This report is a new compilation of the location and extent of folds and faults in Cook Inlet Basin, Alaska. Data sources are previously published maps, well locations, and seismic-reflection data. We also utilize interpretation of new aeromagnetic data and some proprietary seismic-reflection data. Some structures are remarkably well displayed on frequency-filtered aeromagnetic maps, which are a useful tool for constraining the length of some structures. Most anticlines in and around the basin have at least shows of oil or gas, and some structures are considered to be seismically active. The new map better displays the pattern of faulting and folding. Deformation is greatest in upper Cook Inlet, where structures are oriented slightly counterclockwise of the basin bounding faults. The north ends of these structures bend to the northeast, which gives a pattern consistent with right-transpressional deformation.
Subduction of the buoyant Yakutat microplate likely caused deformation to be focused preferentially in upper Cook Inlet. The upper Cook Inlet region has both the highest degree of shortening and the deepest part of the Neogene basin. This forearc region has a long-wavelength magnetic high, a large isostatic gravity low, high conductivity in the lower mantle, low p-wave velocity (Vp), and a high p-wave to shear-wave velocity ratio (Vp/Vs). These data suggest that fluids in the mantle wedge caused serpentinization of mafic rocks, which may, at least in part, contribute to the long-wavelength magnetic anomaly. This area lies adjacent to the subducting and buoyant Yakutat microplate slab. We suggest the buoyant Yakutat slab acts much like a squeegee to focus mantle-wedge fluid flow at the margins of the buoyant slab. Such lateral flow is consistent with observed shear-wave splitting directions. The additional fluid in the adjacent mantle wedge reduces the wedge viscosity and allows greater corner flow. This results in focused subsidence, deformation, and gravity anomalies in the forearc region.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/pp1776D","usgsCitation":"Haeussler, P.J., and Saltus, R.W., 2011, Location and extent of Tertiary structures in Cook Inlet Basin, Alaska, and mantle dynamics that focus deformation and subsidence: U.S. Geological Survey Professional Paper 1776, Report:iv, 26 p.; Data Files, https://doi.org/10.3133/pp1776D.","productDescription":"Report:iv, 26 p.; Data Files","numberOfPages":"30","onlineOnly":"Y","additionalOnlineFiles":"Y","costCenters":[{"id":114,"text":"Alaska Science Center","active":true,"usgs":true}],"links":[{"id":422401,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_95301.htm","linkFileType":{"id":5,"text":"html"}},{"id":22676,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pp/1776/d/","linkFileType":{"id":5,"text":"html"}},{"id":116598,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.er.usgs.gov/thumbnails/pp_1776_D.gif"}],"country":"United States","state":"Alaska","otherGeospatial":"Cook Inlet Basin","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -154,58.5 ], [ -154,62 ], [ -149,62 ], [ -149,58.5 ], [ -154,58.5 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a69e4b07f02db63ba98","contributors":{"authors":[{"text":"Haeussler, Peter J. 0000-0002-1503-6247 pheuslr@usgs.gov","orcid":"https://orcid.org/0000-0002-1503-6247","contributorId":503,"corporation":false,"usgs":true,"family":"Haeussler","given":"Peter","email":"pheuslr@usgs.gov","middleInitial":"J.","affiliations":[{"id":114,"text":"Alaska Science Center","active":true,"usgs":true},{"id":119,"text":"Alaska Science Center Geology Minerals","active":true,"usgs":true}],"preferred":true,"id":351377,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Saltus, Richard W. saltus@usgs.gov","contributorId":777,"corporation":false,"usgs":true,"family":"Saltus","given":"Richard","email":"saltus@usgs.gov","middleInitial":"W.","affiliations":[{"id":211,"text":"Crustal Geophysics and Geochemistry Science Center","active":true,"usgs":true}],"preferred":true,"id":351378,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70004805,"text":"fs20113061 - 2011 - The aquatic real-time monitoring network; in-situ optical sensors for monitoring the nation's water quality","interactions":[],"lastModifiedDate":"2019-07-09T15:16:36","indexId":"fs20113061","displayToPublicDate":"2011-07-12T00:00:00","publicationYear":"2011","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":"2011-3061","title":"The aquatic real-time monitoring network; in-situ optical sensors for monitoring the nation's water quality","docAbstract":"Floods, hurricanes, and longer-term changes in climate and land use can have profound effects on water quality due to shifts in hydrologic flow paths, water residence time, precipitation patterns, connectivity between rivers and uplands, and many other factors. In order to understand and respond to changes in hydrology and water quality, resource managers and policy makers have a need for accurate and early indicators, as well as the ability to assess possible mechanisms and likely outcomes. In-situ optical sensors-those making continuous measurements of constituents by absorbance or fluorescence properties in the environment at timescales of minutes to years-have a long history in oceanography for developing highly resolved concentrations and fluxes, but are not commonly used in freshwater systems. The United States Geological Survey (USGS) has developed the Aquatic Real-Time Monitoring Network, with high-resolution optical data collection for organic carbon, nutrients, and sediment in large coastal rivers, along with continuous measurements of discharge, water temperature, and dissolved inorganic carbon. The collecting of continuous water-quality data in the Nation?s waterways has revealed temporal trends and spatial patterns in constituents that traditional sampling approaches fail to capture, and will serve a critical role in monitoring, assessment and decision-making in a rapidly changing landscape.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/fs20113061","usgsCitation":"Pellerin, B., Bergamaschi, B., Murdoch, P.S., Downing, B.D., Saraceno, J., Aiken, G.R., and Striegl, R.G., 2011, The aquatic real-time monitoring network; in-situ optical sensors for monitoring the nation's water quality: U.S. Geological Survey Fact Sheet 2011-3061, 2 p., https://doi.org/10.3133/fs20113061.","productDescription":"2 p.","startPage":"1","endPage":"2","numberOfPages":"2","onlineOnly":"Y","additionalOnlineFiles":"N","costCenters":[{"id":154,"text":"California Water Science Center","active":true,"usgs":true},{"id":589,"text":"Toxic Substances Hydrology Program","active":true,"usgs":true}],"links":[{"id":116599,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/fs_2011_3061.gif"},{"id":22677,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/fs/2011/3061/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aaae4b07f02db6697af","contributors":{"authors":[{"text":"Pellerin, Brian A.","contributorId":58385,"corporation":false,"usgs":true,"family":"Pellerin","given":"Brian A.","affiliations":[],"preferred":false,"id":351383,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bergamaschi, Brian A. 0000-0002-9610-5581","orcid":"https://orcid.org/0000-0002-9610-5581","contributorId":73241,"corporation":false,"usgs":true,"family":"Bergamaschi","given":"Brian A.","affiliations":[],"preferred":false,"id":351385,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Murdoch, Peter S. 0000-0001-9243-505X pmurdoch@usgs.gov","orcid":"https://orcid.org/0000-0001-9243-505X","contributorId":2453,"corporation":false,"usgs":true,"family":"Murdoch","given":"Peter","email":"pmurdoch@usgs.gov","middleInitial":"S.","affiliations":[{"id":5067,"text":"Northeast Regional Director's Office","active":true,"usgs":true}],"preferred":true,"id":351381,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Downing, Bryan D. 0000-0002-2007-5304 bdowning@usgs.gov","orcid":"https://orcid.org/0000-0002-2007-5304","contributorId":1449,"corporation":false,"usgs":true,"family":"Downing","given":"Bryan","email":"bdowning@usgs.gov","middleInitial":"D.","affiliations":[{"id":154,"text":"California Water Science Center","active":true,"usgs":true}],"preferred":true,"id":351380,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Saraceno, John Franco 0000-0003-0064-1820","orcid":"https://orcid.org/0000-0003-0064-1820","contributorId":71686,"corporation":false,"usgs":true,"family":"Saraceno","given":"John Franco","affiliations":[],"preferred":false,"id":351384,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Aiken, George R. 0000-0001-8454-0984 graiken@usgs.gov","orcid":"https://orcid.org/0000-0001-8454-0984","contributorId":1322,"corporation":false,"usgs":true,"family":"Aiken","given":"George","email":"graiken@usgs.gov","middleInitial":"R.","affiliations":[{"id":5044,"text":"National Research Program - Central Branch","active":true,"usgs":true},{"id":191,"text":"Colorado Water Science Center","active":true,"usgs":true}],"preferred":true,"id":351379,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Striegl, Robert G. 0000-0002-8251-4659 rstriegl@usgs.gov","orcid":"https://orcid.org/0000-0002-8251-4659","contributorId":1630,"corporation":false,"usgs":true,"family":"Striegl","given":"Robert","email":"rstriegl@usgs.gov","middleInitial":"G.","affiliations":[{"id":5044,"text":"National Research Program - Central Branch","active":true,"usgs":true},{"id":200,"text":"Coop Res Unit Seattle","active":true,"usgs":true},{"id":36183,"text":"Hydro-Ecological Interactions Branch","active":true,"usgs":true},{"id":37277,"text":"WMA - Earth System Processes Division","active":true,"usgs":true}],"preferred":false,"id":351382,"contributorType":{"id":1,"text":"Authors"},"rank":7}]}} ,{"id":70004742,"text":"sir20115047 - 2011 - Estimated probabilities, volumes, and inundation area depths of potential postwildfire debris flows from Carbonate, Slate, Raspberry, and Milton Creeks, near Marble, Gunnison County, Colorado","interactions":[],"lastModifiedDate":"2022-01-11T20:54:13.515301","indexId":"sir20115047","displayToPublicDate":"2011-07-12T00:00:00","publicationYear":"2011","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":"2011-5047","title":"Estimated probabilities, volumes, and inundation area depths of potential postwildfire debris flows from Carbonate, Slate, Raspberry, and Milton Creeks, near Marble, Gunnison County, Colorado","docAbstract":"During 2009, the U.S. Geological Survey, in cooperation with Gunnison County, initiated a study to estimate the potential for postwildfire debris flows to occur in the drainage basins occupied by Carbonate, Slate, Raspberry, and Milton Creeks near Marble, Colorado. Currently (2010), these drainage basins are unburned but could be burned by a future wildfire. Empirical models derived from statistical evaluation of data collected from recently burned basins throughout the intermountain western United States were used to estimate the probability of postwildfire debris-flow occurrence and debris-flow volumes for drainage basins occupied by Carbonate, Slate, Raspberry, and Milton Creeks near Marble. Data for the postwildfire debris-flow models included drainage basin area; area burned and burn severity; percentage of burned area; soil properties; rainfall total and intensity for the 5- and 25-year-recurrence, 1-hour-duration-rainfall; and topographic and soil property characteristics of the drainage basins occupied by the four creeks. A quasi-two-dimensional floodplain computer model (FLO-2D) was used to estimate the spatial distribution and the maximum instantaneous depth of the postwildfire debris-flow material during debris flow on the existing debris-flow fans that issue from the outlets of the four major drainage basins. \n\nThe postwildfire debris-flow probabilities at the outlet of each drainage basin range from 1 to 19 percent for the 5-year-recurrence, 1-hour-duration rainfall, and from 3 to 35 percent for 25-year-recurrence, 1-hour-duration rainfall. The largest probabilities for postwildfire debris flow are estimated for Raspberry Creek (19 and 35 percent), whereas estimated debris-flow probabilities for the three other creeks range from 1 to 6 percent. The estimated postwildfire debris-flow volumes at the outlet of each creek range from 7,500 to 101,000 cubic meters for the 5-year-recurrence, 1-hour-duration rainfall, and from 9,400 to 126,000 cubic meters for the 25-year-recurrence, 1-hour-duration rainfall. The largest postwildfire debris-flow volumes were estimated for Carbonate Creek and Milton Creek drainage basins, for both the 5- and 25-year-recurrence, 1-hour-duration rainfalls. \n\nResults from FLO-2D modeling of the 5-year and 25-year recurrence, 1-hour rainfalls indicate that the debris flows from the four drainage basins would reach or nearly reach the Crystal River. The model estimates maximum instantaneous depths of debris-flow material during postwildfire debris flows that exceeded 5 meters in some areas, but the differences in model results between the 5-year and 25-year recurrence, 1-hour rainfalls are small. Existing stream channels or topographic flow paths likely control the distribution of debris-flow material, and the difference in estimated debris-flow volume (about 25 percent more volume for the 25-year-recurrence, 1-hour-duration rainfall compared to the 5-year-recurrence, 1-hour-duration rainfall) does not seem to substantially affect the estimated spatial distribution of debris-flow material. \n\nHistorically, the Marble area has experienced periodic debris flows in the absence of wildfire. This report estimates the probability and volume of debris flow and maximum instantaneous inundation area depths after hypothetical wildfire and rainfall. This postwildfire debris-flow report does not address the current (2010) prewildfire debris-flow hazards that exist near Marble.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/sir20115047","usgsCitation":"Stevens, M.R., Flynn, J.L., Stephens, V.C., and Verdin, K.L., 2011, Estimated probabilities, volumes, and inundation area depths of potential postwildfire debris flows from Carbonate, Slate, Raspberry, and Milton Creeks, near Marble, Gunnison County, Colorado: U.S. Geological Survey Scientific Investigations Report 2011-5047, v, 30 p., https://doi.org/10.3133/sir20115047.","productDescription":"v, 30 p.","numberOfPages":"35","onlineOnly":"Y","additionalOnlineFiles":"N","costCenters":[{"id":191,"text":"Colorado Water Science Center","active":true,"usgs":true},{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":394213,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_95271.htm"},{"id":21945,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2011/5047/","linkFileType":{"id":5,"text":"html"}},{"id":116614,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2011_5047.png"}],"scale":"24000","projection":"Universal Transverst Mercator projection","datum":"North American Datum of 1983","country":"United States","state":"Colorado","county":"Gunnison County","otherGeospatial":"Carbonate, Slate, Raspberry, and Milton Creeks","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -107.28595733642578,\n 39.019450429324024\n ],\n [\n -107.08683013916014,\n 39.019450429324024\n ],\n [\n -107.08683013916014,\n 39.11008335334396\n ],\n [\n -107.28595733642578,\n 39.11008335334396\n ],\n [\n -107.28595733642578,\n 39.019450429324024\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0ce4b07f02db5fcd54","contributors":{"authors":[{"text":"Stevens, Michael R. 0000-0002-9476-6335 mrsteven@usgs.gov","orcid":"https://orcid.org/0000-0002-9476-6335","contributorId":769,"corporation":false,"usgs":true,"family":"Stevens","given":"Michael","email":"mrsteven@usgs.gov","middleInitial":"R.","affiliations":[{"id":191,"text":"Colorado Water Science Center","active":true,"usgs":true}],"preferred":true,"id":351240,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Flynn, Jennifer L.","contributorId":66298,"corporation":false,"usgs":true,"family":"Flynn","given":"Jennifer","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":351243,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Stephens, Verlin C.","contributorId":34479,"corporation":false,"usgs":true,"family":"Stephens","given":"Verlin","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":351242,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Verdin, Kristine L. 0000-0002-6114-4660 kverdin@usgs.gov","orcid":"https://orcid.org/0000-0002-6114-4660","contributorId":3070,"corporation":false,"usgs":true,"family":"Verdin","given":"Kristine","email":"kverdin@usgs.gov","middleInitial":"L.","affiliations":[{"id":222,"text":"Earth Resources Observation and Science (EROS) Center","active":true,"usgs":true},{"id":191,"text":"Colorado Water Science Center","active":true,"usgs":true}],"preferred":true,"id":351241,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70004807,"text":"sir20115056 - 2011 - Hydrologic assessment of three drainage basins in the Pinelands of southern New Jersey, 2004-06","interactions":[],"lastModifiedDate":"2012-03-08T17:16:41","indexId":"sir20115056","displayToPublicDate":"2011-07-12T00:00:00","publicationYear":"2011","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":"2011-5056","title":"Hydrologic assessment of three drainage basins in the Pinelands of southern New Jersey, 2004-06","docAbstract":"The New Jersey Pinelands is an ecologically diverse area in the southern New Jersey Coastal Plain, most of which overlies the Kirkwood-Cohansey aquifer system. The demand for groundwater from this aquifer system is increasing as local development increases. Because any increase in groundwater withdrawals has the potential to affect streamflows and wetland water levels, and ultimately threaten the ecological health and diversity of the Pinelands ecosystem, the U.S. Geological Survey, in cooperation with the New Jersey Pinelands Commission, began a multi-phase hydrologic investigation in 2004 to characterize the hydrologic system supporting the aquatic and wetland communities of the New Jersey Pinelands area (Pinelands). The current investigation of the hydrology of three representative drainage basins in the Pinelands (Albertson Brook, McDonalds Branch, and Morses Mill Stream basins) included a compilation of existing data; collection of water-level and streamflow data; mapping of the water-table altitude and depth to the water table; and analyses of water-level and streamflow variability, subsurface gradients and flow patterns, and water budgets. During 2004-06, a hydrologic database of existing and new data from wells and stream sites was compiled. Methods of data collection and analysis were defined, and data networks consisting of 471 wells and 106 surface-water sites were established. Hydrographs from 26 water-level-monitoring wells and four streamflow-gaging stations were analyzed to show the response of water levels and streamflow to precipitation and recharge with respect to the locations of these wells and streams within each basin. Water-level hydrographs show varying hydraulic gradients and flow potentials, and indicate that responses to recharge events vary with well depth and proximity to recharge and discharge areas. Results of the investigation provide a detailed characterization of hydrologic conditions, processes, and relations among the components of the hydrologic cycle in the Pinelands. In the Pinelands, recharge replenishes the aquifer system and contributes to groundwater flow, most of which moves to wetlands and surface water where natural discharge occurs. Some groundwater flow is intercepted by supply wells. Recharge rates generally are highest during the non-growing season and are inversely related to evapotranspiration. Analysis of subsurface hydraulic gradients, water-table fluctuations, and streamflow variability indicates a strong linkage between groundwater and wetlands, lakes and streams. Gradient analysis indicates that most wetlands are in groundwater discharge areas, but some wetlands are in groundwater recharge areas. The depth to the water table ranges from zero at surface-water features up to about 10 meters in topographically high areas. Depth to water fluctuates seasonally, and the magnitude of these fluctuations generally increases with distance from surface water. Variations in the permeability of the soils and sediments of the aquifer system strongly affect patterns of water movement through the subsurface and the interaction of groundwater with wetlands, lakes and streams. Mean annual streamflow during 2004-06 ranged from 83 to 106 percent of the long-term mean annual discharge, indicating that the data-collection period can be considered representative of average conditions. Measurements of groundwater levels, stream stage, and stream discharge and locations of start-of-flow are illustrated in basin-wide maps of water-table altitude, depth to the water table, and stream base flow during the period. Water-level data collected along 15 hydrologic transects that span the range of environments from uplands through wetlands to surface water were used to determine hydraulic gradients, potential flow directions, and areas of recharge and discharge. These data provide information about the localized interactions of groundwater with wetlands and surface water. Wetlands were categorized with r","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/sir20115056","usgsCitation":"Walker, R.L., Nicholson, R.S., and Storck, D.A., 2011, Hydrologic assessment of three drainage basins in the Pinelands of southern New Jersey, 2004-06: U.S. Geological Survey Scientific Investigations Report 2011-5056, viii, 101 p.; Tables, https://doi.org/10.3133/sir20115056.","productDescription":"viii, 101 p.; Tables","startPage":"i","endPage":"145","numberOfPages":"153","onlineOnly":"N","additionalOnlineFiles":"N","temporalStart":"2004-01-01","temporalEnd":"2006-12-31","costCenters":[{"id":470,"text":"New Jersey Water Science Center","active":true,"usgs":true}],"links":[{"id":204040,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":22680,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2011/5056/","linkFileType":{"id":5,"text":"html"}},{"id":204788,"rank":9999,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1007/BF00186338"}],"scale":"24000","projection":"Universal Transverse Mercator projection","datum":"NAD83","country":"United States","state":"New Jersey","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -75.05,39.45 ], [ -75.05,40 ], [ -74.33333333333333,40 ], [ -74.33333333333333,39.45 ], [ -75.05,39.45 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a29e4b07f02db611781","contributors":{"authors":[{"text":"Walker, Richard L.","contributorId":38961,"corporation":false,"usgs":true,"family":"Walker","given":"Richard","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":351391,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Nicholson, Robert S. rnichol@usgs.gov","contributorId":2283,"corporation":false,"usgs":true,"family":"Nicholson","given":"Robert","email":"rnichol@usgs.gov","middleInitial":"S.","affiliations":[{"id":470,"text":"New Jersey Water Science Center","active":true,"usgs":true}],"preferred":true,"id":351389,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Storck, Donald A. dstorck@usgs.gov","contributorId":4311,"corporation":false,"usgs":true,"family":"Storck","given":"Donald","email":"dstorck@usgs.gov","middleInitial":"A.","affiliations":[],"preferred":true,"id":351390,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70004842,"text":"pp1776C - 2011 - Depositional setting and geochemistry of phosphorites and metalliferous black shales in the Carboniferous-Permian Lisburne Group, Northern Alaska","interactions":[{"subject":{"id":70004842,"text":"pp1776C - 2011 - Depositional setting and geochemistry of phosphorites and metalliferous black shales in the Carboniferous-Permian Lisburne Group, Northern Alaska","indexId":"pp1776C","publicationYear":"2011","noYear":false,"chapter":"C","title":"Depositional setting and geochemistry of phosphorites and metalliferous black shales in the Carboniferous-Permian Lisburne Group, Northern Alaska"},"predicate":"IS_PART_OF","object":{"id":98607,"text":"pp1776 - 2010 - Studies by the U.S. Geological Survey in Alaska, 2008-2009","indexId":"pp1776","publicationYear":"2010","noYear":false,"title":"Studies by the U.S. Geological Survey in Alaska, 2008-2009"},"id":1}],"isPartOf":{"id":98607,"text":"pp1776 - 2010 - Studies by the U.S. Geological Survey in Alaska, 2008-2009","indexId":"pp1776","publicationYear":"2010","noYear":false,"title":"Studies by the U.S. Geological Survey in Alaska, 2008-2009"},"lastModifiedDate":"2022-10-24T13:32:32.274016","indexId":"pp1776C","displayToPublicDate":"2011-07-12T00:00:00","publicationYear":"2011","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":"1776","chapter":"C","title":"Depositional setting and geochemistry of phosphorites and metalliferous black shales in the Carboniferous-Permian Lisburne Group, Northern Alaska","docAbstract":"Phosphatic rocks are distributed widely in the Lisburne Group, a mainly Carboniferous carbonate succession that occurs throughout northern Alaska. New sedimentologic, paleontologic, and geochemical data presented here constrain the geographic and stratigraphic extent of these strata and their depositional and paleogeographic settings. Our findings support models that propose very high oxygen contents of the Permo-Carboniferous atmosphere and oceans, and those that suggest enhanced phosphogenesis in iron-limited sediments; our data also have implications for Carboniferous paleogeography of the Arctic. \n\nLisburne Group phosphorites range from granular to nodular, are interbedded with black shale and lime mudstone rich in radiolarians and sponge spicules, and accumulated primarily in suboxic outer- to middle-ramp environments. Age constraints from conodonts, foraminifers, and goniatite cephalopods indicate that most are middle Late Mississippian (early Chesterian; early late Visean). Phosphorites form 2- to 40-cm-thick beds of sand- to pebble-sized phosphatic peloids, coated grains, and (or) bioclasts cemented by carbonate, silica, or phosphate that occur through an interval =12 m thick. High gamma-ray response through this interval suggests strongly condensed facies related to sediment starvation and development of phosphatic hardgrounds. Phosphorite textures, such as unconformity-bounded coated grains, record multiple episodes of phosphogenesis and sedimentary reworking. Sharp bed bases and local grading indicate considerable redeposition of phosphatic material into deeper water by storms and (or) gravity flows. \n\nLisburne Group phosphorites contain up to 37 weight percent P2O5, 7.6 weight percent F, 1,030 ppm Y, 517 ppm La, and 166 ppm U. Shale-normalized rare earth element (REE) plots show uniformly large negative Ce anomalies Ce/Ce*=0.11 + or - 0.03) that are interpreted to reflect phosphate deposition in seawater that was greatly depleted in Ce due to increased oxygenation of the atmosphere and oceans during the Carboniferous evolution of large vascular land plants. \n\nBlack shales within the phosphorite sections have up to 20.2 weight percent Corg and are potential petroleum source rocks. Locally, these strata also are metalliferous, with up to 1,690 ppm Cr, 2,831 ppm V, 551 ppm Ni, 4,670 ppm Zn, 312 ppm Cu, 43.5 ppm Ag, and 12.3 ppm Tl; concentrations of these metals covary broadly with Corg, suggesting coupled redox variations. Calculated marine fractions (MF) of Cr, V, and Mo, used to evaluate the paleoredox state of the bottom waters, show generally high CrMF/MoMF and VMF/MoMF ratios that indicate deposition of the black shales under suboxic denitrifying conditions; Re/Mo ratios also plot mainly within the suboxic field and support this interpretation. Predominantly seawater and biogenic sources are indicated for Cr, V, Mo, Zn, Cd, Ni, and Cu in the black shales, with an additional hydrothermal contribution inferred for Zn, Cd, Ag, and Tl in some samples. \n\nLisburne Group phosphorites formed in the Ikpikpuk Basin and along both sides of the mud- and chert-rich Kuna Basin, which hosts giant massive sulfide and barite deposits of the Red Dog district. Lisburne Group phosphatic strata are coeval with these deposits and formed in response to a nutrient-rich upwelling regime. Phosphate deposition occurred mainly in suboxic bottom waters based on data for paleoredox proxies (Cr, V, Mo, Re) within contemporaneous black shales. Recent global reconstructions are consistent with Carboniferous upwelling in northern Alaska, but differ in the type of upwelling expected (zonal versus meridional). Paleoenvironmental data suggest that meridional upwelling may better explain phosphorite deposition in the Lisburne Group.","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Studies by the U.S. Geological Survey in Alaska, 2008-2009","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/pp1776C","usgsCitation":"Dumoulin, J.A., Slack, J.F., Whalen, M.T., and Harris, A.G., 2011, Depositional setting and geochemistry of phosphorites and metalliferous black shales in the Carboniferous-Permian Lisburne Group, Northern Alaska: U.S. Geological Survey Professional Paper 1776, iv, 53p., https://doi.org/10.3133/pp1776C.","productDescription":"iv, 53p.","onlineOnly":"Y","ipdsId":"IP-016706","costCenters":[{"id":114,"text":"Alaska Science Center","active":true,"usgs":true},{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"links":[{"id":116126,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/pp_1776_C.gif"},{"id":24365,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pp/1776/c/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Alaska","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -165,68 ], [ -165,69 ], [ -150,69 ], [ -150,68 ], [ -165,68 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ab1e4b07f02db66e7ce","contributors":{"authors":[{"text":"Dumoulin, Julie A. 0000-0003-1754-1287 dumoulin@usgs.gov","orcid":"https://orcid.org/0000-0003-1754-1287","contributorId":203209,"corporation":false,"usgs":true,"family":"Dumoulin","given":"Julie","email":"dumoulin@usgs.gov","middleInitial":"A.","affiliations":[{"id":119,"text":"Alaska Science Center Geology Minerals","active":true,"usgs":true},{"id":114,"text":"Alaska Science Center","active":true,"usgs":true}],"preferred":true,"id":351455,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Slack, John F. 0000-0001-6600-3130 jfslack@usgs.gov","orcid":"https://orcid.org/0000-0001-6600-3130","contributorId":1032,"corporation":false,"usgs":true,"family":"Slack","given":"John","email":"jfslack@usgs.gov","middleInitial":"F.","affiliations":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true},{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true},{"id":387,"text":"Mineral Resources Program","active":true,"usgs":true}],"preferred":true,"id":351456,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Whalen, Michael T.","contributorId":31852,"corporation":false,"usgs":true,"family":"Whalen","given":"Michael","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":351457,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Harris, Anita G.","contributorId":50162,"corporation":false,"usgs":true,"family":"Harris","given":"Anita","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":351458,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70004798,"text":"sir20115072 - 2011 - Potential effects of roadside dry wells on groundwater quality on the Island of Hawai'i — Assessment using numerical groundwater models","interactions":[],"lastModifiedDate":"2022-01-14T14:15:44.087007","indexId":"sir20115072","displayToPublicDate":"2011-07-12T00:00:00","publicationYear":"2011","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":"2011-5072","title":"Potential effects of roadside dry wells on groundwater quality on the Island of Hawai'i — Assessment using numerical groundwater models","docAbstract":"Widespread use of dry wells to dispose of roadside runoff has raised concern about the potential effects on the quality of groundwater on the Island of Hawai‘i. This study used semi-generic numerical models of groundwater flow and contaminant transport to assess the potential effect of dry wells on groundwater quality on the Island of Hawai‘i. The semi-generic models are generalized numerical groundwater-flow and solute-transport models that have a range of aquifer properties and regional groundwater gradients that are characteristic for the island. Several semi-generic models were created to study the effect of dry wells in different hydrogeologic conditions, such as different unsaturated-zone thicknesses or different aquifer characteristics. Results indicate that mixing of contaminated water from the surface with contaminant-free water in the saturated aquifer immediately reduces the contaminant concentration. The amount the concentration is reduced depends on the hydraulic properties of the aquifer in a given area, the thickness of the unsaturated zone, and whether the infiltration is focused in a small area of a dry well or spread naturally over a larger area. Model simulations indicate that focusing infiltration of contaminated runoff through a dry well can substantially increase contaminant concentrations in the underlying saturated aquifer relative to infiltration under natural conditions. Simulated concentrations directly beneath a dry well were nearly 8 times higher than the simulated concentrations directly beneath a broad infiltration area representing the natural condition. Where dry wells are present, contaminant concentrations in the underlying saturated aquifer are lower when the unsaturated zone is thicker and higher when the unsaturated zone is thinner. Contaminant concentrations decline quickly as the contaminant plume migrates, with the regional groundwater flow, away from the dry well. The differences among concentrations resulting from the various unsaturated-zone thicknesses also diminish with distance from the dry well. At a horizontal distance of about 700 ft downgradient from the dry well, all simulated maximum concentrations were less than 1 percent of the concentration in the infiltration water; at about 0.5 mi downgradient from the dry well, all simulated concentrations were equal to or less than 0.1 percent. Actual concentrations may be even lower than indicated by the models because of processes such as decay and reaction that were not simulated. Hydrologic and geologic differences from one location to the next also affect contaminant concentrations—simulations using models with properties representative of aquifers in the Hilo area resulted in lower overall concentrations than models with properties representative of aquifers in the Kona area. Results from this study can be used to assess how contaminants entering a dry well may affect receiving waters in a variety of situations on the Island of Hawai‘i. Better assessment would be obtained by using results from models having the most similar conditions (such as climate, hydraulic properties, regional groundwater gradient) to the dry well in question. The results of this study can help determine which dry wells are likely to have the greatest effect on nearby receiving waters and where more specific data and analyses may be needed.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/sir20115072","usgsCitation":"Izuka, S.K., 2011, Potential effects of roadside dry wells on groundwater quality on the Island of Hawai'i — Assessment using numerical groundwater models: U.S. Geological Survey Scientific Investigations Report 2011-5072, vi, 30 p., https://doi.org/10.3133/sir20115072.","productDescription":"vi, 30 p.","onlineOnly":"Y","additionalOnlineFiles":"N","costCenters":[{"id":525,"text":"Pacific Islands Water Science Center","active":true,"usgs":true}],"links":[{"id":116735,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2011_5072.gif"},{"id":24369,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2011/5072/","linkFileType":{"id":5,"text":"html"}},{"id":394340,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_95298.htm"}],"country":"United States","state":"Hawaii","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -156.2255859375,\n 18.8335153964335\n ],\n [\n -154.76440429687497,\n 18.8335153964335\n ],\n [\n -154.76440429687497,\n 20.58136735381002\n ],\n [\n -156.2255859375,\n 20.58136735381002\n ],\n [\n -156.2255859375,\n 18.8335153964335\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac8e4b07f02db67c0f6","contributors":{"authors":[{"text":"Izuka, Scot K. 0000-0002-8758-9414 skizuka@usgs.gov","orcid":"https://orcid.org/0000-0002-8758-9414","contributorId":2645,"corporation":false,"usgs":true,"family":"Izuka","given":"Scot","email":"skizuka@usgs.gov","middleInitial":"K.","affiliations":[{"id":525,"text":"Pacific Islands Water Science Center","active":true,"usgs":true}],"preferred":true,"id":351356,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70004702,"text":"sir20115091 - 2011 - Estimation of annual suspended-sediment fluxes, 1931-95, and evaluation of geomorphic changes, 1950-2010, in the Arkansas River near Tulsa, Oklahoma","interactions":[],"lastModifiedDate":"2012-03-08T17:16:41","indexId":"sir20115091","displayToPublicDate":"2011-06-22T13:50:04","publicationYear":"2011","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":"2011-5091","title":"Estimation of annual suspended-sediment fluxes, 1931-95, and evaluation of geomorphic changes, 1950-2010, in the Arkansas River near Tulsa, Oklahoma","docAbstract":"An understanding of fluvial sediment transport and changing channel morphology can assist planners in making responsible decisions with future riverine development or restoration projects. Sediment rating curves can serve as simple models and can provide predictive tools to estimate annual sediment fluxes. Sediment flux models can aid in the design of river projects by providing insight to past and potential future sediment fluxes. Historical U.S. Geological Survey suspended-sediment and discharge data were evaluated to estimate annual suspended-sediment fluxes for two stations on the Arkansas River located downstream from Keystone Dam in Tulsa County. Annual suspended-sediment fluxes were estimated from 1931-95 for the Arkansas River at Tulsa streamflow-gaging station (07164500) and from 1973-82 for the Arkansas River near Haskell streamflow-gaging station (07165570). The annual flow-weighted suspended-sediment concentration decreased from 1,970 milligrams per liter to 350 milligrams per liter after the completion of Keystone Dam at the Tulsa station. The streambed elevation at the Arkansas River at Tulsa station has changed less than 1 foot from 1970 to 2005, but the thalweg has shifted from a location near the right bank to a position near the left bank. There was little change in the position of most of the banks of the Arkansas River channel from 1950 to 2009. The most substantial change evident from visual inspection of aerial photographs was an apparent decrease in sediment storage in the form of mid-channel and meander bars. The Arkansas River channel between Keystone Dam and the Tulsa-Wagoner County line showed a narrowing and lengthening (increase in sinuosity) over the transition period 1950-77 followed by a steady widening and shortening of the river channel (decrease in sinuosity) during the post-dam (Keystone) periods 1977-85, 1985-2003, and 2003-10.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/sir20115091","collaboration":"Prepared in cooperation with Tulsa County","usgsCitation":"Lewis, J.M., Smith, S.J., Buck, S.D., and Strong, S.A., 2011, Estimation of annual suspended-sediment fluxes, 1931-95, and evaluation of geomorphic changes, 1950-2010, in the Arkansas River near Tulsa, Oklahoma: U.S. Geological Survey Scientific Investigations Report 2011-5091, v, 21 p., https://doi.org/10.3133/sir20115091.","productDescription":"v, 21 p.","additionalOnlineFiles":"N","costCenters":[{"id":516,"text":"Oklahoma Water Science Center","active":true,"usgs":true}],"links":[{"id":116650,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2011_5091.png"},{"id":21919,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2011/5091/","linkFileType":{"id":5,"text":"html"}}],"geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -96.55,35.583333333333336 ], [ -96.55,36.333333333333336 ], [ -95.16666666666667,36.333333333333336 ], [ -95.16666666666667,35.583333333333336 ], [ -96.55,35.583333333333336 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a5ee4b07f02db633d86","contributors":{"authors":[{"text":"Lewis, Jason M. 0000-0001-5337-1890 jmlewis@usgs.gov","orcid":"https://orcid.org/0000-0001-5337-1890","contributorId":3854,"corporation":false,"usgs":true,"family":"Lewis","given":"Jason","email":"jmlewis@usgs.gov","middleInitial":"M.","affiliations":[{"id":516,"text":"Oklahoma Water Science Center","active":true,"usgs":true}],"preferred":true,"id":351197,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Smith, S. Jerrod 0000-0002-9379-8167 sjsmith@usgs.gov","orcid":"https://orcid.org/0000-0002-9379-8167","contributorId":981,"corporation":false,"usgs":true,"family":"Smith","given":"S.","email":"sjsmith@usgs.gov","middleInitial":"Jerrod","affiliations":[{"id":516,"text":"Oklahoma Water Science Center","active":true,"usgs":true}],"preferred":true,"id":351196,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Buck, Stephanie D. sbuck@usgs.gov","contributorId":4622,"corporation":false,"usgs":true,"family":"Buck","given":"Stephanie","email":"sbuck@usgs.gov","middleInitial":"D.","affiliations":[],"preferred":true,"id":351198,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Strong, Scott A. sstrong@usgs.gov","contributorId":4623,"corporation":false,"usgs":true,"family":"Strong","given":"Scott","email":"sstrong@usgs.gov","middleInitial":"A.","affiliations":[],"preferred":true,"id":351199,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70004686,"text":"ofr20111122 - 2011 - Review of samples of water, sediment, tailings, and biota at the Little Bonanza mercury mine, San Luis Obispo County, California","interactions":[],"lastModifiedDate":"2019-07-19T08:36:24","indexId":"ofr20111122","displayToPublicDate":"2011-06-21T10:50:02","publicationYear":"2011","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":"2011-1122","title":"Review of samples of water, sediment, tailings, and biota at the Little Bonanza mercury mine, San Luis Obispo County, California","docAbstract":"Background and Objectives\n\nThe Little Bonanza mercury (Hg) mine, located in San Luis Obispo County, California, is a relatively small mine with, a historical total Hg production of about 1,000 flasks. The mine workings and tailings are located in the headwaters of the previously unnamed west fork of Las Tablas Creek (WF Las Tablas Creek), which flows into the Nacimiento Reservoir. Wasterock and tailings eroded from the Little Bonanza Hg Mine have contributed Hg-enriched mine wastes to the headwaters of WF Las Tablas Creek. The mine is located on Federal land managed by the U.S. Bureau of Land Management (BLM), which requested that the U.S. Geological Survey (USGS) measure and characterize Hg and other geochemical constituents in tailings, sediment, water, and biota at and downstream from the minesite. This report is in response that request, from the lead agency which is mandated to conduct a Comprehensive Environmental Response, Compensation, and Liability Act (CERCLA) - Removal Site Investigation (RSI). The RSI applies to removal of Hg-contaminated mine waste from the Little Bonanza minesite as a means of reducing Hg transport to WF Las Tablas Creek.\n\nThis report summarizes data obtained from field sampling of mine tailings, wasterock, sediment, water, and biota at the Little Bonanza Mine that was completed on April 6, 2010. Conditions during sampling were dry and no rain had occurred in the watershed for several weeks. Our results permit a preliminary assessment of the mining sources of Hg and associated chemical constituents that could produce elevated levels of monomethyl mercury (MMeHg) in WF Las Tablas Creek and in biota.\nHistory and Geology\n\nThe history of the Little Bonanza Hg mine is summarized here from Yates (1943) and other references as cited. The Little Bonanza Mine, located 20 mi west of Paso Robles, was discovered in 1862. Although production was minor until 1900, from 1900 to 1906, the mine produced about 1,000 flasks of Hg. Intermittent production continued into the 1940s but was relatively limited. Underground workings, now caved and inaccessible, include about 3,000 ft of drifts, crosscuts, and raises on three levels extending 260 ft downward.\n\nThe workings at the Little Bonanza Mine explore a zone of fault breccia, which trends northwest. The breccia is composed of fragments of sandstone, greenstone, serpentine, and chert in a shale matrix. The serpentine has been hydrothermally altered to silica-carbonate rock, and the Hg deposit is hosted within the zone of alteration. The veins are discontinuous and irregular, but form a steplike pattern along the fault zone. The principal mineralization occurring in the veins is irregular, consisting of disseminated zones of cinnabar. Most of the veins in the mine area contain cinnabar.\nSample Sites and Methods\n\nSamples were collected to assess the concentrations of Hg and biogeochemically relevant constituents in tailings and wasterock piles at the Little Bonanza Hg mine. Tailings are present adjacent to a three-pipe retort used to process the Hg ore. The tailings occur in the upper 15 cm of the soil adjacent to the retort and slag from the retort is present on the surface. An area of disturbed soil and rock uphill from the retort was likely formed during construction of a dam that provided water for mining activities. Wasterock in these piles was sampled. The largest amount of tailings is exposed to the west of the retort in the bank of WF Las Tablas Creek. Water, sediment, and biota were sampled from WF Las Tablas Creek, which flows through the mine area. Sample-site locations are shown in figures 10 and 11 and listed in table 1. Samples were collected when streamflow was low and no precipitation had occurred.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr20111122","usgsCitation":"Rytuba, J.J., Hothem, R.L., Goldstein, D., Brussee, B.E., and May, J., 2011, Review of samples of water, sediment, tailings, and biota at the Little Bonanza mercury mine, San Luis Obispo County, California: U.S. Geological Survey Open-File Report 2011-1122, vii, 11 p., https://doi.org/10.3133/ofr20111122.","productDescription":"vii, 11 p.","startPage":"i","endPage":"46","numberOfPages":"53","onlineOnly":"Y","additionalOnlineFiles":"N","costCenters":[{"id":266,"text":"Environmental Resources Science Center","active":false,"usgs":true},{"id":34983,"text":"Contaminant Biology Program","active":true,"usgs":true}],"links":[{"id":116215,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr_2011_1122.gif"},{"id":21913,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2011/1122/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"California","county":"San Luis Obispo","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -121,35.3 ], [ -121,35.6 ], [ -120.5,35.6 ], [ -120.5,35.3 ], [ -121,35.3 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4abde4b07f02db673ec4","contributors":{"authors":[{"text":"Rytuba, James J. jrytuba@usgs.gov","contributorId":3043,"corporation":false,"usgs":true,"family":"Rytuba","given":"James","email":"jrytuba@usgs.gov","middleInitial":"J.","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":351141,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hothem, Roger L. roger_hothem@usgs.gov","contributorId":1721,"corporation":false,"usgs":true,"family":"Hothem","given":"Roger","email":"roger_hothem@usgs.gov","middleInitial":"L.","affiliations":[{"id":651,"text":"Western Ecological Research Center","active":true,"usgs":true}],"preferred":true,"id":351140,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Goldstein, Daniel N.","contributorId":87671,"corporation":false,"usgs":true,"family":"Goldstein","given":"Daniel N.","affiliations":[],"preferred":false,"id":351144,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Brussee, Brianne E. 0000-0002-2452-7101 bbrussee@usgs.gov","orcid":"https://orcid.org/0000-0002-2452-7101","contributorId":4249,"corporation":false,"usgs":true,"family":"Brussee","given":"Brianne","email":"bbrussee@usgs.gov","middleInitial":"E.","affiliations":[{"id":651,"text":"Western Ecological Research Center","active":true,"usgs":true}],"preferred":true,"id":351142,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"May, Jason T. 0000-0002-5699-2112","orcid":"https://orcid.org/0000-0002-5699-2112","contributorId":14791,"corporation":false,"usgs":true,"family":"May","given":"Jason T.","affiliations":[],"preferred":false,"id":351143,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":70004656,"text":"sir20115070 - 2011 - Effects of experimental passive artificial recharge of treated surface water on water quality in the Equus Beds Aquifer, 2009-2010","interactions":[],"lastModifiedDate":"2012-03-08T17:16:40","indexId":"sir20115070","displayToPublicDate":"2011-06-16T16:50:03","publicationYear":"2011","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":"2011-5070","title":"Effects of experimental passive artificial recharge of treated surface water on water quality in the Equus Beds Aquifer, 2009-2010","docAbstract":"Declining water levels and concerns about the migration of a known saltwater plume upgradient from public supply wells prompted the City of Wichita to investigate the feasibility of using artificial recharge to replenish the water supply in the Equus Beds aquifer. After preliminary testing, the City of Wichita began Phase I of the Equus Beds Aquifer Storage and Recovery Project in 2006. In 2009, the City of Wichita installed an experimental passive gravity recharge well and trench system to increase artificial recharge at Recharge Basin 1, one of the six Phase ? recharge sites.\nThe U.S. Geological Survey collected water samples from 13 sites and maintained 8 continuous monitors to test the recharge capacity of the experimental passive recharge system, the effect of the recharge on geochemistry of the aquifer, and the fate of bacteria and viruses present in the recharge water. About 576,000 gallons of treated surface water from the Little Arkansas River were recharged through the passive recharge well and trench system into the Equus Beds aquifer during April 2009. In May 2009, U.S. Geological Survey tests detected that bacterial and viral indicators (total coliform, fecal coliform, Escherichia coli, coliphage virus, and Clostridium perfringens) were entering the Recharge Basin 1 wells through the recharge system and recharge was discontinued. The City of Wichita disconnected the trench collection system from the passive gravity recharge well in July 2009, and in July and August 2009 withdrew 1,825,000 gallons of water from the aquifer at Recharge Basin 1 to remove the recharged water and avoid contamination of the aquifer.\nThe original recharge rate in Recharge Basin 1 was about 10.8 gallons per day per square foot. After installation of the passive recharge system, recharge water entered the aquifer through the passive well at a rate of about 19.2 gallons per day per square foot, a per unit area increase of about 78 percent.\nDuring artificial recharge, continuous monitors recorded rising water-level altitudes in the passive gravity recharge well and nearby monitoring wells as water flowed at about 10 feet per day from the passive recharge well toward nearby downgradient monitoring wells. The increase in water level in this area would have the effect of temporarily slowing the eastward migration of saltwater from the nearby Burrton plume.\nBacterial and viral indicators were detected in water samples from Recharge Basin 1 sites before and immediately after the installation of the passive gravity recharge well and trench system, during artificial recharge, and after artificial recharge. After water withdrawal in August 2009 and through the end of data collection in March 2010, detections of bacterial and viral indicators in groundwater decreased to densities similar to those before installation of the passive recharge system.\nConcentrations of chloride in samples collected from the trench, passive gravity recharge well, and nearby monitoring wells increased from an average of 34 milligrams per liter before artificial recharge to an average of 64 milligrams per liter during artificial recharge, reflecting the addition of recharge water with measured chloride concentrations of 62 to 94 milligrams per liter. When water was being pumped out of the aquifer through the passive gravity recharge well, chloride concentrations increased to 94 milligrams per liter in the removed water and increased to 150 milligrams per liter in the deep monitoring well nearest the passive gravity recharge well, indicating that, as water was being pumped from the passive well, water with a large chloride concentration from elsewhere in the aquifer was flowing toward the passive well. Chloride concentrations did not exceed the U.S. Environmental Protection Agency Secondary Drinking Water Regulation of 250 milligrams per liter in any Recharge Basin 1 samples collected as part of the study.\nIron concentrations exceeded the U.S. Environmental Protection Agency","doi":"10.3133/sir20115070","collaboration":"Prepared in cooperation with the City of Wichita, Kansas as part of the Equus Beds Groundwater Recharge Project","usgsCitation":"Garinger, L.P., King, A.S., and Ziegler, A., 2011, Effects of experimental passive artificial recharge of treated surface water on water quality in the Equus Beds Aquifer, 2009-2010: U.S. Geological Survey Scientific Investigations Report 2011-5070, ix, 106 p., https://doi.org/10.3133/sir20115070.","productDescription":"ix, 106 p.","additionalOnlineFiles":"N","temporalStart":"2008-10-01","temporalEnd":"2010-09-30","costCenters":[{"id":353,"text":"Kansas Water Science Center","active":false,"usgs":true}],"links":[{"id":116091,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2011_5070.jpg"},{"id":21890,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2011/5070/","linkFileType":{"id":5,"text":"html"}}],"scale":"100000","projection":"Universal Transverse Mercator","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -98,37.666666666666664 ], [ -98,38.36666666666667 ], [ -97.3,38.36666666666667 ], [ -97.3,37.666666666666664 ], [ -98,37.666666666666664 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a2ee4b07f02db61596b","contributors":{"authors":[{"text":"Garinger, Linda Pickett","contributorId":92406,"corporation":false,"usgs":true,"family":"Garinger","given":"Linda","email":"","middleInitial":"Pickett","affiliations":[],"preferred":false,"id":351001,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"King, Aaron S.","contributorId":25277,"corporation":false,"usgs":true,"family":"King","given":"Aaron","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":351000,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Ziegler, Andrew C. aziegler@usgs.gov","contributorId":433,"corporation":false,"usgs":true,"family":"Ziegler","given":"Andrew C.","email":"aziegler@usgs.gov","affiliations":[{"id":353,"text":"Kansas Water Science Center","active":false,"usgs":true}],"preferred":false,"id":350999,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70004615,"text":"ofr20111128 - 2011 - Simulation of groundwater flow in a volatile organic compound-contaminated area near Bethpage, Nassau County, New York: A discussion of modeling considerations","interactions":[],"lastModifiedDate":"2022-12-05T22:43:28.232201","indexId":"ofr20111128","displayToPublicDate":"2011-06-13T10:50:04","publicationYear":"2011","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":"2011-1128","title":"Simulation of groundwater flow in a volatile organic compound-contaminated area near Bethpage, Nassau County, New York: A discussion of modeling considerations","docAbstract":"The 2010 Bethpage groundwater-flow model (ARCADIS, 2010) was based on a steady state assumption. Although it is widely acknowledged that significant water-level changes have occurred in the past, the reviewed model does not represent changing water levels. The steady state approach limits the effectiveness of the following:\n\n1. identification of sources of contamination,\n\n2. analysis of model accuracy,\n\n3. model calibration, and\n\n4. simulations of future scenarios.\n\nFuture plume movement was simulated in an incomplete manner through an unchanging groundwater-flow field. Available time-series information on temporal variation of factors affecting groundwater-flow dynamics includes:\n\n1. public-supply pumping,\n\n2. groundwater discharges from systems remediating volatile organic compound (VOC) plumes,\n\n3. recharge and precipitation rates, and\n\n4. water levels and streamflows.\n\nTransient phenomena that might be useful in future hypothetical simulations include pumping variations, redirection of containment-system waters for industrial use, and climate-change scenarios. Public-domain computer programs, U.S. Geological Survey guidance reports on transient-state calibration and uncertainty methods (Doherty and Hunt, 2010), and additional local and regional datasets are available to provide additional confidence in model evaluations and allow better evaluation of their limitations.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr20111128","usgsCitation":"Misut, P.E., 2011, Simulation of groundwater flow in a volatile organic compound-contaminated area near Bethpage, Nassau County, New York: A discussion of modeling considerations: U.S. Geological Survey Open-File Report 2011-1128, vi, 19 p., https://doi.org/10.3133/ofr20111128.","productDescription":"vi, 19 p.","numberOfPages":"23","costCenters":[{"id":474,"text":"New York Water Science Center","active":true,"usgs":true}],"links":[{"id":410083,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_95236.htm","linkFileType":{"id":5,"text":"html"}},{"id":21868,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2011/1128/","linkFileType":{"id":5,"text":"html"}},{"id":116203,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr_2011_1128.gif"}],"scale":"24000","projection":"Universal Transverse Mercator projection","country":"United States","state":"New York","county":"Nassau County","city":"Bethpage","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -73.5308,\n 40.6769\n ],\n [\n -73.5308,\n 40.7728\n ],\n [\n -73.42,\n 40.7728\n ],\n [\n -73.42,\n 40.6769\n ],\n [\n -73.5308,\n 40.6769\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4abce4b07f02db67380d","contributors":{"authors":[{"text":"Misut, Paul E. 0000-0002-6502-5255 pemisut@usgs.gov","orcid":"https://orcid.org/0000-0002-6502-5255","contributorId":1073,"corporation":false,"usgs":true,"family":"Misut","given":"Paul","email":"pemisut@usgs.gov","middleInitial":"E.","affiliations":[{"id":474,"text":"New York Water Science Center","active":true,"usgs":true}],"preferred":true,"id":350864,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70004595,"text":"sir20115065 - 2011 - Hydrogeology and water quality of the Floridan aquifer system and effects of Lower Floridan aquifer pumping on the Upper Floridan aquifer at Fort Stewart, Georgia","interactions":[],"lastModifiedDate":"2017-01-17T11:00:28","indexId":"sir20115065","displayToPublicDate":"2011-06-09T16:50:08","publicationYear":"2011","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":"2011-5065","title":"Hydrogeology and water quality of the Floridan aquifer system and effects of Lower Floridan aquifer pumping on the Upper Floridan aquifer at Fort Stewart, Georgia","docAbstract":"Test drilling, field investigations, and digital modeling were completed at Fort Stewart, GA, during 2009?2010, to assess the geologic, hydraulic, and water-quality characteristics of the Floridan aquifer system and evaluate the effect of Lower Floridan aquifer (LFA) pumping on the Upper Floridan aquifer (UFA). This work was performed pursuant to the Georgia Environmental Protection Division interim permitting strategy for new wells completed in the LFA that requires simulation to (1) quantify pumping-induced aquifer leakage from the UFA to LFA, and (2) identify the equivalent rate of UFA pumping that would produce the same maximum drawdown in the UFA that anticipated pumping from LFA well would induce. Field investigation activities included (1) constructing a 1,300-foot (ft) test boring and well completed in the LFA (well 33P028), (2) constructing an observation well in the UFA (well 33P029), (3) collecting drill cuttings and borehole geophysical logs, (4) collecting core samples for analysis of vertical hydraulic conductivity and porosity, (5) conducting flowmeter and packer tests in the open borehole within the UFA and LFA, (6) collecting depth-integrated water samples to assess basic ionic chemistry of various water-bearing zones, and (7) conducting aquifer tests in new LFA and UFA wells to determine hydraulic properties and assess interaquifer leakage. Using data collected at the site and in nearby areas, model simulation was used to assess the effects of LFA pumping on the UFA. Borehole-geophysical and flowmeter data indicate the LFA at Fort Stewart consists of limestone and dolomitic limestone between depths of 912 and 1,250 ft. Flowmeter data indicate the presence of three permeable zones at depth intervals of 912-947, 1,090-1,139, and 1,211?1,250 ft. LFA well 33P028 received 50 percent of the pumped volume from the uppermost permeable zone, and about 18 and 32 percent of the pumped volume from the middle and lowest permeable zones, respectively. Chemical constituent concentrations increased with depth, and water from all permeable zones contained sulfate at concentrations that exceeded the U.S. Environmental Protection Agency secondary maximum contaminant level of 250 milligrams per liter. A 72-hour aquifer test pumped LFA well 33P028 at 740 gallons per minute (gal/min), producing about 39 ft of drawdown in the pumped well and about 0.4 foot in nearby UFA well 33P029. Simulation using the U.S. Geological Survey finite-difference code MODFLOW was used to determine long-term, steady-state flow in the Floridan aquifer system, assuming the LFA well was pumped continuously at a rate of 740 gal/min. Simulated steady-state drawdown in the LFA was identical to that observed in pumped LFA well 33P028 at the end of the 72-hour test, with values larger than 1 ft extending 4.4 square miles symmetrically around the pumped well. Simulated steady-state drawdown in the UFA resulting from pumping in LFA well 33P028 exceeded 1 ft within a 1.4-square-mile circular area, and maximum drawdown in the UFA was 1.1 ft. Leakage from the UFA through the Lower Floridan confining unit contributed about 98 percent of the water to the well; lateral flow from specified-head model boundaries contributed about 2 percent. About 80 percent of the water supplied to LFA well 33P028 originated from within 1 mile of the well, and 49 percent was derived from within 0.5 mile of the well. Vertical hydraulic gradients and vertical leakage are progressively higher near the LFA pumped well which results in a correspondingly higher contribution of water from the UFA to the pumped well at distances closer to the pumped well. Simulated pumping-induced interaquifer leakage from the UFA to the LFA totaled 725 gal/min (1.04 million gallons per day), whereas simulated pumping at 205 gal/min (0.3 million gallons per day) from UFA well 33P029 produced the equivalent maximum drawdown as pumping LFA well 33P028 at 740 gal/min during the aquifer test. This equivalent pumpin","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/sir20115065","collaboration":"Prepared in cooperation with the U.S. Department of the Army","usgsCitation":"Clarke, J.S., Cherry, G.C., and Gonthier, G., 2011, Hydrogeology and water quality of the Floridan aquifer system and effects of Lower Floridan aquifer pumping on the Upper Floridan aquifer at Fort Stewart, Georgia: U.S. Geological Survey Scientific Investigations Report 2011-5065, viii, 60 p., https://doi.org/10.3133/sir20115065.","productDescription":"viii, 60 p.","additionalOnlineFiles":"N","costCenters":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true}],"links":[{"id":116681,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2011_5065.jpg"},{"id":21861,"rank":200,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/sir/2011/5065/","linkFileType":{"id":5,"text":"html"}}],"scale":"2000000","country":"United States","state":"Georgia","city":"Fort Stewart","otherGeospatial":"Upper Floridan aquifer","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -81.91666666666667,31.5 ], [ -81.91666666666667,32.25 ], [ -80.75,32.25 ], [ -80.75,31.5 ], [ -81.91666666666667,31.5 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad9e4b07f02db6852c5","contributors":{"authors":[{"text":"Clarke, John S. jsclarke@usgs.gov","contributorId":400,"corporation":false,"usgs":true,"family":"Clarke","given":"John","email":"jsclarke@usgs.gov","middleInitial":"S.","affiliations":[{"id":316,"text":"Georgia Water Science Center","active":true,"usgs":true}],"preferred":true,"id":350814,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Cherry, Gregory C.","contributorId":35038,"corporation":false,"usgs":true,"family":"Cherry","given":"Gregory","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":350816,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Gonthier, Gerard 0000-0003-4078-8579 gonthier@usgs.gov","orcid":"https://orcid.org/0000-0003-4078-8579","contributorId":3141,"corporation":false,"usgs":true,"family":"Gonthier","given":"Gerard ","email":"gonthier@usgs.gov","affiliations":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true}],"preferred":false,"id":350815,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70004590,"text":"ofr20111077 - 2011 - Surface-water, water-quality, and meteorological data for the Cambridge, Massachusetts, drinking-water source area, water years 2007-08","interactions":[],"lastModifiedDate":"2012-03-08T17:16:40","indexId":"ofr20111077","displayToPublicDate":"2011-06-08T16:50:09","publicationYear":"2011","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":"2011-1077","title":"Surface-water, water-quality, and meteorological data for the Cambridge, Massachusetts, drinking-water source area, water years 2007-08","docAbstract":"Records of water quantity, water quality, and meteorological parameters were continuously collected from three reservoirs, two primary streams, and five subbasin tributaries in the Cambridge, Massachusetts, drinking-water source area during water years 2007-08 (October 2006 through September 2008). Water samples were collected during base-flow conditions and storms in the Cambridge Reservoir and Stony Brook Reservoir drainage areas and analyzed for dissolved calcium, sodium, chloride, and sulfate; total nitrogen and phosphorus; and polar pesticides and metabolites. Composite samples of stormwater also were analyzed for concentrations of total petroleum hydrocarbons and suspended sediment in one subbasin in the Stony Brook Reservoir drainage basin. These data were collected to assist watershed administrators in managing the drinking-water source area and to identify potential sources of contaminants and trends in contaminant loading to the water supply.\nMonthly reservoir contents for the Cambridge Reservoir ranged from about 30 to 95 percent of capacity during water years 2007-08. Monthly reservoir contents for the Stony Brook Reservoir ranged from about 47 to 91 percent of capacity during water years 2007-08, while the monthly reservoir storage values for Fresh Pond Reservoir were maintained at greater than 92 percent of capacity. If the average water demand by the city of Cambridge is assumed to be 15 million gallons per day, the volume of water released from the Stony Brook Reservoir to the Charles River during water years 2007-08 represents an annual surplus of about 107 and 94 percent, respectively. The annual precipitation total of about 47 in (inches) recorded at the Cambridge reservoir during water year 2007 was about 5 to 21 percent lower than recorded totals for the previous four water years, whereas the annual precipitation total of about 62 in. during water year 2008 was about 5 to 32 percent higher than recorded totals for water years 2002-07.\nIn general, most monthly mean specific-conductance values for water year 2007 for U.S. Geological Survey (USGS) stations on the two primary streams and four subbasin tributaries in the Cambridge, Massachusetts, drinking-water source area were below the previous median monthly values and often were below the previous minimum monthly values for available data since water year 1997. The annual mean specific-conductance value for Fresh Pond Reservoir during water year 2007 was 483 (u or mu)S/cm (microsiemens per centimeter), which was lower than the prior three water years. The monthly mean specific-conductance values for streamflow for Hobbs Brook below the Cambridge Reservoir for December through July 2008 were greater than the 75th percentile for historical data since water year 1997. These relatively high values were caused by the inflow of high specific conductance water from the tributaries when the reservoir water level was low at the onset of winter. Increased rainfall in the watershed beginning in February 2008 caused monthly mean specific-conductance values for Hobbs Brook to decrease to about 700 (u or mu)S/cm by the end of the water year. Monthly mean specific-conductance values for many of the other USGS stations were higher than historical values for several months during the winter of water year 2008. The large amount of rainfall in the watershed also caused the monthly mean specific conductance at these stations to decline to near-median values or to values within the interquartile range for available historical data. The annual mean specific conductance for Fresh Pond Reservoir during water year 2008 was 497 (u or mu)S/cm, slightly greater than the corresponding value for the prior year.\nWater samples were collected in nearly all of the subbasins in the Cambridge drinking-water source area and from Fresh Pond during the study period. Discrete water samples were collected during base-flow conditions with an antecedent dry period of at least 3 days. Composite sampl","doi":"10.3133/ofr20111077","collaboration":"Prepared in cooperation with the City of Cambridge, Massachusetts, Water Department","usgsCitation":"Smith, K.P., 2011, Surface-water, water-quality, and meteorological data for the Cambridge, Massachusetts, drinking-water source area, water years 2007-08: U.S. Geological Survey Open-File Report 2011-1077, v, 107 p., https://doi.org/10.3133/ofr20111077.","productDescription":"v, 107 p.","additionalOnlineFiles":"N","costCenters":[{"id":376,"text":"Massachusetts Water Science Center","active":true,"usgs":true}],"links":[{"id":116229,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr_2011_1077.gif"},{"id":21860,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2011/1077/","linkFileType":{"id":5,"text":"html"}}],"state":"Massachusetts","city":"Cambridge","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -71.31666666666666,42.333333333333336 ], [ -71.31666666666666,42.43333333333333 ], [ -71.11666666666666,42.43333333333333 ], [ -71.11666666666666,42.333333333333336 ], [ -71.31666666666666,42.333333333333336 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae5e4b07f02db68a4e1","contributors":{"authors":[{"text":"Smith, Kirk P. 0000-0003-0269-474X kpsmith@usgs.gov","orcid":"https://orcid.org/0000-0003-0269-474X","contributorId":1516,"corporation":false,"usgs":true,"family":"Smith","given":"Kirk","email":"kpsmith@usgs.gov","middleInitial":"P.","affiliations":[{"id":466,"text":"New England Water Science Center","active":true,"usgs":true},{"id":376,"text":"Massachusetts Water Science Center","active":true,"usgs":true}],"preferred":true,"id":350810,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70004555,"text":"ofr20111084 - 2011 - Principal facts for gravity stations collected in 2010 from White Pine and Lincoln Counties, east-central Nevada","interactions":[],"lastModifiedDate":"2012-02-10T00:11:58","indexId":"ofr20111084","displayToPublicDate":"2011-06-03T03:01:04","publicationYear":"2011","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":"2011-1084","title":"Principal facts for gravity stations collected in 2010 from White Pine and Lincoln Counties, east-central Nevada","docAbstract":"Increasing demands on the Colorado River system within the arid Southwestern United States have focused attention on finding new, alternative sources of water. Particular attention is being paid to the eastern Great Basin, where important ground-water systems occur within a regionally extensive sequence of Paleozoic carbonate rocks and in the Cenozoic basin-fill deposits that occur throughout the region. Geophysical investigations to characterize the geologic framework of aquifers in eastern Nevada and western Utah began in a series of cooperative agreements between the U.S. Geological Survey and the Southern Nevada Water Authority in 2003. These studies were intended to better understand the formation of basins, define their subsurface shape and depth, and delineate structures that may impede or enhance groundwater flow. We have combined data from gravity stations established during the current study with previously available data to produce an up-to-date isostatic-gravity map of the study area, using a gravity inversion method to calculate depths to pre-Cenozoic basement rock and to estimate alluvial/volcanic fill in the valleys.","doi":"10.3133/ofr20111084","collaboration":"In cooperation with the Southern Nevada Water Authority (SNWA)","usgsCitation":"Mankinen, E.A., and McKee, E.H., 2011, Principal facts for gravity stations collected in 2010 from White Pine and Lincoln Counties, east-central Nevada: U.S. Geological Survey Open-File Report 2011-1084, iv, 15 p.; Figures; Tables; Data, https://doi.org/10.3133/ofr20111084.","productDescription":"iv, 15 p.; Figures; Tables; Data","onlineOnly":"Y","additionalOnlineFiles":"Y","temporalStart":"2010-01-01","temporalEnd":"2010-12-31","costCenters":[{"id":671,"text":"Western Region Geology and Geophysics Science Center","active":false,"usgs":true}],"links":[{"id":116285,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr_2011_1084.gif"},{"id":21842,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2011/1084/","linkFileType":{"id":5,"text":"html"}}],"geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -115.33333333333333,37.333333333333336 ], [ -115.33333333333333,40 ], [ -113.33333333333333,40 ], [ -113.33333333333333,37.333333333333336 ], [ -115.33333333333333,37.333333333333336 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aa8e4b07f02db667877","contributors":{"authors":[{"text":"Mankinen, Edward A. 0000-0001-7496-2681 emank@usgs.gov","orcid":"https://orcid.org/0000-0001-7496-2681","contributorId":1054,"corporation":false,"usgs":true,"family":"Mankinen","given":"Edward","email":"emank@usgs.gov","middleInitial":"A.","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":350712,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"McKee, Edwin H. mckee@usgs.gov","contributorId":3728,"corporation":false,"usgs":true,"family":"McKee","given":"Edwin","email":"mckee@usgs.gov","middleInitial":"H.","affiliations":[],"preferred":true,"id":350713,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":99284,"text":"ofr20111125 - 2011 - Threats of habitat and water-quality degradation to mussel diversity in the Meramec River Basin, Missouri, USA","interactions":[],"lastModifiedDate":"2019-07-09T15:47:36","indexId":"ofr20111125","displayToPublicDate":"2011-05-25T00:00:00","publicationYear":"2011","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":"2011-1125","title":"Threats of habitat and water-quality degradation to mussel diversity in the Meramec River Basin, Missouri, USA","docAbstract":"The Meramec River Basin in east-central Missouri is an important stronghold for native freshwater mussels (Order: Unionoida) in the United States. Whereas the basin supports more than 40 mussel species, previous studies indicate that the abundance and distribution of most species are declining. Therefore, resource managers have identified the need to prioritize threats to native mussel populations in the basin and to design a mussel monitoring program. The objective of this study was to identify threats of habitat and water-quality degradation to mussel diversity in the basin. Affected habitat parameters considered as the main threats to mussel conservation included excess sedimentation, altered stream geomorphology and flow, effects on riparian vegetation and condition, impoundments, and invasive non-native species. Evaluating water-quality parameters for conserving mussels was a main focus of this study. Mussel toxicity data for chemical contaminants were compared to national water quality criteria (NWQC) and Missouri water quality standards (MWQS). However, NWQC and MWQS have not been developed for many chemical contaminants and some MWQS may not be protective of native mussel populations. Toxicity data indicated that mussels are sensitive to ammonia, copper, temperature, certain pesticides, pharmaceuticals, and personal care products; these compounds were identified as the priority water-quality parameters for mussel conservation in the basin. Measures to conserve mussel diversity in the basin include expanding the species and life stages of mussels and the list of chemical contaminants that have been assessed, establishing a long term mussel monitoring program that measures physical and chemical parameters of high priority, conducting landscape scale modeling to predict mussel distributions, determining sublethal effects of primary contaminants of concern, deriving risk-based guidance values for mussel conservation, and assessing the effects of wastewater treatment plants and non-point source pollution on mussels. A critical next step to further prioritize these needs is to conduct a watershed risk assessment using local data (for example, land use, flow) when available.\r\n","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr20111125","collaboration":"A report to the Missouri Department of Conservation","usgsCitation":"Hinck, J.E., Ingersoll, C.G., Wang, N., Augspurger, T., Barnhart, M., McMurray, S., Roberts, A.D., and Schrader, L., 2011, Threats of habitat and water-quality degradation to mussel diversity in the Meramec River Basin, Missouri, USA: U.S. Geological Survey Open-File Report 2011-1125, vi, 18 p., https://doi.org/10.3133/ofr20111125.","productDescription":"vi, 18 p.","additionalOnlineFiles":"N","costCenters":[{"id":192,"text":"Columbia Environmental Research Center","active":true,"usgs":true},{"id":34983,"text":"Contaminant Biology Program","active":true,"usgs":true}],"links":[{"id":116647,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr_2011_1125.jpg"},{"id":204783,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2011/1125/","linkFileType":{"id":5,"text":"html"}},{"id":334505,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2011/1125/pdf/of2011_1125.pdf","size":"529 kB","linkFileType":{"id":1,"text":"pdf"}}],"geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -92,37.25 ], [ -92,38.75 ], [ -90,38.75 ], [ -90,37.25 ], [ -92,37.25 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a54e4b07f02db62bc58","contributors":{"authors":[{"text":"Hinck, Jo Ellen 0000-0002-4912-5766","orcid":"https://orcid.org/0000-0002-4912-5766","contributorId":38507,"corporation":false,"usgs":true,"family":"Hinck","given":"Jo","email":"","middleInitial":"Ellen","affiliations":[],"preferred":false,"id":307998,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Ingersoll, Christopher G. 0000-0003-4531-5949 cingersoll@usgs.gov","orcid":"https://orcid.org/0000-0003-4531-5949","contributorId":2071,"corporation":false,"usgs":true,"family":"Ingersoll","given":"Christopher","email":"cingersoll@usgs.gov","middleInitial":"G.","affiliations":[{"id":192,"text":"Columbia Environmental Research Center","active":true,"usgs":true}],"preferred":true,"id":307995,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Wang, Ning 0000-0002-2846-3352 nwang@usgs.gov","orcid":"https://orcid.org/0000-0002-2846-3352","contributorId":2818,"corporation":false,"usgs":true,"family":"Wang","given":"Ning","email":"nwang@usgs.gov","affiliations":[{"id":192,"text":"Columbia Environmental Research Center","active":true,"usgs":true}],"preferred":true,"id":307996,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Augspurger, Tom","contributorId":63921,"corporation":false,"usgs":true,"family":"Augspurger","given":"Tom","affiliations":[],"preferred":false,"id":308001,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Barnhart, M. Christopher","contributorId":78061,"corporation":false,"usgs":true,"family":"Barnhart","given":"M. Christopher","affiliations":[],"preferred":false,"id":308002,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"McMurray, Stephen E.","contributorId":38687,"corporation":false,"usgs":true,"family":"McMurray","given":"Stephen E.","affiliations":[],"preferred":false,"id":307999,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Roberts, Andrew D.","contributorId":52304,"corporation":false,"usgs":true,"family":"Roberts","given":"Andrew","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":308000,"contributorType":{"id":1,"text":"Authors"},"rank":7},{"text":"Schrader, Lynn","contributorId":14551,"corporation":false,"usgs":true,"family":"Schrader","given":"Lynn","email":"","affiliations":[],"preferred":false,"id":307997,"contributorType":{"id":1,"text":"Authors"},"rank":8}]}} ,{"id":99283,"text":"sim3121 - 2011 - Geologic map of the Ganiki Planitia quadrangle (V-14), Venus","interactions":[],"lastModifiedDate":"2023-03-16T10:55:03.655596","indexId":"sim3121","displayToPublicDate":"2011-05-24T00:00:00","publicationYear":"2011","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":333,"text":"Scientific Investigations Map","code":"SIM","onlineIssn":"2329-132X","printIssn":"2329-1311","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"3121","title":"Geologic map of the Ganiki Planitia quadrangle (V-14), Venus","docAbstract":"The Ganiki Planitia (V-14) quadrangle on Venus, which extends from 25° N. to 50° N. and from 180° E. to 210° E., derives its name from the extensive suite of plains that dominates the geology of the northern part of the region. With a surface area of nearly 6.5 x 106 km2 (roughly two-thirds that of the United States), the quadrangle is located northwest of the Beta-Atla-Themis volcanic zone and southeast of the Atalanta Planitia lowlands, areas proposed to be the result of large scale mantle upwelling and downwelling, respectively. The region immediately south of Ganiki Planitia is dominated by Atla Regio, a major volcanic rise beneath which localized upwelling appears to be ongoing, whereas the area just to the north is dominated by the orderly system of north-trending deformation belts that characterize Vinmara Planitia. The Ganiki Planitia quadrangle thus lies at the intersection between several physiographic regions where extensive mantle flow-induced tectonic and volcanic processes are thought to have occurred.\r\nThe geology of the V-14 quadrangle is characterized by a complex array of volcanic, tectonic, and impact-derived features. There are eleven impact craters with diameters from 4 to 64 km, as well as four diffuse 'splotch' features interpreted to be the product of near-surface bolide explosions. Tectonic activity has produced heavily deformed tesserae, belts of complex deformation and rifts as well as a distributed system of fractures and wrinkle ridges. Volcanic activity has produced extensive regional plains deposits, and in the northwest corner of the quadrangle these plains host the initial (or terminal) 700 km of the Baltis Vallis canali, an enigmatic volcanic feature with a net length of ~7,000 km that is the longest channel on Venus. Major volcanic centers in V-14 include eight large volcanoes and eight coronae; all but one of these sixteen features was noted during a previous global survey. The V-14 quadrangle contains an abundance of minor volcanic features including individual shield volcanoes and localized fissure eruptions as well as many small annular structures and domes, which often serve as the source for local lava flows.\r\nThe topographic and geophysical characteristics of the Ganiki Planitia quadrangle are less complex than the surface geology, but they yield equally valuable information about the region’s formation and evolution. Referenced to the mean planetary radius of 6051.84 km, the average elevation in the quadrangle is -0.26±0.86 km (2σ) with a full range of -2.58 km to 1.85 km. The highest 2.5 percent of elevations in the quadrangle (above 0.60 km) are associated primarily with the major tessera blocks and the peaks of a few volcanic edifices, whereas the lowest 2.5 percent (below -1.12 km) mostly occur within corona interiors and in the northwest corner of the quadrangle where the plains begin to merge into the Atalanta Planitia lowlands. At the ~4.6 km/pixel scale of the topography data, the mean point-to-point topographic slope is 0.63° and topographic slopes greater than 2° cover less than 5 percent of the region. Overall, the topography of the Ganiki Planitia quadrangle can be characterized as flat, low lying, and nearly devoid of abrupt topographic variation. Complementing this gentle topography, the geoid anomaly has a generally linear gradient that decreases north-northwest from a high of ~20 m at the southern edge of the quadrangle (the northern border of the Atla Regio anomaly) to a low of -30 to -40 m along the northern edge (Konopliv and others, 1999). The vertical component of the gravity anomaly varies from ~50 mGal to -40 mGal, and integrated analysis of the gravity and topography data indicates that dynamically supported regions and areas of thickened crust are both present within the quadrangle.\r\nBecause the Ganiki Planitia quadrangle is a plains-dominated lowland area that lies between several major physiographic provinces (namely, Atla Regio, Atalanta Planitia, and Vinmara Planitia), a geologic map of the region may yield insight into a wide array of important problems in Venusian geology. The current mapping effort and analysis complements previous efforts to characterize aspects of the region’s geology, for example stratigraphy near parabolic halo crater sites, volcanic plains emplacement, wrinkle ridges, volcanic feature distribution, volcano deformation, coronae characteristics, lithospheric flexure, and various features along a 30±7.58° N. geotraverse. Our current research focuses on addressing four specific questions. Has the dominant style of volcanic expression within the quadrangle varied in a systematic fashion over time? Does the tectonic deformation within the quadrangle record significant regional patterns that vary spatially or temporally, and if so what are the scales, orientations and sources of the stress fields driving this deformation? If mantle upwelling and downwelling have played a significant role in the formation of Atla Regio and Atalanta Planitia as has been proposed, does the geology of Ganiki Planitia record evidence of northwest-directed lateral mantle flow connecting the two sites? Finally, can integration of the tectonic and volcanic histories preserved within the quadrangle help constrain competing resurfacing models for Venus?","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/sim3121","collaboration":"Prepared for the National Aeronautics and Space Administration","usgsCitation":"Grosfils, E.B., Long, S.M., Venechuk, E.M., Hurwitz, D.M., Richards, J.W., Drury, D.E., and Hardin, J., 2011, Geologic map of the Ganiki Planitia quadrangle (V-14), Venus: U.S. Geological Survey Scientific Investigations Map 3121, Map: 43.86 inches x 36.87 inches; Pamphlet: ii, 30 p., https://doi.org/10.3133/sim3121.","productDescription":"Map: 43.86 inches x 36.87 inches; Pamphlet: ii, 30 p.","costCenters":[{"id":131,"text":"Astrogeology Science Center","active":true,"usgs":true}],"links":[{"id":116211,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sim_3121.jpg"},{"id":204782,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sim/3121/","linkFileType":{"id":5,"text":"html"}},{"id":414265,"rank":3,"type":{"id":2,"text":"Additional Report Piece"},"url":"https://doi.org/10.5066/P9NSC8UY","text":"Interactive map","linkHelpText":"- Geologic Map of the Ganiki Planitia Quadrangle (V-14) of Venus, 1:5M. Grosfils and others (2011)"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afee4b07f02db697873","contributors":{"authors":[{"text":"Grosfils, Eric B.","contributorId":27752,"corporation":false,"usgs":true,"family":"Grosfils","given":"Eric","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":307989,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Long, Sylvan M.","contributorId":14699,"corporation":false,"usgs":true,"family":"Long","given":"Sylvan","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":307988,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Venechuk, Elizabeth M.","contributorId":50053,"corporation":false,"usgs":true,"family":"Venechuk","given":"Elizabeth","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":307991,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Hurwitz, Debra M.","contributorId":43614,"corporation":false,"usgs":true,"family":"Hurwitz","given":"Debra","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":307990,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Richards, Joseph W.","contributorId":94926,"corporation":false,"usgs":true,"family":"Richards","given":"Joseph","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":307994,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Drury, Dorothy E.","contributorId":69425,"corporation":false,"usgs":true,"family":"Drury","given":"Dorothy","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":307993,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Hardin, Johanna","contributorId":58151,"corporation":false,"usgs":true,"family":"Hardin","given":"Johanna","email":"","affiliations":[],"preferred":false,"id":307992,"contributorType":{"id":1,"text":"Authors"},"rank":7}]}} ,{"id":99275,"text":"ofr20111123 - 2011 - Estimation of bed-material transport in the lower Chetco River, Oregon, water years 2009-2010","interactions":[],"lastModifiedDate":"2019-04-29T10:18:54","indexId":"ofr20111123","displayToPublicDate":"2011-05-20T00:00:00","publicationYear":"2011","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":"2011-1123","title":"Estimation of bed-material transport in the lower Chetco River, Oregon, water years 2009-2010","docAbstract":"This assessment of bed-material transport uses methods developed in a previous study (Wallick and others, 2010) to estimate bed-material flux at the USGS Chetco River streamflow gaging station located at flood-plain kilometer 15 (14400000). On the basis of regressions between daily mean flow and transport capacity, daily bed-material flux was calculated for the period October 1, 2008 to March 30, 2011. The daily flux estimates were then aggregated by water year (WY) for WY 2009 and WY 2010 and the period April 1-March 31 during 2008-09, 2009-10 and 2010-11. The main findings were: \n\n*Estimated bed-material flux for WY 2009 (October 1, 2008 to September 30, 2009) was 87,300 metric tons as calculated by the Parker (1990a, b) equation (hereinafter \\'the Parker equation\\') and 116,900 metric tons as calculated by the Wilcock and Crowe (2003) equation (hereinafter \\'the Wilcock-Crowe equation\\'). \n*Estimated bed-material flux for water year 2010 (October 1, 2008 to September 30, 2009) was 56,800 metric tons as calculated by the Parker equation and 96,700 metric tons as calculated by the Wilcock-Crowe equation. \n*Estimated bed-material flux for April 1, 2008, to March 31, 2009, was 84,700 metric tons as calculated by the Parker equation and 111,700 metric tons as calculated by the Wilcock-Crowe equation. Flux values from April 1 to September 30, 2008, are from Wallick and others (2010). \n*Estimated bed-material flux for April 1, 2009, to March 31, 2010, was 45,500 metric tons as calculated by the Parker equation and 79,100 metric tons as calculated by the Wilcock-Crowe equation. \n*Estimated bed-material flux for April 1, 2010, to March 31, 2011, was 67,100 metric tons as calculated by the Parker equation and 134,300 metric tons as calculated by the Wilcock-Crowe equation. These calculations used provisional flow data for December 29, 2010, to March 31, 2011, and may be subject to revision. \n*Water years 2009 and 2010 both had less bed-material transport than the average annual transport values of 105,300 and 152,300 metric tons for the period 1970-2010 as calculated by the Parker and Wilcock-Crowe equations, respectively.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr20111123","collaboration":"Prepared in cooperation with the U.S. Army Corps of Engineers and the Oregon Department of State Lands\r\n","usgsCitation":"Wallick, J., and O'Connor, J., 2011, Estimation of bed-material transport in the lower Chetco River, Oregon, water years 2009-2010: U.S. Geological Survey Open-File Report 2011-1123, vi, 12 p., https://doi.org/10.3133/ofr20111123.","productDescription":"vi, 12 p.","numberOfPages":"21","additionalOnlineFiles":"N","costCenters":[{"id":518,"text":"Oregon Water Science Center","active":true,"usgs":true},{"id":615,"text":"Volcano Hazards Program","active":true,"usgs":true}],"links":[{"id":116908,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr_2011_1123.gif"},{"id":204777,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2011/1123/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Oregon","otherGeospatial":"Chetco River","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -124.30240631103514,\n 42.03679931146698\n ],\n [\n -124.1513442993164,\n 42.03679931146698\n ],\n [\n -124.1513442993164,\n 42.14125958838083\n ],\n [\n -124.30240631103514,\n 42.14125958838083\n ],\n [\n -124.30240631103514,\n 42.03679931146698\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e0e4b07f02db5e4788","contributors":{"authors":[{"text":"Wallick, J. Rose 0000-0002-9392-272X rosewall@usgs.gov","orcid":"https://orcid.org/0000-0002-9392-272X","contributorId":3583,"corporation":false,"usgs":true,"family":"Wallick","given":"J. Rose","email":"rosewall@usgs.gov","affiliations":[{"id":518,"text":"Oregon Water Science Center","active":true,"usgs":true}],"preferred":true,"id":307955,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"O'Connor, Jim E. 0000-0002-7928-5883 oconnor@usgs.gov","orcid":"https://orcid.org/0000-0002-7928-5883","contributorId":140771,"corporation":false,"usgs":true,"family":"O'Connor","given":"Jim E.","email":"oconnor@usgs.gov","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true},{"id":518,"text":"Oregon Water Science Center","active":true,"usgs":true}],"preferred":false,"id":307956,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":99268,"text":"ds593 - 2011 - Suspended-sediment and suspended-sand concentrations and loads for selected streams in the Mississippi River Basin, 1940-2009","interactions":[],"lastModifiedDate":"2012-03-08T17:16:14","indexId":"ds593","displayToPublicDate":"2011-05-17T00:00:00","publicationYear":"2011","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":"593","title":"Suspended-sediment and suspended-sand concentrations and loads for selected streams in the Mississippi River Basin, 1940-2009","docAbstract":"This report presents suspended-sediment concentration and streamflow data, describes load-estimation techniques used in the computation of annual suspended-sediment loads, and presents annual suspended-sediment loads for 48 streamgaging stations within the Mississippi River Basin. Available published, unpublished, and computed annual total suspended-sediment and suspended-sand loads are presented for water years 1940 through 2009. When previously published annual loads were not available, total suspended-sediment and sand loads were computed using available data for water years 1949 through 2009. A table of suspended-sediment concentration and daily mean streamflow data used in the computation of annual loads is presented along with a table of compiled and computed annual suspended-sediment and suspended-sand loads, annual streamflows, and flow-weighted concentrations for the 48 stations.\r\n","language":"ENGLISH","publisher":"U.S. Geological Survey","doi":"10.3133/ds593","usgsCitation":"Heimann, D.C., Cline, T.L., and Glaspie, L.M., 2011, Suspended-sediment and suspended-sand concentrations and loads for selected streams in the Mississippi River Basin, 1940-2009: U.S. Geological Survey Data Series 593, vi, 6 p.; Downloads Directory, https://doi.org/10.3133/ds593.","productDescription":"vi, 6 p.; Downloads Directory","additionalOnlineFiles":"Y","costCenters":[{"id":396,"text":"Missouri Water Science Center","active":true,"usgs":true}],"links":[{"id":116112,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ds_593.jpg"},{"id":204771,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/ds/593/","linkFileType":{"id":5,"text":"html"}}],"scale":"2000000","projection":"Albers Equal-Area Conic","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -120,25 ], [ -120,48 ], [ -70,48 ], [ -70,25 ], [ -120,25 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae0e4b07f02db687fc8","contributors":{"authors":[{"text":"Heimann, David C. 0000-0003-0450-2545 dheimann@usgs.gov","orcid":"https://orcid.org/0000-0003-0450-2545","contributorId":3822,"corporation":false,"usgs":true,"family":"Heimann","given":"David","email":"dheimann@usgs.gov","middleInitial":"C.","affiliations":[{"id":396,"text":"Missouri Water Science Center","active":true,"usgs":true},{"id":36532,"text":"Central Midwest Water Science Center","active":true,"usgs":true}],"preferred":true,"id":307941,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Cline, Teri L.","contributorId":80220,"corporation":false,"usgs":true,"family":"Cline","given":"Teri","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":307942,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Glaspie, Lori M.","contributorId":98256,"corporation":false,"usgs":true,"family":"Glaspie","given":"Lori","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":307943,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":9001500,"text":"sir20095120 - 2011 - Borehole geophysical investigation of a formerly used defense site, Machiasport, Maine, 2003-2006","interactions":[],"lastModifiedDate":"2019-10-24T14:19:42","indexId":"sir20095120","displayToPublicDate":"2011-05-12T00:00:00","publicationYear":"2011","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":"2009-5120","title":"Borehole geophysical investigation of a formerly used defense site, Machiasport, Maine, 2003-2006","docAbstract":"The U.S. Geological Survey, in cooperation with the U.S. Army Corps of Engineers, collected borehole geophysical logs in 18 boreholes and interpreted the data along with logs from 19 additional boreholes as part of an ongoing, collaborative investigation at three environmental restoration sites in Machiasport, Maine. These sites, located on hilltops overlooking the seacoast, formerly were used for military defense. At each of the sites, chlorinated solvents, used as part of defense-site operations, have contaminated the fractured-rock aquifer. Borehole geophysical techniques and hydraulic methods were used to characterize bedrock lithology, fractures, and hydraulic properties. In addition, each geophysical method was evaluated for effectiveness for site characterization and for potential application for further aquifer characterization and (or) evaluation of remediation efforts. Results of borehole geophysical logging indicate the subsurface is highly fractured, metavolcanic, intrusive, metasedimentary bedrock. Selected geophysical logs were cross-plotted to assess correlations between rock properties. These plots included combinations of gamma, acoustic reflectivity, electromagnetic induction conductivity, normal resistivity, and single-point resistance. The combined use of acoustic televiewer (ATV) imaging and natural gamma logs proved to be effective for delineating rock types. Each of the rock units in the study area could be mapped in the boreholes, on the basis of the gamma and ATV reflectivity signatures. The gamma and mean ATV reflectivity data were used along with the other geophysical logs for an integrated interpretation, yielding a determination of quartz monzonite, rhyolite, metasedimentary units, or diabase/gabbro rock types. The interpretation of rock types on the basis of the geophysical logs compared well to drilling logs and geologic mapping. These results may be helpful for refining the geologic framework at depth. A stereoplot of all fractures intersecting the boreholes indicates numerous fractures, a high proportion of steeply dipping fractures, and considerable variation in fracture orientation. Low-dip-angle fractures associated with unloading and exfoliation are also present, especially at a depth of less than 100 feet below the top of casing. These sub-horizontal fractures help to connect the steeply dipping fractures, making this a highly connected fracture network. The high variability in the fracture orientations also increases the connectivity of the fracture network. A preliminary comparison of all fracture data from all the boreholes suggests fracturing decreases with depth. Because all the boreholes were not drilled to the same depth, however, there is a clear sampling bias. Hence, the deepest boreholes are analyzed separately for fracture density. For the deepest boreholes in the study, the intensity of fracturing does not decline significantly with depth. It is possible the fractures observed in these boreholes become progressively tighter or closed with depth, but this is difficult to verify with the borehole methods used in this investigation. The fact that there are more sealed fractures at depth (observed in optical televiewer logs in some of the boreholes) may indicate less opening of the sealed fractures, less water moving through the rock, and less weathering of the fracture infilling minerals. Although the fracture orientation remained fairly constant with depth, differences in the fracture patterns for the three restoration sites indicate the orientation of fractures varies across the study area. The fractures in boreholes on Miller Mountain predominantly strike northwest-southeast, and to a lesser degree they strike northeast. The fractures on or near the summit of Howard Mountain strike predominantly east-west and dip north and south, and the fractures near the Transmitter Site strike northeast-southwest and dip northwest and southeast. The fracture populations for the boreholes on or near the summit of Howard Mountain show more variation than at the other two sites. This variation may be related to the proximity of the fault, which is northeast of the summit of Howard Mountain. In a side-by-side comparison of stereoplots from selected boreholes, there was no clear correspondence between fracture orientation and proximity to the fault. There is, however, a difference in the total populations of fractures for the boreholes on or near the summit of Howard Mountain and the boreholes near the Transmitter Site. Further to the southwest and further away from the fault, the fractures at the Transmitter Site predominantly strike northeast-southwest and northwest-southeast.Heat-pulse flowmeter (HPFM) logging was used to identify transmissive fractures and to estimate the hydraulic properties along the boreholes. Ambient downflow was measured in 13 boreholes and ambient upflow was measured in 9 boreholes. In nine other bedrock boreholes, the HPFM did not detect measurable vertical flow. The observed direction of vertical flow in the boreholes generally was consistent with the conceptual flow model of downward movement in recharge locations and upward flow in discharge locations or at breaks in the slope of land surface. Under low-rate pumping or injection rates [0.25 to 1 gallon per minute (gal/min)], one to three inflow zones were identified in each borehole. Two limitations of HPFM methods are (1) the HPFM can only identify zones within 1.5 to 2 orders of magnitude of the most transmissive zone in each borehole, and (2) the HPFM cannot detect flow rates less than 0.010 + or - 0.005 gal/min, which corresponds to a transmissivity of about 1 foot squared per day (ft2/d). Consequently, the HPFM is considered an effective tool for identifying the most transmissive fractures in a borehole, down to its detection level. Transmissivities below that cut-off must be measured with another method, such as packer testing or fluid-replacement logging. Where sufficient water-level and flowmeter data were available, HPFM results were numerically modeled. For each borehole model, the fracture location and measured flow rates were specified, and the head and transmissivity of each fracture zone were adjusted until a model fit was achieved with the interpreted ambient and stressed flow profiles. The transmissivities calculated by this method are similar to the results of an open-hole slug test; with the added information from the flowmeter, however, the head and transmissivity of discrete zones also can be determined. The discrete-interval transmissivities ranged from 0.16 to 330 ft2/d. The flowmeter-derived open-hole transmissivity, which is the combined total of each of the transmissive zones, ranged from 1 to 511 ft2/d. The whole-well open-hole transmissivity values determined with HPFM methods were compared to the results of open-hole hydraulic tests. Despite the fact that the flowmeter-derived transmissivities consistently were lower than the estimates derived from open-hole hydraulic tests alone, the correlation was very strong (with a coefficient of determination, R2, of 0.9866), indicating the HPFM method provides a reasonable estimate of transmissivities for the most transmissive fractures in the borehole. Geologic framework, fracture characterization, and estimates of hydraulic properties were interpreted together to characterize the fracture network. The data and interpretation presented in this report should provide information useful for site investigators as the conceptual site groundwater flow model is refined. Collectively, the results and the conceptual site model are important for evaluating remediation options and planning or implementing the design of a well field and borehole completions that will be adequate for monitoring flow, remediation efforts, groundwater levels, and (or) water quality. Similar kinds of borehole geophysical logging (specifically the borehole imaging, gamma, fluid logs, and HPFM) should be conducted in any newly installed boreholes and integrated with interpretations of any nearby boreholes. If boreholes are installed close to existing or other new boreholes, cross-hole flowmeter surveys may be appropriate and may help characterize the aquifer properties and connections between the boreholes.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/sir20095120","collaboration":"Prepared in cooperation with the\r\nU.S. Army Corps of Engineers, New England District","usgsCitation":"Johnson, C.D., Mondazzi, R.A., and Joesten, P.K., 2011, Borehole geophysical investigation of a formerly used defense site, Machiasport, Maine, 2003-2006: U.S. Geological Survey Scientific Investigations Report 2009-5120, Report: viii, 75 p.; 6 Appendixes, https://doi.org/10.3133/sir20095120.","productDescription":"Report: viii, 75 p.; 6 Appendixes","onlineOnly":"N","additionalOnlineFiles":"Y","temporalStart":"2003-01-01","temporalEnd":"2006-12-31","costCenters":[{"id":474,"text":"New York Water Science Center","active":true,"usgs":true},{"id":486,"text":"OGW Branch of Geophysics","active":true,"usgs":true},{"id":493,"text":"Office of Ground Water","active":true,"usgs":true},{"id":589,"text":"Toxic Substances Hydrology Program","active":true,"usgs":true},{"id":37277,"text":"WMA - Earth System Processes Division","active":true,"usgs":true}],"links":[{"id":116985,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2009_5120.jpg"},{"id":368562,"rank":4,"type":{"id":3,"text":"Appendix"},"url":"https://pubs.usgs.gov/sir/2009/5120/pdf/Appendixes%201-6_individual/sir2009-5120_apx01.pdf","text":"Appendix 1"},{"id":368564,"rank":5,"type":{"id":3,"text":"Appendix"},"url":"https://pubs.usgs.gov/sir/2009/5120/pdf/Appendixes%201-6_individual/sir2009-5120_apx03.pdf","text":"Appendix 3"},{"id":368563,"rank":4,"type":{"id":3,"text":"Appendix"},"url":"https://pubs.usgs.gov/sir/2009/5120/pdf/Appendixes%201-6_individual/sir2009-5120_apx02.pdf","text":"Appendix 2"},{"id":368565,"rank":6,"type":{"id":3,"text":"Appendix"},"url":"https://pubs.usgs.gov/sir/2009/5120/pdf/Appendixes%201-6_individual/sir2009-5120_apx04.pdf","text":"Appendix 4"},{"id":368566,"rank":7,"type":{"id":3,"text":"Appendix"},"url":"https://pubs.usgs.gov/sir/2009/5120/pdf/Appendixes%201-6_individual/sir2009-5120_apx05.pdf","text":"Appendix 5"},{"id":368567,"rank":8,"type":{"id":3,"text":"Appendix"},"url":"https://pubs.usgs.gov/sir/2009/5120/pdf/Appendixes%201-6_individual/sir2009-5120_apx06.pdf","text":"Appendix 6"},{"id":19868,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/sir/2009/5120/pdf/sir2009-5120_text_508.pdf","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Maine","city":"Machiasport","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -67.50240325927734,\n 44.618088532560364\n ],\n [\n -67.24113464355469,\n 44.618088532560364\n ],\n [\n -67.24113464355469,\n 44.75429167998072\n ],\n [\n -67.50240325927734,\n 44.75429167998072\n ],\n [\n -67.50240325927734,\n 44.618088532560364\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a14e4b07f02db602a09","contributors":{"authors":[{"text":"Johnson, Carole D. 0000-0001-6941-1578 cjohnson@usgs.gov","orcid":"https://orcid.org/0000-0001-6941-1578","contributorId":1891,"corporation":false,"usgs":true,"family":"Johnson","given":"Carole","email":"cjohnson@usgs.gov","middleInitial":"D.","affiliations":[{"id":37277,"text":"WMA - Earth System Processes Division","active":true,"usgs":true}],"preferred":true,"id":344636,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Mondazzi, Remo A.","contributorId":77898,"corporation":false,"usgs":true,"family":"Mondazzi","given":"Remo","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":344638,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Joesten, Peter K. pjoesten@usgs.gov","contributorId":1929,"corporation":false,"usgs":true,"family":"Joesten","given":"Peter","email":"pjoesten@usgs.gov","middleInitial":"K.","affiliations":[{"id":474,"text":"New York Water Science Center","active":true,"usgs":true},{"id":486,"text":"OGW Branch of Geophysics","active":true,"usgs":true}],"preferred":true,"id":344637,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":99253,"text":"sir20105223 - 2011 - Effects of recreational flow releases on natural resources of the Indian and Hudson Rivers in the Central Adirondack Mountains, New York, 2004-06","interactions":[],"lastModifiedDate":"2015-03-25T13:33:41","indexId":"sir20105223","displayToPublicDate":"2011-05-10T00:00:00","publicationYear":"2011","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":"2010-5223","title":"Effects of recreational flow releases on natural resources of the Indian and Hudson Rivers in the Central Adirondack Mountains, New York, 2004-06","docAbstract":"The U.S. Geological Survey (USGS), the New York State Department of Environmental Conservation (NYSDEC), and Cornell University carried out a cooperative 2-year study from the fall of 2004 through the fall of 2006 to characterize the potential effects of recreational-flow releases from Lake Abanakee on natural resources in the Indian and Hudson Rivers. Researchers gathered baseline information on hydrology, temperature, habitat, nearshore wetlands, and macroinvertebrate and fish communities and assessed the behavior and thermoregulation of stocked brown trout in study reaches from both rivers and from a control river. The effects of recreational-flow releases (releases) were assessed by comparing data from affected reaches with data from the same reaches during nonrelease days, control reaches in a nearby run-of-the-river system (the Cedar River), and one reach in the Hudson River upstream from the confluence with the Indian River. A streamgage downstream from Lake Abanakee transmitted data by satellite from November 2004 to November 2006; these data were used as the basis for developing a rating curve that was used to estimate discharges for the study period. River habitat at most study reaches was delineated by using Global Positioning System and ArcMap software on a handheld computer, and wetlands were mapped by ground-based measurements of length, width, and areal density. River temperature in the Indian and Hudson Rivers was monitored continuously at eight sites during June through September of 2005 and 2006; temperature was mapped in 2005 by remote imaging made possible through collaboration with the Rochester Institute of Technology. Fish communities at all study reaches were surveyed and characterized through quantitative, nearshore electrofishing surveys. Macroinvertebrate communities in all study reaches were sampled using the traveling-kick method and characterized using standard indices. Radio telemetry was used to track the movement and persistence of stocked brown trout (implanted with temperature-sensitive transmitters) in the Indian and Hudson Rivers during the summer of 2005 and in all three rivers during the summer of 2006. The releases had little effect on river temperatures, but increased discharges by about one order of magnitude. Regardless of the releases, river temperatures at all study sites commonly exceeded the threshold known to be stressful to brown trout. At most sites, mean and median water temperatures on release days were not significantly different, or slightly lower, than water temperatures on nonrelease days. Most differences were very small and, thus, were probably not biologically meaningful. The releases generally increased the total surface area of fast-water habitat (rapids, runs, and riffles) and decreased the total surface area of slow-water habitat (pools, glides, backwater areas, and side channels). The total surface areas of wetlands bordering the Indian River were substantially smaller than the surface areas bordering the Cedar River; however, no channel geomorphology or watershed soil and topographic data were assessed to determine whether the releases or other factors were mainly responsible for observed differences. Results from surveys of resident biota indicate that the releases generally had a limited effect on fish and macroinvertebrate communities in the Indian River and had no effect on communities in the Hudson River. Compared to fish data from Cedar River control sites, the impoundment appeared to reduce total density, biomass, and richness in the Indian River at the first site downstream from Lake Abanakee, moderately reduce the indexes at the other two sites on the Indian River, and slightly reduce the indexes at the first Hudson River site downstream from the confluence with the Indian River. The densities of individual fish populations at all Indian River sites were also reduced, but related effects on fish populations in the Hudson River were less evident. Altho
","language":"ENGLISH","publisher":"U.S. Geological Survey","doi":"10.3133/sir20105223","collaboration":"Prepared in cooperation with the\r\nNew York State Department of Environmental Conservation","usgsCitation":"Baldigo, B., Mulvihill, C., Ernst, A., and Boisvert, B., 2011, Effects of recreational flow releases on natural resources of the Indian and Hudson Rivers in the Central Adirondack Mountains, New York, 2004-06: U.S. Geological Survey Scientific Investigations Report 2010-5223, xix, 72 p., https://doi.org/10.3133/sir20105223.","productDescription":"xix, 72 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":474,"text":"New York Water Science Center","active":true,"usgs":true}],"links":[{"id":116926,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2010_5223.gif"},{"id":14669,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2010/5223/","linkFileType":{"id":5,"text":"html"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a29e4b07f02db611998","contributors":{"authors":[{"text":"Baldigo, Barry P. 0000-0002-9862-9119","orcid":"https://orcid.org/0000-0002-9862-9119","contributorId":25174,"corporation":false,"usgs":true,"family":"Baldigo","given":"Barry P.","affiliations":[{"id":474,"text":"New York Water Science Center","active":true,"usgs":true}],"preferred":true,"id":307877,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Mulvihill, C.I.","contributorId":17350,"corporation":false,"usgs":true,"family":"Mulvihill","given":"C.I.","email":"","affiliations":[],"preferred":false,"id":307876,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Ernst, A.G.","contributorId":8973,"corporation":false,"usgs":true,"family":"Ernst","given":"A.G.","email":"","affiliations":[],"preferred":false,"id":307875,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Boisvert, B.A.","contributorId":79601,"corporation":false,"usgs":true,"family":"Boisvert","given":"B.A.","email":"","affiliations":[],"preferred":false,"id":307878,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":99244,"text":"ofr20111063 - 2011 - Water and rock geochemistry, geologic cross sections, geochemical modeling, and groundwater flow modeling for identifying the source of groundwater to Montezuma Well, a natural spring in central Arizona","interactions":[],"lastModifiedDate":"2012-02-10T00:11:58","indexId":"ofr20111063","displayToPublicDate":"2011-05-04T00:00:00","publicationYear":"2011","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":"2011-1063","title":"Water and rock geochemistry, geologic cross sections, geochemical modeling, and groundwater flow modeling for identifying the source of groundwater to Montezuma Well, a natural spring in central Arizona","docAbstract":"The National Park Service (NPS) seeks additional information to better understand the source(s) of groundwater and associated groundwater flow paths to Montezuma Well in Montezuma Castle National Monument, central Arizona. The source of water to Montezuma Well, a flowing sinkhole in a desert setting, is poorly understood. Water emerges from the middle limestone facies of the lacustrine Verde Formation, but the precise origin of the water and its travel path are largely unknown. Some have proposed artesian flow to Montezuma Well through the Supai Formation, which is exposed along the eastern margin of the Verde Valley and underlies the Verde Formation. The groundwater recharge zone likely lies above the floor of the Verde Valley somewhere to the north or east of Montezuma Well, where precipitation is more abundant. Additional data from groundwater, surface water, and bedrock geology are required for Montezuma Well and the surrounding region to test the current conceptual ideas, to provide new details on the groundwater flow in the area, and to assist in future management decisions. The results of this research will provide information for long-term water resource management and the protection of water rights.","language":"ENGLISH","publisher":"U.S. Geological Survey","doi":"10.3133/ofr20111063","collaboration":"Prepared in cooperation with the National Park Service","usgsCitation":"Johnson, R.H., DeWitt, E., Wirt, L., Arnold, L., and Horton, J.D., 2011, Water and rock geochemistry, geologic cross sections, geochemical modeling, and groundwater flow modeling for identifying the source of groundwater to Montezuma Well, a natural spring in central Arizona: U.S. Geological Survey Open-File Report 2011-1063, x, 62 p.; Downloads Directory, https://doi.org/10.3133/ofr20111063.","productDescription":"x, 62 p.; Downloads Directory","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[{"id":211,"text":"Crustal Geophysics and Geochemistry Science Center","active":true,"usgs":true}],"links":[{"id":116922,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr_2011_1063.png"},{"id":14659,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2011/1063/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Arizona","otherGeospatial":"Montezuma Well;Verde Valley","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -112,34.5 ], [ -112,35 ], [ -111.33333333333333,35 ], [ -111.33333333333333,34.5 ], [ -112,34.5 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49a1e4b07f02db5be02e","contributors":{"authors":[{"text":"Johnson, Raymond H. rhjohnso@usgs.gov","contributorId":707,"corporation":false,"usgs":true,"family":"Johnson","given":"Raymond","email":"rhjohnso@usgs.gov","middleInitial":"H.","affiliations":[],"preferred":true,"id":307850,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"DeWitt, Ed","contributorId":65081,"corporation":false,"usgs":true,"family":"DeWitt","given":"Ed","affiliations":[],"preferred":false,"id":307853,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Wirt, Laurie","contributorId":13204,"corporation":false,"usgs":true,"family":"Wirt","given":"Laurie","affiliations":[],"preferred":false,"id":307852,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Arnold, L. Rick","contributorId":101613,"corporation":false,"usgs":true,"family":"Arnold","given":"L. Rick","affiliations":[],"preferred":false,"id":307854,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Horton, John D. 0000-0003-2969-9073 jhorton@usgs.gov","orcid":"https://orcid.org/0000-0003-2969-9073","contributorId":1227,"corporation":false,"usgs":true,"family":"Horton","given":"John","email":"jhorton@usgs.gov","middleInitial":"D.","affiliations":[{"id":171,"text":"Central Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":307851,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":9001490,"text":"sir20115054 - 2011 - Geology, Hydrology, and Water Quality of the Little Blackwater River Watershed, Dorchester County, Maryland, 2006-09","interactions":[],"lastModifiedDate":"2012-03-08T17:16:40","indexId":"sir20115054","displayToPublicDate":"2011-05-04T00:00:00","publicationYear":"2011","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":"2011-5054","title":"Geology, Hydrology, and Water Quality of the Little Blackwater River Watershed, Dorchester County, Maryland, 2006-09","docAbstract":"The Little Blackwater River watershed is a low-lying tidal watershed in Dorchester County, Maryland. The potential exists for increased residential development in a mostly agricultural watershed that drains into the Blackwater National Wildlife Refuge. Groundwater and surface-water levels were collected along with water-quality samples to document hydrologic and geochemical conditions within the watershed prior to potential land-use changes. Lithologic logs were collected in the Little Blackwater River watershed and interpreted with existing geophysical logs to conceptualize the shallow groundwater-flow system. A shallow water table exists in much of the watershed as shown by sediment cores and surface geophysical surveys. Water-table wells have seasonal variations of 6 feet, with the lowest water levels occurring in September and October. Seasonally low water-table levels are lower than the stage of the Little Blackwater River, creating the potential for surface-water infiltration into the water table. Two stream gages, each equipped with stage, velocity, specific conductance, and temperature sensors, were installed at the approximate mid-point of the watershed and near the mouth of the Little Blackwater River. The gages recorded data continuously and also were equipped with telemetry. Discharge calculated at the mouth of the Little Blackwater River showed a seasonal pattern, with net positive discharge in the winter and spring months and net negative discharge (flow into the watershed from Blackwater National Wildlife Refuge and Fishing Bay) in the summer and fall months. Continuous water-quality records showed an increase in specific conductance during the summer and fall months. Discrete water-quality samples were collected during 2007--08 from 13 of 15 monitoring wells and during 2006--09 from 9 surface-water sites to characterize pre-development conditions and the seasonal variability of inorganic constituents and nutrients. The highest mean values of nitrogen are found in the deep groundwater system, with relatively low values in the water table. Surface-water-quality samples in the lower half of the basin show a significant increase in inorganic seawater constituents, especially in summer, corresponding with net negative discharge from the Little Blackwater River. Samples also were collected from nine wells and four surface-water sites for pesticides in June 2008. The herbicides atrazine, metolachlor, and simazine, and the insecticide fipronil were detected at each of the four surface-water sites, with concentrations less than 2 micrograms per liter. Concentrations of pesticides found in groundwater were typically one to two orders of magnitude lower than pesticide concentrations found in surface water of the Little Blackwater River. Seasonal hydraulic-gradient reversals between the shallow groundwater system and the Little Blackwater River, coincident with the inflow of brackish water from Fishing Bay and Blackwater National Wildlife Refuge, indicate a potential for saltwater intrusion into the water table. The likelihood of saltwater intrusion into the water table is further supported by high chloride concentrations observed in water-table wells near the Little Blackwater River.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/sir20115054","collaboration":"Prepared in cooperation with the Maryland Department of the Environment,\r\nMaryland Department of Natural Resources,\r\nMaryland Department of Agriculture,\r\nDorchester Soil Conservation District, and the\r\nU.S. Fish and Wildlife Service","usgsCitation":"Fleming, B.J., DeJong, B.D., and Phelan, D.J., 2011, Geology, Hydrology, and Water Quality of the Little Blackwater River Watershed, Dorchester County, Maryland, 2006-09: U.S. Geological Survey Scientific Investigations Report 2011-5054, vi, 82 p. , https://doi.org/10.3133/sir20115054.","productDescription":"vi, 82 p. ","numberOfPages":"82","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":374,"text":"Maryland Water Science Center","active":true,"usgs":true}],"links":[{"id":116923,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2011_5054.bmp"},{"id":19274,"rank":200,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/sir/2011/5054/","linkFileType":{"id":5,"text":"html"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c6cc","contributors":{"authors":[{"text":"Fleming, Brandon J. 0000-0001-9649-7485 bjflemin@usgs.gov","orcid":"https://orcid.org/0000-0001-9649-7485","contributorId":4115,"corporation":false,"usgs":true,"family":"Fleming","given":"Brandon","email":"bjflemin@usgs.gov","middleInitial":"J.","affiliations":[{"id":374,"text":"Maryland Water Science Center","active":true,"usgs":true}],"preferred":true,"id":344611,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"DeJong, Benjamin D. bdejong@usgs.gov","contributorId":2506,"corporation":false,"usgs":true,"family":"DeJong","given":"Benjamin","email":"bdejong@usgs.gov","middleInitial":"D.","affiliations":[],"preferred":true,"id":344610,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Phelan, Daniel J.","contributorId":51716,"corporation":false,"usgs":true,"family":"Phelan","given":"Daniel","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":344612,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":9001486,"text":"sir20115049 - 2011 - Paleomagnetic correlation of surface and subsurface basaltic lava flows and flow groups in the southern part of the Idaho National Laboratory, Idaho, with paleomagnetic data tables for drill cores","interactions":[],"lastModifiedDate":"2012-03-08T17:16:39","indexId":"sir20115049","displayToPublicDate":"2011-05-03T00:00:00","publicationYear":"2011","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":"2011-5049","title":"Paleomagnetic correlation of surface and subsurface basaltic lava flows and flow groups in the southern part of the Idaho National Laboratory, Idaho, with paleomagnetic data tables for drill cores","docAbstract":"Paleomagnetic inclination and polarity studies have been conducted on thousands of subcore samples from 51 coreholes located at and near the Idaho National Laboratory. These studies are used to paleomagnetically characterize and correlate successive stratigraphic intervals in each corehole to similar depth intervals in adjacent coreholes. Paleomagnetic results from 83 surface paleomagnetic sites, within and near the INL, are used to correlate these buried lava flow groups to basaltic shield volcanoes still exposed on the surface of the eastern Snake River Plain. Sample handling and demagnetization protocols are described as well as the paleomagnetic data averaging process. Paleomagnetic inclination comparisons between coreholes located only kilometers apart show comparable stratigraphic successions of mean inclination values over tens of meters of depth. At greater distance between coreholes, comparable correlation of mean inclination values is less consistent because flow groups may be missing or additional flow groups may be present and found at different depth intervals. Two shallow intersecting cross-sections, A-A- and B-B- (oriented southwest-northeast and northwest-southeast, respectively), drawn through southwest Idaho National Laboratory coreholes show the corehole to corehole or surface to corehole correlations derived from the paleomagnetic inclination data. From stratigraphic top to bottom, key results included the (1) Quaking Aspen Butte flow group, which erupted from Quaking Aspen Butte southwest of the Idaho National Laboratory, flowed northeast, and has been found in the subsurface in corehole USGS 132; (2) Vent 5206 flow group, which erupted near the southwestern border of the Idaho National Laboratory, flowed north and east, and has been found in the subsurface in coreholes USGS 132, USGS 129, USGS 131, USGS 127, USGS 130, USGS 128, and STF-AQ-01; and (3) Mid Butte flow group, which erupted north of U.S. Highway 20, flowed northwest, and has been found in the subsurface at coreholes ARA-COR-005 and STF-AQ-01. The high K20 flow group erupted from a vent that may now be buried south of U.S. Highway 20 near Middle Butte, flowed north, and is found in the subsurface in coreholes USGS 131, USGS 127, USGS 130, USGS 128, USGS 123, STF-AQ-01, and ARA-COR-005 ending near the Idaho Nuclear Technology and Engineering Center. The vent 5252 flow group erupted just south of U.S. Highway 20 near Middle and East Buttes, flowed northwest, and is found in the subsurface in coreholes ARA-COR-005, STF-AQ-01, USGS 130, USGS 128, ICPP 214, USGS 123, ICPP 023, USGS 121, USGS 127, and USGS 131. The Big Lost flow group erupted from a now-buried vent near the Radioactive Waste Management Complex, flowed southwest to corehole USGS 135, and northeast to coreholes USGS 132, USGS 129, USGS 131, USGS 127, USGS 130, STF-AQ-01, and ARA-COR-005. The AEC Butte flow group erupted from AEC Butte near the Advanced Test Reactor Complex and flowed south to corehole Middle 1823, northwest to corehole USGS 134, northeast to coreholes USGS 133 and NRF 7P, and south to coreholes USGS 121, ICPP 023, USGS 123, and USGS 128. Evidence of progressive subsidence of the axial zone of the ESRP is shown in these cross-sections, distorting the original attitudes of the lava flow groups and interbedded sediments. A deeper cross-section, C-C- (oriented west to east), spanning the entire southern Idaho National Laboratory shows correlations of the lava flow groups in the saturated part of the ESRP aquifer. Areally extensive flow groups in the deep subsurface (from about 100-800 meters below land surface) can be traced over long distances. In cross-section C-C-, the flow group labeled \"Matuyama\" can be correlated from corehole USGS 135 to corehole NPR Test/W-02, a distance of about 28 kilometers (17 miles). The flow group labeled \"Matuyama 1.21 Ma\" can be correlated from corehole Middle 1823 to corehole ANL-OBS-A-001, a distance of 26 kilometers (16 miles). Other flo","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/sir20115049","collaboration":"Prepared in cooperation with the U.S. Department of Energy DOE/ID-22214","usgsCitation":"Champion, D.E., Hodges, M., Davis, L.C., and Lanphere, M.A., 2011, Paleomagnetic correlation of surface and subsurface basaltic lava flows and flow groups in the southern part of the Idaho National Laboratory, Idaho, with paleomagnetic data tables for drill cores: U.S. Geological Survey Scientific Investigations Report 2011-5049, vi, 32 p.; Appendix; 1 Plate; ZIP download of Appendix A, https://doi.org/10.3133/sir20115049.","productDescription":"vi, 32 p.; Appendix; 1 Plate; ZIP download of Appendix A","numberOfPages":"34","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[{"id":343,"text":"Idaho Water Science Center","active":true,"usgs":true}],"links":[{"id":116935,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2011_5049.jpg"},{"id":19272,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2011/5049","linkFileType":{"id":5,"text":"html"}}],"scale":"24000","projection":"Universal Transverse Mercator projection","country":"United States","state":"Idaho","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -113.36749999999999,43.333333333333336 ], [ -113.36749999999999,44.06666666666667 ], [ -112.36749999999999,44.06666666666667 ], [ -112.36749999999999,43.333333333333336 ], [ -113.36749999999999,43.333333333333336 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae4e4b07f02db689bea","contributors":{"authors":[{"text":"Champion, Duane E. 0000-0001-7854-9034 dchamp@usgs.gov","orcid":"https://orcid.org/0000-0001-7854-9034","contributorId":2912,"corporation":false,"usgs":true,"family":"Champion","given":"Duane","email":"dchamp@usgs.gov","middleInitial":"E.","affiliations":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"preferred":true,"id":344603,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hodges, Mary K.V.","contributorId":66848,"corporation":false,"usgs":true,"family":"Hodges","given":"Mary K.V.","affiliations":[],"preferred":false,"id":344604,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Davis, Linda C. lcdavis@usgs.gov","contributorId":2539,"corporation":false,"usgs":true,"family":"Davis","given":"Linda","email":"lcdavis@usgs.gov","middleInitial":"C.","affiliations":[{"id":343,"text":"Idaho Water Science Center","active":true,"usgs":true}],"preferred":true,"id":344601,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Lanphere, Marvin A. alder@usgs.gov","contributorId":2696,"corporation":false,"usgs":true,"family":"Lanphere","given":"Marvin","email":"alder@usgs.gov","middleInitial":"A.","affiliations":[],"preferred":true,"id":344602,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":9001484,"text":"sir20115055 - 2011 - Geologic framework and hydrogeology of the middle Carson River Basin, Eagle, Dayton, and Churchill Valleys, West-Central Nevada","interactions":[],"lastModifiedDate":"2020-10-27T18:52:47.446235","indexId":"sir20115055","displayToPublicDate":"2011-05-03T00:00:00","publicationYear":"2011","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":"2011-5055","title":"Geologic framework and hydrogeology of the middle Carson River Basin, Eagle, Dayton, and Churchill Valleys, West-Central Nevada","docAbstract":"Changes in land use and water use and increasing development of water resources in the middle Carson River basin may affect flow of the river and, in turn, affect downstream water users dependent on sustained river flows to Lahontan Reservoir. The U.S. Geological Survey, in cooperation with the Bureau of Reclamation, began a study in 2008 of the middle Carson River basin, extending from Eagle Valley to Churchill Valley. Various types of geologic and hydrologic data were compiled from previous studies, collected for this study, and compiled and analyzed to provide a framework for development of a numerical model of the groundwater and surface-water flow systems of the basin.
Geologic units that are assumed to have similar hydrologic characteristics were grouped into hydrogeologic units comprised of consolidated rocks of pre-Cenozoic age that underlie a unit of consolidated volcanic rock and semi-consolidated sediments of Tertiary age. The principal aquifer in the study area is comprised of unconsolidated sediments of Quaternary age. The Quaternary sediments include alluvial fan, fluvial, and lake sediments, and were grouped into a basin-fill hydrogeologic unit that overlies the pre-Cenozoic and Tertiary hydrologic units.
The thickness of the combined section of Tertiary volcanic and sedimentary rocks and Quaternary basin-fill deposits previously was estimated to range from zero where pre-Cenozoic rocks are exposed to greater than 10,000 feet in the Bull Canyon subbasin, and greater than 6,000 feet on the western side of Churchill Butte and beneath the Desert Mountains. The thickness of Quaternary basin-fill sediments was estimated using gravity data and lithologic descriptions from driller’s logs. The most permeable parts of basin-fill sediments are greater than 1,000 feet thick in the Carson Plains subbasin, greater than 800 feet and 600 feet thick in the western and northeastern parts of the Stagecoach subbasin, and greater than 1,000 feet and 800 feet thick in the northern and southern parts of Churchill Valley, respectively.
The distribution of aquifer properties was estimated for basin-fill sediments using slug-test and aquifer test data, and the lithologic descriptions of previously mapped geologic units. Slug-test data show hydraulic conductivity is greater than 10 to greater than 100 feet per day for fluvial sediments near the flood plain, less than 10 feet per day for basin-fill sediments outside the flood plain, and less than 1 foot per day for consolidated rocks. Estimates of transmissivity exceed 20,000 feet squared per day near the Carson River in Dayton, Churchill, and western Lahontan Valleys and in the northern part of the Stagecoach subbasin, and exceed 10,000 feet squared per day in the western part of Churchill Valley. A transmissivity of 90,000 feet squared per day was estimated from results of an aquifer test in the Carson Plains subbasin, indicating that permeable gravel and cobble zones at depths greater than 400 feet supplied water to the pumping well. Estimates of specific yield ranged from less than 1 to 2 percent for most consolidated rocks, from 1 to 15 percent for semi-consolidated Tertiary sediments, and from 10 to 40 percent for unconsolidated basin-fill sediments.
Water-level altitude maps based on measurements at about 300 wells in 2009 show water levels have declined as much as 70 feet since 1964 on the northwestern side of Eagle Valley, about 10 feet since 1995 near Dayton in the Carson Plains subbasin, and from 5 to 10 feet since 1982 in the western and northeastern parts of the Stagecoach subbasin and the northwestern part of Churchill Valley. The declines are likely the result of municipal and agricultural pumping. The maps show a groundwater divide between the Carson Plains and Stagecoach subbasins, and a continuous hydraulic gradient between the Stagecoach subbasin and Churchill Valley. Groundwater flow directions are uncertain beneath parts of the boundary of Churchill Valley. The altitude of the top of pre-Cenozoic rocks shows thick sections of saturated Tertiary rocks and sediments south of the Dead Camel Mountains and beneath the eastern part of the Desert Mountains through which groundwater flow between Churchill Valley, Mason Valley, and Lahontan Valley may take place. North of Lahontan reservoir, beneath the Dead Camel Mountains, and beneath the southern part of Adrian Valley, the altitude of pre-Cenozoic rocks indicates groundwater flow between the three valleys is minimal.
Streamflow measurements, supported by data on the deuterium content and specific conductance of surface-water samples, indicate a loss of Carson River streamflow in the Riverview subbasin, streamflow gains in the Moundhouse subbasin and the eastern part of the Carson Plains subbasin, and streamflow losses in the Bull Canyon subbasin. Comparisons of fluctuations in groundwater levels to those in stream stage in the Carson Plains subbasin indicate that streamflow lost to infiltration from the Carson River, from irrigation ditches, and from irrigated fields is an important source of groundwater recharge. Fluctuations in groundwater levels compared with the stage of Lahontan Reservoir in Churchill Valley indicate losses to infiltration from the reservoir during high stage and groundwater seepage to the reservoir during low stage.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/sir20115055","collaboration":"Prepared in cooperation with the Bureau of Reclamation","usgsCitation":"Maurer, D.K., 2011, Geologic framework and hydrogeology of the middle Carson River Basin, Eagle, Dayton, and Churchill Valleys, West-Central Nevada: U.S. Geological Survey Scientific Investigations Report 2011-5055, Report: vii, 62 p.; Data release, https://doi.org/10.3133/sir20115055.","productDescription":"Report: vii, 62 p.; Data release","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":465,"text":"Nevada Water Science Center","active":true,"usgs":true}],"links":[{"id":116937,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2011_5055.jpg"},{"id":379827,"rank":4,"type":{"id":30,"text":"Data Release"},"url":"https://doi.org/10.5066/P9P5LJ3P","text":"USGS data release","description":"USGS data release","linkHelpText":"Data for the report Geologic Framework and Hydrogeology of the Middle Carson River Basin, Eagle, Dayton, and Churchill Valleys, West-Central Nevada"},{"id":379826,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/sir/2011/5055/pdf/sir20115055.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":14655,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2011/5055/","linkFileType":{"id":5,"text":"html"}}],"scale":"100000","projection":"Universal Transverse Mercator projection","country":"United States","state":"Nevada","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -120,38.333333333333336 ], [ -120,40.25 ], [ -118,40.25 ], [ -118,38.333333333333336 ], [ -120,38.333333333333336 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b17e4b07f02db6a5a5d","contributors":{"authors":[{"text":"Maurer, Douglas K. dkmaurer@usgs.gov","contributorId":2308,"corporation":false,"usgs":true,"family":"Maurer","given":"Douglas","email":"dkmaurer@usgs.gov","middleInitial":"K.","affiliations":[],"preferred":true,"id":344593,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70156908,"text":"70156908 - 2011 - Timing, distribution, amount, and style of Cenozoic extension in the northern Great Basin","interactions":[],"lastModifiedDate":"2023-05-24T13:19:08.523688","indexId":"70156908","displayToPublicDate":"2011-05-01T00:00:00","publicationYear":"2011","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1724,"text":"GSA Field Guides","active":true,"publicationSubtype":{"id":10}},"title":"Timing, distribution, amount, and style of Cenozoic extension in the northern Great Basin","docAbstract":"This field trip examines contrasting lines of evidence bearing on the timing and structural style of Cenozoic (and perhaps late Mesozoic) extensional deformation in northeastern Nevada. Studies of metamorphic core complexes in this region report extension beginning in the early Cenozoic or even Late Cretaceous, peaking in the Eocene and Oligocene, and being largely over before the onset of “modern” Basin and Range extension in the middle Miocene. In contrast, studies based on low-temperature thermochronology and geologic mapping of Eocene and Miocene volcanic and sedimentary deposits report only minor, localized extension in the Eocene, no extension at all in the Oligocene and early Miocene, and major, regional extension in the middle Miocene. A wealth of thermochronologic and thermobarometric data indicate that the Ruby Mountains–East Humboldt Range metamorphic core complex (RMEH) underwent ~170 °C of cooling and 4 kbar of decompression between ca. 85 and ca. 50 Ma, and another 450 °C cooling and 4–5 kbar decompression between ca. 50 and ca. 21 Ma. These data require ~30 km of exhumation in at least two episodes, accommodated at least in part by Eocene to early Miocene displacement on the major west-dipping mylonitic zone and detachment fault bounding the RMEH on the west (the mylonitic zone may also have been active during an earlier phase of crustal extension). Meanwhile, Eocene paleovalleys containing 45–40 Ma ash-flow tuffs drained eastward from northern Nevada to the Uinta Basin in Utah, and continuity of these paleovalleys and infilling tuffs across the region indicate little, if any deformation by faults during their deposition. Pre–45 Ma deformation is less constrained, but the absence of Cenozoic sedimentary deposits and mappable normal faults older than 45 Ma is also consistent with only minor (if any) brittle deformation. The presence of ≤1 km of late Eocene sedimentary—especially lacustrine—deposits and a low-angle angular unconformity between ca. 40 and 38 Ma rocks attest to an episode of normal faulting at ca. 40 Ma. Arguably the greatest conundrum is how much extension occurred between ca. 35 and 17 Ma. Major exhumation of the RMEH is interpreted to have taken place in the late Oligocene and early Miocene, but rocks of any kind deposited during this interval are scarce in northeastern Nevada and absent in the vicinity of the RMEH itself. In most places, no angular unconformity is present between late Eocene and middle Miocene rocks, indicating little or no tilting between the late Eocene and middle Miocene. Opinions among authors of this report differ, however, as to whether this indicates no extension during the same time interval. The one locality where Oligocene deposits have been documented is Copper Basin, where Oligocene (32.5–29.5 Ma) conglomerates are ~500 m thick. The contact between Oligocene and Eocene rocks in Copper Basin is conformable, and the rocks are uniformly tilted ~25° NW, opposite to a normal fault system dipping ~35° SE. Middle Miocene rhyolite (ca. 16 Ma) rests nonconformably on the metamorphosed lower plate of this fault system and appears to rest on the tilted upper-plate rocks with angular unconformity, but the contact is not physically exposed. Different authors of this report interpret geologic relations in Copper Basin to indicate either (1) significant episodes of extension in the Eocene, Oligocene, and middle Miocene or (2) minor extension in the Eocene, uncertainty about the Oligocene, and major extension in the middle Miocene. An episode of major middle Miocene extension beginning at ca. 16–17 Ma is indicated by thick (up to 5 km) accumulations of sedimentary deposits in half-graben basins over most of northern Nevada, tilting and fanning of dips in the synextensional sedimentary deposits, and apatite fission-track and (U-Th)/He data from the southern Ruby Mountains and other ranges that indicate rapid middle Miocene cooling through near-surface temperatures (~120–40 °C). Opinions among authors of this report differ as to whether this period of extension was merely the last step in a long history of extensional faulting dating back at least to the Eocene, or whether it accounts for most of the Cenozoic deformation in northeastern Nevada. Since 10–12 Ma, extension appears to have slowed greatly and been accommodated by high-angle, relatively wide-spaced normal faults that give topographic form to the modern ranges. Despite the low present-day rate of extension, normal faults are active and have generated damaging earthquakes as recently as 2008.
","language":"English","publisher":"The Geological Society of America","doi":"10.1130/2011.0021(02)","usgsCitation":"Henry, C., McGrew, A.J., Colgan, J.P., Snoke, A.W., and Brueseke, M.E., 2011, Timing, distribution, amount, and style of Cenozoic extension in the northern Great Basin: GSA Field Guides, v. 21, p. 27-66, https://doi.org/10.1130/2011.0021(02).","productDescription":"40 p.","startPage":"27","endPage":"66","onlineOnly":"N","additionalOnlineFiles":"N","ipdsId":"IP-029038","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":307799,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","otherGeospatial":"Northern Great Basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -124.07958984375001,\n 38.06539235133249\n ],\n [\n -124.07958984375001,\n 41.95131994679697\n ],\n [\n -113.203125,\n 41.95131994679697\n ],\n [\n -113.203125,\n 38.06539235133249\n ],\n [\n -124.07958984375001,\n 38.06539235133249\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"21","noUsgsAuthors":false,"publicationDate":"2011-06-09","publicationStatus":"PW","scienceBaseUri":"560bb70de4b058f706e53f3b","contributors":{"authors":[{"text":"Henry, Christopher D.","contributorId":36556,"corporation":false,"usgs":true,"family":"Henry","given":"Christopher D.","affiliations":[],"preferred":false,"id":571108,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"McGrew, Allen J.","contributorId":147302,"corporation":false,"usgs":false,"family":"McGrew","given":"Allen","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":571109,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Colgan, Joseph P. 0000-0001-6671-1436 jcolgan@usgs.gov","orcid":"https://orcid.org/0000-0001-6671-1436","contributorId":1649,"corporation":false,"usgs":true,"family":"Colgan","given":"Joseph","email":"jcolgan@usgs.gov","middleInitial":"P.","affiliations":[{"id":318,"text":"Geosciences and Environmental Change Science Center","active":true,"usgs":true},{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":571110,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Snoke, Arthur W.","contributorId":23667,"corporation":false,"usgs":true,"family":"Snoke","given":"Arthur","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":571111,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Brueseke, Matthew E.","contributorId":147303,"corporation":false,"usgs":false,"family":"Brueseke","given":"Matthew","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":571112,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":9001474,"text":"ofr20111105 - 2011 - Review of samples of tailings, soils, and stream sediments adjacent to and downstream from the Ruth Mine, Inyo County, California","interactions":[],"lastModifiedDate":"2021-11-10T21:54:17.533869","indexId":"ofr20111105","displayToPublicDate":"2011-04-30T00:00:00","publicationYear":"2011","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":"2011-1105","title":"Review of samples of tailings, soils, and stream sediments adjacent to and downstream from the Ruth Mine, Inyo County, California","docAbstract":"The Ruth Mine and mill are located in the western Mojave Desert in Inyo County, California (fig. 1). The mill processed gold-silver (Au-Ag) ores mined from the Ruth Au-Ag deposit, which is adjacent to the mill site. The Ruth Au-Ag deposit is hosted in Mesozoic intrusive rocks and is similar to other Au-Ag deposits in the western Mojave Desert that are associated with Miocene volcanic centers that formed on a basement of Mesozoic granitic rocks (Bateman, 1907; Gardner, 1954; Rytuba, 1996). The volcanic rocks consist of silicic domes and associated flows, pyroclastic rocks, and subvolcanic intrusions (fig. 2) that were emplaced into Mesozoic silicic intrusive rocks (Troxel and Morton, 1962). The Ruth Mine is on Federal land managed by the U.S. Bureau of Land Management (BLM). Tailings from the mine have been eroded and transported downstream into Homewood Canyon and then into Searles Valley (figs. 3, 4, 5, and 6). The BLM provided recreational facilities at the mine site for day-use hikers and restored and maintained the original mine buildings in collaboration with local citizen groups for use by visitors (fig. 7). The BLM requested that the U.S. Geological Survey (USGS), in collaboration with Chapman University, measure arsenic (As) and other geochemical constituents in soils and tailings at the mine site and in stream sediments downstream from the mine in Homewood Canyon and in Searles Valley (fig. 3). The request was made because initial sampling of the site by BLM staff indicated high concentrations of As in tailings and soils adjacent to the Ruth Mine. This report summarizes data obtained from field sampling of mine tailings and soils adjacent to the Ruth Mine and stream sediments downstream from the mine on June 7, 2009. Our results permit a preliminary assessment of the sources of As and associated chemical constituents that could potentially impact humans and biota.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr20111105","usgsCitation":"Rytuba, J.J., Kim, C., and Goldstein, D., 2011, Review of samples of tailings, soils, and stream sediments adjacent to and downstream from the Ruth Mine, Inyo County, California: U.S. Geological Survey Open-File Report 2011-1105, v, 37 p., https://doi.org/10.3133/ofr20111105.","productDescription":"v, 37 p.","numberOfPages":"37","onlineOnly":"Y","costCenters":[{"id":662,"text":"Western Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"links":[{"id":391590,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_95191.htm"},{"id":19264,"rank":200,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2011/1105/","linkFileType":{"id":5,"text":"html"}},{"id":116902,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr_2011_1105.gif"}],"country":"United States","state":"California","county":"Inyo County","otherGeospatial":"Ruth Mine","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -117.425,\n 35.8139\n ],\n [\n -117.3303,\n 35.8139\n ],\n [\n -117.3303,\n 35.9\n ],\n [\n -117.425,\n 35.9\n ],\n [\n -117.425,\n 35.8139\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4acce4b07f02db67e747","contributors":{"authors":[{"text":"Rytuba, James J. jrytuba@usgs.gov","contributorId":3043,"corporation":false,"usgs":true,"family":"Rytuba","given":"James","email":"jrytuba@usgs.gov","middleInitial":"J.","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":344567,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Kim, Christopher S.","contributorId":69258,"corporation":false,"usgs":true,"family":"Kim","given":"Christopher S.","affiliations":[],"preferred":false,"id":344568,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Goldstein, Daniel N.","contributorId":87671,"corporation":false,"usgs":true,"family":"Goldstein","given":"Daniel N.","affiliations":[],"preferred":false,"id":344569,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ]}