{"pageNumber":"291","pageRowStart":"7250","pageSize":"25","recordCount":10961,"records":[{"id":26814,"text":"wri954154 - 1996 - Technique for estimating magnitude and frequency of peak flows in Maryland","interactions":[],"lastModifiedDate":"2012-02-02T00:08:32","indexId":"wri954154","displayToPublicDate":"1996-09-01T00:00:00","publicationYear":"1996","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"95-4154","title":"Technique for estimating magnitude and frequency of peak flows in Maryland","docAbstract":"Methods are presented for estimating peak-flow magnitudes of selected frequencies for drainage basins in Maryland. The methods were developed by generalized least-squares regression techniques using data from 219 streamflow-gaging stations in and near Maryland, and apply to peak flows with recurrence intervals of 2, 5, 10, 25, 50, 100, and 500 years. The State is divided into five hydrologic regions: the Appalachian Plateaus and Allegheny Ridges region, the Blue Ridge and Great Valley region, the Piedmont region, the Western Coastal Plain region, and the Eastern Coastal Plain region. Sets of equations for calculating peak discharges based on physical basin characteristics and their associated standard errors of prediction are provided for each of the five hydrologic regions. Basin characteristics and flood-frequency characteristics are tabulated for 236 streamflow- gaging stations in Maryland and surrounding States. Methods of estimating peak flows at sites in Maryland for ungaged and gaged sites are presented.","language":"ENGLISH","publisher":"U.S. Geological Survey ;\r\nEarth Science Information Center, Open-File Reports Section [distributor],","doi":"10.3133/wri954154","usgsCitation":"Dillow, J., 1996, Technique for estimating magnitude and frequency of peak flows in Maryland: U.S. Geological Survey Water-Resources Investigations Report 95-4154, iv, 55 p. with errata : ill., maps ; 28 cm., https://doi.org/10.3133/wri954154.","productDescription":"iv, 55 p. with errata : ill., maps ; 28 cm.","costCenters":[],"links":[{"id":158402,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":2097,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri954154/","linkFileType":{"id":5,"text":"html"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adce4b07f02db6861bb","contributors":{"authors":[{"text":"Dillow, Jonathan J.A.","contributorId":18412,"corporation":false,"usgs":true,"family":"Dillow","given":"Jonathan J.A.","affiliations":[],"preferred":false,"id":197052,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":29969,"text":"wri954167 - 1996 - Discharge, water-quality characteristics, and nutrient loads from McKay Bay, Delaney Creek, and East Bay, Tampa, Florida, 1991-1993","interactions":[],"lastModifiedDate":"2012-02-02T00:09:02","indexId":"wri954167","displayToPublicDate":"1996-09-01T00:00:00","publicationYear":"1996","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"95-4167","title":"Discharge, water-quality characteristics, and nutrient loads from McKay Bay, Delaney Creek, and East Bay, Tampa, Florida, 1991-1993","docAbstract":"Nutrient enrichment in Tampa Bay has caused a decline in water quality in the estuary. Efforts to reduce the nutrient loading to Tampa Bay have resulted in improvement in water quality from 1981 to 1991. However, Tampa Bay still is onsidered enriched with nutrients. Water quality in East Bay (located at the northeastern part of Hillsborough Bay, which is an embayment in Tampa Bay) is not improving at the same rate as the rest of the bay. East Bay is the center of shipping activity in Tampa Bay and the seventh largest port in the United States. One of the primary cargoes is phosphate ore and related products such as fertilizer. The potential for nutrient loading to East Bay from shipping activities is high and has not previously been measured. Nitrogen and phosphorus loads from East Bay to Hillsborough Bay were measured during selected time periods during June 1992 through May 1993; these data were used to estimate seasonal and annual loads. These loads were evaluated to determine whether the loss of fertilizer products from shipping activities resulted in increased nutrient loading to Hillsborough Bay. Discharge was measured, and water-quality samples were collected at the head of East Bay (exiting McKay Bay), and at the mouth of East Bay. Discharge and nitrogen and phosphorus concentrations for the period June 1992 through May 1993 were used to compute loads. Discharges from McKay Bay, Delaney Creek, and East Bay are highly variable because of the effect of tide. Flow patterns during discharge measurements generally were unidirectional in McKay Bay and Delaney Creek, but more complex, bidirectional patterns were observed at the mouth of East Bay. Tidally affected discharge data were digitally filtered with the Godin filter to remove the effects of tide so that residual, or net, discharge could be determined. Daily mean discharge from McKay Bay ranged from -1,900 to 2,420 cubic feet per second; from Delaney Creek, -3.8 to 162 cubic feet per second; and from East Bay, -437 to 3,780 cubic feet per second. Water quality in McKay Bay, Delaney Creek, and East Bay varies vertically, areally, and seasonally. Specific conductance and concentrations of phosphorus and ammonia nitrogen were greater near the bottom than near the surface at the head and mouth of East Bay. Concentrations of total nitrogen and ammonia plus organic nitrogen generally were greater at the head of East Bay than at the mouth, indicating that McKay Bay is the primary source of nitrogen to East Bay. Concentrations of total ammonia nitrogen, nitrite plus nitrate nitrogen, phosphorus, orthophosphorus, and suspended solids and values of turbidity and specific conductance generally were greater at the mouth of East Bay than at the head. The greatest concentrations of nitrogen and phosphorus were measured in Delaney Creek. In East Bay and McKay Bay, the greatest concentrations of nitrogen, phosphorus, and ammonia plus organic nitrogen occurred in summer, whereas turbidity, specific conductance, and concentrations of suspended solids were greater in winter. The greatest daily mean loads from McKay Bay and East Bay occurred in late June 1992 and April and May 1993 and coincided with periods of daily mean discharge greater than about 2,000 cubic feet per second. Although concentrations of nitrogen and phosphorus were greater in Delaney Creek than in McKay Bay and East Bay, loads were minimal because of minimal discharges from Delaney Creek. Monthly loads of total nitrogen ranged from about 20 tons to about 83 tons at McKay Bay; from about 1 ton to 4.2 tons at Delaney Creek; and from about 17 tons to 76 tons at the mouth of East Bay. Monthly loads of phosphorus ranged from about 11 tons to about 45 tons at McKay Bay; from about 0.62 ton to 2.6 tons at Delaney Creek; and from about 10 tons to about 45 tons at the mouth of East Bay. The results of this study indicate that nitrogen and phosphorus loads from the basin draining directly to East Bay (excluding loads from the McKa","language":"ENGLISH","publisher":"U.S. Geological Survey ;\r\nEarth Science Information Center, Open-File Reports Section [distributor],","doi":"10.3133/wri954167","usgsCitation":"Stoker, Y., Levesque, V., and Fritz, E., 1996, Discharge, water-quality characteristics, and nutrient loads from McKay Bay, Delaney Creek, and East Bay, Tampa, Florida, 1991-1993: U.S. Geological Survey Water-Resources Investigations Report 95-4167, v, 47 p. :ill. (some col.), maps ;28 cm., https://doi.org/10.3133/wri954167.","productDescription":"v, 47 p. :ill. (some col.), maps ;28 cm.","costCenters":[],"links":[{"id":2434,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri954167","linkFileType":{"id":5,"text":"html"}},{"id":119526,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/wri_95_4167.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a82e4b07f02db64a9ba","contributors":{"authors":[{"text":"Stoker, Y.E.","contributorId":13253,"corporation":false,"usgs":true,"family":"Stoker","given":"Y.E.","email":"","affiliations":[],"preferred":false,"id":202453,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Levesque, V.A.","contributorId":56268,"corporation":false,"usgs":true,"family":"Levesque","given":"V.A.","email":"","affiliations":[],"preferred":false,"id":202455,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Fritz, E.M.","contributorId":26337,"corporation":false,"usgs":true,"family":"Fritz","given":"E.M.","email":"","affiliations":[],"preferred":false,"id":202454,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":26714,"text":"wri954279 - 1996 - Hydrogeology and simulation of ground-water flow at the South Well Field, Columbus, Ohio","interactions":[],"lastModifiedDate":"2012-02-02T00:08:30","indexId":"wri954279","displayToPublicDate":"1996-09-01T00:00:00","publicationYear":"1996","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"95-4279","title":"Hydrogeology and simulation of ground-water flow at the South Well Field, Columbus, Ohio","docAbstract":"The City of Columbus, Ohio, operates four radial collector wells in southern Franklin County. The 'South Well Field' is completed in permeable outwash and ice-contact deposits, upon which flow the Scioto River and Big Walnut Creek. The wells are designed to yield approximately 42 million gallons per day; part of that yield results from induced infiltration of surface water from the Scioto River and Big Walnut Creek. The well field supplied up to 30 percent of the water supply of southern Columbus and its suburbs in 1991. This report describes the hydrogeology of southern Franklin County and a tran sient three-dimensional, numerical ground-water- flow model of the South Well Field.\r\n\r\nThe primary source of ground water in the study area is the glacial drift aquifer. The glacial drift is composed of sand, gravel, and clay depos ited during the Illinoian and Wisconsinan glaciations. In general, thick deposits of till containing lenses of sand and gravel dominate the drift in the area west of the Scioto River. The thickest and most productive parts of the glacial drift aquifer are in the buried valleys in the central and eastern parts of the study area underlying the Scioto River and Big Walnut Creek. Horizontal hydraulic conductivity of the glacial drift aquifer differs spa tially and ranges from 30 to 375 feet per day. The specific yield ranges from 0.12 to 0.30.\r\n\r\nThe secondary source of ground water within the study area is the underlying carbonate bedrock aquifer, which consists of Silurian and Devonian limestones, dolomites, and shales. The horizontal hydraulic conductivity of the carbonate bedrock aquifer ranges from 10 to 15 feet per day. The storage coefficient is about 0.0002. \r\n\r\nThe ground-water-flow system in the South Well Field area is recharged by precipitation, regional ground-water flow, and induced stream infiltration. Yearly recharge rates varied spatially and ranged from 4.0 to 12.0 inches. \r\n\r\nThe three-dimensional, ground-water-flow model was constructed by use of the U.S. Geological Survey three-dimensional finite-difference ground-water-flow code. Recharge, boundary flux, and river leakage are the principal sources of water to the flow system. The study area is bounded on the north and south by streamlines, with flow entering the area from the east and west. Areal recharge is contributed throughout the study area, although a comparatively high percentage of precipitation reaches the water table in the area east of the Scioto River where little surface drain age exists. Ground-water flow is downward in the uplands of the Scioto River, and upward near the river in the glacial drift and carbonate bedrock aquifers.\r\n\r\nThe numerical model contains 53 rows, 45 columns, and 3 layers. The uppermost two layers represent the glacial drift. The bottom layer represents the carbonate bedrock. The horizontal model grid is variably spaced to account for differences in available data and to simulate heads accurately in specific areas of interest. The length and width of grid cells range from 200 to 2,000 feet; the finer spacings are designed to increase detail in the areas near the collector wells. The model uses 7,155 active nodes. \r\n\r\nMeasurements of water levels from October 1979 were used to represent steady-state conditions before municipal pumping at the well field began. Measurements made during March 1986 were used to represent steady-state conditions after commencement of pumping at the well field. Water levels measured during March 1986 - June 1991 were used for calibration targets in the transient simulations. \r\n\r\nThe transient model was discretized into eight stress periods of 93 to 487 days on the basis of recharge, well-field pumpage, and available water-level data. Transient model calibration was based on seven sets of hydraulic-head measure ments made during March 1986 - June 1991. This time period includes large-scale increases in well- field production associated with a drought in the summer of 1988, an","language":"ENGLISH","publisher":"U.S. Geological Survey ;\r\nEarch Science Information Center, Open-File Reports Section [distributor],","doi":"10.3133/wri954279","usgsCitation":"Cunningham, W.L., Bair, E., and Yost, W., 1996, Hydrogeology and simulation of ground-water flow at the South Well Field, Columbus, Ohio: U.S. Geological Survey Water-Resources Investigations Report 95-4279, iv, 56 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri954279.","productDescription":"iv, 56 p. :ill., maps ;28 cm.","costCenters":[],"links":[{"id":121963,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1995/4279/report-thumb.jpg"},{"id":55589,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1995/4279/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4be4b07f02db6253b5","contributors":{"authors":[{"text":"Cunningham, W. L.","contributorId":22801,"corporation":false,"usgs":true,"family":"Cunningham","given":"W.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":196873,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bair, E. Scott","contributorId":73231,"corporation":false,"usgs":true,"family":"Bair","given":"E. Scott","affiliations":[],"preferred":false,"id":196875,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Yost, W.P.","contributorId":51791,"corporation":false,"usgs":true,"family":"Yost","given":"W.P.","email":"","affiliations":[],"preferred":false,"id":196874,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":38238,"text":"pp1538K - 1996 - Axial structures within the Reelfoot Rift delineated with magnetotelluric surveys","interactions":[],"lastModifiedDate":"2012-02-02T00:09:51","indexId":"pp1538K","displayToPublicDate":"1996-09-01T00:00:00","publicationYear":"1996","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":"1538","chapter":"K","title":"Axial structures within the Reelfoot Rift delineated with magnetotelluric surveys","docAbstract":"In the winter of 1811-12, three of the largest historic earthquakes in the United States occurred near New Madrid, Mo. Seismicity continues to the present day throughout a tightly clustered pattern of epicenters centered on the bootheel of Missouri, including parts of northeastern Arkansas, northwestern Tennessee, western Kentucky, and southern Illinois. In 1990, the New Madrid seismic zone/Central United States became the first seismically active region east of the Rocky Mountains to be designated a priority research area within the Natural Earthquake Hazards Reduction Program (NEHRP). This Professional Paper is a collection of papers, some published separately, presenting results of the newly intensified research program in this area. Major components of this research program include tectonic framework studies, seismicity and deformation monitoring and modeling, improved seismic hazard and risk assessments, and cooperative hazard mitigation studies.","language":"ENGLISH","doi":"10.3133/pp1538K","usgsCitation":"Rodriguez, B.D., Stanley, W.D., and Williams, J.M., 1996, Axial structures within the Reelfoot Rift delineated with magnetotelluric surveys: U.S. Geological Survey Professional Paper 1538, p. K1-K30, https://doi.org/10.3133/pp1538K.","productDescription":"p. K1-K30","costCenters":[],"links":[{"id":124266,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/1538k/report-thumb.jpg"},{"id":64605,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/1538k/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a82e4b07f02db64ae60","contributors":{"authors":[{"text":"Rodriguez, B. D.","contributorId":6084,"corporation":false,"usgs":true,"family":"Rodriguez","given":"B.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":219398,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Stanley, W. D.","contributorId":86756,"corporation":false,"usgs":true,"family":"Stanley","given":"W.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":219399,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Williams, J. M.","contributorId":91142,"corporation":false,"usgs":true,"family":"Williams","given":"J.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":219400,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":28519,"text":"wri914035 - 1996 - Hydrogeology and simulation of ground-water flow in the alluvial aquifer at Louisville, Kentucky","interactions":[],"lastModifiedDate":"2012-02-02T00:08:52","indexId":"wri914035","displayToPublicDate":"1996-09-01T00:00:00","publicationYear":"1996","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"91-4035","title":"Hydrogeology and simulation of ground-water flow in the alluvial aquifer at Louisville, Kentucky","docAbstract":"The alluvial aquifer at Louisville, Ky., lies in a valley eroded by glacial meltwater that was later partly filled with outwash sand and gravel deposits. The aquifer is primarily unconfined, and the direction of flow is from the adjacent limestone and shale valley wall toward the Ohio River and major pumping centers. Pumpage and water-level data indicate that the alluvial aquifer was in a steady-state condition in November 1962 and again in November 1983. Between these two dates, water-level data indicate a general rise in the water table. A two-dimensional finite-element ground-water-flow model of the alluvial aquifer was calibrated for both the steady-state and the transient-state period of 1962-83. The year 1962 represented a period in time when pumping was nearly three times that in 1983. The simulated steady-state water budget for 1962 indicated that of the total recharge to the aquifer of 5.19 million feet per day, 37.2 percent was flow from the river to pumped wells, 28.3 percent was recharge from rainfall, 19.7 percent was flow across the eastern valley wall, and 14.8 percent was upward flow from the bedrock. Discharge from the aquifer was to wells (68.9 percent) and to the Ohio River (31.1 percent). The simulated steady-state water budget for 1983 indicated that of the total recharge to the aquifer of 4.11 million feet per day, 42.6 percent was recharge from rainfall, 18.2 percent was flow across the eastern valley wall, 17.8 percent was flow from the river to pumped wells, 15.6 percent was upward flow from the bedrock, and 5.8 percent was flow from septic systems. The transient simulation resulted in an acceptable match between measured and simulated hydrographs. This gave additional confidence to the model calibration, choice of boundary conditions, and published values of specific yield. Both steady-state and transient-state models demonstrated that the main source of water needed to meet increased pumping requirements was induced flow from the Ohio River.","language":"ENGLISH","publisher":"U.S. Geological Survey ;\r\nEarth Science Information Center, Open-File Reports Section [distributor],","doi":"10.3133/wri914035","usgsCitation":"Lyverse, M.A., Starn, J., and Unthank, M., 1996, Hydrogeology and simulation of ground-water flow in the alluvial aquifer at Louisville, Kentucky: U.S. Geological Survey Water-Resources Investigations Report 91-4035, vi, 41 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri914035.","productDescription":"vi, 41 p. :ill., maps ;28 cm.","costCenters":[],"links":[{"id":123608,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1991/4035/report-thumb.jpg"},{"id":57319,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1991/4035/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4be4b07f02db62562d","contributors":{"authors":[{"text":"Lyverse, M. A.","contributorId":89151,"corporation":false,"usgs":true,"family":"Lyverse","given":"M.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":199954,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Starn, J.J.","contributorId":69591,"corporation":false,"usgs":true,"family":"Starn","given":"J.J.","email":"","affiliations":[],"preferred":false,"id":199953,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Unthank, M.D.","contributorId":35351,"corporation":false,"usgs":true,"family":"Unthank","given":"M.D.","email":"","affiliations":[],"preferred":false,"id":199952,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":26473,"text":"wri954215 - 1996 - Soil, water, and streambed quality at a demolished asphalt plant, Fort Bragg, North Carolina, 1992-94","interactions":[],"lastModifiedDate":"2017-01-27T11:47:14","indexId":"wri954215","displayToPublicDate":"1996-09-01T00:00:00","publicationYear":"1996","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"95-4215","title":"Soil, water, and streambed quality at a demolished asphalt plant, Fort Bragg, North Carolina, 1992-94","docAbstract":"A number of potentially hazardous chemicals were used at an asphalt plant on the Fort Bragg U.S. Army Reservation near Fayetteville, North Carolina. This plant was demolished in the late 1960's. Samples collected from soil, ground water, surface water, and streambed sediment were tested for the presence of contaminants. The sediment immediately underlying the demolished asphalt plant site consists mainly of sands, silts, and clayey sands with interbedded clay occurring at various depths. About 12 inches of rainfall per year infiltrate the unconfined surficial aquifer. The water table in this area is about 233 to 243 feet above sea level. Local ground water moves laterally, mainly towards the north- to-northwest at a rate of about 35 feet per year. where it discharges to Tank Creek, Little River, or one of their tributaries. A series of confining clays separate the surficial aquifer from the underlying upper Cape Fear aquifer. These clays help retard vertical migration of constituents dissolved in ground water. The saprolite-bedrock aquifer lies below the upper Cape Fear aquifer. In general ground water in the seven monitoring wells screened in the upper and lower part of the surficial aquifer did not contain detectable concentrations of chemicals related to past asphalt-plant activities. A small number of chemicals that were assumed to be unrelated to the asphalt plant were present in some of the study area monitoring wells. Ground water in four wells contained concentrations of organochlorine pesticides. Of these pesticides, concentrations of gamma-benzene hexachloride (lindane) (maximum of 0.76 micrograms per liter) exceeded the U.S. Environmental Protection Agency maximum contaminant level of 0.2 micrograms per liter in two wells. In addition, one well contained a trichloroethane concentration (7.7 micrograms per liter) that is assumed to be unrelated to demolished asphalt-plant operations, but exceeded the U.S. Environmental Protection Agency maximum contaminant level of 5.0 micrograms per liter. One well contained a fluoride concentration of 5.2 milligrams per liter that exceeded the U.S. Environmental Protection Agency maximum contaminant level of 4.0 milligrams per liter. Total and dissolved metals concentrations were generally typical of background levels. Some of the wells contained elevated levels of chloride (maximum of 749 milligrams per liter), specific conductance (maximum of 2,780 microsiemens per centimeter at 25 degrees Celsius), and dissolved solids (maximum of 1,520 milligrams per liter). Twelve of twenty-two soil samples that were collected at various depths at monitoring-well locations did not contain volatile organic compounds or polynuclear aromatic hydrocarbons. The remaining ten soil samples contained very low concentrations of polynuclear aromatic hydrocarbons and (or) analytical laboratory-related volatile organic compounds. The maximum concentrations were for fluoranthene and pyrene, at 780 and 750 micrograms per kilogram, respectively. In general, the polynuclear aromatic hydrocarbon concentrations were in sediment near the land surface. Streambed sediment from an unnamed, eastern tributary to Tank Creek in the eastern part of the site contained a small number of organochlorine pesticide compounds (a maximum of 1,400 milligrams per kilogram of 4,4'-DDD) and total petroleum hydrocarbons (113 milligrams per kilogram). Concentrations of metals and other inorganic constituents were generally typical of background concentrations. Surface water in this tributary did not contain elevated concentrations of anthropogenic chemicals.","language":"ENGLISH","publisher":"U.S. Geological Survey ;\r\nEarth Science Information Center, Open-File Reports Section [distributor],","doi":"10.3133/wri954215","usgsCitation":"Campbell, T., 1996, Soil, water, and streambed quality at a demolished asphalt plant, Fort Bragg, North Carolina, 1992-94: U.S. Geological Survey Water-Resources Investigations Report 95-4215, viii, 92 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri954215.","productDescription":"viii, 92 p. :ill., maps ;28 cm.","costCenters":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true}],"links":[{"id":158339,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1995/4215/report-thumb.jpg"},{"id":55292,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1995/4215/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"North Carolina","city":"Fort Bragg","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -79.62890625,\n              34.79576153473033\n            ],\n            [\n              -79.62890625,\n              36.09349937380574\n            ],\n            [\n              -78.145751953125,\n              36.09349937380574\n            ],\n            [\n              -78.145751953125,\n              34.79576153473033\n            ],\n            [\n              -79.62890625,\n              34.79576153473033\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49efe4b07f02db5edbc8","contributors":{"authors":[{"text":"Campbell, T.R.","contributorId":99594,"corporation":false,"usgs":true,"family":"Campbell","given":"T.R.","email":"","affiliations":[],"preferred":false,"id":196454,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":22021,"text":"ofr9642 - 1996 - Possible continuous-type (unconventional) gas accumulation in the Lower Silurian \"Clinton\" sands, Medina Group and Tuscarora Sandstone in the Appalachian Basin; a progress report of the 1995 project activities","interactions":[],"lastModifiedDate":"2012-02-02T00:07:45","indexId":"ofr9642","displayToPublicDate":"1996-09-01T00:00:00","publicationYear":"1996","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":"96-42","title":"Possible continuous-type (unconventional) gas accumulation in the Lower Silurian \"Clinton\" sands, Medina Group and Tuscarora Sandstone in the Appalachian Basin; a progress report of the 1995 project activities","docAbstract":"INTRODUCTION: \r\nIn the U.S. Geological Survey's (USGS) 1995 National Assessment of United States oil and gas resources (Gautier and others, 1995), the Appalachian basin was estimated to have, at a mean value, about 61 trillion cubic feet (TCF) of recoverable gas in sandstone and shale reservoirs of Paleozoic age. Approximately one-half of this gas resource is estimated to reside in a regionally extensive, continuous-type gas accumulation whose reservoirs consist of low-permeability sandstone of the Lower Silurian 'Clinton' sands and Medina Group (Gautier and others, 1995; Ryder, 1995). Recognizing the importance of this large regional gas accumulation for future energy considerations, the USGS initiated in January 1995 a multi-year study to evaluate the nature, distribution, and origin of natural gas in the 'Clinton' sands, Medina Group sandstones, and equivalent Tuscarora Sandstone. The project is part of a larger natural gas project, Continuous Gas Accumulations in Sandstones and Carbonates, coordinated in FY1995 by Ben E. Law and Jennie L. Ridgley, USGS, Denver. Approximately 2.6 man years were devoted to the Clinton/Medina project in FY1995.\r\n\r\nA continuous-type gas accumulation, referred to in the project, is a new term introduced by Schmoker (1995a) to identify those natural gas accumulations whose reservoirs are charged throughout with gas over a large area and whose entrapment does not involve a downdip gas-water contact. Gas in these accumulations is located downdip of the water column and, thus, is the reverse of conventional-type hydrocarbon accumulations. Commonly used industry terms that are more or less synonymous with continuous-type gas accumulations include basin- centered gas accumulation (Rose and others, 1984; Law and Spencer, 1993), tight (low-permeability) gas reservoir (Spencer, 1989; Law and others, 1989; Perry, 1994), and deep basin gas (Masters, 1979, 1984).\r\n\r\nThe realization that undiscovered gas in Lower Silurian sandstone reservoirs of the Appalachian basin probably occurs in a continuous accumulation rather than in conventionally trapped, discrete accumulations represents a significant departure from the 1989 National Assessment (Mast and others, 1989; deWitt, 1993). In 1989, a direct assessment (field-size distributions required for play analysis were unavailable) of the Lower Silurian sandstone play gave, at a mean value, about 1.7 TCF of gas. The 1995 estimate (~30 TCF of gas) is so much greater than the 1989 estimate (~1.7 TCF of gas) because of the interpreted continuous nature of the accumulation and the assessment methodology applied. The methodology for continuous hydrocarbon accumulations assumes that the reservoirs in the accumulation are gas-saturated and takes into account: 1) estimated ultimate recovery (EUR) per well probability distributions, 2) optimum area that a well can drain (spacing), 3) number of untested drill sites having the appropriate spacing area, 4) success ratio of previously drilled holes, and 5) risk (Schmoker, 1995b).\r\n\r\nDavis (1984), Zagorski (1988, 1991), and Law and Spencer (1993) were among the first petroleum geologists to suggest that gas in the 'Clinton' sands and Medina Group sandstones was trapped in a basin-centered/deep basin accumulation. They recognized many of the earmarks of a basin-centered/deep basin accumulation such as low-permeability reservoirs, abnormally low formation pressure, coalesced gas fields, gas shows or production in most holes drilled, low water yields, and a general lack of structural control on entrapment. Ryder (1995) adopted this interpretation by defining four continuous-type gas plays (6728-6731) in the 'Clinton' sands-Medina Group interval (fig.1).\r\n\r\nPlay 6728 (Clinton/Medina sandstone gas high potential) covers a 17,000 sq mi region of western New York, northwestern Pennsylvania, eastern Ohio, and a small part of westernmost West Virginia that is very favorable for future gas resources (fig.1). Also, this play includes a l","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/ofr9642","issn":"0094-9140","usgsCitation":"Ryder, R., Aggen, K., Hettinger, R.D., Law, B.E., Miller, J.J., Nuccio, V.F., Perry, W.J., Prensky, S.E., Filipo, J.J., and Wandrey, C.J., 1996, Possible continuous-type (unconventional) gas accumulation in the Lower Silurian \"Clinton\" sands, Medina Group and Tuscarora Sandstone in the Appalachian Basin; a progress report of the 1995 project activities: U.S. Geological Survey Open-File Report 96-42, iv, 82 p. :ill., maps (some col.); 28 cm., https://doi.org/10.3133/ofr9642.","productDescription":"iv, 82 p. :ill., maps (some col.); 28 cm.","costCenters":[],"links":[{"id":152949,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1996/0042/report-thumb.jpg"},{"id":9116,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/1996/of96-042/","linkFileType":{"id":5,"text":"html"}},{"id":51489,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1996/0042/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad6e4b07f02db683d3b","contributors":{"authors":[{"text":"Ryder, Robert T.","contributorId":77918,"corporation":false,"usgs":true,"family":"Ryder","given":"Robert T.","affiliations":[],"preferred":false,"id":186720,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Aggen, Kerry L.","contributorId":106749,"corporation":false,"usgs":true,"family":"Aggen","given":"Kerry L.","affiliations":[],"preferred":false,"id":186724,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hettinger, Robert D.","contributorId":102486,"corporation":false,"usgs":true,"family":"Hettinger","given":"Robert","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":186723,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Law, Ben E.","contributorId":85033,"corporation":false,"usgs":true,"family":"Law","given":"Ben","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":186721,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Miller, John J. 0000-0002-9098-0967 jmiller@usgs.gov","orcid":"https://orcid.org/0000-0002-9098-0967","contributorId":3785,"corporation":false,"usgs":true,"family":"Miller","given":"John","email":"jmiller@usgs.gov","middleInitial":"J.","affiliations":[{"id":164,"text":"Central Energy Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":186717,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Nuccio, Vito F. vnuccio@usgs.gov","contributorId":853,"corporation":false,"usgs":true,"family":"Nuccio","given":"Vito","email":"vnuccio@usgs.gov","middleInitial":"F.","affiliations":[],"preferred":true,"id":186715,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Perry, William J. Jr.","contributorId":32498,"corporation":false,"usgs":true,"family":"Perry","given":"William","suffix":"Jr.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":186718,"contributorType":{"id":1,"text":"Authors"},"rank":7},{"text":"Prensky, Stephen E.","contributorId":96703,"corporation":false,"usgs":true,"family":"Prensky","given":"Stephen","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":186722,"contributorType":{"id":1,"text":"Authors"},"rank":8},{"text":"Filipo, John J.","contributorId":45955,"corporation":false,"usgs":true,"family":"Filipo","given":"John","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":186719,"contributorType":{"id":1,"text":"Authors"},"rank":9},{"text":"Wandrey, Craig J. cwandrey@usgs.gov","contributorId":1590,"corporation":false,"usgs":true,"family":"Wandrey","given":"Craig","email":"cwandrey@usgs.gov","middleInitial":"J.","affiliations":[{"id":164,"text":"Central Energy Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":186716,"contributorType":{"id":1,"text":"Authors"},"rank":10}]}}
,{"id":21979,"text":"ofr9620B - 1996 - Neogene and Quaternary geology of a stratigraphic test hole on Horn Island, Mississippi Sound","interactions":[],"lastModifiedDate":"2020-03-27T06:59:20","indexId":"ofr9620B","displayToPublicDate":"1996-09-01T00:00:00","publicationYear":"1996","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":"96-20","chapter":"B","title":"Neogene and Quaternary geology of a stratigraphic test hole on Horn Island, Mississippi Sound","docAbstract":"<p>No abstract available.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr9620B","issn":"0094-9140","usgsCitation":"Gohn, G., Brewster-Wingard, G., Cronin, T.M., Edwards, L.E., Gibson, T., Rubin, M., and Willard, D., 1996, Neogene and Quaternary geology of a stratigraphic test hole on Horn Island, Mississippi Sound: U.S. Geological Survey Open-File Report 96-20, 23 p., https://doi.org/10.3133/ofr9620B.","productDescription":"23 p.","costCenters":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true},{"id":40020,"text":"Florence Bascom Geoscience Center","active":true,"usgs":true}],"links":[{"id":51453,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1996/0020b/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":152930,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1996/0020b/report-thumb.jpg"}],"country":"United States","state":"Mississippi, Alabama ","otherGeospatial":"Mississippi Sound","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -88.78910064697266,\n              30.208937975696163\n            ],\n            [\n              -88.57315063476562,\n              30.208937975696163\n            ],\n            [\n              -88.57315063476562,\n              30.267370168467806\n            ],\n            [\n              -88.78910064697266,\n              30.267370168467806\n            ],\n            [\n              -88.78910064697266,\n              30.208937975696163\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4affe4b07f02db697e2f","contributors":{"authors":[{"text":"Gohn, Gregory 0000-0003-2000-479X ggohn@usgs.gov","orcid":"https://orcid.org/0000-0003-2000-479X","contributorId":219822,"corporation":false,"usgs":true,"family":"Gohn","given":"Gregory","email":"ggohn@usgs.gov","affiliations":[{"id":40020,"text":"Florence Bascom Geoscience Center","active":true,"usgs":true},{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true}],"preferred":true,"id":186531,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Brewster-Wingard, G. L.","contributorId":102508,"corporation":false,"usgs":true,"family":"Brewster-Wingard","given":"G. L.","affiliations":[],"preferred":false,"id":186533,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Cronin, Thomas M. 0000-0002-2643-0979 tcronin@usgs.gov","orcid":"https://orcid.org/0000-0002-2643-0979","contributorId":2579,"corporation":false,"usgs":true,"family":"Cronin","given":"Thomas","email":"tcronin@usgs.gov","middleInitial":"M.","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":186530,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"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":40020,"text":"Florence Bascom Geoscience Center","active":true,"usgs":true},{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true}],"preferred":true,"id":186529,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Gibson, T. G.","contributorId":103702,"corporation":false,"usgs":true,"family":"Gibson","given":"T. G.","affiliations":[],"preferred":false,"id":186534,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Rubin, Meyer","contributorId":107283,"corporation":false,"usgs":true,"family":"Rubin","given":"Meyer","email":"","affiliations":[],"preferred":false,"id":186535,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Willard, Debra  A. 0000-0003-4878-0942","orcid":"https://orcid.org/0000-0003-4878-0942","contributorId":85982,"corporation":false,"usgs":true,"family":"Willard","given":"Debra  A.","affiliations":[],"preferred":false,"id":186532,"contributorType":{"id":1,"text":"Authors"},"rank":7}]}}
,{"id":70019041,"text":"70019041 - 1996 - Earthquakes and the southeastern boundary of the intact Iapetan margin in eastern North America","interactions":[],"lastModifiedDate":"2025-07-29T16:24:10.187499","indexId":"70019041","displayToPublicDate":"1996-09-01T00:00:00","publicationYear":"1996","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3372,"text":"Seismological Research Letters","onlineIssn":"1938-2057","printIssn":"0895-0695","active":true,"publicationSubtype":{"id":10}},"title":"Earthquakes and the southeastern boundary of the intact Iapetan margin in eastern North America","docAbstract":"<p><span>Earthquakes at three localities in eastern North America have been attributed on geological and seismological grounds to compressional reactivation of some of the late Proterozoic or early Paleozoic normal faults in the northeast-trending Iapetan passive margin. Assessment of seismic hazard can be aided by identifying the boundaries of the area of Iapetan faulting. A previous paper located the northwestern boundary. This report interprets deep seismic-reflection profiles as showing that the margin comprises a seismically active northwestern part, where Precambrian crust contains some Iapetan faults but remains mostly as it was formed, and a southeastern part, where later deformations likely destroyed or modified the Precambrian crust and Iapetan faults. Accordingly, the boundary between the northwestern and southeastern parts of the margin, which coincides approximately with the Appalachian gravity gradient, can be taken as the southeastern limit of potentially seismogenic Iapetan faults.</span></p>","language":"English","publisher":"GeoScienceWorld","doi":"10.1785/gssrl.67.5.77","issn":"00128287","usgsCitation":"Wheeler, R.L., 1996, Earthquakes and the southeastern boundary of the intact Iapetan margin in eastern North America: Seismological Research Letters, v. 67, no. 5, p. 77-83, https://doi.org/10.1785/gssrl.67.5.77.","productDescription":"7 p.","startPage":"77","endPage":"83","costCenters":[],"links":[{"id":226273,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Canada, United States","otherGeospatial":"eastern North America","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -54.2502026221228,\n              52.455495547752676\n            ],\n            [\n              -77.31466901821747,\n              41.2383548936905\n            ],\n            [\n              -80.48862204496822,\n              34.752591778926934\n            ],\n            [\n              -86.90152402114032,\n              31.46634422283111\n            ],\n            [\n              -84.24811384541448,\n              25.84563151864664\n            ],\n            [\n              -79.94840683558355,\n              24.914617306669044\n            ],\n            [\n              -74.23579295630763,\n              30.63667351222948\n            ],\n            [\n              -68.5231790770317,\n              36.35872971778991\n            ],\n            [\n              -59.510799405663164,\n              43.74758113158556\n            ],\n            [\n              -50.81989444848227,\n              47.09943858375916\n            ],\n            [\n              -54.2502026221228,\n              52.455495547752676\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","volume":"67","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a0511e4b0c8380cd50c53","contributors":{"authors":[{"text":"Wheeler, R. L.","contributorId":34916,"corporation":false,"usgs":true,"family":"Wheeler","given":"R.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":381496,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":39630,"text":"pp1404I - 1996 - Hydrogeologic framework of the North Carolina coastal plain","interactions":[{"subject":{"id":16592,"text":"ofr87690 - 1989 - Hydrogeologic framework of the North Carolina Coastal Plain aquifer system","indexId":"ofr87690","publicationYear":"1989","noYear":false,"title":"Hydrogeologic framework of the North Carolina Coastal Plain aquifer system"},"predicate":"SUPERSEDED_BY","object":{"id":39630,"text":"pp1404I - 1996 - Hydrogeologic framework of the North Carolina coastal plain","indexId":"pp1404I","publicationYear":"1996","noYear":false,"chapter":"I","title":"Hydrogeologic framework of the North Carolina coastal plain"},"id":1}],"lastModifiedDate":"2025-04-17T19:50:05.684131","indexId":"pp1404I","displayToPublicDate":"1996-08-01T00:00:00","publicationYear":"1996","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":"1404","chapter":"I","title":"Hydrogeologic framework of the North Carolina coastal plain","docAbstract":"The hydrogeologic framework of the North Carolina Coastal Plain aquifer system consists of 10 aquifers separated by 9 confining units. From top to bottom, the aquifers are the surficial aquifer, Yorktown aquifer, Pungo River aquifer, Castle Hayne aquifer, Beaufort aquifer, Peedee aquifer, Black Creek aquifer, upper Cape Fear aquifer, lower Cape Fear aquifer, and Lower Cretaceous aquifer. The uppermost aquifer (the surficial aquifer in most places) is a water-table aquifer, and the bottom of the system is underlain by crystalline bedrock.\r\n\r\nThe sedimentary deposits forming the aquifers are of Holocene to Cretaceous age and are composed mostly of sand, with lesser amounts of gravel and limestone. The confining units between the aquifers are composed primarily of clay and silt. The thickness of the aquifers ranges from zero along the Fall Line to more than 10,000 feet at Cape Hatteras. Prominent structural features are the increasing easterly homoclinal dip of the sediments and the Cape Fear arch, the axis of which trends in a southeast direction.\r\n\r\nStratigraphic continuity was determined from correlations of 161 geophysical logs along with data from drillers? and geologists? logs. Aquifers were defined by means of these logs as well as water-level and water-quality data and evidence of the continuity of pumping effects. Eighteen hydrogeologic sections depict the correlation of these aquifers throughout the North Carolina Coastal Plain.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/pp1404I","usgsCitation":"Winner, M.D., and Coble, R.W., 1996, Hydrogeologic framework of the North Carolina coastal plain: U.S. Geological Survey Professional Paper 1404, Report: 106 p.; 24 Plates: 52.00 x 25.00 inches or smaller, https://doi.org/10.3133/pp1404I.","productDescription":"Report: 106 p.; 24 Plates: 52.00 x 25.00 inches or 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Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4848.htm","linkFileType":{"id":5,"text":"html"}},{"id":67287,"rank":24,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1404i/plate-22.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67286,"rank":23,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1404i/plate-21.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67284,"rank":21,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1404i/plate-19.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"North Carolina","otherGeospatial":"North Carolina coastal plain","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -80.386962890625,\n              34.813803317113155\n            ],\n            [\n       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         34.488447837809304\n            ],\n            [\n              -76.35498046875,\n              34.642247047768535\n            ],\n            [\n              -76.08032226562499,\n              34.831841149828655\n            ],\n            [\n              -75.948486328125,\n              34.939985151560435\n            ],\n            [\n              -75.73974609375,\n              35.06597313798418\n            ],\n            [\n              -75.5419921875,\n              35.11990857099681\n            ],\n            [\n              -75.333251953125,\n              35.22767235493586\n            ],\n            [\n              -75.333251953125,\n              35.55010533588552\n            ],\n            [\n              -75.322265625,\n              35.746512259918504\n            ],\n            [\n              -75.443115234375,\n              35.951329861522666\n            ],\n            [\n              -75.56396484375,\n              36.19995805932895\n   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      -80.386962890625,\n              34.813803317113155\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a51e4b07f02db62a2c9","contributors":{"authors":[{"text":"Winner, M. D. Jr.","contributorId":51766,"corporation":false,"usgs":true,"family":"Winner","given":"M.","suffix":"Jr.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":221845,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Coble, R. W.","contributorId":49380,"corporation":false,"usgs":true,"family":"Coble","given":"R.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":221844,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":27284,"text":"wri944173 - 1996 - Temporal changes in the configuration of the water table in the vicinity of the management systems evaluation area site, central Nebraska","interactions":[],"lastModifiedDate":"2019-12-05T15:56:26","indexId":"wri944173","displayToPublicDate":"1996-08-01T00:00:00","publicationYear":"1996","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"94-4173","title":"Temporal changes in the configuration of the water table in the vicinity of the management systems evaluation area site, central Nebraska","docAbstract":"To improve understanding of the hydrologic characteristics of the shallow aquifer in the vicinity of the Management Systems Evaluation Area site near Shelton, Nebraska, water levels were measured in approximately 130 observation wells in both June and September 1991. Two water-table maps and a water-level-change map were drawn on the basis of these measurements. In addition, historical data from U.S. Geological Survey computer files and published reports were used to determine the approximate configuration of the water table in 1931 and to draw one short-term and two-long term water- level hydrographs. Comparison of the three water- table maps indicates general similarities. The average horizontal hydraulic gradient in the shallow aquifer is about 7.5 feet per mile, and the flow direction is to the east-northeast. The water table declined 2 to 10 feet between June and September 1991, with the greatest decline occurring in a wedge-shaped area south of the Wood River and north of the Platte River. The 1991 water-table configurations appear to indicate that the aquifer either was discharging to the Platte River in this reach or there was little flow between the river and the aquifer. Comparison of the 1931 and 1991 water-table maps indicates that, except for short-term variations, the water-table configuration changed little during this 61-year period. Two long-term water-level hydrographs confirm this conclusion, indicating that the shallow aquifer in this area has been in long-term, dynamic equilibrium.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri944173","usgsCitation":"Kilpatrick, J.M., 1996, Temporal changes in the configuration of the water table in the vicinity of the management systems evaluation area site, central Nebraska: U.S. Geological Survey Water-Resources Investigations Report 94-4173, 1 Plate: 39.36 x 39.77 inches, https://doi.org/10.3133/wri944173.","productDescription":"1 Plate: 39.36 x 39.77 inches","costCenters":[{"id":589,"text":"Toxic Substances Hydrology Program","active":true,"usgs":true}],"links":[{"id":159037,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1994/4173/report-thumb.jpg"},{"id":278847,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1994/4173/plate-1.pdf"}],"country":"United States","state":"Nebraska","otherGeospatial":"Platte River, Wood River","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -98.916667,40.666667 ], [ -98.916667,40.833333 ], [ -98.633333,40.833333 ], [ -98.633333,40.666667 ], [ -98.916667,40.666667 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db68559e","contributors":{"authors":[{"text":"Kilpatrick, John M. 0000-0002-1180-3752 jmkilpat@usgs.gov","orcid":"https://orcid.org/0000-0002-1180-3752","contributorId":1010,"corporation":false,"usgs":true,"family":"Kilpatrick","given":"John","email":"jmkilpat@usgs.gov","middleInitial":"M.","affiliations":[],"preferred":true,"id":197850,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":28516,"text":"wri964010 - 1996 - Geohydrology and contamination at the Michigan Department of Transportation maintenance garage area, Kalamazoo County, Michigan","interactions":[],"lastModifiedDate":"2017-01-12T13:02:49","indexId":"wri964010","displayToPublicDate":"1996-08-01T00:00:00","publicationYear":"1996","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"96-4010","title":"Geohydrology and contamination at the Michigan Department of Transportation maintenance garage area, Kalamazoo County, Michigan","docAbstract":"A leaking underground storage tank was removed from the Michigan Department of Transportation maintenance garage area in Kalamazoo County., Mich., in 1985. The tank had been leaking unleaded gasoline. Although a remediation system was operational at the site for several years after the tank was removed, ground-water samples collected from monitoring wells in the area consistently showed high concentrations of benzene, toluene. ethylbenzene, and xylenes--indicators of the presence of gasoline.  The U.S. Geological Survey did a study in cooperation with the Michigan Department of Transportation, to define the geology, hydrology, and occurrence of gasoline contamination in the maintenance garage area. The aquifer affected by gasoline contamination is an unconfined glaci'a.l sand and gravel aquifer. The average depth to water in the study area is about 74.7 feet. Water-level fluctuations are small; maximum fluctuation was slightly more than 1 foot during August 1993-August 1994. Hydraulic conductivities based on aquifer-test data collected for the study and estimated by use of the Cooper-Jacob method of solution ranged from 130 to 144 feet per day. Ground water is moving in an east-southeasterly direction at a rate of about I foot per day.  Leakage from perforated pipes leading from the underground storage tanks to the pump station was identified as a second source of gasoline contamination\t   to saturated and unsaturated zones. The existence of this previously unknown second source is part of the reason that previous remediation efforts were ineffective. Residual contaminants in the unsaturated zone are expected to continue to move to the water table with recharge, except in a small area covered by asphalt at the land surface.  The gasoline plume from the perforated pipe source has merged with that from the leaking underground storage tank, and the combined plume in the saturated zone is estimated to cover an area of 30,000 square feet. The combined plume is in the upper 20 feet of the saturated zone. The relative distribution of benzene, toluene, ethylbenzene, and xylenes indicate that factors such as sorption, solubility, and susceptibility to microbial degradation are affecting the movement of the combined plume. Given these factors, the plume is expected to move at a rate of less than 1 foot per day.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Lansing, MI","doi":"10.3133/wri964010","collaboration":"Prepared in cooperation with the Michigan Department of Transportation","usgsCitation":"Lynch, E.A., and Huffman, G., 1996, Geohydrology and contamination at the Michigan Department of Transportation maintenance garage area, Kalamazoo County, Michigan: U.S. Geological Survey Water-Resources Investigations Report 96-4010, v, 31 p., https://doi.org/10.3133/wri964010.","productDescription":"v, 31 p.","costCenters":[{"id":382,"text":"Michigan Water Science Center","active":true,"usgs":true}],"links":[{"id":57316,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1996/4010/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":123586,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1996/4010/report-thumb.jpg"}],"country":"United States","state":"Michigan","county":"Kalamazoo County","otherGeospatial":"Department of Transportation Maintenance Garage Area","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -85.664167,\n              42.283611\n            ],\n            [\n              -85.664167,\n              42.292222\n            ],\n            [\n              -85.659167,\n              42.292222\n            ],\n            [\n              -85.659167,\n              42.283611\n            ],\n            [\n              -85.664167,\n              42.283611\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b24e4b07f02db6aec59","contributors":{"authors":[{"text":"Lynch, E. A.","contributorId":99167,"corporation":false,"usgs":true,"family":"Lynch","given":"E.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":199947,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Huffman, G.C.","contributorId":44150,"corporation":false,"usgs":true,"family":"Huffman","given":"G.C.","email":"","affiliations":[],"preferred":false,"id":199946,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":24470,"text":"ofr96143 - 1996 - Hydrology of the Wolf Branch sinkhole basin, Lake County, east-central Florida","interactions":[],"lastModifiedDate":"2012-02-02T00:08:09","indexId":"ofr96143","displayToPublicDate":"1996-08-01T00:00:00","publicationYear":"1996","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":"96-143","title":"Hydrology of the Wolf Branch sinkhole basin, Lake County, east-central Florida","docAbstract":"A 4-year study of the hydrology of the Wolf Branch sinkhole basin in Lake County, Florida, was conducted from 1991-95 by the U.S. Geological Survey to provide information about the hydrologic characteristics of the drainage basin in the vicinity of Wolf Sink. Wolf Branch drains a 4.94 square mile area and directly recharges the Upper Floridan aquifer through Wolf Sink. Because of the direct connection of the sinkhole with the aquifer, a contaminant spill in the basin could pose a threat to the aquifer. The Wolf Branch drainage basin varies in hydrologic characteristics from its headwaters to its terminus at Wolf Sink. Ground- water seepage provides baseflow to the stream north of Wolf Branch Road, but the stream south of State Road 46 is intermittent and the stream can remain dry for months. A single culvert under a railroad crossing conducts flow from wetlands just south of State Road 46 to a well-defined channel which leads to Wolf Sink. The basin morphology is characterized by karst terrain, with many closed depressions which can provide intermittent surface-water storage. Wetlands in the lower third of the basin (south of State Road 46) also provide surface water storage. The presence of numerous water-control structures (impoundments, canals, and culverts), and the surface-water storage capacity throughout the basin affects the flow characteristics of Wolf Branch. Streamflow records for two stations (one above and one below major wetlands in the basin) indicate the flow about State Road 46 is characterized by rapid runoff and continuous baseflow, whereas below State Road 46, peak discharges are much lower but of longer duration than at the upstream station. Rainfall, discharge, ground-water level, and surface-water level data were collected at selected sites in the basin. Hydrologic conditions during the study ranged from long dry periods when there was no inflow to Wolf Sink, to very wet periods, as when nearly 7 inches of rain fell in a 2-day period in November 1994, following an extended wet season. A comparison to long-term rainfall record (40 years) indicates that this range in hydrologic conditions during the 4-year study is representative of the range of conditions expected during a much longer time period. Two dye-trace studies conducted during the study indicated no direct connections between the sink and local wells. The path of a constituent entering the aquifer through Wolf Sink generally would be to the east, following the gradient of the regional ground-water flow system. The conductance of Wolf Sink (the rate at which the sink conducts water to the underlying aquifer) was estimated from streamflow data, ground-water levels, and water levels in Wolf Sink. The range of hydrologic conditions during the study provided a basis for the determination of a representative conductance value. The regression of streamflow as a function of head difference between the sink water level and the potentiometric surface at an observation well (an approximation of the potentiometric level beneath Wolf Sink) resulted in a significant relation r2=0.91, mean square error = 1.60 cubic feet per second); and the slope of the regression line, representing sink conductance, was 1.48 cubic feet per second per foot of head difference. Flow and storm-volume frequency curves for selected time periods (1-day, 7-days, 14-days, 21-days, and 30-days) were generated based on streamflow data from January 10, 1992, to September 30, 1995. These curves indicate that, based on the available record, the volume of water that would have to be stored (in the event that streamflow had to be diverted from Wolf Sink) during a 30-day period would be equal to or less than about 11 acre-fee 30 percent of the time and 161 acre-feet 80 percent of the time. The maximum volume that would be generated during a 30-day period, based on this study, would be about 570 acre-feet.","language":"ENGLISH","publisher":"U.S. Geological Survey ;\r\nUSGS Information Services,","doi":"10.3133/ofr96143","issn":"0094-9140","usgsCitation":"Schiffer, D., 1996, Hydrology of the Wolf Branch sinkhole basin, Lake County, east-central Florida: U.S. Geological Survey Open-File Report 96-143, iv, 29 p. :ill., maps ;28 cm., https://doi.org/10.3133/ofr96143.","productDescription":"iv, 29 p. :ill., maps ;28 cm.","costCenters":[],"links":[{"id":156454,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1996/0143/report-thumb.jpg"},{"id":53536,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1996/0143/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0ee4b07f02db5fdb68","contributors":{"authors":[{"text":"Schiffer, D. M.","contributorId":102103,"corporation":false,"usgs":true,"family":"Schiffer","given":"D. M.","affiliations":[],"preferred":false,"id":191987,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70211104,"text":"70211104 - 1996 - Hazards and climatic impact of subduction‐zone volcanism: A global and historical perspective","interactions":[],"lastModifiedDate":"2020-07-15T14:28:23.525549","indexId":"70211104","displayToPublicDate":"1996-07-14T14:37:36","publicationYear":"1996","noYear":false,"publicationType":{"id":5,"text":"Book chapter"},"publicationSubtype":{"id":24,"text":"Book Chapter"},"title":"Hazards and climatic impact of subduction‐zone volcanism: A global and historical perspective","docAbstract":"<p>Subduction-zone volcanoes account for more than 80 percent of the documented eruptions in recorded history, even though volcanism--deep and, hence, unobserved--along the global oceanic ridge systems overwhelmingly dominates in eruptive output. Because subduction-zone eruptions can be highly explosive, they pose some of the greatest natural hazards to society if the eruptions occur in densely populated regions. Of the six worst volcanic disasters since A.D. 1600, five have occurred at subduction-zone volcanoes: Unzen, Japan (1792); Tambora, Indonesia (1815); Krakatau, Indonesia (1883); Mont Pe16e, Martinique (1902); and Nevado del Ruiz, Colombia (1985). Sulfuric acid droplets in stratospheric volcanic clouds produced by voluminous explosive eruptions can influence global climate. The 1815 Tambora eruption caused in 1816 a decrease of several Celsius degrees in average summer temperature in Europe and the eastern United States and Canada, resulting in the well-known \"Year Without Summer.\" Similarly, the eruptions of E1 Chichon (Mexico) in 1982 and of Mount Pinatubo (Philippines) in 1991 lowered average temperatures for the northern hemisphere by as much as 0.2 to 0.5 øC, respectively. However, eruption-induced climatic effects of historical eruptions appear to be short-lived, lasting at most for only a few years. </p>","largerWorkType":{"id":4,"text":"Book"},"largerWorkTitle":"Subduction: Top to Bottom","largerWorkSubtype":{"id":15,"text":"Monograph"},"language":"English","publisher":"Springer Nature","doi":"10.1029/GM096p0331","usgsCitation":"Tilling, R.I., 1996, Hazards and climatic impact of subduction‐zone volcanism: A global and historical perspective, chap. <i>of</i> Subduction: Top to Bottom, v. 96, p. 331-335, https://doi.org/10.1029/GM096p0331.","productDescription":"5 p.","startPage":"331","endPage":"335","costCenters":[{"id":153,"text":"California Volcano Observatory","active":false,"usgs":true}],"links":[{"id":376386,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"96","noUsgsAuthors":false,"publicationDate":"2013-03-23","publicationStatus":"PW","contributors":{"authors":[{"text":"Tilling, Robert I. 0000-0003-4263-7221 rtilling@usgs.gov","orcid":"https://orcid.org/0000-0003-4263-7221","contributorId":2567,"corporation":false,"usgs":true,"family":"Tilling","given":"Robert","email":"rtilling@usgs.gov","middleInitial":"I.","affiliations":[],"preferred":true,"id":792781,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":5224,"text":"fs10696 - 1996 - Floods, runoff, and snowpack in Utah, 1995","interactions":[],"lastModifiedDate":"2017-02-03T11:37:25","indexId":"fs10696","displayToPublicDate":"1996-07-01T00:00:00","publicationYear":"1996","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":313,"text":"Fact Sheet","code":"FS","onlineIssn":"2327-6932","printIssn":"2327-6916","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"106-96","title":"Floods, runoff, and snowpack in Utah, 1995","docAbstract":"<p>U<span>tah, like other States in the western United States, has experienced several rapid and extreme changes between wet and dry precipitation cycles during recent years. During the 1995 water year (October 1994 to September 1995), most areas of Utah experienced greater-than-normal precipitation (1961-90), which was reflected in greater-than-average snowpack, moderate flooding, a landslide in southwestern Utah, and prolonged high runoff in northern and eastern Utah. Preliminary monthly streamflow data for January to June 1995 from 11 sites gaged by the U.S. Geological Survey were grouped into three regions of the State and compared with snow-water equivalent data from 6 selected SNOTEL (SNOwpack TELemetered) sites operated by the Natural Resources Conservation Service (fig. 1).</span></p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Salt Lake City, UT","doi":"10.3133/fs10696","usgsCitation":"Allen, D., 1996, Floods, runoff, and snowpack in Utah, 1995: U.S. Geological Survey Fact Sheet 106-96, 2 p., https://doi.org/10.3133/fs10696.","productDescription":"2 p.","numberOfPages":"2","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":125243,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/fs/1996/0106/report-thumb.jpg"},{"id":31947,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/fs/1996/0106/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Utah","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49d8e4b07f02db5df76e","contributors":{"authors":[{"text":"Allen, D.V.","contributorId":6129,"corporation":false,"usgs":true,"family":"Allen","given":"D.V.","email":"","affiliations":[],"preferred":false,"id":150645,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":38231,"text":"pp1416D - 1996 - Hydrology of the Mississippi River valley alluvial aquifer, south-central United States","interactions":[{"subject":{"id":17922,"text":"ofr90358 - 1990 - Hydrology of the Mississippi River Valley alluvial aquifer, South-Central United States","indexId":"ofr90358","publicationYear":"1990","noYear":false,"title":"Hydrology of the Mississippi River Valley alluvial aquifer, South-Central United States"},"predicate":"SUPERSEDED_BY","object":{"id":38231,"text":"pp1416D - 1996 - Hydrology of the Mississippi River valley alluvial aquifer, south-central United States","indexId":"pp1416D","publicationYear":"1996","noYear":false,"chapter":"D","title":"Hydrology of the Mississippi River valley alluvial aquifer, south-central United States"},"id":1}],"lastModifiedDate":"2012-02-02T00:09:51","indexId":"pp1416D","displayToPublicDate":"1996-06-01T00:00:00","publicationYear":"1996","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":"1416","chapter":"D","title":"Hydrology of the Mississippi River valley alluvial aquifer, south-central United States","docAbstract":"Ground-water flow simulation indicates that pumpage from the aquifer since the early 1900's has caused a decrease in ground-water outflow to rivers, an increase in flow from rivers into the aquifer, and an increase in flow to the aquifer through the overlying confining unit. By the mid-1970's, rivers became a source of more than 30 percent of total flow into the aquifer rather than the sink of net outflow, and by 1982 inflow through the overlying confining unit increased about 60 percent. Areas with the greatest potential for additional pumpage are northwestern Mississippi and northern parts of the area east of Crowleys Ridge.","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Regional aquifer-system analysis--Gulf Coastal Plain","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"ENGLISH","doi":"10.3133/pp1416D","usgsCitation":"Ackerman, D.J., 1996, Hydrology of the Mississippi River valley alluvial aquifer, south-central United States: U.S. Geological Survey Professional Paper 1416, p. D1-D56; 8 plates in separate case, https://doi.org/10.3133/pp1416D.","productDescription":"p. D1-D56; 8 plates in separate case","costCenters":[],"links":[{"id":104648,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4877.htm","linkFileType":{"id":5,"text":"html"},"description":"4877"},{"id":122122,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/1416d/report-thumb.jpg"},{"id":64577,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1416d/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":64578,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1416d/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":64579,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1416d/plate-8.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":64580,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/1416d/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":64572,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1416d/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":64573,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1416d/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":64574,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1416d/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":64575,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1416d/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":64576,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1416d/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aaae4b07f02db668a97","contributors":{"authors":[{"text":"Ackerman, D. J.","contributorId":53380,"corporation":false,"usgs":true,"family":"Ackerman","given":"D.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":219383,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":39631,"text":"pp1408A - 1996 - Summary of the Snake River plain Regional Aquifer-System Analysis in Idaho and eastern Oregon","interactions":[{"subject":{"id":19841,"text":"ofr9198 - 1993 - Summary of the Snake River plain Regional Aquifer-System Analysis in Idaho and eastern Oregon","indexId":"ofr9198","publicationYear":"1993","noYear":false,"title":"Summary of the Snake River plain Regional Aquifer-System Analysis in Idaho and eastern Oregon"},"predicate":"SUPERSEDED_BY","object":{"id":39631,"text":"pp1408A - 1996 - Summary of the Snake River plain Regional Aquifer-System Analysis in Idaho and eastern Oregon","indexId":"pp1408A","publicationYear":"1996","noYear":false,"chapter":"A","title":"Summary of the Snake River plain Regional Aquifer-System Analysis in Idaho and eastern Oregon"},"id":1}],"lastModifiedDate":"2013-11-19T15:48:35","indexId":"pp1408A","displayToPublicDate":"1996-05-01T00:00:00","publicationYear":"1996","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":"1408","chapter":"A","title":"Summary of the Snake River plain Regional Aquifer-System Analysis in Idaho and eastern Oregon","docAbstract":"Regional aquifers underlying the 15,600-square-mile Snake River Plain in southern Idaho and eastern Oregon was studied as part of the U.S. Geological Survey's Regional Aquifer-System Analysis program. The largest and most productive aquifers in the Snake River Plain are composed of Quaternary basalt of the Snake River Group, which underlies most of the 10,8000-square-mile eastern plain. Aquifer tests and simulation indicate that transmissivity of the upper 200 feet of the basalt aquifer in the eastern plain commonly ranges from about 100,000 to 1,000,000 feet squared per day. However, transmissivity of the total aquifer thickness may be as much as 10 million feet squared per day. Specific yield of the upper 200 feet of the aquifer ranges from about 0.01 to 0.20. Average horizontal hydraulic conductivity of the upper 200 feet of the basalt aquifer ranges from less than 100 to 9,000 feet per day. Values may be one to several orders of magnitude higher in parts in individual flows, such as flow tops. Vertical hydraulic conductivity is probably several orders of magnitude lower than horizontal hydraulic conductivity and is generally related to the number of joints. Pillow lava in ancestral Snake River channels has the highest hydraulic conductivity of all rock types. Hydraulic conductivity of the basalt decreases with depth because of secondary filling of voids with calcite and silica. An estimated 80 to 120 million acre-feet of water is believed to be stored in the upper 200 feet of the basalt aquifer in the eastern plain. The most productive aquifers in the 4,800-square-mile western plain are alluvial sand and gravel in the Boise River valley. Although aquifer tests indicate that transmissivity of alluvium in the Boise River valley ranges from 5,000 to 160,000 feet squared per day, simulation suggests that average transmissivity of the upper 500 feet is generally less than 20,000 feet squared per day. Vertically averaged horizontal hydraulic conductivity of the upper 500 feet of alluvium ranges from about 4 to 40 feet per day; higher values can be expected in individual sand and gravel zones. Vertical hydraulic conductivity is considerably lower because of the presence of clay layers. Hydraulic heads measured in piezometers, interpreted from diagrams showing ground-water flow and equipotential lines and estimated by computer simulation, demonstrate that water movement is three dimensional through the rock framework. Natural recharge takes place along the margins of the plain where head decreases with depth; discharge takes place near some reaches of the Snake River and the Boise River where head increases with depth. Geothermal water in rhyolitic rocks in the western plain and western part of the eastern plain has higher hydraulic head than the overlying cold water. Geothermal water, therefore, moves upward and merges into the cold-water system. Basin water-budget analyses indicate that the volume of cold water. Carbon-14 age determinations, which indicate that residence time of geothermal water is 17,700 to 20,300 years, plus or minus 4,000 years, imply slow movement of water through the geothermal system. Along much of its length, the Snake River gains large quantities of ground water. On the eastern plain, the river gained about 1.9 million acre-feet of water between Blackfoot and Neeley, Idaho, in 1980. Between Milner and King Hill, Idaho, the river gained 4.7 million acre-feet, mostly as spring flow from the north side. Upstream from Blackfoot and in the vicinity of Lake Walcott, the rover loses flow to ground water during parts or all of the year. On the western plain, river gains from ground water are small relative to those on the eastern plain; most are from seepage. Streams in tributary drainage basins supply calcium/bicarbonate type and calcium/magnesium/bicarbonate type water to the plain. Water type is a reflection of the chemical composition of rocks in the drainage basin, Concentrations of dissolved solids are smallest, about 50 milligrams per liter, in streams such as the Boise River that drain areas of granitic rocks; concentrations are greatest, about 400 milligrams per liter, in streams such as the Owyhee and Raft Rivers that drain area of sedimentary rocks. Water chemistry reflects the interaction of surface water and ground water. The chemical composition of ground water in the plain is essentially the same as that in streamflow and groundwater discharge from tributary drainage basins. Tributary drainage basins supplied 85 percent of the ground-water recharge in the eastern plain during 1980 and a nearly equivalent percentage of the solute load in ground water; human activities and dissolution of minerals supplied the other solutes. Dissolved-solids concentrations in ground water were generally less than 400 milligrams per liter. Water from the lower geothermal system is chemically different from water from the upper cold-water system. Geothermal water typically has greater concentrations of sodium, bicarbonate, sulfate, chloride, fluoride, silica, arsenic, boron, and lithium and smaller concentrations of calcium, magnesium, and hydrogen. Difference are attributed to ion exchange as geothermal moves through the rock framework. Irrigation, mostly on the Snake River Plain, accounted for about 96 percent of consumptive water use in Idaho during 1980. The use of surface water for irrigation for more than 100 years has caused major changes in the hydrologic system on the plain. Construction of dams, reservoirs, and diversifications effected planned changes in the surface-water system but resulted in largely unplanned changes in the ground-water system. During those years of irrigation, annual recharge in the main part of the eastern plain increased to about 6.7 million acre-feet in 1980, or by about 70 percent. Most of the increase was from percolation of surface water diverted for irrigation. From preirrigation to 1952, groundwater storage increased about 24 million acre-feet, and storage decreased from 1952 to 1964 and from 1976 to 1980 because of below-normal precipitation and increased withdrawals of ground water for irrigation. Annual ground-water discharge increased to about 7.1 million acre-feet in 1980, or about 80 percent since the start of irrigation. About 10 percent of the 1980 total discharge was ground-water pumpage. About 3.1 million acres, or almost one-third of the plain, was irrigated during 1980: 2.0 million acres with surface water, 1.0 million acres with ground water, and 0.1 million acres with combined surface and ground water. About 8.9 million acre-feet of Snake River water was diverted for irrigation during 1980 and 2.3 million acre-feet of ground water was pumped from 5,300 wells. Most irrigation wells on the eastern plain are open to basalt. About two-thirds of them yield more than 1,500 gallons per minute with a reported maximum of 7,240 gallons per minute; drawdown is less than 20 feet in two-thirds of the wells. Most irrigation wells on the western plain are open to sedimentary rocks. About one-third of them yield more than 1,00 gallons per minute with a reported maximum of 3,850 gallons per minute; drawndown is less than 20 feet in about one-fifth of the wells. The major instream use of water on the Snake River Plain is hydroelectric power generation. Fifty-two million acre-feet of water generated 2.6 million megawatthours of electricity during 1980. Digital computer ground-water flows models of the eastern and western plain reasonably simulated regional changes in water levels and ground-water discharges from 1880 (preirrigation) to 1980. Model results support the concept of three-dimensional flow and the hypotheses of no underflow between the eastern and western plain. Simulation of the regional aquifer system in the eastern plain indicates that is 1980 hydrologic conditions, including pumpage, were to remain the same for another 30 years, moderate declines in ground-water levels and decreases in spring discharges would continue. Increased ground-water pumpage to irrigate an additional 1 million acres could cause ground-water levels to decline a few tens of feet in the central part of the plain and could cause corresponding decreases in ground-water discharge. A combination of actions such as increased ground-water pumpage and decreased use of surface water for irrigation (resulting in reduced recharge) would accentuate the changes.","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/pp1408A","usgsCitation":"Lindholm, G.F., 1996, Summary of the Snake River plain Regional Aquifer-System Analysis in Idaho and eastern Oregon: U.S. Geological Survey Professional Paper 1408, Report: vii, 59 p.; 1 Plate: 34.00 x 24.00 inches, https://doi.org/10.3133/pp1408A.","productDescription":"Report: vii, 59 p.; 1 Plate: 34.00 x 24.00 inches","numberOfPages":"68","costCenters":[{"id":343,"text":"Idaho Water Science Center","active":true,"usgs":true}],"links":[{"id":104631,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4855.htm","linkFileType":{"id":5,"text":"html"},"description":"4855"},{"id":124963,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/1408a/report-thumb.jpg"},{"id":67291,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1408a/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67292,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/1408a/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Idaho;Oregon","otherGeospatial":"Snake River Plain","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -117.0,42.0 ], [ -117.0,45.0 ], [ -111.0,45.0 ], [ -111.0,42.0 ], [ -117.0,42.0 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b01e4b07f02db6985c3","contributors":{"authors":[{"text":"Lindholm, G. 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,{"id":70018579,"text":"70018579 - 1996 - Chemical evaluation of soil-solution in acid forest soils","interactions":[],"lastModifiedDate":"2025-08-15T16:31:20.052455","indexId":"70018579","displayToPublicDate":"1996-05-01T00:00:00","publicationYear":"1996","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3419,"text":"Soil Science","active":true,"publicationSubtype":{"id":10}},"title":"Chemical evaluation of soil-solution in acid forest soils","docAbstract":"Soil-solution chemistry is commonly studied in forests through the use of soil lysimeters.This approach is impractical for regional survey studies, however, because lysimeter installation and operation is expensive and time consuming. To address these problems, a new technique was developed to compare soil-solution chemistry among red spruce stands in New York, Vermont, New Hampshire, Maine. Soil solutions were expelled by positive air pressure from soil that had been placed in a sealed cylinder. Before the air pressure was applied, a solution chemically similar to throughfall was added to the soil to bring it to approximate field capacity. After the solution sample was expelled, the soil was removed from the cylinder and chemically analyzed. The method was tested with homogenized Oa and Bs horizon soils collected from a red spruce stand in the Adirondack Mountains of New York, a red spruce stand in east-central Vermont, and a mixed hardwood stand in the Catskill Mountains of New York. Reproducibility, effects of varying the reaction time between adding throughfall and expelling soil solution (5-65 minutes) and effects of varying the chemical composition of added throughfall, were evaluated. In general, results showed that (i) the method was reproducible (coefficients of variation were generally < 15%), (ii) variations in the length of reaction-time did not affect expelled solution concentrations, and (iii) adding and expelling solution did not cause detectable changes in soil exchange chemistry. Concentrations of expelled solutions varied with the concentrations of added throughfall; the lower the CEC, the more sensitive expelled solution concentrations were to the chemical concentrations of added throughfall. Addition of a tracer (NaBr) showed that the expelled solution was a mixture of added solution and solution that preexisted in the soil. Comparisons of expelled solution concentrations with concentrations of soil solutions collected by zero-tension and tension lysimetry indicated that expelled solution concentrations were higher than those obtained with either type of lysimeter, although there was less difference with tension lysimeters than zero-tension lysimeters. The method used for collection of soil solution should be taken into consideration whenever soil solution data are being interpreted.","language":"English","publisher":"Wolters Kluwer","doi":"10.1097/00010694-199605000-00005","issn":"0038075X","usgsCitation":"Lawrence, G., and David, M.B., 1996, Chemical evaluation of soil-solution in acid forest soils: Soil Science, v. 161, no. 5, p. 298-313, https://doi.org/10.1097/00010694-199605000-00005.","productDescription":"16 p.","startPage":"298","endPage":"313","costCenters":[],"links":[{"id":227080,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"New York, Vermont","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -75.07854938310682,\n              45.0375693793855\n            ],\n            [\n              -76.84879221247608,\n              43.645207343131446\n            ],\n            [\n              -78.71545121677863,\n              43.65390388320041\n            ],\n            [\n              -79.15472998074212,\n              43.46427693178023\n            ],\n            [\n              -79.80390956890837,\n              42.01496762411051\n            ],\n            [\n              -76.10118224340155,\n              42.06809908544358\n            ],\n            [\n              -75.37117922518975,\n              42.00656159213099\n            ],\n            [\n              -74.92059668437619,\n              41.41942050156172\n            ],\n            [\n              -73.63653860327466,\n              40.94701324452626\n            ],\n            [\n              -73.24938035081587,\n              42.72783107480066\n            ],\n            [\n              -72.44760520406116,\n              42.713014923774494\n            ],\n            [\n              -72.23101112234596,\n              43.7957620531397\n            ],\n            [\n              -71.44624914128815,\n              45.00137034379799\n            ],\n            [\n              -75.07854938310682,\n              45.0375693793855\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","volume":"161","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059f57be4b0c8380cd4c24d","contributors":{"authors":[{"text":"Lawrence, G.B. 0000-0002-8035-2350","orcid":"https://orcid.org/0000-0002-8035-2350","contributorId":76347,"corporation":false,"usgs":true,"family":"Lawrence","given":"G.B.","affiliations":[],"preferred":false,"id":380104,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"David, Mark B.","contributorId":43255,"corporation":false,"usgs":false,"family":"David","given":"Mark","email":"","middleInitial":"B.","affiliations":[{"id":35161,"text":"University of Illinois, Urbana-Champaign","active":true,"usgs":false}],"preferred":false,"id":380103,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70018476,"text":"70018476 - 1996 - Far-travelled Permian chert of the North Fork terrane, Klamath Mountains, California","interactions":[],"lastModifiedDate":"2025-09-09T15:20:52.353171","indexId":"70018476","displayToPublicDate":"1996-04-01T00:00:00","publicationYear":"1996","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3524,"text":"Tectonics","active":true,"publicationSubtype":{"id":10}},"title":"Far-travelled Permian chert of the North Fork terrane, Klamath Mountains, California","docAbstract":"<p><span>Permian chert in the North Fork terrane and correlative rocks of the Klamath Mountains province has a remanent magnetization that is prefolding and presumably primary. Paleomagnetic results indicate that the chert formed at a paleolatitude of 8.6° ± 2.5° but in which hemisphere remains uncertain. This finding requires that these rocks have undergone at least 8.6° ± 4.4° of northward transport relative to Permian North America since their deposition. Paleontological evidence suggests that the Permian limestone of the Eastern Klamath terrane originated thousands of kilometers distant from North America. The limestone of the North Fork terrane may have formed at a similar or even greater distance as suggested by its faunal affinity to the Eastern Klamath terrane and more westerly position. Available evidence indicates that convergence of the North Fork and composite Central Metamorphic-Eastern Klamath terranes occurred during Triassic or Early Jurassic time and that their joining together was a Middle Jurassic event. Primary and secondary magnetizations indicate that the new composite terrane containing these and other rocks of the Western Paleozoic and Triassic belt behaved as a single rigid block that has been latitudinally concordant with the North American craton since Middle Jurassic time.</span></p>","language":"English","publisher":"American Geophysical Union","doi":"10.1029/95TC03054","issn":"02787407","usgsCitation":"Mankinen, E.A., Irwin, W., and Blome, C., 1996, Far-travelled Permian chert of the North Fork terrane, Klamath Mountains, California: Tectonics, v. 15, no. 2, p. 314-328, https://doi.org/10.1029/95TC03054.","productDescription":"15 p.","startPage":"314","endPage":"328","costCenters":[],"links":[{"id":227474,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Klamath Mountains","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -124.036421178256,\n              42.03983525934291\n            ],\n            [\n              -124.036421178256,\n              40.5754601953125\n            ],\n            [\n              -122.57632218936385,\n              40.5754601953125\n            ],\n            [\n              -122.57632218936385,\n              42.03983525934291\n            ],\n            [\n              -124.036421178256,\n              42.03983525934291\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","volume":"15","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a0ef9e4b0c8380cd536d7","contributors":{"authors":[{"text":"Mankinen, Edward A. 0000-0001-7496-2681 emank@usgs.gov","orcid":"https://orcid.org/0000-0001-7496-2681","contributorId":1054,"corporation":false,"usgs":true,"family":"Mankinen","given":"Edward","email":"emank@usgs.gov","middleInitial":"A.","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":379727,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Irwin, W. P.","contributorId":82347,"corporation":false,"usgs":true,"family":"Irwin","given":"W. P.","affiliations":[],"preferred":false,"id":379729,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Blome, C.D.","contributorId":60647,"corporation":false,"usgs":true,"family":"Blome","given":"C.D.","email":"","affiliations":[],"preferred":false,"id":379728,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":38228,"text":"pp1409B - 1996 - Hydrogeologic framework of the Great Basin region of Nevada, Utah, and adjacent states","interactions":[],"lastModifiedDate":"2012-02-02T00:09:57","indexId":"pp1409B","displayToPublicDate":"1996-04-01T00:00:00","publicationYear":"1996","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":"1409","chapter":"B","title":"Hydrogeologic framework of the Great Basin region of Nevada, Utah, and adjacent states","docAbstract":"Regional aquifer systems in the Great Basin consist of carbonate-rock aquifers in the eastern Great Basin and basin-fill aquifers throughout the region. In the carbonate-rock aquifers, barriers to regional flow include Precambrian crystalline basement, upper Precambrian and Lower Cambrian clastic sedimentary rocks, and Jurassic to Tertiary granitic rocks. Basin-fill aquifers are connected to carbonate-rock aquifers in the eastern Great Basin and can be hydraulically connected with each other throughout the Great Basin.","language":"ENGLISH","doi":"10.3133/pp1409B","usgsCitation":"Plume, R., 1996, Hydrogeologic framework of the Great Basin region of Nevada, Utah, and adjacent states: U.S. Geological Survey Professional Paper 1409, p. B1-B64; 5 plates in pocket, https://doi.org/10.3133/pp1409B.","productDescription":"p. B1-B64; 5 plates in pocket","costCenters":[],"links":[{"id":104635,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4860.htm","linkFileType":{"id":5,"text":"html"},"description":"4860"},{"id":119771,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/1409b/report-thumb.jpg"},{"id":64564,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1409b/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":64565,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1409b/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":64566,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1409b/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":64567,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1409b/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":64568,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1409b/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":64569,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/1409b/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4ee4b07f02db627a59","contributors":{"authors":[{"text":"Plume, R. W.","contributorId":21975,"corporation":false,"usgs":true,"family":"Plume","given":"R. W.","affiliations":[],"preferred":false,"id":219378,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70018625,"text":"70018625 - 1996 - Crustal and upper mantle velocity structure of the Salton Trough, southeast California","interactions":[],"lastModifiedDate":"2025-09-09T15:15:05.045292","indexId":"70018625","displayToPublicDate":"1996-04-01T00:00:00","publicationYear":"1996","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3524,"text":"Tectonics","active":true,"publicationSubtype":{"id":10}},"title":"Crustal and upper mantle velocity structure of the Salton Trough, southeast California","docAbstract":"<p><span>This paper presents data and modelling results from a crustal and upper mantle wide-angle seismic transect across the Salton Trough region in southeast California. The Salton Trough is a unique part of the Basin and Range province where mid-ocean ridge/transform spreading in the Gulf of California has evolved northward into the continent. In 1992, the U.S. Geological Survey (USGS) conducted the final leg of the Pacific to Arizona Crustal Experiment (PACE). Two perpendicular models of the crust and upper mantle were fit to wide-angle reflection and refraction travel times, seismic amplitudes, and Bouguer gravity anomalies. The first profile crossed the Salton Trough from the southwest to the northeast, and the second was a strike line that paralleled the Salton Sea along its western edge. We found thin crust (∼21–22 km thick) beneath the axis of the Salton Trough (Imperial Valley) and locally thicker crust (∼27 km) beneath the Chocolate Mountains to the northeast. We modelled a slight thinning of the crust further to the northeast beneath the Colorado River (∼24 km) and subsequent thickening beneath the metamorphic core complex belt northeast of the Colorado River. There is a deep, apparently young basin (∼5–6 km unmetamorphosed sediments) beneath the Imperial Valley and a shallower (∼2–3 km) basin beneath the Colorado River. A regional 6.9-km/s layer (between ∼15-km depth and the Moho) underlies the Salton Trough as well as the Chocolate Mountains where it pinches out at the Moho. This lower crustal layer is spatially associated with a low-velocity (7.6–7.7 km/s) upper mantle. We found that our crustal model is locally compatible with the previously suggested notion that the crust of the Salton Trough has formed almost entirely from magmatism in the lower crust and sedimentation in the upper crust. However, we observe an apparently magmatically emplaced lower crust to the northeast, outside of the Salton Trough, and propose that this layer in part predates Salton Trough rifting. It may also in part result from migration of magmatic spreading centers associated with the southern San Andreas fault system. These spreading centers may have existed east of their current locations in the past and may have influenced the lower crust and upper mantle to the east of the current Salton Trough.</span></p>","language":"English","publisher":"American Geophysical Union","doi":"10.1029/95TC02616","issn":"02787407","usgsCitation":"Parsons, T., and McCarthy, J., 1996, Crustal and upper mantle velocity structure of the Salton Trough, southeast California: Tectonics, v. 15, no. 2, p. 456-471, https://doi.org/10.1029/95TC02616.","productDescription":"16 p.","startPage":"456","endPage":"471","costCenters":[],"links":[{"id":227171,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"southeast California","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -116.22055370171185,\n              33.6645044265011\n            ],\n            [\n              -116.22055370171185,\n              32.7266371497649\n            ],\n            [\n              -114.50255964296149,\n              32.7266371497649\n            ],\n            [\n              -114.50255964296149,\n              33.6645044265011\n            ],\n            [\n              -116.22055370171185,\n              33.6645044265011\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","volume":"15","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059fcd9e4b0c8380cd4e475","contributors":{"authors":[{"text":"Parsons, T.","contributorId":48288,"corporation":false,"usgs":true,"family":"Parsons","given":"T.","email":"","affiliations":[],"preferred":false,"id":380254,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"McCarthy, J.","contributorId":50290,"corporation":false,"usgs":true,"family":"McCarthy","given":"J.","affiliations":[],"preferred":false,"id":380255,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70204855,"text":"70204855 - 1996 - Biomass patterns in seagrass meadows of the Laguna Madre, Texas","interactions":[],"lastModifiedDate":"2019-08-20T09:11:56","indexId":"70204855","displayToPublicDate":"1996-03-01T09:03:37","publicationYear":"1996","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1106,"text":"Bulletin of Marine Science","active":true,"publicationSubtype":{"id":10}},"title":"Biomass patterns in seagrass meadows of the Laguna Madre, Texas","docAbstract":"<p><span id=\"_mce_caret\" data-mce-bogus=\"1\" data-mce-type=\"format-caret\"><span>The Laguna Madre of Texas supports the most extensive seagrass meadows in the western Gulf of Mexico, In 1988 seagrasses covered 730 km</span><sup>2</sup><span>&nbsp;or about three-quarters of the embayment.&nbsp;</span><i>Halodule wrightii</i><span>&nbsp;dominated the entire upper laguna, and total biomass was quite uniform near 160 g˙m</span><sup>-2</sup><span>&nbsp;throughout. Four species shared dominance in the lower laguna. Where present mean biomass of&nbsp;</span><i>Thalassia testudinum</i><span>&nbsp;was 373 g˙m</span><sup>-2</sup><span>;&nbsp;</span><i>Syringodium filiforme</i><span>, 138 g˙m</span><sup>-2</sup><span>;&nbsp;</span><i>Halodule wrightii</i><span>, 78 g˙m</span><sup>-2</sup><span>; and&nbsp;</span><i>Halophila engelmannii</i><span>, 6 g˙m</span><sup>-2</sup><span>. Macroalgae were widespread, at 71 g˙m</span><sup>-2</sup><span>&nbsp;where present.&nbsp;</span><i>Halodule wrightii</i><span>&nbsp;was dominant and biomass was low on sand flats of the barrier island separating the laguna from the gulf.&nbsp;</span><i>Halophila engelmannii</i><span>&nbsp;was limited to the deep edges of meadows. Biomass &gt;300 g˙m</span><sup>-2</sup><span>&nbsp;was limited to one extensive&nbsp;</span><i>T. testudinum</i><span>&nbsp;meadow at the south end of the laguna at all vegetated depths and two small areas with&nbsp;</span><i>S. filiforme</i><span>&nbsp;dominant at intermediate depths. Laguna Madre was similar in biomass to the two regions of extensive development of seagrasses in the eastern gulf: the Big Bend region of Florida (Iverson and Bittaker, 1986) and Florida Bay (Iverson and Bittaker, 1986; Zieman, et al., 1989). The laguna differed from the eastern gulf sites in more turbid waters and much shallower maximum depths of occurrence of seagrasses (&lt;2 m compared to 8–11 m), higher contribution of&nbsp;</span><i>H. wrightii</i><span>&nbsp;to system-wide biomass (although&nbsp;</span><i>H. wrightii</i><span>'s share has rapidly diminished in Laguna Madre as it has been displaced by&nbsp;</span><i>S. filiforme</i><span>&nbsp;and&nbsp;</span><i>T. testudinum</i><span>&nbsp;[Quammen and Onuf, 1993]), and much higher macroalgal biomass (limited to the section of the lower laguna receiving agricultural inflows). Similarities in the environments of Laguna Madre and inner Florida Bay suggest that, if cover and biomass of&nbsp;</span><i>Thalassia</i><span>&nbsp;continue to increase, the laguna may become vulnerable to mass mortalities as are now occurring in Florida Bay.</span></span><br data-mce-bogus=\"1\"></p>","language":"English","publisher":"Ingenta","usgsCitation":"Onuf, C.P., 1996, Biomass patterns in seagrass meadows of the Laguna Madre, Texas: Bulletin of Marine Science, v. 58, no. 2, p. 404-420.","productDescription":"17 p.","startPage":"404","endPage":"420","costCenters":[{"id":455,"text":"National Wetlands Research Center","active":true,"usgs":true},{"id":17705,"text":"Wetland and Aquatic Research Center","active":true,"usgs":true}],"links":[{"id":366678,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":366677,"rank":1,"type":{"id":15,"text":"Index 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             27.068909095463365\n            ],\n            [\n              -97.3828125,\n              27.1618079465197\n            ],\n            [\n              -97.3663330078125,\n              27.293689224852407\n            ],\n            [\n              -97.3663330078125,\n              27.347373810080278\n            ],\n            [\n              -97.3004150390625,\n              27.503399176197842\n            ],\n            [\n              -97.22351074218749,\n              27.61540601339959\n            ],\n            [\n              -97.3004150390625,\n              27.6543381066919\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","volume":"58","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Onuf, Christopher P.","contributorId":55091,"corporation":false,"usgs":true,"family":"Onuf","given":"Christopher","email":"","middleInitial":"P.","affiliations":[{"id":455,"text":"National Wetlands Research Center","active":true,"usgs":true}],"preferred":true,"id":768758,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":52693,"text":"b1988J - 1996 - Mississippian stratigraphic framework of east-central California and southern Nevada with revision of Upper Devonian and Mississippian stratigraphic units in Inyo County, California","interactions":[{"subject":{"id":52693,"text":"b1988J - 1996 - Mississippian stratigraphic framework of east-central California and southern Nevada with revision of Upper Devonian and Mississippian stratigraphic units in Inyo County, California","indexId":"b1988J","publicationYear":"1996","noYear":false,"chapter":"J","title":"Mississippian stratigraphic framework of east-central California and southern Nevada with revision of Upper Devonian and Mississippian stratigraphic units in Inyo County, California"},"predicate":"IS_PART_OF","object":{"id":33239,"text":"b1988 - 1992 - Evolution of sedimentary basins: Eastern Great Basin","indexId":"b1988","publicationYear":"1992","noYear":false,"title":"Evolution of sedimentary basins: Eastern Great Basin"},"id":1}],"isPartOf":{"id":33239,"text":"b1988 - 1992 - Evolution of sedimentary basins: Eastern Great Basin","indexId":"b1988","publicationYear":"1992","noYear":false,"title":"Evolution of sedimentary basins: Eastern Great Basin"},"lastModifiedDate":"2020-05-26T13:48:44.832553","indexId":"b1988J","displayToPublicDate":"1996-03-01T00:00:00","publicationYear":"1996","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1988","chapter":"J","title":"Mississippian stratigraphic framework of east-central California and southern Nevada with revision of Upper Devonian and Mississippian stratigraphic units in Inyo County, California","docAbstract":"<p>No abstract available.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/b1988J","usgsCitation":"Stevens, C., Klingman, D.S., 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Calvin H.","contributorId":59848,"corporation":false,"usgs":true,"family":"Stevens","given":"Calvin H.","affiliations":[],"preferred":false,"id":245839,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Klingman, Darrell S.","contributorId":22422,"corporation":false,"usgs":true,"family":"Klingman","given":"Darrell","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":245837,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Sandberg, Charles A. sandberg@usgs.gov","contributorId":2362,"corporation":false,"usgs":true,"family":"Sandberg","given":"Charles","email":"sandberg@usgs.gov","middleInitial":"A.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":245836,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Stone, Paul 0000-0002-1439-0156 pastone@usgs.gov","orcid":"https://orcid.org/0000-0002-1439-0156","contributorId":273,"corporation":false,"usgs":true,"family":"Stone","given":"Paul","email":"pastone@usgs.gov","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":245834,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Belasky, Paul","contributorId":57930,"corporation":false,"usgs":true,"family":"Belasky","given":"Paul","email":"","affiliations":[],"preferred":false,"id":245838,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Poole, Forrest G. 0000-0001-8487-0799 bpoole@usgs.gov","orcid":"https://orcid.org/0000-0001-8487-0799","contributorId":1543,"corporation":false,"usgs":true,"family":"Poole","given":"Forrest","email":"bpoole@usgs.gov","middleInitial":"G.","affiliations":[{"id":171,"text":"Central Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":245835,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Snow, J. Kent","contributorId":64320,"corporation":false,"usgs":true,"family":"Snow","given":"J.","email":"","middleInitial":"Kent","affiliations":[],"preferred":false,"id":245840,"contributorType":{"id":1,"text":"Authors"},"rank":7}]}}
,{"id":70019357,"text":"70019357 - 1996 - Large-scale right-slip displacement on the East San Francisco Bay region fault system, California: Implications for location of late Miocene to Pliocene Pacific plate boundary","interactions":[],"lastModifiedDate":"2025-09-08T16:41:38.954701","indexId":"70019357","displayToPublicDate":"1996-02-01T00:00:00","publicationYear":"1996","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3524,"text":"Tectonics","active":true,"publicationSubtype":{"id":10}},"title":"Large-scale right-slip displacement on the East San Francisco Bay region fault system, California: Implications for location of late Miocene to Pliocene Pacific plate boundary","docAbstract":"<p><span>A belt of northwardly younging Neogene and Quaternary volcanic rocks and hydrothermal vein systems, together with a distinctive Cretaceous terrane of the Franciscan Complex (the Permanente terrane), exhibits about 160 to 170 km of cumulative dextral offset across faults of the East San Francisco Bay Region (ESFBR) fault system. The offset hydrothermal veins and volcanic rocks range in age from .01 Ma at the northwest end to about 17.6 Ma at the southeast end. In the fault block between the San Andreas and ESFBR fault systems, where volcanic rocks are scarce, hydrothermal vein system ages clearly indicate that the northward younging thermal overprint affected these rocks beginning about 18 Ma. The age progression of these volcanic rocks and hydrothermal vein systems is consistent with previously proposed models that relate northward propagation of the San Andreas transform to the opening of an asthenospheric window beneath the North American plate margin in the wake of subducting lithosphere. The similarity in the amount of offset of the Permanente terrane across the ESFBR fault system to that derived by restoring continuity in the northward younging age progression of volcanic rocks and hydrothermal veins suggests a model in which 80–110 km of offset are taken up 8 to 6 Ma on a fault aligned with the Bloomfield-Tolay-Franklin-Concord-Sunol-Calaveras faults. An additional 50–70 km of cumulative slip are taken up ≤ 6 Ma by the Rogers Creek-Hayward and Concord-Franklin-Sunol-Calaveras faults. An alternative model in which the Permanente terrane is offset about 80 km by pre-Miocene faults does not adequately restore the distribution of 8–12 Ma volcanic rocks and hydrothermal veins to a single northwardly younging age trend. If 80–110 km of slip was taken up by the ESFBR fault system between 8 and 6 Ma, dextral slip rates were 40–55 mm/yr. Such high rates might occur if the ESFBR fault system rather than the San Andreas fault acted as the transform margin at this time. Major transpression across the boundary between the Pacific and North American plates at about 3 to 5 Ma would have resulted in the transfer of significant slip back to the San Francisco Peninsula segment of the San Andreas fault. Since that time, the ESFBR fault system has continued to slip at rates of 11–14 mm/yr. If this interpretation is valid, the ESFBR fault system was the Pacific-North American plate boundary between 8 and 6 Ma, and this boundary has migrated both eastward and westward with time, in response to changing plate margin geometry and plate motions.</span></p>","language":"English","publisher":"American Geophysical Union","doi":"10.1029/95TC02347","issn":"02787407","usgsCitation":"McLaughlin, R.J., Sliter, W., Sorg, D.H., Russell, P., and Sarna-Wojcicki, A., 1996, Large-scale right-slip displacement on the East San Francisco Bay region fault system, California: Implications for location of late Miocene to Pliocene Pacific plate boundary: Tectonics, v. 15, no. 1, p. 1-18, https://doi.org/10.1029/95TC02347.","productDescription":"18 p.","startPage":"1","endPage":"18","costCenters":[],"links":[{"id":226291,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -123.79794127542314,\n              39.40207162437872\n            ],\n            [\n              -124.00613075935172,\n              39.0554561037807\n            ],\n            [\n              -120.82383801002884,\n              34.35878941185911\n            ],\n            [\n              -119.28366673890498,\n              34.374280481902375\n            ],\n            [\n              -122.39329133542982,\n              39.49485922243221\n            ],\n            [\n              -123.79794127542314,\n              39.40207162437872\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","volume":"15","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a449de4b0c8380cd66c65","contributors":{"authors":[{"text":"McLaughlin, R. J. 0000-0002-4390-2288","orcid":"https://orcid.org/0000-0002-4390-2288","contributorId":107271,"corporation":false,"usgs":true,"family":"McLaughlin","given":"R.","middleInitial":"J.","affiliations":[],"preferred":false,"id":382462,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Sliter, W.V.","contributorId":38997,"corporation":false,"usgs":true,"family":"Sliter","given":"W.V.","email":"","affiliations":[],"preferred":false,"id":382458,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Sorg, D. H.","contributorId":63380,"corporation":false,"usgs":true,"family":"Sorg","given":"D.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":382459,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Russell, P.C.","contributorId":102856,"corporation":false,"usgs":true,"family":"Russell","given":"P.C.","email":"","affiliations":[],"preferred":false,"id":382460,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Sarna-Wojcicki, A.M. 0000-0002-0244-9149","orcid":"https://orcid.org/0000-0002-0244-9149","contributorId":104022,"corporation":false,"usgs":true,"family":"Sarna-Wojcicki","given":"A.M.","affiliations":[],"preferred":false,"id":382461,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}}
,{"id":70208252,"text":"70208252 - 1996 - Organic geochemistry applied to environmental assessments of Prince William Sound, Alaska, after the Exxon Valdez oil spill—a review","interactions":[],"lastModifiedDate":"2020-01-31T13:36:55","indexId":"70208252","displayToPublicDate":"1996-01-31T13:31:27","publicationYear":"1996","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2958,"text":"Organic Geochemistry","active":true,"publicationSubtype":{"id":10}},"displayTitle":"Organic geochemistry applied to environmental assessments of Prince William Sound, Alaska, after the <i>Exxon Valdez</i> oil spill—a review","title":"Organic geochemistry applied to environmental assessments of Prince William Sound, Alaska, after the Exxon Valdez oil spill—a review","docAbstract":"<p>Organic geochemistry played a major role in the environmental assessments conducted following the<span>&nbsp;</span><i>Exxon Valdez</i><span>&nbsp;</span>oil spill, which occurred on March 24, 1989, and released about 258,000 bbls (41 million liters) of Alaska North Slope crude oil into Prince William Sound. Geochemical analyses of more than 15,000 sediment, tar, and biological samples and about 5000 water samples provide the largest database yet collected on oil-spill chemistry, and we review the results here. The marine environment of the Sound has a complex background of petrogenic, pyrogenic, and biogenic hydrocarbons from natural and anthropogenic sources. Geochemical evaluation of the fate and effects of the spilled oil required that this oil and its residues be distinguished from the background. A variety of molecular and isotopic techniques were employed to identify various hydrocarbon sources and to distinguish quantitatively among mixed sources in the samples. Although the specific criteria used to distinguish multiple sources in the region affected by the<span>&nbsp;</span><i>Exxon Valdez</i><span>&nbsp;</span>spill are not necessarily applicable to all spill situations, the principles that governed their selection are.</p><p>Distributions of polycyclic aromatic hydrocarbons (PAH) and dibenzothiophenes distinguish<span>&nbsp;</span><i>Exxon Valdez</i><span>&nbsp;</span>oil and its weathered residues from background hydrocarbons in benthic sediments. Ratios of<span>&nbsp;</span><span class=\"math\"><span id=\"MathJax-Element-1-Frame\" class=\"MathJax_SVG\" data-mathml=\"<math xmlns=&quot;http://www.w3.org/1998/Math/MathML&quot;><mtext>C</mtext><msub><mi></mi><mn>2</mn></msub><mtext>-dibenzothiophene</mtext><mtext>C</mtext><msub><mi></mi><mn>2</mn></msub><mtext>-phenanthrene</mtext></math>\"><span class=\"MJX_Assistive_MathML\">C<sub>2</sub>-dibenzothiopheneC<sub>2</sub>-phenanthrene</span></span></span><span>&nbsp;</span>and<span>&nbsp;</span><span class=\"math\"><span id=\"MathJax-Element-2-Frame\" class=\"MathJax_SVG\" data-mathml=\"<math xmlns=&quot;http://www.w3.org/1998/Math/MathML&quot;><mtext>C</mtext><msub><mi></mi><mn>3</mn></msub><mtext>-dibenzothiophene</mtext><mtext>C</mtext><msub><mi></mi><mn>3</mn></msub><mtext>-phenanthrene</mtext></math>\"><span class=\"MJX_Assistive_MathML\">C<sub>3</sub>-dibenzothiopheneC<sub>3</sub>-phenanthrene</span></span></span><span>&nbsp;</span>were particularly useful. Carbon isotopes and terpane distributions distinguished<span>&nbsp;</span><i>Exxon Valdez</i><span>&nbsp;</span>residues found on shorelines from tars from other sources. Diesel and diesel soot were identified by the absence of alkylated chrysenes and a narrow distribution of<span>&nbsp;</span><i>n</i>-alkanes, whereas pyrogenic products were distinguished by the dominance of 4- to 6-ring PAH over 2- to 3-ring PAH and by the dominance of non-alkylated over alkylated homologues of each PAH series. The presence of 18α(H)-oleanane in benthic sediments, coupled with its absence in<span>&nbsp;</span><i>Exxon Valdez</i><span>&nbsp;</span>oil and its residues, confirm another petrogenic source.</p><p>Results of geochemical studies suggest that the petrogenic component in the background of benthic sediments is derived from oil seeps in the eastern Gulf of Alaska. In 1990 and 1991,<span>&nbsp;</span><i>Exxon Valdez</i><span>&nbsp;</span>residues, generally forming a small increment to the pre-spill background, were found to be only sporadically distributed in some shallow, near shore sediments adjacent to shorelines that had been heavily oiled in 1989. In 1994, occurrences of<span>&nbsp;</span><i>Exxon Valdez</i><span>&nbsp;</span>tars on shoreline surfaces were rare, although residues could be found buried in shoreline sediments at some isolated locations along the spill path where they were protected from wave action. Spilled oil residues collected 16 months after the spill were degraded, on average, by nearly 50%. Shoreline residues from sources other than the spill were also identified and are widespread throughout the Sound. These residues include (1) geochemically distinct tars and oils imported from California oil fields to Alaska for fuel and construction purposes prior to the discovery of the Cook Inlet and North Slope oil fields, (2) diesel and diesel soot, and (3) more highly refined products.</p><p>Of the more than 2700 chemical analyses of biological samples of higher life forms (fish, birds, and mammals) about 150 (6%) indicate recognizable residues of<span>&nbsp;</span><i>Exxon Valdez</i><span>&nbsp;</span>oil, which were identified by their distribution of polycyclic aromatic hydrocarbons (PAH). Most of these samples (138) were collected in 1989 and most were associated with external surfaces or the gastrointestinal tract. Rarely do internal tissues or fluids contain recognizable fingerprints of spilled oil. This observation includes samples from marine mammals that were visibly oiled externally. Other hydrocarbon sources, including diesel and a non-petroleum artifact that occurs when concentrations of individual PAH are at or near their method detection limit, are also identified in biological samples.</p>","language":"English","publisher":"Elsevier","doi":"10.1016/0146-6380(96)00010-1","usgsCitation":"Bence, A., Kvenvolden, K.A., and Kennicutt, M., 1996, Organic geochemistry applied to environmental assessments of Prince William Sound, Alaska, after the Exxon Valdez oil spill—a review: Organic Geochemistry, v. 24, no. 1, p. 7-42, https://doi.org/10.1016/0146-6380(96)00010-1.","productDescription":"36 p.","startPage":"7","endPage":"42","costCenters":[{"id":520,"text":"Pacific Coastal and Marine Science Center","active":true,"usgs":true}],"links":[{"id":371827,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"South-central Alaska","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -161.1474609375,\n              56.511017504952136\n            ],\n            [\n              -158.73046875,\n              54.23955053156177\n            ],\n            [\n              -143.1298828125,\n              60.108670463036\n            ],\n            [\n              -150.205078125,\n              62.4107287530686\n            ],\n            [\n              -161.1474609375,\n              56.511017504952136\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","volume":"24","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Bence, A.E.","contributorId":101943,"corporation":false,"usgs":true,"family":"Bence","given":"A.E.","email":"","affiliations":[],"preferred":false,"id":781165,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Kvenvolden, Keith A. kkvenvolden@usgs.gov","contributorId":3384,"corporation":false,"usgs":true,"family":"Kvenvolden","given":"Keith","email":"kkvenvolden@usgs.gov","middleInitial":"A.","affiliations":[{"id":520,"text":"Pacific Coastal and Marine Science Center","active":true,"usgs":true}],"preferred":true,"id":781166,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Kennicutt, M.C. II","contributorId":67665,"corporation":false,"usgs":true,"family":"Kennicutt","given":"M.C.","suffix":"II","affiliations":[],"preferred":false,"id":781167,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
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