MRCSP Phase I Geologic Characterization Report - Midwest ...

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T 54 CHARACTERIZATION OF GEOLOGIC SEQUESTRATION OPPORTUNITIES IN THE MRCSP REGION 500 EXPLANATION Faults 500 500 ft Index contours 50 ft contours Thickness in feet 2000 1000 0 1000 500 300 100 M A P P I N G O F P R O J E C M I T L L I I M I T 0 50 25 0 50 100 Miles 50 25 0 50 100 150 Kilometers ³ Figure A2-2.—Map showing the thickness of the Cambrian basal sandstones interval.
APPENDIX A: CAMBRIAN BASAL SANDSTONES 55 study area (Figure 5). The name Mt. Simon Sandstone was first used by Walcott (1914) to designate a sandstone exposed near Eau Claire, Wisconsin (the type section). The Potsdam, described by Emmons (1838), was named for sandstone cropping out at Potsdam, New York. Haynes (1891) named the Conasauga Group for exposures of shale and limestone in the Conasauga Valley of northwest Georgia. The reader is referred to the following papers which include discussions on formal and informal nomenclature relative to the lower Sauk interval in statewide to semi-regional context (Cohee, 1948; Fettke, 1948; Sloss and others, 1949; Freeman, 1953; McGuire and Howell, 1963; Catacosinos, 1973; Janssens, 1973; Rickard, 1973; Calvert, 1974; Wagner, 1976; Bricker and others, 1983; Patchen and others, 1985a,b; Shaver and others, 1986; Rupp, 1991; Ryder, 1991, 1992a,b; Riley and others, 1993; Ryder and others, 1995, 1996; Harris and others, 2004). NATURE OF LOWER AND UPPER CONTACTS The basal sandstone interval directly overlies the Precambrian unconformity surface, which locally may have significant topographic and/or structural relief (most apparent in western Ohio where well control is greatest). In some local areas, the entire interval is missing or is thicker due to incised channel development. The thickness of the interval can vary dramatically over such features, thus affecting reservoir quality in these areas. The lower contact is generally sharp due to a regolith found at the base of these rocks, but may appear gradational on geophysical logs depending on the underlying Precambrian lithology. A decrease in grain size and an increase in lithic and feldspathic components at the top of the Mt. Simon make the upper contact, where it underlies the Eau Claire Formation, appear gradational in the western part of the MRCSP study area. The upper contact is moderately gradational in the eastern region where thin discontinuous dolomitic sandstone layers of the Conasauga Group and Potsdam mark the top of the interval. The upper contact of the unnamed basal sandstones in the Rome trough and the adjacent eastern region is considered disconformable with the overlying Tomstown and Rome Formations (Harris and others, 2004). Gamma-ray log response of the Mt. Simon in western Ohio and the proto-Illinois/Michigan basin is relatively lower than that of the overlying Eau Claire Formation, indicating sandstone with lower feldspar, shale, and glauconite content. Gamma-ray curve shapes range from blocky-, to funnel-, and bell-shaped. Density and photoelectric (PE) logs are indicative of relatively higher quartz content of the Mt. Simon. The log response of the lower portion of the Mt. Simon locally appears cyclic, and may representing alternating beds of quartz arenite, shale, arkose, and sublitharenite. Conversely, the gamma-ray log response of the unnamed Conasauga sandstones and Potsdam Formation is higher than that of the Mt. Simon, an indicator of higher feldspar, shale, and glauconite content. Gamma-ray curve shapes for the unnamed Conasauga sandstones and Potsdam Formation are typically more ”spikey” than those of the Mt. Simon, indicating the greater cyclicity of lithologic components. PE logs of the Conasauga and Potsdam also indicate a higher dolostone content than the Mt. Simon. In eastern Kentucky, core from one well indicates that basal sandstones in the Rome trough are commonly arkosic, an attribute that affects the gamma ray log, giving a more shaley appearance. LITHOLOGY The Mt. Simon Sandstone is a white, pink, or purple, fine- to coarse-grained, moderately to well-sorted, quartz arenite that can be arkosic. The Mt. Simon also contains thin interbeds of red, green, gray, or black, sandy to silty shale. Locally, thin beds of tight, silicacemented quartz arenite occur. Bedding thickness ranges from thin to medium with many beds containing lamina and wisps of finer grained materials. Graded beds and cross bedding are common. Bioturbation is present but generally, poorly developed. However, in Michigan, preservation of burrowing has been observed to increase upward towards the contact with the overlying Eau Claire. Grains are sub-rounded to rounded, commonly etched and generally poorly cemented and friable. The lower portion is commonly conglomeratic and shaley, and stained by hematite, some of which is mottled. In the Michigan subsurface, dolomite cement is common in some intervals around the basin margin. Deeper in the proto-Michigan basin, below 7,000 feet, there is pervasive quartz overgrowth cement. Secondary porosity is common where carbonate cement and feldspar has been dissolved. The unnamed Conasauga sandstone and Potsdam Sandstone consist of interbedded, cyclical-appearing sandstone and dolostone. The sandstone components are typically white to light-gray and pinkish gray, and fine- to medium-grained, with moderate- to well-sorted, sub-rounded to angular grains, although arkosic sandstones occur in the basal portions of the Potsdam in northwestern Pennsylvania and south-central New York. Authigenic and primary feldspar, glauconite, and bioturbated zones are common. Normal and reverse graded bedding and trough cross-bedding are common thoughout the unit. Coarse to pebbly, normal graded bedding, and thin zones of rip-up clasts mark thin intercyclic intervals. Bedding ranges from thin to medium and massive, to interbedded with laminated and wispy dark gray shale. Bioturbation, including filled vertical burrows (Skolithos), graded bedding, and cross-bedding are common. The dolostone is light to medium gray and pinkish gray, cryptocrystalline, microcrystalline, medium crystalline, and arenaceous. Minor beds and laminae of gray to black shale, frosted quartz grains, vugs filled with selenite and dolomite crystals, ooids, pelloids, disseminated pyrite, laminae and thin beds of glauconite, apatite, flat pebble conglomerate, rip-up clasts, mudcracks, and clay-rich zones are also present (Harris and others, 2004; Baranoski, in preparation). The basal sandstones of the Rome trough are arkosic and, based upon a core from a well in Wolfe County, Kentucky, are interbedded with red and green shale, siltstone, sandy shale, and nodular evaporites. The unit is locally conglomeratic and may contain poorly developed cross beds (Harris and others, 2004). DISCUSSION OF DEPTH AND THICKNESS RANGES Depth to the top of the basal sandstones interval ranges from approximately 2,000-feet below sea level (bsl) in northern Ohio and northwestern Indiana on the Ohio-Indiana platform to 14,000 feet bsl in the center of the Michigan basin, and 20,000 to 25,000 feet bsl in the Rome trough of southwestern Pennsylvania (Figure A2-3). Thickness ranges from zero, where local Precambrian topography (Janssens, 1973; Baranoski, 2002) exists, to more than 2,500 feet in northwestern Indiana and east-central portion of Illinois, just west of the MRCSP study area (Figure A2-2). This thick accumulation of sediments, or depocenter, is unique in its location, not being coincident with depocenters for any younger stratigraphic units. The Mt. Simon reaches a thickness in excess of 1,300 feet in east-central Michigan (Figure A2-2), where again this depositional pattern is not seen in other geologic units. Eastward, away from the Illinois and Michigan basins, the Mt. Simon is 50 to 300 feet thick in Ohio and adjacent central Kentucky. In eastern Kentucky, the Mt. Simon gradually thins eastward toward the Rome trough. The unnamed
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Characterization of Geologic Seques
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ABOUT THE MRCSP The Midwest Regiona
Page 5 and 6:
CONTENTS About the MRCSP ..........
Page 7 and 8:
CONTENTS Figure A14-2.—Structure
Page 9 and 10:
1 CHARACTERIZATION OF GEOLOGIC SEQU
Page 11 and 12: BACKGROUND INFORMATION 3 (a minimum
Page 13 and 14: INTRODUCTION TO THE MRCSP REGION’
Page 21 and 22: GEOLOGIC MAPPING PROCEDURES, DATA S
Page 35 and 36: OIL, GAS, AND GAS STORAGE FIELDS 27
Page 41 and 42: CO 2-SEQUESTRATION STORAGE CAPACITY
Page 53 and 54: CONCLUSIONS AND REGIONAL ASSESSMENT
Page 55 and 56: REFERENCES CITED 47 National Confer
Page 57 and 58: 49 APPENDIX A Geologic Summaries of
Page 59 and 60: APPENDIX A: PRECAMBRIAN UNCONFORMIT
Page 61: APPENDIX A: CAMBRIAN BASAL SANDSTON
Page 65 and 66: APPENDIX A: CAMBRIAN BASAL SANDSTON
Page 67 and 68: APPENDIX A: BASAL SANDSTONES TO TOP
Page 73 and 74: APPENDIX A: UPPER CAMBRIAN ROSE RUN
Page 81 and 82: APPENDIX A: KNOX TO LOWER SILURIAN
Page 87 and 88: N T R APPENDIX A: KNOX TO LOWER SIL
Page 89 and 90: APPENDIX A: MIDDLE ORDOVICIAN ST. P
Page 91 and 92: -6000 -8000 APPENDIX A: MIDDLE ORDO
Page 93 and 94: APPENDIX A: LOWER SILURIAN MEDINA G
Page 101 and 102: APPENDIX A: NIAGARAN/LOCKPORT THROU
Page 103 and 104: APPENDIX A: NIAGARAN/LOCKPORT THROU
Page 105 and 106: A APPENDIX A: NIAGARAN/LOCKPORT THR
Page 107 and 108: APPENDIX A: MIDDLE SILURIAN NIAGARA
Page 109 and 110: -3000 APPENDIX A: MIDDLE SILURIAN N
Page 111 and 112: APPENDIX A: LOWER DEVONIAN MANDATA
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APPENDIX A: LOWER DEVONIAN ORISKANY
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APPENDIX A: LOWER DEVONIAN SYLVANIA
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-2000 APPENDIX A: LOWER DEVONIAN SY
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25 APPENDIX A: LOWER/MIDDLE DEVONIA
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APPENDIX A: DEVONIAN ORGANIC-RICH S
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( ( ( ( APPENDIX A: PENNSYLVANIAN C
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APPENDIX A: PENNSYLVANIAN COAL BEDS
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APPENDIX A: LOWER CRETACEOUS WASTE
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APPENDIX A: REFERENCES CITED 143 Sa
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APPENDIX A: REFERENCES CITED 145 an
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APPENDIX A: REFERENCES CITED 147 lo
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APPENDIX A: REFERENCES CITED 149 Pa
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APPENDIX A: REFERENCES CITED 151 Th
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