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.
","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. of 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":"Utah, 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).
","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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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":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":"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.
","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":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":"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.
","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":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":"The Laguna Madre of Texas supports the most extensive seagrass meadows in the western Gulf of Mexico, In 1988 seagrasses covered 730 km2 or about three-quarters of the embayment. Halodule wrightii dominated the entire upper laguna, and total biomass was quite uniform near 160 g˙m-2 throughout. Four species shared dominance in the lower laguna. Where present mean biomass of Thalassia testudinum was 373 g˙m-2; Syringodium filiforme, 138 g˙m-2; Halodule wrightii, 78 g˙m-2; and Halophila engelmannii, 6 g˙m-2. Macroalgae were widespread, at 71 g˙m-2 where present. Halodule wrightii was dominant and biomass was low on sand flats of the barrier island separating the laguna from the gulf. Halophila engelmannii was limited to the deep edges of meadows. Biomass >300 g˙m-2 was limited to one extensive T. testudinum meadow at the south end of the laguna at all vegetated depths and two small areas with S. filiforme 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 (<2 m compared to 8–11 m), higher contribution of H. wrightii to system-wide biomass (although H. wrightii's share has rapidly diminished in Laguna Madre as it has been displaced by S. filiforme and T. testudinum [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 Thalassia continue to increase, the laguna may become vulnerable to mass mortalities as are now occurring in Florida Bay.
No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/b1988J","usgsCitation":"Stevens, C., Klingman, D.S., Sandberg, C.A., Stone, P., Belasky, P., Poole, F.G., and Snow, J.K., 1996, Mississippian stratigraphic framework of east-central California and southern Nevada with revision of Upper Devonian and Mississippian stratigraphic units in Inyo County, California: U.S. Geological Survey Bulletin 1988, iv, 39 p., https://doi.org/10.3133/b1988J.","productDescription":"iv, 39 p.","costCenters":[{"id":35995,"text":"Geology, Geophysics, and Geochemistry Science Center","active":true,"usgs":true}],"links":[{"id":87025,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1988j/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":174062,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1988j/report-thumb.jpg"}],"country":"United States","state":"California","county":"Inyo 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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":"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.
","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 Exxon Valdez 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":"Organic geochemistry played a major role in the environmental assessments conducted following the Exxon Valdez 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 Exxon Valdez spill are not necessarily applicable to all spill situations, the principles that governed their selection are.
Distributions of polycyclic aromatic hydrocarbons (PAH) and dibenzothiophenes distinguish Exxon Valdez oil and its weathered residues from background hydrocarbons in benthic sediments. Ratios of
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, Exxon Valdez 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 Exxon Valdez 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.
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 Exxon Valdez 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.
","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}]}} ,{"id":70207655,"text":"70207655 - 1996 - 40Ar/39Ar whole-rock data constraints on Acadian diagenesis and Alleghanian cleavage in the Martinsburg formation, eastern Pennsylvania","interactions":[],"lastModifiedDate":"2020-06-04T15:41:04.707768","indexId":"70207655","displayToPublicDate":"1996-01-02T14:15:54","publicationYear":"1996","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":732,"text":"American Journal of Science","active":true,"publicationSubtype":{"id":10}},"displayTitle":"40Ar/39Ar whole-rock data constraints on Acadian diagenesis and Alleghanian cleavage in the Martinsburg formation, eastern Pennsylvania","title":"40Ar/39Ar whole-rock data constraints on Acadian diagenesis and Alleghanian cleavage in the Martinsburg formation, eastern Pennsylvania","docAbstract":"A comparison of 40Ar/39Ar age spectra of whole-rock mudstone and slate samples from the Ordovician Martinsburg Formation at Lehigh Gap, Pennsylvania and stratigraphic and thermal constraints support Alleghanian age for regional slaty cleavage and a late Acadian age for diagenesis in these rocks. Age spectra from mud-stones have a sigmodal shape, with slopes that climb steeply from apparent Mesozoic ages to intermediate saddle regions with Devonian apparent ages, and then climb steeply again to Late Proterozoic apparent ages. The steps with these oldest apparent ages are interpreted to be dominated by late Proterzoic detrial muscovite. The saddle region of the mudstone samples gives very Late Silurian to earliest Devonian ages, which are maximum ages of diagenetic micas and which eliminate a Taconic age for the cleavage. The ages of saddle regions of the slate samples constraining cleavage-forming muscovite is <~375. This is the maximum age of this mica and requires an Alleghanian age for the cleavage. These age constraints are supported by ages of individual mica components calculated with knowledge of the total gas ages and mass fractions of the micas and by predictions from thermal modeling. We conclude that the Taconic orogeny in the Martinsburg Formation in eastern Pennsylvania was a very mild event. Not only is the cleavage in these rocks not Taconic in age, but even the mild (~100C) diagenetic growth of illite was Silurian of younger. Thus the Taconic event in these rocks in limited to loading of lass than about 3 km.
","language":"English","publisher":"International Earth Science Journal","doi":"10.2475/ajs.296.7.766","usgsCitation":"Wintsch, R., Kunk, M.J., and Epstein, J.B., 1996, 40Ar/39Ar whole-rock data constraints on Acadian diagenesis and Alleghanian cleavage in the Martinsburg formation, eastern Pennsylvania: American Journal of Science, v. 296, no. 7, p. 766-788, https://doi.org/10.2475/ajs.296.7.766.","productDescription":"23 p.","startPage":"766","endPage":"788","costCenters":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true}],"links":[{"id":479043,"rank":0,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.2475/ajs.296.7.766","text":"Publisher Index Page"},{"id":370948,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Connecticut, Delaware, Maryland, Pennsylvania, New York, New Jersey","otherGeospatial":"Martinsburg Formation","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -77.76123046875,\n 39.36827914916014\n ],\n [\n -74.06982421875,\n 38.87392853923629\n ],\n [\n -73.0810546875,\n 42.17968819665961\n ],\n [\n -77.67333984375,\n 42.24478535602799\n ],\n [\n -77.76123046875,\n 39.36827914916014\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"296","issue":"7","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Wintsch, R. P.","contributorId":116962,"corporation":false,"usgs":true,"family":"Wintsch","given":"R. P.","affiliations":[],"preferred":false,"id":778771,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Kunk, Michael J. 0000-0003-4424-7825 mkunk@usgs.gov","orcid":"https://orcid.org/0000-0003-4424-7825","contributorId":200968,"corporation":false,"usgs":true,"family":"Kunk","given":"Michael","email":"mkunk@usgs.gov","middleInitial":"J.","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":778772,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Epstein, Jack B. jepstein@usgs.gov","contributorId":1412,"corporation":false,"usgs":true,"family":"Epstein","given":"Jack","email":"jepstein@usgs.gov","middleInitial":"B.","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":778773,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":5223094,"text":"5223094 - 1996 - Using landscape ecology to test hypotheses about large-scale abundance patterns in migratory birds","interactions":[],"lastModifiedDate":"2023-12-14T17:26:40.844146","indexId":"5223094","displayToPublicDate":"1996-01-01T12:17:45","publicationYear":"1996","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1465,"text":"Ecology","active":true,"publicationSubtype":{"id":10}},"title":"Using landscape ecology to test hypotheses about large-scale abundance patterns in migratory birds","docAbstract":"The hypothesis that Neotropical migrant birds may be undergoing widespread declines due to land use activities on the breeding grounds has been examined primarily by synthesizing results from local studies. Growing concern for the cumulative influence of land use activities on ecological systems has heightened the need for large—scale studies to complement what has been observed at local scales. We investigated possible landscape effects on Neotropical migrant bird populations for the eastern United States by linking two large—scale inventories designed to monitor breeding—bird abundances and land use patterns. The null hypothesis of no relation between landscape structure and Neotropical migrant abundance was tested by correlating measures of landscape structure with bird abundance, while controlling for the geographic distance among samples. Neotropical migrants as a group were more sensitive to landscape structure than either temperate migrants or permanent residents. Neotropical migrants tended to be more abundant in landscapes with a greater proportion of forest and wetland habitats, fewer edge habitats, larger forest patches, and with forest habitats well dispersed throughout the scene. Permanent residents showed few correlations with landscape structure and temperate migrants were associated with habitat diversity and edge attributes rather than with the amount, size, and dispersion of forest habitats. The association between Neotropical migrant abundance and forest fragmentation differed among physiographic strata, suggesting that landscape context affects observed relations between bird abundance and landscape structure. Finally, associations between landscape structure and temporal trends in Neotropical migrant abundance were counter to those observed in space. Trends in Neotropical migrant abundance were negatively correlated with forest habitats. These results suggest that extrapolation of patterns observed in some landscapes is not likely to hold regionally, and that conservation policies must consider the variation in landscape structure associations observed among different types of bird species and in physiographic strata with varying land use histories.
","language":"English","publisher":"Ecological Society of America","doi":"10.2307/2265651","usgsCitation":"Flather, C.H., and Sauer, J.R., 1996, Using landscape ecology to test hypotheses about large-scale abundance patterns in migratory birds: Ecology, v. 77, no. 1, p. 28-35, https://doi.org/10.2307/2265651.","productDescription":"8 p.","startPage":"28","endPage":"35","numberOfPages":"8","costCenters":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":198189,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"77","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aefe4b07f02db691540","contributors":{"authors":[{"text":"Flather, Curtis H.","contributorId":177590,"corporation":false,"usgs":false,"family":"Flather","given":"Curtis","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":337865,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Sauer, John R. 0000-0002-4557-3019 jrsauer@usgs.gov","orcid":"https://orcid.org/0000-0002-4557-3019","contributorId":146917,"corporation":false,"usgs":true,"family":"Sauer","given":"John","email":"jrsauer@usgs.gov","middleInitial":"R.","affiliations":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"preferred":true,"id":337864,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1016009,"text":"1016009 - 1996 - Complete migration cycle of golden eagles breeding in northern Quebec","interactions":[],"lastModifiedDate":"2023-11-26T15:20:30.067043","indexId":"1016009","displayToPublicDate":"1996-01-01T00:00:00","publicationYear":"1996","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3551,"text":"The Condor","active":true,"publicationSubtype":{"id":10}},"title":"Complete migration cycle of golden eagles breeding in northern Quebec","docAbstract":"Radio tracking via satellite was initiated to study the year-round movements\r\nof Golden Eagles(Aquila chrysaetosc anadensis) breeding on the east coast of Hudson Bay,\r\nQuebec. In June and August 1992, six Golden Eagles(five adults and one juvenile) were\r\nmarked, three of which completed their year-round movements. The eagles left their breeding\r\narea in mid- to late October and migrated to known wintering areas in the eastern United\r\nStates. They used different routes but each followed the same general path during fall and\r\nspring migrations which lasted between 26 and 40 days,and 25 and 51 days, respectively.\r\nEagles wintered from 93 to 135 days in areas located 1,650 to 3,000 km south of their\r\nbreeding territory. In spring 1993, satellite telemetry located the eagles in their former\r\nbreeding territory in late March, mid-April and early May. This study confirms previous\r\nsuggestion that some breeding Golden Eagles wintering in eastern United States come from\r\nnorthern Quebec and describes the first successful tracking of the complete yearly migration\r\ncycle of a bird of prey.","language":"English","publisher":"Oxford Academic","doi":"10.2307/1369147","usgsCitation":"Brodeur, S., DeCarie, R., Bird, D., and Fuller, M.R., 1996, Complete migration cycle of golden eagles breeding in northern Quebec: The Condor, v. 98, no. 2, p. 293-299, https://doi.org/10.2307/1369147.","productDescription":"7 p.","startPage":"293","endPage":"299","numberOfPages":"7","costCenters":[{"id":290,"text":"Forest and Rangeland Ecosystem Science Center","active":false,"usgs":true}],"links":[{"id":480168,"rank":2,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.2307/1369147","text":"Publisher Index Page"},{"id":133604,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"98","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a7fe4b07f02db648708","contributors":{"authors":[{"text":"Brodeur, Serge","contributorId":102848,"corporation":false,"usgs":true,"family":"Brodeur","given":"Serge","email":"","affiliations":[],"preferred":false,"id":323494,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"DeCarie, R.","contributorId":20293,"corporation":false,"usgs":true,"family":"DeCarie","given":"R.","email":"","affiliations":[],"preferred":false,"id":323492,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Bird, D.M.","contributorId":38521,"corporation":false,"usgs":true,"family":"Bird","given":"D.M.","email":"","affiliations":[],"preferred":false,"id":323493,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Fuller, Mark R. 0000-0001-7459-1729 mark_fuller@usgs.gov","orcid":"https://orcid.org/0000-0001-7459-1729","contributorId":2296,"corporation":false,"usgs":true,"family":"Fuller","given":"Mark","email":"mark_fuller@usgs.gov","middleInitial":"R.","affiliations":[{"id":290,"text":"Forest and Rangeland Ecosystem Science Center","active":false,"usgs":true},{"id":289,"text":"Forest and Rangeland Ecosys Science Center","active":true,"usgs":true}],"preferred":true,"id":323491,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":1007452,"text":"1007452 - 1996 - Geographic variation in migratory behavior of greater white-fronted geese (Anser albifrons)","interactions":[],"lastModifiedDate":"2017-08-23T09:23:12","indexId":"1007452","displayToPublicDate":"1996-01-01T00:00:00","publicationYear":"1996","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3544,"text":"The Auk","onlineIssn":"1938-4254","printIssn":"0004-8038","active":true,"publicationSubtype":{"id":10}},"title":"Geographic variation in migratory behavior of greater white-fronted geese (Anser albifrons)","docAbstract":"We studied the migration and winter distribution of adult Greater White-fronted Geese (Anser albifrons frontalis) radio-marked on the Yukon-Kuskokwim Delta (YKD) and Bristol Bay Lowlands (BBL) of Alaska from 1987 to 1992. The major autumn staging site for geese from both breeding areas was the Klamath Basin on the California/Oregon border. However, temporal use of this area differed markedly between populations. Geese from the BBL arrived at the Klamath Basin nearly 30 days before geese from the YKD and departed before most YKD geese had arrived. Ninety percent of BBL geese used the Klamath Basin in autumn, whereas 30% of YKD geese bypassed the Klamath Basin during autumn and instead flew directly to the Central Valley of California. Nearly all BBL geese migrated directly from the Klamath Basin to wintering areas in Mexico, bypassing the Central Valley. Ninety percent of the BBL geese wintered in Mexico, as opposed to <20% of the YKD geese. Wetlands of the Interior Highlands in the state of Chihuahua, particularly Laguna Babicora, were used by >90% of the radio-marked geese in Mexico. Marshes along the West Coast comprised the other important wintering habitat in Mexico. The Sacramento Valley of California was the predominant wintering area for YKD geese. BBL geese migrated north from Mexico into the San Joaquin Valley or Sacramento-San Joaquin Delta of California by the last week of January. Fifty-five percent of the BBL population used the Klamath Basin in spring, but many birds staged in eastern Oregon and western Idaho. In contrast, geese from the YKD staged almost exclusively in the Klamath Basin during spring before flying to staging areas in Alaska. Breeding allopatry and temporal partitioning on staging and wintering areas likely has contributed to the evolution of previously described phenotypic differences between these populations. These two populations, along with the Tule Greater White-fronted Goose (A. a. gambeli), may constitute a portion of a Rassenkreis, a group of subspecies connected by clines, each ecotype of which has independent conservation needs.
","language":"English","publisher":"American Ornithological Society","doi":"10.2307/4088866","usgsCitation":"Ely, C.R., and Takekawa, J.Y., 1996, Geographic variation in migratory behavior of greater white-fronted geese (Anser albifrons): The Auk, v. 113, no. 4, p. 889-901, https://doi.org/10.2307/4088866.","productDescription":"13 p.","startPage":"889","endPage":"901","costCenters":[{"id":651,"text":"Western Ecological Research Center","active":true,"usgs":true}],"links":[{"id":479102,"rank":2,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.2307/4088866","text":"Publisher Index Page"},{"id":438911,"rank":1,"type":{"id":30,"text":"Data Release"},"url":"https://doi.org/10.5066/P9MBQ2GN","text":"USGS data release","linkHelpText":"Tracking Data for Greater White-fronted Geese (Anser albifrons)"},{"id":130375,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"113","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1be4b07f02db6a9032","contributors":{"authors":[{"text":"Ely, Craig R. 0000-0003-4262-0892 cely@usgs.gov","orcid":"https://orcid.org/0000-0003-4262-0892","contributorId":3214,"corporation":false,"usgs":true,"family":"Ely","given":"Craig","email":"cely@usgs.gov","middleInitial":"R.","affiliations":[{"id":117,"text":"Alaska Science Center Biology WTEB","active":true,"usgs":true},{"id":651,"text":"Western Ecological Research Center","active":true,"usgs":true}],"preferred":true,"id":315387,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Takekawa, John Y. 0000-0003-0217-5907 john_takekawa@usgs.gov","orcid":"https://orcid.org/0000-0003-0217-5907","contributorId":176168,"corporation":false,"usgs":true,"family":"Takekawa","given":"John","email":"john_takekawa@usgs.gov","middleInitial":"Y.","affiliations":[{"id":651,"text":"Western Ecological Research Center","active":true,"usgs":true}],"preferred":false,"id":315386,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1002900,"text":"1002900 - 1996 - Exposure of wild waterfowl to Mycoplasma anatis","interactions":[],"lastModifiedDate":"2017-12-21T11:17:53","indexId":"1002900","displayToPublicDate":"1996-01-01T00:00:00","publicationYear":"1996","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2507,"text":"Journal of Wildlife Diseases","active":true,"publicationSubtype":{"id":10}},"title":"Exposure of wild waterfowl to Mycoplasma anatis","docAbstract":"We developed an ELISA procedure to assess the presence of M. Anatis-specific serum antibody in ducks. Sera from exposed and unexposed Pekin ducks (Anas platyrhynchos) were used to standardize tile ELISA and to establish reference ranges to classify ELISA results as exposed or not exposed. We conducted serological surveys of female waterfowl in the central and eastern United States between 1988 and 1992 to assess the frequency of exposure in wild waterfowl. Adult breeding mallards (Anas platyrhynchos), wintering mallards, and black ducks (Anas rubripes) had high prevalences of exposure to M. Anatis (25% to >80%). In comparison, none of the breeding adult canvasbacks (Aythya valisineria) had serum antibody levels indicating exposure. Approximately 50% of the juvenile mallards and black ducks were exposed to M. Anatis by 8 months of age, indicating high transmission rates among wild birds.","language":"English","publisher":"Wildlife Disease Association","doi":"10.7589/0090-3558-32.2.331","issn":"00903558","usgsCitation":"Samuel, M., Goldberg, D., Thomas, C.B., Sharp, P., Robb, J., Krapu, G., Nersessian, B., Kenow, K., Korschgen, C.E., Chipley, W., and Conroy, M., 1996, Exposure of wild waterfowl to Mycoplasma anatis: Journal of Wildlife Diseases, v. 32, no. 2, p. 331-337, https://doi.org/10.7589/0090-3558-32.2.331.","productDescription":"7 p.","startPage":"331","endPage":"337","numberOfPages":"7","costCenters":[{"id":456,"text":"National Wildlife Health Center","active":true,"usgs":true},{"id":480,"text":"Northern Prairie Wildlife Research Center","active":true,"usgs":true},{"id":606,"text":"Upper Midwest Environmental Sciences Center","active":true,"usgs":true}],"links":[{"id":487063,"rank":1,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.7589/0090-3558-32.2.331","text":"Publisher Index Page"},{"id":198540,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"32","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a07e4b07f02db5f9af5","contributors":{"authors":[{"text":"Samuel, M.D.","contributorId":13910,"corporation":false,"usgs":true,"family":"Samuel","given":"M.D.","affiliations":[],"preferred":false,"id":312284,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Goldberg, Diana R. 0000-0001-8540-8512","orcid":"https://orcid.org/0000-0001-8540-8512","contributorId":82252,"corporation":false,"usgs":true,"family":"Goldberg","given":"Diana R.","affiliations":[{"id":456,"text":"National Wildlife Health Center","active":true,"usgs":true}],"preferred":false,"id":312289,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Thomas, C. B.","contributorId":87888,"corporation":false,"usgs":false,"family":"Thomas","given":"C.","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":312291,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Sharp, P.","contributorId":88685,"corporation":false,"usgs":false,"family":"Sharp","given":"P.","email":"","affiliations":[],"preferred":false,"id":312292,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Robb, J.R.","contributorId":11551,"corporation":false,"usgs":true,"family":"Robb","given":"J.R.","email":"","affiliations":[],"preferred":false,"id":312283,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Krapu, Gary L.","contributorId":56994,"corporation":false,"usgs":true,"family":"Krapu","given":"Gary L.","affiliations":[],"preferred":false,"id":312288,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Nersessian, B.N.","contributorId":35035,"corporation":false,"usgs":true,"family":"Nersessian","given":"B.N.","email":"","affiliations":[],"preferred":false,"id":312287,"contributorType":{"id":1,"text":"Authors"},"rank":7},{"text":"Kenow, K.P.","contributorId":18302,"corporation":false,"usgs":true,"family":"Kenow","given":"K.P.","affiliations":[],"preferred":false,"id":312286,"contributorType":{"id":1,"text":"Authors"},"rank":8},{"text":"Korschgen, C. E.","contributorId":9197,"corporation":false,"usgs":true,"family":"Korschgen","given":"C.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":312282,"contributorType":{"id":1,"text":"Authors"},"rank":9},{"text":"Chipley, W.H.","contributorId":14783,"corporation":false,"usgs":true,"family":"Chipley","given":"W.H.","email":"","affiliations":[],"preferred":false,"id":312285,"contributorType":{"id":1,"text":"Authors"},"rank":10},{"text":"Conroy, M.J.","contributorId":84690,"corporation":false,"usgs":true,"family":"Conroy","given":"M.J.","email":"","affiliations":[],"preferred":false,"id":312290,"contributorType":{"id":1,"text":"Authors"},"rank":11}]}} ,{"id":70018161,"text":"70018161 - 1996 - Record of middle Pleistocene climate change from Buck Lake, Cascade Range, southern Oregon - Evidence from sediment magnetism, trace-element geochemistry, and pollen","interactions":[],"lastModifiedDate":"2023-12-23T14:58:07.523436","indexId":"70018161","displayToPublicDate":"1996-01-01T00:00:00","publicationYear":"1996","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Record of middle Pleistocene climate change from Buck Lake, Cascade Range, southern Oregon - Evidence from sediment magnetism, trace-element geochemistry, and pollen","docAbstract":"Comparison of systematic variations in sediment magnetic properties to changes in pollen assemblages in middle Pleistocene lake sediments from Buck Lake indicates that the magnetic properties are sensitive to changes in climate. Buck Lake is located in southern Oregon just east of the crest of the Cascade Range. Lacustrine sediments, from 5.2 to 19.4 m in depth in core, contain tephra layers with ages of ≈300–400 ka at 9.5 m and ≈400–470 ka at 19.9 m. In these sediments magnetic properties reflect the absolute amount and relative abundances of detrital Fe-oxide minerals, titanomagnetite and hematite. The lacustrine section is divided into four zones on the basis of magnetic properties. Two zones (19.4–17.4 m and 14.5–10.3 m) of high magnetic susceptibility contain abundant Fe oxides and correspond closely to pollen zones that are indicative of cold, dry environments. Two low-susceptibility zones (17.4–14.5 m and 10.3–5.3 m) contain lesser amounts of Fe oxides and largely coincide with zones of warm-climate pollen. Transitions from cold to warm climate based on pollen are preceded by sharp changes in magnetic properties. This relation suggests that land-surface processes responded to these climate changes more rapidly than did changes in vegetation as indicated by pollen frequencies. Magnetic properties have been affected by three factors: (1) dissolution of Fe oxides, (2) variation in heavy-mineral content, and (3) variation in abundance of fresh volcanic rock fragments. Trace-element geochemistry, employing Fe and the immobile elements Ti and Zr, is utilized to detect postdepositional dissolution of magnetic minerals that has affected the magnitude of magnetic properties with little effect on the pattern of magnetic-property variation. Comparison of Ti and Zr values, proxies for heavy-mineral content, to magnetic properties demonstrates that part of the variation in the amount of magnetite and nearly all of the variation in the amount of hematite are due to changes in heavy-mineral content. Variation in the quantity of fresh volcanic rock fragments is the other source of change in magnetite content. Magnetic-property variations probably arise primarily from changes in peak runoff. At low to moderate flows magnetic properties reflect only the quantities of heavy minerals derived from soil and highly weathered rock in the catchment. At high flows, however, fresh volcanic rock fragments may be produced by breaking of pebbles and cobbles, and such fragments greatly increase the magnetite content of the resulting sediment. Climatically controlled factors that would affect peak runoff levels include the accumulation and subsequent melting of winter snow pack, the seasonality of precipitation, and the degree of vegetation cover of the land surface. Our results do not distinguish among the possible contributions of these disparate factors.
One of the major problems in hydrogeologic investigations of glaciated regions is the determination of complex stratigraphic relationships in the subsurface where insufficient information is available from drilling and geophysical records. In this paper, chemical characteristics of groundwater were used to identify stratigraphic changes in glacial deposits that were previously inferred on Block Island, Rhode Island, USA, an emergent remnant of the late Wisconsinan terminal moraine, located approximately 16 km south of the Rhode Island mainland. Two chemically distinct water types are recognized on the island: 1) high-iron, characterized by dissolved silica levels in excess of 20 mg/L, bicarbonate greater than 30 mg/L and dissolved iron ranging from 1-20 mg/L; and 2) low-iron, characterized by dissolved silica levels below 16 mg/L, bicarbonate less than 30 mg/L, and less than 0.3 mg/L dissolved iron. The spatial distribution of iron-bearing minerals and organic matter and the resulting redox conditions are believed to control the occurrence of highiron groundwater. The high-iron waters occur almost exclusively in the eastern half of the island and appear to coincide with the presence of allochthonous blocks of Cretaceous-age coastal-plain sediments that were incorporated into Pleistocene-age deposits derived from the Narragansett Bay-Buzzard's Bay lobe of the Late Wisconsinan Laurentide ice sheet. The low-iron waters occur in the western half of the island, where the occurrence of these Cretaceous-age blocks is rare and the sediments are attributed to a sublobe of the Hudson-Champlain lobe of the Late Wisconsinan ice sheet.
","language":"English","publisher":"Springer","doi":"10.1007/s100400050093","usgsCitation":"Veeger, A., and Stone, B., 1996, Using hydrogeochemical methods to evaluate complex quaternary subsurface stratigraphy Block Island, Rhode Island, USA: Hydrogeology Journal, v. 4, no. 4, p. 69-82, https://doi.org/10.1007/s100400050093.","productDescription":"14 p.","startPage":"69","endPage":"82","numberOfPages":"14","costCenters":[{"id":40020,"text":"Florence Bascom Geoscience Center","active":true,"usgs":true}],"links":[{"id":488745,"rank":1,"type":{"id":41,"text":"Open Access External Repository Page"},"url":"https://digitalcommons.uri.edu/geo_facpubs/178","text":"External Repository"},{"id":228484,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Rhode Island","otherGeospatial":"Block Island","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -71.61918640136719,\n 41.14531119462475\n ],\n [\n -71.54090881347656,\n 41.14531119462475\n ],\n [\n -71.54090881347656,\n 41.233800286547435\n ],\n [\n -71.61918640136719,\n 41.233800286547435\n ],\n [\n -71.61918640136719,\n 41.14531119462475\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"4","issue":"4","noUsgsAuthors":false,"publicationDate":"2012-11-20","publicationStatus":"PW","scienceBaseUri":"505bc05ee4b08c986b32a0ad","contributors":{"authors":[{"text":"Veeger, A.I.","contributorId":100031,"corporation":false,"usgs":true,"family":"Veeger","given":"A.I.","email":"","affiliations":[],"preferred":false,"id":377485,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Stone, B. D. 0000-0001-6092-0798","orcid":"https://orcid.org/0000-0001-6092-0798","contributorId":50919,"corporation":false,"usgs":true,"family":"Stone","given":"B. D.","affiliations":[],"preferred":false,"id":377484,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70018192,"text":"70018192 - 1996 - Magnetic properties and emplacement of the Bishop tuff, California","interactions":[],"lastModifiedDate":"2023-11-08T01:37:03.162425","indexId":"70018192","displayToPublicDate":"1996-01-01T00:00:00","publicationYear":"1996","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1109,"text":"Bulletin of Volcanology","active":true,"publicationSubtype":{"id":10}},"title":"Magnetic properties and emplacement of the Bishop tuff, California","docAbstract":"Anisotropy of magnetic susceptibility (AMS) and characteristic remanence were measured for 45 sites in the 0.76 Ma Bishop tuff, eastern California. Thirty-three sites were sampled in three stratigraphic sections, two in Owens gorge south of Long Valley caldera, and the third in the Adobe lobe north of Long Valley. The remaining 12 sites are widely distributed, but of limited stratigraphic extent. Weakly indurated, highly porous to dense, welded ash-flow tuffs were sampled. Saturation magnetization vs temperature experiments indicate two principal iron oxide phases: low Ti magnetites with 525–570 °C Curie temperatures, and maghemite with 610°–640 °C Curie temperatures. AF demagnetization spectra of isothermal remanent magnetizations are indicative of magnetite/maghemite predominantly in the multidomain to pseudo-single domain size ranges. Remeasurement of AMS after application of saturating direct fields indicates that randomly oriented single-domain grains are also present. The degree of anisotropy is only a few percent, typical of tuffs. The AMS ellipsoids are oblate with Kmin axes normal to subhorizontal foliation and Kmax axes regionally aligned with published source vents. For 12 of 16 locality means, Kmax axes plunge sourceward, confirming previous observations regarding flow sense. Topographic control on flow emplacement is indicated by the distribution of tuff deposits and by flow directions inferred from Kmax axes. Deposition east of the Benton range occurred by flow around the south end of the range and through two gaps (Benton notch and Chidago gap). Flow down Mammoth pass of the Sierra Nevada is also evident. At least some of the Adobe lobe in the northeast flowed around the west end of Glass mountain. Eastward flow directions in the upper Owens gorge and southeast directions in the lower Owens gorge are parallel to the present canyon, suggesting that the present drainage has been established along the pre-Bishop paleodrainage. Characteristic remanence directions from 45 sites (267 samples) yield an overall mean of D=348°, I=53° for the Bishop tuff. A correlation is found in two of the three profiles between density and remanence inclination. A mean remanence direction based on 13 localities together with data from uncompacted xenoliths and data from the ash-fall tuff at Lake Tecopa is: D=353°, I=54°, k=172, α95=2.9°, N=15.
Chemical analyses were done on cores of bottom sediment from three locations in Lake Livingston, a reservoir on the Trinity River in east Texas to identify trends in water quality in the Trinity River using the chemical record preserved in bottom sediments trapped by the reservoir. Sediment cores spanned the period from 1969, when the reservoir was impounded, to 1992, when the cores were collected. Chemical concentrations in reservoir sediment samples were compared to concentrations for 14 streambed sediment samples from the Trinity River Basin and to reported concentrations for soils in the eastern United States and shale. These comparisons indicate that sediments deposited in Lake Livingston are representative of the environmental setting of Lake Livingston within the Trinity River Basin. Vertical changes in concentrations within sediment cores indicate temporal trends of decreasing concentrations of lead, sodium, barium, and total DDT (DDT plus its metabolites DDD and DDE) in the Trinity River. Possible increasing temporal trends are indicated for chlordane and dieldrin. Each sediment-derived trend is related to trends in water quality in the Trinity River or known changes in environmental factors in its drainage basin or both.
","language":"English","publisher":"Springer Link","doi":"10.1007/s002540050093","usgsCitation":"Van Metre, P., and Callender, E., 1996, Identifying water-quality trends in the Trinity River, Texas, USA, 1969-1992, using sediment cores from Lake Livingston: Environmental Geology, v. 28, no. 4, p. 190-200, https://doi.org/10.1007/s002540050093.","productDescription":"11 p.","startPage":"190","endPage":"200","numberOfPages":"11","costCenters":[],"links":[{"id":227369,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Texas","otherGeospatial":"Lake Livington, Trinity River basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -94.28880085646635,\n 29.627392076789917\n ],\n [\n -96.20653031185886,\n 33.77052674928851\n ],\n [\n -98.40319808697573,\n 33.588196456146136\n ],\n [\n -96.21412735441417,\n 31.10174712503047\n ],\n [\n -95.87724430726398,\n 30.11411914907775\n ],\n [\n -95.09389249157088,\n 29.127543787851735\n ],\n [\n -94.28880085646635,\n 29.627392076789917\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"28","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a385ee4b0c8380cd61548","contributors":{"authors":[{"text":"Van Metre, P. C.","contributorId":92999,"corporation":false,"usgs":true,"family":"Van Metre","given":"P. C.","affiliations":[],"preferred":false,"id":378861,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Callender, E.","contributorId":72528,"corporation":false,"usgs":true,"family":"Callender","given":"E.","email":"","affiliations":[],"preferred":false,"id":378860,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70019342,"text":"70019342 - 1996 - Directional topographic site response at Tarzana observed in aftershocks of the 1994 Northridge, California, earthquake: Implications for mainshock motions","interactions":[],"lastModifiedDate":"2023-10-22T14:05:46.417816","indexId":"70019342","displayToPublicDate":"1996-01-01T00:00:00","publicationYear":"1996","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1135,"text":"Bulletin of the Seismological Society of America","onlineIssn":"1943-3573","printIssn":"0037-1106","active":true,"publicationSubtype":{"id":10}},"title":"Directional topographic site response at Tarzana observed in aftershocks of the 1994 Northridge, California, earthquake: Implications for mainshock motions","docAbstract":"The Northridge earthquake caused 1.78 g acceleration in the east-west direction at a site in Tarzana, California, located about 6 km south of the mainshock epicenter. The accelerograph was located atop a hill about 15-m high, 500-m long, and 130-m wide, striking about N78°E. During the aftershock sequence, a temporary array of 21 three-component geophones was deployed in six radial lines centered on the accelerograph, with an average sensor spacing of 35 m. Station C00 was located about 2 m from the accelerograph. We inverted aftershock spectra to obtain average relative site response at each station as a function of direction of ground motion. We identified a 3.2-Hz resonance that is a transverse oscillation of the hill (a directional topographic effect). The top/base amplification ratio at 3.2 Hz is about 4.5 for horizontal ground motions oriented approximately perpendicular to the long axis of the hill and about 2 for motions parallel to the hill. This resonance is seen most strongly within 50 m of C00. Other resonant frequencies were also observed. A strong lateral variation in attenuation, probably associated with a fault, caused substantially lower motion at frequencies above 6 Hz at the east end of the hill. There may be some additional scattered waves associated with the fault zone and seen at both the base and top of the hill, causing particle motions (not spectral ratios) at the top of the hill to be rotated about 20° away from the direction transverse to the hill. The resonant frequency, but not the amplitude, of our observed topographic resonance agrees well with theory, even for such a low hill. Comparisons of our observations with theoretical results indicate that the 3D shape of the hill and its internal structure are important factors affecting its response. The strong transverse resonance of the hill does not account for the large east-west mainshock motions. Assuming linear soil response, mainshock east-west motions at the Tarzana accelerograph were amplified by a factor of about 2 or less compared with sites at the base of the hill. Probable variations in surficial shear-wave velocity do not account for the observed differences among mainshock acceleration observed at Tarzana and at two different sites within 2 km of Tarzana.
Bouldery debris fans and sandy alluvial terraces of the Colorado River developed contemporaneously during the late Holocene at the mouths of nine major tributaries in eastern Grand Canyon. The age of the debris fans and alluvial terraces contributes to understanding river hydraulics and to the history of human activity along the river, which has been concentrated on these surfaces for at least two to three millennia. Poorly sorted, coarse-grained debris-flow deposits of several ages are interbedded with, overlie, or are overlapped by three terrace-forming alluviums. The alluvial deposits are of three age groups: the striped alluvium, deposited from before 770 b.c. to about a.d. 300; the alluvium of Pueblo II age deposited from about a.d. 700 to December 1900; and the alluvium of the upper mesquite terrace, deposited from about a.d. 1400 to 1880. Two elements define the geomorphology of a typical debris fan: the large, inactive surface of the fan and a smaller, entrenched, active debris-flow channel and fan that is about one-sixth the area of the inactive fan. The inactive fan is segmented into at least three surfaces with distinctive weathering characteristics. These surfaces are conformable with underlying debris-flow deposits that date from before 770 b.c. to around a.d. 660, a.d. 660 to before a.d. 1200, and from a.d. 1200 to slightly before 1890, respectively, based on late-19th-century photographs, radiocarbon and archaeologic dating of the three stratigraphically related alluviums, and radiocarbon dating of fine-grained debris-flow deposits. These debris flows aggraded the fans in at least three stages beginning about 2.8 ka, if not earlier in the late Holocene. Several main-stem floods eroded the margin of the segmented fans, reducing fan symmetry. The entrenched, active debris-flow channels contain deposits <100 yr old, which form debris fans at the mouth of the channel adjacent to the river. Early and middle Holocene debris-flow and alluvial deposits have not been recognized, as they were evidently not preserved adjacent to the river or are buried by younger deposits.