{"pageNumber":"140","pageRowStart":"3475","pageSize":"25","recordCount":11004,"records":[{"id":70117081,"text":"pp1806 - 2014 - Two hundred years of magma transport and storage at Kīlauea Volcano, Hawai'i, 1790-2008","interactions":[],"lastModifiedDate":"2019-03-15T10:34:25","indexId":"pp1806","displayToPublicDate":"2014-08-19T08:22:00","publicationYear":"2014","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":"1806","title":"Two hundred years of magma transport and storage at Kīlauea Volcano, Hawai'i, 1790-2008","docAbstract":"<p>This publication summarizes the evolution of the internal plumbing of Kīlauea Volcano on the Island of Hawaiʻi from the first documented eruption in 1790 to the explosive eruption of March 2008 in Halemaʻumaʻu Crater. For the period before the founding of the Hawaiian Volcano Observatory in 1912, we rely on written observations of eruptive activity, earthquake swarms, and periodic draining of magma from the lava lake present in Kīlauea Caldera. After 1912 the written observations are supplemented by continuous measurement of tilting of the ground at Kīlauea’s summit and by a continuous instrumental record of earthquakes, both measurements made during 1912–56 by a single pendulum seismometer housed on the northeast edge of Kīlauea’s summit. Interpretations become more robust following the installation of seismic and deformation networks in the 1960s. A major advance in the 1990s was the ability to continuously record and telemeter ground deformation to allow its precise correlation with seismic activity before and after eruptions, intrusions, and large earthquakes.</p><p>We interpret specific events in Kīlauea’s 200- year written history as steps in a broad transition from summit lava-lake activity in Kīlauea Caldera to shield building on the east rift zone. The ability of the magmatic plumbing to deliver magma to eruption is critical to the history of eruption and intrusion. When the rate of magma supply equals the rate of eruption, there is little ground deformation or intrusion. When the magma supply rate is greater than the rate of eruption, then the edifice responds through any or all of summit inflation, intrusion, increased spreading rate, and large flank earthquakes.</p><p>In Kīlauea’s 200-year history we identify three regions of the volcano in which magma is stored and supplied from below. Source 1 is at 1-km depth or less beneath Kīlauea’s summit and fed Kīlauea’s summit lava lakes throughout most of the 19th century and again from 1907 to 1924. Source 1 was used up in the series of small Halemaʻumaʻu eruptions following the end of lava-lake activity in the summit collapse of 1924. Source 2 is the magma reservoir at a depth of 2–6 km beneath Kīlauea’s summit that has been imaged by seismic and deformation measurements beginning in the 1960s. This source was first identified in the summit collapses of 1922 and 1924. Source 3 is a diffuse volume of magma-permeated rock between 5 and 11 km depth beneath the east rift zone and above the near-horizontal decollement at the base of the Kīlauea edifice.</p><p>Magma distribution within source 2 has been derived by combining petrologic study of the three chemically uniform summit eruptions of 1952, 1961, and 1967–68 and the east rift eruptions within this interval with both observation of migrating centers of inflation determined from leveling surveys conducted before the 1967–68 eruption and with published models of expected deformation from different source geometries. We adopt a model of concatenated magmatic plugs with nodes beneath the inflation centers. Addition of erupted and intruded volumes of the three summit magma batches yields a liquid magma volume of about 0.2 km3, with dimensions of ~1 km by 1 km by 200 m centered at about 3-km depth within source 2. Following the Halemaʻumaʻu eruption of 1967–68, the chemistry of magma coming into Kīlauea’s summit reservoir has changed frequently, and during the eruption that began in 1983, chemical changes have been subtle and continuous. In this period we interpret changes in chemistry as related to an increase in magma supply resulting from increased partial melting in an expanding mantle source volume.</p><p>We know from instrumental recording of eruptions since the long Halemaʻumaʻu eruption in 1952 that stress in the edifice accumulates as magma is added underground and is relieved by eruption and by dilation of the rift zones associated with seaward movement (spreading) of Kīlauea’s south flank. During and after the last half of the 20th century, magma transfer to the rift zone has dominantly occurred from source 2. High rates of flank motion have been correlated with high rates of endogenous growth; alternatively, lower rates of motion have characterized periods when the underground magmatic plumbing was being refilled following lateral removal of magma, as well as periods when a more open magmatic plumbing favored continuous eruption.</p><p>Since at least 1952, source 3 has not drained during deflations, which was apparently not the case before 1924. Triangulation and leveling conducted in 1912, 1921, and 1926, combined with post-1912 tilt measurements, identified a broad regional uplift in 1918–19 and an equally broad collapse in 1924, neither of which has been seen since. We associate these elevation changes with addition or subtraction of magma from all three magma sources, dominantly source 3. We interpret the intrusion beneath the east rift zone during the 1924 collapse to have stabilized the rift zone-south flank relationship, preventing loss of magma from source 3 in subsequent collapses. Rates of seaward spreading were low until 1952, when earthquakes in 1950 and 1951 associated with surges of magma from the hotspot triggered a large offshore south flank earthquake swarm that unlocked the south flank and enabled a greatly increased rate of seaward spreading.</p><p>Magma supply rates have been derived for the entire period of study. Between 1823 and 1840, magma was supplied from source 1 at a very high rate of more than 0.2 km<sup>3</sup>/yr, which we interpret as recovery from a substantial draining of magma from beneath Kīlauea in 1790. Inferred magma supply rates diminished to one-tenth of that value after 1840, in part because of increase in the activity of Mauna Loa beginning in 1843. Magma supply rates between 1918 and 1924 were about 0.024 km<sup>3</sup>/yr, matching that of the period from 1840 to 1894. During 1950–52 the magma supply rate increased to about 0.06 km<sup>3</sup>/yr, in part because of the great reduction in Mauna Loa activity following its large eruption in June 1950. Following the summit eruption of 1967–68, magma supply increased further to ~0.1 km<sup>3</sup>/yr, and further increases to more than 0.2 km<sup>3</sup>/yr occurred during the east rift eruption that began in 1983.</p><p>Eruption at Kīlauea’s summit took place in 1952, and eruptive activity steadily increased as increased magma supply also drove increased spreading rates. The inability of magma supply to be accommodated by a combination of eruption and spreading during the 1969–74 Mauna Ulu period stressed Kīlauea’s south flank. The stress was relieved in part by the M7.2 earthquake of 29 November 1975. That earthquake, in turn, dilated Kīlauea’s east rift zone as the south flank moved seaward, producing a favorable condition for continuous east rift eruption, which began in 1983. The 1975 earthquake also resulted in the ability of the south flank to move independently under the influence of gravity, effectively decoupling the spreading rate from changes in the magma supply rate. The continuing increase in magma supply after 1983 was instead manifested in rift dilation, increased intrusion, and ultimately in the launching of a second eruption in Halemaʻumaʻu in March 2008, the first instance in Kīlauea’s recorded history of simultaneous eruption at the summit and on the east rift zone.</p><p>Kīlauea’s history can be considered in cycles of equilibrium, crisis, and recovery. The approach of a crisis is driven by a magma supply rate that greatly exceeds the capacity of the plumbing to deliver magma to the surface. Crises can be anticipated by inflation measured at Kīlauea’s summit coupled with an increase in overall seismicity, particularly manifest by intrusion and eruption in the southwest sector of the volcano. Unfortunately the nature of the crisis—for example, large earthquake, new eruption, or edifice-changing intrusion—cannot be specified ahead of time. We conclude that Kīlauea’s cycles are controlled by nonlinear dynamics, which underscores the difficulty in predicting eruptions and earthquakes.</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/pp1806","usgsCitation":"Wright, T., and Klein, F.W., 2014, Two hundred years of magma transport and storage at Kīlauea Volcano, Hawai'i, 1790-2008: U.S. Geological Survey Professional Paper 1806, Report: xiii, 240 p.; Appendixes B-I; Chapters: Contents and Abstract, Chapters 1-8, References; Appendixes: Appendixes Readme, Appendixes A-I, https://doi.org/10.3133/pp1806.","productDescription":"Report: xiii, 240 p.; Appendixes B-I; Chapters: Contents and Abstract, Chapters 1-8, References; Appendixes: Appendixes Readme, Appendixes A-I","numberOfPages":"258","onlineOnly":"N","additionalOnlineFiles":"Y","temporalStart":"1789-12-21","temporalEnd":"2008-12-31","ipdsId":"IP-035005","costCenters":[{"id":615,"text":"Volcano Hazards 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,{"id":70118312,"text":"sir20145143 - 2014 - Streamflow statistics for development of water rights claims for the Jarbidge Wild and Scenic River, Owyhee Canyonlands Wilderness, Idaho, 2013-14: a supplement to Scientific Investigations Report 2013-5212","interactions":[],"lastModifiedDate":"2014-08-19T08:16:57","indexId":"sir20145143","displayToPublicDate":"2014-08-18T16:49:00","publicationYear":"2014","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":334,"text":"Scientific Investigations Report","code":"SIR","onlineIssn":"2328-0328","printIssn":"2328-031X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2014-5143","title":"Streamflow statistics for development of water rights claims for the Jarbidge Wild and Scenic River, Owyhee Canyonlands Wilderness, Idaho, 2013-14: a supplement to Scientific Investigations Report 2013-5212","docAbstract":"The U.S. Geological Survey (USGS), in cooperation with the Bureau of Land Management (BLM), estimated streamflow statistics for stream segments designated “Wild,” “Scenic,” or “Recreational” under the National Wild and Scenic Rivers System in the Owyhee Canyonlands Wilderness in southwestern Idaho. The streamflow statistics were used by the BLM to develop and file a draft, federal reserved water right claim to protect federally designated “outstanding remarkable values” in the Jarbidge River. The BLM determined that the daily mean streamflow equaled or exceeded 20, 50, and 80 percent of the time during bimonthly periods (two periods per month) and the bankfull (66.7-percent annual exceedance probability) streamflow are important thresholds for maintaining outstanding remarkable values. Although streamflow statistics for the Jarbidge River below Jarbidge, Nevada (USGS 13162225) were published previously in 2013 and used for the draft water right claim, the BLM and USGS have since recognized the need to refine streamflow statistics given the approximate 40 river mile distance and intervening tributaries between the original point of estimation (USGS 13162225) and at the mouth of the Jarbidge River, which is the downstream end of the Wild and Scenic River segment. A drainage-area-ratio method was used in 2013 to estimate bimonthly exceedance probability streamflow statistics at the mouth of the Jarbidge River based on available streamgage data on the Jarbidge and East Fork Jarbidge Rivers. The resulting bimonthly streamflow statistics were further adjusted using a scaling factor calculated from a water balance on streamflow statistics calculated for the Bruneau and East Fork Bruneau Rivers and Sheep Creek. The final, adjusted bimonthly exceedance probability and bankfull streamflow statistics compared well with available verification datasets (including discrete streamflow measurements made at the mouth of the Jarbidge River) and are considered the best available estimates for streamflow statistics in the Jarbidge Wild and Scenic River segment.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/sir20145143","collaboration":"Prepared in cooperation with the Bureau of Land Management","usgsCitation":"Wood, M.S., 2014, Streamflow statistics for development of water rights claims for the Jarbidge Wild and Scenic River, Owyhee Canyonlands Wilderness, Idaho, 2013-14: a supplement to Scientific Investigations Report 2013-5212: U.S. Geological Survey Scientific Investigations Report 2014-5143, iv, 14 p., https://doi.org/10.3133/sir20145143.","productDescription":"iv, 14 p.","numberOfPages":"22","onlineOnly":"Y","ipdsId":"IP-056976","costCenters":[{"id":343,"text":"Idaho Water Science Center","active":true,"usgs":true}],"links":[{"id":292486,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir20145143.jpg"},{"id":292485,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/sir/2014/5143/pdf/sir2014-5143.pdf"},{"id":292484,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2014/5143/"}],"projection":"Transverse Mercator projection","datum":"North American Datum of 1983","country":"United States","state":"Idaho","otherGeospatial":"Jarbidge River;Owyhee Canyonlands Wilderness","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -116.25,42.00 ], [ -116.25,42.75 ], [ -115.50,42.75 ], [ -115.50,42.00 ], [ -116.25,42.00 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53f30530e4b0094694f94571","contributors":{"authors":[{"text":"Wood, Molly S. 0000-0002-5184-8306 mswood@usgs.gov","orcid":"https://orcid.org/0000-0002-5184-8306","contributorId":788,"corporation":false,"usgs":true,"family":"Wood","given":"Molly","email":"mswood@usgs.gov","middleInitial":"S.","affiliations":[{"id":502,"text":"Office of Surface Water","active":true,"usgs":true},{"id":37786,"text":"WMA - Observing Systems Division","active":true,"usgs":true},{"id":343,"text":"Idaho Water Science Center","active":true,"usgs":true}],"preferred":true,"id":496739,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70120289,"text":"ofr20131267B - 2014 - Geologic framework of thermal springs, Black Canyon, Nevada and Arizona","interactions":[],"lastModifiedDate":"2023-05-26T15:17:46.602521","indexId":"ofr20131267B","displayToPublicDate":"2014-08-13T16:45:00","publicationYear":"2014","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2013-1267","chapter":"B","title":"Geologic framework of thermal springs, Black Canyon, Nevada and Arizona","docAbstract":"<p>Thermal springs in Black Canyon of the Colorado River, downstream of Hoover Dam, are important recreational, ecological, and scenic features of the Lake Mead National Recreation Area. This report presents the results from a U.S. Geological Survey study of the geologic framework of the springs. The study was conducted in cooperation with the National Park Service and funded by both the National Park Service and National Cooperative Geologic Mapping Program of the U.S. Geological Survey. The report has two parts: A, a 1:48,000-scale geologic map created from existing geologic maps and augmented by new geologic mapping and geochronology; and B, an interpretive report that presents results based on a collection of fault kinematic data near springs within Black Canyon and construction of 1:100,000-scale geologic cross sections that extend across the western Lake Mead region.</p>\n<br/>\n<p>Exposures in Black Canyon are mostly of Miocene volcanic rocks, underlain by crystalline basement composed of Miocene plutonic rocks or Proterozoic metamorphic rocks. The rocks are variably tilted and highly faulted. Faults strike northwest to northeast and include normal and strike-slip faults. Spring discharge occurs along faults intruded by dacite dikes and plugs; weeping walls and seeps extend away from the faults in highly fractured rock or relatively porous volcanic breccias, or both.</p>\n<br/>\n<p>Results of kinematic analysis of fault data collected along tributaries to the Colorado River indicate two episodes of deformation, consistent with earlier studies. The earlier episode formed during east-northeast-directed extension, and the later during east-southeast-directed extension. At the northern end of the study area, pre-existing fault blocks that formed during the first episode were rotated counterclockwise along the left-lateral Lake Mead Fault System. The resulting fault pattern forms a complex arrangement that provides both barriers and pathways for groundwater movement within and around Black Canyon.</p>\n<br/>\n<p>Regional cross sections in this report show that thick Paleozoic carbonate aquifer rocks of east-central Nevada do not extend into the Black Canyon area and generally are terminated to the south at a major tectonic boundary defined by the northeast-striking Lake Mead Fault System and the northwest-striking Las Vegas Valley shear zone. Faults to the west of Black Canyon strike dominantly north-south and form a complicated pattern that may inhibit easterly groundwater movement from Eldorado Valley. To the east of Black Canyon, crystalline Proterozoic rocks locally overlain by Tertiary volcanic rocks in the Black Mountains are bounded by steep north-south normal faults. These faults may also inhibit westerly groundwater movement from Detrital Valley toward Black Canyon. Finally, the cross sections show clearly that Proterozoic basement rocks and (or) Tertiary plutonic rocks are shallow in the Black Canyon area (at the surface to a few hundred meters depth) and are cut by several major faults that discharge most of the springs in the Black Canyon. Therefore, the faults most likely provide groundwater pathways to sufficient depths that the groundwater is heated to the observed temperatures of up to 55 °C.</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr20131267B","collaboration":"Prepared in cooperation with the National Park Service","usgsCitation":"Beard, L.S., Anderson, Z.W., Felger, T.J., and Seixas, G.B., 2014, Geologic framework of thermal springs, Black Canyon, Nevada and Arizona: U.S. Geological Survey Open-File Report 2013-1267, Report: v, 58 p.; 1 Plate: 40.72 x 24.96 inches, https://doi.org/10.3133/ofr20131267B.","productDescription":"Report: v, 58 p.; 1 Plate: 40.72 x 24.96 inches","numberOfPages":"68","onlineOnly":"Y","additionalOnlineFiles":"Y","ipdsId":"IP-040846","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":292133,"rank":4,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr20131267B.jpg"},{"id":417500,"rank":5,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_100545.htm","linkFileType":{"id":5,"text":"html"}},{"id":292131,"rank":1,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2013/1267/b/pdf/ofr2013-1267B.pdf"},{"id":292132,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/2013/1267/b/pdf/ofr2013-1267B_plate1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":292122,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2013/1267/b/","linkFileType":{"id":5,"text":"html"}}],"scale":"250000","country":"United States","state":"Arizona, Nevada","otherGeospatial":"Black Canyon","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -115.00,35.75 ], [ -115.00,36.75 ], [ -114.25,36.75 ], [ -114.25,35.75 ], [ -115.00,35.75 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53ec6dafe4b02bf5a766a9c1","contributors":{"authors":[{"text":"Beard, L. Sue","contributorId":87607,"corporation":false,"usgs":true,"family":"Beard","given":"L.","email":"","middleInitial":"Sue","affiliations":[],"preferred":false,"id":498103,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Anderson, Zachary W. zanderson@usgs.gov","contributorId":4604,"corporation":false,"usgs":true,"family":"Anderson","given":"Zachary","email":"zanderson@usgs.gov","middleInitial":"W.","affiliations":[],"preferred":true,"id":498101,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Felger, Tracey J. 0000-0003-0841-4235 tfelger@usgs.gov","orcid":"https://orcid.org/0000-0003-0841-4235","contributorId":1117,"corporation":false,"usgs":true,"family":"Felger","given":"Tracey","email":"tfelger@usgs.gov","middleInitial":"J.","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":498100,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Seixas, Gustav B.","contributorId":36062,"corporation":false,"usgs":true,"family":"Seixas","given":"Gustav","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":498102,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}}
,{"id":70055701,"text":"ofr20131267A - 2014 - Preliminary geologic map of Black Canyon and surrounding region, Nevada and Arizona","interactions":[],"lastModifiedDate":"2023-05-26T15:20:43.245806","indexId":"ofr20131267A","displayToPublicDate":"2014-08-13T16:30:00","publicationYear":"2014","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2013-1267","chapter":"A","title":"Preliminary geologic map of Black Canyon and surrounding region, Nevada and Arizona","docAbstract":"<p>Thermal springs in Black Canyon of the Colorado River, downstream of Hoover Dam, are important recreational, ecological, and scenic features of the Lake Mead National Recreation Area. This report presents the results from a U.S. Geological Survey study of the geologic framework of the springs. The study was conducted in cooperation with the National Park Service and funded by both the National Park Service and National Cooperative Geologic Mapping Program of the U.S. Geological Survey. The report has two parts: A, a 1:48,000-scale geologic map created from existing geologic maps and augmented by new geologic mapping and geochronology; and B, an interpretive report that presents results based on a collection of fault kinematic data near springs within Black Canyon and construction of 1:100,000-scale geologic cross sections that extend across the western Lake Mead region.</p>\n<br/>\n<p>Exposures in Black Canyon are mostly of Miocene volcanic rocks, underlain by crystalline basement composed of Miocene plutonic rocks or Proterozoic metamorphic rocks. The rocks are variably tilted and highly faulted. Faults strike northwest to northeast and include normal and strike-slip faults. Spring discharge occurs along faults intruded by dacite dikes and plugs; weeping walls and seeps extend away from the faults in highly fractured rock or relatively porous volcanic breccias, or both.</p>\n<br/>\n<p>Results of kinematic analysis of fault data collected along tributaries to the Colorado River indicate two episodes of deformation, consistent with earlier studies. The earlier episode formed during east-northeast-directed extension, and the later during east-southeast-directed extension. At the northern end of the study area, pre-existing fault blocks that formed during the first episode were rotated counterclockwise along the left-lateral Lake Mead Fault System. The resulting fault pattern forms a complex arrangement that provides both barriers and pathways for groundwater movement within and around Black Canyon.</p>\n<br/>\n<p>Regional cross sections in this report show that thick Paleozoic carbonate aquifer rocks of east-central Nevada do not extend into the Black Canyon area and generally are terminated to the south at a major tectonic boundary defined by the northeast-striking Lake Mead Fault System and the northwest-striking Las Vegas Valley shear zone. Faults to the west of Black Canyon strike dominantly north-south and form a complicated pattern that may inhibit easterly groundwater movement from Eldorado Valley. To the east of Black Canyon, crystalline Proterozoic rocks locally overlain by Tertiary volcanic rocks in the Black Mountains are bounded by steep north-south normal faults. These faults may also inhibit westerly groundwater movement from Detrital Valley toward Black Canyon. Finally, the cross sections show clearly that Proterozoic basement rocks and (or) Tertiary plutonic rocks are shallow in the Black Canyon area (at the surface to a few hundred meters depth) and are cut by several major faults that discharge most of the springs in the Black Canyon. Therefore, the faults most likely provide groundwater pathways to sufficient depths that the groundwater is heated to the observed temperatures of up to 55 °C.</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr20131267A","usgsCitation":"Felger, T.J., Beard, L.S., Anderson, Z.W., Fleck, R.J., Wooden, J., and Seixas, G.B., 2014, Preliminary geologic map of Black Canyon and surrounding region, Nevada and Arizona: U.S. Geological Survey Open-File Report 2013-1267, Pamphlet: iii, 20 p.; 1 Plate: 42.00 x 42.00 inches; Readme; Metadata; Geodatabase; Shapefiles, https://doi.org/10.3133/ofr20131267A.","productDescription":"Pamphlet: iii, 20 p.; 1 Plate: 42.00 x 42.00 inches; Readme; Metadata; Geodatabase; Shapefiles","numberOfPages":"23","onlineOnly":"Y","additionalOnlineFiles":"Y","ipdsId":"IP-041664","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":292128,"rank":8,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr20131267A.jpg"},{"id":398947,"rank":9,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_100544.htm","linkFileType":{"id":5,"text":"html"}},{"id":292121,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2013/1267/a/","linkFileType":{"id":5,"text":"html"}},{"id":292124,"rank":1,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2013/1267/a/pdf/ofr2013-1267A_pamphlet.pdf"},{"id":292134,"rank":5,"type":{"id":20,"text":"Read Me"},"url":"https://pubs.usgs.gov/of/2013/1267/a/downloads/ofr2013-1267A_readme.txt"},{"id":292125,"rank":3,"type":{"id":16,"text":"Metadata"},"url":"https://pubs.usgs.gov/of/2013/1267/a/downloads/ofr2013-1267A_metadata.txt"},{"id":292126,"rank":6,"type":{"id":23,"text":"Spatial Data"},"url":"https://pubs.usgs.gov/of/2013/1267/a/downloads/ofr2013-1267A_database.zip"},{"id":292127,"rank":7,"type":{"id":23,"text":"Spatial Data"},"url":"https://pubs.usgs.gov/of/2013/1267/a/downloads/ofr2013-1267A_shape.zip"},{"id":292123,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/2013/1267/a/pdf/ofr2013-1267A_map.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"48000","projection":"Transverse Mercator projection","datum":"North American 1983","country":"United States","state":"Arizona, Nevada","otherGeospatial":"Black Canyon","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -115,\n              35.75\n            ],\n            [\n              -114.5689,\n              35.75\n            ],\n            [\n              -114.5689,\n              36.1292\n            ],\n            [\n              -115,\n              36.1292\n            ],\n            [\n              -115,\n              35.75\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53ec6dafe4b02bf5a766a9c5","contributors":{"authors":[{"text":"Felger, Tracey J. 0000-0003-0841-4235 tfelger@usgs.gov","orcid":"https://orcid.org/0000-0003-0841-4235","contributorId":1117,"corporation":false,"usgs":true,"family":"Felger","given":"Tracey","email":"tfelger@usgs.gov","middleInitial":"J.","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":486222,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Beard, L. Sue","contributorId":87607,"corporation":false,"usgs":true,"family":"Beard","given":"L.","email":"","middleInitial":"Sue","affiliations":[],"preferred":false,"id":486226,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Anderson, Zachary W. zanderson@usgs.gov","contributorId":4604,"corporation":false,"usgs":true,"family":"Anderson","given":"Zachary","email":"zanderson@usgs.gov","middleInitial":"W.","affiliations":[],"preferred":true,"id":486223,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Fleck, Robert J. 0000-0002-3149-8249 fleck@usgs.gov","orcid":"https://orcid.org/0000-0002-3149-8249","contributorId":1048,"corporation":false,"usgs":true,"family":"Fleck","given":"Robert","email":"fleck@usgs.gov","middleInitial":"J.","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":486221,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Wooden, Joseph L.","contributorId":32209,"corporation":false,"usgs":true,"family":"Wooden","given":"Joseph L.","affiliations":[],"preferred":false,"id":486224,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Seixas, Gustav B.","contributorId":36062,"corporation":false,"usgs":true,"family":"Seixas","given":"Gustav","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":486225,"contributorType":{"id":1,"text":"Authors"},"rank":6}]}}
,{"id":70121421,"text":"70121421 - 2014 - Spring migration ecology of the mid-continent sandhill crane population with an emphasis on use of the Central Platte River Valley, Nebraska","interactions":[],"lastModifiedDate":"2018-01-02T11:32:09","indexId":"70121421","displayToPublicDate":"2014-08-13T10:24:00","publicationYear":"2014","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3773,"text":"Wildlife Monographs","active":true,"publicationSubtype":{"id":10}},"title":"Spring migration ecology of the mid-continent sandhill crane population with an emphasis on use of the Central Platte River Valley, Nebraska","docAbstract":"<p>We conducted a 10-year study (1998–2007) of the Mid-Continent Population (MCP) of sandhill cranes (Grus canadensis) to identify spring-migration corridors, locations of major stopovers, and migration chronology by crane breeding affiliation (western Alaska–Siberia [WA–S], northern Canada–Nunavut [NC–N], west-central Canada–Alaska [WC–A], and east-central Canada–Minnesota [EC–M]). In the Central Platte River Valley (CPRV) of Nebraska, we evaluated factors influencing staging chronology, food habits, fat storage, and habitat use of sandhill cranes. We compared our findings to results from the Platte River Ecology Study conducted during 1978–1980. We determined spring migration corridors used by the breeding affiliations (designated subpopulations for management purposes) by monitoring 169 cranes marked with platform transmitter terminals (PTTs). We also marked and monitored 456 cranes in the CPRV with very high frequency (VHF) transmitters to evaluate length and pattern of stay, habitat use, and movements. An estimated 42% and 58% of cranes staging in the CPRV were greater sandhill cranes (G. c. tabida) and lesser sandhill cranes (G. c. canadensis), and they stayed for an average of 20 and 25 days (2000–2007), respectively. Cranes from the WA–S, NC–N, WC–A, and EC–M affiliations spent an average of 72, 77, 52, and 53 days, respectively, in spring migration of which 28, 23, 24, and 18 days occurred in the CPRV. The majority of the WA–S subpopulation settled in the CPRV apparently because of inadequate habitat to support more birds upstream, although WA–S cranes accounted for >90% of birds staging in the North Platte River Valley. Crane staging duration in the CPRV was negatively correlated with arrival dates; 92% of cranes stayed >7 days. A program of annual mechanical removal of mature stands of woody growth and seedlings that began in the early 1980s primarily in the main channel of the Platte River has allowed distribution of crane roosts to remain relatively stable over the past 2 decades. Most cranes returned to nocturnal roost sites used in previous years. Corn residues dominated the diet of sandhill cranes in the CPRV, as in the 1970s, despite a marked decline in standing crop of corn residues. Only 14% (10 of 74) of PTT-marked migrant cranes stayed at stopovers for ≥5 days before arriving in the CPRV, which limited the contribution of sites south of the CPRV for fat accumulation needed for migration and reproduction. Body masses of cranes (after adjusting for body size [an index of fat]) at arrival in the CPRV varied widely among years (1998–2006), indicating the importance of maintaining productive habitats on the wintering grounds to condition cranes for migration and reproduction. Average rates of fat gain by adult females while in the CPRV remained similar from 1978–1979 to 1998–1999 but declined among males. Distances cranes flew to feeding grounds in the CPRV increased as the percentage of cropland planted to soybeans increased and as density of cranes on nocturnal roosts increased. These results suggest that as habitats of limited or no value to cranes increase on the landscape, more flight time and higher maintenance costs may reduce fat storage. An estimated 40% of diurnal use occurred north of Interstate 80 (I-80) where ≤5% of lands dedicated to crane conservation are located. Seventy-four and 40% of PTT-marked EC–M and WC–A cranes had spring migrations that included staging in eastern South Dakota for an average of 11 and 10 days, respectively. Cranes of the NC–N, WA–S, and WC–A subpopulations staged an average of 25, 17, and 12 days in central and western Saskatchewan/eastern Alberta. Females in these affiliations increased their fat reserves after leaving Nebraska by an estimated 450, 451, and 452 g, respectively, underscoring the key role of these staging areas in preparing the 3 subpopulations for reproduction. After departing Nebraska, MCP cranes roosted primarily in basin wetlands. Most of these wetlands are in private ownership and lack adequate protection, emphasizing the need for effective laws and policies to ensure their long-term protection. The continued success of the current management goal of maintaining the MCP at approximately its current size and providing diverse recreational opportunities over a wide area of midcontinent and western North America is predicated on the ability of MCP cranes to continue to store large fat reserves in the CPRV in advance of breeding. For the CPRV to remain a key fat storage site, active channel maintenance (e.g., clearing of woody vegetation) likely will need to continue, along with establishing minimum stream flows. These actions would help ensure nocturnal roosting habitat remains sufficiently dispersed to provide cranes with daily intake of high-energy food adequate for major fat storage and limit risk of high mortality from storms and disease. Published 2014. This article is a U.S. Government work and is in the public domain in the USA.</p>","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Wildlife Monographs","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisher":"Wiley","doi":"10.1002/wmon.1013","usgsCitation":"Krapu, G.L., Brandt, D., Kinzel, P.J., and Pearse, A.T., 2014, Spring migration ecology of the mid-continent sandhill crane population with an emphasis on use of the Central Platte River Valley, Nebraska: Wildlife Monographs, v. 189, no. 1, p. 1-41, https://doi.org/10.1002/wmon.1013.","productDescription":"42 p.","startPage":"1","endPage":"41","ipdsId":"IP-041333","costCenters":[{"id":480,"text":"Northern Prairie Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":292849,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":292803,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1002/wmon.1013"}],"country":"United States","state":"Nebraska","otherGeospatial":"Platte River Valley","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -100.6762,40.6541 ], [ -100.6762,41.4623 ], [ -97.3034,41.4623 ], [ -97.3034,40.6541 ], [ -100.6762,40.6541 ] ] ] } } ] }","volume":"189","issue":"1","noUsgsAuthors":false,"publicationDate":"2014-08-13","publicationStatus":"PW","scienceBaseUri":"53f85991e4b03f038c5c192b","chorus":{"doi":"10.1002/wmon.1013","url":"http://dx.doi.org/10.1002/wmon.1013","publisher":"Wiley-Blackwell","authors":"Krapu Gary L., Brandt David A., Kinzel Paul J., Pearse Aaron T.","journalName":"Wildlife Monographs","publicationDate":"8/2014","auditedOn":"11/1/2014"},"contributors":{"authors":[{"text":"Krapu, Gary L. 0000-0001-8482-6130 gkrapu@usgs.gov","orcid":"https://orcid.org/0000-0001-8482-6130","contributorId":3074,"corporation":false,"usgs":true,"family":"Krapu","given":"Gary","email":"gkrapu@usgs.gov","middleInitial":"L.","affiliations":[{"id":480,"text":"Northern Prairie Wildlife Research Center","active":true,"usgs":true}],"preferred":false,"id":499062,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Brandt, David A. dbrandt@usgs.gov","contributorId":3073,"corporation":false,"usgs":true,"family":"Brandt","given":"David A.","email":"dbrandt@usgs.gov","affiliations":[{"id":480,"text":"Northern Prairie Wildlife Research Center","active":true,"usgs":true}],"preferred":false,"id":499061,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Kinzel, Paul J. 0000-0002-6076-9730 pjkinzel@usgs.gov","orcid":"https://orcid.org/0000-0002-6076-9730","contributorId":743,"corporation":false,"usgs":true,"family":"Kinzel","given":"Paul","email":"pjkinzel@usgs.gov","middleInitial":"J.","affiliations":[{"id":438,"text":"National Research Program - Western Branch","active":true,"usgs":true},{"id":5044,"text":"National Research Program - Central Branch","active":true,"usgs":true},{"id":191,"text":"Colorado Water Science Center","active":true,"usgs":true},{"id":37778,"text":"WMA - Integrated Modeling and Prediction Division","active":true,"usgs":true}],"preferred":true,"id":499059,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Pearse, Aaron T. 0000-0002-6137-1556 apearse@usgs.gov","orcid":"https://orcid.org/0000-0002-6137-1556","contributorId":1772,"corporation":false,"usgs":true,"family":"Pearse","given":"Aaron","email":"apearse@usgs.gov","middleInitial":"T.","affiliations":[{"id":480,"text":"Northern Prairie Wildlife Research Center","active":true,"usgs":true}],"preferred":true,"id":499060,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}}
,{"id":70119859,"text":"70119859 - 2014 - Sediment accretion in tidal freshwater forests and oligohaline marshes of the Waccamaw and Savannah Rivers, USA","interactions":[],"lastModifiedDate":"2014-08-11T15:40:52","indexId":"70119859","displayToPublicDate":"2014-08-11T15:29:00","publicationYear":"2014","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1584,"text":"Estuaries and Coasts","active":true,"publicationSubtype":{"id":10}},"title":"Sediment accretion in tidal freshwater forests and oligohaline marshes of the Waccamaw and Savannah Rivers, USA","docAbstract":"Sediment accretion was measured at four sites in varying stages of forest-to-marsh succession along a fresh-to-oligohaline gradient on the Waccamaw River and its tributary Turkey Creek (Coastal Plain watersheds, South Carolina) and the Savannah River (Piedmont watershed, South Carolina and Georgia). Sites included tidal freshwater forests, moderately salt-impacted forests at the freshwater–oligohaline transition, highly salt-impacted forests, and oligohaline marshes. Sediment accretion was measured by use of feldspar marker pads for 2.5 year; accessory information on wetland inundation, canopy litterfall, herbaceous production, and soil characteristics were also collected. Sediment accretion ranged from 4.5 mm year<sup>−1</sup> at moderately salt-impacted forest on the Savannah River to 19.1 mm year<sup>−1</sup> at its relict, highly salt-impacted forest downstream. Oligohaline marsh sediment accretion was 1.5–2.5 times greater than in tidal freshwater forests. Overall, there was no significant difference in accretion rate between rivers with contrasting sediment loads. Accretion was significantly higher in hollows than on hummocks in tidal freshwater forests. Organic sediment accretion was similar to autochthonous litter production at all sites, but inorganic sediment constituted the majority of accretion at both marshes and the Savannah River highly salt-impacted forest. A strong correlation between inorganic sediment accumulation and autochthonous litter production indicated a positive feedback between herbaceous plant production and allochthonous sediment deposition. The similarity in rates of sediment accretion and sea level rise in tidal freshwater forests indicates that these habitats may become permanently inundated if the rate of sea level rise increases.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Estuaries and Coasts","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisher":"Springer","doi":"10.1007/s12237-013-9744-7","usgsCitation":"Ensign, S., Hupp, C.R., Noe, G., Krauss, K.W., and Stagg, C.L., 2014, Sediment accretion in tidal freshwater forests and oligohaline marshes of the Waccamaw and Savannah Rivers, USA: Estuaries and Coasts, v. 37, no. 5, p. 1107-1119, https://doi.org/10.1007/s12237-013-9744-7.","productDescription":"13 p.","startPage":"1107","endPage":"1119","numberOfPages":"13","ipdsId":"IP-050841","costCenters":[{"id":436,"text":"National Research Program - Eastern Branch","active":true,"usgs":true}],"links":[{"id":291979,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":291928,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1007/s12237-013-9744-7"}],"country":"United States","state":"Georgia;South Carolina","otherGeospatial":"Savannah River;Waccamaw River","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -81.16,32.16 ], [ -81.16,33.56 ], [ -79.08,33.56 ], [ -79.08,32.16 ], [ -81.16,32.16 ] ] ] } } ] }","volume":"37","issue":"5","noUsgsAuthors":false,"publicationDate":"2013-12-18","publicationStatus":"PW","scienceBaseUri":"53e9cab0e4b008eaa4f35a89","contributors":{"authors":[{"text":"Ensign, Scott H.","contributorId":81397,"corporation":false,"usgs":true,"family":"Ensign","given":"Scott H.","affiliations":[],"preferred":false,"id":497801,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hupp, Cliff R. 0000-0003-1853-9197 crhupp@usgs.gov","orcid":"https://orcid.org/0000-0003-1853-9197","contributorId":2344,"corporation":false,"usgs":true,"family":"Hupp","given":"Cliff","email":"crhupp@usgs.gov","middleInitial":"R.","affiliations":[{"id":436,"text":"National Research Program - Eastern Branch","active":true,"usgs":true},{"id":37277,"text":"WMA - Earth System Processes Division","active":true,"usgs":true}],"preferred":true,"id":497798,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Noe, Gregory B.","contributorId":77805,"corporation":false,"usgs":true,"family":"Noe","given":"Gregory B.","affiliations":[],"preferred":false,"id":497800,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Krauss, Ken W. 0000-0003-2195-0729 kraussk@usgs.gov","orcid":"https://orcid.org/0000-0003-2195-0729","contributorId":2017,"corporation":false,"usgs":true,"family":"Krauss","given":"Ken","email":"kraussk@usgs.gov","middleInitial":"W.","affiliations":[{"id":455,"text":"National Wetlands Research Center","active":true,"usgs":true},{"id":17705,"text":"Wetland and Aquatic Research Center","active":true,"usgs":true}],"preferred":true,"id":497797,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Stagg, Camille L. 0000-0002-1125-7253 staggc@usgs.gov","orcid":"https://orcid.org/0000-0002-1125-7253","contributorId":4111,"corporation":false,"usgs":true,"family":"Stagg","given":"Camille","email":"staggc@usgs.gov","middleInitial":"L.","affiliations":[{"id":17705,"text":"Wetland and Aquatic Research Center","active":true,"usgs":true},{"id":455,"text":"National Wetlands Research Center","active":true,"usgs":true}],"preferred":true,"id":497799,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}}
,{"id":70099972,"text":"sir20145051 - 2014 - Quality of groundwater in the Denver Basin aquifer system, Colorado, 2003-5","interactions":[],"lastModifiedDate":"2016-08-05T12:18:15","indexId":"sir20145051","displayToPublicDate":"2014-08-11T11:29:00","publicationYear":"2014","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":334,"text":"Scientific Investigations Report","code":"SIR","onlineIssn":"2328-0328","printIssn":"2328-031X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2014-5051","title":"Quality of groundwater in the Denver Basin aquifer system, Colorado, 2003-5","docAbstract":"<p>Groundwater resources from alluvial and bedrock aquifers of the Denver Basin are critical for municipal, domestic, and agricultural uses in Colorado along the eastern front of the Rocky Mountains. Rapid and widespread urban development, primarily along the western boundary of the Denver Basin, has approximately doubled the population since about 1970, and much of the population depends on groundwater for water supply. As part of the National Water-Quality Assessment Program, the U.S. Geological Survey conducted groundwater-quality studies during 2003&ndash;5 in the Denver Basin aquifer system to characterize water quality of shallow groundwater at the water table and of the bedrock aquifers, which are important drinking-water resources. For the Denver Basin, water-quality constituents of concern for human health or because they might otherwise limit use of water include total dissolved solids, fluoride, sulfate, nitrate, iron, manganese, selenium, radon, uranium, arsenic, pesticides, and volatile organic compounds. For the water-table studies, two monitoring-well networks were installed and sampled beneath agricultural (31 wells) and urban (29 wells) land uses at or just below the water table in either alluvial material or near-surface bedrock. For the bedrock-aquifer studies, domestic- and municipal-supply wells completed in the bedrock aquifers were sampled. The bedrock aquifers, stratigraphically from youngest (shallowest) to oldest (deepest), are the Dawson, Denver, Arapahoe, and Laramie-Fox Hills aquifers. The extensive dataset collected from wells completed in the bedrock aquifers (79 samples) provides the opportunity to evaluate factors and processes affecting water quality and to establish a baseline that can be used to characterize future changes in groundwater quality. Groundwater samples were analyzed for inorganic, organic, isotopic, and age-dating constituents and tracers. This report discusses spatial and statistical distributions of chemical constituents and evaluates natural and human-related processes that affect water quality. Findings are synthesized to assess the vulnerability of the Denver Basin aquifer system to groundwater contamination.</p>\n<p>The chemistry of groundwater samples collected from the water-table wells was generally different from that of samples collected from the bedrock-aquifer wells. Samples from the water-table wells tended to have higher concentrations of total dissolved solids and most major ions. Concentrations of several constituents with potential human-health concerns, including nitrate, selenium, uranium, and arsenic, decreased with depth and were highest in samples from the water-table wells. Exceedances of drinking-water standards and water-quality benchmarks were more frequently associated with shallow groundwater samples; concentrations of total dissolved solids and sulfate exceeded water-quality benchmarks for about half or more of samples from the water-table wells. The sediments and rocks of the Denver Basin are natural sources of the trace elements selenium, uranium, and arsenic, which affect their concentrations in groundwater. Detections of organic contaminants, which are typically indicative of human sources of contamination to groundwater, were more frequent in samples from the water-table wells. Pesticide compounds and volatile organic compounds were detected in 33 and 62 percent, respectively, of water-table well samples. Detected organic contaminant concentrations were much less than the associated drinking-water standards. Samples collected from the bedrock aquifers had lower concentrations of total dissolved solids than did samples collected from the water-table wells, although within the bedrock-aquifer samples, concentrations increased from the Dawson to Denver to Arapahoe to Laramie-Fox Hills aquifers. Concentrations of total dissolved solids and many constituents varied spatially and with depth in the bedrock aquifers, likely as a result of ion-exchange and oxidation-reduction reactions, which are important processes affecting water quality. Major-ion chemistry generally evolved from a calcium-bicarbonate to calcium-sulfate composition, with some sodium-bicarbonate and sodium-sulfate facies in the deeper bedrock aquifers, likely resulting from longer residence times and more extensive water-rock interaction. Oxidation-reduction conditions generally evolved from oxic at the water table to anoxic with increasing depth in the bedrock aquifers. Most samples from the bedrock aquifers were anoxic. Exceedances of drinking-water standards and water-quality benchmarks for the bedrock aquifers occurred in 1 percent or less of samples for nitrate, selenium, or arsenic; there were no exceedances for uranium. Exceedances for total dissolved solids, sulfate, manganese, and iron were generally between about 10 and 20 percent for the bedrock-aquifer samples. Radon concentrations, which were only measured in samples collected from two of the bedrock aquifers, exceeded the lower proposed drinking-water standard for more than 90 percent of samples but exceeded the higher alternative standard for less than 5 percent of samples. Pesticide compounds and volatile organic compounds were detected in 3 and 22 percent, respectively, of bedrock-aquifer samples, all at concentrations that were that were much less than drinking-water standards.</p>\n<p>Water-quality data were synthesized to evaluate factors that affect spatial and depth variability in water quality and to assess aquifer vulnerability to contaminants from geologic materials and those of human origin. The quality of shallow groundwater in the alluvial aquifer and shallow bedrock aquifer system has been adversely affected by development of agricultural and urban areas. Land use has altered the pattern and composition of recharge. Increased recharge from irrigation water has mobilized dissolved constituents and increased concentrations in the shallow groundwater. Concentrations of most constituents associated with poor or degraded water quality in shallow groundwater decreased with depth; many of these constituents are not geochemically conservative and are affected by geochemical reactions such as oxidation-reduction reactions. Groundwater age tracers provide additional insight into aquifer vulnerability and help determine if young groundwater of potentially poor quality has migrated to deeper parts of the bedrock aquifers used for drinking-water supply. Age-tracer results were used to group samples into categories of young, mixed, and old groundwater. Groundwater ages transitioned from mostly young in the water-table wells to mostly mixed in the shallowest bedrock aquifer, the Dawson aquifer, to mostly old in the deeper bedrock aquifers. Although the bedrock aquifers are mostly old groundwater of good water quality, several lines of evidence indicate that young, contaminant-bearing recharge has reached shallow to moderate depths in some areas of the bedrock aquifers. The Dawson aquifer is the most vulnerable of the bedrock aquifers to contamination, but results indicate that the older (deeper) bedrock aquifers are also vulnerable to groundwater contamination and that mixing with young recharge has occurred in some areas. Heavy pumping has caused water-level declines in the bedrock aquifers in some parts of the Denver Basin, which has the potential to enhance the transport of contaminants from overlying units. Results of this study are consistent with the existing conceptual understanding of aquifer processes and groundwater issues in the Denver Basin and add new insight into the vulnerability of the bedrock aquifers to groundwater contamination.</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/sir20145051","collaboration":"National Water-Quality Assessment Program","usgsCitation":"Musgrove, M., Beck, J., Paschke, S.S., Bauch, N.J., and Mashburn, S.L., 2014, Quality of groundwater in the Denver Basin aquifer system, Colorado, 2003-5: U.S. Geological Survey Scientific Investigations Report 2014-5051, xi, 107 p., https://doi.org/10.3133/sir20145051.","productDescription":"xi, 107 p.","numberOfPages":"123","onlineOnly":"N","additionalOnlineFiles":"N","temporalStart":"2003-01-01","temporalEnd":"2005-12-31","ipdsId":"IP-051259","costCenters":[{"id":191,"text":"Colorado Water Science Center","active":true,"usgs":true},{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":291953,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir20145051.jpg"},{"id":291950,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2014/5051/"},{"id":291952,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/sir/2014/5051/pdf/sir2014-5051.pdf"}],"country":"United States","state":"Colorado","otherGeospatial":"Denver Basin","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -108.0,38.0 ], [ -108.0,40.0 ], [ -102.0,40.0 ], [ -102.0,38.0 ], [ -108.0,38.0 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53e9caafe4b008eaa4f35a85","contributors":{"authors":[{"text":"Musgrove, MaryLynn","contributorId":34878,"corporation":false,"usgs":true,"family":"Musgrove","given":"MaryLynn","affiliations":[],"preferred":false,"id":492078,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Beck, Jennifer A.","contributorId":53922,"corporation":false,"usgs":true,"family":"Beck","given":"Jennifer A.","affiliations":[],"preferred":false,"id":492079,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Paschke, Suzanne S. 0000-0002-3471-4242 spaschke@usgs.gov","orcid":"https://orcid.org/0000-0002-3471-4242","contributorId":1347,"corporation":false,"usgs":true,"family":"Paschke","given":"Suzanne","email":"spaschke@usgs.gov","middleInitial":"S.","affiliations":[{"id":191,"text":"Colorado Water Science Center","active":true,"usgs":true}],"preferred":true,"id":492076,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Bauch, Nancy J. 0000-0002-0302-2892 njbauch@usgs.gov","orcid":"https://orcid.org/0000-0002-0302-2892","contributorId":1297,"corporation":false,"usgs":true,"family":"Bauch","given":"Nancy","email":"njbauch@usgs.gov","middleInitial":"J.","affiliations":[{"id":451,"text":"National Water Quality Assessment Program","active":true,"usgs":true}],"preferred":true,"id":492075,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Mashburn, Shana L. 0000-0001-5163-778X shanam@usgs.gov","orcid":"https://orcid.org/0000-0001-5163-778X","contributorId":2140,"corporation":false,"usgs":true,"family":"Mashburn","given":"Shana","email":"shanam@usgs.gov","middleInitial":"L.","affiliations":[{"id":516,"text":"Oklahoma Water Science Center","active":true,"usgs":true}],"preferred":true,"id":492077,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}}
,{"id":70113247,"text":"sim3304 - 2014 - Detailed north-south cross section showing environments of deposition, organic richness, and thermal maturities of lower Tertiary rocks in the Uinta Basin, Utah","interactions":[],"lastModifiedDate":"2014-08-11T10:05:36","indexId":"sim3304","displayToPublicDate":"2014-08-11T09:52:00","publicationYear":"2014","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":333,"text":"Scientific Investigations Map","code":"SIM","onlineIssn":"2329-132X","printIssn":"2329-1311","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"3304","title":"Detailed north-south cross section showing environments of deposition, organic richness, and thermal maturities of lower Tertiary rocks in the Uinta Basin, Utah","docAbstract":"The Uinta Basin of northeast Utah has produced large amounts of hydrocarbons from lower Tertiary strata since the 1960s. Recent advances in drilling technologies, in particular the development of efficient methods to drill and hydraulically fracture horizontal wells, has spurred renewed interest in producing hydrocarbons from unconventional low-permeability dolomite and shale reservoirs in the lacustrine, Eocene Green River Formation. The Eocene Green River Formation was deposited in Lake Uinta, a long-lived saline lake that occupied the Uinta Basin, the Piceance Basin to the east, and the intervening Douglas Creek arch. The focus of recent drilling activity has been the informal Uteland Butte member of the Green River Formation and to a much lesser extent the overlying R-0 oil shale zone of the Green River Formation. Initial production rates ranging from 500 to 1,500 barrels of oil equivalent per day have been reported from the Uteland Butte member from horizontal well logs that are as long as 4,000 feet (ft);. The cross section presented here extends northward from outcrop on the southern margin of the basin into the basin’s deep trough, located just south of the Uinta Mountains, and transects the area where this unconventional oil play is developing. The Monument Butte field, which is one of the fields located along this line of section, has produced hydrocarbons from conventional sandstone reservoirs in the lower part of the Green River Formation and underlying Wasatch Formation since 1981. A major fluvial-deltaic system entered Lake Uinta from the south, and this new line of section is ideal for studying the effect of the sediments delivered by this drainage on hydrocarbon reservoirs in the Green River Formation. The cross section also transects the Greater Altamont-Bluebell field in the deepest part of the basin, where hydrocarbons have been produced from fractured, highly overpressured marginal lacustrine and fluvial reservoirs in the Green River, Wasatch, and North Horn Formations since 1970. Datum for the cross section is sea level so that hydrocarbon source rocks and reservoir rocks could be integrated into the structural framework of the basin.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/sim3304","usgsCitation":"Johnson, R.C., 2014, Detailed north-south cross section showing environments of deposition, organic richness, and thermal maturities of lower Tertiary rocks in the Uinta Basin, Utah: U.S. Geological Survey Scientific Investigations Map 3304, Report: iv, 12 p.; Cross Section: 69.0 x 45.01 inches, https://doi.org/10.3133/sim3304.","productDescription":"Report: iv, 12 p.; Cross Section: 69.0 x 45.01 inches","numberOfPages":"19","onlineOnly":"Y","additionalOnlineFiles":"Y","ipdsId":"IP-051246","costCenters":[{"id":164,"text":"Central Energy Resources Science Center","active":true,"usgs":true}],"links":[{"id":291935,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sim3304.jpg"},{"id":291932,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sim/3304/"},{"id":291934,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/sim/3304/pdf/sim3304_map.pdf"},{"id":291933,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/sim/3304/pdf/sim3304_pamphlet.pdf"}],"country":"United States","state":"Utah","otherGeospatial":"Uinta Basin","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -112.25,38.0 ], [ -112.25,43.5 ], [ -106.25,43.5 ], [ -106.25,38.0 ], [ -112.25,38.0 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53e9caafe4b008eaa4f35a71","contributors":{"authors":[{"text":"Johnson, Ronald C. 0000-0002-6197-5165 rcjohnson@usgs.gov","orcid":"https://orcid.org/0000-0002-6197-5165","contributorId":1550,"corporation":false,"usgs":true,"family":"Johnson","given":"Ronald","email":"rcjohnson@usgs.gov","middleInitial":"C.","affiliations":[{"id":164,"text":"Central Energy Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":495019,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70111236,"text":"sim3302 - 2014 - California State Waters Map Series: Offshore of Coal Oil Point, California","interactions":[],"lastModifiedDate":"2022-04-18T18:54:40.14922","indexId":"sim3302","displayToPublicDate":"2014-08-08T08:21:00","publicationYear":"2014","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":333,"text":"Scientific Investigations Map","code":"SIM","onlineIssn":"2329-132X","printIssn":"2329-1311","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"3302","title":"California State Waters Map Series: Offshore of Coal Oil Point, California","docAbstract":"<p>In 2007, the California Ocean Protection Council initiated the California Seafloor Mapping Program (CSMP), designed to create a comprehensive seafloor map of high-resolution bathymetry, marine benthic habitats, and geology within the 3-nautical-mile limit of California’s State Waters. The CSMP approach is to create highly detailed seafloor maps through collection, integration, interpretation, and visualization of swath sonar data, acoustic backscatter, seafloor video, seafloor photography, high-resolution seismic-reflection profiles, and bottom-sediment sampling data. The map products display seafloor morphology and character, identify potential marine benthic habitats, and illustrate both the surficial seafloor geology and shallow (to about 100 m) subsurface geology.</p>\n<br/>\n<p>The Offshore of Coal Oil Point map area lies within the central Santa Barbara Channel region of the Southern California Bight. This geologically complex region forms a major biogeographic transition zone, separating the cold-temperate Oregonian province north of Point Conception from the warm-temperate California province to the south. The map area is in the southern part of the Western Transverse Ranges geologic province, which is north of the California Continental Borderland. Significant clockwise rotation—at least 90°—since the early Miocene has been proposed for the Western Transverse Ranges province, and geodetic studies indicate that the region is presently undergoing north-south shortening. Uplift rates (as much as 2.0 mm/yr) that are based on studies of onland marine terraces provide further evidence of significant shortening.</p>\n<br/>\n<p>The cities of Goleta and Isla Vista, the main population centers in the map area, are in the western part of a contiguous urban area that extends eastward through Santa Barbara to Carpinteria. This urban area is on the south flank of the east-west-trending Santa Ynez Mountains, on coalescing alluvial fans and uplifted marine terraces underlain by folded and faulted Miocene bedrock. In the map area, the relatively low-relief, elevated coastal bajada narrows from about 2.5 km wide in the east to less than 500 m wide in the west. Several beaches line the actively utilized coastal zone, including Isla Vista County Park beach, Coal Oil Point Reserve, and Goleta Beach County Park. The beaches are subject to erosion each winter during storm-wave attack, and then they undergo gradual recovery or accretion during the more gentle wave climate of the late spring, summer, and fall months.</p>\n<br/>\n<p>The Offshore of Coal Oil Point map area lies in the central part of the Santa Barbara littoral cell, which is characterized by littoral drift to the east-southeast. Longshore drift rates have been reported to range from about 160,000 to 800,000 tons/yr, averaging 400,000 tons/yr. Sediment supply to the western and central parts of the littoral cell, including the map area, is largely from relatively small transverse coastal watersheds. Within the map area, these coastal watersheds include (from east to west) Las Llagas Canyon, Gato Canyon, Las Varas Canyon, Dos Pueblos Canyon, Eagle Canyon, Tecolote Canyon, Winchester Canyon, Ellwood Canyon, Glen Annie Canyon, and San Jose Creek. The Santa Ynez and Santa Maria Rivers, the mouths of which are about 100 to 140 km northwest of the map area, are not significant sediment sources because Point Conception and Point Arguello provide obstacles to downcoast sediment transport and also because much of their sediment load is trapped in dams. The Ventura and Santa Clara Rivers, the mouths of which are about 45 to 55 km southeast of the map area, are much larger sediment sources. Still farther east, eastward-moving sediment in the littoral cell is trapped by Hueneme and Mugu Canyons and then transported to the deep-water Santa Monica Basin.</p>\n<br/>\n<p>The offshore part of the map area consists of a relatively flat and shallow continental shelf, which dips gently seaward (about 0.8° to 1.0°) so that water depths at the shelf break, roughly coincident with the California’s State Waters limit, are about 90 m. This part of the Santa Barbara Channel is relatively well protected from large Pacific swells from the north and northwest by Point Conception and from the south and southwest by offshore islands and banks. The shelf is underlain by variable amounts of upper Quaternary marine and fluvial sediments deposited as sea level fluctuated in the late Pleistocene.</p>\n<br/>\n<p>The large (130 km2) Goleta landslide complex lies along the shelf break in the southern part of the map area. This compound slump complex may have been initiated more than 200,000 years ago, but it also includes three recent failures that may have been generated between 8,000 to 10,000 years ago. A local, 5- to 10-m-high tsunami may have been generated from these failure events.</p>\n<br/>\n<p>The map area has had a long history of hydrocarbon development, which began in 1928 with discovery of the Ellwood oil field. Subsequent discoveries in the offshore include South Ellwood offshore oil field, Coal Oil Point oil field, and Naples oil and gas field. Development of South Ellwood offshore field began in 1966 from platform “Holly,” the last platform to be installed in California’s State Waters. The area also is known for “the world’s most spectacular marine hydrocarbon seeps,” and large tar seeps are exposed on beaches east of the mouth of Goleta Slough. Offshore seeps adjacent to South Ellwood oil field release about 40 tons per day of methane and about 19 tons per day of ethane, propane, butane, and higher hydrocarbons.</p>\n<br/>\n<p>Seafloor habitats in the broad Santa Barbara Channel region consist of significant amounts of soft sediment and isolated areas of rocky habitat that support kelp-forest communities nearshore and rocky-reef communities in deep water. The potential marine benthic habitat types mapped in the Offshore of Coal Oil Point map area are directly related to its Quaternary geologic history, geomorphology, and active sedimentary processes. These potential habitats, which lie primarily within the Shelf (continental shelf) but also partly within the Flank (basin flank or continental slope) megahabitats, range from soft, unconsolidated sediment to hard sedimentary bedrock. This heterogeneous seafloor provides promising habitat for rockfish, groundfish, crabs, shrimp, and other marine benthic organisms.</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/sim3302","usgsCitation":"Johnson, S.Y., Dartnell, P., Cochrane, G.R., Golden, N., Phillips, E., Ritchie, A.C., Kvitek, R.G., Dieter, B., Conrad, J.E., Lorenson, T., Krigsman, L., Greene, H., Endris, C.A., Seitz, G., Finlayson, D.P., Sliter, R.W., Wong, F.L., Erdey, M.D., Gutierrez, C.I., Leifer, I., Yoklavich, M.M., Draut, A.E., Hart, P.E., Hostettler, F.D., Peters, K., Kvenvolden, K.A., Rosenbauer, R.J., and Fong, G., 2014, California State Waters Map Series: Offshore of Coal Oil Point, California: U.S. Geological Survey Scientific Investigations Map 3302, Pamphlet: v, 57 p.; 12 Sheets: 55.0 x 36.0 inches or smaller; Metadata; Data Catalog, https://doi.org/10.3133/sim3302.","productDescription":"Pamphlet: v, 57 p.; 12 Sheets: 55.0 x 36.0 inches 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}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53e5d62fe4b0b6c2798a65c5","contributors":{"editors":[{"text":"Johnson, Samuel Y. 0000-0001-7972-9977 sjohnson@usgs.gov","orcid":"https://orcid.org/0000-0001-7972-9977","contributorId":2607,"corporation":false,"usgs":true,"family":"Johnson","given":"Samuel","email":"sjohnson@usgs.gov","middleInitial":"Y.","affiliations":[{"id":520,"text":"Pacific Coastal and Marine Science Center","active":true,"usgs":true}],"preferred":true,"id":509856,"contributorType":{"id":2,"text":"Editors"},"rank":1},{"text":"Cochran, Susan A.","contributorId":27533,"corporation":false,"usgs":true,"family":"Cochran","given":"Susan A.","affiliations":[],"preferred":false,"id":509857,"contributorType":{"id":2,"text":"Editors"},"rank":2}],"authors":[{"text":"Johnson, Samuel Y. 0000-0001-7972-9977 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,{"id":70117567,"text":"ofr20141156 - 2014 - Karst in the United States: A digital map compilation and database","interactions":[],"lastModifiedDate":"2020-03-27T06:28:59","indexId":"ofr20141156","displayToPublicDate":"2014-08-07T10:26:00","publicationYear":"2014","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2014-1156","title":"Karst in the United States: A digital map compilation and database","docAbstract":"<p>This report describes new digital maps delineating areas of the United States, including Puerto Rico and the U.S. Virgin Islands, having karst or the potential for development of karst and pseudokarst. These maps show areas underlain by soluble rocks and also by volcanic rocks, sedimentary deposits, and permafrost that have potential for karst or pseudokarst development. All 50 States contain rocks with potential for karst development, and about 18 percent of their area is underlain by soluble rocks having karst or the potential for development of karst features. The areas of soluble rocks shown are based primarily on selection from State geologic maps of rock units containing significant amounts of carbonate or evaporite minerals. Areas underlain by soluble rocks are further classified by general climate setting, degree of induration, and degree of exposure. Areas having potential for volcanic pseudokarst are those underlain chiefly by basaltic-flow rocks no older than Miocene in age. Areas with potential for pseudokarst features in sedimentary rocks are in relatively unconsolidated rocks from which pseudokarst features, such as piping caves, have been reported. Areas having potential for development of thermokarst features, mapped exclusively in Alaska, contain permafrost in relatively thick surficial deposits containing ground ice. This report includes a GIS database with links from the map unit polygons to online geologic unit descriptions.</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr20141156","usgsCitation":"Weary, D.J., and Doctor, D.H., 2014, Karst in the United States: A digital map compilation and database: U.S. Geological Survey Open-File Report 2014-1156, Report: iv, 23 p.; 6 Figures; Downloads Directory, https://doi.org/10.3133/ofr20141156.","productDescription":"Report: iv, 23 p.; 6 Figures; Downloads Directory","numberOfPages":"27","onlineOnly":"Y","ipdsId":"IP-052217","costCenters":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true},{"id":40020,"text":"Florence Bascom Geoscience Center","active":true,"usgs":true}],"links":[{"id":291826,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr20141156.jpg"},{"id":373540,"rank":11,"type":{"id":20,"text":"Read Me"},"url":"https://pubs.usgs.gov/of/2014/1156/downloads/README.txt","linkFileType":{"id":2,"text":"txt"}},{"id":291823,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2014/1156/"},{"id":291825,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2014/1156/pdf/of2014-1156.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":291824,"type":{"id":7,"text":"Companion Files"},"url":"https://pubs.usgs.gov/of/2014/1156/downloads","text":"Downloads Directory"},{"id":373534,"rank":5,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/2014/1156/pdf/of2014-1156_hi-res-pdfs/of2014-1156_figure_1.pdf","text":"Figure 1","linkFileType":{"id":1,"text":"pdf"}},{"id":373535,"rank":6,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/2014/1156/pdf/of2014-1156_hi-res-pdfs/of2014-1156_figure_2.pdf","text":"Figure 2","linkFileType":{"id":1,"text":"pdf"}},{"id":373539,"rank":10,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/2014/1156/pdf/of2014-1156_hi-res-pdfs/of2014-1156_figure_6.pdf","text":"Figure 6","linkFileType":{"id":1,"text":"pdf"}},{"id":373536,"rank":7,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/2014/1156/pdf/of2014-1156_hi-res-pdfs/of2014-1156_figure_3.pdf","text":"Figure 3","linkFileType":{"id":1,"text":"pdf"}},{"id":373537,"rank":8,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/2014/1156/pdf/of2014-1156_hi-res-pdfs/of2014-1156_figure_4.pdf","text":"Figure 4","linkFileType":{"id":1,"text":"pdf"}},{"id":373538,"rank":9,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/2014/1156/pdf/of2014-1156_hi-res-pdfs/of2014-1156_figure_5.pdf","text":"Figure 5","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -124.8,24.5 ], [ -124.8,49.383333 ], [ -66.95,49.383333 ], [ -66.95,24.5 ], [ -124.8,24.5 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53e484b6e4b0fff4042801c5","contributors":{"authors":[{"text":"Weary, David J. 0000-0002-6115-6397 dweary@usgs.gov","orcid":"https://orcid.org/0000-0002-6115-6397","contributorId":545,"corporation":false,"usgs":true,"family":"Weary","given":"David","email":"dweary@usgs.gov","middleInitial":"J.","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":496021,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Doctor, Daniel H. 0000-0002-8338-9722 dhdoctor@usgs.gov","orcid":"https://orcid.org/0000-0002-8338-9722","contributorId":2037,"corporation":false,"usgs":true,"family":"Doctor","given":"Daniel","email":"dhdoctor@usgs.gov","middleInitial":"H.","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":496022,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70118860,"text":"ofr20141162 - 2014 - Preliminary simulation of chloride transport in the <i>Equus</i> Beds aquifer and simulated effects of well pumping and artificial recharge on groundwater flow and chloride transport near the city of Wichita, Kansas, 1990 through 2008","interactions":[],"lastModifiedDate":"2014-08-07T10:26:26","indexId":"ofr20141162","displayToPublicDate":"2014-08-07T10:18:00","publicationYear":"2014","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2014-1162","title":"Preliminary simulation of chloride transport in the <i>Equus</i> Beds aquifer and simulated effects of well pumping and artificial recharge on groundwater flow and chloride transport near the city of Wichita, Kansas, 1990 through 2008","docAbstract":"<p>The <i>Equus</i> Beds aquifer in south-central Kansas is a primary water-supply source for the city of Wichita. Water-level declines because of groundwater pumping for municipal and irrigation needs as well as sporadic drought conditions have caused concern about the adequacy of the Equus Beds aquifer as a future water supply for Wichita. In March 2006, the city of Wichita began construction of the Equus Beds Aquifer Storage and Recovery project, a plan to artificially recharge the aquifer with excess water from the Little Arkansas River. Artificial recharge will raise groundwater levels, increase storage volume in the aquifer, and deter or slow down a plume of chloride brine approaching the Wichita well field from the Burrton, Kansas area caused by oil production activities in the 1930s. Another source of high chloride water to the aquifer is the Arkansas River. This study was prepared in cooperation with the city of Wichita as part of the Equus Beds Aquifer Storage and Recovery project.</p>\n<br/>\n<p>Chloride transport in the <i>Equus</i> Beds aquifer was simulated between the Arkansas and Little Arkansas Rivers near the Wichita well field. Chloride transport was simulated for the <i>Equus</i> Beds aquifer using SEAWAT, a computer program that combines the groundwater-flow model MODFLOW-2000 and the solute-transport model MT3DMS. The chloride-transport model was used to simulate the period from 1990 through 2008 and the effects of five well pumping scenarios and one artificial recharge scenario. The chloride distribution in the aquifer for the beginning of 1990 was interpolated from groundwater samples from around that time, and the chloride concentrations in rivers for the study period were interpolated from surface water samples.</p>\n<br/>\n<p>Five well-pumping scenarios and one artificial-recharge scenario were assessed for their effects on simulated chloride transport and water levels in and around the Wichita well field. The scenarios were: (1) existing 1990 through 2008 pumping conditions, to serve as a baseline scenario for comparison with the hypothetical scenarios; (2) no pumping in the model area, to demonstrate the chloride movement without the influence of well pumping; (3) double municipal pumping from the Wichita well field with existing irrigation pumping; (4) existing municipal pumping with no irrigation pumping in the model area; (5) double municipal pumping in the Wichita well field and no irrigation pumping in the model area; and (6) increasing artificial recharge to the Phase 1 Artificial Storage and Recovery project sites by 2,300 acre-feet per year.</p>\n<br/>\n<p>The effects of the hypothetical pumping and artificial recharge scenarios on simulated chloride transport were measured by comparing the rate of movement of the 250-milligrams-per-liter-chloride front for each hypothetical scenario with the baseline scenario at the Arkansas River area near the southern part of the Wichita well field and the Burrton plume area. The scenarios that increased the rate of movement the most compared to the baseline scenario of existing pumping between the Arkansas River and the southern boundary of the well field were those that doubled the city of Wichita’s pumping from the well field (scenarios 3 and 5), increasing the rate of movement by 50 to 150 feet per year, with the highest rate increases in the shallow layer and the lowest rate increases in the deepest layer. The no pumping and no irrigation pumping scenarios (2 and 4) slowed the rate of movement in this area by 150 to 210 feet per year and 40 to 70 feet per year, respectively. In the double Wichita pumping scenario (3), the rate of movement in the shallow layer of the Burrton area decreased by about 50 feet per year. Simulated chloride rate of movement in the deeper layers of the Burrton area was decreased in the no pumping and no irrigation scenarios (2 and 4) by 80 to 120 feet per year and 50 feet per year, respectively, and increased in the scenarios that double Wichita’s pumping (3 and 5) from the well field by zero to 130 feet per year, with the largest increases in the deepest layer. In the increased Phase 1 artificial recharge scenario (6), the rate of chloride movement in the Burrton area increased in the shallow layer by about 30 feet per year, and decreased in the middle and deepest layer by about 10 and 60 feet per year, respectively. Comparisons of the rate of movement of the simulated 250-milligrams-per-liter-chloride front in the hypothetical scenarios to the baseline scenario indicated that, in general, increases to pumping in the well field area increased the rate of simulated chloride movement toward the well field area by as much as 150 feet per year. Reductions in pumping slowed the advance of chloride toward the well field by as much as 210 feet per year, although reductions did not stop the movement of chloride toward the well field, including when pumping rates were eliminated. If pumping is completely discontinued, the rate of chloride movement is about 500 to 600 feet per year in the area between the Arkansas River and the southern part of the Wichita well field, and 70 to 500 feet per year in the area near Burrton with the highest rate of movement in the shallow aquifer layer.</p>\n<br/>\n<p>The averages of simulated water-levels in index monitoring wells in the Wichita well field at the end of 2008 were calculated for each scenario. Compared to the baseline scenario, the average simulated water level was 5.05 feet higher for the no pumping scenario, 4.72 feet lower for the double Wichita pumping with existing irrigation scenario, 2.49 feet higher for the no irrigation pumping with existing Wichita pumping scenario, 1.53 feet lower for the double Wichita pumping with no irrigation scenario, and 0.48 feet higher for the increased Phase 1 artificial recharge scenario.</p>\n<br/>\n<p>The groundwater flow was simulated with a preexisting groundwater-flow model, which was not altered to calibrate the solute-transport model to observed chloride-concentration data. Therefore, some areas in the model had poor fit between simulated chloride concentrations and observed chloride concentrations, including the area between Arkansas River and the southern part of the Wichita well field, and the Hollow-Nikkel area about 6 miles north of Burrton. Compared to the interpreted location of the 250-milligrams per liter-chloride front based on data collected in 2011, in the Arkansas River area the simulated 250-milligrams per liter-chloride front moved from the river toward the well field about twice the rate of the actual 250-milligrams per liter-chloride front in the shallow layer and about four times the rate of the actual 250-milligrams per liter-chloride front in the deep layer. Future groundwater-flow and chloride-transport modeling efforts may achieve better agreement between observed and simulated chloride concentrations in these areas by taking the chloride-transport model fit into account when adjusting parameters such as hydraulic conductivity, riverbed conductance, and effective porosity during calibration.</p>\n<br/>\n<p>Results of the hypothetical scenarios simulated indicate that the Burrton chloride plume will continue moving toward the well field regardless of pumping in the area and that one alternative may be to increase pumping from within the plume area to reverse the groundwater-flow gradients and remove the plume. Additionally, the results of modeling these scenarios indicate that eastward movement of the Burrton plume could be slowed by the additional artificial recharge at the Phase 1 sites and that decreasing pumping along the Arkansas River or increasing water levels could retard the movement of chloride and may prevent further encroachment into the southern part of the well field area.</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr20141162","collaboration":"In cooperation with the City of Wichita","usgsCitation":"Klager, B.J., Kelly, B.P., and Ziegler, A., 2014, Preliminary simulation of chloride transport in the <i>Equus</i> Beds aquifer and simulated effects of well pumping and artificial recharge on groundwater flow and chloride transport near the city of Wichita, Kansas, 1990 through 2008: U.S. Geological Survey Open-File Report 2014-1162, Report: viii, 76 p.; Appendix 1, https://doi.org/10.3133/ofr20141162.","productDescription":"Report: viii, 76 p.; Appendix 1","numberOfPages":"84","onlineOnly":"Y","additionalOnlineFiles":"Y","temporalStart":"1990-01-01","temporalEnd":"2008-12-31","ipdsId":"IP-052749","costCenters":[{"id":353,"text":"Kansas Water Science Center","active":false,"usgs":true}],"links":[{"id":291822,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr20141162.jpg"},{"id":291821,"type":{"id":3,"text":"Appendix"},"url":"https://pubs.usgs.gov/of/2014/1162/downloads/"},{"id":291819,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2014/1162/pdf/ofr2014-1162.pdf"},{"id":291804,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2014/1162/"}],"projection":"Universal Transverse Mercator projection, Zone 14","datum":"North American Datum of 1983","country":"United States","state":"Kansas","city":"Wichita","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -98.333333,37.633333 ], [ -98.333333,38.5 ], [ -97.0,38.5 ], [ -97.0,37.633333 ], [ -98.333333,37.633333 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53e484b6e4b0fff4042801cd","contributors":{"authors":[{"text":"Klager, Brian J. 0000-0001-8361-6043 bklager@usgs.gov","orcid":"https://orcid.org/0000-0001-8361-6043","contributorId":5543,"corporation":false,"usgs":true,"family":"Klager","given":"Brian","email":"bklager@usgs.gov","middleInitial":"J.","affiliations":[{"id":353,"text":"Kansas Water Science Center","active":false,"usgs":true}],"preferred":true,"id":497339,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Kelly, Brian P. 0000-0001-6378-2837 bkelly@usgs.gov","orcid":"https://orcid.org/0000-0001-6378-2837","contributorId":897,"corporation":false,"usgs":true,"family":"Kelly","given":"Brian","email":"bkelly@usgs.gov","middleInitial":"P.","affiliations":[{"id":396,"text":"Missouri Water Science Center","active":true,"usgs":true},{"id":353,"text":"Kansas Water Science Center","active":false,"usgs":true}],"preferred":true,"id":497338,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Ziegler, Andrew C. aziegler@usgs.gov","contributorId":433,"corporation":false,"usgs":true,"family":"Ziegler","given":"Andrew C.","email":"aziegler@usgs.gov","affiliations":[{"id":353,"text":"Kansas Water Science Center","active":false,"usgs":true}],"preferred":false,"id":497337,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":70116916,"text":"fs20143063 - 2014 - Powder X-ray diffraction laboratory, Reston, Virginia","interactions":[],"lastModifiedDate":"2014-08-07T10:14:36","indexId":"fs20143063","displayToPublicDate":"2014-08-07T10:11:00","publicationYear":"2014","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":"2014-3063","title":"Powder X-ray diffraction laboratory, Reston, Virginia","docAbstract":"<p>The powder x-ray diffraction (XRD) laboratory is managed jointly by the Eastern Mineral and Environmental Resources and Eastern Energy Resources Science Centers. Laboratory scientists collaborate on a wide variety of research problems involving other U.S. Geological Survey (USGS) science centers and government agencies, universities, and industry. Capabilities include identification and quantification of crystalline and amorphous phases, and crystallographic and atomic structure analysis for a wide variety of sample media. Customized laboratory procedures and analyses commonly are used to characterize non-routine samples including, but not limited to, organic and inorganic components in petroleum source rocks, ore and mine waste, clay minerals, and glassy phases. Procedures can be adapted to meet a variety of research objectives.</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/fs20143063","usgsCitation":"Piatak, N., Dulong, F.T., Jackson, J.C., and Folger, H.W., 2014, Powder X-ray diffraction laboratory, Reston, Virginia: U.S. Geological Survey Fact Sheet 2014-3063, 2 p., https://doi.org/10.3133/fs20143063.","productDescription":"2 p.","numberOfPages":"2","onlineOnly":"Y","ipdsId":"IP-054045","costCenters":[{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"links":[{"id":291813,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/fs20143063.jpg"},{"id":291811,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/fs/2014/3063/pdf/fs2014-3063.pdf"},{"id":291812,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/fs/2014/3063/"}],"country":"United States","state":"Virginia","city":"Reston","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -77.393259,38.908241 ], [ -77.393259,39.002923 ], [ -77.304864,39.002923 ], [ -77.304864,38.908241 ], [ -77.393259,38.908241 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53e484b6e4b0fff4042801cb","contributors":{"authors":[{"text":"Piatak, Nadine M.","contributorId":23621,"corporation":false,"usgs":true,"family":"Piatak","given":"Nadine M.","affiliations":[],"preferred":false,"id":495892,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dulong, Frank T. 0000-0001-7388-647X fdulong@usgs.gov","orcid":"https://orcid.org/0000-0001-7388-647X","contributorId":650,"corporation":false,"usgs":true,"family":"Dulong","given":"Frank","email":"fdulong@usgs.gov","middleInitial":"T.","affiliations":[{"id":241,"text":"Eastern Energy Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":495889,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Jackson, John C. jjackson@usgs.gov","contributorId":2652,"corporation":false,"usgs":true,"family":"Jackson","given":"John","email":"jjackson@usgs.gov","middleInitial":"C.","affiliations":[{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":495890,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Folger, Helen W. 0000-0003-1376-5996 hfolger@usgs.gov","orcid":"https://orcid.org/0000-0003-1376-5996","contributorId":3219,"corporation":false,"usgs":true,"family":"Folger","given":"Helen","email":"hfolger@usgs.gov","middleInitial":"W.","affiliations":[{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":495891,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}}
,{"id":70119250,"text":"70119250 - 2014 - Refining the link between the Holocene development of the Mississippi River Delta and the geologic evolution of Cat Island, MS: implications for delta-associated barrier islands","interactions":[],"lastModifiedDate":"2014-08-05T15:26:24","indexId":"70119250","displayToPublicDate":"2014-08-05T15:16:00","publicationYear":"2014","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2667,"text":"Marine Geology","active":true,"publicationSubtype":{"id":10}},"title":"Refining the link between the Holocene development of the Mississippi River Delta and the geologic evolution of Cat Island, MS: implications for delta-associated barrier islands","docAbstract":"The geologic evolution of barrier islands is profoundly influenced by the nature of the deposits underlying them. Many researchers have speculated on the origin and evolution of Cat Island in Mississippi, but uncertainty remains about whether or not the island is underlain completely or in part by deposits associated with the past growth of the Mississippi River delta. In part, this is due to a lack of comprehensive geological information offshore of the island that could augment previous stratigraphic interpretations based on terrestrial borings. An extensive survey of Cat Island and its surrounding waters was conducted, including shallow-water geophysics (e.g., high-resolution chirp seismic, side-scan sonar, and swath and single-beam bathymetry) and both terrestrial and marine vibracoring. High-resolution seismic data and vibracores from south and east of the island show two horizontally laminated silt units; marine radiocarbon dates indicate that they are St. Bernard delta complex (SBDC) deposits. Furthermore, seismic data reveal that the SBDC deposits taper off toward the southern shoreline of Cat Island and to the west, morphology consistent with the distal edge of a delta complex. The sedimentology and extent of each unit suggest that the lower unit may have been deposited during an earlier period of continuous river flow while the upper unit may represent reduced or sporadic river flow. OSL dates from the island platform (beneath beach ridge complexes) indicate three stages of terrestrial evolution: island emergence resulting from relative sea-level rise (~ 5400 ybp) island aggradation via littoral transport (~ 2500–4000 ybp) and island degradation due to delta-mediated changes in wave direction (present– ~ 3600 ybp). Finally, the combination of terrestrial and marine data shows that portions of Cat Island that are lower in elevation than the central part of the island are younger and are likely underlain by a thin layer of deltaic sediments. This underscores the potential for increased future vulnerability of barrier islands that develop adjacent to major river delta complexes.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Marine Geology","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisher":"Elsevier","doi":"10.1016/j.margeo.2014.05.021","usgsCitation":"Miselis, J.L., Buster, N.A., and Kindinger, J.L., 2014, Refining the link between the Holocene development of the Mississippi River Delta and the geologic evolution of Cat Island, MS: implications for delta-associated barrier islands: Marine Geology, v. 355, p. 274-290, https://doi.org/10.1016/j.margeo.2014.05.021.","productDescription":"17 p.","startPage":"274","endPage":"290","numberOfPages":"17","ipdsId":"IP-053421","costCenters":[{"id":574,"text":"St. Petersburg Coastal and Marine Science Center","active":true,"usgs":true}],"links":[{"id":291730,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":291722,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1016/j.margeo.2014.05.021"}],"country":"United States","state":"Mississippi","otherGeospatial":"Cat Island;Mississippi River Delta","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -89.2,30.183333 ], [ -89.2,30.266667 ], [ -89.041667,30.266667 ], [ -89.041667,30.183333 ], [ -89.2,30.183333 ] ] ] } } ] }","volume":"355","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53e1e1b4e4b0fe532be24a89","contributors":{"authors":[{"text":"Miselis, Jennifer L. 0000-0002-4925-3979 jmiselis@usgs.gov","orcid":"https://orcid.org/0000-0002-4925-3979","contributorId":3914,"corporation":false,"usgs":true,"family":"Miselis","given":"Jennifer","email":"jmiselis@usgs.gov","middleInitial":"L.","affiliations":[{"id":574,"text":"St. Petersburg Coastal and Marine Science Center","active":true,"usgs":true}],"preferred":true,"id":497629,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Buster, Noreen A. 0000-0001-5069-9284 nbuster@usgs.gov","orcid":"https://orcid.org/0000-0001-5069-9284","contributorId":3750,"corporation":false,"usgs":true,"family":"Buster","given":"Noreen","email":"nbuster@usgs.gov","middleInitial":"A.","affiliations":[{"id":574,"text":"St. Petersburg Coastal and Marine Science Center","active":true,"usgs":true}],"preferred":true,"id":497628,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Kindinger, Jack L. jkindinger@usgs.gov","contributorId":815,"corporation":false,"usgs":true,"family":"Kindinger","given":"Jack","email":"jkindinger@usgs.gov","middleInitial":"L.","affiliations":[{"id":574,"text":"St. Petersburg Coastal and Marine Science Center","active":true,"usgs":true}],"preferred":false,"id":497627,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":70119244,"text":"70119244 - 2014 - Monitoring Everglades freshwater marsh water level using L-band synthetic aperture radar backscatter","interactions":[],"lastModifiedDate":"2014-08-05T15:15:12","indexId":"70119244","displayToPublicDate":"2014-08-05T15:06:00","publicationYear":"2014","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3254,"text":"Remote Sensing of Environment","printIssn":"0034-4257","active":true,"publicationSubtype":{"id":10}},"title":"Monitoring Everglades freshwater marsh water level using L-band synthetic aperture radar backscatter","docAbstract":"The Florida Everglades plays a significant role in controlling floods, improving water quality, supporting ecosystems, and maintaining biodiversity in south Florida. Adaptive restoration and management of the Everglades requires the best information possible regarding wetland hydrology. We developed a new and innovative approach to quantify spatial and temporal variations in wetland water levels within the Everglades, Florida. We observed high correlations between water level measured at in situ gages and L-band SAR backscatter coefficients in the freshwater marsh, though C-band SAR backscatter has no close relationship with water level. Here we illustrate the complementarity of SAR backscatter coefficient differencing and interferometry (InSAR) for improved estimation of high spatial resolution water level variations in the Everglades. This technique has a certain limitation in applying to swamp forests with dense vegetation cover, but we conclude that this new method is promising in future applications to wetland hydrology research.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Remote Sensing of Environment","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisher":"Elsevier","doi":"10.1016/j.rse.2014.03.031","usgsCitation":"Kim, J., Lu, Z., Jones, J., Shum, C., Lee, H., and Jia, Y., 2014, Monitoring Everglades freshwater marsh water level using L-band synthetic aperture radar backscatter: Remote Sensing of Environment, v. 150, p. 66-81, https://doi.org/10.1016/j.rse.2014.03.031.","productDescription":"16 p.","startPage":"66","endPage":"81","numberOfPages":"16","ipdsId":"IP-046291","costCenters":[{"id":242,"text":"Eastern Geographic Science Center","active":true,"usgs":true}],"links":[{"id":291726,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":291700,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1016/j.rse.2014.03.031"}],"country":"United States","state":"Florida","otherGeospatial":"Everglades","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -83.0,23.5 ], [ -83.0,27.5 ], [ -78.0,27.5 ], [ -78.0,23.5 ], [ -83.0,23.5 ] ] ] } } ] }","volume":"150","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53e1e1b4e4b0fe532be24a83","contributors":{"authors":[{"text":"Kim, Jin-Woo","contributorId":69486,"corporation":false,"usgs":true,"family":"Kim","given":"Jin-Woo","affiliations":[],"preferred":false,"id":497614,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lu, Zhong 0000-0001-9181-1818 lu@usgs.gov","orcid":"https://orcid.org/0000-0001-9181-1818","contributorId":901,"corporation":false,"usgs":true,"family":"Lu","given":"Zhong","email":"lu@usgs.gov","affiliations":[],"preferred":true,"id":497610,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Jones, John W. 0000-0001-6117-3691 jwjones@usgs.gov","orcid":"https://orcid.org/0000-0001-6117-3691","contributorId":2220,"corporation":false,"usgs":true,"family":"Jones","given":"John","email":"jwjones@usgs.gov","middleInitial":"W.","affiliations":[{"id":242,"text":"Eastern Geographic Science Center","active":true,"usgs":true},{"id":37786,"text":"WMA - Observing Systems Division","active":true,"usgs":true}],"preferred":true,"id":497611,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Shum, C. K.","contributorId":85373,"corporation":false,"usgs":true,"family":"Shum","given":"C. K.","affiliations":[],"preferred":false,"id":497615,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Lee, Hyongki","contributorId":14748,"corporation":false,"usgs":true,"family":"Lee","given":"Hyongki","email":"","affiliations":[],"preferred":false,"id":497612,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Jia, Yuanyuan","contributorId":35660,"corporation":false,"usgs":true,"family":"Jia","given":"Yuanyuan","email":"","affiliations":[],"preferred":false,"id":497613,"contributorType":{"id":1,"text":"Authors"},"rank":6}]}}
,{"id":70119129,"text":"70119129 - 2014 - Lateral baroclinic forcing enhances sediment transport from shallows to channel in an estuary","interactions":[],"lastModifiedDate":"2017-10-30T11:25:10","indexId":"70119129","displayToPublicDate":"2014-08-05T14:39:00","publicationYear":"2014","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1584,"text":"Estuaries and Coasts","active":true,"publicationSubtype":{"id":10}},"title":"Lateral baroclinic forcing enhances sediment transport from shallows to channel in an estuary","docAbstract":"We investigate the dynamics governing exchange of sediment between estuarine shallows and the channel based on field measurements at eight stations spanning the interface between the channel and the extensive eastern shoals of South San Francisco Bay. The study site is characterized by longitudinally homogeneous bathymetry and a straight channel, with friction more important than the Coriolis forcing. Data were collected for 3 weeks in the winter and 4 weeks in the late summer of 2009, to capture a range of hydrologic and meteorologic conditions. The greatest sediment transport from shallows to channel occurred during a pair of strong, late-summer wind events, with westerly winds exceeding 10 m/s for more than 24 h. A combination of wind-driven barotropic return flow and lateral baroclinic circulation caused the transport. The lateral density gradient was produced by differences in temperature and suspended sediment concentration (SSC). During the wind events, SSC-induced vertical density stratification limited turbulent mixing at slack tides in the shallows, increasing the potential for two-layer exchange. The temperature- and SSC-induced lateral density gradient was comparable in strength to salinity-induced gradients in South Bay produced by seasonal freshwater inflows, but shorter in duration. In the absence of a lateral density gradient, suspended sediment flux at the channel slope was directed towards the shallows, both in winter and during summer sea breeze conditions, indicating the importance of baroclinically driven exchange to supply of sediment from the shallows to the channel in South San Francisco Bay and systems with similar bathymetry.","language":"English","publisher":"Springer","doi":"10.1007/s12237-013-9748-3","usgsCitation":"Lacy, J.R., Gladding, S., Brand, A., Collignon, A., and Stacey, M., 2014, Lateral baroclinic forcing enhances sediment transport from shallows to channel in an estuary: Estuaries and Coasts, v. 37, no. 5, p. 1058-1077, https://doi.org/10.1007/s12237-013-9748-3.","productDescription":"20 p.","startPage":"1058","endPage":"1077","ipdsId":"IP-044083","costCenters":[{"id":520,"text":"Pacific Coastal and Marine Science Center","active":true,"usgs":true},{"id":552,"text":"San Francisco Bay-Delta","active":false,"usgs":true}],"links":[{"id":291723,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"South San Francisco Bay","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -122.262079,37.550057 ], [ -122.262079,37.610474 ], [ -122.16324,37.610474 ], [ -122.16324,37.550057 ], [ -122.262079,37.550057 ] ] ] } } ] }","volume":"37","issue":"5","noUsgsAuthors":false,"publicationDate":"2014-01-15","publicationStatus":"PW","scienceBaseUri":"53e1e1b4e4b0fe532be24a7d","contributors":{"authors":[{"text":"Lacy, Jessica R. 0000-0002-2797-6172 jlacy@usgs.gov","orcid":"https://orcid.org/0000-0002-2797-6172","contributorId":3158,"corporation":false,"usgs":true,"family":"Lacy","given":"Jessica","email":"jlacy@usgs.gov","middleInitial":"R.","affiliations":[{"id":520,"text":"Pacific Coastal and Marine Science Center","active":true,"usgs":true}],"preferred":true,"id":497576,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Gladding, Steve","contributorId":54481,"corporation":false,"usgs":false,"family":"Gladding","given":"Steve","email":"","affiliations":[{"id":12776,"text":"Department of Civil and Environmental Engineering,  University of California, Berkeley, California, USA","active":true,"usgs":false}],"preferred":false,"id":497579,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Brand, Andreas","contributorId":32415,"corporation":false,"usgs":false,"family":"Brand","given":"Andreas","email":"","affiliations":[{"id":12775,"text":"Department of Surface Waters – Research and Management, Swiss Federal Institute of Aquatic Science and Technology (Eawag), Kastanienbaum, Switzerland","active":true,"usgs":false}],"preferred":false,"id":497577,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Collignon, Audric","contributorId":42895,"corporation":false,"usgs":true,"family":"Collignon","given":"Audric","email":"","affiliations":[],"preferred":false,"id":497578,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Stacey, Mark T.","contributorId":94531,"corporation":false,"usgs":false,"family":"Stacey","given":"Mark T.","affiliations":[{"id":12776,"text":"Department of Civil and Environmental Engineering,  University of California, Berkeley, California, USA","active":true,"usgs":false}],"preferred":false,"id":497580,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}}
,{"id":70100259,"text":"70100259 - 2014 - Spatial extent and dissipation of the deep chlorophyll layer in Lake Ontario during the Lake Ontario lower foodweb assessment, 2003 and 2008","interactions":[],"lastModifiedDate":"2017-10-20T11:03:46","indexId":"70100259","displayToPublicDate":"2014-08-01T15:31:00","publicationYear":"2014","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":865,"text":"Aquatic Ecosystem Health & Management","active":true,"publicationSubtype":{"id":10}},"title":"Spatial extent and dissipation of the deep chlorophyll layer in Lake Ontario during the Lake Ontario lower foodweb assessment, 2003 and 2008","docAbstract":"<p><span>Increasing water clarity in Lake Ontario has led to a vertical redistribution of phytoplankton and an increased importance of the deep chlorophyll layer in overall primary productivity. We used in situ fluorometer profiles collected in lakewide surveys of Lake Ontario in 2008 to assess the spatial extent and intensity of the deep chlorophyll layer. In situ fluorometer data were corrected with extracted chlorophyll data using paired samples from Lake Ontario collected in August 2008. The deep chlorophyll layer was present offshore during the stratified conditions of late July 2008 with maximum values from 4-13&nbsp;μg l<sup>-</sup></span><sup>1</sup><span> corrected chlorophyll </span><i>a</i><span> at 10 to 17&nbsp;m depth within the metalimnion. Deep chlorophyll layer was closely associated with the base of the thermocline and a subsurface maximum of dissolved oxygen, indicating the feature's importance as a growth and productivity maximum. Crucial to the deep chlorophyll layer formation, the photic zone extended deeper than the surface mixed layer in mid-summer. The layer extended through most of the offshore in July 2008, but was not present in the easternmost transect that had a deeper surface mixed layer. By early September 2008, the lakewide deep chlorophyll layer had dissipated. A similar formation and dissipation was observed in the lakewide survey of Lake Ontario in 2003.</span></p>","language":"English","publisher":"Taylor & Francis","doi":"10.1080/14634988.2014.937316","usgsCitation":"Watkins, J., Weidel, B.M., Rudstam, L., and Holek, K.T., 2014, Spatial extent and dissipation of the deep chlorophyll layer in Lake Ontario during the Lake Ontario lower foodweb assessment, 2003 and 2008: Aquatic Ecosystem Health & Management, v. 18, no. 1, p. 18-27, https://doi.org/10.1080/14634988.2014.937316.","productDescription":"10 p.","startPage":"18","endPage":"27","ipdsId":"IP-050791","costCenters":[{"id":324,"text":"Great Lakes Science Center","active":true,"usgs":true}],"links":[{"id":294944,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Canada, United States","otherGeospatial":"Lake Ontario","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": 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,{"id":70155212,"text":"70155212 - 2014 - Estimating earthquake magnitudes from reported intensities in the central and eastern United States","interactions":[],"lastModifiedDate":"2016-11-09T12:17:29","indexId":"70155212","displayToPublicDate":"2014-08-01T12:15:00","publicationYear":"2014","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":"Estimating earthquake magnitudes from reported intensities in the central and eastern United States","docAbstract":"<p><span>A new macroseismic intensity prediction equation is derived for the central and eastern United States and is used to estimate the magnitudes of the 1811&ndash;1812 New Madrid, Missouri, and 1886 Charleston, South Carolina, earthquakes. This work improves upon previous derivations of intensity prediction equations by including additional intensity data, correcting magnitudes in the intensity datasets to moment magnitude, and accounting for the spatial and temporal population distributions. The new relation leads to moment magnitude estimates for the New Madrid earthquakes that are toward the lower range of previous studies. Depending on the intensity dataset to which the new macroseismic intensity prediction equation is applied, mean estimates for the 16 December 1811, 23 January 1812, and 7 February 1812 mainshocks, and 16 December 1811 dawn aftershock range from 6.9 to 7.1, 6.8 to 7.1, 7.3 to 7.6, and 6.3 to 6.5, respectively. One‐sigma uncertainties on any given estimate could be as high as 0.3&ndash;0.4 magnitude units. We also estimate a magnitude of 6.9&plusmn;0.3 for the 1886 Charleston, South Carolina, earthquake. We find a greater range of magnitude estimates when also accounting for multiple macroseismic intensity prediction equations. The inability to accurately and precisely ascertain magnitude from intensities increases the uncertainty of the central United States earthquake hazard by nearly a factor of two. Relative to the 2008 national seismic hazard maps, our range of possible 1811&ndash;1812 New Madrid earthquake magnitudes increases the coefficient of variation of seismic hazard estimates for Memphis, Tennessee, by 35%&ndash;42% for ground motions expected to be exceeded with a 2% probability in 50 years and by 27%&ndash;35% for ground motions expected to be exceeded with a 10% probability in 50 years.</span></p>","language":"English","publisher":"Seismological Society of America","publisherLocation":"Stanford, CA","doi":"10.1785/0120120352","usgsCitation":"Boyd, O.S., and Cramer, C.H., 2014, Estimating earthquake magnitudes from reported intensities in the central and eastern United States: Bulletin of the Seismological Society of America, v. 104, no. 4, p. 1709-1722, https://doi.org/10.1785/0120120352.","productDescription":"14 p.","startPage":"1709","endPage":"1722","numberOfPages":"14","onlineOnly":"N","additionalOnlineFiles":"N","ipdsId":"IP-055669","costCenters":[{"id":300,"text":"Geologic Hazards Science Center","active":true,"usgs":true}],"links":[{"id":306314,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"104","issue":"4","publishingServiceCenter":{"id":2,"text":"Denver PSC"},"noUsgsAuthors":false,"publicationDate":"2014-07-15","publicationStatus":"PW","scienceBaseUri":"55c090ade4b033ef52104293","contributors":{"authors":[{"text":"Boyd, Oliver S. 0000-0001-9457-0407 olboyd@usgs.gov","orcid":"https://orcid.org/0000-0001-9457-0407","contributorId":140739,"corporation":false,"usgs":true,"family":"Boyd","given":"Oliver","email":"olboyd@usgs.gov","middleInitial":"S.","affiliations":[{"id":234,"text":"Earthquake Hazards Program","active":true,"usgs":true},{"id":237,"text":"Earthquake Science Center","active":true,"usgs":true},{"id":300,"text":"Geologic Hazards Science Center","active":true,"usgs":true}],"preferred":true,"id":565106,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Cramer, Chris H.","contributorId":32196,"corporation":false,"usgs":true,"family":"Cramer","given":"Chris","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":565107,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70123176,"text":"70123176 - 2014 - Synthesis of thirty years of surface water quality and aquatic biota data in Shenandoah National Park: Collaboration between the US Geological Survey and the National Park Service","interactions":[],"lastModifiedDate":"2017-03-27T13:57:08","indexId":"70123176","displayToPublicDate":"2014-08-01T11:27:00","publicationYear":"2014","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3561,"text":"The George Wright Forum","active":true,"publicationSubtype":{"id":10}},"title":"Synthesis of thirty years of surface water quality and aquatic biota data in Shenandoah National Park: Collaboration between the US Geological Survey and the National Park Service","docAbstract":"The eastern United States has been the recipient of acidic atmospheric deposition (hereinafter, “acid rain”) for many decades. Deleterious effects of acid rain on natural resources have been well documented for surface water (e.g., Likens et al. 1996; Stoddard et al. 2001), soils (Bailey et al. 2005), forest health (Long et al. 2009), and habitat suitability for stream biota (Baker et al. 1993). Shenandoah National Park (SNP) is located in northern and central Virginia and consists of a long, narrow strip of land straddling the Blue Ridge Mountains (Figure 1). The park’s elevated topography and location downwind of the Ohio River valley, where many acidic emissions to the atmosphere are generated (NSTC 2005), have made it a target for acid rain. Characterizing the link between air quality and water quality as related to acid rain, contaminants, soil conditions, and forest health is a high priority for research and monitoring in SNP. The US Geological Survey (USGS) and SNP have had a long history of collaboration on documenting acid rain effects on the park’s natural resources, starting in 1985 and continuing to the present (Lynch and Dise 1985; Rice et al. 2001, 2004, 2005, 2007; Deviney et al. 2006, 2012; Jastram et al. 2013).","language":"English","publisher":"George Wright Society","issn":"0732-4715","usgsCitation":"Rice, K.C., Jastram, J.D., Wofford, J.E., and Schaberl, J.P., 2014, Synthesis of thirty years of surface water quality and aquatic biota data in Shenandoah National Park: Collaboration between the US Geological Survey and the National Park Service: The George Wright Forum, v. 31, no. 2, p. 198-204.","productDescription":"7 p.","startPage":"198","endPage":"204","ipdsId":"IP-055092","costCenters":[{"id":614,"text":"Virginia Water Science 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,{"id":70099391,"text":"ofr20141063 - 2014 - Preliminary geologic map of the eastern Willapa Hills, Cowlitz, Lewis, and Wahkiakum Counties, Washington","interactions":[{"subject":{"id":47216,"text":"ofr81674 - 1981 - Geologic map of the eastern Willapa Hills, Cowlitz, Lewis, Pacific, and Wahkiakum counties, Washington","indexId":"ofr81674","publicationYear":"1981","noYear":false,"title":"Geologic map of the eastern Willapa Hills, Cowlitz, Lewis, Pacific, and Wahkiakum counties, Washington"},"predicate":"SUPERSEDED_BY","object":{"id":70099391,"text":"ofr20141063 - 2014 - Preliminary geologic map of the eastern Willapa Hills, Cowlitz, Lewis, and Wahkiakum Counties, Washington","indexId":"ofr20141063","publicationYear":"2014","noYear":false,"title":"Preliminary geologic map of the eastern Willapa Hills, Cowlitz, Lewis, and Wahkiakum Counties, Washington"},"id":1}],"lastModifiedDate":"2023-05-26T15:23:05.59424","indexId":"ofr20141063","displayToPublicDate":"2014-08-01T08:52:00","publicationYear":"2014","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2014-1063","title":"Preliminary geologic map of the eastern Willapa Hills, Cowlitz, Lewis, and Wahkiakum Counties, Washington","docAbstract":"This digital map database and the PDF derived from the database were created from the analog geologic map: Wells, R.E. (1981), “Geologic map of the eastern Willapa Hills, Cowlitz, Lewis, and Wahkiakum Counties, Washington.” The geodatabase replicates the geologic mapping of the 1981 report with minor exceptions along water boundaries and also along the north and south map boundaries. Slight adjustments to contacts along water boundaries were made to correct differences between the topographic base map used in the 1981 compilation (analog USGS 15-minute series quadrangle maps at 1:62,500 scale) and the base map used for this digital compilation (scanned USGS 7.5-minute series quadrangle maps at 1:24,000 scale). These minor adjustments, however, did not materially alter the geologic map. No new field mapping was performed to create this digital map database, and no attempt was made to fit geologic contacts to the new 1:24,000 topographic base, except as noted above. We corrected typographical errors, formatting errors, and attribution errors (for example, the name change of Goble Volcanics to Grays River Volcanics following current State of Washington usage; Walsh and others, 1987). We also updated selected references, substituted published papers for abstracts, and cited published radiometric ages for the volcanic and plutonic rocks. The reader is referred to Magill and others (1982), Wells and Coe (1985), Walsh and others (1987), Moothart (1993), Payne (1998), Kleibacker (2001), McCutcheon (2003), Wells and others (2009), Chan and others (2012), and Wells and others (in press) for subsequent interpretations of the Willapa Hills geology.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr20141063","collaboration":"Prepared in cooperation with the State of Washington Department of Natural Resources, Division of Geology and Earth Resources","usgsCitation":"Wells, R., and Sawlan, M.G., 2014, Preliminary geologic map of the eastern Willapa Hills, Cowlitz, Lewis, and Wahkiakum Counties, Washington: U.S. Geological Survey Open-File Report 2014-1063, 2 Sheets: 33.36 x 51.01 inches and 31.54 and 33.49 inches; Database; Shape Files; Metadata, https://doi.org/10.3133/ofr20141063.","productDescription":"2 Sheets: 33.36 x 51.01 inches and 31.54 and 33.49 inches; Database; Shape Files; Metadata","onlineOnly":"Y","additionalOnlineFiles":"Y","ipdsId":"IP-053867","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":291508,"rank":6,"type":{"id":23,"text":"Spatial Data"},"url":"https://pubs.usgs.gov/of/2014/1063/downloads/ofr2014-1063_shp.zip"},{"id":291506,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/2014/1063/pdf/ofr2014-1063_sheet2.pdf"},{"id":291510,"rank":7,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr20141063.jpg"},{"id":398954,"rank":8,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_100480.htm"},{"id":291501,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2014/1063/"},{"id":291505,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/2014/1063/pdf/ofr2014-1063_sheet1.pdf"},{"id":291509,"rank":3,"type":{"id":16,"text":"Metadata"},"url":"https://pubs.usgs.gov/of/2014/1063/downloads/metadata/"},{"id":291507,"rank":1,"type":{"id":9,"text":"Database"},"url":"https://pubs.usgs.gov/of/2014/1063/downloads/ofr2014-1063_db.zip"}],"scale":"50000","projection":"Universal Transverse Mercator projection","country":"United States","state":"Washington","county":"Cowlitz County, Lewis County, Wahkiakum County","otherGeospatial":"Willapa Hills","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -123.5,46.1425 ], [ -123.5,46.636944 ], [ -123.0,46.636944 ], [ -123.0,46.1425 ], [ -123.5,46.1425 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53dc9bafe4b076157862d964","contributors":{"authors":[{"text":"Wells, Ray E. 0000-0002-7796-0160 rwells@usgs.gov","orcid":"https://orcid.org/0000-0002-7796-0160","contributorId":2692,"corporation":false,"usgs":true,"family":"Wells","given":"Ray E.","email":"rwells@usgs.gov","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":false,"id":491973,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Sawlan, Michael G. 0000-0003-0637-2051 msawlan@usgs.gov","orcid":"https://orcid.org/0000-0003-0637-2051","contributorId":2291,"corporation":false,"usgs":true,"family":"Sawlan","given":"Michael","email":"msawlan@usgs.gov","middleInitial":"G.","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":491972,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70120181,"text":"70120181 - 2014 - Time-averaged discharge rate of subaerial lava at Kīlauea Volcano, Hawai‘i, measured from TanDEM-X interferometry: Implications for magma supply and storage during 2011-2013","interactions":[],"lastModifiedDate":"2019-03-13T15:06:08","indexId":"70120181","displayToPublicDate":"2014-08-01T08:51:24","publicationYear":"2014","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2314,"text":"Journal of Geophysical Research B: Solid Earth","active":true,"publicationSubtype":{"id":10}},"title":"Time-averaged discharge rate of subaerial lava at Kīlauea Volcano, Hawai‘i, measured from TanDEM-X interferometry: Implications for magma supply and storage during 2011-2013","docAbstract":"<p>Differencing digital elevation models (DEMs) derived from TerraSAR add-on for Digital Elevation Measurements (TanDEM-X) synthetic aperture radar imagery provides a measurement of elevation change over time. On the East Rift Zone (EZR) of Kīlauea Volcano, Hawai&lsquo;i, the effusion of lava causes changes in topography. When these elevation changes are summed over the area of an active lava flow, it is possible to quantify the volume of lava emplaced at the surface during the time spanned by the TanDEM-X data&mdash;a parameter that can be difficult to measure across the entirety of an ~100&thinsp;km<sup>2</sup> lava flow field using ground-based techniques or optical remote sensing data. Based on the differences between multiple TanDEM-X-derived DEMs collected days to weeks apart, the mean dense-rock equivalent time-averaged discharge rate of lava at Kīlauea between mid-2011 and mid-2013 was approximately 2&thinsp;m<sup>3</sup>/s, which is about half the long-term average rate over the course of Kīlauea's 1983&ndash;present ERZ eruption. This result implies that there was an increase in the proportion of lava stored versus erupted, a decrease in the rate of magma supply to the volcano, or some combination of both during this time period. In addition to constraining the time-averaged discharge rate of lava and the rates of magma supply and storage, topographic change maps derived from space-based TanDEM-X data provide insights into the four-dimensional evolution of Kīlauea's ERZ lava flow field. TanDEM-X data are a valuable complement to other space-, air-, and ground-based observations of eruptive activity at Kīlauea and offer great promise at locations around the world for aiding with monitoring not just volcanic eruptions but any hazardous activity that results in surface change, including landslides, floods, earthquakes, and other natural and anthropogenic processes.</p>","language":"English","publisher":"American Geophysical Union","publisherLocation":"Richmond, VA","doi":"10.1002/2014JB011132","usgsCitation":"Poland, M., 2014, Time-averaged discharge rate of subaerial lava at Kīlauea Volcano, Hawai‘i, measured from TanDEM-X interferometry: Implications for magma supply and storage during 2011-2013: Journal of Geophysical Research B: Solid Earth, v. 119, no. 7, p. 5464-5481, https://doi.org/10.1002/2014JB011132.","productDescription":"18 p.","startPage":"5464","endPage":"5481","onlineOnly":"N","additionalOnlineFiles":"N","ipdsId":"IP-055642","costCenters":[{"id":336,"text":"Hawaiian Volcano Observatory","active":false,"usgs":true},{"id":615,"text":"Volcano Hazards Program","active":true,"usgs":true},{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"links":[{"id":292052,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Hawai'i","otherGeospatial":"Kilauea Volcano","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -155.303007,19.410477 ], [ -155.303007,19.431523 ], [ -155.270993,19.431523 ], [ -155.270993,19.410477 ], [ -155.303007,19.410477 ] ] ] } } ] }","volume":"119","issue":"7","noUsgsAuthors":false,"publicationDate":"2014-07-29","publicationStatus":"PW","scienceBaseUri":"53ec7bd4e4b02bf5a76740c0","contributors":{"authors":[{"text":"Poland, Michael P. 0000-0001-5240-6123 mpoland@usgs.gov","orcid":"https://orcid.org/0000-0001-5240-6123","contributorId":635,"corporation":false,"usgs":true,"family":"Poland","given":"Michael P.","email":"mpoland@usgs.gov","affiliations":[{"id":336,"text":"Hawaiian Volcano Observatory","active":false,"usgs":true}],"preferred":false,"id":497965,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70170271,"text":"70170271 - 2014 - Late Holocene sea level variability and Atlantic Meridional Overturning Circulation","interactions":[],"lastModifiedDate":"2016-08-08T13:44:05","indexId":"70170271","displayToPublicDate":"2014-08-01T00:00:00","publicationYear":"2014","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3002,"text":"Paleoceanography","active":true,"publicationSubtype":{"id":10}},"title":"Late Holocene sea level variability and Atlantic Meridional Overturning Circulation","docAbstract":"<p><span>Pre-twentieth century sea level (SL) variability remains poorly understood due to limits of tide gauge records, low temporal resolution of tidal marsh records, and regional anomalies caused by dynamic ocean processes, notably multidecadal changes in Atlantic Meridional Overturning Circulation (AMOC). We examined SL and AMOC variability along the eastern United States over the last 2000 years, using a SL curve constructed from proxy sea surface temperature (SST) records from Chesapeake Bay, and twentieth century SL-sea surface temperature (SST) relations derived from tide gauges and instrumental SST. The SL curve shows multidecadal-scale variability (20&ndash;30&thinsp;years) during the Medieval Climate Anomaly (MCA) and Little Ice Age (LIA), as well as the twentieth century. During these SL oscillations, short-term rates ranged from 2 to 4&thinsp;mm&thinsp;yr</span><span>&minus;1</span><span>, roughly similar to those of the last few decades. These oscillations likely represent internal modes of climate variability related to AMOC variability and originating at high latitudes, although the exact mechanisms remain unclear. Results imply that dynamic ocean changes, in addition to thermosteric, glacio-eustatic, or glacio-isostatic processes are an inherent part of SL variability in coastal regions, even during millennial-scale climate oscillations such as the MCA and LIA and should be factored into efforts that use tide gauges and tidal marsh sediments to understand global sea level rise.</span></p>","language":"English","publisher":"AGU Publications","doi":"10.1002/2014PA002632","usgsCitation":"Cronin, T.M., Farmer, J.R., Marzen, R.E., Thomas, E., and Varekamp, J., 2014, Late Holocene sea level variability and Atlantic Meridional Overturning Circulation: Paleoceanography, v. 29, no. 8, p. 765-777, https://doi.org/10.1002/2014PA002632.","productDescription":"13 p.","startPage":"765","endPage":"777","onlineOnly":"N","additionalOnlineFiles":"N","ipdsId":"IP-030583","costCenters":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true}],"links":[{"id":472850,"rank":0,"type":{"id":41,"text":"Open Access External Repository Page"},"url":"https://doi.org/10.7916/d86d5rkn","text":"External Repository"},{"id":326241,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"29","issue":"8","publishingServiceCenter":{"id":9,"text":"Reston PSC"},"noUsgsAuthors":false,"publicationDate":"2014-08-07","publicationStatus":"PW","scienceBaseUri":"57a9ad60e4b05e859bdfba13","contributors":{"authors":[{"text":"Cronin, Thomas M. 0000-0002-2643-0979 tcronin@usgs.gov","orcid":"https://orcid.org/0000-0002-2643-0979","contributorId":2579,"corporation":false,"usgs":true,"family":"Cronin","given":"Thomas","email":"tcronin@usgs.gov","middleInitial":"M.","affiliations":[{"id":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":626714,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Farmer, Jesse R.","contributorId":35564,"corporation":false,"usgs":true,"family":"Farmer","given":"Jesse","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":626715,"contributorType":{"id":1,"text":"Authors"},"rank":11},{"text":"Marzen, R. E.","contributorId":147453,"corporation":false,"usgs":false,"family":"Marzen","given":"R.","email":"","middleInitial":"E.","affiliations":[{"id":6676,"text":"USGS (retired)","active":true,"usgs":false}],"preferred":false,"id":644991,"contributorType":{"id":1,"text":"Authors"},"rank":12},{"text":"Thomas, E.","contributorId":64467,"corporation":false,"usgs":true,"family":"Thomas","given":"E.","email":"","affiliations":[],"preferred":false,"id":644992,"contributorType":{"id":1,"text":"Authors"},"rank":13},{"text":"Varekamp, J.C.","contributorId":56006,"corporation":false,"usgs":true,"family":"Varekamp","given":"J.C.","email":"","affiliations":[],"preferred":false,"id":644993,"contributorType":{"id":1,"text":"Authors"},"rank":14}]}}
,{"id":70118369,"text":"70118369 - 2014 - Identifying dominant controls on hydrologic parameter transfer from gauged to ungauged catchments: a comparative hydrology approach","interactions":[],"lastModifiedDate":"2014-07-29T14:04:05","indexId":"70118369","displayToPublicDate":"2014-07-29T13:58:00","publicationYear":"2014","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2342,"text":"Journal of Hydrology","active":true,"publicationSubtype":{"id":10}},"title":"Identifying dominant controls on hydrologic parameter transfer from gauged to ungauged catchments: a comparative hydrology approach","docAbstract":"Daily streamflow information is critical for solving various hydrologic problems, though observations of continuous streamflow for model calibration are available at only a small fraction of the world’s rivers. One approach to estimate daily streamflow at an ungauged location is to transfer rainfall–runoff model parameters calibrated at a gauged (donor) catchment to an ungauged (receiver) catchment of interest. Central to this approach is the selection of a hydrologically similar donor. No single metric or set of metrics of hydrologic similarity have been demonstrated to consistently select a suitable donor catchment. We design an experiment to diagnose the dominant controls on successful hydrologic model parameter transfer. We calibrate a lumped rainfall–runoff model to 83 stream gauges across the United States. All locations are USGS reference gauges with minimal human influence. Parameter sets from the calibrated models are then transferred to each of the other catchments and the performance of the transferred parameters is assessed. This transfer experiment is carried out both at the scale of the entire US and then for six geographic regions. We use classification and regression tree (CART) analysis to determine the relationship between catchment similarity and performance of transferred parameters. Similarity is defined using physical/climatic catchment characteristics, as well as streamflow response characteristics (signatures such as baseflow index and runoff ratio). Across the entire US, successful parameter transfer is governed by similarity in elevation and climate, and high similarity in streamflow signatures. Controls vary for different geographic regions though. Geology followed by drainage, topography and climate constitute the dominant similarity metrics in forested eastern mountains and plateaus, whereas agricultural land use relates most strongly with successful parameter transfer in the humid plains.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Journal of Hydrology","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisher":"Elsevier","doi":"10.1016/j.jhydrol.2014.06.030","usgsCitation":"Singh, R., Archfield, S., and Wagener, T., 2014, Identifying dominant controls on hydrologic parameter transfer from gauged to ungauged catchments: a comparative hydrology approach: Journal of Hydrology, v. 517, p. 985-996, https://doi.org/10.1016/j.jhydrol.2014.06.030.","productDescription":"12 p.","startPage":"985","endPage":"996","numberOfPages":"12","ipdsId":"IP-054107","costCenters":[{"id":436,"text":"National Research Program - Eastern Branch","active":true,"usgs":true}],"links":[{"id":291335,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":291202,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1016/j.jhydrol.2014.06.030"}],"country":"United States","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -124.8,24.5 ], [ -124.8,49.383333 ], [ -66.95,49.383333 ], [ -66.95,24.5 ], [ -124.8,24.5 ] ] ] } } ] }","volume":"517","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"57f7f097e4b0bc0bec09f85f","contributors":{"authors":[{"text":"Singh, R.","contributorId":82591,"corporation":false,"usgs":true,"family":"Singh","given":"R.","email":"","affiliations":[],"preferred":false,"id":496835,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Archfield, S.A.","contributorId":38763,"corporation":false,"usgs":true,"family":"Archfield","given":"S.A.","affiliations":[],"preferred":false,"id":496834,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Wagener, T.","contributorId":36350,"corporation":false,"usgs":true,"family":"Wagener","given":"T.","affiliations":[],"preferred":false,"id":496833,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":70118536,"text":"70118536 - 2014 - Changing amounts and sources of moisture in the U.S. southwest since the Last Glacial Maximum in response to global climate change","interactions":[],"lastModifiedDate":"2014-07-29T10:58:29","indexId":"70118536","displayToPublicDate":"2014-07-29T10:49:00","publicationYear":"2014","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1427,"text":"Earth and Planetary Science Letters","active":true,"publicationSubtype":{"id":10}},"title":"Changing amounts and sources of moisture in the U.S. southwest since the Last Glacial Maximum in response to global climate change","docAbstract":"The U.S. southwest has a limited water supply and is predicted to become drier in the 21st century. An improved understanding of factors controlling moisture sources and availability is aided by reconstruction of past responses to global climate change. New stable isotope and growth-rate records for a central Texas speleothem indicate a strong influence of Gulf of Mexico (GoM) moisture and increased precipitation from 15.5 to 13.5 ka, which includes the majority of the Bølling–Allerød warming (BA: 14.7–12.9 ka). Coeval speleothem records from 900 and 1200 km to the west allow reconstruction of regional moisture sources and atmospheric circulation. The combined isotope and growth-rate time series indicates 1) increased GoM moisture input during the majority of the BA, producing greater precipitation in Texas and New Mexico; and 2) a retreat of GoM moisture during Younger Dryas cooling (12.9–11.5 ka), reducing precipitation. These results portray how late-Pleistocene atmospheric circulation and moisture distribution in this region responded to global changes, providing information to improve models of future climate.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Earth and Planetary Science Letters","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisher":"Elsevier","doi":"10.1016/j.epsl.2014.05.046","usgsCitation":"Feng, W., Hardt, B.F., Banner, J., Meyer, K.J., James, E.W., Musgrove, M., Edwards, R., Cheng, H., and Min, A., 2014, Changing amounts and sources of moisture in the U.S. southwest since the Last Glacial Maximum in response to global climate change: Earth and Planetary Science Letters, v. 401, p. 47-56, https://doi.org/10.1016/j.epsl.2014.05.046.","productDescription":"10 p.","startPage":"47","endPage":"56","numberOfPages":"10","ipdsId":"IP-040447","costCenters":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true}],"links":[{"id":291275,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":291258,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1016/j.epsl.2014.05.046"}],"country":"United States","state":"Texas","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -125.82,18.9 ], [ -125.82,45.18 ], [ -83.98,45.18 ], [ -83.98,18.9 ], [ -125.82,18.9 ] ] ] } } ] }","volume":"401","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"57f7f097e4b0bc0bec09f867","contributors":{"authors":[{"text":"Feng, Weimin","contributorId":36470,"corporation":false,"usgs":true,"family":"Feng","given":"Weimin","email":"","affiliations":[],"preferred":false,"id":496938,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hardt, Benjamin F. bhardt@usgs.gov","contributorId":4127,"corporation":false,"usgs":true,"family":"Hardt","given":"Benjamin","email":"bhardt@usgs.gov","middleInitial":"F.","affiliations":[],"preferred":true,"id":496936,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Banner, Jay L.","contributorId":58200,"corporation":false,"usgs":true,"family":"Banner","given":"Jay L.","affiliations":[],"preferred":false,"id":496941,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Meyer, Kevin J.","contributorId":54129,"corporation":false,"usgs":true,"family":"Meyer","given":"Kevin","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":496939,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"James, Eric W.","contributorId":93405,"corporation":false,"usgs":true,"family":"James","given":"Eric","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":496944,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Musgrove, MaryLynn","contributorId":34878,"corporation":false,"usgs":true,"family":"Musgrove","given":"MaryLynn","affiliations":[],"preferred":false,"id":496937,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Edwards, R. Lawrence","contributorId":55752,"corporation":false,"usgs":true,"family":"Edwards","given":"R. Lawrence","affiliations":[],"preferred":false,"id":496940,"contributorType":{"id":1,"text":"Authors"},"rank":7},{"text":"Cheng, Hai","contributorId":85896,"corporation":false,"usgs":true,"family":"Cheng","given":"Hai","affiliations":[],"preferred":false,"id":496943,"contributorType":{"id":1,"text":"Authors"},"rank":8},{"text":"Min, Angela","contributorId":68664,"corporation":false,"usgs":true,"family":"Min","given":"Angela","email":"","affiliations":[],"preferred":false,"id":496942,"contributorType":{"id":1,"text":"Authors"},"rank":9}]}}
,{"id":70188534,"text":"70188534 - 2014 - Imaging P and S attenuation in the Sacramento-San Joaquin Delta region, northern California","interactions":[],"lastModifiedDate":"2017-06-14T15:08:54","indexId":"70188534","displayToPublicDate":"2014-07-29T00:00:00","publicationYear":"2014","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":"Imaging P and S attenuation in the Sacramento-San Joaquin Delta region, northern California","docAbstract":"We obtain 3-D Qp and Qs models for the Delta region of the Sacramento and San Joaquin Rivers, a large fluvial-agricultural portion of the Great Valley located between the Sierra Nevada batholith and the San Francisco Bay - Coast Ranges region of active faulting. Path attenuation t* values have been obtained for P and S data from 124 distributed earthquakes, with a longer variable window for S based on the energy integral.  We use frequency dependence of 0.5 consistent with other studies, and weakly favored by the t* S data.  A regional initial model was obtained by solving for Q as a function of velocity.  In the final model, the Great Valley basin has low Q with very low Q (<50) for the shallowest portion of the Delta.  There is an underlying strong Q contrast to the ophiolite basement which is thickest with highest Q under the Sacramento basin, and a change in structure is apparent across the Suisun Bay as a transition to thinner ophiolite.  Moderately low Q is found in the upper crust west of the Delta region along the faults in the eastern North Bay Area, while, moderately high Q is found south of the Delta, implying potentially stronger ground motion for earthquake sources to the south.  Very low Q values in the shallow crust along parts of the major fault zones may relate to sediment and abundant microfractures.  In the lower crust below the San Andreas and Calaveras-Hayward-Rodgers Creek fault zones, the observed low Q is consistent with grain-size reduction in ductile shear zones and is lowest under the San Andreas which has large cumulative strain.  Similarly moderately low Q in the ductile lower crust of the Bay Area block between the major fault zones implies a broad distributed shear zone.","language":"English","publisher":"Seismological Society of America","doi":"10.1785/0120130336","usgsCitation":"Eberhart-Phillips, D., Thurber, C., and Fletcher, J.P., 2014, Imaging P and S attenuation in the Sacramento-San Joaquin Delta region, northern California: Bulletin of the Seismological Society of America, v. 104, no. 5, p. 2322-2336, https://doi.org/10.1785/0120130336.","productDescription":"15 p. 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,{"id":70123167,"text":"70123167 - 2014 - Decreased atmospheric sulfur deposition across the southeastern U.S.: When will watersheds release stored sulfate?","interactions":[],"lastModifiedDate":"2017-07-19T15:47:42","indexId":"70123167","displayToPublicDate":"2014-07-21T13:55:51","publicationYear":"2014","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1565,"text":"Environmental Science & Technology","onlineIssn":"1520-5851","printIssn":"0013-936X","active":true,"publicationSubtype":{"id":10}},"title":"Decreased atmospheric sulfur deposition across the southeastern U.S.: When will watersheds release stored sulfate?","docAbstract":"Emissions of sulfur dioxide (SO<sub>2</sub>) to the atmosphere lead to atmospheric deposition of sulfate (SO<sub>4</sub><sup>2-</sup>), which is the dominant strong acid anion causing acidification of surface waters and soils in the eastern United States (U.S.). Since passage of the Clean Air Act and its Amendments, atmospheric deposition of SO<sub>2</sub> in this region has declined by over 80%, but few corresponding decreases in stream-water SO<sub>4</sub><sup>2-</sup> concentrations have been observed in unglaciated watersheds. We calculated SO<sub>4</sub><sup>2-</sup> mass balances for 27 forested, unglaciated watersheds from Pennsylvania to Georgia, by using total atmospheric deposition (wet plus dry) as input. Many of these watersheds still retain SO<sub>4</sub><sup>2-</sup>, unlike their counterparts in the northeastern U.S. and southern Canada. Our analysis showed that many of these watersheds should convert from retaining to releasing SO<sub>4</sub><sup>2-</sup> over the next two decades. The specific years when the watersheds crossover from retaining to releasing SO<sub>4</sub><sup>2-</sup> correspond to a general geographical pattern of later net watershed release from north to south. The single most important variable that explained the crossover year was the runoff ratio, defined as the ratio of annual mean stream discharge to precipitation. Percent clay content and mean soil depth were secondary factors in predicting crossover year. The conversion of watersheds from net SO<sub>4</sub><sup>2-</sup> retention to release anticipates more widespread reductions in stream-water SO<sub>4</sub><sup>2-</sup> concentrations in this region.","language":"English","publisher":"The American Chemical Society","publisherLocation":"Easton, PA","doi":"10.1021/es501579s","usgsCitation":"Rice, K.C., Scanlon, T.M., Lynch, J.A., and Cosby, B.J., 2014, Decreased atmospheric sulfur deposition across the southeastern U.S.: When will watersheds release stored sulfate?: Environmental Science & Technology, v. 48, no. 17, p. 10071-10078, https://doi.org/10.1021/es501579s.","productDescription":"8 p.","startPage":"10071","endPage":"10078","ipdsId":"IP-056001","costCenters":[{"id":614,"text":"Virginia Water Science Center","active":true,"usgs":true}],"links":[{"id":293311,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","volume":"48","issue":"17","noUsgsAuthors":false,"publicationDate":"2014-08-11","publicationStatus":"PW","scienceBaseUri":"5406d9c6e4b044dc0e82892b","contributors":{"authors":[{"text":"Rice, Karen C. 0000-0002-9356-5443 kcrice@usgs.gov","orcid":"https://orcid.org/0000-0002-9356-5443","contributorId":1998,"corporation":false,"usgs":true,"family":"Rice","given":"Karen","email":"kcrice@usgs.gov","middleInitial":"C.","affiliations":[{"id":614,"text":"Virginia Water Science Center","active":true,"usgs":true}],"preferred":false,"id":499909,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Scanlon, Todd M.","contributorId":178235,"corporation":false,"usgs":false,"family":"Scanlon","given":"Todd","email":"","middleInitial":"M.","affiliations":[{"id":25492,"text":"University of Virginia","active":true,"usgs":false}],"preferred":false,"id":499910,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Lynch, Jason A.","contributorId":55702,"corporation":false,"usgs":true,"family":"Lynch","given":"Jason","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":499911,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Cosby, Bernard J.","contributorId":107578,"corporation":false,"usgs":true,"family":"Cosby","given":"Bernard","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":499912,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}}
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