Introduction

Buried valleys are prominent features that have been identified in the Pleistocene sedimentary record from glaciated terrains worldwide, especially in the Northern Hemisphere. They have been the focus of recent studies, especially in North America and Europe, because they hold significant supplies of groundwater and economic shallow gas, contain aggregate for construction, may be pathways for the movement of contaminated groundwater and typically have a more complete sedimentary record that can be used to model past geological processes and Earth’s climatic conditions. Determining the architecture and internal complexity of these heterogeneous deposits is of critical importance in understanding how the natural resources can be utilized in an economical and environmentally responsible manner.

By definition, buried valleys are deep channel-form features incised into the underlying sediment or bedrock by flowing water or glacial scouring, which have been completely filled in and covered over by more recent deposits of unconsolidated sediment (Type I valleys; Reference SainesSaines, 1968). They are present near the land surface, but because of the aforementioned sediment mask, these features have no geomorphological expression at the land surface. Therefore, they cannot be mapped from surficial geological data. Also, they are particularly difficult to delineate from the available geologic logs in boreholes drilled for water resources and engineering testing in these areas. Typically, these boreholes do not fully penetrate the valley fills, are irregularly spaced and/or are too few in number. Collecting the required subsurface information that alone would thoroughly delineate these features is too expensive.

Owing to these limitations, complementary geophysical methods have been employed to investigate buried valleys (Reference Hunter, Pullan, Burns, Gagne and GoodHunter and others, 1984; Reference Gabriel, Kirsch, Siemon and WiederholdGabriel and others, 2003; Reference Jørgensen, Lykke-Andersen, Sandersen, Auken and NørmarkJørgensen and others, 2003). These non-invasive methods have been effective in delineating their morphology and dimensions. Buried valleys are typically long, extending several kilometers to tens of kilometers, hundreds of meters to kilometers wide and are several tens to hundreds of meters deep (e.g. Reference Huuse and Lykke-AndersenHuuse and Lykke-Andersen, 2000; Reference StackebrandtStackebrandt, 2009; Reference Cummings, Russell and SharpeCummings and others, 2012). The glacially derived sediments that fill buried valleys often have a lithology, mineralogy, consistency and moisture content that differs significantly from the surrounding bedrock or sediments into which the valleys have been incised. These differences allow many geophysical methods to be used in their study. The geophysical methods provide laterally continuous information across the buried valleys.

Of these geophysical methods, high-resolution seismic reflection (HRSR) surveys have been the primary method used in North America (Reference Sharpe, Pugin, Pullan and GorrellSharpe and others, 2003; Reference Ahmad, Schmitt, Rokosh and PawlowiczAhmad and others, 2009; Reference Pugin, Pullan, Hunter and OldenborgerPugin and others, 2009; Reference Pugin and PullanPugin and Pullan, 2011) and northern Europe (Reference Huuse, Lykke-Andersen and PiotrowskiHuuse and others, 2003; Reference Kristensen, Huuse, Piotrowski and ClausenKristensen and others, 2007; Reference AukenAuken and others, 2009; Reference Reitner, Gruber, Römer and MorawetzReitner and others, 2010) to delineate buried glacial valleys. The use of HRSR surveys has increased in the past decade because seismic land-streamer technologies have been developed that are more efficient than the conventional method of planting geophones (Reference Van der Veen and GreenVan der Veen and Green, 1998; Reference Van der Veen, Spitzer, Green and WildVan der Veen and others, 2001). Subsequently, data from HRSR surveys enable a better delineation of finegrained sediments (silt and clay) from coarse-grained sediments (medium to very coarse sand and gravel) if the deposits being imaged are sufficiently thick relative to the wavelength of the applied seismic signals (Reference Bradford, Sawyer, Zelt and OldowBradford and others, 1998; Reference MusilMusil and others, 2002; Reference Kilner, West and MurrayKilner and others, 2005; Reference Jørgensen and SandersenJørgensen and Sandersen, 2008; Reference Pugin and PullanPugin and Pullan, 2011). The analysis and interpretation of the HRSR data allow for quantitative descriptions of heterogeneity of sedimentary sequences in buried valleys that can be utilized to develop conceptual models for buried-valley incision (e.g. Reference Cummings, Russell and SharpeCummings and others, 2012).

In northern and central Illinois, HRSR surveys have been conducted over the last 10 years to delineate bedrock valley systems concealed by thick sequences of glacial sediment deposited during multiple Pleistocene glaciations (Reference Pugin, Larson, Sargent, McBride and BexfieldPugin and others, 2004; Reference Ismail and SargentIsmail and Sargent, 2006; Reference Ismail, Smith, Phillips and StumpfIsmail and others, 2012). This geophysical method was found to be best suited to subsurface investigations in Illinois because of the relatively high clay and moisture contents in the glacial sediment and the presence of shale bedrock, subsurface properties that limit the use of many other geophysical methods, including electrical resistivity and electromagnetic methods (Reference AhmadAhmad, 2006; Reference Smith and SjogrenSmith and Sjogren, 2006). Likewise, ground-penetrating radar was found to have a very limited depth of penetration, typically less than a few meters (Reference Larson, Phillips, Sargent and HardyLarson and others, 1999).

Typically, the HRSR data are collected as part of an integrated research program where other types of geophysical data are collected and exploratory drilling is conducted. Without this complementary subsurface information, the development of a conceptual geological framework from the HRSR data is difficult due to the complex character of valley-fill sediments (cf. Reference Kilner, West and MurrayKilner and others, 2005; Reference AhmadAhmad, 2006; Reference Pugin, Pullan, Hunter and OldenborgerPugin and others, 2009). Commonly, the buried valleys are filled with heterogeneous deposits containing fluid-saturated porous and permeable sand and gravel interstratified with low-porosity and low-permeability diamicton, very fine sand, silt or clay.

This study will demonstrate the application of HRSR profiling using a land streamer to delineate a buried valley (Pesotum Bedrock Valley) and characterize its filling sediments where limited subsurface information from drilling or down-hole geophysical surveys is available. This research was undertaken as part of an integrated geological and geophysical investigation to support the construction of a regional-scale hydrogeological model for central Illinois. The HRSR profiling will provide laterally continuous images of the subsurface that can be compared with the geological and geophysical data collected in boreholes along the lines of survey. These results can be used to delineate the architecture and structure of the buried valley, which may hold insight into the subaerial and subglacial processes that were active in front of, or under, glaciers.

Regional Geology

Over the last ∼1 Ma, the landscapes in Illinois have been repeatedly modified by glaciers and their associated melt-waters during at least three major glacial periods during the Pleistocene epoch. In central Illinois, the present-day topography has little or no resemblance to the preglacial landscape that formed over many millions of years since 4 the Pennsylvanian period that ended 299 Ma ago. Prior to the first glacial advance during the pre-Illinois Episode, the landscape was characterized by rolling to gently undulating uplands that were dissected by an integrated system of valleys deeply incised into the bedrock (Fig. 1a; Reference Herzog, Stiff, Chenowith, Warner, Sieverling and AveryHerzog and others, 1994). These valleys contained steeply sloping walls much like the modern-day Ozark Plateau in Missouri, USA (Reference Kolata, Kolata and NimzKolata, 2010). The bedrock surface has since been buried completely by thick successions of sediment deposited during glacial and interglacial periods.

Fig. 1. Location of the study area in central Illinois, USA. (a) Regional view of the Mahomet aquifer covering 15 counties in central Illinois. The axes of major bedrock valleys are shown. (b) Axes of bedrock valleys superimposed on a hill-shaded digital elevation model representing the topography of the land surface. End moraines form the concave-shaped ridges shown on the model and mark the position of ice margins of glacial advances during the Wisconsin Episode. Glaciers during the Wisconsin Episode reached their terminal positions ∼60 km south of the study area. The study area is outlined by the black box. On the inset map, the three seismic reflection surveys and three control boreholes (discussed in the text) are located over the Pesotum Bedrock Valley. A fourth borehole was drilled over another bedrock valley under the cities of Champaign and Urbana.

Prior to the first glacial advance into Illinois, the bedrock valleys in central Illinois formed part of an expansive drainage network (Teays-Mahomet Bedrock Valley System; Reference FidlarFidlar, 1943; Reference HorbergHorberg, 1945; Reference Ver SteegVer Steeg, 1946) containing rivers and streams with headwaters in the Appalachian Mountains (Reference Kempton, Johnson, Heigold, Cartwright, Melhorn and KemptonKempton and others, 1991) that flowed several hundreds of miles to the west, draining into the Middle Illinois and Mackinaw Bedrock Valleys (Fig. 1a) in western Illinois. At this time, the Ancient Mississippi River flowed in the Middle Illinois and Mackinaw Bedrock Valleys. The Pesotum Bedrock Valley, the focus of this study, was a northwest-southeast-trending tributary of the Mahomet Bedrock Valley (Fig. 1b). The Pesotum Bedrock Valley is a preglacial valley incised into Pennsylvanian-age shale and siltstone bedrock that is present on the western flank of the La Salle Anticlinorium. Along this structure folded Silurian-age dolomite and limestone (444-398Ma old) outcrops at the bedrock surface (Reference NelsonNelson, 1995).

A conceptual geological framework for the Pleistocene glaciations and the preglacial period in central Illinois has been developed from the available subsurface information. These data were collected from exploratory boreholes drilled to install groundwater-monitoring wells and domestic water supply wells, including three control boreholes (Figs 1 and 2a-c) completed for this study (Stumpf and Dey, in press).

Fig. 2. Geological and geophysical logs for control boreholes over the Pesotum Bedrock Valley and an adjacent bedrock valley under Champaign and Urbana. (a) Borehole 1 : 39.9438098°N, 88.3125008° W; (b) borehole 2: 40.0181168°N, 88.3319428°W; (c) borehole 3: 40.0123768°N, 88.2749308° W; and (d) borehole 4: 40.1008548°N, 88.2290668°W. The lithostratigraphic units of Stumpf and Dey (in press) are assigned to seismic units and correlated with a diachronic classification and marine oxygen isotope stages of Reference Cohen and GibbardCohen and Gibbard (2011).

During the Pleistocene glacial advances, ice flowed along and across the bedrock valleys in central Illinois to terminal margins in western and southern Illinois (Reference Curry, Grimley, McKay, Ehlers, Gibbard and HughesCurry and others, 2011). Glaciers of the earliest advances during the pre-Illinois and Illinois Episodes disrupted and diverted the preglacial drainage patterns in these bedrock valleys (Reference Kempton, Johnson, Heigold, Cartwright, Melhorn and KemptonKempton and others, 1991; Reference Soller, Price, Kempton and BergSoller and others, 2000; Stumpf and Dey, in press). In the major valleys, meltwater flowing away from the ice margins carried large amounts of coarse-grained sediment (sand and gravel) down-valley. In the tributary valleys, the meltwater was ponded behind dams of ice or sediment. Where the meltwater entered lakes, deposits of finer-grained sediment (fine sand, silt and clay) accumulated. Subsequently, after these glacial advances, the valleys were completely filled in with the outwash and lake sediment, and thick layers of clayey diamicton (till).

Later glacial advances during the Illinois and Wisconsin Episodes deposited additional sediments over the buried valleys (Reference Kempton, Johnson, Heigold, Cartwright, Melhorn and KemptonKempton and others, 1991; Reference Hansel and JohnsonHansel and Johnson, 1996; Stumpf and Dey, in press). In one area of central Illinois, predominantly west-east-trending end moraines (Fig. 1b), formed during the last glaciation (Wisconsin Episode) ending ∼10 000 years ago, overlie the buried bedrock valleys, completely obscuring the topography of older land surfaces. Specifically, over the Pesotum Bedrock Valley, deposits of glacial sediment (∼50m thick) lie above the valley, which is filled by 35 m of glacial and nonglacial sediment (Fig. 2a-c).

The sediments encountered in the Pesotum Bedrock Valley have been classified by Stumpf and Dey (in press) to lithostratigraphic units in the same manner as Reference Willman and FryeWillman and Frye (1970) and Reference Hansel and JohnsonHansel and Johnson (1996). Diamicton, silt and clay, and sand and gravel were deposited during multiple glacial and nonglacial periods. The oldest sediments (diamicton, silt and sand, and sand and gravel) are preglacial in origin, classified to the undifferentiated lowermost unit of the Banner Formation (Fig. 2a-c), were encountered at the bottom of bedrock valley and compose alluvial or colluvial deposits. These sediments overlie bedrock that is commonly soft and friable, suggesting that the bedrock surface was exposed to a period of surficial weathering before being buried.

In the Pesotum Bedrock Valley, the preglacial sediment is stratigraphically overlain by diamictons (tills) and glacial lake sediment (Fig. 2a-c) deposited during the pre-Illinois Episode (marine isotope stages (MIS) 16 (∼620 ka) and 12 (∼430 ka); Reference JohnsonJohnson, 1986; Reference Hansel, McKay, Kolata and NimzHansel and McKay, 2010). These sediments are classified to the Banner Formation of Reference Willman and FryeWillman and Frye (1970). The deposits of glacial lake sediment are conformably overlain by tills. Massive deposits of clay with silt at the bottom part of the glacial lake sequence coarsen upwards into laminated or bedded silt and clay with drop stones and then interbedded silt, very fine sand and diamicton lying under massive diamicton (till). The uppermost till of the Banner Formation, the Hillery Member till, contains remnants of a paleosol that contains a Bt soil horizon (cf. Reference Hall and AndersonHall and Anderson, 2000), represented by intense oxidation, well-expressed soil structure and clay films, and leaching of primary carbonate minerals thought to be part of the Yarmouth Geosol of Reference LeverettLeverett (1898) and Reference Willman and FryeWillman and Frye (1970). The Yarmouth Geosol developed during an interglacial that was part of a ∼230ka long period (Yarmouth Episode) following the end of the pre-Illinois Episode glaciation (Reference Hansel, McKay, Kolata and NimzHansel and McKay, 2010). The Pesotum Bedrock Valley has a more complete record of the pre-Illinois Episode glaciation than the larger Mahomet Bedrock Valley to the north (Fig. 1) where erosion during later glacial advances removed much of the pre-Illinois stratigraphy (Stumpf and Dey, in press).

In the Pesotum Bedrock Valley, the Hillery Member till is overlain by sand and gravel (outwash) and/or diamicton and silt and clay (glacial lake sediment) (Fig. 2a-c) deposited during the Illinois Episode (MIS 6) between ∼190 and 130ka (Reference Curry, Grimley, McKay, Ehlers, Gibbard and HughesCurry and others, 2011). These sediments are classified to the Pearl and Glasford Formations of Reference Willman and FryeWillman and Frye (1970). The diamicton present in the lower part of the Illinois Episode stratigraphy is classified to the Vandalia Member till, whereas diamicton in the upper part of the Glasford Formation is interstratified with deposits of sand and gravel or silt and clay and interpreted as ice-marginal and ice-contact sediments that were deposited as glaciers of the Illinois Episode melted (Reference Atkinson, Ross, Stumpf and IsmailAtkinson and others, 2011a,Reference Atkinson, Ross, Stumpf and Ismailb), and classified to the undifferentiated unit of the Glasford Formation (Stumpf and Dey, in press). Remnants of a second interglacial soil (Sangamon Geosol; Reference Willman and FryeWillman and Frye 1970; Reference Follmer, McKay, Lineback and GrossFollmer and others, 1979) are present in sediments at the top of the Illinois Episode stratigraphy. An organic-rich A soil horizon and/or thin B soil horizon in the paleosol are represented by olive to very dark brown clayey sediments that developed during the Sangamon Episode.

In the study area, deposits of the Illinois Episode are overlain by loam- to silt loam-textured diamictons (tills) classified to the Tiskilwa and Lemont Formations (Fig. 2a–c) deposited during the Wisconsin Episode glaciation (Reference Hansel and JohnsonHansel and Johnson, 1996). Collectively, these tills are 25–35 m thick. The uppermost till, classified to the Batestown Member, Lemont Formation, is the lithology that comprises most of the moraines encountered on land surface (Fig. 1b).

Data and Methods

HRSR data were acquired along three profiles (710, 801 and 802) totaling 21 km over the Pesotum Bedrock Valley in central Illinois (Fig. 1b) using a land-streamer system. The land-streamer system comprises 48 40 Hz geophones spaced 3 m apart, and the source was a 50 kg accelerated weight drop. The source and streamer were moved at 6 m intervals, resulting in a 12 common depth point (CDP) fold of coverage.

The seismic data were processed using Landmark Graphics ProMax software. A basic processing scheme was applied to the data following the processing conceptions of Reference Hunter, Pullan, Burns, Gagne and GoodHunter and others (1984), Reference MillerMiller (1992) and Reference YilmazYilmaz (2001). A very careful top mute of the direct and refracted arrivals was applied to avoid interpreting these arrivals as coherent reflector events (Reference Steeples and MillerSteeples and Miller, 1998). A combination of top mute, bandpass filtering and f-k filtering was effective in suppressing the noise in the data caused by high-frequency airwaves and low-frequency ground roll (Fig. 3). The processed data were imported into the Seismic Micro-Technology Kingdom Suite software for plotting and interpretation.

Fig. 3. P-wave land-streamer seismic record from profile 801. A dramatic improvement in signal-to-noise ratio is obtained by processing the data. (a) Raw shot gather, (b) top mute, (c) bandpass filter and automatic gain control (AGC), and (d) f-k filtered.

To facilitate and verify the seismic interpretations, synthetic seismograms were derived from down-hole P-wave velocity data collected by vertical seismic profiling from control boreholes 1 and 2 drilled over the Pesotum Bedrock Valley (Figs 1 and 2a and b). A third borehole was drilled over the valley, but only a P-wave velocity log was collected using a full waveform sonic probe (Fig. 2c). Continuous cores of the sediments and shallow bedrock were obtained in boreholes 2 and 3. In borehole 1, core was not collected; only sieved samples of the drill cuttings were obtained every 0.6 m. These data were compared with measured HRSR data collected at the same borehole location (Fig. 4). This procedure ensures direct correlation between the seismic reflectors and lithological boundaries and supports seismic interpretations. Interpretations of the seismic profiles, based on a mix of seismic stratigraphic and facies analysis, are constrained by sediments encountered in a borehole.

Fig. 4. Correlating the synthetic seismogram generated from the seismic velocity log assuming constant density (middle panel) with the measured seismic reflection data (to the left) from borehole 2. The generalized log of the geology encountered in the borehole with corresponding diachronic and seismic units is shown on the right.

Results

The P-waves penetrated through the entire valley fill, reaching the more compacted preglacial sediment of the Banner Formation at the bottom of the Pesotum Bedrock Valley and imaging the underlying bedrock surface. The configuration or frequency, amplitude and continuity of the seismic reflections are described and used, in part, to characterize the sediments and bedrock following the procedure of seismic facies interpretation introduced by Reference Mitchum, Vail, Thompson and PaytonMitchum and others (1977) and Reference Sangree and WidmierSangree and Widmier (1979). In this study, the high-amplitude reflectors correspond to the following lithological contacts: (1) the base of Tiskilwa Formation till; and (2) the bedrock surface (Fig. 4). Other reflectors of medium to weak amplitude correspond to other lithological boundaries and intra-unit boundaries, specifically within sediments of the Banner Formation. Accordingly, the sediments were categorized into packages or assemblages informally classified to seven seismo-stratigraphic units (A, B, C, C-1, D, E and F), assigned alphabetically from the land surface to the bedrock (e.g. Figs 5–7).

Fig. 5. (a) The time version of the processed P-wave seismic reflection profile 801 and (b) the interpreted depth version of the same profile. The control borehole 2 along the profile and the P-wave seismic velocity log are also shown. The log of the geology in the borehole is provided in Figure 2a. Descriptions of seismic units A–F are provided in the text.

Fig. 6. (a) The time version of the processed P-wave seismic reflection profile 710 and (b) the interpreted depth version of the same profile. The control borehole 1 along the profile and the P-wave seismic velocity log are also shown. The log of the geology in the borehole is provided in Figure 2b. Descriptions of seismic units A–F are provided in the text.

Fig. 7. (a, b) The time version of the processed P-wave seismic reflection profile 802 and (c, d) the interpreted depth version of the same profile. The control borehole 3 along the profile and the P-wave seismic velocity log are also shown. The log of the geology in the borehole is provided in Figure 2c. Descriptions of seismic units A–F are provided in the text.

Seismic unit B

Flat-lying, closely spaced and high-amplitude reflections characterize seismic unit B (e.g. Fig. 6). Based upon the borehole geological and geophysical data, seismic unit B includes an assemblage of interstratified layers of diamicton, silt and clay, and sand and gravel classified to the undifferentiated unit of the Glasford Formation. Seismic unit B is continuous along all the seismic profiles, with well-defined upper and lower boundaries. The seismic unit is 8–23 m thick.

In seismic profile 801, a decrease in the amplitude of reflectors marking the lower contact of seismic unit B was observed north of 2000 m (Fig. 5). From the available geological data, the change in seismic properties between seismic units B and C (i.e. the strongest prominent reflectors) is present where sand and gravel classified to seismic unit B overlie diamicton classified to seismic unit C, whereas the weakest reflectors are present where diamictons of each seismic unit overlie each other (Figs 2b and 5). The decrease in amplitude at the contact of these seismic units is not continuous, but rather present over short distances separated by higher-amplitude reflectors. The longest interval where the lower amplitudes were measured was along the profile from 4000 to 4700 m (Fig. 5). The weakest reflectors also extend ∼500 m to the west and east of the intersection with profile 802 (Fig. 8). Here the reflectors lie at higher elevation, ∼30m above the same reflectors along adjacent parts of profile 801 (Fig. 5).

Fig. 8. A view in three dimensions of the intersection between seismic profiles 801 and 802. The reflectors marking the contact between seismic units B and C significantly increase in elevation towards the intersection from the west.

Seismic unit f

Preglacial sediment having low-amplitude reflections is assigned to seismic unit F. Delineating the contact between seismic units E and F was much easier in profile 801 than 802. In profile 801, there is a highly undulating and partially interconnected upper boundary of seismic unit F, which was the only way to distinguish it from the overlying seismic unit E which has similar reflections (Figs 5 and 7). The character of a strong reflector separating the two seismic units suggests a large seismic velocity contrast between them. We were not able to trace the top of unit F in profile 710, although this contact is marked by a change of lithology in borehole 1 (Fig. 2a). This could be due to the lack of acoustic impedance contrast between sediments of seismic units E and F. However, low-reflectivity sediments of seismic unit F have sufficient contrast with the underlying bedrock surface to delineate the lower contact.

The geological and geophysical data from boreholes in the profiles (Fig. 2a–c) indicate that seismic unit F includes diamicton, silt, and sand and gravel, sediments deposited during the pre-Illinois Episode bedrock (Stumpf and Dey, in press). These sediments are typically leached of primary carbonate minerals or weakly calcareous and contain numerous clasts of the local bedrock. Localized incision into these sediments, either by water or ice, was identified in profiles 802 and 710 (e.g. Fig. 9). In these areas, narrow channels have been incised into seismic unit F. The channel mapped in profile 801 is 500 m wide and 15 m deep (Figs 5 and 9), whereas the channel in profile 710 is 800m wide (between 3300 and 4100 m) and has a maximum depth of 10 m (Fig. 6).

Fig. 9. Close-up view of a small channel eroded into silty and clayey sediments of seismic unit F along profile 801. The channel is likely filled with deposits of sand and gravel.

Summary and Discussion

The complex stratigraphy uncovered in the Pesotum Bedrock Valley undoubtedly provides additional information to better understand the depositional and erosional histories of the Pleistocene glaciations and preglacial times in central Illinois. Integrating HRSR results with drilling and borehole geophysics has allowed us to delineate the spatial distribution of seismic and lithostratigraphic units in order to characterize the sediments comprising the valley fill. This would not have been possible with the available subsurface information from the sparse wide-spaced boreholes over the buried valley.

Buried bedrock valleys in central Illinois have dimensions comparable with buried or tunnel valleys described in glaciated terrain in other parts of North America and northern Europe. Most valleys are tens of kilometers long, hundreds of meters to kilometers wide and have depths ranging from several tens to hundreds of meters. Specifically in this study the Pesotum Bedrock Valley is ∼80 km long, at least 3 km at its widest (although the entire width of the valley was not imaged) and incised 60 m into the bedrock.

Unlike tunnel valleys in northern Europe (e.g. Reference PiotrowskiPiotrowski, 1994; Reference Van der Vegt, Janszen, Moscariello, Huuse, Redfern, Le Heron, Dixon, Moscariello and CraigVan der Vegt and others, 2012) and those formed during melting of the Laurentide ice sheet during the Wisconsin Episode glaciation (e.g. Reference O CofaighO Cofaigh, 1996; Reference Hooke and JenningsHooke and Jennings, 2006; Reference Kehew, Piotrowski and JørgensenKehew and others, 2012), many buried valleys in central Illinois contain a relatively complete record of the Pleistocene glaciations with little or no evidence of incision by glacial meltwaters, for example Pesotum Bedrock Valley (this study), the unnamed bedrock valley below the cities of Champaign and Urbana (borehole 4 in Figs 1 and 2d), Danville Bedrock Valley (Reference Larson, Kempton and MeyerLarson and others, 1997) and Chatsworth Bedrock Valley (Reference Visocky and SchichtVisocky and Schicht, 1969) (Fig. 1). Exceptions to these stratigraphies are in the larger Mahomet and Middle Illinois Bedrock Valleys where thick deposits of sand and gravel (outwash) have been encountered (Reference Kempton, Johnson, Heigold, Cartwright, Melhorn and KemptonKempton and others, 1991; Reference McKay, Berg, Hansel, Kemmis and StumpfMcKay and others, 2008; Stumpf and Dey, in press). These sediments are thought to have been deposited by successive meltwater flows in front of retreating ice margins that have incised into older deposits of finer-grained sediment.

Many of the buried valleys in central Illinois have been filled over the course of multiple glaciations with proglacial lake development in front of advancing ice margins during pre-Illinois and Illinois Episodes. The glacially derived sediments lie over deposits of preglacial riverine sediment and slope wash, or weathered bedrock. The glacial lake sediment is conformably overlain by diamicton deposited in a subglacial environment. Only thin deposits of sand and gravel were encountered below glacial lake sediment or till of the earliest glacial advance during the Illinois Episode. The sedimentary sequence in the Pesotum Bedrock Valley is similar to the buried valleys in the Canadian Prairies containing mud-rich diamicton (Reference Cummings, Russell and SharpeCummings and others, 2012) and some buried bedrock valleys in southern Ontario, Canada (Reference Meyer and EylesMeyer and Eyles, 2007). Based on the analyses of channels and valley fills by Reference GiblingGibling (2006), these buried valleys are classified as valley fills on bedrock unconformities (B1).

Over these buried valleys, the relatively thick layers of sand and gravel interstratified with diamicton and silt and clay that are classified to the undifferentiated unit of the Glasford Formation (Fig. 2a-c) may indeed fill tunnel valleys. These sediments are interpreted as deglacial deposits associated with melting of the Laurentide ice sheet during the Illinois Episode (Stumpf and Dey, in press). Further, the significant rise in elevation of the lower contact of seismic unit B (Fig. 8) may delineate a buried ice margin associated with this glaciation. Additional investigation will be required to determine the spatial extent and interconnectivity of these deposits of sand and gravel regionally.

The stratigraphic position of glacial lake sediment comprising valley-fill sequences indicates that these valleys were not completely filled in until after the first glacial advance of the Illinois Episode. Prior to being buried, these valleys were sinks for proglacial drainage. The valley fill contains evidence suggesting that drainage along these valleys was blocked multiple times during the pre-Illinois and Illinois Episodes. Further, additional subsurface information in the Teays-Mahomet Bedrock Valley System outside the study area suggests that these glacial lakes of the pre-Illinois Episodes may not have been confined entirely within tributary valleys to the Mahomet Bedrock Valley. Deposits of silt and clay classified to the Banner Formation encountered occasionally in the Mahomet Bedrock Valley in Illinois (Reference Herzog, Wilson, Larson, Smith, Larson and GreenslateHerzog and others, 1995; Reference Soller, Price, Kempton and BergSoller and others, 2000; Stumpf and Dey, in press) and the Teays Bedrock Valley in western Indiana (Reference Bleuer, Melhorn and KemptonBleuer, 1991) may be correlative with deposits of fine-grained sediment in the Pesotum Bedrock Valley classified to the Hillery Member, Banner Formation. If so, this proglacial lake may have inundated a much larger area than previously reported (Reference Kempton, Johnson, Heigold, Cartwright, Melhorn and KemptonKempton and others, 1991), occupying the western part of the Teays-Mahomet Bedrock Valley System. Presumably, the dam of either ice or sediment holding back the lake was located in the extreme western part of the Mahomet Bedrock Valley or the Middle Illinois-Mackinaw Bedrock Valleys.

Preliminary calculations suggest that this proglacial lake would have covered an area of ∼8500km² in Illinois. Although covering a much smaller area than Glacial Lake Agassiz in central North America (840 000 km²; Reference Teller and LeveringtonTeller and Leverington, 2004) or Vostok Subglacial Lake in Antarctica (>19200 km²; Reference Siegert, Popov, Studinger, Siegert, Kennicutt and Bind-schadlerSiegert and others, 2011), the total area inundated is comparable with the size of Glacial Lake Missoula in Montana, USA (∼9700km²; Reference Petteri, Baker and SmithPetteri and others, 2010), or Glacial Lake Fraser in British Columbia, Canada (>9800 km²; Reference ClagueClague, 1987; Reference FultonFulton, 1995). Further investigation is required to determine the volume of water held in the lake and its drainage history.