relating groundwater occurrence to the hydraulic properties within the classical geologic framework, (3) showing groundwater as a resource, (4) showing the relationship of groundwater to water-bearing characteristics of the rocks and the dynamics of the hydrogeological regime, and (5) hydrostratigraphic units. Usage and mapping has been strongly influenced by existing conventions. The term aquifer has been used in many different senses in the past in Kane County, but only hydrostratigraphic nomenclature is used in this report. A comparison of the hydrostratigraphic names used in this report and previous, informal usage is given in table 1 . Table 1 Informal classifications of drift aquifers compared with hydrostratigraphic units in the Prairie Aquigroup, as used in this report McFadden et al. (1989) Upper sand and gravel aquifer Lower sand and gravel aquifer Schicht et al. (1976) Surficial sand and gravel aquifer Interbedded sand and gravel aquifer Basal sand and gravel aquifer Graese et al. (1988) Surficial drift aquifer Basal drift aquifer Buried drift aquifer This report (Prairie Aquigroup) Valparaiso aquifer Kaneville aquifer, Elburn aquiformation Bloomington aquifer Pingree Grove aqui- formation St. Charles aquifer 21 Bloomington aquifer Marengo aquitard Kaneville aquifer member of the Elburn aquiformation Valparaiso aquifer Elburn aquiformation Kaneville aquifer member Marengo aquitard silt till sand and gravel ^^^ buried soil \//\ bedrock Marengo aquitard St. Charles aquifer Figure 11a Schematic diagram showing relations of hydrostratigraphic units identified in this report. Haeger Till Member, Wedron Fm Figure 11b Schematic diagram showing relations of glacial drift units identified in this report. 22 Table 2 Hydrostratigraphic hierarchy in Kane County. Aquigroup Aquiformation Aquimember "Valparaiso aquifer Elburn aquiformation Kaneville aquifer member Prairie — | Bloomington aquifer Pingree Grove aquiformation Marengo aquitard St. Charles aquifer Hydrostratigraphy Hydrostratigraphy is the classification and mapping of significant units of rock with respect to distinctive porosity and permeability. It provides a framework within which to evaluate flow systems-whether the flow system is statewide or larger (regional), countywide (intermediate), or local. A hydrostratigraphic unit, which may occur in one or more material rock units, is unified and delimited by its hydrologic characteristics and interstices or voids. They are defined by the number, size, shape, arrangement and interconnection of the interstices, and recognized on the basis of the nature, extent, and magnitude of the interstices in any body of sedimentary, metamorphic, or igneous rock. Concepts of hydrostratigraphy are reviewed in Seaber (1988), and practical applications are presented in Visocky, Sherrill, and Cartwright (1985). The hierarchy of hydrostratigraphic units, in order of decreasing rank, is aquigroup, aquiformation, aquimember, and aquibed. The fundamental unit of hydrostratigraphic classification is the aquiformation. One criteria of aquiformation is that it be mappable at the scale in the area where the aquiformation is defined. Table 2 shows the relations of the various divisions or hierarchy of hydrostratigraphic units used in this report. Informal hydrostratigraphic names are used for aquiformations (such as the St. Charles aquifer; table 2, fig. 11a), which are subdivisions of aquigroups. Aquigroups and aquiformations are part of the concept of hydrostratigraphic units. Aquigroups are large bodies of rock distinguished by porosity and permeability, as well as by lithology, from overlying and underlying rock groupings. Aquiformations, which are equivalent to formations in geologic mapping, are the fundamental units of hydrogeologic mapping. Hydrostratigraphic units were formally defined for the area by Visocky, Sherrill, and Cartwright (1985). The Prairie and Upper Bedrock Aquigroups provide the shallow groundwater resources for Kane County (fig. 6). As figures 11a and 11b show, the physical relations of hydrostratigraphic and glacial drift units may be complex. Both horizontal and vertical distribution must be used for proper aquifer assessment. The relationship of the glacial units, which are lithostratigraphic in nature, and the hydrostratigraphic units, which are dependent upon porosity and permeability, must be carefully detailed. Upper Bedrock Aquigroup The Upper Bedrock Aquigroup consists of local and intermediate flow systems in indurated sediments with open connection to the glacial drift that composes the Prairie Aquigroup. The rocks are of Ordovician and Silurian age. The most significant and productive aquifer is the Silurian dolomite aquifer or shallow dolomite aquifer (fig. 7), which is most productive in the eastern half of Kane County where this resource sustains pumping rates as great as 100 to 200 gpm (Visocky, Sherrill, and Cartwright, 1985). In these areas, large yields are sometimes obtained, reducing the dependence on the deeper aquifers. Most of the water is obtained in the uppermost 100 feet of rock; however, it is difficult to predict where the fractured and 23 vuggy bedrock occurs. The most productive wells constructed in the drift likely will be those that take advantage of buried bedrock valleys with sand and gravel aquifers that are hydrologically connected to fractured bedrock. Prairie Aquigroup Prairie Aquigroup deposits are Quaternary in age; most are late Pleistocene deposits of Wisconsinan age. In Kane County, the Prairie Aquigroup has local and intermediate flow systems in noncemented geologic materials — glacial drift, alluvium, and other Holocene sediments. The aquifers are confined locally by fine-grained sediments. Recharge to the system is mainly from local precipitation. The aquifers shown on figure 2 and plate 1 are at least 50 feet thick, whereas the actual hydrostratigraphic units have greater areal extent. Visocky, Sherrill, and Cartwright (1985) provided a framework for bedrock hydrostratigraphy and named the Upper Bedrock Aquigroup; they also named the Prairie Aquigroup as the hydrostratigraphic unit composed of glacial drift. However, no previous reports describe or define subunits, such as aquiformations or aquimembers within the Prairie Aquigroup. Kane County is geographically unique in that several regionally important aquifers lie within the drift. The areas of relative potential for groundwater development in the Prairie Aquigroup, where the units are more than 50 feet thick, are shown on figure 2 and plate 1. St. Charles aquifer Composed chiefly of stratified to massive sand and gravel deposits up to 120 feet thick, the St. Charles aquifer also includes beds of diamicton. A continuous aquifer thickness of 50 feet is maintained to about 3,000 feet laterally across the buried bedrock valleys; the continuity may be interrupted by restricted deposits of till or other non- water-yielding materials (figs. 12 and 13). The St. Charles aquifer is composed chiefly of sand and gravel facies of the Wedron and the Glasford Formations. The distribution of the St. Charles aquifer, where it exceeds 50 feet in thickness, is shown along with other glacial drift (Prairie Aquigroup) aquifers on plate 1. The vertical relation of the St. Charles aquifer to other Prairie Aquigroup members is shown in several cross sections (figs. 12 and 13). The large vertical exaggeration of these cross sections highlights the relations between units. 700 MSL Elburn aquiformation 600 Elburn aquiformation MSL 700 feet 600 vertical exaggeration = 105.6 Figure 12 Cross sections of Aurora bedrock valley. Section lines B-B' and C-C are located on figure 2 and plate 1. 24 MSL — 700- Elburn aquiformation Kaneville aquifer "' member Marengo aquit&fljj- 600 — 500 MSL — 700 — 600 — 700 feet 600 500 — i MSL Marengo aquitard - 500 3 tin sand and gravel ^^^ buried soil [//] bedrock Marengo aquitard St. Charles aquifer 700 feet 600 1500 vertical exaggeration = 105.6 Figure 13 Cross sections of the St. Charles bedrock valley. Section lines D-D' and E-E' are located on figure 2 and plate 1. The Marengo aquitard is shaded. 25 MSL 1000- 900- 800- Marengo aquitard Bloomington aquifer <<#£,## ■ 90 ° Upper Bedrock Aquigroup 1000 feet - 800 MSL 1000- MSL Pingree Grove Aquiformation j — Marengo aquitard I Pingree Grove Aquiformation - 900 70(>I Bloomington aquifer wX^C^f - >t\ ->i\\*?? 1000 feet 800 700 I- ■'.'/'-''" J sand and gravel ^^n buried soil \//\ bedrock Marengo aquitard Figure 14 Cross sections showing the Marengo aquitard in relation to the Bloomington aquifer. 26 Marengo aqultard As much as 300 feet thick beneath the Marengo moraine, the Marengo aquitard covers the St. Charles aquifer in much of Kane County (fig. 12 and 13). The aquitard is chiefly made up of diamicton in the Tiskilwa Till Member of the Wedron Formation (Wickham, Johnson, and Glass, 1988). This fades is predominantly composed of pinkish, massive loam diamicton (till). The Marengo aquitard has a field-measured hydraulic conductivity on the order of 10' 6 and 10" 8 cm/sec (Jennings, 1987). Relatively small bodies of sand and gravel have been sporadically found in the Marengo aquitard, but these supply only small, local groundwater supplies for households. Pingree Grove aquiformation This unit is composed of stratified sands, silt, clay, marl, and peat; it underlies present lakes, rivers, and streams. The aquiformation is thickest and most widespread beneath former lakes, most of which have naturally dried up or been drained for agriculture. The Pingree Grove aquiformation is as much as 50 feet thick on the north of Kane County, where the lower portion is commonly composed of sorted sands (Wickham, Johnson, and Glass, 1988) that may have limited potential as aquifers for households. Most commonly, however, the Pingree Grove is less than 20 feet thick and should not be considered an aquifer for large municipal, agricultural, and industrial supplies; thus it is not shown on figure 2 and plate 1 . The Pingree Grove aquiformation is composed of the Equality Formation, Greyslake Peat, and Cahokia Alluvium. Bloomington aquifer Located west of the Marengo ridge or moraine, the Bloomington aquifer is a surficial deposit or locally buried by the Marengo aquitard (fig. 14). It does not necessarily occur in the buried bedrock valleys. The deposit is composed of very poorly sorted gravelly sand generally less than 50 feet thick, and becomes thinner and finer grained to the west. The water quality and yield characteristics of this aquifer have not been tested. The Bloomington aquifer is composed of the Henry Formation and the sand and gravel facies of the Tiskilwa Till Member of the Wedron Formation. North of Kane County, the Bloomington aquifer merges with the Valparaiso aquifer. Elburn aquiformation This unit, which underlies most of central and south-central Kane County, is primarily an aquitard (chiefly diamicton, but also lacustrine deposits); it also contains mappable bodies of sand and gravel that can be considered aquifers. Thus the Elburn is designated an aquiformation rather than an aquifer or aquitard. The Kaneville aquifer member of the Elburn aquiformation represents a mappable body of rock that is an aquifer but is thought to be limited in extent and somewhat discontinuous. The Kaneville aquifer member is as much as 100 feet thick and overlies the St. Charles aquifer in the Sugar Grove and Montgomery areas (fig. 13). The Elburn aquiformation is composed of parts of several lithostratigraphic units, including the Henry Formation, and the Maiden and Yorkville Till Members of the Wedron Formation. Valparaiso aquifer Currently the most productive drift aquifer in Kane County (Appendix 4- 5), the Valparaiso aquifer is the least extensive areally (plate 1, fig. 2). It is located immediately below ground surface on the northeast of Kane County; it is more extensive east and north of the county. The aquifer is more than 100 feet thick and composed of sand and gravel that becomes thinner and finer grained to the west (Fraser and Cobb, 1982; Hansel, Masters, and Socha, 1985). Significant reserves have been removed as sand and gravel aggregate (Masters, 1978). In Kane County, the Valparaiso aquifer is composed of the Henry Formation and Haeger Till Member of the Wedron Formation. SUMMARY OF FINDINGS OF THE INVESTIGATION Conditions are favorable for development of shallow groundwater resources for public, industrial, and agricultural supplies in Kane County. In this report, the Illinois State 27 Geological Survey defined and described hydrogeologic units within the Prairie Aquigroup and Upper Bedrock Aquigroup, both hydrostratigraphic groupings. Aquiformations, or mappable hydrogeologic units, were defined for the first time for the Prairie Aquigroup. The areas with the best potential for groundwater development in the glacial drift are shown on figure 2 and plate 1 . The entire extent of the hydrostratigraphic units is not shown on figure 2 and plate 1 , but only those areas where the thickness of the aquifers exceeds 50 feet. These are the most favorable areas for the development of municipal, industrial, and agricultural supplies of water because an aquifer with a thickness of 50 feet or more will produce the largest yields to individual wells and well fields. "How much groundwater is available?" is a reasonable question frequently raised by local officials charged with the task of managing groundwater resources (Illinois Technical Advisory Committee on Water Resources, 1967). The resource lends itself to quantitative assessment (U.S. Water Resources Council, 1973). However, groundwater reservoirs are dynamic in nature; their withdrawal rates and patterns of extraction can be managed. Therefore, the development of the resource is subject to alternative plans, which may differ in their effects on yield potential, longevity of the supply, cost of recovery, impacts on other groundwater reservoirs or interconnection with surface water, and water quality. The Illinois State Water Survey is preparing a separate report on the water quality and potential yield of these hydrostratigraphic units. The Illinois State Geological and State Water Surveys are also preparing reports on several communities in Kane County. 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Mabey, 1974, Application of surface geophysics to ground-water investigations, chapter D1 , Techniques of Water-Resources Investigations of the USGS, book 2: U.S. Geological Survey, 116 p. 33 APPENDIX !e sill :l llll „„ £ . 34 If i »» o i- no 8 * | uu|||5| o" o 0) j) 2 IE !2 g I $Z If si « »1 " « — -c~~ E S * 1 O < "O m uj 3 E E V) 0) Q.Q. m tO iC -a »-c .c _* . uut-o) uji oioi l 3 u _* > a>a> oo a> o <_> o < -, l_ i- l_ % U iO C C t- E -O <0 C O.Q. t-I- r— . - f— I3334J 3«— 003 •— •— r- 0) m ^wq.« > > j . i -. r- oo i- «r in co ■» co •»■ O -J CO te i — (nj in co If! ,--6 2 pi 36 Table A-5 Mean and sample standard deviation of water quality data from the Prairie Aquigroup, Upper Bedrock Aquigroup, and Midwest Bedrock Aquigroup in Kane County (|ig/l) Aquifer (no. analyses) Alkalinity Ca ++ CI" Hard- ness Fe ++ , Fe t++ Mg ++ K + Na + so/' TDS Ba ++ Prairie Aquigroup (29) 329.2± 32.3 88.7± 19.9 33.9± 32.5 400.8± 83.7 1.3± 1.0 44.8± 8.3 2.3± 1.0 18.4± 13.7 67.5± 33.9 472.6± 93.3 0.1± 0.1 Upper Bedrock Aquifer (13) 323.5± 28.3 73.2± 22.5 10.1± 7.9 347.8± 98.3 1.5± 1.9 39.9± 10.5 2.7± 1.8 34.3± 36.9 88.4± 38.5 472.5± 81.6 0.0± 0.1 Midwest Bedrock Aquigroup (12) 287.0± 15.6 58.7± 4.3 8.9± 10.4 247.0± 19.2 0.1± 0.1 24.3± 2.5 11. 5± 2.6 26.2± 10.0 17.6± 17.7 340.3± 24.3 1.8± 3.0 37 MOW mi NZtl 3NV)I Nl mvM onand jo d hum saajinov saDjnosad iBiniBN pug A6j9u 3 |o luaujpedaa A3AHHS 1V0I9O1O3O 31V1S SI0NIT1I Contract Report v AQUIFERS WITH POTENTIAL FOR DEVELOPMENT OF PUBLIC WATER SUPPLIES: PRAIRIE AQUIGROUP IN KANE COUNTY, ILLINOIS [HH ST. CHARLES AQUIFER 50-100 ft >100 ft CD | 1 VALPARAIS0 AQUIFER CZ3 I I BL00MINGT0N AQUIFER R— i r-r— j KANEVILLE AQUIFER MEMBER UluiU) bii^J 0F TH[ [LBURN AQUIF0RMATI0N specific capacity tests (gpm/ft) H >150