We analyzed the behavior of 3–4‐d‐old prolarval and 28–33‐d‐old metalarval American shad Alosa sapidissima in groups of 3–1,000 fish per 22‐L glass tank, to determine whether (1) previously described juvenile behavior patterns first develop in larvae, (2) group size or density alters the behavior of larvae, and (3) schooling or other forms of cohesive behavior develop in larvae to promote social interactions. Twelve discrete behaviors or modal action patterns (MAPS) oflarvae were observed at all group sizes; halfthese patterns are unique to larval stages. Conversely, larvae do not develop five previously described juvenile MAPS. Stereotyped metalarval feeding sequences were absent or poorly developed in prolarvae. Group size was directly related to duration of free swimming in water column (metalarvae only) and to frequencies of “proximity to another fish” (all larvae), “contact another fish” (all larvae), and “escape or flee” (all larvae). Age or larval stage significantly affected all swimming‐related activities and three feeding behaviors. Larvae foraged and fed independently of one another and used MAPs typical of other larval fishes (“fixate,” “sigmoid,” “lunge,” and “capture”). With one exception (a direct relationship between frequency of food capture and metalarval size), group size and individual size did not significantly affect larval feeding success. Neither schooling nor forms of behavior leading to coordinated group swimming were observed at either larval stage. Larval behavior differed from juvenile behavior in a way that suggests survival in riverine habitats is promoted by behavior that disperses larvae and enables them to function nonsocially.
","language":"English","publisher":"American Fisheries Society","doi":"10.1577/1548-8659(1992)121<0508:LASEOA>2.3.CO;2","usgsCitation":"Ross, R.M., and Backman, T.W., 1992, Larval American shad: Effects of age and group size on swimming and feeding behavior: Transactions of the American Fisheries Society, v. 121, no. 4, p. 508-516, https://doi.org/10.1577/1548-8659(1992)121<0508:LASEOA>2.3.CO;2.","productDescription":"9 p.","startPage":"508","endPage":"516","costCenters":[{"id":365,"text":"Leetown Science Center","active":true,"usgs":true}],"links":[{"id":129951,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"121","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1be4b07f02db6a8df7","contributors":{"authors":[{"text":"Ross, R. 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The mapped compilation reveals much warmer climate conditions on average than present in both terrestrial and marine environments, and indicates a northward shift of subpolar and boreal bioclimatic zones. The data also suggest that temperature and precipitation gradients were significantly different than those of the Holocene, with particularly efficient latitudinal and eastward transport of warm air masses.
The paleoenvironmental and paleoclimate trends through the last interglacial sensu lato (Isotopic Stage 5) are more difficult to assess because the chronostratigraphical framework is poorly constrained. Nevertheless, the data suggest important regionalism in the climatostratigraphical trends. In particular, the large amplitude climatic cyclicity that characterizes the last interglacial of Europe is barely observed elsewhere. Moreover, by the end of the last interglacial (Isotopic Substage 5a), conditions slightly cooler than present are recorded in western Europe, while relatively warm conditions, similar to today, apparently prevailed in circumpolar regions adjacent to the North Atlantic despite the onset of ice growth.
The last interglacial provides paleosynoptic situations, unlike those of the present, that may contribute to understanding interactions within the environmental system on a hemispheric scale. There is, however, an imperative need for uniformization of data sets and for more accurate chronological control on regional scales.
","language":"English","publisher":"Elsevier","doi":"10.1016/1040-6182(91)90038-P","usgsCitation":"Anderson, P., Borisova, O., de Beaulieu, J.#., De Vernal, A., Eiriksson, J., Funder, S., Gibbard, P., Hamilton, T.D., Harrison, S.P., Houmark- Nielsen, M., Huntley, B., Knudsen, K., Larsen, E., Maher, L., Matthews, J., Miller, G., Raukas, A., Reeh, N., Robertsson, A., Rutter, N., Schweger, C.E., Sejrup, H., Sher, A., Telka, A., Turner, C., Velichko, A., and Ward, B., 1991, Report of 1st discussion group: The last interglacial in high latitudes of the Northern Hemisphere: Terrestrial and marine evidence: Quaternary International, v. 10-12, p. 9-28, https://doi.org/10.1016/1040-6182(91)90038-P.","productDescription":"20 p.","startPage":"9","endPage":"28","costCenters":[],"links":[{"id":371802,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"10-12","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Anderson, P.","contributorId":102682,"corporation":false,"usgs":true,"family":"Anderson","given":"P.","affiliations":[],"preferred":false,"id":781064,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Borisova, O.","contributorId":222049,"corporation":false,"usgs":false,"family":"Borisova","given":"O.","affiliations":[],"preferred":false,"id":781065,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"de Beaulieu, J. #NAME?","contributorId":49567,"corporation":false,"usgs":true,"family":"de Beaulieu","given":"J.","email":"","middleInitial":"#NAME?","affiliations":[],"preferred":false,"id":781066,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"De Vernal, Anne","contributorId":42057,"corporation":false,"usgs":true,"family":"De Vernal","given":"Anne","email":"","affiliations":[],"preferred":false,"id":781067,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Eiriksson, J.","contributorId":222050,"corporation":false,"usgs":false,"family":"Eiriksson","given":"J.","email":"","affiliations":[],"preferred":false,"id":781068,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Funder, S.","contributorId":24243,"corporation":false,"usgs":true,"family":"Funder","given":"S.","affiliations":[],"preferred":false,"id":781069,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Gibbard, P.","contributorId":222051,"corporation":false,"usgs":false,"family":"Gibbard","given":"P.","affiliations":[],"preferred":false,"id":781070,"contributorType":{"id":1,"text":"Authors"},"rank":7},{"text":"Hamilton, T. D.","contributorId":36921,"corporation":false,"usgs":true,"family":"Hamilton","given":"T.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":781071,"contributorType":{"id":1,"text":"Authors"},"rank":8},{"text":"Harrison, S. P.","contributorId":78488,"corporation":false,"usgs":false,"family":"Harrison","given":"S.","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":781072,"contributorType":{"id":1,"text":"Authors"},"rank":9},{"text":"Houmark- Nielsen, M.","contributorId":222052,"corporation":false,"usgs":false,"family":"Houmark- Nielsen","given":"M.","email":"","affiliations":[],"preferred":false,"id":781073,"contributorType":{"id":1,"text":"Authors"},"rank":10},{"text":"Huntley, B.","contributorId":52754,"corporation":false,"usgs":true,"family":"Huntley","given":"B.","email":"","affiliations":[],"preferred":false,"id":781074,"contributorType":{"id":1,"text":"Authors"},"rank":11},{"text":"Knudsen, Karen","contributorId":222062,"corporation":false,"usgs":false,"family":"Knudsen","given":"Karen","affiliations":[{"id":17957,"text":"GEOTOP and Department of Earth & Planetary Sciences, McGill University, Montreal, Canada","active":true,"usgs":false}],"preferred":false,"id":781075,"contributorType":{"id":1,"text":"Authors"},"rank":12},{"text":"Larsen, E.A.","contributorId":222061,"corporation":false,"usgs":false,"family":"Larsen","given":"E.A.","email":"","affiliations":[],"preferred":false,"id":781076,"contributorType":{"id":1,"text":"Authors"},"rank":13},{"text":"Maher, L.J. 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E.","contributorId":63549,"corporation":false,"usgs":true,"family":"Schweger","given":"C.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":781084,"contributorType":{"id":1,"text":"Authors"},"rank":21},{"text":"Sejrup, H.P.","contributorId":16569,"corporation":false,"usgs":true,"family":"Sejrup","given":"H.P.","email":"","affiliations":[],"preferred":false,"id":781085,"contributorType":{"id":1,"text":"Authors"},"rank":22},{"text":"Sher, A.","contributorId":222055,"corporation":false,"usgs":false,"family":"Sher","given":"A.","email":"","affiliations":[],"preferred":false,"id":781086,"contributorType":{"id":1,"text":"Authors"},"rank":23},{"text":"Telka, A.","contributorId":53668,"corporation":false,"usgs":true,"family":"Telka","given":"A.","email":"","affiliations":[],"preferred":false,"id":781087,"contributorType":{"id":1,"text":"Authors"},"rank":24},{"text":"Turner, Charles","contributorId":222064,"corporation":false,"usgs":false,"family":"Turner","given":"Charles","email":"","affiliations":[{"id":17957,"text":"GEOTOP and Department of Earth & Planetary Sciences, McGill University, Montreal, Canada","active":true,"usgs":false}],"preferred":false,"id":781088,"contributorType":{"id":1,"text":"Authors"},"rank":25},{"text":"Velichko, A.A.","contributorId":40079,"corporation":false,"usgs":true,"family":"Velichko","given":"A.A.","email":"","affiliations":[],"preferred":false,"id":781089,"contributorType":{"id":1,"text":"Authors"},"rank":26},{"text":"Ward, B.","contributorId":222056,"corporation":false,"usgs":false,"family":"Ward","given":"B.","email":"","affiliations":[],"preferred":false,"id":781090,"contributorType":{"id":1,"text":"Authors"},"rank":27}]}} ,{"id":70016348,"text":"70016348 - 1991 - The library as a reference tool: online catalogs","interactions":[],"lastModifiedDate":"2018-02-07T19:07:52","indexId":"70016348","displayToPublicDate":"1991-01-01T00:00:00","publicationYear":"1991","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3550,"text":"The Compass: Earth Science Journal of Sigma Gamma Epsilon","printIssn":"0894-802X","active":true,"publicationSubtype":{"id":10}},"title":"The library as a reference tool: online catalogs","docAbstract":"Online catalogs are computerized listings of materials in a particular library or group of libraries. General characteristics of online catalogs include ability for searching interactively and for locating descriptions of books, maps, and reports on regional or topical geology. Suggestions for searching, evaluating results, modifying searches, and limitations of searching are presented. -Author","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Compass of Sigma Gamma Epsilon","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","usgsCitation":"Stark, M., 1991, The library as a reference tool: online catalogs: The Compass: Earth Science Journal of Sigma Gamma Epsilon, v. 68, no. 2, p. 81-86.","startPage":"81","endPage":"86","numberOfPages":"6","costCenters":[],"links":[{"id":223158,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"68","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bad8de4b08c986b323cb7","contributors":{"authors":[{"text":"Stark, M.","contributorId":105055,"corporation":false,"usgs":true,"family":"Stark","given":"M.","email":"","affiliations":[],"preferred":false,"id":373239,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70015077,"text":"70015077 - 1991 - Louisiana coastal GIS network: Graphical user interface for access to spatial data","interactions":[],"lastModifiedDate":"2017-09-06T14:48:50","indexId":"70015077","displayToPublicDate":"1991-01-01T00:00:00","publicationYear":"1991","noYear":false,"publicationType":{"id":24,"text":"Conference Paper"},"publicationSubtype":{"id":19,"text":"Conference Paper"},"title":"Louisiana coastal GIS network: Graphical user interface for access to spatial data","docAbstract":"Louisiana's coastal wetlands support a large percentage of the nation's seafood and fur industries, vast deposits of oil and natural gas, habitat for thousands of species of plants and animals, winter nesting grounds and migratory paths for numerous waterfowl, and many recreational resources enjoyed by residents and tourists. Louisiana's wetlands also have the highest rates of coastal erosion and wetland loss in the nation. While numerous studies across many disciplines have been conducted on both local and regional scales, no complete inventory exists for this information. The Louisiana Coastal Geographic Information System Network (LCGISN) is currently being developed to facilitate access to existing data for coastal zone planners, managers, and researchers. The Louisiana Geological Survey (LGS), in cooperation with the LSU Department of Geography and Anthropology, the Computer Aided Design and Geographic Information Systems Research Laboratory (CADGIS), and others, is pursuing this project under the terms of a cooperative agreement with the U.S. Geological Survey. LCGISN is an automated system for searching and retrieving geographic, cartographic, and bibliographic data. By linking original programming with an existing GIS software package and an industry standard relational database management system, LCGISN will provide the capability for users to search for data references by interactively defining the area of interest on a displayed map/image reference background. Several agencies will be networked to provide easy access to a wide variety of information. LCGISN, with its headquarters at LGS, will serve as the central node on the network, providing data format conversions, projection and datum transformations, and storage of several of the most commonly used data sets. Thematic mapper data, USGS 7.5-minute quadrangle map boundaries, political and legal boundaries, major transportation routes, and other digital data will provide a base map to aid the user in selecting the exact area of interest. Then, the user will set search criteria by proceeding through a series of menu-driven options. The system will then return any or all of the following: a list of digital maps or imagery that can be displayed immediately and visually overlayed, a list of maps/remotely sensed data and information on their availability, and a list of bibliographic references concerning the area and subject defined.","largerWorkTitle":"GIS/LIS 1991 Proceedings","conferenceTitle":"Proceedings of GIS/LIS '91","conferenceDate":"28 October 1991 through 1 November 1991","conferenceLocation":"Atlanta, GA, USA","language":"English","publisher":"Publ by ASPRS","publisherLocation":"Bethesda, MD, United States","isbn":"0944426751","usgsCitation":"Hiland, M., McBride, R., Davis, D., Braud, D., Streiffer, H., Jones, F., Lewis, A., and Williams, S., 1991, Louisiana coastal GIS network: Graphical user interface for access to spatial data, in GIS/LIS 1991 Proceedings, v. 2, Atlanta, GA, USA, 28 October 1991 through 1 November 1991, p. 845-856.","productDescription":"12 p.","startPage":"845","endPage":"856","costCenters":[{"id":678,"text":"Woods Hole Coastal and Marine Science Center","active":true,"usgs":true}],"links":[{"id":223579,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -91.4501953125,\n 29.03215782622282\n ],\n [\n -88.39599609375,\n 29.03215782622282\n ],\n [\n -88.39599609375,\n 30.453409130203596\n ],\n [\n -91.4501953125,\n 30.453409130203596\n ],\n [\n -91.4501953125,\n 29.03215782622282\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a49ece4b0c8380cd689ba","contributors":{"authors":[{"text":"Hiland, Matteson","contributorId":101390,"corporation":false,"usgs":true,"family":"Hiland","given":"Matteson","email":"","affiliations":[],"preferred":false,"id":370004,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"McBride, Randolph A.","contributorId":48711,"corporation":false,"usgs":false,"family":"McBride","given":"Randolph A.","affiliations":[{"id":5115,"text":"Louisiana State University","active":true,"usgs":false}],"preferred":false,"id":370000,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Davis, Donald","contributorId":90471,"corporation":false,"usgs":true,"family":"Davis","given":"Donald","affiliations":[],"preferred":false,"id":370003,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Braud, Dewitt","contributorId":66853,"corporation":false,"usgs":true,"family":"Braud","given":"Dewitt","affiliations":[],"preferred":false,"id":370001,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Streiffer, Henry","contributorId":105057,"corporation":false,"usgs":true,"family":"Streiffer","given":"Henry","email":"","affiliations":[],"preferred":false,"id":370005,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Jones, Farrell","contributorId":105860,"corporation":false,"usgs":true,"family":"Jones","given":"Farrell","affiliations":[],"preferred":false,"id":370006,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Lewis, Anthony","contributorId":67221,"corporation":false,"usgs":true,"family":"Lewis","given":"Anthony","affiliations":[],"preferred":false,"id":370002,"contributorType":{"id":1,"text":"Authors"},"rank":7},{"text":"Williams, S.","contributorId":18514,"corporation":false,"usgs":true,"family":"Williams","given":"S.","email":"","affiliations":[],"preferred":false,"id":369999,"contributorType":{"id":1,"text":"Authors"},"rank":8}]}} ,{"id":70015076,"text":"70015076 - 1991 - Importance of hydrologic data for interpreting wetland maps and assessing wetland loss and mitigation","interactions":[],"lastModifiedDate":"2012-03-12T17:18:59","indexId":"70015076","displayToPublicDate":"1991-01-01T00:00:00","publicationYear":"1991","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1022,"text":"Biological Report - US Fish & Wildlife Service","active":true,"publicationSubtype":{"id":10}},"title":"Importance of hydrologic data for interpreting wetland maps and assessing wetland loss and mitigation","docAbstract":"The US Geological Survey collects and disseminates, in written and digital formats, groundwater and surface-water information related to the tidal and nontidal wetlands of the United States. This information includes quantity, quality, and availability of groundwater and surface water; groundwater and surface-water interactions (recharge-discharge); groundwater flow; and the basic surface-water characteristics of streams, rivers, lakes, and wetlands. Water resources information in digital format can be used in geographic information systems (GISs) for many purposes related to wetlands. US Geological Survey wetland-related activities include collection of information important for assessing and mitigating coastal wetland loss and modification, hydrologic data collection and interpretation, GIS activities, identification of national trends in water quality and quantity, and process-oriented wetland research. -Author","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Biological Report - US Fish & Wildlife Service","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","usgsCitation":"Carter, V., 1991, Importance of hydrologic data for interpreting wetland maps and assessing wetland loss and mitigation: Biological Report - US Fish & Wildlife Service, v. 90, no. 18, p. 79-85.","startPage":"79","endPage":"85","numberOfPages":"7","costCenters":[],"links":[{"id":224403,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"90","issue":"18","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a393be4b0c8380cd61856","contributors":{"authors":[{"text":"Carter, V.","contributorId":61115,"corporation":false,"usgs":true,"family":"Carter","given":"V.","email":"","affiliations":[],"preferred":false,"id":369998,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70015988,"text":"70015988 - 1990 - Bowers Swell: Evidence for a zone of compressive deformation concentric with Bowers Ridge, Bering Sea","interactions":[],"lastModifiedDate":"2013-03-01T15:24:31","indexId":"70015988","displayToPublicDate":"1990-01-01T00:00:00","publicationYear":"1990","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2682,"text":"Marine and Petroleum Geology","active":true,"publicationSubtype":{"id":10}},"title":"Bowers Swell: Evidence for a zone of compressive deformation concentric with Bowers Ridge, Bering Sea","docAbstract":"Bowers Swell is a newly discovered bathymetric feature which is up to 90 m high, between 12 and 20 km wide, and which extends arcuately about 400 km along the northern and eastern sides of Bowers Ridge. The swell was first revealed on GLORIA sonographs and subsequently mapped on seismic reflection and 3.5 kHz bathymetric profiles. These geophysical data show that the swell caps an arcuate anticlinal ridge, which is composed of deformed strata in an ancient trench on the northern and eastern sides of Bowers Ridge. The trench fill beneath the swell is actively deforming, as shown by faulting of the sea floor and by thinning of the strata across the crest of the swell. Thinning and faulting of the trench strata preclude an origin for the swell by simple sediment draping over an older basement high. We considered several models for the origin of Bowers Swell, including folding and uplift of the underlying trench sediment during the interaction between the Pacific plate beneath the Aleutian Ridge and a remnant oceanic slab beneath Bowers Ridge. However, such plate motions should generate extensive seismicity beneath Bowers Ridge, which is aseismic, and refraction data do not show any remnant slab beneath Bowers Ridge. Another origin considered for Bowers Swell invokes sediment deformation resulting from differential loading and diapirism in the trench fill. However, diapirism is not evident on seismic reflection profiles across the swell. We favour a model in which sediment deformation and swell formation resulted from a few tens of kilometers of low seismicity motion by intraplate crustal blocks beneath the Aleutian Basin. This motion may result from the translation of blocks in western Alaska to the south-west, forcing the movement of the Bering Sea margin west of Alaska into the abyssal Aleutian Basin. ?? 1990.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Marine and Petroleum Geology","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisher":"Elsevier","doi":"10.1016/0264-8172(90)90017-B","issn":"02648172","usgsCitation":"Marlow, M.S., Cooper, A.K., Dadisman, S.V., Geist, E., and Carlson, P., 1990, Bowers Swell: Evidence for a zone of compressive deformation concentric with Bowers Ridge, Bering Sea: Marine and Petroleum Geology, v. 7, no. 4, p. 398-409, https://doi.org/10.1016/0264-8172(90)90017-B.","startPage":"398","endPage":"409","numberOfPages":"12","costCenters":[],"links":[{"id":222933,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":268646,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1016/0264-8172(90)90017-B"}],"volume":"7","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059f248e4b0c8380cd4b0d1","contributors":{"authors":[{"text":"Marlow, M. S.","contributorId":76743,"corporation":false,"usgs":true,"family":"Marlow","given":"M.","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":372264,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Cooper, A. K.","contributorId":50149,"corporation":false,"usgs":true,"family":"Cooper","given":"A.","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":372262,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Dadisman, S. V.","contributorId":98735,"corporation":false,"usgs":true,"family":"Dadisman","given":"S.","middleInitial":"V.","affiliations":[],"preferred":false,"id":372266,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Geist, E.L. 0000-0003-0611-1150","orcid":"https://orcid.org/0000-0003-0611-1150","contributorId":71993,"corporation":false,"usgs":true,"family":"Geist","given":"E.L.","affiliations":[],"preferred":false,"id":372263,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Carlson, P.R.","contributorId":97055,"corporation":false,"usgs":true,"family":"Carlson","given":"P.R.","email":"","affiliations":[],"preferred":false,"id":372265,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":39648,"text":"pp1403I - 1989 - Geochemistry of the Floridan aquifer system in Florida and in parts of Georgia, South Carolina, and Alabama","interactions":[],"lastModifiedDate":"2025-04-17T18:52:27.70877","indexId":"pp1403I","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1989","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":"1403","chapter":"I","title":"Geochemistry of the Floridan aquifer system in Florida and in parts of Georgia, South Carolina, and Alabama","docAbstract":"The chemical quality of the ground water in the Floridan aquifer system is determined primarily by mineral-water interaction. However, some changes in water quality have been imposed by development, particularly near coastal pumping centers. A total of 601 chemical analyses, all from different wells, most completed in the upper part of the aquifer system, were used to describe the variations in water chemistry and to study the processes responsible for observed changes. \r\n\r\nThe Floridan aquifer system is a vertically continuous sequence of Tertiary carbonate rocks that are of generally high permeability and are hydraulically connected in varying degrees. The rocks are principally limestone and dolomite, but they grade into limy sands and clays near the aquifer system's updip limits. Major minerals in the aquifer system are calcite, dolomite, and, locally, gypsum or quartz; minor minerals include apatite, glauconite, and clay minerals such as kaolinite and montmorillonite. Trace amounts of metallic oxides or sulfides are present in some areas. \r\n\r\nThe aquifer system consists of the Upper and Lower Floridan aquifers, separated in most places by a less permeable confining unit that has highly variable hydraulic properties. Only the Upper Floridan aquifer is present throughout the study area. Freshwater enters the aquifer system in outcrop areas located primarily in central Georgia and north-central Florida. Discharge occurs chiefly to streams and springs and, to a lesser extent, directly into the sea. Most of the flow into and out of the system takes place where it is unconfined or where the upper confining unit is thin. Secondary permeability developed by dissolution of aquifer material is most prominent in these areas of dynamic flow. \r\n\r\nDissolved-solids concentrations in water from the Upper Floridan aquifer generally range from less than 25 milligrams per liter near outcrops to more than 25,000 milligrams per liter along the coasts. The dominant cations in the ground water are Ca2+, Mg2+, and Na+; the dominant anions are HCO3-, Cl-, and SO42-, The concentration of Ca2+ is controlled primarily by calcite saturation. Concentrations of Mg2+, NA+, and Cl- are highest where mixing of freshwater and saltwater occurs. Concentrations of HCO3- reflect the control of calcite solubility. The concentration of SO42- is highest where gypsiferous rock units are present in the aquifer system. \r\n\r\nThe major geochemical processes that occur in the Upper Floridan aquifer, based on water-quality maps and computations using a geochemical model, are (1) dissolution of aquifer minerals toward equilibrium, (2) mixing of ground water with recharge, leakage, or seawater, (3) sulfate reduction, and (4) cation exchange between water and aquifer minerals. \r\n\r\nSimilar processes apparently control minor dissolved constituents, although quantification is difficult with the available data. Statistical tests of available nutrient data indicate that concentrations of N (nitrogen) species in unconfined recharge areas may be increasing over time; more detailed studies of all N species are needed to test this hypothesis, however. Data on trace metals, radionuclides, and man-made organic contaminants are limited. Available data indicate that most freshwater within the Upper Floridan is potable, but detection of pesticides in a few samples indicates that the system is susceptible to contamination from the land surface in some areas, particularly where its upper confining unit is thin or absent. \r\n\r\nGeochemical models were used to examine changes in major chemical elements along selected ground-water paths within the Upper Floridan aquifer. Water in the Upper Floridan aquifer can be categorized into four hydrochemical facies, whose exact distribution is determined by confined or unconfined conditions of the aquifer and by chloride concentrations. The reaction models are considered plausible based on available chemical, isotopic, and hydrologic information, and they","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/pp1403I","usgsCitation":"Geochemistry of the Floridan aquifer system in Florida and in parts of Georgia, South Carolina, and Alabama; 1989; PP; 1403-I; Sprinkle, Craig L.","productDescription":"Report: 105 p.; 9 Plates: 21.00 x 26.30 inches or smaller; Database","numberOfPages":"105","costCenters":[{"id":27821,"text":"Caribbean-Florida Water Science Center","active":true,"usgs":true}],"links":[{"id":119386,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/1403i/coverthb.jpg"},{"id":67334,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/1403i/report.pdf","text":"Report","size":"21.6 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U.S. Geological Survey
3321 College Avenue
Davie, FL 33314
The changes in water levels in the High Plains aquifer from the nonirrigation season 1986-87 through the nonirrigation season 1987-88 and from the nonirrigation season 1979-80 through the nonirrigation season 1987-88 are presented in maps for the entire High Plains aquifer area. Water level changes are caused by interacting changes in precipitation, land use, and annual pumpage. Water levels declined from conditions prior to development until 1980 through parts of the High Plains of Nebraska, Colorado, New Mexico, Oklahoma, and Texas. From 1980 through 1987 water level changes were mixed, with declines of more than 10 ft in the highly developed areas of Kansas, New Mexico, Oklahoma, and Texas and relatively stable to rising water tables throughout the remaining aquifer area. The net change was a rise of 0.8 ft. The 1981-87 period was generally wetter than normal and pumping for irrigated agriculture was therefore reduced. Water level changes were mixed during 1987. Declines continued in some highly developed areas, but water levels generally rose throughout most of the aquifer. The average area-weighted change was a rise of 0.28 ft. This rise was due to the generally greater than normal precipitation, decreased acreage under irrigation, and decreased pumpage for those areas irrigated. At the end of the growing season, the drought in the Midwest in 1988 affected only limited areas of the High Plains. The effects of the drought on water levels can not be assessed until the water-level measurements for the nonirrigation season of 1988-89 are compiled.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri894073","usgsCitation":"Kastner, W.M., Schild, D.E., and Spahr, D.S., 1989, Water-level changes in the High Plains aquifer underlying parts of South Dakota, Wyoming, Nebraska, Colorado, Kansas, New Mexico, Oklahoma, and Texas: Predevelopment through nonirrigation season 1987-88: U.S. Geological Survey Water-Resources Investigations Report 89-4073, vi, 61 p., https://doi.org/10.3133/wri894073.","productDescription":"vi, 61 p.","costCenters":[],"links":[{"id":403084,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_47183.htm","linkFileType":{"id":5,"text":"html"}},{"id":56794,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1989/4073/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":123167,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1989/4073/report-thumb.jpg"}],"country":"United States","state":"Colorado, Kansas, Nebraska, New Mexico, Oklahoma, South Dakota, Texas, Wyoming","otherGeospatial":"High Plains aquifer","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -105.5,\n 32\n ],\n [\n -97,\n 32\n ],\n [\n -97,\n 43.5\n ],\n [\n -105.5,\n 43.5\n ],\n [\n -105.5,\n 32\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e6e4b07f02db5e75a6","contributors":{"authors":[{"text":"Kastner, W. M.","contributorId":67921,"corporation":false,"usgs":true,"family":"Kastner","given":"W.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":198999,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Schild, D. E.","contributorId":77559,"corporation":false,"usgs":true,"family":"Schild","given":"D.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":199000,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Spahr, D. S.","contributorId":88783,"corporation":false,"usgs":true,"family":"Spahr","given":"D.","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":199001,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70015697,"text":"70015697 - 1989 - Accounting for intracell flow in models with emphasis on water table recharge and stream-aquifer interaction: 2. A procedure","interactions":[],"lastModifiedDate":"2018-02-21T13:13:30","indexId":"70015697","displayToPublicDate":"1989-01-01T00:00:00","publicationYear":"1989","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3722,"text":"Water Resources Research","onlineIssn":"1944-7973","printIssn":"0043-1397","active":true,"publicationSubtype":{"id":10}},"title":"Accounting for intracell flow in models with emphasis on water table recharge and stream-aquifer interaction: 2. A procedure","docAbstract":"Intercepted intracell flow, especially if cell includes water table recharge and a stream ((sink), can result in significant model error if not accounted for. A procedure utilizing net flow per cell (Fn) that accounts for intercepted intracell flow can be used for both steady state and transient simulations. Germane to the procedure is the determination of the ratio of area of influence of the interior sink to the area of the cell (Ai/Ac). Ai is the area in which water table recharge has the potential to be intercepted by the sink. Determining Ai/Ac requires either a detailed water table map or observation of stream conditions within the cell. A proportioning parameter M, which is equal to 1 or slightly less and is a function of cell geometry, is used to determine how much of the water that has potential for interception is intercepted by the sink within the cell. Also germane to the procedure is the determination of the flow across the streambed (Fs), which is not directly a function of cell size, due to difference in head between the water level in the stream and the potentiometric surface of the aquifer underlying the streambed. The use of Fn for steady state simulations allows simulation of water levels without utilizing head-dependent or constant head boundary conditions which tend to constrain the model-calculated water levels, an undesirable result if a comparison of measured and calculated water levels is being made. Transient simulations of streams usually utilize a head-dependent boundary condition and a leakance value to model a stream. Leakance values for each model cell can be determined from a steady state simulation, which used the net flow per cell procedure. For transient simulation, Fn would not include Fs. Also, for transient simulation it is necessary to check Fn at different time intervals because M and Ai/Ac are not constant and change with time. The procedure was used successfully in two different models of the aquifer system in the Ozarks. The use of Fn was essential to the two model studies because most model cells in both models contained water table recharge and multiple sinks.
","language":"English","publisher":"American Geophysical Union","doi":"10.1029/WR025i004p00677","usgsCitation":"Jorgensen, D.G., Signor, D.C., and Imes, J.L., 1989, Accounting for intracell flow in models with emphasis on water table recharge and stream-aquifer interaction: 2. A procedure: Water Resources Research, v. 25, no. 4, p. 677-684, https://doi.org/10.1029/WR025i004p00677.","productDescription":"8 p.","startPage":"677","endPage":"684","costCenters":[],"links":[{"id":224170,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"25","issue":"4","noUsgsAuthors":false,"publicationDate":"2010-07-09","publicationStatus":"PW","scienceBaseUri":"5059e66ee4b0c8380cd47404","contributors":{"authors":[{"text":"Jorgensen, Donald G.","contributorId":19537,"corporation":false,"usgs":true,"family":"Jorgensen","given":"Donald","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":371549,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Signor, Donald C.","contributorId":13220,"corporation":false,"usgs":true,"family":"Signor","given":"Donald","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":371548,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Imes, Jeffrey L. jimes@usgs.gov","contributorId":2983,"corporation":false,"usgs":true,"family":"Imes","given":"Jeffrey","email":"jimes@usgs.gov","middleInitial":"L.","affiliations":[],"preferred":true,"id":371547,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70014779,"text":"70014779 - 1988 - Resonance of a fluid-driven crack: Radiation properties and implications for the source of long-period events and harmonic tremor","interactions":[],"lastModifiedDate":"2024-05-30T16:52:20.906978","indexId":"70014779","displayToPublicDate":"1988-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":6453,"text":"Journal of Geophysical Research Solid Earth","active":true,"publicationSubtype":{"id":10}},"title":"Resonance of a fluid-driven crack: Radiation properties and implications for the source of long-period events and harmonic tremor","docAbstract":"A dynamic source model is presented, in which a three-dimensional crack containing a viscous compressible fluid is excited into resonance by an impulsive pressure transient applied over a small area ΔS of the crack surface. The crack excitation depends critically on two dimensionless parameters called the crack stiffness, C = (b/μ)(L/d), and viscous damping loss, F = (12ηL)/(ρƒd2α), where b is the bulk modulus, η is the viscosity, ρƒ is the density of the fluid, μ is the rigidity, α is the compressional velocity of the solid, L is the crack length, and d is the crack thickness. The first parameter characterizes the ability of the crack to vibrate and shapes the spectral signature of the source, and the second quantifies the effect of fluid viscosity on the duration of resonance. Resonance is sustained by a very slow wave trapped in the fluid-filled crack. This guided wave, called the crack wave, is similar to the tube wave propagating in a fluid-filled borehole; it is inversely dispersive, showing a phase velocity that decreases with increasing wavelength, and its wave speed is always lower than the acoustic velocity of the fluid, decreasing rapidly as the crack stiffness increases. The source spectrum shows many sharp peaks characterizing the individual modes of vibration of the crack; the variation of spectral shape, both in the number and width of peaks, is surprisingly complex, reflecting the interference between the lateral and longitudinal modes of resonance, as well as nodes for these modes. The far-field spectrum is marked by narrow-band dominant and subdominant peaks that reflect the interaction of the various source modes. The frequency of the dominant spectral peak radiated by the source is independent of the radiation direction. The frequency, bandwidth, and spacing of the resonant peaks are strongly dependent on the crack stiffness, larger values of the stiffness factor shifting these peaks to lower frequencies and decreasing their bandwidth. The excitation of a particular mode depends on the position of the trigger and on the extent of the crack surface affected by the pressure transient. Fluid viscosity decreases the amplitudes of the main spectral peaks, smears out the finer structure of the spectrum, and greatly reduces the duration of the radiated signal. The energy loss by radiation is stronger for high frequencies, producing a seismic signature that is marked by a high-frequency content near the onset of the signal and dominated by a longer-period component of much longer duration in the signal coda. Such signature is in harmony with those displayed by long-period events observed on active volcanoes and in hydrofracture experiments. The very low velocity which is possible in a crack with high stiffness (C ≥ 100) also provides an attractive explanation for very long period tremor, such as type 2 tremor at Aso volcano, Japan, without the requirement of an unrealistically large magma container. The standing wave pattern set up on the crack surface by the sustained resonance in the fluid is observable in the near field of the crack, suggesting that the location and extent of the source may be estimated from the mapping of the pattern of nodes and antinodes seen in its vicinity. According to the model, the long-period event and harmonic tremor share the same source but differ in the boundary conditions for fluid flow and in the triggering mechanism setting up the resonance of the source, the former being viewed as the impulse response of the tremor generating system and the latter representing the excitation due to more complex forcing functions.
","language":"English","publisher":"American Geophysical Union","doi":"10.1029/JB093iB05p04375","issn":"01480227","usgsCitation":"Chouet, B., 1988, Resonance of a fluid-driven crack: Radiation properties and implications for the source of long-period events and harmonic tremor: Journal of Geophysical Research Solid Earth, v. 93, no. B5, p. 4375-4400, https://doi.org/10.1029/JB093iB05p04375.","productDescription":"26 p.","startPage":"4375","endPage":"4400","numberOfPages":"26","costCenters":[],"links":[{"id":225598,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"93","issue":"B5","noUsgsAuthors":false,"publicationDate":"2012-09-20","publicationStatus":"PW","scienceBaseUri":"505aa9dee4b0c8380cd86004","contributors":{"authors":[{"text":"Chouet, B.","contributorId":68465,"corporation":false,"usgs":true,"family":"Chouet","given":"B.","affiliations":[],"preferred":false,"id":369274,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":14600,"text":"ofr87676 - 1987 - An interactive program to display user-generated or file-based maps on a personal computer monitor","interactions":[],"lastModifiedDate":"2012-02-02T00:06:59","indexId":"ofr87676","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1987","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":"87-676","title":"An interactive program to display user-generated or file-based maps on a personal computer monitor","docAbstract":"PC MAP-MAKER is an ADVANCED BASIC program written to provide users of IBM XT, IBM AT, and compatible computers with a straight-forward, flexible method to display geographical data on a color or monochrome PC (personal computer) monitor. Data can be political boundaries such as State and county boundaries; natural curvilinear features such as rivers, drainage areas, and geological contacts; and points such as well locations and mineral localities. Essentially any point defined by a latitude and longitude and any line defined by a series of latitude and longitude values can be displayed using the program. PC MAP MAKER allows users to view tabular data from U.S. Geological Survey files such as WATSTORE (National Water Data Storage and Retrieval System) in a map format in a time much shorter than required by sending the data to a line plotter. The screen image can be saved to disk for recall at a later date, and hard copies can be printed with a dot matrix printer. The program is user-friendly, using menus or prompts to guide user input. It is fully documented and structured to allow the user to tailor the program to the user 's specific needs. The documentation includes a tutorial designed to introduce users to the capabilities of the program using the State of Colorado as a demonstration map area. (Author 's abstract)","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/ofr87676","usgsCitation":"Langer, W.H., and Stephens, R., 1987, An interactive program to display user-generated or file-based maps on a personal computer monitor: U.S. Geological Survey Open-File Report 87-676, iii, 69 p. :ill. ;28 cm.; 5.25 inch diskette, https://doi.org/10.3133/ofr87676.","productDescription":"iii, 69 p. :ill. ;28 cm.; 5.25 inch diskette","costCenters":[],"links":[{"id":148240,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1987/0676/report-thumb.jpg"},{"id":43263,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1987/0676/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad7e4b07f02db684474","contributors":{"authors":[{"text":"Langer, W. H.","contributorId":44932,"corporation":false,"usgs":true,"family":"Langer","given":"W.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":169717,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Stephens, R.W.","contributorId":83134,"corporation":false,"usgs":true,"family":"Stephens","given":"R.W.","email":"","affiliations":[],"preferred":false,"id":169718,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2311,"text":"wsp2234E - 1987 - Shore erosion as a sediment source to the tidal Potomac River, Maryland and Virginia","interactions":[],"lastModifiedDate":"2012-02-02T00:05:20","indexId":"wsp2234E","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1987","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2234","chapter":"E","title":"Shore erosion as a sediment source to the tidal Potomac River, Maryland and Virginia","docAbstract":"The shoreline of the tidal Potomac River attained its present form as a result of the Holocene episode of sea-level rise; the drowned margins of the system are modified by wave activity in the shore zone and by slope processes on banks steepened by basal-wave erosion. Shore erosion leaves residual sand and gravel in shallow water and transports silt and clay offshore to form a measurable component of the suspended-sediment load of the tidal Potomac River. \r\n\r\nErosion rates were measured by comparing digitized historical shoreline maps and modern maps, and by comparing stereopairs of aerial photographs taken at different points in time, with the aid of an interactive computer-graphics system and a digitizing stereoplotter. Cartographic comparisons encompassed 90 percent of the study reach and spanned periods of 38 to 109 years, with most measurements spanning at least 84 years. Photogrammetric comparisons encompassed 49 percent of the study reach and spanned 16 to 40 years. Field monitoring of erosion rates and processes at two sites, Swan Point Neck, Maryland, and Mason Neck, Virginia, spanned periods of 10 to 18 months. \r\n\r\n\r\nEstimated average recession rates of shoreline in the estuary, based on cartographic and photogrammetric measurements, were 0.42 to 0.52 meter per annum (Virginia shore) and 0.31 to 0.41 meter per annum (Maryland shore). Average recession rates of shoreline in the tidal river and transition zone were close to 0.15 meter per annum. Estimated average volume-erosion rates along the estuary were 1.20 to 1.87 cubic meters per meter of shoreline per annum (Virginia shore) and 0.56 to 0.73 cubic meter per meter of shoreline per annum (Maryland shore); estimated average volume-erosion rates along the shores of the tidal river and transition zone were 0.55 to 0.74 cubic meter per meter of shoreline per annum. \r\n\r\nEstimated total sediment contributed to the tidal Potomac River by shore erosion was 0.375 x 10 6 to 0.565 x 10 6 metric tons per annum; of this, the estimated amount of silt and clay ranged from 0.153x10 6 to 0.226x10 6 metric tons per annum. Between 49 and 60 percent of the sediment was derived from the Virginia shore of the estuary; 14 to 18 percent was derived from the Maryland shore of the estuary; and 23 to 36 percent was derived from the shores of the tidal river and transition zone. The adjusted modern estimate of sediment eroded from the shoreline of the estuary is about 55 percent of the historical estimate.\r\n\r\nSediment eroded from the shoreline accounted for about 6 to 9 percent of the estimated total suspended load for the tidal Potomac River during water years 1979 through 1981 and for about 11 to 18 percent of the suspended load delivered to the estuary during the same period. Annual suspended-sediment loads derived from upland source areas fluctuated by about an order of magnitude during the 3 years of record (1979-81); shore erosion may have been a more important component of the sediment budget during periods of low flow than during periods of higher discharges. Prior to massive land clearance during the historical period of intensive agriculture in the 18th and 19th centuries, annual sediment loads from upland sources probably were smaller than they are at present; under these circumstances shore erosion would have been an important component of the sediment budget. \r\n\r\nAt current rates of sediment supply, relative sea-level rise, and shoreline recession, the landward parts of the tidal Potomac River are rapidly being filled by sediment. If these rates were to remain constant over time, and no sediment were to escape into Chesapeake Bay, the tidal river and transition zone would be filled within 600 years, and the total system would be filled in less than 4,000 years. Given a slower rate of sediment supply, comparable to the measured rate during the low-flow 1981 water year, the volume of the tidal Potomac River might remain relatively stable or even increase over time. Changes in rates","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp2234E","usgsCitation":"Miller, A.J., 1987, Shore erosion as a sediment source to the tidal Potomac River, Maryland and Virginia: U.S. Geological Survey Water Supply Paper 2234, vi, 45 p. :ill., maps ;28 cm., https://doi.org/10.3133/wsp2234E.","productDescription":"vi, 45 p. :ill., maps ;28 cm.","costCenters":[],"links":[{"id":137736,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/2234e/report-thumb.jpg"},{"id":28141,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/2234e/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49fae4b07f02db5f3e42","contributors":{"authors":[{"text":"Miller, Andrew J.","contributorId":7559,"corporation":false,"usgs":true,"family":"Miller","given":"Andrew","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":144992,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70201411,"text":"70201411 - 1987 - I. Thermal evolution of Ganymede and implications for surface features. II. Magnetohydrodynamic constraints on deep zonal flow in the giant planets. III. A fast finite-element algorithm for two-dimensional photoclinometry","interactions":[],"lastModifiedDate":"2022-11-22T15:18:10.64313","indexId":"70201411","displayToPublicDate":"1987-01-09T14:46:20","publicationYear":"1987","noYear":false,"publicationType":{"id":21,"text":"Thesis"},"publicationSubtype":{"id":28,"text":"Thesis"},"title":"I. Thermal evolution of Ganymede and implications for surface features. II. Magnetohydrodynamic constraints on deep zonal flow in the giant planets. III. A fast finite-element algorithm for two-dimensional photoclinometry","docAbstract":"The work is divided into three independent papers:
PAPER I:
Thermal evolution models are presented for Ganymede, assuming a mostly differentiated initial state of a water ocean overlying a rock layer. The only heat sources are assumed to be primordial heat (provided by accretion) and the long-lived radiogenic heat sources in the rock component. As Ganymede cools, the ocean thins, and two ice layers develop, one above composed of ice I, and the other below composed of high-pressure polymorphs of ice. Subsolidus convection proceeds separately in each ice layer, its transport of heat calculated using a simple parameterized convection scheme and the most recent data on ice rheology. The model requires that the average entropy of the deep ice layer exceed that of the ice I layer. If the residual ocean separating these layers becomes thin enough, then a Rayleigh-Taylor-like (\"diapiric\") instability may ensue, driven by the greater entropy of the deeper ice and merging the two ice mantles into a single convective layer. This instability is not predicted by linear analysis but occurs for plausible finite amplitude perturbations associated with large Rayleigh number convection. The resulting warm ice diapirs may lead to a dramatic \"heat pulse\" at the surface and to fracturing of the lithosphere, and may be directly or indirectly responsible for resurfacing and grooved terrain formation on Ganymede. The timing of this event depends rather sensitively on poorly known rheological parameters but could be consistent with chronologies deduced from estimated cratering rates. Irrespective of the occurrence or importance of the heat pulse, we find that lithospheric fracturing requires rapid stress loading (on a timescale ≾ 104) years). Such a timescale can be realized by warm ice diapirism, but not directly by gradual global expansion. In the absence of any quantitative and self-consistent model for the resurfacing of Ganymede by liquid water, we favor resurfacing by warm ice flows,which we demonstrate to be physically possible, a plausible consequence of our models, compatible with existing observations, and a hypothesis testable by Galileo. We discuss core formation as an alternative driver for resurfacing, and conclude that it is less attractive. We also consider anew the puzzle of why Callisto differs so greatly from Ganymede, offering several possible explanations. The models presented do not provide a compelling explanation for all aspects of Ganymedean geological evolution, since we have identified several potential problems, most notably the apparently extended period of grooved terrain formation (several hundred million years), which is difficult to reconcile with the heat pulse phenomenon.
PAPER II:
The observed zonal flows of the giant planets will, if they penetrate below the visible atmosphere, interact significantly with the planetary magnetic field outside the metalized core. The appropriate measure of this interaction is the Chandrasekhar number Q = (H2)/(4πρνα2λ) (where H = radial component of the magnetic field, ν = eddy viscosity, λ = magnetic diffusivity, α-1 = lengthscale on which λ varies); at depths where Q ≳ 1 the velocity will be forced to oscillate on a small lengthscale or decay to zero. We estimate the conductivity due to semiconduction in H2 (Jupiter, Saturn) and ionization in H2O (Uranus, Neptune) as a function of depth; the value λ ≃ 1010 cm2s-1 needed for Q = 1 is readily obtained well outside the metallic core (where λ ≃ 102 cm2s-1).
These assertions are quantified by a simple model of the equatorial zonal jet in which the flow is assumed uniform on cylinders concentric with the spin axis, and the viscous and magnetic torques on each cylinder are balanced. We solve this \"Taylor constraint\" simultaneously with the dynamo equation to obtain the velocity and magnetic field in the equatorial plane. With this model we reproduce the widely differing jet widths of Jupiter and Saturn (though not the flow at very high or low latitudes) using ν = 2500 cm2s-1, consistent with the requirement that viscous dissipation not exceed the specific luminosity. A model Uranian jet consistent with the limited Voyager data can also be constructed, with appropriately smaller ν, but only if one assumes a two-layer interior. We tentatively predict a wide Neptunian jet.
For Saturn (but not Jupiter or Uranus) the model has a large magnetic Reynolds number where Q = 1 and hence exhibits substantial axisymmetrization of the field in the equatorial plane. This effect may or may not persist at higher latitudes. The one-dimensional model presented is only a first step. Variation of the velocity and magnetic field parallel to the spin axis must be modeled in order to answer several important questions, including: 1) What is the behavior of flows at high latitudes, whose Taylor cylinders are interrupted by the region with Q ≳ 1? 2) To what extent is differential rotation in the envelope responsible for the spin-axisymmetry of Saturn's magnetic field?
PAPER III:
It is shown that the problem of two-dimensional photoclinometry (PC) -- the reconstruction of a surface z(x,y) from a brightness image B(x,y) -- may be formulated in a natural way in terms of finite elements. The resulting system of equations is underdetermined as a consequence of the lack of boundary conditions for z, but a unique solution may be chosen by minimizing a function S expressing the \"roughness\" of the surface. An efficient PC algorithm based on this formulation is presented, requiring ~ 10.66 (four-byte) memory locations and ~104 floating multiplications/additions per pixel, and incorporating: 1) Minimization of the roughness by the penalty method, which yields the smallest set of equations. 2) Iterative solution of the nonlinear equations by Newton's method. 3) Solution of the linearized equations by an inner iterative cycle of successive over-relaxation, which takes advantage of the extreme sparseness of the system. 4) Multigridding, in which the solutions to the smaller problems obtained by reducing the resolution are used recursively to greatly speed convergence at the higher resolutions, and 5) A rapid noniterative initial estimate of z obtained by exploiting the special symmetry of the equations obtained in the first linearization.
The algorithm is extensively demonstrated on 200 by 200 pixel synthetic \"images\" generated from digital topographic data for northern Utah over a range of phase angles. Rms error in the solution is ~ 22 m, out of ~ 660 m total relief. The error is dominated by \"stripes\" with the same azimuth as the light source, resulting from use of the roughness criterion in lieu of boundary conditions; the rms error along profiles parallel to the stripes is only ~ 2-8 m, depending on the phase angle. Satisfactory solutions are obtained even in the presence of quantization error, noise, and moderate blur in the image.
Applications of the PC algorithm to both remote sensing and photomicrography are sketched; a photoclinometric map of a low-relief Precambrian era fossil is presented as an example of the latter. Prospects for dealing with photometrically inhomogeneous surfaces, and an extension of the method to the analysis of side-looking radar data (\"radarclinometry\") are also discussed.
","language":"English","publisher":"California Institute of Technology","publisherLocation":"Pasadena, California","doi":"10.7907/T5PT-S948","usgsCitation":"Kirk, R.L., 1987, I. Thermal evolution of Ganymede and implications for surface features. II. Magnetohydrodynamic constraints on deep zonal flow in the giant planets. III. A fast finite-element algorithm for two-dimensional photoclinometry, 272 p., https://doi.org/10.7907/T5PT-S948.","productDescription":"272 p.","costCenters":[{"id":131,"text":"Astrogeology Science Center","active":true,"usgs":true}],"links":[{"id":360219,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"otherGeospatial":"Ganymede","publicComments":"Submitted for a Doctorate degree in Philosophy.","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5c122c5de4b034bf6a856a40","contributors":{"authors":[{"text":"Kirk, Randolph L. 0000-0003-0842-9226 rkirk@usgs.gov","orcid":"https://orcid.org/0000-0003-0842-9226","contributorId":2765,"corporation":false,"usgs":true,"family":"Kirk","given":"Randolph","email":"rkirk@usgs.gov","middleInitial":"L.","affiliations":[{"id":131,"text":"Astrogeology Science Center","active":true,"usgs":true}],"preferred":true,"id":754064,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":29124,"text":"wri874015 - 1987 - Ground-water flow and shallow-aquifer properties in the Rio Grande inner valley south of Albuquerque, Bernalillo County, New Mexico","interactions":[],"lastModifiedDate":"2023-04-11T20:27:18.117104","indexId":"wri874015","displayToPublicDate":"1987-01-01T00:00:00","publicationYear":"1987","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":"87-4015","title":"Ground-water flow and shallow-aquifer properties in the Rio Grande inner valley south of Albuquerque, Bernalillo County, New Mexico","docAbstract":"The purpose of this investigation was to describe the water table configuration and its temporal variations, estimate aquifer properties, and evaluate the interaction of groundwater and surface water in the inner valley of the Rio Grande in southern Albuquerque, New Mexico, where groundwater contamination is a continuing concern. The upper 150 ft of sedimentary deposits in the inner valley, mostly alluvium that consists of cobbles, gravel, sand, silt, and clay, was emphasized because of its susceptibility to contamination. A map of the water table on February 28, 1986 shows that flow generally is parallel to the river and the gradient is approximately 5 ft/mi or 0.0001. In areas affected by municipal and industrial groundwater withdrawals, declines may exceed 10 ft, and the water table gradient is as much as 20 ft/mi or 0.004. The gradient also is steeper near drains, particularly during the irrigation season. In the area east of the community of Mountainview the direction of water movement may have reversed between 1936 and 1986; flow near appears to be toward the east or southeast. Groups of four piezometers, each screened at a different depth, were monitored to describe seasonal changes of the water table. Vertical gradients between piezometers ranged from 0.014 upward to 0.047 downward from July 1985 to June 1986, but were downward most of the year, particulary during the irrigation season. The horizontal hydraulic conductivity of a 15-ft-thick clay and silt bed beneath Rio Bravo Boulevard is estimated to be 0.0001 ft/day. The average interstitial velocity down through this bed is estimated to range from about 0.0002 to 0.0005 ft/day. The fluctuations of the water table at the piezometers nearest the Rio Grande do not appear to be affected by the riverside drain.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri874015","usgsCitation":"Peter, K.D., 1987, Ground-water flow and shallow-aquifer properties in the Rio Grande inner valley south of Albuquerque, Bernalillo County, New Mexico: U.S. Geological Survey Water-Resources Investigations Report 87-4015, iv, 29 p., https://doi.org/10.3133/wri874015.","productDescription":"iv, 29 p.","costCenters":[],"links":[{"id":57994,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1987/4015/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":123690,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1987/4015/report-thumb.jpg"},{"id":415599,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_46703.htm","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"New Mexico","county":"Bernalillo County","city":"Albuquerque","otherGeospatial":"Rio Grande Valley","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -106.5833,\n 35.095\n ],\n [\n -106.7292,\n 35.095\n ],\n [\n -106.7292,\n 34.9394\n ],\n [\n -106.5833,\n 34.9394\n ],\n [\n -106.5833,\n 35.095\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aafe4b07f02db66cd65","contributors":{"authors":[{"text":"Peter, K. D.","contributorId":94319,"corporation":false,"usgs":true,"family":"Peter","given":"K.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":200984,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70015523,"text":"70015523 - 1986 - Radarclinometry","interactions":[],"lastModifiedDate":"2012-03-12T17:19:00","indexId":"70015523","displayToPublicDate":"1986-01-01T00:00:00","publicationYear":"1986","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1429,"text":"Earth, Moon and Planets","active":true,"publicationSubtype":{"id":10}},"title":"Radarclinometry","docAbstract":"A mathematical theory and a corresponding algorithm have been developed to derive topographic maps from radar images as photometric arrays. Thus, as radargrammetry is to photogrammetry, so radarclinometry is to photoclinometry. Photoclinometry is endowed with a fundamental indeterminacy principle even for terrain homogeneous in normal albedo. This arises from the fact that the geometric locus of orientations of the local surface normal that is consistent with a given reflected specific-intensity of radiation is more complicated than a fixed line in space. For a radar image, the locus is a cone whose half-angle is the incidence angle and whose axis contains the radar. The indeterminacy is removed throughout a region if one possesses a control profile as a boundary-condition. In the absence of such ground-truth, a point-boundary-condition will suffice only in conjunction with a heuristic assumption, such as that the strike-line runs perpendicularly to the line-of-sight. In the present study I have implemented a more reasonable assumption which I call 'the hypothesis of local cylindricity'. Firstly, a general theory is derived, based solely on the implicit mathematical determinacy. This theory would be directly indicative of procedure if images were completely devoid of systematic error and noise. The theory produces topography by an area integration of radar brightness, starting from a control profile, without need of additional idealistic assumptions. But we have also theorized separately a method of forming this control profile, which method does require an additional assumption about the terrain. That assumption is that the curvature properties of the terrain are locally those of a cylinder of inferable orientation, within a second-order mathematical neighborhood of every point of the terrain. While local strike-and-dip completely determine the radar brightness itself, the terrain curvature determines the brightness-gradient in the radar image. Therefore, the control profile is formed as a line integration of brightness and its local gradient starting from a single point of the terrain where the local orientation of the strike-line is estimated by eye. Secondly, and independently, the calibration curve for pixel brightness versus incidence-angle is produced. I assume that an applicable curve can be found from the literature or elsewhere so that our problem is condensed to that of properly scaling the brightness-axis of the calibration curve. A first estimate is found by equating the average image brightness to the point on the brightness axis corresponding to the complement of the effective radar depression-angle, an angle assumed given. A statistical analysis is then used to correct, on the one hand, for the fact that the average brightness is not the brightness that corresponds to the average incidence angle, as a result of the non-linearity of the calibration curve; and on the other hand, we correct for the fact that the average incidence angle is not the same for a rough surface as it is for a flat surface (and therefore not the complement of the depression angle). Lastly, the practical modifications that were interactively evolved to produce an operational algorithm for treating real data are developed. They are by no means considered optimized at present. Such a possibility is thus far precluded by excessive computer-time. Most noteworthy in this respect is the abandonment of area integration away from a control profile. Instead, the topography is produced as a set of independent line integrations down each of the parallel range lines of the image, using the theory for control-profile formation. An adaptive technique, which now appears excessive, was also employed so that SEASAT images of sand dunes could be processed. In this, the radiometric calibration was iterated to force the endpoints of each profile to zero elevation. A secondary algorithm then employed line-averages of appropriate quantities to adjust the mean t","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Earth, Moon and Planets","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisherLocation":"Kluwer Academic Publishers","doi":"10.1007/BF00055161","issn":"01679295","usgsCitation":"Wildey, R., 1986, Radarclinometry: Earth, Moon and Planets, v. 36, no. 3, p. 217-247, https://doi.org/10.1007/BF00055161.","startPage":"217","endPage":"247","numberOfPages":"31","costCenters":[],"links":[{"id":205398,"rank":9999,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1007/BF00055161"},{"id":223668,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"36","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a938be4b0c8380cd80eb1","contributors":{"authors":[{"text":"Wildey, R.L.","contributorId":9700,"corporation":false,"usgs":true,"family":"Wildey","given":"R.L.","email":"","affiliations":[],"preferred":false,"id":371149,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70014546,"text":"70014546 - 1986 - A spherical electron-channelling pattern map for use in quartz petrofabric analysis","interactions":[],"lastModifiedDate":"2024-05-13T23:52:54.727182","indexId":"70014546","displayToPublicDate":"1986-01-01T00:00:00","publicationYear":"1986","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2468,"text":"Journal of Structural Geology","active":true,"publicationSubtype":{"id":10}},"title":"A spherical electron-channelling pattern map for use in quartz petrofabric analysis","docAbstract":"Electron channelling patterns (ECP's) are formed in the scanning electron microscope (SEM) by the interaction between the incident electrons and the lattice of crystalline specimens. The patterns are unique for a particular crystallographic orientation and are therefore of considerable potential in petrofabric studies provided they can be accurately indexed. Indexing requires an ECP-map of the crystallographic stereogram or unit triangle covering all possible orientations and hence ECP patterns. Due to the presence of long-range distortions in planar ECP-maps, it is more convenient to construct the maps over a spherical surface. This also facilitates the indexing of individual ECP's. A spherical ECP-map for quartz is presented together with an example of its use in petrofabric analysis.
Basaltic lava flows and high-silica rhyolite domes form the Pleistocene part of the Coso volcanic field in southeastern California. The distribution of vents maps the areal zonation inferred for the upper parts of the Coso magmatic system. Subalkalic basalts (<50% SiO2) were erupted well away from the rhyolite field at any given time. Compositional variation among these basalts can be ascribed to crystal fractionation. Erupted volumes of these basalts decrease with increasing differentiation. Mafic lavas containing up to 58% SiO2, erupted adjacent to the rhyolite field, formed by mixing of basaltic and silicic magma. Basaltic magma interacted with crustal rocks to form other SiO2-rich mafic lavas erupted near the Sierra Nevada fault zone.
Several rhyolite domes in the Coso volcanic field contain sparse andesitic inclusions (55–61% SiO2). Pillow-like forms, intricate commingling and local diffusive mixing of andesite and rhyolite at contacts, concentric vesicle distribution, and crystal morphologies indicative of undercooling show that inclusions were incorporated in their rhyolitic hosts as blobs of magma. Inclusions were probably dispersed throughout small volumes of rhyolitic magma by convective (mechanical) mixing. Inclusion magma was formed by mixing (hybridization) at the interface between basaltic and rhyolitic magmas that coexisted in vertically zoned igneous systems. Relict phenocrysts and the bulk compositions of inclusions suggest that silicic endmembers were less differentiated than erupted high-silica rhyolite. Changes in inferred endmembers of magma mixtures with time suggest that the steepness of chemical gradients near the silicic/mafic interface in the zoned reservoir may have decreased as the system matured, although a high-silica rhyolitic cap persisted.
The Coso example is an extreme case of large thermal and compositional contrast between inclusion and host magmas; lesser differences between intermediate composition magmas and inclusions lead to undercooling phenomena that suggest smaller ΔT. Vertical compositional zonation in magma chambers has been documented through study of products of voluminous pyroclastic eruptions. Magmatic inclusions in volcanic rocks provide evidence for compositional zonation and mixing processes in igneous systems when only lava is erupted.
","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Contributions to Mineralogy and Petrology","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisherLocation":"Springer-Verlag","doi":"10.1007/BF01150292","issn":"00107999","usgsCitation":"Bacon, C., and Metz, J., 1984, Magmatic inclusions in rhyolites, contaminated basalts, and compositional zonation beneath the Coso volcanic field, California: Contributions to Mineralogy and Petrology, v. 85, no. 4, p. 346-365, https://doi.org/10.1007/BF01150292.","productDescription":"20 p.","startPage":"346","endPage":"365","numberOfPages":"20","costCenters":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"links":[{"id":205009,"rank":9999,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1007/BF01150292"},{"id":220127,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","volume":"85","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a4b47e4b0c8380cd69411","contributors":{"authors":[{"text":"Bacon, C. R. 0000-0002-2165-5618","orcid":"https://orcid.org/0000-0002-2165-5618","contributorId":21522,"corporation":false,"usgs":true,"family":"Bacon","given":"C. R.","affiliations":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"preferred":false,"id":365431,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Metz, J.","contributorId":59942,"corporation":false,"usgs":true,"family":"Metz","given":"J.","email":"","affiliations":[],"preferred":false,"id":365432,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":7588,"text":"ofr83270 - 1983 - The U.S. Geological Survey's water resources program in New York","interactions":[],"lastModifiedDate":"2012-02-02T00:05:50","indexId":"ofr83270","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1983","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"83-270","title":"The U.S. Geological Survey's water resources program in New York","docAbstract":"The U.S. Geological Survey performs hydrologic investigations throughout the United States to appraise the Nation's water resources. The Geological Survey began its water-resources investigations in New York in 1895. To meet the objectives of assessing New York's water resources, the Geological Survey (1) monitors the quantity and quality of surface and ground water, (2) conducts investigations of the occurrence, availability, and chemical quality of water in specific areas of the State, (3) develops methods and techniques of data-collection and interpretation, (4) provides scientific guidance to the research community, to Federal, State, and local governments, and to the public, and (5) disseminates data and results of research through reports, maps, news releases, conferences, and workshops. \r\n\r\nMany of the joint hydrologic investigations are performed by the Geological Survey in cooperation with State, county, and nonprofit organizations. The data collection network in New York includes nearly 200 gaging stations and 250 observation wells; chemical quality of water is measured at 260 sites. Data collected at these sites are published annually and are filed in the WATSTORE computer system. Some of the interpretive studies performed by the Geological Survey in New York include (1) determining the suitability of ground-water reservoirs for public-water supply in urban areas, (2) assessing geohydrologic impacts of leachate from hazardous waste sites on stream and ground-water quality, (3) evaluating the effects of precipitation quality and basin characteristics on streams and lakes, and (4) developing digital models of the hydrology of aquifers to simulate ground-water flow and the interaction between ground water and streams.","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/ofr83270","usgsCitation":"Wiltshire, D.A., 1983, The U.S. Geological Survey's water resources program in New York: U.S. Geological Survey Open-File Report 83-270, 15 p. ;27 cm., https://doi.org/10.3133/ofr83270.","productDescription":"15 p. ;27 cm.","costCenters":[],"links":[{"id":139857,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1983/0270/report-thumb.jpg"},{"id":35074,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1983/0270/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a80e4b07f02db6498d8","contributors":{"authors":[{"text":"Wiltshire, Denise A.","contributorId":78717,"corporation":false,"usgs":true,"family":"Wiltshire","given":"Denise","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":156237,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":11052,"text":"ofr83410 - 1983 - Computer-generated mineral commodity deposit maps","interactions":[],"lastModifiedDate":"2012-02-02T00:06:20","indexId":"ofr83410","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1983","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"83-410","title":"Computer-generated mineral commodity deposit maps","docAbstract":"This report describes an automated method of generating deposit maps of mineral commodity information. In addition, it serves as a user's manual for the authors' mapping system. Procedures were developed which allow commodity specialists to enter deposit information, retrieve selected data, and plot deposit symbols in any geographic area within the conterminous United States. The mapping system uses both micro- and mainframe computers. The microcomputer is used to input and retrieve information, thus minimizing computing charges. The mainframe computer is used to generate map plots which are printed by a Calcomp plotter. \r\n\r\nSelector V data base system is employed for input and retrieval on the microcomputer. A general mapping program (Genmap) was written in FORTRAN for use on the mainframe computer. Genmap can plot fifteen symbol types (for point locations) in three sizes. The user can assign symbol types to data items interactively. Individual map symbols can be labeled with a number or the deposit name. Genmap also provides several geographic boundary file and window options.","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/ofr83410","usgsCitation":"Schruben, P.G., and Hanley, J.T., 1983, Computer-generated mineral commodity deposit maps: U.S. Geological Survey Open-File Report 83-410, 22 p. ill., map ;28 cm., https://doi.org/10.3133/ofr83410.","productDescription":"22 p. ill., map ;28 cm.","costCenters":[],"links":[{"id":142302,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1983/0410/report-thumb.jpg"},{"id":38818,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1983/0410/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b19e4b07f02db6a75bb","contributors":{"authors":[{"text":"Schruben, Paul G.","contributorId":38974,"corporation":false,"usgs":true,"family":"Schruben","given":"Paul","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":162445,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hanley, J. Thomas","contributorId":85594,"corporation":false,"usgs":true,"family":"Hanley","given":"J.","email":"","middleInitial":"Thomas","affiliations":[],"preferred":false,"id":162446,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":9694,"text":"ofr83727 - 1983 - Assessment of gray whale feeding grounds and sea floor interaction in the northeastern Bering Sea","interactions":[],"lastModifiedDate":"2012-02-02T00:06:10","indexId":"ofr83727","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1983","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"83-727","title":"Assessment of gray whale feeding grounds and sea floor interaction in the northeastern Bering Sea","docAbstract":"A dense ampeliscid amphipod community in Chirikov Basin and around St. Lawrence Island in the northeastern Bering Sea has been outlined by summarizing biological studies, analyzing bioturbation in sediment samples, and examining sea floor photos and videotapes. The amphipod population is associated with a homogeneous, relict fine-grained sand body 0.10-1.5 m thick that is deposited during the marine transgression over the Bering land bridge 8,000-10,000 yr B.P. Modern current and water mass movements and perhaps whale feeding activity prevent modern deposition in this area. \r\n\r\nThe distribution of the transgressive sand sheet, associated amphipod community and feeding gray whales mapped by aerial survey correlate closely with three types of sea-floor pits observed on high (500 kHz) and low (105 kHz) resolution side-scan sonar; they are attributed to gray whale feeding traces and their subsequent current scour modification. The fresh and modified feeding pits are present in 22,000 km2 of the basin and they cover a total of 2 to 18% of the sea floor in different areas of the feeding region. The smallest size class of pits approximates whale mouth gape size and is assumed to represent fresh whale feeding pits. Fresh feeding disturbance of the sea floor is estimated to average about 5.7% for a full feeding season. Combined with information that 34% of the measured benthic biomass is amphipod prey species, and calculating the number of gray whale feeding days in the Alaskan waters plus amount consumed per day, it can be estimated that Chirikov Basin, 2% of the feeding area, supplies a minimum of 5.3 to 7.1% of the gray whale's food resource in the Bering Sea and Arctic Ocean. If a maximum of 50% of the fresh feeding features are assumed to be missed because they parallel side-scan beam paths, then a maximum whale food resource of 14.2% is possible in northeastern Bering Sea. Because of side-scan techniques and possible higher amphipod biomass estimates, a reasonable minimum estimate of the total whale food resource in northeastern Bering Sea is 10%. \r\n\r\nThese data show that side-scan sonar is a powerful new technique for analyzing marine mammal benthic feeding grounds. Sonographs reveal that the gray whales profoundly disturb the substrate and initiate substantial further erosion by bottom currents, all of which enhances productivity of the prey species and results in a 'farming of the sea floor'. In turn, because of the high concentration of whale prey species in a prime feeding ground that is vulnerable to the development of petroleum and mining for sand, great care is required in the exploitation of these resources in the Chirikov Basin.","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/ofr83727","usgsCitation":"Nelson, C., Johnson, K., and Barber, J., 1983, Assessment of gray whale feeding grounds and sea floor interaction in the northeastern Bering Sea: U.S. Geological Survey Open-File Report 83-727, 112 p. ill., maps ;28 cm., https://doi.org/10.3133/ofr83727.","productDescription":"112 p. ill., maps ;28 cm.","costCenters":[],"links":[{"id":141014,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1983/0727/report-thumb.jpg"},{"id":37413,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1983/0727/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4abae4b07f02db671f9e","contributors":{"authors":[{"text":"Nelson, C.H.","contributorId":88346,"corporation":false,"usgs":true,"family":"Nelson","given":"C.H.","email":"","affiliations":[],"preferred":false,"id":160141,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Johnson, K.R.","contributorId":28599,"corporation":false,"usgs":true,"family":"Johnson","given":"K.R.","email":"","affiliations":[],"preferred":false,"id":160140,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Barber, John H.","contributorId":90305,"corporation":false,"usgs":true,"family":"Barber","given":"John H.","affiliations":[],"preferred":false,"id":160142,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ]}