The buried Mahomet Valley in east-central Illinois is a complex lowland carved into the surface of Pennsylvanian and older rocks. It consists of a deep channel throughout most of its length and contains numerous benches below erosional remnant hills, suggesting several cycles of early to middle Quaternary erosion. Recent local and regional studies utilizing existing borehole data, including down-hole geophysical logs and seismic profiles, have provided new insights into the valley’s configuration. The usual techniques for interpreting shallow seismic refraction and reflection data are complicated by a seismic velocity inversion in the Quaternary sediments filling the deeper parts of the valley. Based on the 500-ft (152 m) elevation contour to define the upper limit of the Mahomet Valley Lowland, the valley is about 8 mi (13 km) wide at the Illinois/Indiana border. Westward, the lowland widens to as much as 18 mi (29 km) in Ford County, where a major tributary enters from the north. Here, several ridges rise above a broad bench ranging from 400 to 450 ft (121 to 137 m) in elevation. Sparse well data and some seismic profiling suggest a deep channel at or slightly below an elevation of 350 ft (106 m) in northeastern Ford and northwestern Vermilion Counties. This deep channel extends southwestward where it passes under the villages of Mahomet (Champaign County) and Monticello (Piatt County) and then westward to just east of Clinton (De Witt County). Between Mahomet and Clinton, where there are also several isolated bedrock hills that rise to elevations as much as 500 ft (152 m), the intermediate bench lowers to 350 to 400 ft (106 to 121 m). The valley narrows to an average of 14 mi (22 km) wide between Monticello and its confluence with the Mackinaw Valley segment of the Ancient Mississippi Bedrock Valley in southwestern Tazewell County. Southeast of Clinton, a narrow bedrock “diversion” channel (Kenney Valley) provides a nearly straight connection between the Mahomet Valley and the Ancient Mississippi Valley below the confluence with the Mahomet. A complex Quaternary history has been established for the Mahomet Bedrock Valley, but as yet no evidence has been found for late Tertiary or preglacial alluvial deposits. Deposits filling the valley include the widespread Mahomet Sand Member, as much as 200 ft (60 m) thick, locally overlying or interbedded with tills of the Banner Formation (pre-Illinoian). Above this succession are Glasford Formation (Ulinoian) and Wedron Formation (Wisconsinan) tills and associated deposits. The varied nature of the bedrock valley topography, the scattered presence of till-like material on bedrock hills underlying the Mahomet Sand, and the presence of lower Banner Formation till interbedded with the Mahomet Sand suggest several episodes of valley erosion and glacial deposition during a long pre-Illinoian history. The deepest bedrock channel probably originated before deposition of the Mahomet Sand but postdates at least one early Quaternary glaciation. Near the Indiana border, the uppermost surface of the Mahomet Sand, at elevation 560 ft (170 m), appears locally eroded, forming broad terraces that continue down valley at progressively lower elevations. The surface of the Banner Formation forms a broad sag over much of the valley and rises slightly over the uplands. Deposits of the Glasford Formation form the upper fill in the valley and include a significant outwash related to the Vandalia Till Member. The Sangamon Soil, developed in the Glasford, together with the overlying Roxana Silt and Robein Silt, locally forms an important subsurface marker. The topographic expression of this pre-Woodfordian surface shows no evidence of the Mahomet Valley; it was completely buried by the end of the Illinoian. Aquifers associated with the Mahomet Bedrock Valley and the Ancient Mississippi Bedrock Valley to the west are the only highly productive, nonalluvial sand and gravel aquifers in the southern three-fourths of Illinois. The aquifers associated with the buried Mahomet Valley provide the only large source of irrigation, industrial, and municipal supplies of groundwater in east-central Illinois; 40 municipalities and water districts are currently obtaining groundwater from these aquifers. The largest groundwater withdrawals occur in the Champaign-Urbana area, averaging 17 × 10 6 gal (64 × 10 6 l/day. Total groundwater withdrawals from the valley are estimated to be at least 42 × 10 6 gal (16 × 10 7 l)/day. The coefficients of storage for the Mahomet Sand range from 2 × 10 −5 to 2 × 10 −3 , with hydraulic conductivities and transmissivities up to 4,237 gpd/ft 2 (2 × 10 −3 m/s), and 510,000 gpd/ft (5 × 10 −2 m 2 /s), respectively; for the Glasford sand the coefficients range from 1 × 10 −5 to 8 × 10 −2 , with hydraulic conductivities and transmissivities up to 4,660 gpd/ft 2 (2 × 10 −3 m/s), and 233,000 gpd/ft (2 × 10 −2 m 2 /s), respectively. Coefficients of vertical hydraulic conductivity of the confining beds range from 2.12 × 10 −3 to 0.4 gpd/ft 2 (1 × 10 −9 to 2 × 10 −7 m/s).

Abstract Within and at the base of the Paleozoic strata in the Illinois basin, a number of stratigraphic interfaces have large acoustic impedance contrasts that can produce mappable seismic reflections. Noteworthy interfaces that produce large-amplitude continuous reflections are (1) Late Devonian clastic rocks (New Albany Group) with predominantly carbonate Devonian and Silurian rocks (Hunton Supergroup); (2) Upper Ordovician clastic rocks (Maquoketa Group) with underlying Upper Ordovician limestone and dolomite rocks (Galena Group); (3) Middle Ordovician rocks of the St. Peter Sandstone with the underlying Ordovician/Cambrian dolomite of the Knox Supergroup; and (4) dolomite rocks of the Knox Supergroup with underlying interbedded clastics. The fourth interface may have an associated negative reflection coefficient and, therefore, a phase inversion; nevertheless, it produces a relatively large amplitude reflection. Discernible reflections of other interfaces (e.g., the contact of the Valmeyeran Aux Vases Sandstone with the Mississippian Ste. Genevieve Limestone, Table 12-1) are generally smaller in amplitude and less continuous than those of the four interfaces mentioned above. The interface between Cambrian and Precambrian rocks in the Illinois basin does not always produce large-amplitude, coherent seismic reflections. The Precambrian surface, north of the Cottage Grove fault system and the Shawneetown fault zone, is for the most part a granite-rhyolite terrane. Most wells that have penetrated Precambrian igneous rock in the Illinois basin have encountered fresh-looking granites or rhyolites. In some of these holes, sonic logs of the upper hundred feet of Precambrian rock show compressional-wave velocities that are somewhat less than expected for fresh granites or

Abstract The structure of the earth's crust in the Mid-Continent has historically been assumed to be uncomplicated. However, with the increase in the number of studies in earthquake seismology and seismic refraction and as the potential fields of this region have multiplied, the earth's crust in the Mid-Continent is now seen to be far more complicated than once assumed. The New Madrid rift complex (Figure 17-1) has played a fundamental role in the initiation and development of the Illinois basin. According to Hildenbrand (1985), rifting in the northern Mississippi Embayment was first suggested by A. V. Heyl (USGS), based on discussions of gravity anomalies with H. R. Joesting and L. Cordell (USGS). Burke and Dewey (1973) suggested that the Mississippi Embayment originated as a Mesozoic failed-arm rift. Ervin and McGinnis (1975) synthesized gravity data with seismic, stratigraphic, and petrologic data and suggested that the rift, which they called the Reelfoot rift, formed in late Precambrian or early Paleozoic time and was reactivated in the Cretaceous. Interpretations of gravity data by Ervin and McGinnis (1975) and by Cordell (1977) indicated an anomalously dense lower crustal layer in the Reelfoot rift that was compatible with interpretations of deep seismic refraction data by McCamy and Meyer (1966) and Mooney et al. (1983) (Figures 17-2A, 17-2B). In an attempt to delineate the structures in the northern Mississippi Embayment that may be responsible for seismicity, Hildenbrand et al. (1977), Kane et al. (1979), and Hildenbrand (1985) examined aeromagnetic and gravity data. These authors delineated a north-east