MRCSP Phase I Geologic Characterization Report - Midwest ...

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136 CHARACTERIZATION OF GEOLOGIC SEQUESTRATION OPPORTUNITIES IN THE <strong>MRCSP</strong> REGION Figure A17-2.—Outcrop belt of the Potomac Group and the Magothy Formation (from Glaser, 1969). known, but Hansen (1984) suggests that these offshore units may represent lower deltaic distributory facies and marine shelf or deltafront facies, whereas the Waste Gate beds underlying the Delmarva Peninsula may represent upper deltaic fluvial facies. The Waste Gate Formation is dated Berriasian to Hauterivian() because it contains pre-Zone I palynomorphs apparently older than the mid-Barremian to early Albian assemblages characteristic of the overlying Patuxent Formation (Doyle, 1982; Hansen, 1982, 1984). ORIGIN OF NAMES, TYPE SECTION, SIGNIFICANT EARLIER STUDIES ON THIS INTERVAL The Waste Gate Formation was originally proposed and defined in an open-file report by Hansen (1982) and subsequently formally named in an information circular by Hansen (1984). The type section was actually designated from the Ohio Oil Company L. G. Hammond No. 1 well (Maryland <strong>Geologic</strong>al Survey well number
APPENDIX A: LOWER CRETACEOUS WASTE GATE FORMATION 137 Figure A17-3.—Diagram showing the Fall Zone, the Salisbury Embayment and other tectonic features of the middle Atlantic area (from Hansen, 1978). Wi-Cg 37) at a depth interval of 4,745 to 5,360 feet. The well was drilled in Maryland about 22 miles west of the Atlantic coast, about 8.5 miles south of the Delaware state line, and slightly west of a place referred to as “Waste Gate”. Waste Gate appears to be an informal name for an area around the intersection of Waste Gate Road and Route 350 that is in the vicinity of Waste Gate Creek. The well was drilled in 1944; core descriptions and electric logs were published by Anderson and others (1948). NATURE OF LOWER AND UPPER CONTACTS Hansen (1982) defined the Waste Gate Formation on the basis of significant differences in age, lithology and petrophysics from the overlying Patuxent Formation and Arundel Formations. In the type well, the top of the Waste Gate occurs at a depth of 4,745 feet. At this depth, the electric log shows a general increase in resistance associated with sandier intervals (Anderson, 1948, figs. 10 and 20), and an increase in garnet content (Anderson, 1948, fig. 3). Anderson (1948, p. 71) noted “the sands below the 4,750 foot level are all soft, partially consolidated, and poorly sorted and doubtless possess a relatively high permeability.” However, Anderson (1948) did not recognize the Waste Gate as a separate unit, instead including these sediments in the Patuxent Formation. The Waste Gate is characterized as an overlapped subsurface sequence of interbedded sandstones and shales; however, the nature of the upper contact of the Waste Gate Formation is not clearly defined. Various diagrams in Hansen (1984) seem to emphasize the undetermined nature of the contact by showing it as a questionable unconformity or possibly a conformable contact. Due largely to the paucity of data, it is not clear if significant time is missing at the contact or how the nature of the contact may vary at different locations. Hansen (1982, 1984) reported that palynology data indicate the sediments from the Waste Gate Formation are “pre-palynozone I of Brenner (1963),” largely, if not wholly, Berriasian to Hauterivian() in age, and thus older than the overlying Patuxent Formation (Berrimanian and younger). However, Hansen did note that, in one well, an angiosperm type common in the Palynozone I, associated with the younger (overlying) Patuxent-Arundel Formations (undivided), was reported in the upper part of an interval assigned to the Waste Gate, thus leaving open the possibility of upper beds of the Waste Gate possibly being as young as early Barremian. Therefore, it is possible that little or no time separates the Waste Gate from the overlying Patuxent Formation. In Maryland, the Waste Gate has been penetrated in only four wells (referred to as Hammond No. 1, Bethards No. 1, DOE Crisfield, and Esso No. 1), and even fewer penetrate into the underlying basement rocks. In general, in the vicinity of the Hammond No. 1 well, and to the east of this well, Cretaceous units are underlain by rocks of Jurassic() or Triassic() age (Anderson and others, 1948; Hansen, 1982). To the west, the Waste Gate Formation is presumably underlain by older, pre-Mesozoic basement metamorphic rocks. In the Hammond No. 1 well, there are approximately 135 feet of what are referred to as Triassic() rocks by Anderson and others (1948) and Jurassic() by Hansen (1982). The top of the sequence is a hard, indurated quartz conglomerate containing some white feldspars and lime cement. Below the conglomerate are hard, reddish-brown and apple-green shales, sandy shales, and sandstones. In the Bethards No. 1 well, there are approximately 585 feet of Triassic()/Jurassic() rocks (assigned to the Newark series) characterized by sandstones, sandy shales, and shales with a basal conglomerate (Anderson and others, 1948). Anderson and others (1948) indicate that, at the Hammond No. 1 well, the top of the pre-Mesozoic basement contact is characterized by “rotten schistose rock containing mica, chlorite, and feldspar and cut by small veins of pegmatite in which the feldspars are almost entirely decomposed.” This weathered zone was estimated to be approximately 31 feet thick and underlain by either a biotite-rich quartzite or a mica gneiss and cut by veins of pegmatite. At the Bethards No. 1 well, pre-Mesozoic basement rock appears to be characterized by dark greenish-black gabbros containing joints occasionally filled with carbonate). LITHOLOGY Hansen (1984) described the Waste Gate lithology as follows: The Waste Gate Formation consists largely of an unconsolidated to moderately lithified sequence of interbedded light gray to white arkosic to feldspathic sandstones and drab to occasionally mottled, silty shales (or clays), often fi nely laminated with carbonaceous material. Anderson (1948, p. 14) reports that the sandstones (sands) are relatively poorly sorted, ranging from fi ne to very coarse-grained with an occasional pebbly bed. The feldspars are often strongly kaolinized, resulting in a pervasive, clayey matrix suffi ciently binding to form friable sandstones in place. The more indurated sandstones are associated with occasional occurrences of calcareous cement. Core descriptions provided by Anderson and others (1948, p. 408-412) indicate that about 27 percent of the arenaceous footage is suffi ciently lithified to be called “sandstone,”
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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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APPENDIX A: UPPER CAMBRIAN ROSE RUN
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APPENDIX A: KNOX TO LOWER SILURIAN
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N T R APPENDIX A: KNOX TO LOWER SIL
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APPENDIX A: MIDDLE ORDOVICIAN ST. P
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-6000 -8000 APPENDIX A: MIDDLE ORDO
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Page 125 and 126: 25 APPENDIX A: LOWER/MIDDLE DEVONIA
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Page 137 and 138: APPENDIX A: PENNSYLVANIAN COAL BEDS
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