Until recently, the sedimentary processes on the United States Atlantic Continental Slope were inferred mainly from descriptive studies based on the bathymetry and on widely spaced grab samples, bottom photographs, and seismic-reflection profiles. Over the past 6 years, however, much additional information has been collected on the bottom morphology, characteristics of shallow-subbottom strata, velocity of bottom currents, and transport of suspended and bottom sediments. A review of these new data provides a much clearer understanding of the kinds and relative importance of gravitational and hydrodynamic processes that affect the surface sediments. On the rugged slope between Georges Bank and Cape Lookout, N.C., these processes include: (1) small scale mass wasting within submarine canyons and peripheral gullies; (2) density flows within some submarine valleys; (3) sand spillover near the shelf break; (4) sediment creep on the upper slope; and (5) hemipelagic sedimentation on the middle and lower slope. The area between Georges Bank and Hudson Canyon is further distinguished by the relative abundance of large-scale slump scars and deposits on the open slope, the presence of ice-rafted debris, and the transport of sand within the heads of some submarine canyons. Between Cape Lookout and southern Florida, the slope divides into two physiographic units, and the topography is smooth and featureless. On the Florida—Hatteras Slope, offshelf sand spillover and sediment winnowing, related to Gulf Stream flow and possibly to storm-driven currents, are the major processes, whereas hemipelagic sedimentation is dominant over the offshore slope along the seaward edge of the Blake Plateau north of the Blake Spur. Slumping generally is absent south of Cape Lookout, although one large slump scarp (related to uplift over salt diapirs) has been identified east of Cape Romain. Future studies concerning sedimentary processes on the Atlantic slope need to resolve: (1) the ages and mechanisms of mass wasting; (2) the accumulation rates and thicknesses of hemipelagic sediments; and (3) the causes and variability of offshelf sand spillover, sediment winnowing, and canyon transport.
","language":"English","publisher":"Elsevier","doi":"10.1016/0025-3227(84)90107-5","usgsCitation":"Knebel, H.J., 1984, Sedimentary processes on the Atlantic Continental Slope of the United States: Marine Geology, v. 61, no. 1, p. 43-74, https://doi.org/10.1016/0025-3227(84)90107-5.","productDescription":"32 p.","startPage":"43","endPage":"74","costCenters":[{"id":678,"text":"Woods Hole Coastal and Marine Science Center","active":true,"usgs":true}],"links":[{"id":219941,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"61","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505b8a32e4b08c986b3170a9","contributors":{"authors":[{"text":"Knebel, Harley J.","contributorId":25930,"corporation":false,"usgs":true,"family":"Knebel","given":"Harley","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":366826,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70199548,"text":"70199548 - 1984 - Offshore exploration and industry change: The case of the Gulf of Mexico","interactions":[],"lastModifiedDate":"2024-05-13T14:50:04.105169","indexId":"70199548","displayToPublicDate":"1984-09-01T15:19:19","publicationYear":"1984","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":5748,"text":"Journal of Petroleum Technology","active":true,"publicationSubtype":{"id":10}},"title":"Offshore exploration and industry change: The case of the Gulf of Mexico","docAbstract":"This paper considers industry structure and the exploration performance (by size class of operator) of firms searching for oil and gas in the U.S. Gulf of Mexico. It also tracks the changes in industry structure that have occurred in response to a decline in the quality of remaining prospects in the area. Data presented indicate that because vertically integrated majors dominated in exploration in the early years of the Gulf of Mexico exploration history, they were able to discover 86% of the total hydrocarbons discovered through 1975. However, the data also show a dynamic relationship between the structure of the industry operating in an area and the quality of remaining prospects. The relative share of both credited discoveries and wildcat wells of nonmajor operators has increased as exploration in the gulf proceeded. For example, in state-owned waters from 1951 to 1955, major inns accounted for 85% of all wildcat wells drilled, whereas from 1971 to 1975 these firms accounted for only 30% of the wildcat wells. During these same two periods in the federal Gulf of Mexico, the majors' share of wildcats fell from 98% to 70%.
","doi":"10.2118/11152-PA","usgsCitation":"Attanasi, E., and Drew, L.J., 1984, Offshore exploration and industry change: The case of the Gulf of Mexico: Journal of Petroleum Technology, v. 36, no. 3, p. 437-442, https://doi.org/10.2118/11152-PA.","productDescription":"6 p.","startPage":"437","endPage":"442","costCenters":[{"id":241,"text":"Eastern Energy Resources Science Center","active":true,"usgs":true}],"links":[{"id":357564,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"36","issue":"3","noUsgsAuthors":false,"publicationDate":"1984-03-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Attanasi, Emil D. 0000-0001-6845-7160 attanasi@usgs.gov","orcid":"https://orcid.org/0000-0001-6845-7160","contributorId":198728,"corporation":false,"usgs":true,"family":"Attanasi","given":"Emil D.","email":"attanasi@usgs.gov","affiliations":[{"id":241,"text":"Eastern Energy Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":745827,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Drew, L. J.","contributorId":118947,"corporation":false,"usgs":true,"family":"Drew","given":"L.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":745828,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70221677,"text":"70221677 - 1984 - Age of the Comfort Member of the Castle Hayne Formation, North Carolina","interactions":[],"lastModifiedDate":"2021-06-28T16:27:57.791133","indexId":"70221677","displayToPublicDate":"1984-09-01T11:20:43","publicationYear":"1984","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1723,"text":"GSA Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Age of the Comfort Member of the Castle Hayne Formation, North Carolina","docAbstract":"The biostratigraphic and chronostratigraphic position of the Comfort Member of the Castle Hayne Formation has been the subject of much debate. At the Martin-Marietta Quarry at Castle Hayne, New Hanover County, North Carolina, the planktic foraminifers indicate an assignment within an interval of the uppermost Turborotalia frontosa Zone to the Turborotalia pomeroli Zone. The calcareous nannofossils indicate an assignment to the middle part of the Chiasmolithus solitus Zone. The dinocyst data indicate placement in the upper part of the Kisselovia coleothrypta Zone of Costa and Downie. These zonal units are considered to be within the middle Eocene of international usage, and, on the basis of the time scale used in this paper, the Chiasmolithus solitus Zone represents a time interval of 42.1 to 45.4 megaannums (Ma). This differs significantly from a Rb/Sr glauconite date of 34.8 ± 1.0 Ma previously obtained at the same locality.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1984)95<1040:AOTCMO>2.0.CO;2","usgsCitation":"Hazel, J.E., Bybell, L.M., Edwards, L.E., Jones, G.D., and Ward, L.W., 1984, Age of the Comfort Member of the Castle Hayne Formation, North Carolina: GSA Bulletin, v. 95, no. 9-10, p. 1040-1044, https://doi.org/10.1130/0016-7606(1984)95<1040:AOTCMO>2.0.CO;2.","productDescription":"5 p.","startPage":"1040","endPage":"1044","costCenters":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true}],"links":[{"id":386803,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"North Carolina","county":"New Hanover County","city":"Castle Hayne","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -77.92791366577148,\n 34.33401010846338\n ],\n [\n -77.86688804626465,\n 34.33401010846338\n ],\n [\n -77.86688804626465,\n 34.38049178631383\n ],\n [\n -77.92791366577148,\n 34.38049178631383\n ],\n [\n -77.92791366577148,\n 34.33401010846338\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"95","issue":"9-10","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Hazel, J. E.","contributorId":89187,"corporation":false,"usgs":false,"family":"Hazel","given":"J.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":818409,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bybell, Laurel M. 0000-0002-4760-7542 lbybell@usgs.gov","orcid":"https://orcid.org/0000-0002-4760-7542","contributorId":1760,"corporation":false,"usgs":true,"family":"Bybell","given":"Laurel","email":"lbybell@usgs.gov","middleInitial":"M.","affiliations":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true}],"preferred":true,"id":818410,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Edwards, Lucy E. 0000-0003-4075-3317 leedward@usgs.gov","orcid":"https://orcid.org/0000-0003-4075-3317","contributorId":2647,"corporation":false,"usgs":true,"family":"Edwards","given":"Lucy","email":"leedward@usgs.gov","middleInitial":"E.","affiliations":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true},{"id":40020,"text":"Florence Bascom Geoscience Center","active":true,"usgs":true}],"preferred":true,"id":818411,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Jones, G. D.","contributorId":31971,"corporation":false,"usgs":false,"family":"Jones","given":"G.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":818412,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Ward, L. W.","contributorId":58704,"corporation":false,"usgs":true,"family":"Ward","given":"L.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":818413,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":70013809,"text":"70013809 - 1984 - Sinking of volcanic ash in uncompacted sediment in Williams Lake, Washington","interactions":[],"lastModifiedDate":"2025-11-17T16:53:03.564208","indexId":"70013809","displayToPublicDate":"1984-08-03T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3338,"text":"Science","active":true,"publicationSubtype":{"id":10}},"title":"Sinking of volcanic ash in uncompacted sediment in Williams Lake, Washington","docAbstract":"Volcanic ash from the eruption of Mount St. Helens on 18 May 1980 fell into Williams Lake in eastern Washington and was temporarily suspended at the sediment-water interface. After several months of compaction, the ash layer broke up and sank into lower density uncompacted lake sediment. Stratigraphic time displacements of several hundred years and a failure to recognize discontinuous ash layers in sediment cores are possible consequences of this process.","language":"English","publisher":"American Association for the Advancement of Science","doi":"10.1126/science.225.4661.505","issn":"00368075","usgsCitation":"Anderson, R., Nuhfer, E., and Dean, W., 1984, Sinking of volcanic ash in uncompacted sediment in Williams Lake, Washington: Science, v. 225, no. 4661, p. 505-508, https://doi.org/10.1126/science.225.4661.505.","productDescription":"4 p.","startPage":"505","endPage":"508","costCenters":[],"links":[{"id":220613,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Washington","otherGeospatial":"Williams Lake","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -117.71303740955221,\n 47.336647953925194\n ],\n [\n -117.71303740955221,\n 47.31700552527329\n ],\n [\n -117.66661224970237,\n 47.31700552527329\n ],\n [\n -117.66661224970237,\n 47.336647953925194\n ],\n [\n -117.71303740955221,\n 47.336647953925194\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"225","issue":"4661","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505b90e9e4b08c986b3196d2","contributors":{"authors":[{"text":"Anderson, R.Y.","contributorId":22789,"corporation":false,"usgs":true,"family":"Anderson","given":"R.Y.","email":"","affiliations":[],"preferred":false,"id":366908,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Nuhfer, E.B.","contributorId":89281,"corporation":false,"usgs":true,"family":"Nuhfer","given":"E.B.","email":"","affiliations":[],"preferred":false,"id":366909,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Dean, W.E.","contributorId":97099,"corporation":false,"usgs":true,"family":"Dean","given":"W.E.","email":"","affiliations":[],"preferred":false,"id":366910,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70014072,"text":"70014072 - 1984 - Shoreface translation and the Holocene stratigraphic record: Examples from Nova Scotia, the Mississippi Delta and eastern Australia","interactions":[],"lastModifiedDate":"2024-10-16T18:22:01.660768","indexId":"70014072","displayToPublicDate":"1984-08-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2667,"text":"Marine Geology","active":true,"publicationSubtype":{"id":10}},"title":"Shoreface translation and the Holocene stratigraphic record: Examples from Nova Scotia, the Mississippi Delta and eastern Australia","docAbstract":"Classic descriptive models of barrier sedimentation have been developed with data from the Atlantic and Gulf coasts of the United States. These models are dominated by low to moderate rates of relative sea level (RSL) rise and wave energy. Barriers respond by landward recycling of sediment through the mechanism of shoreface retreat. Sedimentation processes on the central coast of New South Wales (N.S.W.), Australia, consist of rapid RSL rise in early Holocene times followed by a stillstand since 6500 B.P. Wave energy is relatively high year-round and sand sources for barrier formation are only found on the inner shelf. Barrier sedimentation on the central coast of N.S.W. exhibits a thick, composite sequence composed of a basal marine transgressive sand overlain by regressive beach and dune facies.
The Louisiana coast surrounding the Mississippi delta is underlain by compacting deltaic muds which generate very rapid rates of RSL rise. The Louisiana coast experiences low wave energy punctuated by high-energy tropical and extra-tropical storm events. Barrier sediments accumulate from the erosion of deltaic headlands and undergo a transformation from subaerial barrier island systems to subaqueous shoals located on the inner shelf. Drumlins experience coastal erosion on the Eastern Shore of Nova Scotia and provide a sediment source for compartmented estuary mouth barriers. An ongoing, moderate rise of RSL results from the passage of a glacial forebulge. Wave energy is intermediate between Louisiana and N.S.W. and displays a seasonal pattern dominated by frequent winter storms. Coastal barrier sedimentation is episodic, consisting of a period of beach ridge progradation followed by barrier destruction and re-establishment further landward.
The three contrasting sedimentary sequences found in examples from Louisiana, N.S.W. and Nova Scotia indicate that presently available sedimentation models from locations such as the middle Atlantic or Texas coasts of the United States may only represent well-documented regional case studies. A true generalised coastal sedimentation model is required which can identify the parameters controlling vertical and horizontal translation of the depositional surface and provide relationships between these parameters which quantitatively predict the genesis, distribution and geometry of coastal sedimentary facies.
","language":"English","publisher":"Elsevier","doi":"10.1016/0025-3227(84)90159-2","usgsCitation":"Boyd, R., and Penland, S., 1984, Shoreface translation and the Holocene stratigraphic record: Examples from Nova Scotia, the Mississippi Delta and eastern Australia: Marine Geology, v. 60, no. 1-4, p. 391-412, https://doi.org/10.1016/0025-3227(84)90159-2.","productDescription":"22 p.","startPage":"391","endPage":"412","costCenters":[],"links":[{"id":225553,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"60","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505b8e8fe4b08c986b3189e7","contributors":{"authors":[{"text":"Boyd, Ron","contributorId":54737,"corporation":false,"usgs":false,"family":"Boyd","given":"Ron","email":"","affiliations":[],"preferred":false,"id":367495,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Penland, S.","contributorId":58778,"corporation":false,"usgs":true,"family":"Penland","given":"S.","email":"","affiliations":[],"preferred":false,"id":367496,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":5220768,"text":"5220768 - 1984 - Movements of translocated wolves in Minnesota","interactions":[],"lastModifiedDate":"2024-11-04T17:11:22.117423","indexId":"5220768","displayToPublicDate":"1984-07-02T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2508,"text":"Journal of Wildlife Management","active":true,"publicationSubtype":{"id":10}},"title":"Movements of translocated wolves in Minnesota","docAbstract":"From Feb. 1975-May 1978, 104 wolves (Canis lupus) captured at or near Minnesota farms where depredations on livestock had been reported were translocated northward and eastward for 50-317 km into extensive forests; 3 others were released westward. Nine wolves were translocated twice, and 1 three times. Information on movements was obtained by radiotracking 17 wolves and by recovery of 16 others. All radio-tagged wolves left the release areas; adults left quickly, but pups generally remained longer, behaved less decisively, and settled nearby temporarily. Wolves released together did not remain together. Initial travel of most radio-tagged adults was between south and west, the general direction to their original location. Final directions were primarily to the west and northwest, due in part to physiographic barriers. Eight adults homed, 1 twice, to capture areas that were < 64 km from release sites. Nonhoming wolves were radiotracked and/or recovered 32-351 km from their capture sites and 23-302 km from their release sites. Translocation was largely unsuccessful at keeping problem wolves out of lifestock production areas. The problem of initial travel away from release sites in wolf reintroductions probably could be minimized by transport and release of 6-9 mo. old wolves.
","language":"English","publisher":"Wiley","doi":"10.2307/3801418","usgsCitation":"Fritts, S., Paul, W., and Mech, L., 1984, Movements of translocated wolves in Minnesota: Journal of Wildlife Management, v. 48, no. 3, p. 709-721, https://doi.org/10.2307/3801418.","productDescription":"13 p.","startPage":"709","endPage":"721","costCenters":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":197771,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United 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\"}}]}","volume":"48","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b02e4b07f02db698bc5","contributors":{"authors":[{"text":"Fritts, Steven H.","contributorId":93975,"corporation":false,"usgs":true,"family":"Fritts","given":"Steven H.","affiliations":[],"preferred":false,"id":332435,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Paul, W.J.","contributorId":60579,"corporation":false,"usgs":false,"family":"Paul","given":"W.J.","email":"","affiliations":[],"preferred":false,"id":332436,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Mech, L.D. 0000-0003-3944-7769","orcid":"https://orcid.org/0000-0003-3944-7769","contributorId":75466,"corporation":false,"usgs":false,"family":"Mech","given":"L.D.","email":"","affiliations":[],"preferred":false,"id":332437,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70013742,"text":"70013742 - 1984 - The 1984 Morgan Hill, California, earthquake","interactions":[],"lastModifiedDate":"2025-11-17T16:57:27.209174","indexId":"70013742","displayToPublicDate":"1984-06-20T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3338,"text":"Science","active":true,"publicationSubtype":{"id":10}},"title":"The 1984 Morgan Hill, California, earthquake","docAbstract":"The Morgan Hill, California, earthquake (magnitude 6.1) of 24 April 1984 ruptured a 30-kilometer-long segment of the Calaveras fault zone to the east of San Jose. Although it was recognized in 1980 that an earthquake of magnitude 6 occurred on this segment in 1911 and that a repeat of this event might reasonably be expected, no short-term precursors were noted and so the time of the 1984 earthquake was not predicted. Unilateral rupture propagation toward the south-southeast and an energetic late source of seismic radiation located near the southeast end of the rupture zone contributed to the highly focused pattern of strong motion, including an exceptionally large horizontal acceleration of 1.29g at a site on a dam abutment near the southeast end of the rupture zone.","language":"English","publisher":"American Association for the Advancement of Science","doi":"10.1126/science.225.4659.288","issn":"00368075","usgsCitation":"Bakun, W.H., Clark, M.M., Cockerham, R., Ellsworth, W., Lindh, A., Prescott, W., Shakal, A., and Spudich, P., 1984, The 1984 Morgan Hill, California, earthquake: Science, v. 225, no. 4659, p. 288-291, https://doi.org/10.1126/science.225.4659.288.","productDescription":"4 p.","startPage":"288","endPage":"291","costCenters":[],"links":[{"id":220392,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","city":"Morgan Hill","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -121.67997194384967,\n 37.15785438793927\n ],\n [\n -121.67997194384967,\n 37.11621667214587\n ],\n [\n -121.62087504633425,\n 37.11621667214587\n ],\n [\n -121.62087504633425,\n 37.15785438793927\n ],\n [\n -121.67997194384967,\n 37.15785438793927\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"225","issue":"4659","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505ba62be4b08c986b320f2f","contributors":{"authors":[{"text":"Bakun, W. H.","contributorId":67055,"corporation":false,"usgs":true,"family":"Bakun","given":"W.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":366772,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Clark, M. M.","contributorId":41877,"corporation":false,"usgs":true,"family":"Clark","given":"M.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":366770,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Cockerham, R.S.","contributorId":21421,"corporation":false,"usgs":true,"family":"Cockerham","given":"R.S.","email":"","affiliations":[],"preferred":false,"id":366768,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Ellsworth, W.L.","contributorId":48541,"corporation":false,"usgs":true,"family":"Ellsworth","given":"W.L.","email":"","affiliations":[],"preferred":false,"id":366771,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Lindh, A.G.","contributorId":24784,"corporation":false,"usgs":true,"family":"Lindh","given":"A.G.","email":"","affiliations":[],"preferred":false,"id":366769,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Prescott, W.H.","contributorId":96337,"corporation":false,"usgs":true,"family":"Prescott","given":"W.H.","email":"","affiliations":[],"preferred":false,"id":366775,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Shakal, A.F.","contributorId":70156,"corporation":false,"usgs":true,"family":"Shakal","given":"A.F.","email":"","affiliations":[],"preferred":false,"id":366773,"contributorType":{"id":1,"text":"Authors"},"rank":7},{"text":"Spudich, P.","contributorId":85700,"corporation":false,"usgs":true,"family":"Spudich","given":"P.","affiliations":[],"preferred":false,"id":366774,"contributorType":{"id":1,"text":"Authors"},"rank":8}]}} ,{"id":70175808,"text":"70175808 - 1984 - Areal lithologic changes in bedrock aquifers in southeastern Minnesota as determined from natural-gamma borehole logs methods","interactions":[],"lastModifiedDate":"2018-04-02T12:16:32","indexId":"70175808","displayToPublicDate":"1984-06-12T11:45:00","publicationYear":"1984","noYear":false,"publicationType":{"id":24,"text":"Conference Paper"},"publicationSubtype":{"id":19,"text":"Conference Paper"},"title":"Areal lithologic changes in bedrock aquifers in southeastern Minnesota as determined from natural-gamma borehole logs methods","docAbstract":"Sedimentary rocks of Paleozoic age in the Hollandale embayment in southeastern Minnesota are as much as 2,000 feet thick and, with the underlying Hinckley sandstone of Proterozoic age, comprise the following five layered aquifers (beginning with the oldest): the Mount Simon-Hinckley, Ironton-Galesville, Prairie du Chien-Jordan, St. Peter and Upper Carbonate. Many of the Paleozoic formations show transitional facies changes from a deep marine depositional environment in the middle of the embayment to a near shore environment along the periphery. Borehole natural-gamma logs were collected to investigate the effects of regional lithologic changes on the hydrology of the Ironton-Galesville, Prairie du Chien-Jordan and St. Peter aquifers.
\nInterpretation of natural-gamma logs shows that a fine-grained sandstone at the base of the Galesville sandstone (basal part of the Ironton-Galesville aquifer) thickens toward the central part of the embayment, which may account for the decrease in hydraulic conductivity of the Ironton-Galesville aquifer in that direction.
\nThe Jordan sandstone, which underlies the Prairie du Chien Group, consists of three members in southeastern Minnesota: the basal Norwalk member, a silty, fine-grained sandstone; the middle Van Oser member, a coarse- to medium-grained quartzose sandstone; and the upper Sunset Point member, a clayey dolomitic sandstone. The Norwalk and Van Oser members were identified by interpretation of natural-gamma logs. Hydraulic conductivity of the Prairie du Chien-Jordan aquifer generally is highest in the Twin City basin (50 feet per day) where the Van Oser is the predominant member; it is lowest to the east and southeast (25 feet per day) where the Norwalk member thickens.
\nInterpretation of natural-gamma logs indicates that the shaley and silty sandstones that comprise the basal St. Peter confining bed, which separates the St. Peter and Prairie du Chien aquifers, are as much as 80 feet thick in the Twin City basin, but are absent in the southern part of the embayment. Differences in potentiometric head across the basal St. Peter are about 30 feet in the Twin City basin where the confining bed is present but only 5 to 10 feet to the south where the confining bed is absent and where the St. Peter aquifer directly overlies the Prairie du Chien-Jordan aquifer.
","conferenceTitle":"Conference on Surface and Borehole Geophysical Investigations","conferenceDate":"February 7-9, 1984","conferenceLocation":"San Antonio, Texas","language":"English","publisher":"National Water Well Association/Environmental Protection Agency","usgsCitation":"Woodward, D.G., 1984, Areal lithologic changes in bedrock aquifers in southeastern Minnesota as determined from natural-gamma borehole logs methods, Conference on Surface and Borehole Geophysical Investigations, San Antonio, Texas, February 7-9, 1984, p. 788-800.","productDescription":"13 p.","startPage":"788","endPage":"800","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science Center","active":true,"usgs":true}],"links":[{"id":326935,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Minnesota","otherGeospatial":"Twin Cities Metropolitan Area","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-93.5093,45.4163],[-93.1289,45.4153],[-93.0186,45.4131],[-93.0188,45.2984],[-92.7894,45.297],[-92.7439,45.2963],[-92.7516,45.2935],[-92.7551,45.2927],[-92.7583,45.2904],[-92.7597,45.2872],[-92.7604,45.2845],[-92.7591,45.2794],[-92.7559,45.2739],[-92.7527,45.2694],[-92.7515,45.2657],[-92.7526,45.2626],[-92.7535,45.2584],[-92.7561,45.2541],[-92.7575,45.2502],[-92.7569,45.2443],[-92.7557,45.2397],[-92.7553,45.2356],[-92.7538,45.2305],[-92.7536,45.2276],[-92.7521,45.2236],[-92.752,45.2196],[-92.7527,45.2168],[-92.7546,45.2136],[-92.7573,45.2107],[-92.7603,45.2065],[-92.7619,45.2041],[-92.7632,45.2009],[-92.7637,45.1972],[-92.764,45.1895],[-92.7629,45.1853],[-92.7557,45.178],[-92.7522,45.1759],[-92.7493,45.173],[-92.748,45.1698],[-92.7472,45.1634],[-92.7483,45.1597],[-92.7475,45.1551],[-92.7473,45.1515],[-92.7484,45.1483],[-92.749,45.1419],[-92.7484,45.1373],[-92.7441,45.1264],[-92.7415,45.1172],[-92.7422,45.1135],[-92.7446,45.11],[-92.7467,45.1076],[-92.7513,45.1045],[-92.7591,45.0999],[-92.7624,45.0972],[-92.7803,45.0849],[-92.7847,45.083],[-92.7885,45.0806],[-92.7917,45.0791],[-92.795,45.0772],[-92.7982,45.0746],[-92.8001,45.0723],[-92.8019,45.0647],[-92.8016,45.0597],[-92.8005,45.0567],[-92.7984,45.0531],[-92.7952,45.0499],[-92.7926,45.0481],[-92.7881,45.0453],[-92.7837,45.0421],[-92.7745,45.0373],[-92.7707,45.0344],[-92.7683,45.0325],[-92.7645,45.0265],[-92.7639,45.0237],[-92.7639,45.0196],[-92.7682,45.0005],[-92.7694,44.9909],[-92.7686,44.9796],[-92.7646,44.9711],[-92.7547,44.9571],[-92.7527,44.9527],[-92.7523,44.9481],[-92.753,44.9369],[-92.7534,44.9237],[-92.7547,44.9159],[-92.7569,44.9105],[-92.7606,44.9068],[-92.7645,44.9046],[-92.767,44.9039],[-92.7707,44.9023],[-92.7729,44.901],[-92.775,44.8982],[-92.7738,44.8933],[-92.7689,44.8848],[-92.7632,44.8759],[-92.7628,44.8716],[-92.763,44.8671],[-92.7644,44.8622],[-92.7682,44.8554],[-92.7683,44.853],[-92.7671,44.8494],[-92.7652,44.8462],[-92.7646,44.8423],[-92.7644,44.8382],[-92.766,44.8308],[-92.7679,44.8265],[-92.7719,44.8211],[-92.7751,44.8161],[-92.7784,44.8125],[-92.7801,44.8095],[-92.781,44.8056],[-92.7823,44.8029],[-92.783,44.7966],[-92.7858,44.7893],[-92.7909,44.7842],[-92.7993,44.7765],[-92.802,44.7729],[-92.8046,44.7683],[-92.8059,44.7624],[-92.8073,44.7524],[-92.8061,44.7483],[-92.8054,44.7473],[-92.8022,44.7446],[-92.7901,44.7381],[-92.7805,44.7344],[-92.7722,44.7317],[-92.7658,44.7289],[-92.7569,44.7234],[-92.7536,44.7226],[-92.7471,44.7204],[-92.7415,44.7192],[-92.7339,44.7157],[-92.737,44.658],[-92.7386,44.6329],[-92.7957,44.6305],[-92.7915,44.5452],[-92.9165,44.5449],[-92.9179,44.5221],[-92.9218,44.518],[-92.9282,44.5158],[-92.9321,44.513],[-92.941,44.5149],[-92.9449,44.5131],[-92.9494,44.5104],[-92.9584,44.514],[-92.9634,44.5177],[-92.975,44.5159],[-92.9827,44.5173],[-92.991,44.5215],[-93.0057,44.5197],[-93.0121,44.5175],[-93.0166,44.5166],[-93.0275,44.5198],[-93.0301,44.5148],[-93.0346,44.5148],[-93.039,44.5171],[-93.0406,44.4729],[-93.2826,44.473],[-93.2798,44.546],[-93.5259,44.5466],[-93.9091,44.5446],[-93.9117,44.5492],[-93.9078,44.5528],[-93.9027,44.5524],[-93.9008,44.5492],[-93.8956,44.5483],[-93.8937,44.5515],[-93.8963,44.5561],[-93.9008,44.5606],[-93.8996,44.5647],[-93.8957,44.5675],[-93.8958,44.5711],[-93.8996,44.5743],[-93.8958,44.5775],[-93.8939,44.5807],[-93.8959,44.5871],[-93.8991,44.5903],[-93.8908,44.5962],[-93.8857,44.5967],[-93.8838,44.6012],[-93.878,44.6013],[-93.878,44.6077],[-93.8716,44.6063],[-93.8658,44.6063],[-93.8569,44.6168],[-93.8563,44.6218],[-93.8505,44.6219],[-93.8447,44.6201],[-93.8422,44.6233],[-93.8358,44.6242],[-93.8319,44.6251],[-93.8217,44.6297],[-93.8031,44.6366],[-93.7999,44.6361],[-93.7967,44.6343],[-93.7935,44.6311],[-93.7883,44.632],[-93.78,44.6362],[-93.7768,44.6385],[-93.7729,44.6366],[-93.7723,44.6325],[-93.7691,44.6312],[-93.7665,44.6362],[-93.7685,44.6417],[-93.7686,44.675],[-93.8887,44.6756],[-93.8902,44.7185],[-94.0104,44.719],[-94.0085,44.8947],[-94.0136,44.8951],[-94.0117,44.9796],[-93.7692,44.9789],[-93.7702,45.0734],[-93.7663,45.077],[-93.7631,45.0839],[-93.7534,45.0853],[-93.7399,45.0894],[-93.7341,45.0922],[-93.7322,45.0963],[-93.7257,45.1022],[-93.7225,45.11],[-93.72,45.1205],[-93.7155,45.1269],[-93.7019,45.1374],[-93.6852,45.1489],[-93.6793,45.1525],[-93.6716,45.1562],[-93.6574,45.1585],[-93.6554,45.1599],[-93.6529,45.1631],[-93.6503,45.169],[-93.6516,45.1841],[-93.6549,45.1905],[-93.6555,45.1969],[-93.6562,45.201],[-93.6471,45.2079],[-93.6387,45.2074],[-93.6361,45.206],[-93.6329,45.2056],[-93.6258,45.2092],[-93.6167,45.2115],[-93.6096,45.2111],[-93.6031,45.2111],[-93.5967,45.2134],[-93.5857,45.2189],[-93.5792,45.2189],[-93.5734,45.2202],[-93.5676,45.2225],[-93.5617,45.2289],[-93.554,45.2298],[-93.5462,45.2289],[-93.5371,45.2294],[-93.5332,45.2317],[-93.5197,45.2417],[-93.5158,45.2458],[-93.5138,45.2454],[-93.5093,45.4163]]]},\"properties\":{\"name\":\"Anoka\",\"state\":\"MN\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"57b82daee4b03fd6b7da3618","contributors":{"authors":[{"text":"Woodward, D. G.","contributorId":106458,"corporation":false,"usgs":true,"family":"Woodward","given":"D.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":646387,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70013307,"text":"70013307 - 1984 - Discovery of two new large submarine canyons in the Bering Sea","interactions":[],"lastModifiedDate":"2024-10-16T17:01:52.772728","indexId":"70013307","displayToPublicDate":"1984-04-02T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2667,"text":"Marine Geology","active":true,"publicationSubtype":{"id":10}},"title":"Discovery of two new large submarine canyons in the Bering Sea","docAbstract":"The Beringian continental margin is incised by some of the world's largest submarine canyons. Two newly discovered canyons, St. Matthew and Middle, are hereby added to the roster of Bering Sea canyons. Although these canyons are smaller and not cut back into the Bering shelf like the five very large canyons, they are nonetheless comparable in size to most of the canyons that have been cut into the U.S. eastern continental margin and much larger than the well-known southern California canyons. Both igneous and sedimentary rocks of Eocene to Pliocene age have been dredged from the walls of St. Matthew and Middle Canyons as well as from the walls of several of the other Beringian margin canyons, thus suggesting a late Tertiary to Quaternary genesis of the canyons. We speculate that the ancestral Yukon and possibly Anadyr Rivers were instrumental in initiating the canyon-cutting processes, but that, due to restrictions imposed by island and subsea bedrock barriers, cutting of the two newly discovered canyons may have begun later and been slower than for the other five canyons.
","language":"English","publisher":"Elsevier","doi":"10.1016/0025-3227(84)90011-2","usgsCitation":"Carlson, P.R., and Karl, H.A., 1984, Discovery of two new large submarine canyons in the Bering Sea: Marine Geology, v. 56, no. 1-4, p. 159-179, https://doi.org/10.1016/0025-3227(84)90011-2.","productDescription":"21 p.","startPage":"159","endPage":"179","costCenters":[],"links":[{"id":220365,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Russia, United States","otherGeospatial":"Bering Sea","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -175.70567061914593,\n 64.7045344412486\n ],\n [\n -175.70567061914593,\n 60.36782445864782\n ],\n [\n -166.4061387257148,\n 60.36782445864782\n ],\n [\n -166.4061387257148,\n 64.7045344412486\n ],\n [\n -175.70567061914593,\n 64.7045344412486\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"56","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a01f3e4b0c8380cd4fdec","contributors":{"authors":[{"text":"Carlson, Paul R.","contributorId":81469,"corporation":false,"usgs":true,"family":"Carlson","given":"Paul","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":365776,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Karl, Herman A.","contributorId":80649,"corporation":false,"usgs":true,"family":"Karl","given":"Herman","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":365775,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70208969,"text":"70208969 - 1984 - Recent studies indicate that major structures in northeastern Nevada and the Golconda thrust in north-central Nevada are of Jurassic or Cretaceous age","interactions":[],"lastModifiedDate":"2020-03-09T14:16:46","indexId":"70208969","displayToPublicDate":"1984-03-09T14:08:51","publicationYear":"1984","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1796,"text":"Geology","active":true,"publicationSubtype":{"id":10}},"title":"Recent studies indicate that major structures in northeastern Nevada and the Golconda thrust in north-central Nevada are of Jurassic or Cretaceous age","docAbstract":"Geologic mapping recently completed in four areas of northeastern Nevada indicates that major folds and thrusts are of post-Early Triassic age and probably are Jurassic or Cretaceous. Previously published data for northeastern Nevada lead to, or permit, the same conclusion. Basinal deposits of Early Triassic age in the northern Adobe Range are easterly derived clay and carbonate. The apparent lack of westerly derived siliceous orogenic sediments of Sonoma age (Late Permian to Early Triassic) suggests that the Sonoma orogeny took place at some unknown location far from northeastern Nevada and that rocks deformed then, the Golconda allochthon, were emplaced in northern Nevada at a later date.
","language":"English","publisher":"GSA","doi":"10.1130/0091-7613(1984)12<483:RSITMS>2.0.CO;2","usgsCitation":"Ketner, K.B., 1984, Recent studies indicate that major structures in northeastern Nevada and the Golconda thrust in north-central Nevada are of Jurassic or Cretaceous age: Geology, v. 12, no. 8, p. 483-486, https://doi.org/10.1130/0091-7613(1984)12<483:RSITMS>2.0.CO;2.","productDescription":"4 p.","startPage":"483","endPage":"486","costCenters":[],"links":[{"id":373023,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Nevada","otherGeospatial":"Northeastern Nevada","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -116.38916015624999,\n 39.87601941962116\n ],\n [\n -114.06005859375,\n 39.87601941962116\n ],\n [\n -114.06005859375,\n 41.983994270935625\n ],\n [\n -116.38916015624999,\n 41.983994270935625\n ],\n [\n -116.38916015624999,\n 39.87601941962116\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"12","issue":"8","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Ketner, Keith B.","contributorId":957,"corporation":false,"usgs":true,"family":"Ketner","given":"Keith","email":"","middleInitial":"B.","affiliations":[],"preferred":true,"id":784228,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70209998,"text":"70209998 - 1984 - A seismic refraction survey of the Imperial Valley Region, California","interactions":[],"lastModifiedDate":"2020-05-08T14:33:17.65006","indexId":"70209998","displayToPublicDate":"1984-02-10T09:24:57","publicationYear":"1984","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2314,"text":"Journal of Geophysical Research B: Solid Earth","active":true,"publicationSubtype":{"id":10}},"title":"A seismic refraction survey of the Imperial Valley Region, California","docAbstract":"The U.S. Geological Survey conducted an extensive seismic refraction survey in the Imperial Valley region of California in 1979. The Imperial Valley is located in the Salton Trough, an active rift between the Pacific and North American plates. Forty shots fired at seven shot points were recorded by 100 portable seismic instruments at typical spacing of 0.5–1 km. More than 1300 recording locations were occupied, and more than 3000 usable seismograms were obtained. We analyzed five profiles using a standard ray‐tracing program, constructed a contour map of reduced travel times from our most widely recorded shot point, and modeled an existing gravity profile across the Salton Trough. Results are itemized: (1) All models have in common a sedimentary layer (Vp = 1.8–5.0 km/s), a “transition zone” (Vp = 5.0–5.65 km/s), a basement (Vp = 5.65 km/s in the Imperial Valley, 5.9 km/s on the bordering mesas), and subbasement (Vp = 7.2 km/s). (2) The sedimentary layer ranges in thickness along the axis of the Salton Trough from 3.7 km (Salton Sea) to 4.8 km (U.S.‐Mexican border). On the bordering mesas it is quite variable in thickness. (3) The “transition” zone is about 1 km thick in most places. In the Imperial Valley there are no marked velocity discontinuities in this zone between the sedimentary layer and basement. On the bordering mesas, however, there is a discontinuity at the top of this zone. (4) There are apparently two types of basement. On the bordering mesas, basement is crystalline igneous and metamorphic rocks. In the Imperial Valley, basement is mostly lower‐greenshist‐facies sedimentary rocks, based primarily on the smooth transition in character from sediment to basement arrivals, the low value of basement velocity, and the fact that deep (4 km) wells in the valley penetrate only the upper part of the known Cenozoic stratigraphic column for the Salton Trough. (5) The subbasement, or intermediate crustal layer, ranges in depth along the axis of the Salton Trough from 16 km (Salton Sea) to 10 km (U.S.‐Mexican border). Gravity modeling requires that this layer deepen and/or pinch out beneath the bordering mesas and mountain ranges. Based on its high velocity and the presence of intrusive basaltic rocks in the sedimentary section in the Imperial Valley, the subbasement is thought to be a mafic intrusive complex similar to oceanic middle crust. (6) Several structures are seen that affect basement, transition zone, and deeper parts of the sedimentary layer. They include a scarp along the Imperial fault, as much as 1 km down to the northeast, and a scarp passing roughly along the topographic boundary between the Imperial Valley and the bordering mesa to the west, as much as 3½ km down to the east. We interpret the latter scarp to be the suture, or rift boundary, between the older crystalline basement on the mesa and the younger metasedimentary basement in the Imperial Valley. (7) On a contour map of reduced travel time from our most widely recorded shot point, subtle patches of early arrivals among otherwise late arrivals in the central Imperial Valley correlate well with known geothermal resource areas having reservoir temperatures of more than 150°C. Apparently the Salton Trough is a location where new crust is being generated. As the rift opens, mafic intrusive rocks fill it from below as sedimentary rocks fill it from above. Rifting and intrusion produce high heat flow that metamorphoses the sedimentary rocks to shallow depth (metasedimentary basement in the Imperial Valley) and thus consolidates the new crust.
Red fox (Vulpes vulpes) predation on nesting ducks was assessed by examining 1,857 adult duck remains found at 1,432 fox rearing dens from 1968 to 1973. Dabbling ducks were much more vulnerable to foxes than diving ducks. Dabbling ducks (1,798) found at dens consisted of 27% blue-winged teals (Anas discors), 23% mallards (A. platyrhynchos), 20% northern pintails (A. acuta), 9% northern shovelers (Spatula clypeata), 8% gadwalls (A. strepera), 3% green-winged teals (A. crecca), 2% American wigeons (A. americana), and 10% unidentified. Relative abundance of individual species and nesting chronology were the most important factors affecting composition of ducks taken by foxes. Seventy-six percent of 1,376 adult dabbling ducks and 40% of 30 adult diving ducks for which sex was determined were hens. In western North Dakota and western South Dakota, 65% of mallard and northern pintail remains found at dens were hens compared with 76% in eastern North Dakota and eastern South Dakota (P < 0.05). Percentage hens varied among the 5 most common dabbling ducks found at dens. In eastern North Dakota and eastern South Dakota, where predation on ducks was greatest, an average of 64% of gadwall, 73% of northern pintail, 81% of blue-winged teal, 81% of mallard, and 90% of northern shoveler remains found at dens were hens. Percentage hens among duck remains found at dens increased as the duck nesting season progressed.
\nNumbers of adult ducks found at individual dens ranged from 0 to 67. The average number of ducks found in and around den entrances was used as an index of fox predation rates on ducks. Predation rate indices ranged from 0.01 duck/den in Iowa to 1.80 ducks/den in eastern North Dakota. Average annual predation rate indices for dabbling ducks in a 3-county intensive study area in eastern North Dakota were closely correlated with May pond numbers (r = 0.874, P < 0.10) and duck population size (r = 0.930, P < 0.05), but all species were not affected in the same manner or to the same degree. Drought had least effect on populations and predation rate indices of mallards and gadwalls and had greatest effect on those of northern pintails and northern shovelers. Hens of early nesting species were more vulnerable to foxes than hens of late nesting species. Predation rate indices were expanded to estimate total numbers of ducks taken by fox families during the denning season. Estimated numbers of dabbling ducks taken annually by individual fox families in 2 physiographic regions comprising the intensive study area ranged from 16.1 to 65.9. Predation was highest during wet years and lowest during dry years and averaged lower, but was more variable, in the region where tillage was greatest and wetland water levels were least stable. Predation in the intensive study area averaged 2.97 adult dabbling ducks/ km2/year and represented an estimated average annual loss of 13.5% of hen and 4.5% of drake populations in that area. Of 5,402 individual food items found at dens in the intensive study area, 24% were adult ducks. Ducks made up an estimated maximum average of 16% of the prey biomass required by fox families during the denning season.
\nThe average annual take of adult ducks by foxes in the midcontinent area was estimated to be about 900,000. This estimate included both scavenged and fox-killed ducks, as well as ducks taken after the denning season. Fox impact on midcontinent ducks was greatest in eastern North Dakota where both fox and duck densities were relatively high. Predation in that area was likely increased by environmental factors, especially intensive agriculture that concentrated nesting and reduced prey abundance.
\nPredation by red foxes and other predators severely reduces duck production in the midcontinent area. Effective management to increase waterfowl production will necessitate coping with or reducing high levels of predation.
","language":"English","publisher":"The Wildlife Society","usgsCitation":"Sargeant, A.B., Allen, S.H., and Eberhardt, R.T., 1984, Red fox predation on breeding ducks in midcontinent North America: Wildlife Monograph 89, 41 p.","productDescription":"41 p.","startPage":"1","endPage":"41","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":480,"text":"Northern Prairie Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":199278,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Canada, United States","state":"Iowa, Manitoba, Minnesota, Nebraska, North Dakota, South Dakota, Wisconsin","county":"Barnes County, Kidder County, Stutsman County","otherGeospatial":"Prairie Pothole Region","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -100.1513671875,\n 50.54136296522161\n ],\n [\n -101.513671875,\n 50.51342652633956\n ],\n [\n -101.42578124999999,\n 49.03786794532644\n ],\n [\n -104.19433593749999,\n 48.951366470947725\n ],\n [\n -104.0625,\n 41.0130657870063\n ],\n [\n -91.14257812499999,\n 41.409775832009565\n ],\n [\n -90.3955078125,\n 42.35854391749705\n ],\n [\n -92.8125,\n 48.516604348867475\n ],\n [\n -93.603515625,\n 48.545705491847464\n ],\n [\n -94.5703125,\n 48.66194284607008\n ],\n [\n -95.361328125,\n 48.951366470947725\n ],\n [\n -100.1513671875,\n 50.54136296522161\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a60e4b07f02db635370","contributors":{"authors":[{"text":"Sargeant, Alan B.","contributorId":89185,"corporation":false,"usgs":true,"family":"Sargeant","given":"Alan","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":326506,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Allen, Stephen H.","contributorId":46620,"corporation":false,"usgs":true,"family":"Allen","given":"Stephen","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":326507,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Eberhardt, Robert T.","contributorId":156332,"corporation":false,"usgs":false,"family":"Eberhardt","given":"Robert","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":326508,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70013604,"text":"70013604 - 1984 - Modification of wave-cut and faulting-controlled landforms","interactions":[],"lastModifiedDate":"2024-06-27T16:24:22.78454","indexId":"70013604","displayToPublicDate":"1984-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":6453,"text":"Journal of Geophysical Research Solid Earth","active":true,"publicationSubtype":{"id":10}},"title":"Modification of wave-cut and faulting-controlled landforms","docAbstract":"From a casual observation that the form of degraded fault scarps resembles the error function, this investigation proceeds through an elementary diffusion equation representation of landform evolution to the application of the resulting equations to the modern topography of scarplike landforms. The morphologic observations can be analyzed either in the form of one or more cross-strike elevation profiles or in the form of the slope-offset plot, a point plot of maximum scarp slope versus scarp offset. Working with either or both of these data representations for nine geologic structures, which range in age from 3 to 400 ka B.P. and in offset from 1 to 50 m, we apply analytical solutions for the vertical initial value scarp, the vertical continuous offset scarp, and the finite slope, initial value scarp. The model calculations are intrinsically ambiguous, yielding as the final answer only the product κt (in the case of the initial value problem) or the product κA−1 (in the case of the repeated faulting problem); here t is the age of a single scarp-forming event, 2A is the vertical slip rate, and κ is the “mass diffusivity.” A single profile across three sea cliffs along the Santa Cruz, California, coast is analyzed as three separate initial value problems. A reasonably constrained age for the sea cliff standing above the Highway 1 platform returns κ = 11 GKG (1 GKG = 1 m2/ka). With this κ, we can date the two older sea cliffs. In fact, we do the converse: age estimates for these two older sea cliffs based on a uniform rate of uplift both yield the same κ as for the lower sea cliff. We treat a single profile of the Raymond fault in Pasadena/San Marino in terms of the repeated faulting problem; for it the uplift rate of R. Crook and others yields κ = 16 GKG. The very substantial preexisting offset across the Raymond fault must have been buried/leveled some 230 ka B.P., when the modern topography began to form. Our analysis of the Lake Bonneville shoreline scarps reveals a dependence of κt on 2a, suggestive of nonlinear modification processes. This appearance is treated with the finite slope initial value scarp model to determine κ=1.1 GKG for the Lake Bonneville shoreline scarps. The suggestion of M. N. Machette that approximately 100,000-year-old, meter-high scarps are “unobservable” in weakly consolidated alluvial terranes of the Basin and Range and Rio Grande Rift Valley provinces can be formulated as κ ≳ 1 GKG. The coincidence between this inequality and the Lake Bonneville shoreline κ is striking, and it suggests that the value of κ = 1 GKG may be generally applicable, as a good first approximation, to the modification of alluvial terranes within the semiarid regions of the western United States. The Lake Bonneville shoreline κ is the basis for dating four sets of fault scarps in west-central Utah. The Drum Mountains fault scarps can be modeled in several different circumstances, but the most likely interpretation is that these fault scarps formed as the result of a single episode of normal faulting 3.6 to 5.7 ka B.P. The younger age is associated with quite low initial slope angles (25°). The other three sets of fault scarps show no evidence for finite initial value slopes. Fault scarps along the eastern base of the Fish Springs Range are very young, 3 ka B.P. We estimate the age of fault scarps along the western flank of the Oquirrh Mountains to be 32 ka B.P., which meets the weak geologic constraint that they be older than the Lake Bonneville shoreline. Fault scarps along the northeastern margin of the Sheeprock Mountains are even older, 53 ka B.P. An intriguing consequence of our single-event analysis of these scarps is that an 11.5-m offset occurred in a single earthquake.
","language":"English","publisher":"American Geophysical Union","doi":"10.1029/JB089iB07p05771","issn":"01480227","usgsCitation":"Hanks, T.C., Bucknam, R., Lajoie, K.R., and Wallace, R.E., 1984, Modification of wave-cut and faulting-controlled landforms: Journal of Geophysical Research Solid Earth, v. 89, no. B7, p. 5771-5790, https://doi.org/10.1029/JB089iB07p05771.","productDescription":"20 p.","startPage":"5771","endPage":"5790","numberOfPages":"20","costCenters":[],"links":[{"id":219865,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"89","issue":"B7","noUsgsAuthors":false,"publicationDate":"2012-09-20","publicationStatus":"PW","scienceBaseUri":"505a5cb4e4b0c8380cd6feb9","contributors":{"authors":[{"text":"Hanks, Thomas C.","contributorId":35763,"corporation":false,"usgs":true,"family":"Hanks","given":"Thomas","middleInitial":"C.","affiliations":[],"preferred":false,"id":366464,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bucknam, R.C.","contributorId":35744,"corporation":false,"usgs":true,"family":"Bucknam","given":"R.C.","affiliations":[],"preferred":false,"id":366463,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Lajoie, K. R.","contributorId":6828,"corporation":false,"usgs":true,"family":"Lajoie","given":"K.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":366462,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Wallace, R. E.","contributorId":6823,"corporation":false,"usgs":true,"family":"Wallace","given":"R.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":366461,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":1003917,"text":"1003917 - 1984 - Avian cholera in Nebraska's Rainwater Basin","interactions":[],"lastModifiedDate":"2022-08-17T16:38:37.373948","indexId":"1003917","displayToPublicDate":"1984-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3638,"text":"Transactions of the North American Wildlife and Natural Resources Conference","active":true,"publicationSubtype":{"id":10}},"title":"Avian cholera in Nebraska's Rainwater Basin","docAbstract":"The first report of avian cholera in North America occurred in northwestern Texas in winter 1944 (Quortrup et al. 1946). In 1975, mortality from avian cholera occurred for the first time in waterfowl in the Rainwater Basin of Nebraska when an estimated 25,000 birds died (Zinkl et al. 1977). Avian cholera has continued to cause mortality in wild birds in specific areas of the Basin each spring since. Losses of waterfowl from avian cholera continue to be much greater in some of the wetlands in the western part of the Basin than in the east. Several wetlands in the west have consistently higher mortality and are most often the wetlands where initial mortality is noticed each spring (Figure 1). The establishment of this disease in Nebraska is of considerable concern because of the importance of the Rainwater Basin as a spring staging area for waterfowl migrating to their breeding grounds. The wetlands in this area are on a major migration route used by an estimated 5 to 9 million ducks and several hundred thousand geese. A large portion of the western mid-continental greater white-fronted goose (Anser albifrons) population stage in the Basin each spring. Occasionally, whooping cranes (Grus americana) use these wetlands during migration, and lesser sandhill cranes (Grus canadensis) staging on the nearby Platte River sometimes use wetlands where avian cholera occurs (Anonymous 1981). Our objectives were to determine whether certain water quality variables in the Rainwater Basin differed between areas of high and low avian cholera incidence. These results would then be used for laboratory studies involving the survivability of Pasteurella multocida, the causative bacterium of avian cholera. Those studies will be reported elsewhere.
","language":"English","publisher":"Wildlife Management Institute","usgsCitation":"Windingstad, R.M., Hurt, J.J., Trout, A.K., and Cary, J., 1984, Avian cholera in Nebraska's Rainwater Basin: Transactions of the North American Wildlife and Natural Resources Conference, v. 49, p. 576-583.","productDescription":"8 p.","startPage":"576","endPage":"583","numberOfPages":"8","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":456,"text":"National Wildlife Health Center","active":true,"usgs":true}],"links":[{"id":135845,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United 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The first was on October 4 in northern Chile. the second occurred in the United States in the State of Idaho on October 28. This was the first major earthquake in the conterminous United States since a magnitude 7.2 event occurred near the coast of northern California on November 8, 1980, and was the first earthquake to cause fatalities in the conterminous United States since February 9, 1971. The most deadly earthquake occurred in eastern Turkey on October 30.
","language":"English","publisher":"U.S Geological Survey","usgsCitation":"Person, W., 1984, Earthquakes; September-October 1983: Earthquake Information Bulletin (USGS), v. 16, no. 3, p. 148-151.","productDescription":"4 p.","startPage":"148","endPage":"151","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":318596,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"16","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"56dabfd8e4b015c306f84c77","contributors":{"authors":[{"text":"Person, W. J.","contributorId":91472,"corporation":false,"usgs":true,"family":"Person","given":"W. J.","affiliations":[],"preferred":false,"id":621979,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":8913,"text":"ofr84454 - 1984 - Statistical summaries of streamflow data in Oregon; Volume 1, eastern Oregon","interactions":[],"lastModifiedDate":"2023-05-03T21:17:30.451514","indexId":"ofr84454","displayToPublicDate":"1984-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"84-454","title":"Statistical summaries of streamflow data in Oregon; Volume 1, eastern Oregon","docAbstract":"Statistical summaries of streamflow data at 335 streamgaging sites are presented in this two volume report to aid in appraising the hydrology of river basins in Oregon. Records for 31 gaging stations were compiled into separate periods owing to changes in regulation during the period of data collection. The periods before and after regulation are presented for comparison. A brief station description is given describing the physical and operational features for each gaging station. Following the station description are tables of monthly and annual flow statistics, flood frequency data, low-flow and high-flow frequency data, and flow-duration information. (USGS)","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr84454","usgsCitation":"Friday, J., and Miller, S.J., 1984, Statistical summaries of streamflow data in Oregon; Volume 1, eastern Oregon: U.S. Geological Survey Open-File Report 84-454, Report: iii, 150 p.; 1 Plate: 21.96 x 21.76 inches, https://doi.org/10.3133/ofr84454.","productDescription":"Report: iii, 150 p.; 1 Plate: 21.96 x 21.76 inches","costCenters":[{"id":518,"text":"Oregon Water Science Center","active":true,"usgs":true}],"links":[{"id":416685,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_13414.htm","linkFileType":{"id":5,"text":"html"}},{"id":36519,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1984/0454/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":36520,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1984/0454/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":141611,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1984/0454/report-thumb.jpg"}],"country":"United States","state":"Oregon","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -116.62552231910621,\n 46.08638618051495\n ],\n [\n -123,\n 46.08638618051495\n ],\n [\n -123,\n 41.97364185360769\n ],\n [\n -116.62552231910621,\n 41.97364185360769\n ],\n [\n -116.62552231910621,\n 46.08638618051495\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49dce4b07f02db5e19f9","contributors":{"authors":[{"text":"Friday, John","contributorId":19160,"corporation":false,"usgs":true,"family":"Friday","given":"John","email":"","affiliations":[],"preferred":false,"id":158535,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Miller, S. J.","contributorId":54198,"corporation":false,"usgs":true,"family":"Miller","given":"S.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":158536,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":20922,"text":"ofr83170E - 1984 - Geomorphic domains and linear features on Landsat images, Circle quadrangle, Alaska","interactions":[],"lastModifiedDate":"2023-08-24T20:19:08.896426","indexId":"ofr83170E","displayToPublicDate":"1984-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"83-170","chapter":"E","title":"Geomorphic domains and linear features on Landsat images, Circle quadrangle, Alaska","docAbstract":"A remote sensing study using Landsat images was undertaken as part of the Alaska Mineral Resource Assessment Program (AMRAP). Geomorphic domains A and B, identified on enhanced Landsat images, divide Circle quadrangle south of Tintina fault zone into two regional areas having major differences in surface characteristics. Domain A is a roughly rectangular, northeast-trending area of relatively low relief and simple, widely spaced drainages, except where igneous rocks are exposed. In contrast, domain B, which bounds two sides of domain A, is more intricately dissected showing abrupt changes in slope and relatively high relief. The northwestern part of geomorphic domain A includes a previously mapped tectonostratigraphic terrane. The southeastern boundary of domain A occurs entirely within the adjoining tectonostratigraphic terrane. The sharp geomorphic contrast along the southeastern boundary of domain A and the existence of known faults along this boundary suggest that the southeastern part of domain A may be a subdivision of the adjoining terrane. Detailed field studies would be necessary to determine the characteristics of the subdivision. \r\n\r\nDomain B appears to be divisible into large areas of different geomorphic terrains by east-northeast-trending curvilinear lines drawn on Landsat images. Segments of two of these lines correlate with parts of boundaries of mapped tectonostratigraphic terranes. On Landsat images prominent north-trending lineaments together with the curvilinear lines form a large-scale regional pattern that is transected by mapped north-northeast-trending high-angle faults. The lineaments indicate possible lithlogic variations and/or structural boundaries. \r\n\r\nA statistical strike-frequency analysis of the linear features data for Circle quadrangle shows that northeast-trending linear features predominate throughout, and that most northwest-trending linear features are found south of Tintina fault zone. A major trend interval of N.64-72E. in the linear feature data, corresponds to the strike of foliations in metamorphic rocks and magnetic anomalies reflecting compositional variations suggesting that most linear features in the southern part of the quadrangle probably are related to lithologic variations brought about by folding and foliation of metamorphic rocks. A second important trend interval, N.14-35E., may be related to thrusting south of the Tintina fault zone, as high concentrations of linear features within this interval are found in areas of mapped thrusts. Low concentrations of linear features are found in areas of most igneous intrusives. High concentrations of linear features do not correspond to areas of mineralization in any consistent or significant way that would allow concentration patterns to be easily used as an aid in locating areas of mineralization. \r\n\r\nThe results of this remote sensing study indicate that there are several possibly important areas where further detailed studies are warranted.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr83170E","usgsCitation":"Simpson, S.L., 1984, Geomorphic domains and linear features on Landsat images, Circle quadrangle, Alaska: U.S. Geological Survey Open-File Report 83-170, Report: iii, 31 p.; 1 Plate: 37.23 x 22.84 inches, https://doi.org/10.3133/ofr83170E.","productDescription":"Report: iii, 31 p.; 1 Plate: 37.23 x 22.84 inches","costCenters":[],"links":[{"id":50512,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1983/0170e/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":50513,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1983/0170e/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":153918,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1983/0170e/report-thumb.jpg"},{"id":420135,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_13921.htm","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Alaska","otherGeospatial":"Circle quadrangle","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -147,\n 66\n ],\n [\n -147,\n 65\n ],\n [\n -144,\n 65\n ],\n [\n -144,\n 66\n ],\n [\n -147,\n 66\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c553","contributors":{"authors":[{"text":"Simpson, S. L.","contributorId":46508,"corporation":false,"usgs":true,"family":"Simpson","given":"S.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":183505,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":6516,"text":"pp1151E - 1984 - Lithostratigraphy of Upper Ordovician strata exposed in Kentucky, with a section on biostratigraphy","interactions":[],"lastModifiedDate":"2023-11-27T20:15:18.328772","indexId":"pp1151E","displayToPublicDate":"1984-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"1151","chapter":"E","title":"Lithostratigraphy of Upper Ordovician strata exposed in Kentucky, with a section on biostratigraphy","docAbstract":"Ordovician formations above the Lexington Limestone crop out in the Blue Grass region of Kentucky and along the Cumberland River and its tributaries. The formations are all conformable and in places intertongue and intergrade.
The major Ordovician units above the Lexington Limestone in the Blue Grass region are: The Clays Ferry Formation, the Kope Formation, the Garrard Siltstone, the Fairview Formation, the Calloway Creek Limestone, the Grant Lake Limestone, the Ashlock Formation, the Bull Fork Formation, and the Drakes Formation. The Clays Ferry Formation is made up of subequal amounts of fossiliferous limestone and shale and minor siltstone; the Clays Ferry is as much as 300 ft thick and intertongues with the Lexington Limestone and the Kope Formation. The Kope Formation resembles the partly equivalent Clays Ferry but has a higher shale content (60-80 percent) and thicker layers of shale; the Kope, as much as 275 ft thick, is mostly restricted to the northern part of the State. The Garrard Siltstone, which consists of very calcitic siltstone and minor shale, overlies the Clays Ferry Formation in the southeastern part of the Blue Grass region; the Garrard, as much as 100 ft thick, feathers out into the upper part of the Clays Ferry in southern central and northern east-central Kentucky.
The Fairview Formation is characterized by even-bedded limestone interlayered with nearly equal amounts of shale and minor siltstone. The Fairview crops out in the northern part of the Blue Grass region, where it generally overlies the Kope Formation or the Garrard Siltstone; it grades southward into the Calloway Creek Limestone. The Calloway Creek contains more limestone (generally at least 70 percent) and is more irregularly and thinner bedded than the Fairview.
The Grant Lake Limestone is composed of nodular-bedded limestone (70-90 percent), interlayered and intermixed with shale; it overlies the Fairview Formation in the northern part of the Blue Grass region and the Calloway Creek Limestone in the western and central parts. In east-central Kentucky, the Grant Lake is classified as a member of the Ashlock Formation, an assemblage of lithologically distinct units that were combined to facilitate mapping in the southeastern and southern part of the region. The Ashlock consists of the following members, in ascending order: The Tate (calcitic and dolomitic mudstone), the Grant Lake, the Gilbert (micrograined limestone and shale), the Stingy Creek (nodular-bedded mudstone and limestone), the Terrill (dolomitic and calcitic mudstone), the Sunset (micrograined limestone), and the Reba (nodular-bedded limestone and shale).
The Bull Fork Formation, which overlies the Grant Lake Limestone, is made up of subequal amounts of thin-bedded highly fossiliferous limestone and shale; limestone makes up about 80 percent of the basal part of the formation and decreases in abundance irregularly upward to only 20 percent of the top part. On the east side of the Blue Grass region, the Bull Fork grades into the Reba Member of the Ashlock Formation; on the west side, it grades into the Grant Lake.
The uppermost formation in the region is the Drakes Formation, which in east-central Kentucky consists of the Rowland Member (calcitic to dolomitic mudstone) overlain by the Preachersville Member (dolomitic to calcitic mudstone and dolomite and dolomitic siltstone). In northeast Kentucky, the Drakes is represented by only the Preachersville Member. In most of central and north-central Kentucky, the formation consists of three members: the Rowland at the base (dolomitic mudstone to muddy limestone), the Bardstown (fossiliferous limestone and shale), and the Saluda Dolomite (dolomite, in part calcitic and muddy). In northern north-central Kentucky, the Drakes is represented by only the Saluda Dolomite Member.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/pp1151E","usgsCitation":"Weir, G.W., Peterson, W.L., Swadley, W.C., and Pojeta, J., 1984, Lithostratigraphy of Upper Ordovician strata exposed in Kentucky, with a section on biostratigraphy: U.S. Geological Survey Professional Paper 1151, v, 121 p.; 7 Plates: 37.00 x 21.00 inches or smaller, https://doi.org/10.3133/pp1151E.","productDescription":"v, 121 p.; 7 Plates: 37.00 x 21.00 inches or smaller","costCenters":[],"links":[{"id":104561,"rank":10,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4738.htm","linkFileType":{"id":5,"text":"html"},"description":"4738"},{"id":33985,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1151e/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":33984,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1151e/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":33983,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1151e/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":33982,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1151e/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":33989,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/1151e/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":33988,"rank":9,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1151e/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":33987,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1151e/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":33986,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1151e/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":121559,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/1151e/report-thumb.jpg"}],"country":"United States","state":"Kentucky","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -83.333,\n 39.1\n ],\n [\n -86,\n 39.1\n ],\n [\n -86,\n 36.61568653049616\n ],\n [\n -83.333,\n 36.61568653049616\n ],\n [\n -83.333,\n 39.1\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a61e4b07f02db635f33","contributors":{"authors":[{"text":"Weir, Gordon Whitney","contributorId":59790,"corporation":false,"usgs":true,"family":"Weir","given":"Gordon","email":"","middleInitial":"Whitney","affiliations":[],"preferred":false,"id":152854,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Peterson, Warren Lee","contributorId":68303,"corporation":false,"usgs":true,"family":"Peterson","given":"Warren","email":"","middleInitial":"Lee","affiliations":[],"preferred":false,"id":152855,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Swadley, W. C.","contributorId":46940,"corporation":false,"usgs":true,"family":"Swadley","given":"W.","middleInitial":"C.","affiliations":[],"preferred":false,"id":152853,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Pojeta, John Jr.","contributorId":44514,"corporation":false,"usgs":true,"family":"Pojeta","given":"John","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":888718,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":10136,"text":"ofr83930 - 1984 - Preliminary map showing the difference between the potentiometric surfaces of the Aquia aquifer of April 1979 and September 1982 in southern Maryland","interactions":[],"lastModifiedDate":"2023-05-05T21:47:19.916652","indexId":"ofr83930","displayToPublicDate":"1984-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"83-930","title":"Preliminary map showing the difference between the potentiometric surfaces of the Aquia aquifer of April 1979 and September 1982 in southern Maryland","docAbstract":"A map was prepared that shows the net change in the potentiometric surface of the Aquia aquifer in southern Maryland between April 1979 and September 1983. During this period, the potentiometric surface declined (1) at least a few feet throughout the entire southern Maryland area, and (2) more than 10 feet in the eastern Charles County area and in a few scattered localized areas. The network of observation wells was part of the cooperative program between the U.S. Geological Survey, the Maryland Geological Survey, and the Maryland Energy Administration.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr83930","usgsCitation":"Mack, F.K., Wheeler, J.C., and Curtin, S.E., 1984, Preliminary map showing the difference between the potentiometric surfaces of the Aquia aquifer of April 1979 and September 1982 in southern Maryland: U.S. Geological Survey Open-File Report 83-930, 1 p., https://doi.org/10.3133/ofr83930.","productDescription":"1 p.","costCenters":[],"links":[{"id":37986,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1983/0930/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":143617,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1983/0930/report-thumb.jpg"},{"id":416791,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_14281.htm","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Maryland","otherGeospatial":"Aquia aquifer","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -77,\n 39.2\n ],\n [\n -77,\n 38\n ],\n [\n -76,\n 38\n ],\n [\n -76,\n 39.2\n ],\n [\n -77,\n 39.2\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aafe4b07f02db66cf12","contributors":{"authors":[{"text":"Mack, F. K.","contributorId":93471,"corporation":false,"usgs":true,"family":"Mack","given":"F.","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":160875,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wheeler, J. C.","contributorId":66225,"corporation":false,"usgs":true,"family":"Wheeler","given":"J.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":160874,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Curtin, S. E.","contributorId":17235,"corporation":false,"usgs":true,"family":"Curtin","given":"S.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":160873,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":44047,"text":"ofr84235 - 1984 - Water-table contour map of the carbonate rocks of eastern Chester County, Pennsylvania, October 1983","interactions":[],"lastModifiedDate":"2023-04-05T21:33:36.423201","indexId":"ofr84235","displayToPublicDate":"1984-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"84-235","title":"Water-table contour map of the carbonate rocks of eastern Chester County, Pennsylvania, October 1983","docAbstract":"No abstract available
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr84235","usgsCitation":"Sloto, R.A., 1984, Water-table contour map of the carbonate rocks of eastern Chester County, Pennsylvania, October 1983: U.S. Geological Survey Open-File Report 84-235, 1 Plate: 30.00 x 21.00 inches, https://doi.org/10.3133/ofr84235.","productDescription":"1 Plate: 30.00 x 21.00 inches","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":172358,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":415305,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_13322.htm","linkFileType":{"id":5,"text":"html"}},{"id":20993,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1984/0235/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Pennsylvania","county":"Chester County","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -75.4,\n 40.083\n ],\n [\n -75.597,\n 40.083\n ],\n [\n -75.597,\n 40.031\n ],\n [\n -75.4,\n 40.031\n ],\n [\n -75.4,\n 40.083\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e2e4b07f02db5e4d14","contributors":{"authors":[{"text":"Sloto, Ronald A. rasloto@usgs.gov","contributorId":424,"corporation":false,"usgs":true,"family":"Sloto","given":"Ronald","email":"rasloto@usgs.gov","middleInitial":"A.","affiliations":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"preferred":true,"id":229052,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":21188,"text":"ofr84101 - 1984 - Geochemical assessment of mineral resources in the Goshute Canyon Survey Area (NV 040-015), east-central Nevada","interactions":[],"lastModifiedDate":"2023-03-23T19:35:16.979417","indexId":"ofr84101","displayToPublicDate":"1984-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"84-101","title":"Geochemical assessment of mineral resources in the Goshute Canyon Survey Area (NV 040-015), east-central Nevada","docAbstract":"No abstract available.
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\"}}]}","volume":"284","issue":"9","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a48a9e4b0c8380cd6801d","contributors":{"authors":[{"text":"Hatch, Norman L. 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Despite significant compositional variation within lavas forming the Honolulu Volcanics, these lavas are isotopically (Sr, Nd, Pb) very similar which contrasts with the isotopic heterogeneity of the Koolau tholeiites. Among Hawaiian tholeiitic suites, the Koolau lavas are geochemically distinct because of their lower iron contents and Sr and Nd isotopic ratios which range to bulk earth values. These geochemical data preclude simple models such as derivation of the Honolulu Volcanics and Koolau tholeiites from a common source by different degrees of melting or by mixing of two geochemically distinct sources. There may be no genetic relationship between the origin and evolution of these two lava suites; however, the trend shown by Koolau Range lavas of increasing 143Nd/144Nd and decreasing 87Sr/86Sr with decreasing eruption age and increasing alkalinity also occurs at Haleakala, East Molokai and Kauai volcanoes. A complex mixing model proposed for Haleakala lavas can account for the variations in Sr and Nd isotopic ratios and incompatible element abundances found in lavas from the Koolau Range. This model may reflect mixing and melting processes occurring during ascent of relatively enriched mantle through relatively depleted MORB-related lithosphere. Although two isotopically distinct components may be sufficient to explain Sr and Nd isotopic variations at individual Hawaiian volcanoes, more than two isotopically distinct materials are required to explain variations of Sr, Nd and Pb isotopic ratios in all Hawaiian lavas.
Black shales of Devonian age in the Appalachian Basin are a unique rock sequence. The high content of organic matter, which imparts the characteristic lithology, has for years attracted considerable interest in the shales as a possible source of energy. The recent energy shortage prompted the U.S. Department of Energy through the Eastern Gas Shales Project of the Morgantown Energy Technology Center to underwrite a research program to determine the geologic, geochemical, and structural characteristics of the Devonian black shales in order to enhance the recovery of gas from the shales. Geologic studies by Federal and State agencies and academic institutions produced a regional stratigraphic network that correlates the 15 ft black shale sequence in Tennessee with 3000 ft of interbedded black and gray shales in central New York. These studies correlate the classic Devonian black shale sequence in New York with the Ohio Shale of Ohio and Kentucky and the Chattanooga Shale of Tennessee and southwestern Virginia. Biostratigraphic and lithostratigraphic markers in conjunction with gamma-ray logs facilitated long-range correlations within the Appalachian Basin. Basinwide correlations, including the subsurface rocks, provided a basis for determining the areal distribution and thickness of the important black shale units. The organic carbon content of the dark shales generally increases from east to west across the basin and is sufficient to qualify as a hydrocarbon source rock. Significant structural features that involve the black shale and their hydrocarbon potential are the Rome trough, Kentucky River and Irvine-Paint Creek fault zone, and regional decollements and ramp zones.
","language":"English","publisher":"Elsevier","doi":"10.1016/0146-6380(84)90011-1","usgsCitation":"Roen, J.B., 1984, Geology of the Devonian black shales of the Appalachian Basin: Organic Geochemistry, v. 5, no. 4, p. 241-254, https://doi.org/10.1016/0146-6380(84)90011-1.","productDescription":"14 p.","startPage":"241","endPage":"254","costCenters":[],"links":[{"id":225802,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Kentucky, Maryland, New York, Ohio, Pennsylvania, Tennessee, Virginia, West Virginia","otherGeospatial":"Appalachian Basin","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"MultiPolygon\",\"coordinates\":[[[[-89.5391,36.498201],[-89.55264,36.577178],[-89.493495,36.4787],[-89.236542,36.566824],[-89.041263,37.202881],[-88.476127,37.068223],[-88.482612,37.354915],[-88.109417,37.472369],[-88.125033,37.707094],[-87.940069,37.88767],[-87.672397,37.829127],[-87.380247,37.935596],[-87.14195,37.816176],[-86.794985,37.988982],[-86.604624,37.858272],[-86.431749,38.126121],[-86.271802,38.137874],[-86.048458,37.959369],[-85.823764,38.280569],[-85.425787,38.52873],[-85.456978,38.689135],[-84.835672,38.784289],[-84.806082,41.696089],[-83.504334,41.731547],[-82.513827,41.384257],[-81.768898,41.491663],[-79.148723,42.553672],[-78.868556,42.770258],[-79.061388,43.251349],[-78.370221,43.376505],[-76.952174,43.270692],[-76.235834,43.529256],[-76.133697,43.940356],[-76.360306,44.070907],[-76.312647,44.199044],[-75.26825,44.855119],[-74.868663,45.001274],[-73.343124,45.01084],[-73.430325,43.590532],[-73.247631,43.51924],[-73.276421,42.746019],[-73.508142,42.086257],[-73.482709,41.21276],[-73.727775,41.100696],[-73.782577,40.837601],[-72.635374,40.990536],[-72.245348,41.161217],[-72.273657,41.051533],[-72.116368,40.999796],[-71.869558,41.075046],[-73.145266,40.645491],[-73.934512,40.545175],[-74.013784,40.756601],[-73.896479,40.981697],[-74.694914,41.357423],[-74.838366,41.277286],[-75.135526,40.973807],[-75.19872,40.705298],[-75.061489,40.422848],[-74.733804,40.174509],[-75.140006,39.888465],[-75.662822,39.82115],[-75.788395,39.700287],[-75.693521,38.460128],[-75.053483,38.451274],[-75.87767,37.135604],[-76.023664,37.268971],[-75.712065,37.936082],[-75.846621,37.925785],[-75.938577,38.272329],[-76.188644,38.267434],[-76.320843,38.459862],[-76.190902,38.621092],[-76.308922,38.813346],[-76.205063,38.892726],[-76.333703,38.984607],[-76.168332,38.996546],[-76.27566,39.160304],[-75.986298,39.510398],[-76.497977,39.204697],[-76.438845,39.0529],[-76.559697,38.767443],[-76.329433,38.073986],[-77.040638,38.444618],[-77.256412,38.396755],[-77.175969,38.604113],[-77.26443,38.582845],[-77.286202,38.347025],[-77.024866,38.386791],[-76.910832,38.197073],[-76.265998,37.91138],[-76.339892,37.655966],[-76.722156,37.83668],[-76.252415,37.447274],[-76.475927,37.250543],[-76.300352,37.00885],[-76.780532,37.209336],[-76.482407,36.917364],[-76.058154,36.916947],[-75.867044,36.550754],[-81.680137,36.585518],[-81.718282,36.350388],[-82.02664,36.130222],[-82.325169,36.119363],[-82.531292,35.972188],[-82.701065,36.034404],[-82.955751,35.809802],[-83.880074,35.518745],[-84.052612,35.269982],[-84.28252,35.227877],[-84.321869,34.988408],[-90.309297,34.995694],[-90.09061,35.118287],[-90.166594,35.274588],[-89.992975,35.560774],[-89.923161,35.514428],[-89.915491,35.754917],[-89.68182,35.88999],[-89.699677,36.230821],[-89.534507,36.261802],[-89.5391,36.498201]],[[-77.038598,38.791513],[-77.002498,38.96541],[-77.0915,38.95651],[-77.038598,38.791513]]],[[[-74.144428,40.53516],[-74.219787,40.502603],[-74.120186,40.642201],[-74.144428,40.53516]]]]},\"properties\":{\"name\":\"Kentucky\",\"nation\":\"USA \"}}]}","volume":"5","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a256fe4b0c8380cd588db","contributors":{"authors":[{"text":"Roen, John B.","contributorId":14425,"corporation":false,"usgs":true,"family":"Roen","given":"John","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":367086,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ]}