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GeoRef Categories
Era and Period
Epoch and Age
Book Series
Date
Availability
Greendale Syncline
Implications of Gentle Ordovician Folding in Western Virginia Available to Purchase
Exploration Strategy for Unconventional Natural Gas Resource—Devonian Shales: ABSTRACT Free
—Data for comparison purposes plotted on conventional base map of central A... Available to Purchase
Upper Devonian Black Shales Across Appalachian Basin: ABSTRACT Free
Oil and Gas Exploration in Appalachian Overthrust Belt of Southwestern Virginia: ABSTRACT Free
Exploration Concepts in Deformed Belt of Appalachians Available to Purchase
Wildcat Valley Sandstone in Southwest Virginia—Possible Reservoir Sandstone Available to Purchase
Mississippian Gas Sands of Central Michigan Area Available to Purchase
Palinspastic Maps of Central Appalachians Available to Purchase
Lithostratigraphy of the Early Mississippian Grainger Formation and related strata in northeastern Tennessee Available to Purchase
ABSTRACT Data from 33 locations were utilized in a stratigraphic study of the Early Mississippian Grainger Formation and related units in northeast Tennessee. Isopach maps, stratigraphic cross sections, and lithologic trends indicate the Grainger Formation was deposited in four deltaic lobes: Monroe, Rock Haven, Hancock, and Grainger-Borden. Each is in a separate outcrop belt: Chilhowie Mountain, Clinch Mountain, Newman Ridge, and Cumberland Mountain. The Monroe lobe is the eastern and southernmost of the lobes. Within it, the Grainger Formation is thicker and coarser than in the other locales. It is underlain by gray and black shale; the gray shale is a probable nearshore gray version of the usually greenish Maury Formation. The Greasy Cove Formation, a heterogeneous unit of sandstone, shale, red beds, and limestone, overlies the Grainger Formation and occupies the stratigraphic position of the Maccrady Formation and Newman Limestone in outcrop belts to the northwest. The Greasy Cove Formation is recognized only in the Monroe lobe. In the Rock Haven lobe, both the Grainger Formation and Chattanooga Shale are divisible into mappable members. The Chattanooga Shale consists of an upper Big Stone Gap Member, a middle Brallier Member, and a lower Millboro Member. The Chattanooga Shale locally is 600+ m thick. The Grainger Formation in the Rock Haven lobe is divisible into three newly named members: an upper Hayters Sandstone member, a middle Greendale member, and a basal Bean Station member. The Alumwell glauconite zone, within the upper part of the Greendale member, is also new. The center of the zone approximates a time line and is a key stratigraphic horizon. All Grainger members and the Alumwell glauconite are traceable into the Price Formation of southwest Virginia. In the Rock Haven lobe, the Chattanooga Shale, Grainger Formation, and Maccrady Formation were deposited in a subsiding trough; subsidence began in the Givetian and perhaps in the Eifelian, caused by a migrating peripheral bulge generated by Neoacadian deformation in the Carolina Piedmont. Highlands created by the deformation were the eastern sediment source for the Chattanooga, Grainger, and Maccrady formations in this lobe. Sediment for the Hancock and Grainger-Borden lobes originated from northerly sources. In the Hancock lobe, the Chattanooga Shale and Grainger Formation are thinner, and the Grainger Formation has increased shale content to the south. Paleocurrent data indicate a north-south current flow. The Hancock lobe is likely a southern extension of the Price delta system in southwest Virginia. The Grainger-Borden lobe is the southern terminus of the Borden delta system of Kentucky. Both the Chattanooga Shale and Grainger Formation thin to the south and southeast. The Floyds Knob glauconite bed was deposited during a pause in sediment delivery and separates the Fort Payne Chert from the underlying Grainger Formation as a distinct sedimentary unit. The Fort Payne Chert overlaps the Grainger Formation from a deeper southern basin where the dolostone and chert have little or no interbedded shale. The overlap does not interfinger with the Grainger Formation. The Fort Payne Chert becomes thinner as it progresses northward, finally passing into the Muldraugh Formation in Kentucky. It also made a minor incursion eastward into the western margin of the Hancock lobe, where some chert(y) beds occur at the Maccrady position.
Early Palaeozoic magmatism in the English Lake District Available to Purchase
National Seismic Hazard Model for New Zealand: 2010 Update Available to Purchase
Tyrone-Mt. Union Cross-Strike Lineament of Pennsylvania: A Major Paleozoic Basement Fracture and Uplift Boundary Available to Purchase
Oil and Gas Developments in Mid-Eastern States in 1984 Available to Purchase
Oil and Gas Developments in Mid-Eastern States in 1983 Available to Purchase
Oil and Gas Developments in Maryland, Ohio, Pennsylvania, Virginia, and West Virginia Available to Purchase
Oil and Gas Developments in Mid-Eastern States in 1982 Available to Purchase
The Caradoc volcanoes of the English Lake District Available to Purchase
Tectonic significance of Late Ordovician silicic magmatism, Avalon terrane, northern Antigonish Highlands, Nova Scotia 1 This article is one of a series of papers published in CJES Special Issue: In honour of Ward Neale on the theme of Appalachian and Grenvillian geology. 2 Contribution to International Geological Correlation Programme (IGCP) Project 497. Available to Purchase
Sequence Response of a Distal-To-Proximal Foreland Ramp to Glacio-Eustasy and Tectonics: Mississippian, Appalachian Basin, West Virginia-Virginia, U.S.A. Available to Purchase
Abstract This paper evaluates the limits of using well-cuttings data and wireline logs in conjunction with limited core and outcrop data to generate a regional, high-resolution sequence stratigraphy for upper Mississippian (Chesterian) Greenbrier carbonates, West Virginia, U.S.A. These data are then used to document the stratigraphic response of the distal to proximal foreland basin to tectonics and Carboniferous glacio-eustasy during the transition into ice-house times. The major mappable sequences are fourth-order sequences, a few meters to over a hundred meters thick. They consist of updip red beds and eolianites, lagoonal muddy carbonates, ooid grainstone and skeletal grainstone-packstone shoal complexes, open-ramp skeletal wackestone, and slope-basinal laminated argillaceous carbonates. The sequences are bounded downdip by lowstand sandstones and calcareous siltstones, and locally on the ramp by basal transgressive shales; only a few sequence boundaries are calichified, compared with updip sections in Kentucky, where caliche and breccias are common. Transgressive systems tracts range from thin units to others that constitute the lower half of the sequence. The highstand systems tracts contain significant grainstone units. Maximum flooding surfaces on the ramp slope occur at the base of slope or basinal facies that rest on lowstand to transgressive complexes, whereas on the ramp they occur beneath widespread grainstones that overlie nearshore shale or lime mudstone. In the Greenbrier succession, fourth-order sequences are arranged into weak third-order composite sequences bounded updip by red beds, and by lowstand sands and oolite along the ramp slope. The composite sequences contain three to four fourth-order sequences. Correlation of the foreland basin units with third-order global sea-level curves, and with high-frequency sequences within the intracratonic Illinois Basin, shows that in spite of differential subsidence rates ranging from 2 to 30 cm/ky across the foreland, global third-and fourth-order sea-level changes whose amplitude increased with time were a strong influence on sequence development. Thrust-load-induced differential subsidence of fault blocks of the foreland basement controlled the rapid basinward thickening of the depositional wedge, and modified the eustatic effects on the accumulating succession. Moderate-amplitude eustatic sea-level change and semiarid climate were the dominant causes of the widespread reservoirs of ooid grainstone and lowstand sands. The overall stratigraphy suggests upward increase in amplitudes of sea-level change, and cooling, which likely records the initiation of Gondwana ice-sheet growth.