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We present porosity data from the oilfield data base of Holtz (1997). Note that these values are representative of productive intervals.<\/SPAN><\/SPAN><\/P>

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Permeability data for producing fields were summarized by Galloway and others (1983), but we have used the raw data extracted from the Railroad Commission of Texas well files (Holtz, 1997) to provide an overview of the properties of Woodbine producing intervals.<\/SPAN><\/SPAN><\/P>

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There currently is no published map of Tuscaloosa Group percent-shale distribution for the Mobile region (Jack Pashin, Alabama Geological Survey, personal communication, April 2000). We used the geophysical logs from the cross sections of Mancini and others (1987) to generate a semiquantitative estimate of percent shale within the lower Tuscaloosa Group. A large number of geophysical logs that penetrate the Tuscaloosa Group are available. From these logs, it would possible to construct a more accurate shale distribution, if CO<\/SPAN><\/SPAN>2<\/SPAN><\/SPAN> sequestration in the area becomes a serious possibility. <\/SPAN><\/SPAN><\/P>

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This is data for rock mineralogy for the Tuscaloosa group<\/SPAN><\/P><\/DIV><\/DIV>", "geometryType": "esriGeometryPoint", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Tucker, W. E., and Kidd, R. 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Permeability data were extracted from the oil-field data base of Holtz (1997). These data were extracted from Railroad Commission of Texas files and normalized to hydraulic conductivity.<\/SPAN><\/SPAN><\/P>

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This shapefile serves water chemistry data for wells in theTuscaloosa group<\/SPAN><\/P><\/DIV><\/DIV>", "geometryType": "esriGeometryPoint", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Alverson, R. 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Different literature sources were used to find porosity information for the Pottsville Formation (Galicki, 1986; Beard and Meylan, 1987; E. Doherty, personal communication, 1999). This information from the oil fields was added to one of the oil- and gas-field maps. Although porosity data from oil fields range between 1.2 and 15 percent, normal faulting and lineaments present in the basin are the main factors that seems to control both porosity and permeability (Ortiz and others, 1993).<\/SPAN><\/SPAN><\/P>

<\/P><\/DIV><\/DIV>", "geometryType": "esriGeometryPoint", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Beard, R. H., and Meylan, M. A., 1987, Petrology and hydrocarbon reservoir potential of subsurface Pottsville (Pennsylvanian) sandstones, Black Warrior Basin, Mississippi: Gulf Coast Association of Geological Societies Transactions, v. 33. p 11\u201323.\n*\nGalicki, S., 1986, Mesozoic-Paleozoic producing areas of Mississippi and Alabama: Mississippi Geological Society.\n*\nOrtiz, I., Weller, R., and others, 1993, Disposal of produced waters: underground injection option in the Black Warrior Basin: Proceedings of the 1993 International Symposium: The University of Alabama/Tuscaloosa, p. 339\u2013364.", "parentLayer": null, "subLayers": [], "minScale": 0, "maxScale": 0, "referenceScale": 0.0, "drawingInfo": { "renderer": { "type": "simple", "symbol": { "type": "esriSMS", "style": "esriSMSCircle", "color": [ 173, 96, 71, 255 ], "size": 4, "angle": 0, "xoffset": 0, "yoffset": 0, "outline": { "color": [ 0, 0, 0, 255 ], "width": 0.7 } } }, "scaleSymbols": true, "transparency": 0, "labelingInfo": null }, 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There currently is no published map of Tuscaloosa Group net-sand-thickness distribution for the Mobile region (Jack Pashin, Alabama Geological Survey, personal communication, April 2000). We used the geophysical logs from the cross sections of Mancini and others (1987) to generate a semiquantitative estimate of net sand thickness of the lower Tuscaloosa Group (c4tuscaloosag). A large number of geophysical logs that penetrate the Tuscaloosa Group are available. From these logs, it would possible to construct a more accurate spatial distribution of sands in a future study. <\/SPAN><\/SPAN><\/P>

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Porosity data are derived from an oilfield data base (Holtz, 1997). Kreitler and others (1983) presented an average porosity. <\/SPAN><\/SPAN><\/P>

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This shapefile contains pressure data collected for Carbon Dioxide Sequestration analysis for Paluxy sand in east texas<\/SPAN><\/P><\/DIV><\/DIV><\/DIV>", "geometryType": "esriGeometryPoint", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Holtz, M. 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There currently is no published map of Tuscaloosa Group thickness distribution for the Mobile region (Jack Pashin, Alabama Geological Survey, personal communication, April 2000). We used the thickness information from the cross sections of Mancini and others (1987) to generate the lower Tuscaloosa Group thickness-distribution map for the GIS. We also digitized unpublished data supplied by Jack Pashin (Alabama Geological Survey, personal communication, 2000)<\/SPAN><\/SPAN><\/P>

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The chemical composition of the Paluxy water is variable. Some of the waters are NaCl water, similar to Woodbine, whereas others are Na-Ca-Cl waters and appear intermediary between the chemical composition of Woodbine waters and Travis Peak or Glen Rose waters. The chemistry and hydrology suggest that waters from the Glen Rose and Travis Peak Formations are leaking into the Paluxy\" (Kreitler and others, 1983, p. 105).<\/SPAN><\/P>

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The Woodbine Formation was originally at hydrostatic pressure, but it has been extensively depressurized by production (Kreitler and others, 1984, their fig. 44).<\/SPAN><\/SPAN><\/P>

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Only the partial net sand map for the Lower Pennsylvanian (Cleaves, 1983) was found and digitized.<\/SPAN><\/P>

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Structure for the Pottsville Formation Black Warrior Basin, Alabama/Mississippi<\/SPAN><\/P><\/DIV><\/DIV><\/DIV>", "geometryType": "esriGeometryPolyline", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Hewitt, J., 1984, Geologic overview, coal, and coalbed methane resources of the Black Warrior Basin\u2014Alabama and Mississippi, in Rightmire, C., Eddy, G., and Kirr, J., eds., Coalbed methane resources of the United States: American Association of Petroleum Geologists, Studies in Geology Series 17, p. 73\u2013104.\n*\nPashin, J. 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This structure map was digitized from Moffett and others (1984a) because it covers most of the Tuscaloosa Group<\/SPAN><\/P>

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There are several low permeability units above the Paluxy sand in the area of interest, including the Goodland Formation and Edwards Limestone. However, argillite/carbonate facies in these units are not mapped in detail in this area. Therefore, we have chosen the Kiamichi Formation as the top seal for the Paluxy aquifer. The Kiamichi is widespread throughout the area. In electric-log cross sections presented by Anderson (1989) it appears to be a fine-grained, low-resistivity unit. Anderson mentioned that it is composed of terrigenous clastics. Neeley (1991) described the Kiamichi in southeastern Oklahoma outcrops as being composed of mostly argillaceous oyster biostromes with minor interbedded, dark-gray clay and shale and a few hard, argillaceous limestone beds. We assume that basinward (in the study area), the Kiamichi consists of mostly clay and shale. Thus, we identified the Kiamichi as a seal for the Paluxy<\/SPAN><\/SPAN><\/P>

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The isopach map of Seni (1981) was digitized for this shapefile. It shows thinning of the Paluxy over salt structures and thickening in areas away from the structures.<\/SPAN><\/P>

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Digitized structure map of the top of the Paluxy sand From Core Laboratories (1972). <\/SPAN><\/P>

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The Selma Chalk, which overlies the Tuscaloosa Group is widely recognized as a regional aquiclude. In the Mobile area, it generally ranges in thickness from 300 to 400 m (Raymond and others, 1988; Pashin and others, 1998). There currently is no published thickness map for the Selma Chalk. However, there are published maps of the top of the Selma and Eutaw Formations. (Hinkle and others, 1983; Moffett and others, 1984a). These were gridded and the top Tuscaloosa subtracted to determine the thickness of the Selma Chalk<\/SPAN><\/SPAN><\/P>

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The effect of the salt structures is not as apparent on the net-sand-thickness map of the Paluxy (Core Laboratories, 1972) as it is in the formation-thickness map. Therefore, the salt structures affected both coarse- and finer grained clastics essentially equally. 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The Kiamichi may be discontinuous at faults and along the flanks of diapers.<\/SPAN><\/SPAN><\/P>

<\/P><\/DIV><\/DIV>", "geometryType": "esriGeometryPolyline", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Jackson, M. P. A., and Seni, S. 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The Selma Chalk is thick and generally impermeable. However, Pashin and others (1998) demonstrated that fault-induced fracturing can greatly enhance fracturing in the Selma interval. Therefore, we used a map showing the configuration of the top of the Selma (Moffett and others, 1984a), which shows the location of major faults, to characterize the continuity of the top seal.<\/SPAN><\/SPAN><\/P>

<\/P><\/DIV><\/DIV><\/DIV>", "geometryType": "esriGeometryPolyline", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Pashin, J. C., Raymond, D. E., Rindsberg, A. K., Alabi, G. G., Carroll, R. E., Groshong, R. 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Formation-water salinity. Ortiz and others (1993) presented a subsea-depth map of waters containing 10,000 mg/L of TDS provided by the Alabama Department of Environmental Management (ADEM). Although this map covers only the Alabama side of the Black Warrior Basin, it can be combined with the depth map in the GIS data base to infer salinity throughout the Pottsville Formation<\/SPAN><\/P><\/DIV><\/DIV><\/DIV>", "geometryType": "esriGeometryPolyline", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Ortiz, I., Weller, R., and others, 1993, Disposal of produced waters: underground injection option in the Black Warrior Basin: Proceedings of the 1993 International Symposium: The University of 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The Pottsville Formation of the Black Warrior Basin comprises as much as 12,000 ft of shale, sandstone, and coal (Cleaves and Broussard, 1980). The sequence has a southwestward thickening, which represents the thick clastic wedge shed from the Ouachita Orogenic Belt. The Lower Pottsville thickens from 1,000 to 1,500 ft in the north to 2,000 ft in the southwest. <\/SPAN><\/SPAN><\/P>

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A northwest-trending, high-angle normal fault, which probably formed in response to the compressional forces associated with the Ouachita Orogenic Belt, is the main structural feature of the basin. Two major lineaments are also present. One trend, N30-60E, is parallel to the main trend of normal faults (Pashin and others, 1991). The faulting influenced sediment deposition and induced natural fractures that often enhance permeability and affect diagenesis.<\/SPAN><\/SPAN><\/P>

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We chose to use the maps of Renkin and others (1989) because they provided a detailed, regional map of the top of the Cape Fear aquifer, and they clearly documented the stratigraphic position of the top of the unit<\/SPAN><\/SPAN><\/P>

<\/P><\/DIV><\/DIV>", "geometryType": "esriGeometryPolyline", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Renkin, R. A., Mahon, G. L., and Davis, M. E., 1989, Hydrogeology of clastic Tertiary and Cretaceous regional aquifers and confining units in the southeastern coastal plain aquifer system of the United States: U.S. Geological Survey Hydrologic Investigations Atlas HA-701, 3 sheets.", "parentLayer": null, "subLayers": [], "minScale": 0, "maxScale": 0, "referenceScale": 0.0, "drawingInfo": { "renderer": { "type": "simple", "symbol": { "type": "esriSLS", "style": "esriSLSSolid", "color": [ 76, 114, 155, 255 ], "width": 1 } }, "scaleSymbols": true, "transparency": 0, "labelingInfo": null }, "defaultVisibility": true, "extent": { "xmin": -9193324.6689, "ymin": 3605523.530100003, "xmax": -8744846.7011, "ymax": 4118832.6128999963, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 } }, "hasAttachments": false, "htmlPopupType": 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Several authors have characterized ground-water flow in the Cape Fear interval (Aucott and Speiran, 1985; Miller and others, 1986; Aucott, 1988; Miller, 1990). A number of authors determined that the deep aquifers directly below the coast is a marine/terrestrial ground-water interface zone in which waters tend to be stagnant. Miller and others (1986; their fig. 5) showed that the NA+ concentrations increase with distance along the aquifer flow path, and several authors showed that the Cape Fear aquifer in southeastern South Carolina contains relatively high concentrations of NA+ (Miller and others, 1986; Miller, 1990). On the basis of these data, we conclude that residence times in the Cape Fear aquifer of southeastern South Carolina are long, and may be as much as 5,000 yr.<\/SPAN><\/P><\/DIV><\/DIV>", "geometryType": "esriGeometryPolyline", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Aucott, W. R., 1988, The predevelopment ground-water flow system and hydrologic characteristics of the Coastal Plain aquifers of south Carolina: U.S. Geological Survey, Water-Resources Investigations Report 86\u20134347, 66 p..\n*\nAucott, W. R., Davis, M. E., and Speiran, G. K., 1987, Geohydrologic framework of the Coastal Plain aquifers of South Carolina: U.S. Geological Survey, Water-Resources Investigations Report 85-4271, 7 sheets.\n*\nAucott, W. R., and Speiran, G. K., 1985, Ground-water flow in the coastal plain aquifers of South Carolina: Ground Water, v. 23, p. 736\u2013745\n*\nMiller, J. A., Barker, R. A., and Renkin, R. A., 1986, Hydrology of the Southeastern Coastal Plain Aquifer System, in Vecchioli, J., and Johnson, A. I., eds., Regional aquifer systems of the United States: aquifers of the Atlantic and Gulf Coastal Plain: American Water Resources Association Monograph Series No. 9, p. 53\u201377.\n*\nMiller, J. 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This shapefile contains a top seal thickness isopach for cedar keys/ Lawson<\/SPAN><\/P><\/DIV><\/DIV>", "geometryType": "esriGeometryPolyline", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "unknown", "parentLayer": null, "subLayers": [], "minScale": 0, "maxScale": 0, "referenceScale": 0.0, "drawingInfo": { "renderer": { "type": "simple", "symbol": { "type": "esriSLS", "style": "esriSLSSolid", "color": [ 175, 87, 114, 255 ], "width": 1 } }, "scaleSymbols": true, "transparency": 0, "labelingInfo": null }, 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There is essentially no information regarding flow direction for the hydrostratigraphic units below the Floridan aquifer. For the GIS, we used the map of Meyer (1989), which characterizes flow in the Floridan. Flow in the lower Cedar Keys and upper Lawson Dolomite is unknown.<\/SPAN><\/SPAN><\/P>

<\/P><\/DIV><\/DIV>", "geometryType": "esriGeometryPolyline", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Meyer, F. 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To characterize the continuity of the top seal, we chose the map of Chen (1965), which shows the percent evaporites in the Paleocene Cedar Keys Dolomite<\/SPAN><\/SPAN><\/P>

<\/P><\/DIV><\/DIV>", "geometryType": "esriGeometryPolyline", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Chen, S. 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"capefear_001_depthtotop_basement", "type": "Feature Layer", "description": "

The top of basement contours digitized from Colquhoun and others (1983) and Aucott and others (1987).<\/SPAN><\/P>

<\/P><\/DIV><\/DIV>", "geometryType": "esriGeometryPolyline", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Aucott, W. R., Davis, M. E., and Speiran, G. K., 1987, Geohydrologic framework of the Coastal Plain aquifers of South Carolina: U.S. Geological Survey, Water-Resources Investigations Report 85-4271, 7 sheets.\n*\nColquhoun, D. J., Woollen, L. D., Van Nienwenhuise, D. S., Padgett, G. G., Oldham, R. W., Boylan, D. C., Bishop, J. W., and Howell, P. 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Several researchers have reported that salinity in the Cape Fear aquifer is moderately high but below 10,000 mg/L (Manheim and Horn, 1968; Brown and others, 1979; Lee, 1985; Miller and others, 1986; Miller, 1990). However, there has not been a systematic study of water chemistry in southeastern South Carolina because of low prospect for use. We used the map of Lee (1985) for the GIS, who referred to the Cape Fear hydrostratigraphic interval as the middle water-bearing zone of the A4 regional aquifer.<\/SPAN><\/SPAN><\/P>

<\/P><\/DIV><\/DIV><\/DIV>", "geometryType": "esriGeometryPolyline", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Brown, P. M., Brown, D. L., Reid, M. S., and Lloyd, O. B., Jr., 1979, Evaluation of the geologic and hydrologic factors related to the water-storage potential of Mesozoic aquifers in the southern part of the Atlantic coastal plain, South Carolina and Georgia: U.S. Geological Survey, Professional Paper 1088, 37 p., 11 plates. \n*\nLee, R. 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I., eds., Regional aquifer systems of the United States: aquifers of the Atlantic and Gulf Coastal Plain: American Water Resources Association Monograph Series No. 9, p. 53\u201377.", "parentLayer": null, "subLayers": [], "minScale": 0, "maxScale": 0, "referenceScale": 0.0, "drawingInfo": { "renderer": { "type": "simple", "symbol": { "type": "esriSLS", "style": "esriSLSSolid", "color": [ 131, 46, 132, 255 ], "width": 1 } }, "scaleSymbols": true, "transparency": 0, "labelingInfo": null }, "defaultVisibility": true, "extent": { "xmin": -9165121.0593, "ymin": 3638155.3748999983, "xmax": -8843975.9563, "ymax": 4037163.9707999974, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 } }, "hasAttachments": false, "htmlPopupType": "esriServerHTMLPopupTypeAsHTMLText", "displayField": "SEG_ID", 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11.5, "cimVersion": "3.5.0", "id": 39, "name": "cedarlawson_003_formation_thick", "type": "Feature Layer", "description": "

This shapefile is a digitized isopach map from Randazzo. Randazzo (1997; his fig. 4.2c) presented a map showing the thickness distribution of the Upper Cretaceous interval across the Florida Peninsula. His map shows that (1) the entire Upper Cretaceous interval in Polk County is about 2,400 ft and (2) the thickness of the Upper Cretaceous does not vary that much across Florida. The lower Cedar Keys and Lawson Dolomite compose about half of the Upper Cretaceous section. <\/SPAN><\/P>

<\/P><\/DIV><\/DIV><\/DIV>", "geometryType": "esriGeometryPolyline", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Randazzo, A. F., 1997, The sedimentary platform of Florida: Mesozoic to Cenozoic, in Randazzo, A. F., and Jones, D. 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Smith and Lord (1997; their fig. 2.10) presented a map showing geothermal gradients across Florida. Their map, in combination with the depth to formation, was used to derive the formation-brine temperature distribution in the GIS. Note that the geothermal gradients of Smith and Lord closely match those of Blackwell and others (2000). Vernon (1970) reported some significant decreases in temperature with depth in some wells and attributed these reversals to fresh-water flow thorough cavernous zones.<\/SPAN><\/SPAN><\/P>

<\/P><\/DIV><\/DIV>", "geometryType": "esriGeometryPolyline", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Smith, D. L., and Lord, K. M., 1997, Tectonic evolution and geophysics of the Florida basement, in Randazzo, A. F., and Jones, D. S., eds., The geology of Florida: Tallahassee, University of Florida Press, p. 13\u201326.\n*\nVernon, R. 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Chen (1965) presented a map showing the elevation of the top of the Upper Cretaceous, which is the top of the Lawson Dolomite, and we used this map for the GIS.<\/SPAN><\/SPAN><\/P>

<\/P><\/DIV><\/DIV>", "geometryType": "esriGeometryPolyline", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Chen, S. 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Thickness in meters of the dominantly coarse-grained part of the Tuscaloosa Formation. Data interpreted from the Florida Geological Survey and from geophysical logs presented in Renkin and others (1989).<\/SPAN><\/P><\/DIV><\/DIV><\/DIV>", "geometryType": "esriGeometryPolyline", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "References for Florida and South Georgia Tuscaloosa data collection:\n\n *Barker, R. A., and Pernik, M., 1994, Regional hydrology and simulation of deep ground-water flow in the Southeastern Coastal Plain Aquifer system in Mississippi, Alabama, Georgia, and South Carolina: U.S. Geological Survey Professional Paper 1410-C, 87 p.\n\n *Gohn, G. S., Smith, C. C., Christopher, R. A., and Owens, J. P., 1980, Preliminary stratigraphic cross sections of Atlantic coastal plain sediments of the southeastern United States: U.S. Geological Survey, Miscellaneous Field Studies Map MF-1015-C.\n\n *Miller, James A., 1979, Potential subsurface zones for liquid-waste storage in Florida: Bureau of Geology, Florida Department of Natural Resources, Map Series No. 94.\n\n *Renkin, R. A., Mahon, G. L., and Davis, M. E., 1989, Hydrogeology of clastic Tertiary and Cretaceous regional aquifers and confining units in the southeastern coastal plain aquifer system of the United States: U.S. Geological Survey Hydrologic Investigations Atlas HA-701, 3 sheets.\n\n *Scholle, P. A., 1979, Data summary and petroleum potential: in cholle, P. A., editor, Geological studies of the COST-GE-1 well, United States South Atlantic Outer Continental Shelf area: U. S. 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We digitized the generalized net-sandstone map presented by Oliver (1971). More detailed data are available at field scale and by interpreting finer stratigraphic elements within the Woodbine.<\/SPAN><\/P>

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The Woodbine Formation was originally at hydrostatic pressure, but it has been extensively depressurized by production (Kreitler and others, 1984, their fig. 44).<\/SPAN><\/SPAN><\/P>

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The Eagle Ford has been eroded over the Sabine Uplift in the eastern part of the study area (see 7woodbine); however, the low-transmissivity Austin Chalk extends over this area. Faults of the Mexia-Talco and Elkhart-Mt. Enterprise fault zones cut the seals. These faults create traps for oil fields, the extent to which they may locally leak unknown. Fault zones have isolated Woodbine sandstones within the basin from recharge zones in Woodbine outcrops on the east and north basin edges (Kreitler and others, 1984). If these faults can be shown to be tight to CO<\/SPAN><\/SPAN>2<\/SPAN><\/SPAN>, this geometry may create a desirably large but hydrologically isolated brine volume. Salt diapers penetrate the Cretaceous section, and there is some evidence of at least geologic rates of discharge up some dome flanks (Kreitler and others, 1984). In the structurally and stratigraphically complex areas around salt diapers, site-specific data on the potential for leakage are needed. Nonpenetrative salt pillows may also impact flow at depth.<\/SPAN><\/SPAN><\/P>

<\/P><\/DIV><\/DIV>", "geometryType": "esriGeometryPolyline", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Kreitler, C. W., Collins. E. W., Fogg, G. E., Jackson, M. P. A., and Seni, S. J., 1984, Hydrogeological characterization of the saline aquifers, East Texas Basin\u2014implications to nuclear waste storage in East Texas salt domes: The University of Texas at Austin, Bureau of Economic Geology, contract report prepared for U.S. Department of Energy, under contract no. DE-AC97-80ET46617, 156 p. \n*\nSeni, S. J., and Jackson, M. P. A., 1984, Sedimentary records of Cretaceous and Tertiary salt movement, East Texas Basin: times, rates, and volumes of flow, implications to nuclear waste isolation and petroleum exploration: The University of Texas at Austin, Bureau of Economic Geology Report of Investigations No. 139, 89 p.", "parentLayer": null, "subLayers": [], "minScale": 0, "maxScale": 0, "referenceScale": 0.0, "drawingInfo": { "renderer": { "type": "simple", "symbol": { "type": "esriSLS", "style": "esriSLSSolid", "color": [ 57, 125, 142, 255 ], "width": 1 } }, "scaleSymbols": true, "transparency": 0, "labelingInfo": null }, "defaultVisibility": true, "extent": { "xmin": -1.07710689275E7, "ymin": 3663401.8698000014, "xmax": -1.05363993775E7, "ymax": 3949686.8117000014, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 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We digitized the formation-thickness map of Calavan (1985).<\/SPAN><\/P>

<\/P><\/DIV><\/DIV><\/DIV>", "geometryType": "esriGeometryPolyline", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Calavan, C. 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depth in meters to the top of the principal injection sand in the Cretaceous Tuscaloosa Formation. Data Modified from Miller (1979).<\/SPAN><\/P><\/DIV><\/DIV><\/DIV>", "geometryType": "esriGeometryPolyline", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "References for Florida and South Georgia Tuscaloosa data collection:\n\n *Barker, R. A., and Pernik, M., 1994, Regional hydrology and simulation of deep ground-water flow in the Southeastern Coastal Plain Aquifer system in Mississippi, Alabama, Georgia, and South Carolina: U.S. Geological Survey Professional Paper 1410-C, 87 p.\n\n *Gohn, G. S., Smith, C. C., Christopher, R. A., and Owens, J. P., 1980, Preliminary stratigraphic cross sections of Atlantic coastal plain sediments of the southeastern United States: U.S. Geological Survey, Miscellaneous Field Studies Map MF-1015-C.\n\n *Miller, James A., 1979, Potential subsurface zones for liquid-waste storage in Florida: Bureau of Geology, Florida Department of Natural Resources, Map Series No. 94.\n\n *Renkin, R. A., Mahon, G. L., and Davis, M. E., 1989, Hydrogeology of clastic Tertiary and Cretaceous regional aquifers and confining units in the southeastern coastal plain aquifer system of the United States: U.S. Geological Survey Hydrologic Investigations Atlas HA-701, 3 sheets.\n\n *Scholle, P. A., 1979, Data summary and petroleum potential: in cholle, P. A., editor, Geological studies of the COST-GE-1 well, United States South Atlantic Outer Continental Shelf area: U. S. 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The Eagle Ford shale is the low-permeability unit immediately on top of the Woodbine. A thickness map was digitized from Surles (1986) and gridded (c7woodbineg). More regional-scale stratigraphic and facies information is available from this source. The Eagle Ford has been eroded over the Sabine Uplift in the eastern part of the study area; however, the low-transmissivity Austin Chalk extends over this area.<\/SPAN><\/SPAN><\/P>

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Structure on top of the Woodbine was digitized from Core Labs (1972)<\/SPAN><\/SPAN><\/P>

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Two data points from oil fields were found for the Pottsville Formation (Galicki, 1986; Beard and Meylan, 1987), <\/SPAN><\/SPAN><\/P>

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A number of authors have reported that DSC in the Tuscaloosa Group in southwestern Alabama is high (Alverson, 1970; Tucker and Kidd, 1973; Miller, 1990) However, there are few published numbers (see Tucker and Kidd (1973; their table 3 in which they report one calculated DSC for the Tuscaloosa Group of 151,000 mg/L). For the GIS, we used a map of Miller (1990), which shows the portion of southwest Alabama, Tuscaloosa Group (Black Warrior River aquifer), in which formation waters are more than 10,000 mg/L<\/SPAN><\/SPAN><\/P>

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Several studies characterize the confining unit above the Cape Fear Formation as a tight marine shale (Aucott and others, 1987; Aucott, 1988; Miller, 1990), and the shale interval is easy to recognize in published cross sections (Colquhoun and others, 1983; Aucott and others, 1987). Aucott (1988) provided a map showing the distribution leakage coefficient of the Cape Fear confining unit. He defined the leakage coefficient as the vertical hydraulic conductivity (~2 ´ 10 <\/SPAN><\/SPAN>-7<\/SPAN><\/SPAN> ft/day) divided by the confining unit thickness (~50 ft). The map in the GIS is from Aucott (1988; his fig. 31). <\/SPAN><\/SPAN><\/P>

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K., 1987, Geohydrologic framework of the Coastal Plain aquifers of South Carolina: U.S. Geological Survey, Water-Resources Investigations Report 85-4271, 7 sheets.\n*\nColquhoun, D. J., Woollen, L. D., Van Nienwenhuise, D. S., Padgett, G. G., Oldham, R. W., Boylan, D. C., Bishop, J. W., and Howell, P. D., 1983, Surface and subsurface stratigraphy, structure and aquifers of the South Carolina Coastal Plain: Columbia, SC, State of South Carolina, Office of the Governor, 78 p.\n*\nMiller, J. 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The Lower Pottsville strata (800 to 1,000 ft thick) contain orthoquartzitic sandstone, shale, and coal interpreted as the deposits of barrier-bar, tidal-flat, and lagoonal sediments in a north-northeast progradational system of a massive clastic wedge shed from the Ouachita orogen (Cleaves and Broussard, 1980). The Upper Pottsville consists of lithoarenite, shale, coal, and minor amounts of orthoquartzite and represents a lateral gradation from lower delta-plain distributary channels, to interdistributary bays, to a barrier bar. The Lower and the Upper Pottsville sediments were deposited in two different delta systems (Horsey, 1981). The Pottsville in the north is exposed and has been eroded as a result of upwarping of the Nashville Dome. Approximately 35 separate coal beds occur in the Pottsville Formation; most are fairly local seams, but few are extensive and have been used to define seven coal groups in the Upper Pottsville. Several authors have stratigraphically divided the Pottsville; however, because of limited information, we have characterized the whole interval. <\/SPAN><\/SPAN><\/P>

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Different literature sources were used to find porosity information for the Pottsville Formation (Galicki, 1986; Beard and Meylan, 1987; E. Doherty, personal communication, 1999). This information from the oil fields was added to one of the oil- and gas-field maps. Although porosity data from oil fields range between 1.2 and 15 percent, normal faulting and lineaments present in the basin are the main factors that seems to control both porosity and permeability (Ortiz and others, 1993).<\/SPAN><\/SPAN><\/P>

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According to Owen's (1979) outcrop study of the Paluxy sand in north central Texas, the Paluxy is a quartzarenite consisting of medium to very fine quartz sand and coarse silt, with variable amounts of limonite, hematite, pyrite, and magnetite and insignificant amounts of tourmaline and feldspar. The Paluxy also contains significant amounts (as much as 50 percent in Hood, Parker, and Tarrant Counties) of clay. In general the clay fraction consists of 40 to 50 percent quartz, 5 to 25 percent feldspar, 30 to 40 percent montmorillonite, and less than 10 percent illite and kaolinite. Most of the quartz is of plutonic origin, with lesser amounts of volcanic and vein quartz.<\/SPAN><\/SPAN><\/P>

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Permeability data from oil fields (Galicki, 1986; Beard and Meylan 1987; E. Doherty, personal communication, 1999) are presented on the 2pottsville GIS map. Permeability values range from 0.06 to 54 md. Permeability also appears to occur in fracture-enhanced sands and silts (Ortiz and others, 1993). The normal faulting and lineaments present in the basin are the main factors that seem to control the permeability. Two types of lineaments are characteristic of the N30-60E and N30-60W areas. Some disposal wells have shown good injection rates. But because the permeability is not associated with the rock matrix, injection zones into fractures may have to be determined during drilling with loss of circulation (Ortiz and others, 1993).<\/SPAN><\/SPAN><\/P>

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Several authors have characterized ground-water flow in the Cape Fear interval (Aucott and Speiran, 1985; Miller and others, 1986; Aucott, 1988; Miller, 1990). A number of authors determined that the deep aquifers directly below the coast is a marine/terrestrial ground-water interface zone in which waters tend to be stagnant. Miller and others (1986; their fig. 5) showed that the NA+ concentrations increase with distance along the aquifer flow path, and several authors showed that the Cape Fear aquifer in southeastern South Carolina contains relatively high concentrations of NA+ (Miller and others, 1986; Miller, 1990). On the basis of these data, we conclude that residence times in the Cape Fear aquifer of southeastern South Carolina are long, and may be as much as 5,000 yr.<\/SPAN><\/SPAN><\/P>

<\/P><\/DIV><\/DIV><\/DIV>", "geometryType": "esriGeometryPolygon", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Aucott, W. R., 1988, The predevelopment ground-water flow system and hydrologic characteristics of the Coastal Plain aquifers of south Carolina: U.S. Geological Survey, Water-Resources Investigations Report 86\u20134347, 66 p.\n\n\nAucott, W. R., and Speiran, G. K., 1985, Ground-water flow in the coastal plain aquifers of South Carolina: Ground Water, v. 23, p. 736\u2013745.\n\n\nMiller, J. 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There are few studies that provide estimates of hydraulic conductivity or permeability for the Cape Fear interval. Temples and Waddell (1996) reported permeabilities ranging from 1,000 to 6,000 millidarcys. Aucott (1988), in his modeling studies of regional aquifers, presented a map showing spatial distribution of transmissivities in the Cape Fear interval. We used his transmissivity values. Recalling Hydraulic Conductivity = Transmissivity/Aquifer Thickness, we used the Cape Fear aquifer thickness GIS data layer to convert Aucott's (1988) transmissivity values to hydraulic conductivity.<\/SPAN><\/SPAN><\/P>

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The lower Tertiary and Upper Cretaceous carbonate units are continuous across central Florida (Randazzo, 1997). Moreover, it has been clearly and thoroughly demonstrated that the highly permeable intervals, including the Boulder Zones, in the Floridan aquifer are regionally continuous (Miller, 1986, 1997; Winston, 1996). However, there is no published information regarding the continuity of permeable zones in the lower Cedar Keys and upper Lawson Dolomites. Winston (1977) stated that porosity in the Lawson Dolomite in central Florida is occasionally present and can be quite high. Applin and Applin (1944, 1967), Vernon (1951), and Winston (1994) indicated that this interval is permeable. The cross sections of Chen (1965, his figs. 20, 21) are perhaps the best published information regarding the lithologic variability in these units. On the basis of the variation in lithologic descriptions from this interval, we infer that permeability varies in these units as a function of both sedimentologic and diagenetic processes, which is characteristic of carbonate units. It is possible to map the continuity of porous/permeable zones using geophysical logs but is beyond the scope of the present project.<\/SPAN><\/SPAN><\/P>

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C., 1965, The regional stratigraphic analysis of Paleocene and Eocene rocks of Florida: Florida Geological Survey Bulletin No. 45, 105 p.\n*\nMiller, J. A., 1986, Hydrogeologic framework of the Floridan Aquifer system in Florida and in parts of Georgia, Alabama, and South Carolina: U.S. Geological Survey, Professional Paper 1403-B, 91 p., 33 plates.\n*\n___________ 1997, Hydrogeology of Florida, in Randazzo, A. F., and Jones, D. S., eds., The geology of Florida: Tallahassee, University of Florida Press, p. 69\u201388.\n* \nRandazzo, A. F., 1997, The sedimentary platform of Florida: Mesozoic to Cenozoic, in Randazzo, A. F., and Jones, D. S., eds., The geology of Florida: Tallahassee, University of Florida Press, p. 39\u201356.\n*\nVernon, R. O., 1951, The geology of Citrus and Levy counties, Florida: Florida Geological Survey Bulletin 33, 256 p.\n*\nWinston, G. O., 1977, Cotype wells for the five classic formations in peninsular Florida: Gulf Coast Association of Geological Societies Transactions, v. 27, p. 421\u2013427.\n*\n___________ 1994, The Paleogene of Florida, v. 3. 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Published lithologic descriptions of the lower Cedar Keys and Lawson Dolomites vary (Applin and Applin, 1944, 1967; Vernon, 1951; Chen, 1965), indicating that (1) the boundaries of these units remain poorly defined and/or (2) these units vary laterally. Difference in lithology is primarily degree of dolomitization, crystal size, and relative proportion of anhydrite. As discussed earlier, the formation waters are saline, have been in place for many millennia, and therefore have probably approached equilibrium with the surrounding rock mass. Relatively clean carbonates are the phases that would react with injected CO<\/SPAN><\/SPAN>2.<\/SPAN><\/SPAN><\/P>

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These are dolomites and contain virtually no sand. As is typical in carbonates, the thickness of permeable strata requires more detailed study. <\/SPAN><\/SPAN><\/P>

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Several authors have indicated that the sands in the lower Tuscaloosa Group are regionally continuous (Tucker and Kidd, 1973; Mancini and others, 1987). Alverson (1970) referred to lower Tuscaloosa Groups as a regionally continuous sand reservoir. The cross sections of Mancini and others (1987) provide direct evidence of the degree of sand-body continuity in the Lower Tuscaloosa Group. A large number of geophysical logs that penetrate the Tuscaloosa Group are available. From these logs, it would possible to determine sand-body continuity for the region, if CO<\/SPAN><\/SPAN>2<\/SPAN><\/SPAN> sequestration in the area becomes a serious possibility.<\/SPAN><\/SPAN><\/P>

<\/P><\/DIV><\/DIV>", "geometryType": "esriGeometryPolygon", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Alverson, R. M., 1970, Deep well disposal study for Baldwin, Escambia and Mobile Counties, Alabama: Alabama Geological Survey, Circular 58, 49 p.\n*\nMancini, E. A., Mink, R. M., Payton, J. W., and Bearden, B. 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Porosity data come from two sources, hydrocarbon and waste-disposal-potential assessments (Tucker and Kidd, 1973; Mancini and others, 1987). The data from Tucker and Kidd (1973; their table 2) are primarily used for the GIS. The data in the GIS are ranges of their data. A large number of geophysical logs that penetrate the Tuscaloosa Group are available. From these logs, it would possible to construct a more accurate spatial distribution of porosity, if CO<\/SPAN><\/SPAN>2<\/SPAN><\/SPAN> sequestration in the area becomes a serious possibility. <\/SPAN><\/SPAN><\/P>

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Pressure for Pottsville formation<\/SPAN><\/P>

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Sand-body continuity was related to the depositional systems and facies map (Caughey, 1977) and a map of the salt structures (domes, diapirs, etc.) in the East Texas Basin (Jackson and Seni, 1984) as a means to determine the continuity of the Paluxy Formation.<\/SPAN><\/SPAN><\/P>

<\/P><\/DIV><\/DIV>", "geometryType": "esriGeometryPolygon", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Caughey, C. A., 1977, Depositional systems in the Paluxy Formation (Lower Cretaceous), Northeast Texas; oil, gas, and groundwater resources: The University of Texas at Austin, Bureau of Economic Geology, Geological Circular 77-8, 59 p.\n*\nJackson, M. P. A., and Seni, S. 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Few data are available to determine fluid residence times in the Tuscaloosa Group in the Mobile area. Miller (1990) generally described ground-water flow through the Black Warrior River aquifer (Tuscaloosa Group). He determined that water infiltrates from the surface outcrop belt into the Tuscaloosa Group. The ground water generally flows downdip toward the coast. Miller (1990) determined that the increase in dissolved solid concentration (DSC) in the subsurface water with depth (that is, distance downdip from the outcrop area) is a direct function of fluid residence time. In addition, Miller (1990) concluded that as the ground water encounters the marine water beneath the coastal zone, stagnant conditions prevail. Because the ground water in the Tuscaloosa Group is highly saline (Alverson, 1970; Tucker and Kidd, 1973; Miller, 1990), we determined that the ground water in the Mobile area has protracted residence times. Tuscaloosa ground water in the Mobile area is perhaps as old as 18,000 yr. At that time sea level was about 120 m lower than the present level, the shoreline was near the present shelf edge, and ground-water flow in the Tuscaloosa Formation (in the Mobile area) was more active and not influenced by the marine saltwater wedge. We used a modified version of the Black Warrior River ground-water-flow map of Miller (1990) to describe fluid residence times in the GIS<\/SPAN><\/SPAN><\/P>

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Rock/water reactions are largely a function of formation mineralogy and (if applicable) cement composition. Pore-water chemistry and pore-water residence also significantly influence rock/water reactions. Little information is available regarding the mineralogic composition of the Tuscaloosa Group in the subsurface of southwest Alabama. Alverson (1970; his appendix ) and Tucker and Kidd (1973; their appendix C) provided sample descriptions of the Tuscaloosa Group from two wells. These descriptions indicate that the Tuscaloosa Group sands are mostly composed of rather mature, siliceous sand. Some mica and lignite are reported. Some shell and calcareous material is also reported. From this limited information, we conclude that the potential for significant rock/water reaction with injected CO<\/SPAN><\/SPAN>2<\/SPAN><\/SPAN> is low.<\/SPAN><\/SPAN><\/P>

<\/P><\/DIV><\/DIV>", "geometryType": "esriGeometryPolygon", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Alverson, R. M., 1970, Deep well disposal study for Baldwin, Escambia and Mobile Counties, Alabama: Alabama Geological Survey, Circular 58, 49 p.\n\nTucker, W. E., and Kidd, R. 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Core Laboratory (J. Haberfeld, Florida Department of Environmental Protection, personal communication, 2000) determined porosity of sidewall core samples from 4,500 to 4,950 in the Lawson Dolomite from the Kaiser Mulberry waste-injection well in Polk County, central Florida (J. Haberfeld, Florida Department of Environmental Protection, personal communication, 2000). Their analysis shows that porosity varies between 24.5 and 28.0 percent. For lack of other data, we used this range for the GIS. However, descriptions of the lower Cedar Keys and upper Lawson Dolomites indicate that because porosity varies vertically and horizontally in these units, so this range may not be representative throughout central and southern Florida. <\/SPAN><\/P><\/DIV><\/DIV>", "geometryType": "esriGeometryPolygon", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Haberfeld (Florida Department of Environmental Protection, personal communication, 2000)", "parentLayer": null, "subLayers": [], "minScale": 0, "maxScale": 0, 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Although we have no direct evidence, we do know that the lower Cedar Keys and Lawson Dolomites are platform carbonates, and therefore we conclude that the clay content is low (<5 percent). It would be possible to calculate clay percent from geophysical logs that penetrate this interval.<\/SPAN><\/SPAN><\/P>

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A number of studies present cross sections of the Cape Fear interval that include geophysical logs (gamma ray, spontaneous potential) (Colquhoun and others, 1983; Aucott and others, 1987; Temples and Waddell, 1996). These logs are a source of semiquantitative estimates of percent shale in the Cape Fear interval. Brown and others (1979) provided actual percentages for the Cape Fear interval (their Unit E), but these estimates are from wells in Georgia. Gohn and others (1977) presented results of textural and mineralogical analysis of the Cape Fear Formation conducted on samples from a well near Charleston. Their analyses indicate that the Cape Fear interval is primarily silt and that shale composes between 20 and 40 percent of the unit. For the GIS, we combined the analysis of Gohn and others (1977; their fig. 3) and Brown and others (1979). These shale percentages generally agree with the estimates derived from the geophysical logs.<\/SPAN><\/SPAN><\/P>

<\/P><\/DIV><\/DIV>", "geometryType": "esriGeometryPolygon", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Aucott, W. R., Davis, M. E., and Speiran, G. K., 1987, Geohydrologic framework of the Coastal Plain aquifers of South Carolina: U.S. Geological Survey, Water-Resources Investigations Report 85-4271, 7 sheets.\n*\nBrown, P. M., Brown, D. L., Reid, M. S., and Lloyd, O. B., Jr., 1979, Evaluation of the geologic and hydrologic factors related to the water-storage potential of Mesozoic aquifers in the southern part of the Atlantic coastal plain, South Carolina and Georgia: U.S. Geological Survey, Professional Paper 1088, 37 p., 11 plates.\n* \nColquhoun, D. J., Woollen, L. D., Van Nienwenhuise, D. S., Padgett, G. G., Oldham, R. W., Boylan, D. C., Bishop, J. W., and Howell, P. D., 1983, Surface and subsurface stratigraphy, structure and aquifers of the South Carolina Coastal Plain: Columbia, SC, State of South Carolina, Office of the Governor, 78 p. \n*\nGohn, G. S., Higgins, B. B., Smith, C. C., and Owens, J. P., 1977, Lithostratigraphy of the deep corehole (Clubhouse Crossroads Corehole 1) near Charleston, South Carolina: U.S. Geological Survey, Professional Paper 1028E, p. 59\u201370.\n*\nTemples, T. J., and Waddell, M. 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There are essentially no data on ground-water flow rates and directions in the lower Cedar Keys and upper Lawson Dolomites. However, Meyers (1989, his fig. 13) showed that ground water in the lower Floridan aquifer are 10,000 yr old. In all probability the ground waters in the underlying lower Cedar Keys and upper Lawson Dolomites are significantly older. Therefore, we assign a date of more than 20,000 yr for fluid residence time in the lower Cedar Keys and upper Lawson Dolomites of southern Florida.<\/SPAN><\/SPAN><\/P>

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Permeability has been determined for the Lawson Dolomite in a liquid waste-disposal well located in Mulberry, Polk County, Florida (J. Haberfeld, Florida Department of Environmental Protection, personal communication, 2000). The permeabilities were determined by Core Lab, Incorporated, from sidewall cores. Permeabilities from eight samples range from 5 to 28 millidarcys. Because we lack any other permeability, we assign this range for all of southern Florida. More permeability data are available from geophysical logs taken for petroleum exploration and production from Lower Cretaceous horizons. It is surprising that reported permeabilities are so low, considering that porosities are 24 to 28 percent. <\/SPAN><\/SPAN><\/P>

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A number of studies present cross sections of the Cape Fear interval that include geophysical logs (gamma ray, spontaneous potential) (Colquhoun and others, 1983; Aucott and others, 1987; Temples and Waddell, 1996). These logs are a source of semiquantitative estimates of sand thickness in the Cape Fear interval. Brown and others (1979) provided actual sand thickness for the Cape Fear interval (their Unit E), but these estimates are from wells in Georgia. Gohn and others (1977) presented results of textural and mineralogical analyses of the Cape Fear Formation conducted on samples from a well near Charleston. Their analyses indicate that the Cape Fear interval is primarily silt, but there are some sand intervals. Sand-thickness estimates are considerably lower than estimates derived from the geophysical logs (which are typically 50 ft). We attribute the difference to the geophysical-log response to silt intervals being similar to that of sand. Temples and Waddell (1996) reported that for the Middendorf and Cape Fear aquifers in southeasternmost South Carolina, between 2,770 and 3,763, there is 381 ft of aquifer sand. Brown and others (1979) determined that the sands in the Cape Fear interval (their unit E) in Georgia generally range from 40 to 58, with an average of 49. We attribute the thicker sands in southeasternmost South Carolina and in Georgia to a deeper basement and thicker Cape Fear interval. For the GIS we combined sand-thickness information of Gohn and others (1977), Brown and others (1979), and Temples and Waddell (1996).<\/SPAN><\/SPAN><\/P>

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The Cape Fear Formation contains substantial volumes of clays and labile minerals that can potentially react with ground water (Gohn and others, 1977). Miller and others (1986) provided an excellent discussion of sediment/water interaction as a function of ground-water residence time in southeastern U.S. coastal plain aquifers. For the GIS we used information from Miller and others (1986) to characterize rock/water reactions that can be expected in the Cape Fear hydrostratigraphic interval. Immature sands may have moderate potential for interaction with high-CO<\/SPAN><\/SPAN>2<\/SPAN><\/SPAN> fluids.<\/SPAN><\/SPAN><\/P>

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Few data were available on the chemistry of brines in the deep subsurface. We chose to use the data of Vernon (1970), who presented water-chemistry-analysis results from selected oil fields in the Coral Gables area. Also a formation water chemistry table from the Lower Cretaceous Sunniland Limestone was added to the GIS data base.<\/SPAN><\/P>

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Digitized data from Kreitler and others (1984, their table 1) chemical analyses of produced waters.<\/SPAN><\/P>

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Few data were available on the chemistry of brines in the deep subsurface. We chose to use the data of Vernon (1970), who presented water-chemistry-analysis results from selected oil fields in the Coral Gables area. Also a formation water chemistry table from the Lower Cretaceous Sunniland Limestone was added to the GIS data base.<\/SPAN><\/P><\/DIV><\/DIV><\/DIV>", "geometryType": "esriGeometryPolygon", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Vernon, R. 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Porosity data for Cape Fear<\/SPAN><\/P>

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Several studies characterize the confining unit above the Cape Fear Formation as a tight marine shale (Aucott and others, 1987; Aucott, 1988; Miller, 1990), and the shale interval is apparent in published cross-sections (Colquhoun and others, 1983; Aucott and others, 1987). However, there is no published map showing thickness of the Cape Fear confining unit. On the basis of evaluation of logs in published cross sections, we determined that the thickness of the confining unit is consistent across southeastern South Carolina and averages about 50 ft. <\/SPAN><\/SPAN><\/P>

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Vernon (1970, his app. I) demonstrated that salinity within the Floridan aquifer increases with depth and at about 2,900 ft (in the Coral Gables area) that total dissolved solids (TDS) is 35,000 mg/L. Brines from oil fields that produce from the Lower Cretaceous Sunniland Limestone have TDS concentrations of about 200,000 mg/L (Meyer, 1989, his table 11). We therefore conclude that TDS concentrations in the lower Cedar Keys and upper Lawson Dolomites are between 35,000 and 200,000 mg/L, which is shown in the GIS.<\/SPAN><\/SPAN><\/P>

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A number of studies present cross sections of the Cape Fear interval that include geophysical logs (gamma ray, spontaneous potential) (Colquhoun and others, 1983; Aucott and others, 1987; Temples and Waddell, 1996). These cross sections indicate that sands are generally discontinuous (R. Willoughby, South Carolina Geological Survey, personal communication, 2000). Brown and others, (1979; their table 7) determined that the thickest potential reservoir sand in the Cape Fear interval ranges from 40 to 58, with an average of 49. These thicker sands tend to be more continuous. For the GIS, we chose to use the thickness of reservoir sand as determined by Brown and others (1979).<\/SPAN><\/SPAN><\/P>

<\/P><\/DIV><\/DIV>", "geometryType": "esriGeometryPolygon", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Aucott, W. R., Davis, M. E., and Speiran, G. K., 1987, Geohydrologic framework of the Coastal Plain aquifers of South Carolina: U.S. Geological Survey, Water-Resources Investigations Report 85-4271, 7 sheets.\n*\nBrown, P. M., Brown, D. L., Reid, M. S., and Lloyd, O. 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Temples and Waddell (1996) provided the results of chemical analysis of water samples from the Cape Fear interval from a well on Hilton Head Island. Their results are presented in the GIS. Their results indicate that salinities are very low for the interval.<\/SPAN><\/P><\/DIV><\/DIV><\/DIV>", "geometryType": "esriGeometryPolygon", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Temples, T. J., and Waddell, M. 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Single value of hydraulic conductivity (meters/day) averaged from values reported by the Florida Geological Survey for saltwater disposal wells injecting into the Tuscaloosa Formation in the Jay Field, northwestern Florida. Single representative porosity value, as a fraction of rock volume, averaged from values reported by the Florida Geological Survey for saltwater disposal wells injecting into the Tuscaloosa Formation in the Jay Field, northwestern Florida.<\/SPAN><\/P><\/DIV><\/DIV><\/DIV>", "geometryType": "esriGeometryPolygon", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "References for Florida and South Georgia Tuscaloosa data collection:\n\n *Barker, R. A., and Pernik, M., 1994, Regional hydrology and simulation of deep ground-water flow in the Southeastern Coastal Plain Aquifer system in Mississippi, Alabama, Georgia, and South Carolina: U.S. Geological Survey Professional Paper 1410-C, 87 p.\n\n *Gohn, G. S., Smith, C. C., Christopher, R. A., and Owens, J. P., 1980, Preliminary stratigraphic cross sections of Atlantic coastal plain sediments of the southeastern United States: U.S. Geological Survey, Miscellaneous Field Studies Map MF-1015-C.\n\n *Miller, James A., 1979, Potential subsurface zones for liquid-waste storage in Florida: Bureau of Geology, Florida Department of Natural Resources, Map Series No. 94.\n\n *Renkin, R. A., Mahon, G. L., and Davis, M. E., 1989, Hydrogeology of clastic Tertiary and Cretaceous regional aquifers and confining units in the southeastern coastal plain aquifer system of the United States: U.S. Geological Survey Hydrologic Investigations Atlas HA-701, 3 sheets.\n\n *Scholle, P. A., 1979, Data summary and petroleum potential: in cholle, P. A., editor, Geological studies of the COST-GE-1 well, United States South Atlantic Outer Continental Shelf area: U. S. 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Sand-body continuity can be found by using a generalized map of depositional systems (Oliver, 1971). A more detailed facies map is available (Calavan, 1985). Site studies are needed to asses the site-specific complexity of this heterogeneous system.<\/SPAN><\/SPAN><\/P>

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Permeability data come from two sources, hydrocarbon and waste-disposal-potential assessments (Tucker and Kidd, 1973; Mancini and others, 1987). The data from Tucker and Kidd (1973; their table 2) are primarily used for the GIS. The data in the GIS are ranges of their data. A large number of geophysical logs that penetrate the Tuscaloosa Group are available. From these logs, it would possible to construct a more accurate spatial distribution of permeability, if CO<\/SPAN><\/SPAN>2<\/SPAN><\/SPAN> sequestration in the area becomes a serious possibility. <\/SPAN><\/SPAN><\/P>

<\/P><\/DIV><\/DIV>", "geometryType": "esriGeometryPolygon", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "Mancini, E. A., Mink, R. M., Payton, J. W., and Bearden, B. L., 1987, Environments of deposition and petroleum geology of the Tuscaloosa Group (Upper Cretaceous), South Carlton and Pollard Fields, southwestern Alabama: American Association of Petroleum Geologists Bulletin, v. 71, p. 1128\u20131142.\n\nTucker, W. E., and Kidd, R. 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The Eagle Ford has been eroded over the Sabine Uplift in the eastern part of the study area (see 7woodbine); however, the low-transmissivity Austin Chalk extends over this area. Faults of the Mexia-Talco and Elkhart-Mt. Enterprise fault zones cut the seals. These faults create traps for oil fields, the extent to which they may locally leak unknown. Fault zones have isolated Woodbine sandstones within the basin from recharge zones in Woodbine outcrops on the east and north basin edges (Kreitler and others, 1984). If these faults can be shown to be tight to CO<\/SPAN><\/SPAN>2<\/SPAN><\/SPAN>, this geometry may create a desirably large but hydrologically isolated brine volume. Salt diapers penetrate the Cretaceous section, and there is some evidence of at least geologic rates of discharge up some dome flanks (Kreitler and others, 1984). In the structurally and stratigraphically complex areas around salt diapers, site-specific data on the potential for leakage are needed. Nonpenetrative salt pillows may also impact flow at depth.<\/SPAN><\/SPAN><\/P>

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DE-AC97-80ET46617, 156 p. \n*\nSeni, S. J., and Jackson, M. P. 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Shapefile containing a polygon outlining the primary area of possible sequestration interest.<\/SPAN><\/P><\/DIV><\/DIV><\/DIV>", "geometryType": "esriGeometryPolygon", "sourceSpatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "spatialReference": { "wkid": 102100, "latestWkid": 3857, "xyTolerance": 0.001, "zTolerance": 0.001, "mTolerance": 0.001, "falseX": -20037700, "falseY": -30241100, "xyUnits": 10000, "falseZ": -100000, "zUnits": 10000, "falseM": -100000, "mUnits": 10000 }, "copyrightText": "References for Florida and South Georgia Tuscaloosa data collection:\n\n *Barker, R. A., and Pernik, M., 1994, Regional hydrology and simulation of deep ground-water flow in the Southeastern Coastal Plain Aquifer system in Mississippi, Alabama, Georgia, and South Carolina: U.S. Geological Survey Professional Paper 1410-C, 87 p.\n\n *Gohn, G. S., Smith, C. C., Christopher, R. A., and Owens, J. P., 1980, Preliminary stratigraphic cross sections of Atlantic coastal plain sediments of the southeastern United States: U.S. Geological Survey, Miscellaneous Field Studies Map MF-1015-C.\n\n *Miller, James A., 1979, Potential subsurface zones for liquid-waste storage in Florida: Bureau of Geology, Florida Department of Natural Resources, Map Series No. 94.\n\n *Renkin, R. A., Mahon, G. L., and Davis, M. E., 1989, Hydrogeology of clastic Tertiary and Cretaceous regional aquifers and confining units in the southeastern coastal plain aquifer system of the United States: U.S. Geological Survey Hydrologic Investigations Atlas HA-701, 3 sheets.\n\n *Scholle, P. A., 1979, Data summary and petroleum potential: in cholle, P. A., editor, Geological studies of the COST-GE-1 well, United States South Atlantic Outer Continental Shelf area: U. S. 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