MRCSP Phase I Geologic Characterization Report - Midwest ...

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112 CHARACTERIZATION OF GEOLOGIC SEQUESTRATION OPPORTUNITIES IN THE MRCSP REGION Table A11-1.—Summary of data for Oriskany Sandstone gas storage fi elds in the Appalachian basin. Modifi ed from American Gas Association (2001) Storage Field/ Max. Reservoir Name County Depth Min. Total Gas Maximum Avgerage Year Year Depth # Wells (Base + Working) Pressure State/Province Thickness Discovered Activated (ft) (MMcf) (psi) Accident Garrett 7900 7300 100 75 61978 3050 1953 1966 Maryland Columbiana Columbiana 3558 nr 6 16 3111 1450 1944 1950 Ohio Guernsey Guernsey, Coshocton 3580 3114 8 48 7100 1150 1942 1954 Ohio Artemas “A” Bedford 6095 5643 50 16 14457 2100 1962 1972 Pennsylvania Artemas “B” Bedford, Allegany 4931 4774 50 4 2147 1900 1963 1972 Pennsylvania Ellisburg Potter 5382 4889 27 84 98430 2200 1933 1963 Pennsylvania Greenlick Potter, Clinton 6860 6443 39 46 53220 4240 1955 1961 Pennsylvania Harrison Potter, Steuben 5243 4702 24 44 34100 2140 1934 1953 Pennsylvania Hebron Potter 5403 4842 18 48 29280 2200 1931 1953 Pennsylvania Leidy Clinton, Potter 6609 5605 22 64 102003 4200 1950 1959 Pennsylvania Meeker Tioga 4307 4135 5 3 5200 1680 1931 1943 Pennsylvania Palmer Tioga 4320 3987 5 13 16000 1680 1930 1938 Pennsylvania Sabinsville Tioga 4951 4171 23 41 35618 2130 1935 1951 Pennsylvania Sharon Potter 4979 4642 17 12 4500 860 1938 1948 Pennsylvania Summit Erie 2450 2279 20 45 4200 800 1946 1959 Pennsylvania Tamarack Clinton 7159 6740 40 11 11220 4200 1952 1971 Pennsylvania Tioga Tioga 4128 3679 24 31 36000 1680 1930 1951 Pennsylvania Wharton Potter, Cameron 6552 5371 19 71 31668 3600 1933 1963 Pennsylvania Augusta Hampshire 5749 4806 147 6 6961 2797 1953 1971 West Virginia Coco “A” Kanawha 6761 4955 20 74 44500 1800 1944 1950 West Virginia Coco “B” Kanawha 5446 5041 20 20 9700 1800 1944 1951 West Virginia Coco “C” Kanawha 5556 5094 20 27 17270 1800 1944 1957 West Virginia Hunt Kanawha 5386 5027 20 19 5839 1200 1947 1951 West Virginia Little Capon Hampshire 5761 5243 150 6 7451 2804 1965 1971 West Virginia Ripley Jackson 5184 4777 20 49 25050 1675 1945 1954 West Virginia Rockport Wirt; Wood 5401 4855 20 25 8160 1800 1948 1953 West Virginia Blackhawk Beaver 4673 4660 10 7 2655 2000 1936 1969 Pennsylvania North Summit Fayette 7145 6394 168 22 21851 3000 1937 1991 Pennsylvania Glady Randolph, Pocahontas 6930 4914 150 49 31200 2050 1954 1964 West Virginia Terra Alta Preston 6227 4676 150 32 41663 2350 1946 1960 West Virginia Terra Alta South Preston 6582 4954 150 30 16600 2350 1953 1970 West Virginia Rager Mtn. Cambria 8045 7680 42 7 20493 3200 1965 1971 Pennsylvania TOTAL = 809625
APPENDIX A: LOWER DEVONIAN SYLVANIA SANDSTONE 113 any other formations within the northern Appalachian basin (AGA, 2001). At least 32 gas storage fields are found within the Oriskany, with a combined storage capacity of nearly 1 TCF, and located in pinchout, stratigraphic, and structural traps (Table A11-1). Many of these storage fields have been in operation since the 1950s, attesting to the integrity of the fields and seals. In all likelihood the Oriskany Sandstone would make a suitable target for storage of CO 2-miscible fluids, but only after thorough evaluation of the formation at potential target sites. Such target sites include: 1) zones of high porosity and high permeability associated with updip sandstone pinchout, typical of eastern Ohio, and along the southern and eastern boundaries of the “Oriskany no-sand area” in northwestern Pennsylvania; 2) areas of highly fractured Oriskany Sandstone associated with salt solution and migration within the central depositional area of western Pennsylvania and central West Virginia; and 3) areas of intensely faulted and multi-tiered (duplexed) Oriskany Sandstone in the Valley and Ridge of central Pennsylvania, western Maryland, and eastern West Virginia. 12. LOWER DEVONIAN SYLVANIA SANDSTONE The Sylvania Sandstone, late Early Devonian in age, is a quartzose sandstone that grades laterally into sandy limestone and dolostone in parts of the Michigan basin. The Sylvania is the basal formation of the Detroit River Group and, along with the Bois Blanc and Garden Island Formations, overlie the Kaskaskia unconformity (Figure 5). Gardner (1974) suggests the lower part of the Sylvania may be in facies relationship with the underlying Bois Blanc, especially in northern and western regions of the Michigan basin. However, the relationship of this lower contact is poorly documented, and the recent revision of the Michigan stratigraphic column by the Michigan Geological Survey shows an unconformity between the Sylvania and Bois Blanc Formations. The upper part of the Sylvania intertongues with carbonates of the overlying Amherstburg Formation, another unit in the Detroit River Group. Although arenaceous units are present at various stratigraphic positions above the Kaskaskia unconformity in Michigan, as well as in the Appalachian basin portion of the MRCSP study area—for example the Oriskany Sandstone in Ohio, Pennsylvania, and West Virginia—use of the name Sylvania Sandstone should be restricted to the sandstone that occurs at the base of the Detroit River Group in the Michigan basin (Fisher and others, 1988). In general, details on the vertical and lateral stratigraphic relationships of the Sylvania, its internal lithologic variations, and those attributes making it suitable as a geologic reservoir for CO 2 sequestration, are uncertain for most of the Michigan basin. ORIGIN OF NAMES, TYPE SECTION, SIGNIFICANT EARLIER STUDIES Orton (1888) applied the name Sylvania Sandstone to exposures, incorrectly identified as Oriskany by Newberry (1871), in Sylvania Township, Lucas County, Ohio. Other significant investigations on the Sylvania include Grabau and Sherzer (1910), Alty (1933), Carman (1936), and Hatfield and others (1968). Also, Gardner (1974), as part of a detailed subsurface study, presented regional isopach and lithofacies maps of the Sylvania Sandstone in Michigan. NATURE OF LOWER AND UPPER CONTACTS The Sylvania Sandstone overlies the Kaskaskia unconformity in southeastern Michigan above the truncated Silurian-age Bass Islands Group. The Sylvania is thin, discontinuous, or completely absent in some areas, especially on the southern and western margins of the Michigan basin. Typically the Bois Blanc underlies the Sylvania although the exact stratigraphic relationship between these two units is unclear. The lateral extent and isopach pattern of the Sylvania Sandstone (Figure A12-1) and Bois Blanc Formation suggests a northwest- to southeast-trending shallow marine basin existed in the area at the time of deposition of the Sylvania (Gardner, 1974). This basin may be related to the trend of the Mid-Michigan rift (Figure 6). The Sylvania Sandstone is the basal unit of the Detroit River Group; its upper contact with the overlying Amherstburg Formation is gradational and intertonguing. LITHOLOGY Regional lithologic variations within the Sylvania Sandstone are known mainly from the analysis of geophysical logs (Gardner, 1974). These analyses suggest the Sylvania Sandstone typically consists of dolomitic to cherty, fine- to medium-grained, well-sorted and rounded, quartzose sandstone in central and southeastern lower Michigan but grades into cherty, sandy carbonate in other regions of the Michigan basin. Carbonate interbeds, sometimes containing chert, are common throughout the unit. The Sylvania, in general, is very porous in outcrops and in materials recovered from shallow subsurface cores and exploratory drill holes, particularly in southeastern lower Michigan. Locally, quartz overgrowths and carbonate cement are present in the unit. Most quartz sand grains of the Sylvania are frosted and pitted. Marine fossils, mainly brachiopods, are common in many of the calcareous interbeds. Cross beds and other current-induced sedimentary structures are common in outcrops but rarely observed in cores. DISCUSSION OF DEPTH AND THICKNESS RANGES The Sylvania Sandstone ranges from just a few feet thick in northeastern and southwestern areas of the Michigan basin to a maximum thickness of about 350 feet; the area of maximum thickness occurs mostly along a northwest- to southeast-trending belt across the central portion of the basin (Figure A12-1). These thickness estimates are based on geophysical log picks but are problematic due to the complex lithologic variations above, below, and within the geologic interval containing the Sylvania. As previously noted, the northwest- to southeast-oriented isopach pattern is similar to the underlying Bois Blanc Formation, suggesting a similar depositional and structural setting for both units. Moreover, the area of maximum thickness of the Sylvania closely mimics the eastern margin of the Mid-Michigan rift, a feature interpreted as a pre-Paleozoic age failed continental rift. Structural movement resulting from reactivation of parts of the rift may have influenced depositional trends within the Sylvania. These structures may have created basin topography/bathymetry that existed during the transgressive phase of Lower and Middle Devonian sediments that were deposited on top of the Kaskaskia unconformity. The Sylvania Sandstone ranges in depth from in excess of 400 feet above sea level in the southeastern corner of the state to over 4,400 feet below sea level in the central portion of the basin (Figure A12-2).
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Characterization of Geologic Seques
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ABOUT THE MRCSP The Midwest Regiona
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CONTENTS About the MRCSP ..........
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CONTENTS Figure A14-2.—Structure
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1 CHARACTERIZATION OF GEOLOGIC SEQU
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BACKGROUND INFORMATION 3 (a minimum
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INTRODUCTION TO THE MRCSP REGION’
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GEOLOGIC MAPPING PROCEDURES, DATA S
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OIL, GAS, AND GAS STORAGE FIELDS 27
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CO 2-SEQUESTRATION STORAGE CAPACITY
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CONCLUSIONS AND REGIONAL ASSESSMENT
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REFERENCES CITED 47 National Confer
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49 APPENDIX A Geologic Summaries of
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APPENDIX A: PRECAMBRIAN UNCONFORMIT
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APPENDIX A: CAMBRIAN BASAL SANDSTON
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APPENDIX A: BASAL SANDSTONES TO TOP
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