{"pageNumber":"189","pageRowStart":"4700","pageSize":"25","recordCount":10951,"records":[{"id":98974,"text":"fs20103112 - 2010 - Forecasting the effects of land-use and climate change on wildlife communities and habitats in the lower Mississippi Valley","interactions":[],"lastModifiedDate":"2024-03-05T12:09:37.315699","indexId":"fs20103112","displayToPublicDate":"2010-12-29T00:00:00","publicationYear":"2010","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":"2010-3112","title":"Forecasting the effects of land-use and climate change on wildlife communities and habitats in the lower Mississippi Valley","docAbstract":"Landscape patterns and processes reflect both natural ecosystem attributes and the policy and management decisions of individual Federal, State, county, and private organizations. Land-use regulation, water management, and habitat conservation and restoration efforts increasingly rely on landscape-level approaches that incorporate scientific information into the decision-making process. Since management actions are implemented to affect future conditions, decision-support models are necessary to forecast potential future conditions resulting from these decisions. Spatially explicit modeling approaches enable testing of different scenarios and help evaluate potential outcomes of management actions in conjunction with natural processes such as climate change. The ability to forecast the effects of changing land use and climate is critically important to land and resource managers since their work is inherently site specific, yet conservation strategies and practices are expressed at higher spatial and temporal scales that must be considered in the decisionmaking process.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/fs20103112","usgsCitation":"Faulkner, S.P., 2010, Forecasting the effects of land-use and climate change on wildlife communities and habitats in the lower Mississippi Valley (-=): U.S. Geological Survey Fact Sheet 2010-3112, 6 p., https://doi.org/10.3133/fs20103112.","productDescription":"6 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":365,"text":"Leetown Science Center","active":true,"usgs":true},{"id":50464,"text":"Eastern Ecological Science Center","active":true,"usgs":true}],"links":[{"id":126058,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/fs_2010_3112.bmp"},{"id":14407,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/fs/2010/3112/","linkFileType":{"id":5,"text":"html"}}],"edition":"-=","contact":"

Contact Pubs Warehouse

","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e492ae4b07f02db57d1aa","contributors":{"authors":[{"text":"Faulkner, Stephen P. 0000-0001-5295-1383 faulkners@usgs.gov","orcid":"https://orcid.org/0000-0001-5295-1383","contributorId":374,"corporation":false,"usgs":true,"family":"Faulkner","given":"Stephen","email":"faulkners@usgs.gov","middleInitial":"P.","affiliations":[{"id":365,"text":"Leetown Science Center","active":true,"usgs":true}],"preferred":false,"id":307124,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":9000523,"text":"ofr20101304 - 2010 - Reducing Uncertainty in the Distribution of Hydrogeologic Units within Volcanic Composite Units of Pahute Mesa Using High-Resolution 3-D Resistivity Methods, Nevada Test Site, Nevada","interactions":[],"lastModifiedDate":"2012-02-10T00:11:57","indexId":"ofr20101304","displayToPublicDate":"2010-12-28T00:00:00","publicationYear":"2010","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":"2010-1304","title":"Reducing Uncertainty in the Distribution of Hydrogeologic Units within Volcanic Composite Units of Pahute Mesa Using High-Resolution 3-D Resistivity Methods, Nevada Test Site, Nevada","docAbstract":"The U.S. Department of Energy (DOE) and the National Nuclear Security Administration (NNSA) at their Nevada Site Office (NSO) are addressing groundwater contamination resulting from historical underground nuclear testing through the Environmental Management program and, in particular, the Underground Test Area (UGTA) project. From 1951 to 1992, 828 underground nuclear tests were conducted at the Nevada Test Site (NTS) northwest of Las Vegas (DOE UGTA, 2003). Most of these tests were conducted hundreds of feet above the groundwater table; however, more than 200 of the tests were near, or within, the water table. This underground testing was limited to specific areas of the NTS including Pahute Mesa, Rainier Mesa/Shoshone Mountain, Frenchman Flat, and Yucca Flat. Volcanic composite units make up much of the area within the Pahute Mesa Corrective Action Unit (CAU) at the NTS, Nevada. The extent of many of these volcanic composite units extends throughout and south of the primary areas of past underground testing at Pahute and Rainier Mesas. As situated, these units likely influence the rate and direction of groundwater flow and radionuclide transport. Currently, these units are poorly resolved in terms of their hydrologic properties introducing large uncertainties into current CAU-scale flow and transport models. In 2007, the U.S. Geological Survey (USGS), in cooperation with DOE and NNSA-NSO acquired three-dimensional (3-D) tensor magnetotelluric data at the NTS in Area 20 of Pahute Mesa CAU. A total of 20 magnetotelluric recording stations were established at about 600-m spacing on a 3-D array and were tied to ER20-6 well and other nearby well control (fig. 1). The purpose of this survey was to determine if closely spaced 3-D resistivity measurements can be used to characterize the distribution of shallow (600- to 1,500-m-depth range) devitrified rhyolite lava-flow aquifers (LFA) and zeolitic tuff confining units (TCU) in areas of limited drill hole control on Pahute Mesa within the Calico Hills zeolitic volcanic composite unit (VCU), an important hydrostratigraphic unit in Area 20. The resistivity response was evaluated and compared with existing well data and hydrogeologic unit tops from the current Pahute Mesa framework model. In 2008, the USGS processed and inverted the magnetotelluric data into a 3-D resistivity model. We interpreted nine depth slices and four west-east profile cross sections of the 3-D resistivity inversion model. This report documents the geologic interpretation of the 3-D resistivity model. Expectations are that spatial variations in the electrical properties of the Calico Hills zeolitic VCU can be detected and mapped with 3-D resistivity, and that these changes correlate to differences in rock permeability. With regard to LFA and TCU, electrical resistivity and permeability are typically related. Tuff confining units will typically have low electrical resistivity and low permeability, whereas LFA will have higher electrical resistivity and zones of higher fracture-related permeability. If expectations are shown to be correct, the method can be utilized by the UGTA scientists to refine the hydrostratigraphic unit (HSU) framework in an effort to more accurately predict radionuclide transport away from test areas on Pahute and Rainier Mesas.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr20101304","usgsCitation":"Rodriguez, B.D., Sweetkind, D., and Burton, B., 2010, Reducing Uncertainty in the Distribution of Hydrogeologic Units within Volcanic Composite Units of Pahute Mesa Using High-Resolution 3-D Resistivity Methods, Nevada Test Site, Nevada: U.S. Geological Survey Open-File Report 2010-1304, v, 32 p.; Appendices; Figures; Tables , https://doi.org/10.3133/ofr20101304.","productDescription":"v, 32 p.; Appendices; Figures; Tables ","numberOfPages":"498","onlineOnly":"Y","additionalOnlineFiles":"N","costCenters":[{"id":211,"text":"Crustal Geophysics and Geochemistry Science Center","active":true,"usgs":true}],"links":[{"id":126009,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr_2010_1304.png"},{"id":19182,"rank":200,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2010/1304/","linkFileType":{"id":5,"text":"html"}}],"scale":"24000","country":"United States","state":"Nevada","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -116.45,37.25 ], [ -116.45,37.28333333333333 ], [ -116.4,37.28333333333333 ], [ -116.4,37.25 ], [ -116.45,37.25 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a60e4b07f02db63527c","contributors":{"authors":[{"text":"Rodriguez, Brian D. 0000-0002-2263-611X brod@usgs.gov","orcid":"https://orcid.org/0000-0002-2263-611X","contributorId":836,"corporation":false,"usgs":true,"family":"Rodriguez","given":"Brian","email":"brod@usgs.gov","middleInitial":"D.","affiliations":[{"id":211,"text":"Crustal Geophysics and Geochemistry Science Center","active":true,"usgs":true}],"preferred":true,"id":344202,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Sweetkind, Don","contributorId":28725,"corporation":false,"usgs":true,"family":"Sweetkind","given":"Don","email":"","affiliations":[],"preferred":false,"id":344204,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Burton, Bethany L. 0000-0001-5011-7862 blburton@usgs.gov","orcid":"https://orcid.org/0000-0001-5011-7862","contributorId":1341,"corporation":false,"usgs":true,"family":"Burton","given":"Bethany L.","email":"blburton@usgs.gov","affiliations":[{"id":35995,"text":"Geology, Geophysics, and Geochemistry Science Center","active":true,"usgs":true}],"preferred":false,"id":344203,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70044753,"text":"70044753 - 2010 - Two mechanisms of aquatic and terrestrial habitat change along an Alaskan Arctic coastline","interactions":[],"lastModifiedDate":"2013-03-29T15:06:20","indexId":"70044753","displayToPublicDate":"2010-12-28T00:00:00","publicationYear":"2010","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3093,"text":"Polar Biology","active":true,"publicationSubtype":{"id":10}},"title":"Two mechanisms of aquatic and terrestrial habitat change along an Alaskan Arctic coastline","docAbstract":"Arctic habitats at the interface between land and sea are particularly vulnerable to climate change. The northern Teshekpuk Lake Special Area (N-TLSA), a coastal plain ecosystem along the Beaufort Sea in northern Alaska, provides habitat for migratory waterbirds, caribou, and potentially, denning polar bears. The 60-km coastline of N-TLSA is experiencing increasing rates of coastline erosion and storm surge flooding far inland resulting in lake drainage and conversion of freshwater lakes to estuaries. These physical mechanisms are affecting upland tundra as well. To better understand how these processes are affecting habitat, we analyzed long-term observational records coupled with recent short-term monitoring. Nearly the entire coastline has accelerating rates of erosion ranging from 6 m/year from 1955 to 1979 and most recently peaking at 17 m/year from 2007 to 2009, yet an intensive monitoring site along a higher bluff (3–6 masl) suggested high interannual variability. The frequency and magnitude of storm events appears to be increasing along this coastline and these patterns correspond to a greater number of lake tapping and flooding events since 2000. For the entire N-TLSA, we estimate that 6% of the landscape consists of salt-burned tundra, while 41% is prone to storm surge flooding. This offset may indicate the relative frequency of low-magnitude flood events along the coastal fringe. Monitoring of coastline lakes confirms that moderate westerly storms create extensive flooding, while easterly storms have negligible effects on lakes and low-lying tundra. This study of two interacting physical mechanisms, coastal erosion and storm surge flooding, provides an important example of the complexities and data needs for predicting habitat change and biological responses along Arctic land–ocean interfaces.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Polar Biology","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisher":"Springer","publisherLocation":"Amsterdam, Netherlands","doi":"10.1007/s00300-010-0800-5","usgsCitation":"Arp, C.D., Jones, B.M., Schmutz, J.A., Urban, F., and Jorgenson, M., 2010, Two mechanisms of aquatic and terrestrial habitat change along an Alaskan Arctic coastline: Polar Biology, v. 33, no. 12, p. 1629-1640, https://doi.org/10.1007/s00300-010-0800-5.","productDescription":"12 p.","startPage":"1629","endPage":"1640","numberOfPages":"12","ipdsId":"IP-020828","costCenters":[{"id":120,"text":"Alaska Science Center Water","active":true,"usgs":true}],"links":[{"id":475631,"rank":0,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.1007/s00300-010-0800-5","text":"Publisher Index Page"},{"id":270397,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":270396,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1007/s00300-010-0800-5"}],"country":"United States","state":"Alaska","otherGeospatial":"Northern Teshekpuk Lake Special Area","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -0.015,0.0016666666666666668 ], [ -0.015,0.0019444444444444444 ], [ -0.015555555555555555,0.0019444444444444444 ], [ -0.015555555555555555,0.0016666666666666668 ], [ -0.015,0.0016666666666666668 ] ] ] } } ] }","volume":"33","issue":"12","noUsgsAuthors":false,"publicationDate":"2010-04-27","publicationStatus":"PW","scienceBaseUri":"5156b7eee4b06ea905cdc043","contributors":{"authors":[{"text":"Arp, Christopher D.","contributorId":17330,"corporation":false,"usgs":false,"family":"Arp","given":"Christopher","email":"","middleInitial":"D.","affiliations":[{"id":6752,"text":"University of Alaska Fairbanks","active":true,"usgs":false}],"preferred":false,"id":476283,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Jones, Benjamin M. 0000-0002-1517-4711 bjones@usgs.gov","orcid":"https://orcid.org/0000-0002-1517-4711","contributorId":2286,"corporation":false,"usgs":true,"family":"Jones","given":"Benjamin","email":"bjones@usgs.gov","middleInitial":"M.","affiliations":[{"id":114,"text":"Alaska Science Center","active":true,"usgs":true},{"id":118,"text":"Alaska Science Center Geography","active":true,"usgs":true}],"preferred":true,"id":476282,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Schmutz, Joel A. 0000-0002-6516-0836 jschmutz@usgs.gov","orcid":"https://orcid.org/0000-0002-6516-0836","contributorId":1805,"corporation":false,"usgs":true,"family":"Schmutz","given":"Joel","email":"jschmutz@usgs.gov","middleInitial":"A.","affiliations":[{"id":117,"text":"Alaska Science Center Biology WTEB","active":true,"usgs":true},{"id":114,"text":"Alaska Science Center","active":true,"usgs":true}],"preferred":true,"id":476281,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Urban, Frank E. 0000-0002-1329-1703","orcid":"https://orcid.org/0000-0002-1329-1703","contributorId":80918,"corporation":false,"usgs":true,"family":"Urban","given":"Frank E.","affiliations":[],"preferred":false,"id":476285,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Jorgenson, M. 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Most of the subsidence in the Houston-Galveston region has occurred as a direct result of groundwater withdrawals for municipal supply, industrial use, and irrigation that depressured and dewatered the Chicot and Evangeline aquifers causing compaction of the clay layers of the aquifer sediments. This report, prepared by the U.S. Geological Survey, in cooperation with the Harris-Galveston Subsidence District, City of Houston, Fort Bend Subsidence District, and Lone Star Groundwater Conservation District, is one in an annual series of reports depicting water-level altitudes and water-level changes in the Chicot, Evangeline, and Jasper aquifers and compaction in the Chicot and Evangeline aquifers in the Houston-Galveston region. The report contains maps showing 2010 water-level altitudes for the Chicot, Evangeline, and Jasper aquifers, respectively; maps showing 1-year (2009-10) water-level-altitude changes for each aquifer; maps showing 5-year (2005-10) water-level-altitude changes for each aquifer; maps showing long-term (1990-2010 and 1977-2010) water-level-altitude changes for the Chicot and Evangeline aquifers; a map showing long-term (2000-10) water-level-altitude change for the Jasper aquifer; a map showing locations of borehole extensometer sites; and graphs showing measured compaction of subsurface material at the extensometers from 1973, or later, through 2009. Tables listing the data used to construct each aquifer-data map and the compaction graphs are included. Water levels in the Chicot, Evangeline, and Jasper aquifers were measured during December 2009-March 2010. In 2010, water-level-altitude contours for the Chicot aquifer ranged from 200 feet below National Geodetic Vertical Datum of 1929 or North American Vertical Datum of 1988 (hereinafter, datum) in a small area in southwestern Harris County to 200 feet above datum in central to southwestern Montgomery County. Water-level-altitude changes in the Chicot aquifer ranged from a 49-foot decline to a 67-foot rise (2009-10), from a 25-foot decline to a 35-foot rise (2005-10), from a 40-foot decline to an 80-foot rise (1990-2010), and from a 140-foot decline to a 200-foot rise (1977-2010). In 2010, water-level-altitude contours for the Evangeline aquifer ranged from 300 feet below datum in north-central Harris County to 200 feet above datum at the boundary of Waller, Montgomery, and Grimes Counties. Water-level-altitude changes in the Evangeline aquifer ranged from a 58-foot decline to a 69-foot rise (2009-10), from an 80-foot decline to an 80-foot rise (2005-10), from a 200-foot decline to a 220-foot rise (1990-2010), and from a 320-foot decline to a 220-foot rise (1977-2010). In 2010, water-level-altitude contours for the Jasper aquifer ranged from 200 feet below datum in south-central Montgomery County to 250 feet above datum in eastern-central Grimes County. Water-level-altitude changes in the Jasper aquifer ranged from a 39-foot decline to a 39-foot rise (2009-10), from a 110-foot decline to no change (2005-10), and from a 180-foot decline to no change (2000-10). Compaction of subsurface materials (mostly in the clay layers) composing the Chicot and Evangeline aquifers was recorded continuously at 13 borehole extensometers at 11 sites. For the period of record beginning in 1973, or later, and ending in December 2009, cumulative clay compaction data measured by 12 extensometers ranged from 0.088 foot at the Texas City-Moses Lake site to 3.559 foot at the Addicks site. The rate of compaction varies from site to site because of differences in groundwater withdrawals near each site and differences among sites in the clay-to-sand ratio in the subsurface materials. Therefore, it is not possible to extrapolate or infer a rate of clay compaction for an area based on the rate of compaction measured at a nearby extensometer.

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Before and during the 2006 eruption of Augustine Volcano, the Alaska Volcano Observatory (AVO) installed a network of telemetered and nontelemetered cameras in Homer, Alaska, and on Augustine Island. On December 1, 2005, a network camera was installed at the Homer Field Station, a University of Alaska Fairbanks Geophysical Institute (UAF/GI) facility on a bluff near Homer, where telemetered Augustine data are received. The camera placed there provides observations of the volcano from a distance of 126 km (78 miles) in daylight hours during clear sky conditions. On January 9, 2006, a radio-telemetered network camera was installed on the lower eastern flank of the volcano at 'Mound,' 4.4 km (2.7 miles) from the summit. The proximity of this camera provided for near-field images of the volcano. A nontelemetered camera with onsite recording was installed 3.8 km (2.4 miles) north of the volcano's summit near Burr Point on December 17, 2005. This camera recorded high-resolution images at a rate of 4 images per hour through much of the eruptive sequence. A low-light camera was installed on February 8, 2006, at the Homer facility to augment the extreme low-light camera installed by the UAF/GI (Sentman and others, this volume). On September 10, 2006, a second radio-telemetered network camera was installed at Lagoon camp on the west side of Augustine Island, 5.4 km (3.3 miles) west-northwest of the summit. The installation of these camera systems proved valuable for assessing volcanic activity, determining ground hazards and on-island weather for visiting field teams, and deciphering depositional history after the eruption.

","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"The 2006 eruption of Augustine Volcano, Alaska","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/pp176912","usgsCitation":"Paskievitch, J., Read, C., and Parker, T., 2010, Remote telemetered and time-lapse cameras at Augustine Volcano: Chapter 12 in The 2006 eruption of Augustine Volcano, Alaska: U.S. Geological Survey Professional Paper 1769, 9 p., https://doi.org/10.3133/pp176912.","productDescription":"9 p.","startPage":"286","endPage":"293","onlineOnly":"Y","additionalOnlineFiles":"N","costCenters":[{"id":121,"text":"Alaska Volcano Observatory","active":false,"usgs":true}],"links":[{"id":203782,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/pp176912.gif"},{"id":14365,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pp/1769/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Alaska","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -153.51470947265625,\n 59.412945785071\n ],\n [\n -153.47625732421875,\n 59.41993301322722\n ],\n [\n -153.446044921875,\n 59.428315784042574\n ],\n [\n -153.39385986328125,\n 59.428315784042574\n ],\n [\n -153.36090087890622,\n 59.41574084934491\n ],\n [\n -153.34442138671875,\n 59.39477224351409\n ],\n [\n -153.31695556640625,\n 59.37658895163648\n ],\n [\n -153.32794189453125,\n 59.33599107056162\n ],\n [\n -153.37188720703125,\n 59.32338185310805\n ],\n [\n -153.446044921875,\n 59.31777625443006\n ],\n [\n -153.5394287109375,\n 59.31076795603884\n ],\n [\n -153.577880859375,\n 59.32618430580267\n ],\n [\n -153.577880859375,\n 59.35139598294652\n ],\n [\n -153.60260009765625,\n 59.379387015928536\n ],\n [\n -153.59161376953125,\n 59.404559208021745\n ],\n [\n -153.55865478515625,\n 59.410150490100754\n ],\n [\n -153.51470947265625,\n 59.412945785071\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adde4b07f02db686bee","contributors":{"editors":[{"text":"Power, John A. 0000-0002-7233-4398 jpower@usgs.gov","orcid":"https://orcid.org/0000-0002-7233-4398","contributorId":2768,"corporation":false,"usgs":true,"family":"Power","given":"John","email":"jpower@usgs.gov","middleInitial":"A.","affiliations":[],"preferred":true,"id":647330,"contributorType":{"id":2,"text":"Editors"},"rank":1},{"text":"Coombs, Michelle L. 0000-0002-6002-6806 mcoombs@usgs.gov","orcid":"https://orcid.org/0000-0002-6002-6806","contributorId":2809,"corporation":false,"usgs":true,"family":"Coombs","given":"Michelle","email":"mcoombs@usgs.gov","middleInitial":"L.","affiliations":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"preferred":true,"id":647331,"contributorType":{"id":2,"text":"Editors"},"rank":2},{"text":"Freymueller, Jeffrey T.","contributorId":97458,"corporation":false,"usgs":true,"family":"Freymueller","given":"Jeffrey","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":647332,"contributorType":{"id":2,"text":"Editors"},"rank":3}],"authors":[{"text":"Paskievitch, John","contributorId":74050,"corporation":false,"usgs":true,"family":"Paskievitch","given":"John","affiliations":[],"preferred":false,"id":307004,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Read, Cyrus cread@usgs.gov","contributorId":3707,"corporation":false,"usgs":true,"family":"Read","given":"Cyrus","email":"cread@usgs.gov","affiliations":[],"preferred":true,"id":307002,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Parker, Thomas","contributorId":51891,"corporation":false,"usgs":true,"family":"Parker","given":"Thomas","affiliations":[],"preferred":false,"id":307003,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":98939,"text":"pp176910 - 2010 - Pyroclastic flows, lahars, and mixed avalanches generated during the 2006 eruption of Augustine Volcano: Chapter 10 in The 2006 eruption of Augustine Volcano, Alaska","interactions":[{"subject":{"id":98939,"text":"pp176910 - 2010 - Pyroclastic flows, lahars, and mixed avalanches generated during the 2006 eruption of Augustine Volcano: Chapter 10 in The 2006 eruption of Augustine Volcano, Alaska","indexId":"pp176910","publicationYear":"2010","noYear":false,"chapter":"10","title":"Pyroclastic flows, lahars, and mixed avalanches generated during the 2006 eruption of Augustine Volcano: Chapter 10 in The 2006 eruption of Augustine Volcano, Alaska"},"predicate":"IS_PART_OF","object":{"id":98929,"text":"pp1769 - 2010 - The 2006 eruption of Augustine Volcano, Alaska","indexId":"pp1769","publicationYear":"2010","noYear":false,"title":"The 2006 eruption of Augustine Volcano, Alaska"},"id":1}],"isPartOf":{"id":98929,"text":"pp1769 - 2010 - The 2006 eruption of Augustine Volcano, Alaska","indexId":"pp1769","publicationYear":"2010","noYear":false,"title":"The 2006 eruption of Augustine Volcano, Alaska"},"lastModifiedDate":"2016-12-21T22:07:39","indexId":"pp176910","displayToPublicDate":"2010-12-16T00:00:00","publicationYear":"2010","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":"1769","chapter":"10","title":"Pyroclastic flows, lahars, and mixed avalanches generated during the 2006 eruption of Augustine Volcano: Chapter 10 in The 2006 eruption of Augustine Volcano, Alaska","docAbstract":"

Each of the three phases of the 2006 eruption at Augustine Volcano had a distinctive eruptive style and flowage deposits. From January 11 to 28, the explosive phase comprised short vulcanian eruptions that punctuated dome growth and produced volcanowide pyroclastic flows and more energetic hot currents whose mobility was influenced by efficient mixing with and vaporization of snow. Initially, hot flows moved across winter snowpack, eroding it to generate snow, water, and pyroclastic slurries that formed mixed avalanches and lahars, first eastward, then northward, and finally southward, but subsequent flows produced no lahars or mixed avalanches. During a large explosive event on January 27, disruption of a lava dome terminated the explosive phase and emplaced the largest pyroclastic flow of the 2006 eruption northward toward Rocky Point. From January 28 to February 10, activity during the continuous phase comprised rapid dome growth and frequent dome-collapse pyroclastic flows and a lava flow restricted to the north sector of the volcano. Then, after three weeks of inactivity, during the effusive phase of March 3 to 16, the volcano continued to extrude the lava flow, whose steep sides collapsed infrequently to produce block-and-ash flows.

\n

The three eruptive phases were each unique not only in terms of eruptive style, but also in terms of the types and morphologies of deposits that were produced, and, in particular, of their lithologic components. Thus, during the explosive phase, low-silica andesite scoria predominated, and intermediate- and high-silica andesite were subordinate. During the continuous phase, the eruption shifted predominantly to high-silica andesite and, during the effusive phase, shifted again to dense low-silica andesite. Each rock type is present in the deposits of each eruptive phase and each flow type, and lithologic proportions are unique and consistent within the deposits that correspond to each eruptive phase.

\n

The chief factors that influenced pyroclastic currents and the characteristics of their deposits were genesis, grain size, and flow surface. Column collapse from short-lived vulcanian blasts, dome collapses, and collapses of viscous lavas on steep slopes caused the pyroclastic currents documented in this study. Column-collapse flows during the explosive phase spread widely and probably were affected by vaporization of ingested snow where they overran snowpack. Such pyroclastic currents can erode substrates formed of snow or ice through a combination of mechanical and thermal processes at the bed, thus enhancing the spread of these flows across snowpack and generating mixed avalanches and lahars. Grain-size characteristics of these initial pyroclastic currents and overburden pressures at their bases favored thermal scour of snow and coeval fluidization. These flows scoured substrate snow and generated secondary slurry flows, whereas subsequent flows did not. Some secondary flows were wetter and more laharic than others. Where secondary flows were quite watery, recognizable mixed-avalanche deposits were small or insignificant, and lahars were predominant. Where such flows contained substantial amounts of snow, mixed-avalanche deposits blanketed medial reaches of valleys and formed extensive marginal terraces and axial islands in distal reaches. Flows that contained significant amounts of snow formed cogenetic mixed avalanches that slid across surfaces protected by snowpack, whereas water-rich axial lahars scoured channels.

\n
Correlations of planimetric area (A) versus volume (V) for pyroclastic deposits with similar origins and characteristics exhibit linear trends, such that A=cV2/3, where c is a constant for similar groups of flows. This relationship was tested and calibrated for dome-collapse, column-collapse, and surgelike flows using area-volume data from this study and examples from Montserrat, Merapi, and Mount St. Helens. The ratio A/V2/3=c gives a dimensionless measure of mobility calibrated for each of these three types of flow. Surgelike flows are highly mobile, with c≈520; column-collapse flows have c≈150; and dome-collapse flows have c≈35, about that of simple rock avalanches. Such calibrated mobility factors have a potential use in volcano-hazard assessments.
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2010 - Ejecta and landslides from Augustine Volcano before 2006: Chapter 13 in The 2006 eruption of Augustine Volcano, Alaska","interactions":[{"subject":{"id":98942,"text":"pp176913 - 2010 - Ejecta and landslides from Augustine Volcano before 2006: Chapter 13 in The 2006 eruption of Augustine Volcano, Alaska","indexId":"pp176913","publicationYear":"2010","noYear":false,"chapter":"13","title":"Ejecta and landslides from Augustine Volcano before 2006: Chapter 13 in The 2006 eruption of Augustine Volcano, Alaska"},"predicate":"IS_PART_OF","object":{"id":98929,"text":"pp1769 - 2010 - The 2006 eruption of Augustine Volcano, Alaska","indexId":"pp1769","publicationYear":"2010","noYear":false,"title":"The 2006 eruption of Augustine Volcano, Alaska"},"id":1}],"isPartOf":{"id":98929,"text":"pp1769 - 2010 - The 2006 eruption of Augustine Volcano, Alaska","indexId":"pp1769","publicationYear":"2010","noYear":false,"title":"The 2006 eruption of Augustine Volcano, Alaska"},"lastModifiedDate":"2016-08-29T13:40:01","indexId":"pp176913","displayToPublicDate":"2010-12-16T00:00:00","publicationYear":"2010","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":"1769","chapter":"13","title":"Ejecta and landslides from Augustine Volcano before 2006: Chapter 13 in The 2006 eruption of Augustine Volcano, Alaska","docAbstract":"

A late Wisconsin volcano erupted onto the JurassicCretaceous sedimentary bedrock of Augustine Island in lower Cook Inlet in Alaska. Olivine basalt interacting with water erupted explosively. Rhyolitic eruptive debris then swept down the south volcano flank while late Wisconsin glaciers from mountains on western mainland surrounded the island. Early to middle Holocene deposits probably erupted onto the island but are now largely buried. About 5,200, 3,750, 3,500, and 2,275 yr B.P. Augustine ash fell 70 to 110 km away.

\n

Since about 2,300 yr B.P. several large eruptions deposited coarse-pumice fall beds on the volcano flanks; many smaller eruptions dropped sand and silt ash. The steep summit erupting viscous andesite domes has repeatedly collapsed into rocky avalanches that flowed into the sea. After a collapse, new domes rebuilt the summit. One to three avalanches shed east before about 2,100 yr B.P., two large ones swept east and southeast between about 2,100 and 1,700 yr B.P., and one shed east and east-northeast between 1,700 and 1,450 yr B.P. Others swept into the sea on the volcano’s south, southwest, and north-northwest between about 1,450 and 1,100 yr B.P., and pyroclastic fans spread southeast and southwest. Pyroclastic flows and surges poured down the west and south flanks and a debris avalanche plowed into the western sea between about 1,000 and 750 yr B.P. A small debris avalanche shed south-southeast between about 750 and 390 yr B.P., and large lithic pyroclastic flows went southeast.

\n

From about 390 to 200 yr B.P., three rocky avalanches swept down the west-northwest, north-northwest, and north flanks. The large West Island avalanche reached far beyond a former sea cliff and initiated a tsunami. Augustine’s only conspicuous lava flow erupted on the north flank.

\n

In October 1883 a debris avalanche plowed into the sea to form Burr Point on the north-northeast; then came ashfall, pyroclastic surge, and pyroclastic flows. Eruptions in 1935 and 1963–64 grew summit lava domes that shed coarse rubbly lithic pyroclastic flows down the southwest and south flanks. Eruptions in 1976 and 1986 grew domes that shed large pyroclastic flows northeast, north, and north-northwest.

\n

The largest debris avalanches off Augustine sweep into the sea and radiate tsunami about lower Cook Inlet.

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2010 - Preliminary slope-stability analysis of Augustine Volcano: Chapter 14 in The 2006 eruption of Augustine Volcano, Alaska","interactions":[{"subject":{"id":98943,"text":"pp176914 - 2010 - Preliminary slope-stability analysis of Augustine Volcano: Chapter 14 in The 2006 eruption of Augustine Volcano, Alaska","indexId":"pp176914","publicationYear":"2010","noYear":false,"chapter":"14","title":"Preliminary slope-stability analysis of Augustine Volcano: Chapter 14 in The 2006 eruption of Augustine Volcano, Alaska"},"predicate":"IS_PART_OF","object":{"id":98929,"text":"pp1769 - 2010 - The 2006 eruption of Augustine Volcano, Alaska","indexId":"pp1769","publicationYear":"2010","noYear":false,"title":"The 2006 eruption of Augustine Volcano, Alaska"},"id":1}],"isPartOf":{"id":98929,"text":"pp1769 - 2010 - The 2006 eruption of Augustine Volcano, Alaska","indexId":"pp1769","publicationYear":"2010","noYear":false,"title":"The 2006 eruption of Augustine Volcano, Alaska"},"lastModifiedDate":"2016-08-29T15:03:32","indexId":"pp176914","displayToPublicDate":"2010-12-16T00:00:00","publicationYear":"2010","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":"1769","chapter":"14","title":"Preliminary slope-stability analysis of Augustine Volcano: Chapter 14 in The 2006 eruption of Augustine Volcano, Alaska","docAbstract":"

Augustine Volcano has been a prolific producer of large debris avalanches during the Holocene. Originating as landslides from the steep upper edifice, these avalanches typically slide into the surrounding ocean. At least one debris avalanche that occurred in 1883 during an eruption initiated a far-traveled tsunami. The possible occurrence of another edifice collapse and ensuing tsunami was a concern during the 2006 eruption of Augustine. To aid in hazard assessments, we have evaluated the slope stability of Augustine's edifice, using a quasi-three-dimensional, geotechnically based slope-stability model implemented in the computer program SCOOPS. We analyzed the effects of topography, variations in rock strength, and earthquake-induced strong ground motion on the relative stability of millions of potential large (>0.1 km3 volume) slope failures throughout the edifice. Preliminary results from pre-2006 topography provide three insights. First, the predicted stability of all parts of the upper edifice is approximately the same, suggesting an equal likelihood of slope failure, in agreement with geologic observations that debris avalanches have swept all sectors of the volcano. Second, the least stable (by a small amount) sector is on the east flank where a debris avalanche would flow into deeper ocean water and a resulting tsunami would be directed toward the southwestern part of the Kenai Peninsula. Third, most model scenarios predict stable edifice slopes, and only scenarios assuming extensive weak rocks and moderate to strong ground shaking predict potential large collapses. Because other transient triggering mechanisms, such as shallow magma intrusion, may be needed to instigate slope instability, monitoring ground deformation and seismicity could

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2010 - Timing, distribution, and volume of proximal products of the 2006 eruption of Augustine Volcano: Chapter 8 in The 2006 eruption of Augustine Volcano, Alaska","interactions":[{"subject":{"id":98937,"text":"pp17698 - 2010 - Timing, distribution, and volume of proximal products of the 2006 eruption of Augustine Volcano: Chapter 8 in The 2006 eruption of Augustine Volcano, Alaska","indexId":"pp17698","publicationYear":"2010","noYear":false,"chapter":"8","title":"Timing, distribution, and volume of proximal products of the 2006 eruption of Augustine Volcano: Chapter 8 in The 2006 eruption of Augustine Volcano, Alaska"},"predicate":"IS_PART_OF","object":{"id":98929,"text":"pp1769 - 2010 - The 2006 eruption of Augustine Volcano, Alaska","indexId":"pp1769","publicationYear":"2010","noYear":false,"title":"The 2006 eruption of Augustine Volcano, Alaska"},"id":1}],"isPartOf":{"id":98929,"text":"pp1769 - 2010 - The 2006 eruption of Augustine Volcano, Alaska","indexId":"pp1769","publicationYear":"2010","noYear":false,"title":"The 2006 eruption of Augustine Volcano, Alaska"},"lastModifiedDate":"2020-10-02T13:55:17.551167","indexId":"pp17698","displayToPublicDate":"2010-12-16T00:00:00","publicationYear":"2010","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":"1769","chapter":"8","title":"Timing, distribution, and volume of proximal products of the 2006 eruption of Augustine Volcano: Chapter 8 in The 2006 eruption of Augustine Volcano, Alaska","docAbstract":"

During and after the 2006 eruption of Augustine Volcano, we compiled a geologic map and chronology of new lava and flowage deposits using observational flights, oblique and aerial photography, infrared imaging, satellite data, and field investigations. After approximately 6 months of precursory activity, the explosive phase of the eruption commenced with two explosions on January 11, 2006 (events 1 and 2) that produced snow-rich avalanches; little or no juvenile magma was erupted. Seismicity suggests that a small lava dome may have extruded on January 12, but, if so, it was subsequently destroyed. A series of six explosions on January 13–14 (events 3–8) produced widespread but thin (0–30 cm) pyroclastic-current deposits on the upper flanks above 300 m altitude and lobate, 0.5- to 2-m-thick pyroclastic flows that traveled down most flanks of the volcano. Between January 14 and 17, a smooth lava lobe formed in the east half of the roughly 400-m-wide summit crater and was only partially covered by later deposits. An explosion on January 17 (event 9) opened a crater in the new lava dome and produced a ballistic fall deposit and pyroclastic flow on the southwest flank. During the interval from January 17 to 27, a rubbly lava dome effused. On January 27, explosive event 10 generated a pyroclastic current that left a deposit, rich in dense clasts, on the north-northwest flank. Immediately following the pyroclastic current, a voluminous 4.7-km-long pyroclastic flow swept down the north flank. Three more explosive blasts on January 27 and 28 produced unknown but likely minor on-island deposits. The cumulative volume of erupted material from the explosive phase, including domes, flows, and fall deposits (Wallace and others, this volume), was 30×106 m3 dense-rock equivalent (DRE).

\n

The continuous phase of the eruption (January 28 through February 10) began with a 4-day period of nearly continuous block-and-ash flows, which deposited small individual flow lobes that cumulatively formed fans to the north and northeast of the summit. A single larger pyroclastic flow on January 30 formed a braided deposit on the northwest flank. Roughly 9×106 m3 (DRE) of magma erupted during this period. Around February 2, the magma flux rate waned and a northward lava flow effused and reached a length of approximately 900 m by February 10. Approximately 11×106 m3 (DRE) of magma erupted during the second half of the continuous phase.

\n

After a 23-day hiatus, lava effusion recommenced in early March (the effusive phase) and was accompanied by frequent (but volumetrically minor) block-and-ash flows. From March 7 to 14, extrusion increased markedly; two blocky lava-flow lobes, each tens of meters thick, moved down the north and northeast flank of the volcano; and a new summit lava dome grew to be ~70 m taller than the pre-2006 summit. This phase produced 26×106 m3 (DRE) of lava. Active effusion had ceased about March 16, but, in April and May, three gravitational collapses from the west margin of the north lava flow produced additional block-and-ash flows. The basic sequence of the 2006 eruption closely matches that of eruptions in 1976 and 1986.

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They were likely transported as larvae or young adults inside the ballast tanks of large ocean-going ships originating from Europe. Since their introduction, they have spread throughout the Eastern, Midwestern, and Southern United States. In 2007, Quagga mussels (Dreissena rostriformis bugensis) were found in the Western United States in Lake Mead, Nevada; part of the Lower Colorado River Basin. State and Federal managers are concerned that the mussels (hereafter referred to as dreissenid mussels or mussels) will continue to spread to the Columbia River Basin and have a major impact on the region?s ecosystem, water delivery infrastructure, hydroelectric projects, and the economy. The transport and use of recreational watercraft throughout the Western United States could easily result in spreading mussels to the Columbia River Basin. The number of recreational watercraft using Lake Mead can range from 350 to 3,500 a day (Bryan Moore, National Park Service, oral commun., June 21, 2008). Because recreational watercrafts are readily moved around and mussels may survive for a period of time when they are out of the water, there is a high potential to spread mussels from Lake Mead to other waterways in the Western United States. Efforts are being made to prevent the spread of mussels; however, there is great concern that these efforts will not be 100 percent successful. When prevention efforts fail, early detection of mussels may provide an opportunity to implement rapid response management actions to minimize the impact. Control and eradication efforts are more likely to be successful if they are implemented when the density of mussels is low and the area of infestation is small. Once the population grows and becomes established, the mussels are extremely difficult, if not impossible, to control. Although chemicals may be used to kill the mussels, the chemicals that are currently available also can kill other aquatic life. Early implementation of containment and eradication efforts requires getting reliable information to confirm the location of the infestation. One way to get this information is through the use of properly trained SCUBA divers. This document provides SCUBA divers with the necessary information to conduct underwater searchers for mussels. However, using SCUBA divers to search for mussels over a large geographic area is relatively expensive and inefficient. Early detection monitoring methods can be used to optimize the use of SCUBA divers. Early detection monitoring can be accomplished by collecting water samples or deploying artificial settlement substrates (fig. 1). Water samples are used to look for free-swimming larval mussels (called veligers). Because the veligers cannot be identified with the naked eye, the water samples are sent to a laboratory where they are examined under a microscope and/or analyzed using molecular techniques to detect veligers. To detect the presences of adult mussels, artificial substrates are deployed and periodically retrieved to determine if mussels have settled on the substrate. If veligers or adults are identified, SCUBA divers can be deployed to confirm the presence of mussels.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr20101308","collaboration":"Prepared in cooperation with the U.S. Fish and Wildlife Service","usgsCitation":"Adams, N., 2010, Procedures for conducting underwater searches for invasive mussels (Dreissena sp.): U.S. Geological Survey Open-File Report 2010-1308, iv, 30 p.; Appendices, https://doi.org/10.3133/ofr20101308.","productDescription":"iv, 30 p.; Appendices","numberOfPages":"44","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":654,"text":"Western Fisheries Research Center","active":true,"usgs":true}],"links":[{"id":126071,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr_2010_1308.jpg"},{"id":19173,"rank":200,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2010/1308/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9ee4b07f02db6608e6","contributors":{"authors":[{"text":"Adams, Noah","contributorId":91604,"corporation":false,"usgs":true,"family":"Adams","given":"Noah","affiliations":[],"preferred":false,"id":344164,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":9000513,"text":"sir20105196 - 2010 - Hydrology, water quality, and response to changes in phosphorus loading of Minocqua and Kawaguesaga Lakes, Oneida County, Wisconsin, with special emphasis on effects of urbanization","interactions":[],"lastModifiedDate":"2024-06-17T20:50:51.982684","indexId":"sir20105196","displayToPublicDate":"2010-12-13T00:00:00","publicationYear":"2010","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":"2010-5196","title":"Hydrology, water quality, and response to changes in phosphorus loading of Minocqua and Kawaguesaga Lakes, Oneida County, Wisconsin, with special emphasis on effects of urbanization","docAbstract":"

Minocqua and Kawaguesaga Lakes are 1,318- and 690-acre interconnected lakes in the popular recreation area of north-central Wisconsin. The lakes are the lower end of a complex chain of lakes in Oneida and Vilas Counties, Wis. There is concern that increased stormwater runoff from rapidly growing residential/commercial developments and impervious surfaces from the urbanized areas of the Town of Minocqua and Woodruff, as well as increased effluent from septic systems around their heavily developed shoreline has increased nutrient loading to the lakes. Maintaining the quality of the lakes to sustain the tourist-based economy of the towns and the area was a concern raised by the Minocqua/Kawaguesaga Lakes Protection Association. Following several small studies, a detailed study during 2006 and 2007 was done by the U.S. Geological Survey, in cooperation with the Minocqua/Kawaguesaga Lakes Protection Association through the Town of Minocqua to describe the hydrology and water quality of the lakes, quantify the sources of phosphorus including those associated with urban development and to better understand the present and future effects of phosphorus loading on the water quality of the lakes.

The water quality of Minocqua and Kawaguesaga Lakes appears to have improved since 1963, when a new sewage-treatment plant was constructed and its discharge was bypassed around the lakes, resulting in a decrease in phosphorus loading to the lakes. Since the mid-1980s, the water quality of the lakes has changed little in response to fluctuations in phosphorus loading from the watershed. From 1986 to 2009, summer average concentrations of near-surface total phosphorus in the main East Basin of Minocqua Lake fluctuated from 0.009 mg/L to 0.027 mg/L but generally remained less than 0.022 mg/L, indicating that the lake is mesotrophic. Phosphorus concentrations from 1988 through 1996, however, were lower than the long-term average, possibly the result of an extended drought in the area. Water‑quality data for Kawaguesaga Lake had a similar pattern to that of Minocqua Lake. Summer average chlorophyll a concentrations and Secchi depths also indicate that the lakes generally are mesotrophic but occasionally borderline eutrophic, with no long-term trends.

During the study, major water and phosphorus sources were measured directly, and minor sources were estimated to construct detailed water and phosphorus budgets for the lakes for monitoring years (MY) 2006 and 2007. During these years, the Minocqua Thoroughfare contributed about 38 percent of the total inflow to the lakes, and Tomahawk Thoroughfare contributed 34 percent; near-lake inflow, precipitation, and groundwater contributed about 1, 16, and 11 percent of the total inflow, respectively. Water leaves the lakes primarily through the Tomahawk River outlet (83 percent) or by evaporation (14 percent), with minor outflow to groundwater. Total input of phosphorus to both lakes was about 3,440 pounds in MY 2006 and 2,200 pounds in MY 2007. The largest sources of phosphorus entering the lakes were the Minocqua and Tomahawk Thoroughfares, which delivered about 39 and 26 percent of the total, respectively. The near-lake drainage area, containing most of the urban and residential developments, disproportionately accounted for about 12 percent of the total phosphorus input but only about 1 percent of the total water input (estimated with WinSLAMM). The next largest contributions were from septic systems and precipitation, each contributing about 10 percent, whereas groundwater delivered about 4 percent of the total phosphorus input.

Empirical lake water-quality models within BATHTUB were used to simulate the response of Minocqua and Kawaguesaga Lakes to 19 phosphorus-loading scenarios. These scenarios included the current base years (2006–07) for which lake water quality and loading were known, nine general increases or decreases in phosphorus loading from controllable external sources (inputs from the tributaries and nearshore areas around the lakes and input from septic systems), and nine scenarios corresponding to future changes in phosphorus loading from residential and urban development, referred to as “2030 buildout,” and removal of septic system inputs. The 2030 buildout scenario with existing stormwater controls resulted in a degradation in water quality: phosphorus concentrations increased by about 0.001 mg/L, chlorophyll a concentrations increased by 0.2–0.8 μg/L, and Secchi depths decreased slightly. The largest degradation in water quality was estimated to occur in Kawaguesaga Lake. If 2030 buildout occurred with implementation of best management practices to achieve a 50-percent reduction in loading from near-lake drainages, it is possible that water quality would change very little from existing conditions. Numerous noncontributing areas exist within the watershed that help minimize surface runoff and nutrient loading to the lakes; however, if future development included extending or connecting drainage from these areas into the lakes, loading to the lakes could greatly increase and cause a degradation in the water quality of the lakes. Simulations of removal of phosphorus loading from septic systems around Minocqua Lake improved the water quality of the lakes: in simulations for that scenario, phosphorus concentrations decreased by about 0.001 mg/L, chlorophyll a concentrations decreased by 0.5–0.7 μg/L, and Secchi depths increased by 0.3–0.7 ft. If all controllable external phosphorus loading could be reduced by 50 percent, the lakes would become oligotrophic with respect to phosphorus concentration but would still remain mesotrophic with respect to chlorophyll a concentration and Secchi depth. Improvements in the water quality of the lakes are likely only with a combination of management actions that decrease inputs from the developed near-lake drainage areas and from septic systems.

","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/sir20105196","collaboration":"Prepared in cooperation with the Minocqua/Kawaguesaga Lakes Protection Association through the Town of Minocqua, Wisconsin","usgsCitation":"Garn, H.S., Robertson, D.M., Rose, W., and Saad, D.A., 2010, Hydrology, water quality, and response to changes in phosphorus loading of Minocqua and Kawaguesaga Lakes, Oneida County, Wisconsin, with special emphasis on effects of urbanization: U.S. Geological Survey Scientific Investigations Report 2010-5196, viii, 54 p., https://doi.org/10.3133/sir20105196.","productDescription":"viii, 54 p.","numberOfPages":"54","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":677,"text":"Wisconsin Water Science Center","active":true,"usgs":true}],"links":[{"id":430335,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_94651.htm","linkFileType":{"id":5,"text":"html"}},{"id":19174,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2010/5196/","linkFileType":{"id":5,"text":"html"}},{"id":126069,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2010_5196.htm"}],"country":"United States","state":"Wisconsin","county":"Oneida County","otherGeospatial":"Minocqua and Kawaguesaga Lakes","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -89.7565226213236,\n 45.88642438539571\n ],\n [\n -89.7565226213236,\n 45.85592970552128\n ],\n [\n -89.66475756839306,\n 45.85592970552128\n ],\n [\n -89.66475756839306,\n 45.88642438539571\n ],\n [\n -89.7565226213236,\n 45.88642438539571\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0ce4b07f02db5fc6ed","contributors":{"authors":[{"text":"Garn, Herbert S. hsgarn@usgs.gov","contributorId":2592,"corporation":false,"usgs":true,"family":"Garn","given":"Herbert","email":"hsgarn@usgs.gov","middleInitial":"S.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":344168,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Robertson, Dale M. 0000-0001-6799-0596 dzrobert@usgs.gov","orcid":"https://orcid.org/0000-0001-6799-0596","contributorId":150760,"corporation":false,"usgs":true,"family":"Robertson","given":"Dale","email":"dzrobert@usgs.gov","middleInitial":"M.","affiliations":[{"id":37947,"text":"Upper Midwest Water Science Center","active":true,"usgs":true}],"preferred":true,"id":344165,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Rose, William J. wjrose@usgs.gov","contributorId":2182,"corporation":false,"usgs":true,"family":"Rose","given":"William J.","email":"wjrose@usgs.gov","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":344167,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Saad, David A. dasaad@usgs.gov","contributorId":121,"corporation":false,"usgs":true,"family":"Saad","given":"David","email":"dasaad@usgs.gov","middleInitial":"A.","affiliations":[{"id":677,"text":"Wisconsin Water Science Center","active":true,"usgs":true}],"preferred":true,"id":344166,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":98925,"text":"ofr20101265 - 2010 - Geologic map of the White Hall quadrangle, Frederick County, Virginia, and Berkeley County, West Virginia","interactions":[],"lastModifiedDate":"2022-04-14T21:56:46.974717","indexId":"ofr20101265","displayToPublicDate":"2010-12-11T00:00:00","publicationYear":"2010","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":"2010-1265","title":"Geologic map of the White Hall quadrangle, Frederick County, Virginia, and Berkeley County, West Virginia","docAbstract":"The White Hall 7.5-minute quadrangle is located within the Valley and Ridge province of northern Virginia and the eastern panhandle of West Virginia. The quadrangle is one of several being mapped to investigate the geologic framework and groundwater resources of Frederick County, Va., as well as other areas in the northern Shenandoah Valley of Virginia and West Virginia. All exposed bedrock outcrops are clastic and carbonate strata of Paleozoic age ranging from Middle Cambrian to Late Devonian. Surficial materials include unconsolidated alluvium, colluvium, and terrace deposits of Quaternary age, and local paleo-terrace deposits possibly of Tertiary age. The quadrangle lies across the northeast plunge of the Great North Mountain anticlinorium and includes several other regional folds. The North Mountain fault zone cuts through the eastern part of the quadrangle; it is a series of thrust faults generally oriented northeast-southwest that separate the Silurian and Devonian clastic rocks from the Cambrian and Ordovician carbonate rocks and shales. Karst development in the quadrangle occurs in all of the carbonate rocks. Springs occur mainly near or on faults. Sinkholes occur within all of the carbonate rock units, especially where the rocks have undergone locally intensified deformation through folding, faulting, or some combination.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr20101265","usgsCitation":"Doctor, D.H., Orndorff, R.C., Parker, R., Weary, D.J., and Repetski, J.E., 2010, Geologic map of the White Hall quadrangle, Frederick County, Virginia, and Berkeley County, West Virginia: U.S. Geological Survey Open-File Report 2010-1265, 1 Plate: 46.00 × 42.00 inches; Downloads Directory, https://doi.org/10.3133/ofr20101265.","productDescription":"1 Plate: 46.00 × 42.00 inches; Downloads Directory","onlineOnly":"Y","additionalOnlineFiles":"Y","costCenters":[{"id":40020,"text":"Florence Bascom Geoscience Center","active":true,"usgs":true}],"links":[{"id":126115,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr_2010_1265.gif"},{"id":398792,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_94646.htm"},{"id":14347,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2010/1265/","linkFileType":{"id":5,"text":"html"}}],"scale":"24000","projection":"Polyconic projection","country":"United States","state":"Virginia, West Virginia","county":"Berkeley County, Frederick County","otherGeospatial":"White Hall quadrangle","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -78.25,\n 39.25\n ],\n [\n -78.125,\n 39.25\n ],\n [\n -78.125,\n 39.375\n ],\n [\n -78.25,\n 39.375\n ],\n [\n -78.25,\n 39.25\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4acce4b07f02db67e9e2","contributors":{"authors":[{"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":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":306953,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Orndorff, Randall C. 0000-0002-8956-5803 rorndorf@usgs.gov","orcid":"https://orcid.org/0000-0002-8956-5803","contributorId":2739,"corporation":false,"usgs":true,"family":"Orndorff","given":"Randall","email":"rorndorf@usgs.gov","middleInitial":"C.","affiliations":[{"id":501,"text":"Office of Science Quality and Integrity","active":true,"usgs":true},{"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":306955,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Parker, Ronald A.","contributorId":70350,"corporation":false,"usgs":true,"family":"Parker","given":"Ronald A.","affiliations":[],"preferred":false,"id":306956,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"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":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":306952,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Repetski, John E. 0000-0002-2298-7120 jrepetski@usgs.gov","orcid":"https://orcid.org/0000-0002-2298-7120","contributorId":2596,"corporation":false,"usgs":true,"family":"Repetski","given":"John","email":"jrepetski@usgs.gov","middleInitial":"E.","affiliations":[{"id":40020,"text":"Florence Bascom Geoscience Center","active":true,"usgs":true},{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true}],"preferred":true,"id":306954,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":98923,"text":"sir20105227 - 2010 - Groundwater-flow model and effects of projected groundwater use in the Ozark Plateaus Aquifer System in the vicinity of Greene County, Missouri — 1907-2030","interactions":[],"lastModifiedDate":"2022-01-24T22:28:24.710479","indexId":"sir20105227","displayToPublicDate":"2010-12-11T00:00:00","publicationYear":"2010","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":"2010-5227","title":"Groundwater-flow model and effects of projected groundwater use in the Ozark Plateaus Aquifer System in the vicinity of Greene County, Missouri — 1907-2030","docAbstract":"

Recent and historical periods of rapid growth have increased the stress on the groundwater resources in the Ozark aquifer in the Greene County, Missouri area. Historical pumpage from the Ozark aquifer has caused a cone of depression beneath Springfield, Missouri. In an effort to ease its dependence on groundwater for supply, the city of Springfield built a pipeline in 1996 to bring water from Stockton Lake to the city. Rapid population growth in the area coupled with the expanding cone of depression raised concern about the sustainability of groundwater as a resource for future use. A groundwater-flow model was developed by the U.S. Geological Survey in cooperation with Greene County, Missouri, the U. S. Army Corps of Engineers, and the Missouri Department of Natural Resources to assess the effect that increased groundwater demand is having on the long-term availability of groundwater in and around Greene County, Missouri.

Three hydrogeologic units were represented in the groundwater-flow model: the Springfield Plateau aquifer, the Ozark confining unit, and the Ozark aquifer. The Springfield Plateau aquifer is less than 350 feet thick in the model area and generally is a low yield aquifer suitable only for domestic use. The Ozark aquifer is composed of a more than 900-foot thick sequence of dolomite and sandstone in the model area and is the primary aquifer throughout most of southern Missouri. Wells open to the entire thickness of the Ozark aquifer typically yield 1,000 gallons per minute or more. Between the two aquifers is the Ozark confining unit composed of as much as 98 feet of shale and limestone. Karst features such as sinkholes, springs, caves, and losing streams are present in both aquifers, but the majority of these features occur in the Springfield Plateau aquifer. The solution-enlarged fracture and bedding plane conduits in the karst system, particularly in the Springfield Plateau aquifer, are capable of moving large quantities of groundwater through the aquifer in relatively short periods of time.

Pumpage rates in the model area increased from 1,093,268 cubic feet per day in 1962 to 2,693,423 cubic feet per day in 1987 to 4,330,177 cubic feet per day in 2006. Annual precipitation ranged from 25.21 inches in 1953 to 62.45 inches in 1927 from 1915 to 2006 in the model area. Recharge to the model was calculated as 2.53 percent of the annual precipitation and was varied annually. Recharge was distributed over the model area based on land slope and was adjusted in the city limits of Springfield to account for the impervious surface.

A groundwater model with annual stress periods from 1907 to 2030 was developed using a transient calibration period from 1987 to 2006 and a prediction period from 2007 to 2030 to simulate flow in the Springfield Plateau aquifer and the Ozark aquifer. For the model area of approximately 2,870 square miles, the model hydrogeologic units and hydraulic properties were discretized into 253 rows, 316 columns, and 3 layers with the layer boundaries crossing hydrogeologic unit boundaries in some areas. The horizontal cell spacing was 1,000 feet by 1,000 feet. The model was calibrated by minimizing the difference between simulated head and observed water levels and simulated and observed flows in rivers and springs.

Population and the associated groundwater use were estimated for 12 communities and the unincorporated area of Greene County based on past growth. Each was analyzed individually, and a low and high annual rate of growth relative to the 2006 population was computed for each community or group. Low growth rates ranged from 0.215 percent per year in Springfield to 6.997 percent per year in Rogersville. Total growth from 2006 to 2030 at the low growth rate ranged from 5.2 percent in Springfield to 167.9 percent in Rogersville. High growth rates ranged from 0.236 percent per year in Springfield to 7.345 percent per year in Rogersville. Total growth from 2006 to 2030 at the high growth rate ranged from 5.7 percent in Springfield to 176.3 percent in Rogersville.

Response of the flow system to selected hypothetical pumping stresses and recharge conditions was simulated using the calibrated model. Seven hypothetical scenarios were simulated from 2007 to 2030 to test the effects of various stresses on the head in the Ozark aquifer. Hypothetical scenario 1 continued the 2006 pumping rates without change to the end of 2030. Scenario 2 assumed a low population growth rate with a 4-year drought at the beginning of the prediction period. Scenario 3 assumed a low population growth rate with a 4-year drought at the end of the prediction period. Scenario 4 assumed a high population growth rate with a 4-year drought at the beginning of the prediction period. Scenario 5 assumed a high population growth rate with a 4-year drought at the end of the prediction period. Scenario 6 and 7 had one new industrial well installed within the city limits of Springfield and one new industrial well installed about 3.5 miles east of Rogersville. Scenario 6 assumed a low population growth rate and scenario 7 assumed a high population growth rate.

Results were compared by examining differences in head at the end of the simulation period. All scenarios examined resulted in potentiometric-surface declines from 2006 levels. Results from scenario 1 indicated that even with no increase in pumping, the potentiometric surface in the Springfield area continued to decline. The maximum decline of approximately 62 feet from the 2006 potentiometric surface occurred in Springfield. The maximum decline from the 2006 potentiometric surface in scenarios 2 and 3 was approximately 203 feet and in scenarios 4 and 5 was approximately 207 feet. The drought occurring at the end of the simulation period tended to broaden the drawdown area relative to the drought at the beginning. Drought timing did not substantially affect the potentiometric surface in the Ozark aquifer except for where the Ozark aquifer was exposed. Although not a substantial difference, the high population growth rate scenarios tended to have larger declines than the low population growth rate scenarios. As in the previous scenarios, little difference was noted between the low and high growth rate in scenario 6 and 7. Scenarios 6 and 7 showed declines of more than 640 feet from the 2006 potentiometric surface at the new well located in Springfield. The drawdown at the new wells decreased relatively quickly with increased distance from the well. Simulated head in the nearby cities of Nixa, Ozark, and Republic was nearly the same for scenarios 2 through 7 and was lower than the head predicted for scenario 1. Results from scenarios 2 through 7 indicate that the potentiometric surface in 2030 near these cities could decline 100 feet or more from the 2006 levels. Because model layers 2 and 3, representing the Ozark confining unit and most of the thickness of the Ozark aquifer, were simulated as confined, drawdown in the wells in the area of the Ozark aquifer that is unconfined or becomes unconfined during the simulation period will likely be under predicted.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/sir20105227","usgsCitation":"Richards, J.M., 2010, Groundwater-flow model and effects of projected groundwater use in the Ozark Plateaus Aquifer System in the vicinity of Greene County, Missouri — 1907-2030: U.S. Geological Survey Scientific Investigations Report 2010-5227, x, 106 p., https://doi.org/10.3133/sir20105227.","productDescription":"x, 106 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":396,"text":"Missouri Water Science Center","active":true,"usgs":true}],"links":[{"id":126113,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2010_5227.jpg"},{"id":394791,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_94644.htm"},{"id":14345,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2010/5227/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Missouri","county":"Greene County","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -93.6859130859375,\n 36.87522650673951\n ],\n [\n -92.79602050781249,\n 36.87522650673951\n ],\n [\n -92.79602050781249,\n 37.4530574713902\n ],\n [\n -93.6859130859375,\n 37.4530574713902\n ],\n [\n -93.6859130859375,\n 36.87522650673951\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a93e4b07f02db6587a9","contributors":{"authors":[{"text":"Richards, Joseph M. 0000-0002-9822-2706 richards@usgs.gov","orcid":"https://orcid.org/0000-0002-9822-2706","contributorId":2370,"corporation":false,"usgs":true,"family":"Richards","given":"Joseph","email":"richards@usgs.gov","middleInitial":"M.","affiliations":[{"id":36532,"text":"Central Midwest Water Science Center","active":true,"usgs":true}],"preferred":true,"id":306947,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":98879,"text":"ofr20101190 - 2010 - Floods of May 30 to June 15, 2008, in the Iowa River and Cedar River Basins, eastern Iowa","interactions":[],"lastModifiedDate":"2021-11-22T20:48:46.379912","indexId":"ofr20101190","displayToPublicDate":"2010-11-13T00:00:00","publicationYear":"2010","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":"2010-1190","title":"Floods of May 30 to June 15, 2008, in the Iowa River and Cedar River Basins, eastern Iowa","docAbstract":"As a result of prolonged and intense periods of rainfall in late May and early June, 2008, along with heavier than normal snowpack the previous winter, record flooding occurred in Iowa in the Iowa River and Cedar River Basins. The storms were part of an exceptionally wet period from May 29 through June 12, when an Iowa statewide average of 9.03 inches of rain fell; the normal statewide average for the same period is 2.45 inches. From May 29 to June 13, the 16-day rainfall totals recorded at rain gages in Iowa Falls and Clutier were 14.00 and 13.83 inches, respectively. Within the Iowa River Basin, peak discharges of 51,000 cubic feet per second (flood-probability estimate of 0.2 to 1 percent) at the 05453100 Iowa River at Marengo, Iowa streamflow-gaging station (streamgage) on June 12, and of 39,900 cubic feet per second (flood-probability estimate of 0.2 to 1 percent) at the 05453520 Iowa River below Coralville Dam near Coralville, Iowa streamgage on June 15 are the largest floods on record for those sites. A peak discharge of 41,100 cubic feet per second (flood-probability estimate of 0.2 to 1 percent) on June 15 at the 05454500 Iowa River at Iowa City, Iowa streamgage is the fourth highest on record, but is the largest flood since regulation by the Coralville Dam began in 1958.\r\n\r\nWithin the Cedar River Basin, the May 30 to June 15, 2008, flood is the largest on record at all six streamgages in Iowa located on the mainstem of the Cedar River and at five streamgages located on the major tributaries. Flood-probability estimates for 10 of these 11 streamgages are less than 1 percent. Peak discharges of 112,000 cubic feet per second (flood-probability estimate of 0.2 to 1 percent) at the 05464000 Cedar River at Waterloo, Iowa streamgage on June 11 and of 140,000 cubic feet per second (flood-probability estimate of less than 0.2 percent) at the 05464500 Cedar River at Cedar Rapids, Iowa streamgage on June 13 are the largest floods on record for those sites. Downstream from the confluence of the Iowa and Cedar Rivers, the peak discharge of 188,000 cubic feet per second (flood-probability estimate of less than 0.2 percent) at the 05465500 Iowa River at Wapello, Iowa streamgage on June 14, 2008, is the largest flood on record in the Iowa River and Cedar River Basins since 1903.\r\n\r\nHigh-water marks were measured at 88 locations along the Iowa River between State Highway 99 near Oakville and U.S. Highway 69 in Belmond, a distance of 319 river miles. High-water marks were measured at 127 locations along the Cedar River between Fredonia near the mouth (confluence with the Iowa River) and Riverview Drive north of Charles City, a distance of 236 river miles. The high-water marks were used to develop flood profiles for the Iowa and Cedar River.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr20101190","usgsCitation":"Linhart, M.S., and Eash, D.A., 2010, Floods of May 30 to June 15, 2008, in the Iowa River and Cedar River Basins, eastern Iowa: U.S. Geological Survey Open-File Report 2010-1190, vi, 99 p., https://doi.org/10.3133/ofr20101190.","productDescription":"vi, 99 p.","onlineOnly":"N","additionalOnlineFiles":"N","temporalStart":"2008-05-30","temporalEnd":"2008-06-15","costCenters":[{"id":351,"text":"Iowa Water Science Center","active":true,"usgs":true}],"links":[{"id":126063,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr_2010_1190.jpg"},{"id":392010,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_94596.htm"},{"id":14297,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2010/1190/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Iowa","otherGeospatial":"Iowa River and Cedar River Basins","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -93.8167,\n 41.0125\n ],\n [\n -91.7069,\n 41.0125\n ],\n [\n -91.7069,\n 43.9333\n ],\n [\n -93.8167,\n 43.9333\n ],\n [\n -93.8167,\n 41.0125\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b26e4b07f02db6af9a0","contributors":{"authors":[{"text":"Linhart, Mike S.","contributorId":99945,"corporation":false,"usgs":true,"family":"Linhart","given":"Mike","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":306817,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Eash, David A. 0000-0002-2749-8959 daeash@usgs.gov","orcid":"https://orcid.org/0000-0002-2749-8959","contributorId":1887,"corporation":false,"usgs":true,"family":"Eash","given":"David","email":"daeash@usgs.gov","middleInitial":"A.","affiliations":[{"id":351,"text":"Iowa Water Science Center","active":true,"usgs":true}],"preferred":true,"id":306816,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70168477,"text":"70168477 - 2010 - Seasonal meso- and microhabitat selection by the northern snakehead (Channa argus) in the Potomac river system","interactions":[],"lastModifiedDate":"2016-02-16T14:56:02","indexId":"70168477","displayToPublicDate":"2010-11-11T00:00:00","publicationYear":"2010","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1471,"text":"Ecology of Freshwater Fish","active":true,"publicationSubtype":{"id":10}},"title":"Seasonal meso- and microhabitat selection by the northern snakehead (Channa argus) in the Potomac river system","docAbstract":"

 The northern snakehead (Channa argus) is a large piscivorous fish that is invasive in eastern Europe and has recently been introduced in North America. We examined the seasonal habitat selection at meso- and microhabitat scales using radio-telemetry to increase understanding of the ecology of this species, which will help to inform management decisions. After the spawning season (postspawn season, September–November), northern snakeheads preferred offshore Eurasian water-milfoil (Myriophyllum spicatum) beds with shallow water (∼115 cm) and soft substrate. In the winter (November–April), these fish moved to deeper water (∼135 cm) with warmer temperatures, but habitat selection was weak at both scales. Northern snakeheads returned to shallower water (∼95 cm) in the prespawn season (April–June) and used milfoil and other cover. Habitat selection was the strongest at both meso- and microhabitat scales during the spawning season (June–September), when fish preferred macrophytes and cover in shallow water (∼88 cm). Our results help to identify habitats at the risk of invasion by northern snakeheads. We suggest that control efforts and future research focus on shallow waters, and take into consideration the seasonal habitat preferences.

","language":"English","publisher":"Munksgaard","publisherLocation":"Copenhagen, Denmark","doi":"10.1111/j.1600-0633.2010.00437.x","usgsCitation":"Lapointe, N., Thorson, J., and Angermeier, P., 2010, Seasonal meso- and microhabitat selection by the northern snakehead (Channa argus) in the Potomac river system: Ecology of Freshwater Fish, v. 19, no. 10, p. 566-577, https://doi.org/10.1111/j.1600-0633.2010.00437.x.","productDescription":"12 p.","startPage":"566","endPage":"577","onlineOnly":"N","additionalOnlineFiles":"N","ipdsId":"IP-019480","costCenters":[{"id":199,"text":"Coop Res Unit Leetown","active":true,"usgs":true}],"links":[{"id":318084,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Maryland, Virginia","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -77.20298767089842,\n 38.63457282385875\n ],\n [\n -77.20298767089842,\n 38.74444410121548\n ],\n [\n -77.0526123046875,\n 38.74444410121548\n ],\n [\n -77.0526123046875,\n 38.63457282385875\n ],\n [\n -77.20298767089842,\n 38.63457282385875\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"19","issue":"10","publishingServiceCenter":{"id":9,"text":"Reston PSC"},"noUsgsAuthors":false,"publicationDate":"2010-11-11","publicationStatus":"PW","scienceBaseUri":"56c45655e4b0946c652185bf","contributors":{"authors":[{"text":"Lapointe, N.W.R.","contributorId":76558,"corporation":false,"usgs":true,"family":"Lapointe","given":"N.W.R.","email":"","affiliations":[],"preferred":false,"id":620482,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Thorson, J.T.","contributorId":72626,"corporation":false,"usgs":true,"family":"Thorson","given":"J.T.","email":"","affiliations":[],"preferred":false,"id":620568,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Angermeier, P. L. 0000-0003-2864-170X","orcid":"https://orcid.org/0000-0003-2864-170X","contributorId":6410,"corporation":false,"usgs":true,"family":"Angermeier","given":"P. L.","affiliations":[],"preferred":false,"id":620569,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":98858,"text":"sir20105122 - 2010 - Lithologic and physicochemical properties and hydraulics of flow in and near the freshwater/saline-water transition zone, San Antonio segment of the Edwards aquifer, south-central Texas, based on water-level and borehole geophysical log data, 1999-2007","interactions":[],"lastModifiedDate":"2024-01-08T22:22:15.060274","indexId":"sir20105122","displayToPublicDate":"2010-11-02T00:00:00","publicationYear":"2010","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":"2010-5122","title":"Lithologic and physicochemical properties and hydraulics of flow in and near the freshwater/saline-water transition zone, San Antonio segment of the Edwards aquifer, south-central Texas, based on water-level and borehole geophysical log data, 1999-2007","docAbstract":"

The freshwater zone of the San Antonio segment of the Edwards aquifer in south-central Texas (hereinafter, the Edwards aquifer) is bounded to the south and southeast by a zone of transition from freshwater to saline water (hereinafter, the transition zone). The boundary between the two zones is the freshwater/saline-water interface (hereinafter, the interface), defined as the 1,000-milligrams per liter dissolved solids concentration threshold. This report presents the findings of a study, done by the U.S. Geological Survey in cooperation with the San Antonio Water System, to obtain lithologic properties (rock properties associated with known stratigraphic units) and physicochemical properties (fluid conductivity and temperature) and to analyze the hydraulics of flow in and near the transition zone of the Edwards aquifer on the basis of water-level and borehole geophysical log data collected from 15 monitoring wells in four transects during 1999-2007. No identifiable relation between conductivity values from geophysical logs in monitoring wells in all transects and equivalent freshwater heads in the wells at the times the logs were run is evident; and no identifiable relation between conductivity values and vertical flow in the boreholes concurrent with the times the logs were run is evident. The direction of the lateral equivalent freshwater head gradient and thus the potential lateral flow at the interface in the vicinity of the East Uvalde transect fluctuates between into and out of the freshwater zone, depending on recharge and withdrawals. Whether the prevailing direction on average is into or out of the freshwater zone is not clearly indicated. Equivalent freshwater head data do not indicate a prevailing direction of the lateral gradient at the interface in the vicinity of the Tri-County transect. The prevailing direction on average of the lateral gradient and thus potential lateral flow at the interface in the vicinity of the Kyle transect likely is from the transition zone into the freshwater zone. The hypothesis regarding the vertical gradient at the East Uvalde transect, and thus the potential for vertical flow near an interface conceptualized as a surface sloping upward in the direction of the dip of the stratigraphic units, is that the potential for vertical flow fluctuates between into and out of the freshwater zone, depending on recharge and withdrawals. At the Tri-County transect, a downward gradient on the fresh-water side of the interface and an upward gradient on the saline-water side are evidence of opposing potentials that appear to have stabilized the position of the interface over the range of hydrologic conditions that occurred at the times the logs were run. At the Fish Hatchery transect, an upward gradient on the saline-water side of the interface, coupled with the assumption of a sloping interface, implies a vertical gradient from the transition zone into the freshwater zone. This potential for vertical movement of the interface apparently was opposed by the potential (head) on the freshwater side of the interface that kept the interface relatively stable over the range of hydrologic conditions during which the logs were run. The five flow logs for Kyle transect freshwater well KY1 all indicate upward flow that originates from the Glen Rose Limestone, the uppermost unit of the Trinity aquifer; and one log for well KY2 shows upward flow entering the borehole from the Trinity aquifer. These flow data constitute evidence of the potential for flow from the Trinity aquifer into the Edwards aquifer in the vicinity of the Kyle transect. Subsurface temperature data indicate that flow on average is more active, or vigorous, on the freshwater side of the interface than on the saline-water side. A hydraulic connection between the transition zone and the freshwater zone is indicated by similar patterns in the hydrographs of the 15 transect monitoring wells in and near the transition zone and three county index wel

","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, Virginia","doi":"10.3133/sir20105122","collaboration":"In cooperation with the San Antonio Water System","usgsCitation":"Lambert, R.B., Hunt, A.G., Stanton, G.P., and Nyman, M.B., 2010, Lithologic and physicochemical properties and hydraulics of flow in and near the freshwater/saline-water transition zone, San Antonio segment of the Edwards aquifer, south-central Texas, based on water-level and borehole geophysical log data, 1999-2007: U.S. Geological Survey Scientific Investigations Report 2010-5122, Report: ix, 69 p.; 4 Appendices, https://doi.org/10.3133/sir20105122.","productDescription":"Report: ix, 69 p.; 4 Appendices","onlineOnly":"N","additionalOnlineFiles":"Y","temporalStart":"1999-10-01","temporalEnd":"2007-09-30","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":424200,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_94500.htm","linkFileType":{"id":5,"text":"html"}},{"id":14271,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2010/5122/","linkFileType":{"id":5,"text":"html"}},{"id":126089,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2010_5122.jpg"}],"projection":"Universal Transverse Mercator","country":"United States","state":"Texas","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -100.66666666666667,28.5 ], [ -100.66666666666667,30.5 ], [ -97.5,30.5 ], [ -97.5,28.5 ], [ -100.66666666666667,28.5 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0be4b07f02db5fc211","contributors":{"authors":[{"text":"Lambert, Rebecca B. 0000-0002-0611-1591 blambert@usgs.gov","orcid":"https://orcid.org/0000-0002-0611-1591","contributorId":1135,"corporation":false,"usgs":true,"family":"Lambert","given":"Rebecca","email":"blambert@usgs.gov","middleInitial":"B.","affiliations":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"preferred":true,"id":306731,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hunt, Andrew G. 0000-0002-3810-8610 ahunt@usgs.gov","orcid":"https://orcid.org/0000-0002-3810-8610","contributorId":1582,"corporation":false,"usgs":true,"family":"Hunt","given":"Andrew","email":"ahunt@usgs.gov","middleInitial":"G.","affiliations":[{"id":211,"text":"Crustal Geophysics and Geochemistry Science Center","active":true,"usgs":true}],"preferred":true,"id":306732,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Stanton, Gregory P. 0000-0001-8622-0933 gstanton@usgs.gov","orcid":"https://orcid.org/0000-0001-8622-0933","contributorId":1583,"corporation":false,"usgs":true,"family":"Stanton","given":"Gregory","email":"gstanton@usgs.gov","middleInitial":"P.","affiliations":[],"preferred":true,"id":306733,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Nyman, Michael B. mbnyman@usgs.gov","contributorId":1584,"corporation":false,"usgs":true,"family":"Nyman","given":"Michael","email":"mbnyman@usgs.gov","middleInitial":"B.","affiliations":[],"preferred":true,"id":306734,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70236323,"text":"70236323 - 2010 - Very rapid geomagnetic field change recorded by the partial remagnetization of a lava flow","interactions":[],"lastModifiedDate":"2022-09-01T16:57:57.380757","indexId":"70236323","displayToPublicDate":"2010-11-01T11:43:46","publicationYear":"2010","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1807,"text":"Geophysical Research Letters","active":true,"publicationSubtype":{"id":10}},"title":"Very rapid geomagnetic field change recorded by the partial remagnetization of a lava flow","docAbstract":"

A new paleomagnetic result from a lava flow with a distinctive, two-part remanence reinforces the controversial hypothesis that geomagnetic change during a polarity reversal can be much faster than normal. The 3.9-m-thick lava (“Flow 20”) is exposed in the Sheep Creek Range (north central Nevada) and was erupted during a reverse-to-normal (R-N) geomagnetic polarity switch at 15.6 Ma. Flow 20 began to acquire a primary thermoremanence while the field was pointing east and down but was soon buried, reheated, and partially-remagnetized in a north-down direction by the 8.2-m-thick flow that succeeded it. A simple conductive cooling calculation shows that the observed remagnetization could not have occurred unless Flow 20 was still warm (about 150°C near its base) when buried and that the 53° change from east-down to north-down field occurred at an average rate of approximately 1°/week, several orders of magnitude faster than typical of secular variation.

","language":"English","publisher":"American Geophysical Union","doi":"10.1029/2010GL044286","usgsCitation":"Bogue, S.W., and Glen, J.M., 2010, Very rapid geomagnetic field change recorded by the partial remagnetization of a lava flow: Geophysical Research Letters, v. 37, no. 21, L21308, 5 p., https://doi.org/10.1029/2010GL044286.","productDescription":"L21308, 5 p.","costCenters":[],"links":[{"id":406077,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Nevada","otherGeospatial":"Sheep Creek Range","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -116.84646606445312,\n 40.66293116628907\n ],\n [\n -116.72561645507812,\n 40.69834018178775\n ],\n [\n -116.52511596679688,\n 40.85433181694295\n ],\n [\n -116.42623901367188,\n 40.985081625514354\n ],\n [\n -116.45095825195311,\n 41.03067934862969\n ],\n [\n -116.62261962890624,\n 41.088667173210624\n ],\n [\n -116.73934936523438,\n 41.047252515172424\n ],\n [\n -116.87118530273436,\n 40.93426521177941\n ],\n [\n -116.92611694335938,\n 40.80029619806279\n ],\n [\n -116.90963745117188,\n 40.7202010588415\n ],\n [\n -116.84646606445312,\n 40.66293116628907\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"37","issue":"21","noUsgsAuthors":false,"publicationDate":"2010-11-10","publicationStatus":"PW","contributors":{"authors":[{"text":"Bogue, Scott W.","contributorId":20476,"corporation":false,"usgs":true,"family":"Bogue","given":"Scott","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":850608,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Glen, Jonathan M.G. 0000-0002-3502-3355 jglen@usgs.gov","orcid":"https://orcid.org/0000-0002-3502-3355","contributorId":176530,"corporation":false,"usgs":true,"family":"Glen","given":"Jonathan","email":"jglen@usgs.gov","middleInitial":"M.G.","affiliations":[{"id":309,"text":"Geology and Geophysics Science Center","active":true,"usgs":true},{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":850609,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":98844,"text":"ofr20101217 - 2010 - Coastal circulation and sediment dynamics in Maunalua Bay, Oahu, Hawaii: Measurements of waves, currents, temperature, salinity, and turbidity: November 2008-February 2009","interactions":[],"lastModifiedDate":"2022-11-30T22:56:33.215057","indexId":"ofr20101217","displayToPublicDate":"2010-10-28T00:00:00","publicationYear":"2010","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":"2010-1217","title":"Coastal circulation and sediment dynamics in Maunalua Bay, Oahu, Hawaii: Measurements of waves, currents, temperature, salinity, and turbidity: November 2008-February 2009","docAbstract":"

High-resolution measurements of waves, currents, water levels, temperature, salinity and turbidity were made in Maunalua Bay, southern Oahu, Hawaii, during the 2008–2009 winter to better understand coastal circulation, water-column properties, and sediment dynamics during a range of conditions (trade winds, kona storms, relaxation of trade winds, and south swells). A series of bottom-mounted instrument packages were deployed in water depths of 20 m or less to collect long-term, high-resolution measurements of waves, currents, water levels, temperature, salinity, and turbidity. These data were supplemented with a series of profiles through the water column to characterize the vertical and spatial variability in water-column properties within the bay. These measurements support the ongoing process studies being done as part of the U.S. Geological Survey (USGS) Coastal and Marine Geology Program’s Pacific Coral Reef Project; the ultimate goal of these studies is to better understand the transport mechanisms of sediment, larvae, pollutants, and other particles in coral reef settings.

Project Objectives

The objective of this study was to understand the temporal variations in currents, waves, tides, temperature, salinity and turbidity within a coral-lined embayment that receives periodic discharges of freshwater and sediment from multiple terrestrial sources in the Maunalua Bay. Instrument packages were deployed for a three-month period during the 2008–2009 winter and a series of vertical profiles were collected in November 2008, and again in February 2009, to characterize water-column properties within the bay. Measurements of flow and water-column properties in Maunalua Bay provided insight into the potential fate of terrestrial sediment, nutrient, or contaminant delivered to the marine environment and coral larval transport within the embayment. Such data are useful for providing baseline information for future watershed decisions and for establishing guidelines for the U.S. Coral Reef Task Force’s (USCRTF) Hawaiian Local Action Strategy to address Land-Based Pollution (LAS-LBP) threats to coral reefs adjacent to the urbanized watersheds of Manualua Bay.

Study Area

Maunalua Bay is on the south side of Oahu, Hawaii, and is approximately 10 km long and 3 km wide. The bay is flanked by two large, dormant craters: Koko Head to the east and Diamond Head to the west. Rainfall in the watersheds that drain into Maunalua Bay ranges from more than 200 cm/year at the top of the Ko‘olau Range that borders the northwestern part of the bay to less than 70 cm/year to the east at Koko Head. Seven major channels flow into the bay, and all but one have been altered by engineering structures.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr20101217","usgsCitation":"Storlazzi, C., Presto, M., Logan, J., and Field, M.E., 2010, Coastal circulation and sediment dynamics in Maunalua Bay, Oahu, Hawaii: Measurements of waves, currents, temperature, salinity, and turbidity: November 2008-February 2009: U.S. Geological Survey Open-File Report 2010-1217, v, 59 p., https://doi.org/10.3133/ofr20101217.","productDescription":"v, 59 p.","onlineOnly":"Y","additionalOnlineFiles":"N","costCenters":[{"id":520,"text":"Pacific Coastal and Marine Science Center","active":true,"usgs":true}],"links":[{"id":126052,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr_2010_1217.jpg"},{"id":409906,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_94462.htm","linkFileType":{"id":5,"text":"html"}},{"id":14255,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2010/1217/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Hawaii","otherGeospatial":"Maunalua Bay, Oahu","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -157.6833,\n 21.2833\n ],\n [\n -157.8261,\n 21.2833\n ],\n [\n -157.8261,\n 21.2333\n ],\n [\n -157.6833,\n 21.2333\n ],\n [\n -157.6833,\n 21.2833\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b24e4b07f02db6aeb08","contributors":{"authors":[{"text":"Storlazzi, Curt D. 0000-0001-8057-4490","orcid":"https://orcid.org/0000-0001-8057-4490","contributorId":77889,"corporation":false,"usgs":true,"family":"Storlazzi","given":"Curt D.","affiliations":[],"preferred":false,"id":306675,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Presto, M. Katherine","contributorId":30192,"corporation":false,"usgs":true,"family":"Presto","given":"M. Katherine","affiliations":[],"preferred":false,"id":306673,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Logan, Joshua B.","contributorId":34470,"corporation":false,"usgs":true,"family":"Logan","given":"Joshua B.","affiliations":[],"preferred":false,"id":306674,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Field, Michael E. mfield@usgs.gov","contributorId":2101,"corporation":false,"usgs":true,"family":"Field","given":"Michael","email":"mfield@usgs.gov","middleInitial":"E.","affiliations":[{"id":520,"text":"Pacific Coastal and Marine Science Center","active":true,"usgs":true}],"preferred":true,"id":306672,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70188525,"text":"70188525 - 2010 - Climate change lessons from a warm world","interactions":[],"lastModifiedDate":"2017-06-14T12:52:25","indexId":"70188525","displayToPublicDate":"2010-10-26T00:00:00","publicationYear":"2010","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":5425,"text":"Transactions of the Leicester Literary & Philosophical Society","active":true,"publicationSubtype":{"id":10}},"title":"Climate change lessons from a warm world","docAbstract":"

In the early 1970’s to early 1980’s Soviet climatologists were making comparisons to past intervals of warmth in the geologic record and suggesting that these intervals could be possible analogs for 21st century “greenhouse” conditions. Some saw regional warming as a benefit to the Soviet Union and made comments along the lines of “Set fire to the coal mines!” These sentiments were alarming to some, and the United States Geological Survey (USGS) leadership thought they could provide a more quantitative analysis of the data the Soviets were using for the most recent of these warm intervals, the Early Pliocene.

","language":"English","publisher":"Leicester Literary & Philosophical Society","usgsCitation":"Dowsett, H.J., 2010, Climate change lessons from a warm world: Transactions of the Leicester Literary & Philosophical Society, v. 104, p. 50-55.","productDescription":"6 p.","startPage":"50","endPage":"55","ipdsId":"IP-020793","costCenters":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true}],"links":[{"id":342490,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"104","publishingServiceCenter":{"id":9,"text":"Reston PSC"},"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"59424b3de4b0764e6c65dc84","contributors":{"authors":[{"text":"Dowsett, Harry J. 0000-0003-1983-7524 hdowsett@usgs.gov","orcid":"https://orcid.org/0000-0003-1983-7524","contributorId":949,"corporation":false,"usgs":true,"family":"Dowsett","given":"Harry","email":"hdowsett@usgs.gov","middleInitial":"J.","affiliations":[{"id":40020,"text":"Florence Bascom Geoscience Center","active":true,"usgs":true},{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true}],"preferred":true,"id":698140,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":98826,"text":"sir20105068 - 2010 - Estimation of groundwater use for a groundwater-flow model of the Lake Michigan Basin and adjacent areas, 1864-2005","interactions":[],"lastModifiedDate":"2012-02-10T00:10:05","indexId":"sir20105068","displayToPublicDate":"2010-10-22T00:00:00","publicationYear":"2010","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":"2010-5068","title":"Estimation of groundwater use for a groundwater-flow model of the Lake Michigan Basin and adjacent areas, 1864-2005","docAbstract":"The U.S. Geological Survey, at the request of Congress, is assessing the availability and use of the Nation's water resources to help characterize how much water is available now, how water availability is changing, and how much water can be expected to be available in the future. The Great Lakes Basin Pilot project of the U.S. Geological Survey national assessment of water availability and use focused on the Great Lakes Basin and included detailed studies of the processes governing water availability in the Great Lakes Basin. One of these studies included the development of a groundwater-flow model of the Lake Michigan Basin. This report describes the compilation and estimation of the groundwater withdrawals in those areas in Wisconsin, Michigan, Indiana, and Illinois that were needed for the Lake Michigan Basin study groundwater-flow model. These data were aggregated for 12 model time intervals spanning 1864 to 2005 and were summarized by model area, model subregion, category of water use, aquifer system, aquifer type, and hydrogeologic unit model layer.\r\n\r\n\r\nThe types and availability of information on groundwater withdrawals vary considerably among states because water-use programs often differ in the types of data collected and in the methods and frequency of data collection. As a consequence, the methods used to estimate and verify the data also vary. Additionally, because of the different sources of data and different terminologies applied for the purposes of this report, the water-use data published in this report may differ from water-use data presented in other reports. These data represent only a partial estimate of groundwater use in each state because estimates were compiled only for areas in Wisconsin, Michigan, Indiana, and Illinois within the Lake Michigan Basin model area. Groundwater-withdrawal data were compiled for both nearfield and farfield model areas in Wisconsin and Illinois, whereas these data were compiled primarily for the nearfield model area in Michigan and Indiana.\r\n\r\n\r\nOverall water use for the selected areas in Wisconsin, Michigan, Indiana, and Illinois was less during early time intervals than during more recent intervals, with large increases beginning around the 1960s. Total estimated groundwater withdrawals for model input range from 18.01 million gallons per day (Mgal/d) for interval 1 (1864-1900) to 1,280.25 Mgal/d for interval 12 (2001-5). Withdrawals for the public-supply category make up the majority of the withdrawals in each of the four states. In Wisconsin and Michigan, the second largest withdrawals are for the irrigation category; in Indiana and Illinois, industrial withdrawals account for the second largest withdrawal amounts. The smallest withdrawals are for miscellaneous uses in Wisconsin and irrigation uses in Indiana and Illinois.\r\n\r\n\r\nEstimated groundwater withdrawals in the Southern Lower Peninsula of Michigan, Northeastern Illinois, and the farfield model area are generally larger than in the other model subregions. Withdrawals in Michigan and Indiana are predominantly from the Quaternary aquifer system, whereas withdrawals in Illinois are predominantly from the Cambrian-Ordovician aquifer systems. Withdrawals in Wisconsin are about equal from the Quaternary and Cambrian-Ordovician aquifer systems. Estimated groundwater withdrawals in Michigan and Indiana are predominantly from the unconfined unconsolidated aquifer type. Withdrawals in Illinois are largely from the deep confined bedrock aquifer type, although they decreased considerably in more recent time intervals. Wisconsin withdrawals are about equal from unconfined unconsolidated and deep confined bedrock aquifer types.\r\n\r\n\r\nGroundwater-withdrawal estimates in Wisconsin were compiled for the 47 easternmost counties within the boundary of the Lake Michigan Basin model, of which 32 counties, though not entirely contained, are at least partly within the Lake Michigan Basin. Overall, 6,457 withdrawal locations were estima","language":"ENGLISH","publisher":"U.S. Geological Survey","doi":"10.3133/sir20105068","collaboration":"National Water Availability and Use Pilot Program\r\n","usgsCitation":"Buchwald, C.A., Luukkonen, C.L., and Rachol, C.M., 2010, Estimation of groundwater use for a groundwater-flow model of the Lake Michigan Basin and adjacent areas, 1864-2005: U.S. Geological Survey Scientific Investigations Report 2010-5068, x, 90 p.; Appendices, https://doi.org/10.3133/sir20105068.","productDescription":"x, 90 p.; Appendices","additionalOnlineFiles":"N","costCenters":[{"id":446,"text":"National Water Availability and Use Great Lakes Pilot","active":false,"usgs":true}],"links":[{"id":126173,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2010_5068.jpg"},{"id":14240,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2010/5068/","linkFileType":{"id":5,"text":"html"}}],"geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -90,41 ], [ -90,46 ], [ -82,46 ], [ -82,41 ], [ -90,41 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a59e4b07f02db62f60e","contributors":{"authors":[{"text":"Buchwald, Cheryl A. 0000-0001-8968-5023 cabuchwa@usgs.gov","orcid":"https://orcid.org/0000-0001-8968-5023","contributorId":1943,"corporation":false,"usgs":true,"family":"Buchwald","given":"Cheryl","email":"cabuchwa@usgs.gov","middleInitial":"A.","affiliations":[{"id":37947,"text":"Upper Midwest Water Science Center","active":true,"usgs":true}],"preferred":true,"id":306627,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Luukkonen, Carol L. clluukko@usgs.gov","contributorId":3489,"corporation":false,"usgs":true,"family":"Luukkonen","given":"Carol","email":"clluukko@usgs.gov","middleInitial":"L.","affiliations":[{"id":382,"text":"Michigan Water Science Center","active":true,"usgs":true}],"preferred":true,"id":306629,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Rachol, Cynthia M. 0000-0001-9984-3435 crachol@usgs.gov","orcid":"https://orcid.org/0000-0001-9984-3435","contributorId":3488,"corporation":false,"usgs":true,"family":"Rachol","given":"Cynthia","email":"crachol@usgs.gov","middleInitial":"M.","affiliations":[{"id":423,"text":"National Geospatial Program","active":true,"usgs":true}],"preferred":true,"id":306628,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70156525,"text":"70156525 - 2010 - Integrated simulation of consumptive use and land subsidence in the Central Valley, California, for the past and for a future subject to urbanization and climate change","interactions":[],"lastModifiedDate":"2021-11-09T16:54:44.832371","indexId":"70156525","displayToPublicDate":"2010-10-17T00:00:00","publicationYear":"2010","noYear":false,"publicationType":{"id":24,"text":"Conference Paper"},"publicationSubtype":{"id":19,"text":"Conference Paper"},"title":"Integrated simulation of consumptive use and land subsidence in the Central Valley, California, for the past and for a future subject to urbanization and climate change","docAbstract":"

Competition for water resources is growing throughout California, particularly in the Central Valley where about 20% of all groundwater used in the United States is consumed for agriculture and urban water supply. Continued agricultural use coupled with urban growth and potential climate change would result in continued depletion of groundwater storage and associated land subsidence throughout the Central Valley. For 1962-2003, an estimated 1,230 hectare meters (hm3) of water was withdrawn from fine-grained beds, resulting in more than three meters (m) of additional land subsidence locally. Linked physically-based, supply-constrained and emanddriven hydrologic models were used to simulate future hydrologic conditions under the A2 climate projection scenario that assumes continued \"business as usual\" greenhouse gas emissions. Results indicate an increased subsidence in the second half of the twenty-first century. Potential simulated land subsidence extends into urban areas and the eastern side of the valley where future surface-water deliveries may be depleted. 

","largerWorkType":{"id":4,"text":"Book"},"largerWorkTitle":"Land subsidence, associated hazards and the role of natural resources development: EISOLS 2010 proceedings","largerWorkSubtype":{"id":12,"text":"Conference publication"},"conferenceTitle":"Eighth International Symposium on Land Subsidence (EISOLS) 2010","conferenceDate":"October 17-22, 2010","conferenceLocation":"Querétaro, Mexico","language":"English","publisher":"International Association of Hydrological Sciences","isbn":"1907161120 9781907161124","usgsCitation":"Hanson, R.T., Flint, A.L., Faunt, C., Cayan, D.R., Flint, L.E., Leake, S.A., and Schmid, W., 2010, Integrated simulation of consumptive use and land subsidence in the Central Valley, California, for the past and for a future subject to urbanization and climate change, in Land subsidence, associated hazards and the role of natural resources development: EISOLS 2010 proceedings, v. 339, Querétaro, Mexico, October 17-22, 2010, p. 467-471.","productDescription":"5 p.","startPage":"467","endPage":"471","onlineOnly":"N","additionalOnlineFiles":"N","ipdsId":"IP-020430","costCenters":[{"id":128,"text":"Arizona Water Science Center","active":true,"usgs":true},{"id":154,"text":"California Water Science Center","active":true,"usgs":true},{"id":657,"text":"Western Geographic Science Center","active":true,"usgs":true}],"links":[{"id":307245,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Central Valley","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -122.3876953125,\n 40.212440718286466\n ],\n [\n -122.4755859375,\n 39.24927084622338\n ],\n [\n -122.01416015625,\n 38.25543637637947\n ],\n [\n -121.04736328125,\n 37.10776507118514\n ],\n [\n -120.34423828125,\n 36.03133177633187\n ],\n [\n 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Center","active":true,"usgs":true}],"preferred":true,"id":569389,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Flint, Alan L. 0000-0002-5118-751X aflint@usgs.gov","orcid":"https://orcid.org/0000-0002-5118-751X","contributorId":1492,"corporation":false,"usgs":true,"family":"Flint","given":"Alan","email":"aflint@usgs.gov","middleInitial":"L.","affiliations":[{"id":154,"text":"California Water Science Center","active":true,"usgs":true},{"id":657,"text":"Western Geographic Science Center","active":true,"usgs":true}],"preferred":true,"id":569390,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Faunt, Claudia C. 0000-0001-5659-7529 ccfaunt@usgs.gov","orcid":"https://orcid.org/0000-0001-5659-7529","contributorId":1491,"corporation":false,"usgs":true,"family":"Faunt","given":"Claudia C.","email":"ccfaunt@usgs.gov","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":569391,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Cayan, Daniel R. 0000-0002-2719-6811 drcayan@usgs.gov","orcid":"https://orcid.org/0000-0002-2719-6811","contributorId":1494,"corporation":false,"usgs":true,"family":"Cayan","given":"Daniel","email":"drcayan@usgs.gov","middleInitial":"R.","affiliations":[],"preferred":false,"id":569392,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Flint, Lorraine E. 0000-0002-7868-441X lflint@usgs.gov","orcid":"https://orcid.org/0000-0002-7868-441X","contributorId":1184,"corporation":false,"usgs":true,"family":"Flint","given":"Lorraine","email":"lflint@usgs.gov","middleInitial":"E.","affiliations":[{"id":154,"text":"California Water Science Center","active":true,"usgs":true}],"preferred":true,"id":569393,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Leake, Stanley A. 0000-0003-3568-2542 saleake@usgs.gov","orcid":"https://orcid.org/0000-0003-3568-2542","contributorId":1846,"corporation":false,"usgs":true,"family":"Leake","given":"Stanley","email":"saleake@usgs.gov","middleInitial":"A.","affiliations":[{"id":128,"text":"Arizona Water Science Center","active":true,"usgs":true}],"preferred":true,"id":569394,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Schmid, Wolfgang","contributorId":84020,"corporation":false,"usgs":false,"family":"Schmid","given":"Wolfgang","affiliations":[{"id":13040,"text":"Department of Hydrology and Water Resources, University of Arizona","active":true,"usgs":false}],"preferred":false,"id":569395,"contributorType":{"id":1,"text":"Authors"},"rank":7}]}} ,{"id":98805,"text":"sir20105109 - 2010 - Regional groundwater-flow model of the Lake Michigan Basin in support of Great Lakes Basin water availability and use studies","interactions":[],"lastModifiedDate":"2022-10-17T21:05:34.176595","indexId":"sir20105109","displayToPublicDate":"2010-10-13T00:00:00","publicationYear":"2010","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":"2010-5109","title":"Regional groundwater-flow model of the Lake Michigan Basin in support of Great Lakes Basin water availability and use studies","docAbstract":"A regional groundwater-flow model of the Lake Michigan Basin and surrounding areas has been developed in support of the Great Lakes Basin Pilot project under the U.S. Geological Survey's National Water Availability and Use Program. The transient 2-million-cell model incorporates multiple aquifers and pumping centers that create water-level drawdown that extends into deep saline waters. The 20-layer model simulates the exchange between a dense surface-water network and heterogeneous glacial deposits overlying stratified bedrock of the Wisconsin/Kankakee Arches and Michigan Basin in the Lower and Upper Peninsulas of Michigan; eastern Wisconsin; northern Indiana; and northeastern Illinois. The model is used to quantify changes in the groundwater system in response to pumping and variations in recharge from 1864 to 2005. Model results quantify the sources of water to major pumping centers, illustrate the dynamics of the groundwater system, and yield measures of water availability useful for water-resources management in the region.\r\n\r\nThis report is a complete description of the methods and datasets used to develop the regional model, the underlying conceptual model, and model inputs, including specified values of material properties and the assignment of external and internal boundary conditions. The report also documents the application of the SEAWAT-2000 program for variable-density flow; it details the approach, advanced methods, and results associated with calibration through nonlinear regression using the PEST program; presents the water-level, drawdown, and groundwater flows for various geographic subregions and aquifer systems; and provides analyses of the effects of pumping from shallow and deep wells on sources of water to wells, the migration of groundwater divides, and direct and indirect groundwater discharge to Lake Michigan. The report considers the role of unconfined conditions at the regional scale as well as the influence of salinity on groundwater flow. Lastly, it describes several categories of limitations and discusses ways of extending the regional model to address issues at the local scale.\r\n\r\nResults of the simulations portray a regional groundwater-flow system that, over time, has largely maintained its natural predevelopment configuration but that locally has been strongly affected by well withdrawals. The quantity of rainfall in the Lake Michigan Basin and adjacent areas supports a dense surface-water network and recharge rates consistent with generally shallow water tables and predominantly shallow groundwater flow. At the regional scale, pumping has not caused major modifications of the shallow flow system, but it has resulted in decreases in base flow to streams and in direct discharge to Lake Michigan (about 2 percent of the groundwater discharged and about 0.5 cubic foot per second per mile of shoreline).\r\n\r\nOn the other hand, well withdrawals have caused major reversals in regional flow patterns around pumping centers in deep, confined aquifers - most noticeably in the Cambrian-Ordovician aquifer system on the west side of Lake Michigan near the cities of Green Bay and Milwaukee in eastern Wisconsin, and around Chicago in northeastern Illinois, as well as in some shallow bedrock aquifers (for example, in the Marshall aquifer near Lansing, Mich.). The reversals in flow have been accompanied by large drawdowns with consequent local decrease in storage. On the west side of Lake Michigan, groundwater withdrawals have caused appreciable migration of the deep groundwater divides. Before the advent of pumping, the deep Lake Michigan groundwater-basin boundaries extended west of the Lake Michigan surface-water basin boundary, in some places by tens of miles. Over time, the pumping centers have replaced Lake Michigan as the regional sink for the deep flow system.\r\n\r\nThe regional model is intended to support the framework pilot study of water availability and use for the Great Lakes Basin (Reeves, in press).","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/sir20105109","collaboration":"National Water Availability and Use Pilot Program","usgsCitation":"Feinstein, D.T., Hunt, R.J., and Reeves, H.W., 2010, Regional groundwater-flow model of the Lake Michigan Basin in support of Great Lakes Basin water availability and use studies: U.S. Geological Survey Scientific Investigations Report 2010-5109, Report: xix, 379 p.; 9 Appendices, https://doi.org/10.3133/sir20105109.","productDescription":"Report: xix, 379 p.; 9 Appendices","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[{"id":448,"text":"National Water Availability and Use Program","active":false,"usgs":true}],"links":[{"id":126010,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2010_5109.jpg"},{"id":14217,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2010/5109/","linkFileType":{"id":5,"text":"html"}},{"id":408437,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_94378.htm","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Illinois, Indiana, Michigan, Wisconsin","otherGeospatial":"Lake Michigan Basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -90,\n 41.25\n ],\n [\n -84,\n 41.25\n ],\n [\n -84,\n 46.6167\n ],\n [\n -90,\n 46.6167\n ],\n [\n -90,\n 41.25\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c5de","contributors":{"authors":[{"text":"Feinstein, D. T.","contributorId":47328,"corporation":false,"usgs":true,"family":"Feinstein","given":"D.","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":306561,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hunt, R. J.","contributorId":40164,"corporation":false,"usgs":true,"family":"Hunt","given":"R.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":306560,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Reeves, H. W.","contributorId":53739,"corporation":false,"usgs":true,"family":"Reeves","given":"H.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":306562,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70217565,"text":"70217565 - 2010 - Age and sex specific timing, frequency, and spatial distribution of horseshoe crab spawning in Delaware Bay: Insights from a large-scale radio telemetry array","interactions":[],"lastModifiedDate":"2021-01-21T23:39:59.605592","indexId":"70217565","displayToPublicDate":"2010-10-01T16:42:39","publicationYear":"2010","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1362,"text":"Current Zoology","active":true,"publicationSubtype":{"id":10}},"title":"Age and sex specific timing, frequency, and spatial distribution of horseshoe crab spawning in Delaware Bay: Insights from a large-scale radio telemetry array","docAbstract":"

To study horseshoe crab Limulus polyphemus spawning behavior and migration over a large-spatial extent (>100 km), we arrayed fixed station radio receivers throughout Delaware Bay and deployed radio transmitters and archival tags on adult horseshoe crabs prior to their spawning season. We tagged and released 160 females and 60 males in 2004 and 217 females in 2005. The array covered approximately 140 km of shoreline. Recapture rates were >70% with multi-year recaptures. We categorized adult age by carapace wear. Older females tended to spawn earlier in the season and more frequently than young females, but those tendencies were more apparent in 2004 when spawning overall occurred earlier than in 2005 when spawning was delayed possibly due to decreased water temperatures. Timing of initial spawning within a year was correlated with water temperature. After adjusting for day of first spring tide, the day of first spawning was 4 days earlier for every 1 degree (̊C) rise in mean daily water temperature in May. Seventy nine % of spawning occurred during nighttime high tides. Fifty five % of spawning occurred within 3 d of a spring tide, which was slightly higher than the 47% expected if spawning was uniformly distributed regardless of tidal cycle. Within the same spawning season, males and females were observed spawning or intertidally resting at more than one beach separated by >5 km. Between years, most (77%) did not return to spawn at the same beach. Probability of stranding was strongly age dependent for males and females with older adults experiencing higher stranding rates. Horseshoe crabs staging in the shallow waters east of the channel spawned exclusively along the eastern (NJ) shoreline, but those staging west of the channel spawned throughout the bay. Overall, several insights emerged from the use of radio telemetry, which advances our understanding of horseshoe crab ecology and will be useful in conserving the Delaware Bay horseshoe crab population and habitats.

","language":"English","publisher":"Oxford Academic","doi":"10.1093/czoolo/56.5.563","usgsCitation":"Smith, D.R., Brousseau, L.J., Mandt, M.T., and Millard, M.J., 2010, Age and sex specific timing, frequency, and spatial distribution of horseshoe crab spawning in Delaware Bay: Insights from a large-scale radio telemetry array: Current Zoology, v. 56, no. 5, p. 563-574, https://doi.org/10.1093/czoolo/56.5.563.","productDescription":"12 p.","startPage":"563","endPage":"574","costCenters":[{"id":365,"text":"Leetown Science Center","active":true,"usgs":true}],"links":[{"id":475656,"rank":0,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.1093/czoolo/56.5.563","text":"Publisher Index Page"},{"id":382468,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Delaware, New Jersey","otherGeospatial":"Delaware Bay","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -75.6134033203125,\n 38.70694605159386\n ],\n [\n -74.849853515625,\n 38.70694605159386\n ],\n [\n -74.849853515625,\n 39.53370327008705\n ],\n [\n -75.6134033203125,\n 39.53370327008705\n ],\n [\n -75.6134033203125,\n 38.70694605159386\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"56","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Smith, David R. 0000-0001-6074-9257 drsmith@usgs.gov","orcid":"https://orcid.org/0000-0001-6074-9257","contributorId":168442,"corporation":false,"usgs":true,"family":"Smith","given":"David","email":"drsmith@usgs.gov","middleInitial":"R.","affiliations":[{"id":365,"text":"Leetown Science Center","active":true,"usgs":true}],"preferred":true,"id":808688,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Brousseau, L. J.","contributorId":24534,"corporation":false,"usgs":false,"family":"Brousseau","given":"L.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":808689,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Mandt, Mary T.","contributorId":248260,"corporation":false,"usgs":false,"family":"Mandt","given":"Mary","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":808690,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Millard, Michael J.","contributorId":23411,"corporation":false,"usgs":false,"family":"Millard","given":"Michael","email":"","middleInitial":"J.","affiliations":[{"id":6987,"text":"U.S. Fish and Wildlife Sevice","active":true,"usgs":false}],"preferred":false,"id":808691,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70236110,"text":"70236110 - 2010 - Development of characterization technology for fault zone hydrology","interactions":[],"lastModifiedDate":"2022-08-29T15:40:00.044797","indexId":"70236110","displayToPublicDate":"2010-10-01T10:06:32","publicationYear":"2010","noYear":false,"publicationType":{"id":24,"text":"Conference Paper"},"publicationSubtype":{"id":19,"text":"Conference Paper"},"title":"Development of characterization technology for fault zone hydrology","docAbstract":"

Several deep trenches were cut, and a number of geophysical surveys were conducted across the Wildcat Fault in the hills east of Berkeley, California. The Wildcat Fault is believed to be a strike-slip fault and a member of the Hayward Fault System, with over 10 km of displacement. So far, three boreholes of ∼ 150m deep have been core-drilled and borehole geophysical logs were conducted. The rocks are extensively sheared and fractured; gouges were observed at several depths and a thick cataclasitic zone was also observed. While confirming some earlier, published conclusions from shallow observations about Wildcat, some unexpected findings were encountered. Preliminary analysis indicates that Wildcat near the field site consists of multiple faults. The hydraulic test data suggest the dual properties of the hydrologic structure of the fault zone. A fourth borehole is planned to penetrate the main fault believed to lie in-between the holes. The main philosophy behind our approach for the hydrologic characterization of such a complex fractured system is to let the system take its own average and monitor a long term behavior instead of collecting a multitude of data at small length and time scales, or at a discrete fracture scale and to “up-scale,” which is extremely tenuous.

","largerWorkType":{"id":4,"text":"Book"},"largerWorkTitle":"Conference proceedings: International Conference on Environmental Remediation and Radioactive Waste Management","largerWorkSubtype":{"id":12,"text":"Conference publication"},"conferenceTitle":"13th International Conference on Environmental Remediation and Radioactive Waste Management","conferenceDate":"October 3-7, 2010","conferenceLocation":"Tsukuba, Japan","language":"English","publisher":"American Society of Mechanical Engineers","doi":"10.1115/ICEM2010-40121","usgsCitation":"Karasaki, K., Onishi, C.T., Gasperikova, E., Goto, J., Tsuchi, H., Miwa, T., Ueta, K., Kiho, K., and Miyakawa, K., 2010, Development of characterization technology for fault zone hydrology, in Conference proceedings: International Conference on Environmental Remediation and Radioactive Waste Management, Tsukuba, Japan, October 3-7, 2010, p. 297-303, https://doi.org/10.1115/ICEM2010-40121.","productDescription":"ICEM2010-40121, 7 p.","startPage":"297","endPage":"303","costCenters":[],"links":[{"id":475661,"rank":0,"type":{"id":41,"text":"Open Access External Repository Page"},"url":"https://digital.library.unt.edu/ark:/67531/metadc1014656/","text":"External Repository"},{"id":405795,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Berkeley Hills, Wildcat Fault","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -122.431640625,\n 37.96477144899956\n ],\n [\n -122.34649658203124,\n 37.769629187677\n ],\n [\n -122.16796875,\n 37.790251927933284\n ],\n [\n -122.27508544921875,\n 38.04592811939909\n ],\n [\n -122.37533569335936,\n 38.023213306976814\n ],\n [\n -122.431640625,\n 37.96477144899956\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationDate":"2011-04-05","publicationStatus":"PW","contributors":{"authors":[{"text":"Karasaki, K.","contributorId":30004,"corporation":false,"usgs":true,"family":"Karasaki","given":"K.","email":"","affiliations":[],"preferred":false,"id":850094,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Onishi, Celia Tiemi","contributorId":295897,"corporation":false,"usgs":false,"family":"Onishi","given":"Celia","email":"","middleInitial":"Tiemi","affiliations":[],"preferred":false,"id":850095,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Gasperikova, Erika","contributorId":193561,"corporation":false,"usgs":false,"family":"Gasperikova","given":"Erika","affiliations":[],"preferred":false,"id":850096,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Goto, Junichi","contributorId":295898,"corporation":false,"usgs":false,"family":"Goto","given":"Junichi","email":"","affiliations":[],"preferred":false,"id":850097,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Tsuchi, Hiroyuki","contributorId":295899,"corporation":false,"usgs":false,"family":"Tsuchi","given":"Hiroyuki","email":"","affiliations":[],"preferred":false,"id":850098,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Miwa, Tadashi","contributorId":295900,"corporation":false,"usgs":false,"family":"Miwa","given":"Tadashi","email":"","affiliations":[],"preferred":false,"id":850099,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Ueta, Keiichi","contributorId":295901,"corporation":false,"usgs":false,"family":"Ueta","given":"Keiichi","email":"","affiliations":[],"preferred":false,"id":850100,"contributorType":{"id":1,"text":"Authors"},"rank":7},{"text":"Kiho, Kenzo","contributorId":295902,"corporation":false,"usgs":false,"family":"Kiho","given":"Kenzo","email":"","affiliations":[],"preferred":false,"id":850101,"contributorType":{"id":1,"text":"Authors"},"rank":8},{"text":"Miyakawa, Kimio","contributorId":295903,"corporation":false,"usgs":false,"family":"Miyakawa","given":"Kimio","email":"","affiliations":[],"preferred":false,"id":850102,"contributorType":{"id":1,"text":"Authors"},"rank":9}]}} ,{"id":98757,"text":"ds303 - 2010 - Database for the geologic map of the Bend 30- x 60-minute quadrangle, central Oregon","interactions":[],"lastModifiedDate":"2023-11-01T21:42:54.683315","indexId":"ds303","displayToPublicDate":"2010-09-30T00:00:00","publicationYear":"2010","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":310,"text":"Data Series","code":"DS","onlineIssn":"2327-638X","printIssn":"2327-0271","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"303","title":"Database for the geologic map of the Bend 30- x 60-minute quadrangle, central Oregon","docAbstract":"The Bend 30- x 60-minute quadrangle has been the locus of volcanism, faulting, and sedimentation for the past 35 million years. It encompasses parts of the Cascade Range and Blue Mountain geomorphic provinces, stretching from snowclad Quaternary stratovolcanoes on the west to bare rocky hills and sparsely forested juniper plains on the east. The Deschutes River and its large tributaries, the Metolius and Crooked Rivers, drain the area. Topographic relief ranges from 3,157 m (10,358 ft) at the top of South Sister to 590 m (1,940 ft) at the floor of the Deschutes and Crooked Rivers where they exit the area at the north-central edge of the map area. The map encompasses a part of rapidly growing Deschutes County. The city of Bend, which has over 70,000 people living in its urban growth boundary, lies at the south-central edge of the map. Redmond, Sisters, and a few smaller villages lie scattered along the major transportation routes of U.S. Highways 97 and 20.\r\n\r\nThis geologic map depicts the geologic setting as a basis for structural and stratigraphic analysis of the Deschutes basin, a major hydrologic discharge area on the east flank of the Cascade Range. The map also provides a framework for studying potentially active faults of the Sisters fault zone, which trends northwest across the map area from Bend to beyond Sisters.\r\n\r\nThis digital release contains all of the information used to produce the geologic map published as U.S. Geological Survey Geologic Investigations Series I-2683 (Sherrod and others, 2004). The main component of this digital release is a geologic map database prepared using ArcInfo GIS. This release also contains files to view or print the geologic map and accompanying descriptive pamphlet from I-2683.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ds303","usgsCitation":"Koch, R.D., Ramsey, D.W., Sherrod, D.R., Taylor, E.M., Ferns, M., Scott, W.E., Conrey, R.M., and Smith, G.A., 2010, Database for the geologic map of the Bend 30- x 60-minute quadrangle, central Oregon: U.S. Geological Survey Data Series 303, HTML Document; CD-ROM, https://doi.org/10.3133/ds303.","productDescription":"HTML Document; CD-ROM","onlineOnly":"Y","additionalOnlineFiles":"Y","costCenters":[{"id":271,"text":"Federal Center","active":false,"usgs":true},{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"links":[{"id":422320,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_94310.htm","linkFileType":{"id":5,"text":"html"}},{"id":14167,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/ds/303/","linkFileType":{"id":5,"text":"html"}},{"id":125990,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ds_303.jpg"}],"country":"United States","state":"Oregon","otherGeospatial":"Bend 30- x 60-minute quadrangle","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -122,\n 44.5\n ],\n [\n -122,\n 44\n ],\n [\n -121,\n 44\n ],\n [\n -121,\n 44.5\n ],\n [\n -122,\n 44.5\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4abbe4b07f02db672a4d","contributors":{"authors":[{"text":"Koch, Richard D. rkoch@usgs.gov","contributorId":4413,"corporation":false,"usgs":true,"family":"Koch","given":"Richard","email":"rkoch@usgs.gov","middleInitial":"D.","affiliations":[],"preferred":true,"id":306380,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Ramsey, David W. 0000-0003-1698-2523 dramsey@usgs.gov","orcid":"https://orcid.org/0000-0003-1698-2523","contributorId":3819,"corporation":false,"usgs":true,"family":"Ramsey","given":"David","email":"dramsey@usgs.gov","middleInitial":"W.","affiliations":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"preferred":true,"id":306379,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Sherrod, David R. 0000-0001-9460-0434 dsherrod@usgs.gov","orcid":"https://orcid.org/0000-0001-9460-0434","contributorId":527,"corporation":false,"usgs":true,"family":"Sherrod","given":"David","email":"dsherrod@usgs.gov","middleInitial":"R.","affiliations":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"preferred":true,"id":306377,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Taylor, Edward M.","contributorId":65932,"corporation":false,"usgs":true,"family":"Taylor","given":"Edward","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":306383,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Ferns, Mark L.","contributorId":13703,"corporation":false,"usgs":true,"family":"Ferns","given":"Mark L.","affiliations":[],"preferred":false,"id":306381,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Scott, William E. 0000-0001-8156-979X wescott@usgs.gov","orcid":"https://orcid.org/0000-0001-8156-979X","contributorId":1725,"corporation":false,"usgs":true,"family":"Scott","given":"William","email":"wescott@usgs.gov","middleInitial":"E.","affiliations":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"preferred":true,"id":306378,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Conrey, Richard M.","contributorId":41911,"corporation":false,"usgs":true,"family":"Conrey","given":"Richard","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":306382,"contributorType":{"id":1,"text":"Authors"},"rank":7},{"text":"Smith, Gary A.","contributorId":81196,"corporation":false,"usgs":true,"family":"Smith","given":"Gary","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":306384,"contributorType":{"id":1,"text":"Authors"},"rank":8}]}} ]}