Zebra and quagga mussels are fresh water invaders that have the potential to \ncause severe ecological and economic damage. It is estimated that mussels cause $1 \nbillion dollars per year in damages to water infrastructure and industries in the \nUnited States (Pimentel et al., 2004). Following their introduction to the Great \nLakes in the late 1980s, mussels spread rapidly throughout the Mississippi River \nBasin and the Eastern U.S. The mussel invasion in the West is young. Mussels were \nfirst identified in Nevada in 2007, and have since been identified in California, \nArizona, Colorado, Utah, and Texas.
\nWestern water systems are very different from those found in the East. The \nrapid spread of mussels through the eastern system was facilitated by connected \nand navigable waterways. Western water systems are less connected and are \ncharacterized by man-made reservoirs and canals. The main vector of spread for \nmussels in the West is overland on recreational boats (Bossenbroek et al., 2001). In \nresponse to the invasion, many western water managers have implemented \npreventative management programs to slow the overland spread of mussels on \nrecreational boats. In Colorado, the Colorado Department of Wildlife (CDOW) has \nimplemented a mandatory boat inspection program that requires all trailered boats \nto be inspected before launching in any Colorado water body. The objective of this \nstudy is to analyze the costs and benefits of the CDOW boat inspection program in Colorado, and to identify variables that affect the net benefits of preventative \nmanagement.
\nPredicting the potential economic benefits of slowing the spread of mussels \nrequires integrating information about mussel dispersal potential with estimates of \ncontrol costs (Keller et al., 2009). Uncertainty surrounding the probabilities of \nestablishment, the timing of invasions, and the damage costs associated with an \ninvasion make a simulation model an excellent tool for addressing \"what if\" \nscenarios and shedding light on the net benefits of preventative management \nstrategies. This study builds a bioeconomic simulation model to predict and compare the expected economic costs of the CDOW boat inspection program ot the benefits of reduced expected control costs to water conveyance systems, hydropower generation stations, and minicipal water treatment facilities. The model is based on a case study water delivery and storage system, the Colorado-Big Thompson system. The Colorado-Big Thomspon system is an excellent example of water systems in the Rocky Mountain West. The system is nearly entirely man-made, with all of its reservoirs and delivery points connected via pipelines, tunnels, and canals. The structures and hydropower systems of the Colorado-Big Thompson system are common to other western storage and delivery systems, making the methods and insight developed from this case study transferal to other western systems.
\nThe model developed in this study contributes to the bioeconomic literature in several ways. Foremost, the model predicts the spread of dreissena mussels and associated damage costs for a connected water system in the Rocky Mountain West. Very few zebra mussel studies have focused on western water systems. Another distinguishing factor is the simultaneous consideration of spread from propagules introduced by boats and by flows. Most zebra mussel dispersal models consider boater movement patterns combined with limnological characteristics as predictors of spread. A separate set of studies have addressed mussel spread via downstream flows. To the author's knowledge, this is the first study that builds a zebra mussel spread model that specifically accounts for propagule pressure from boat introductions and from downstream flow introductions. By modeling an entire connected system, the study highlights how the spatial layout of a system, and the risk of invasion within a system affect the benefits of preventative management.
\nThis report is presented in five chapters. The first chapter provides background information including a history of the zebra mussel invasion in the U.S. and in the West, and details about the Colorado preventative management program and the Colorado-Big Thompson system. The chapter also includes a literature review of mussel dispersal models and economic studies that address control costs and preventative management for aquatic invasive species. Chapter 2 presents the methodological approach used to analyze the costs and benefits of preventative management in the Colorado-Big Thompson system and provides details of the bioeconomic simulation model used to predict invasion patterns and the net benefits of preventative management. Results of the analysis and sensitivity testing of model parameters are presented in Chapter 3. Chapter 4 provides a summary of the analysis and conclusions. A discussion of the limitations of the model and areas for future research is presented in Chapter 5.
","language":"English","publisher":"Colorado State University","publisherLocation":"Fort Collins, CO","usgsCitation":"Thomas, C.M., 2010, A cost-benefit analysis of preventative management for zebra and quagga mussels in the Colorado-Big Thompson System, xi, 185 p.","productDescription":"xi, 185 p.","numberOfPages":"194","costCenters":[],"links":[{"id":291487,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg","text":"https://pubs.er.usgs.gov/manager/#bibliodata-pane"},{"id":350426,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://dspace.library.colostate.edu/handle/10217/39343"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53db583fe4b0fba533fa355f","contributors":{"authors":[{"text":"Thomas, Catherine M. 0000-0001-8168-1271","orcid":"https://orcid.org/0000-0001-8168-1271","contributorId":29331,"corporation":false,"usgs":true,"family":"Thomas","given":"Catherine","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":497522,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70227366,"text":"70227366 - 2010 - A chronicle of Miocene extension near the Colorado Plateau-Basin and Range boundary, southern White Hills, northwestern Arizona: Paleogeographic and tectonic implications","interactions":[],"lastModifiedDate":"2022-01-11T14:54:06.238118","indexId":"70227366","displayToPublicDate":"2010-06-01T08:43:05","publicationYear":"2010","noYear":false,"publicationType":{"id":5,"text":"Book chapter"},"publicationSubtype":{"id":24,"text":"Book Chapter"},"title":"A chronicle of Miocene extension near the Colorado Plateau-Basin and Range boundary, southern White Hills, northwestern Arizona: Paleogeographic and tectonic implications","docAbstract":"In northwestern Arizona, the high-standing, relatively unextended Colorado Plateau abruptly gives way across a system of major west-dipping normal faults to a highly extended part of the Basin and Range province known as the northern Colorado River extensional corridor. The transition from unextended to highly extended upper crust is unusually sharp within this region, contrasting with a broad transition zone elsewhere. The southern White Hills lie near the eastern margin of the extensional corridor in northwestern Arizona and contain a large east-tilted half graben that chronicles Miocene extension and constrains the timing of structural demarcation between the Colorado Plateau and Basin and Range province during Neogene time. This growth-fault basin is bounded on the east by the west-dipping Cyclopic and Cerbat Mountains fault zones. Greater tilts in the hanging walls suggest that these faults have listric geometries. The stratigraphy in the half graben consists of Miocene vol canic rocks intercalated with an eastward-thickening wedge of synextensional fanglomerates. Tilts in the Miocene units decrease up section from ~75° to 5°. Recent 40Ar/39Ar dating (11 new dates) of variably tilted volcanic rocks in the growth-fault basin and regional relations constrain the timing of east-west extension between ca. 16.6 and <9 Ma, with peak extension from ca. 16.6 to 15.2 Ma. Capping 8.7 Ma basalts are tilted 5°–10° and record the waning stages of extension. Thus, the sharp boundary between the Colorado Plateau and Basin and Range began developing by ca. 16.5 Ma and has changed little since ca. 9 Ma. Major extension and basin development significantly lowered base level within the extensional corridor and induced headward erosion into the western margin of the Colorado Plateau, which ultimately facilitated development of the western Grand Canyon. Abundant clasts of 1.7 Ga megacrystic granite in the eastward-thickening fanglomerates within the growth-fault basin suggest a partial provenance from the Garnet Mountain area along or near the western margin of the Colorado Plateau beginning as early as ca. 16 Ma and continuing to ca. 9 Ma.
","largerWorkType":{"id":4,"text":"Book"},"largerWorkTitle":"Miocene tectonics of the Lake Mead Region, central basin and range","largerWorkSubtype":{"id":15,"text":"Monograph"},"language":"English","publisher":"Geological Society of America","doi":"10.1130/2010.2463(05)","usgsCitation":"Faulds, J., Price, L.M., Snee, L.W., and Gans, P.B., 2010, A chronicle of Miocene extension near the Colorado Plateau-Basin and Range boundary, southern White Hills, northwestern Arizona: Paleogeographic and tectonic implications, chap. of Miocene tectonics of the Lake Mead Region, central basin and range, p. 87-119, https://doi.org/10.1130/2010.2463(05).","productDescription":"33 p.","startPage":"87","endPage":"119","costCenters":[],"links":[{"id":394182,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Arizona","otherGeospatial":"southern White HIlls","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -114.4830322265625,\n 35.65729624809628\n ],\n [\n -113.8348388671875,\n 35.65729624809628\n ],\n [\n -113.8348388671875,\n 35.93798832265393\n ],\n [\n -114.4830322265625,\n 35.93798832265393\n ],\n [\n -114.4830322265625,\n 35.65729624809628\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Faulds, James E.","contributorId":252834,"corporation":false,"usgs":false,"family":"Faulds","given":"James E.","affiliations":[{"id":50442,"text":"Great Basin Center for Geothermal Energy, Nevada Bureau of Mines and Geology, University of Nevada, Reno","active":true,"usgs":false}],"preferred":false,"id":830608,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Price, Linda M.","contributorId":271055,"corporation":false,"usgs":false,"family":"Price","given":"Linda","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":830609,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Snee, Lawrence W.","contributorId":199028,"corporation":false,"usgs":false,"family":"Snee","given":"Lawrence","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":830610,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Gans, Philip B.","contributorId":66791,"corporation":false,"usgs":false,"family":"Gans","given":"Philip","email":"","middleInitial":"B.","affiliations":[{"id":30783,"text":"Department of Earth Science, University of California, Santa Barbara, CA","active":true,"usgs":false}],"preferred":false,"id":830611,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70156473,"text":"70156473 - 2010 - Coalbed methane resources of the Appalachian Basin, eastern USA","interactions":[],"lastModifiedDate":"2022-11-08T19:49:11.743877","indexId":"70156473","displayToPublicDate":"2010-06-01T00:00:00","publicationYear":"2010","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2033,"text":"International Journal of Coal Geology","active":true,"publicationSubtype":{"id":10}},"title":"Coalbed methane resources of the Appalachian Basin, eastern USA","docAbstract":"In 2002, the U.S. Geological Survey (USGS) assessed the technically recoverable, undiscovered coalbed-gas resources in the Appalachian basin and Black Warrior basin Assessment Provinces as about 15.5 trillion cubic feet. 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]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"554200cfe4b0a658d793b2f7","contributors":{"authors":[{"text":"Irani, Frederick M. firani@usgs.gov","contributorId":2932,"corporation":false,"usgs":true,"family":"Irani","given":"Frederick M.","email":"firani@usgs.gov","affiliations":[{"id":242,"text":"Eastern Geographic Science Center","active":true,"usgs":true}],"preferred":true,"id":545750,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Claggett, Peter R. 0000-0002-5335-2857 pclaggett@usgs.gov","orcid":"https://orcid.org/0000-0002-5335-2857","contributorId":176287,"corporation":false,"usgs":true,"family":"Claggett","given":"Peter","email":"pclaggett@usgs.gov","middleInitial":"R.","affiliations":[{"id":24708,"text":"Lower Mississippi-Gulf Water Science Center","active":true,"usgs":true},{"id":242,"text":"Eastern Geographic Science Center","active":true,"usgs":true}],"preferred":true,"id":545751,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70210253,"text":"70210253 - 2010 - Comparative analysis of Mourning Dove population change in North America","interactions":[],"lastModifiedDate":"2020-05-27T12:11:47.772599","indexId":"70210253","displayToPublicDate":"2010-05-26T14:00:55","publicationYear":"2010","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2508,"text":"Journal of Wildlife Management","active":true,"publicationSubtype":{"id":10}},"title":"Comparative analysis of Mourning Dove population change in North America","docAbstract":"Mourning doves (Zenaida macroura) are surveyed in North America with a Call-Count Survey (CCS) and the North American Breeding Bird Survey (BBS). Analyses in recent years have identified inconsistencies in results between surveys, and a need exists to analyze the surveys using modern methods and examine possible causes of differences in survey results. Call-Count Survey observers collect separate information on number of doves heard and number of doves seen during counting, whereas BBS observers record one index containing all doves observed. We used hierarchical log-linear models to estimate trend and annual indices of abundance for 1966–2007 from BBS data, CCS-heard data, and CCS-seen data. Trend estimates from analyses provided inconsistent results for several states and for eastern and central dovemanagement units. We examined differential effects of change in land use and noise-related disturbance on the CCS indices. Changes in noiserelated disturbance along CCS routes had a larger influence on the heard index than on the seen index, but association analyses among states of changes in temperature and of amounts of developed land suggest that CCS indices are differentially influenced by changes in these environmental features. Our hierarchical model should be used to estimate population change from dove surveys, because it provides an efficient framework for estimating population trends from dove indices while controlling for environmental features that differentially influence the indices.
","language":"English","publisher":"BioOne","doi":"10.2193/2008-459","usgsCitation":"Sauer, J.R., Link, W.A., Kendall, W.L., and Dolton, D., 2010, Comparative analysis of Mourning Dove population change in North America: Journal of Wildlife Management, v. 74, no. 5, p. 1059-1069, https://doi.org/10.2193/2008-459.","productDescription":"11 p.","startPage":"1059","endPage":"1069","costCenters":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":375039,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"74","issue":"5","noUsgsAuthors":false,"publicationDate":"2010-12-13","publicationStatus":"PW","contributors":{"authors":[{"text":"Sauer, John R. 0000-0002-4557-3019 jrsauer@usgs.gov","orcid":"https://orcid.org/0000-0002-4557-3019","contributorId":146917,"corporation":false,"usgs":true,"family":"Sauer","given":"John","email":"jrsauer@usgs.gov","middleInitial":"R.","affiliations":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"preferred":true,"id":789767,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Link, William A. 0000-0002-9913-0256 wlink@usgs.gov","orcid":"https://orcid.org/0000-0002-9913-0256","contributorId":146920,"corporation":false,"usgs":true,"family":"Link","given":"William","email":"wlink@usgs.gov","middleInitial":"A.","affiliations":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"preferred":true,"id":789768,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Kendall, William L. 0000-0003-0084-9891","orcid":"https://orcid.org/0000-0003-0084-9891","contributorId":204844,"corporation":false,"usgs":true,"family":"Kendall","given":"William","email":"","middleInitial":"L.","affiliations":[{"id":200,"text":"Coop Res Unit Seattle","active":true,"usgs":true}],"preferred":true,"id":789769,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Dolton, David D.","contributorId":100452,"corporation":false,"usgs":true,"family":"Dolton","given":"David D.","affiliations":[],"preferred":false,"id":789770,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":98404,"text":"sir20105011 - 2010 - Effects of surface-water diversion on streamflow, recharge, physical habitat, and temperature, Na Wai Eha, Maui, Hawai'i","interactions":[],"lastModifiedDate":"2024-01-09T23:05:03.443684","indexId":"sir20105011","displayToPublicDate":"2010-05-20T00:00:00","publicationYear":"2010","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":334,"text":"Scientific Investigations Report","code":"SIR","onlineIssn":"2328-0328","printIssn":"2328-031X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2010-5011","displayTitle":"Effects of Surface-Water Diversion on Streamflow, Recharge, Physical Habitat, and Temperature, Nā Wai 'Ehā, Maui, Hawai‘i","title":"Effects of surface-water diversion on streamflow, recharge, physical habitat, and temperature, Na Wai Eha, Maui, Hawai'i","docAbstract":"The perennial flow provided by Waihe‘e River, Waiehu Stream, ‘Īao Stream, and Waikapū Stream, collectively known as Nā Wai ‘Ehā (“The Four Streams”), made it possible for widespread agricultural activities to flourish in the eastern part of West Maui, Hawai‘i. The streams of the Nā Wai ‘Ehā area flow in their upper reaches even during extended dry-weather conditions because of persistent groundwater discharge to the streams. Overall, the lower reaches of these streams lose water, which may contribute to groundwater recharge.
During climate years 1984–2007 (when complete streamflow records were available for Waihe‘e River and ‘Īao Stream), Waihe‘e River had the greatest median flow of the four streams upstream of the uppermost diversion on each stream. The median flows, in million gallons per day, during climate years 1984–2007 were: 34 for Waihe‘e River near an altitude of 605 feet; 25 for ‘Īao Stream near an altitude of 780 feet; and estimated to be 4.3 for Waikapū Stream near an altitude of 1,160 feet; 3.2 for North Waiehu Stream near an altitude of 880 feet; and 3.2 for South Waiehu Stream near an altitude of 870 feet. Existing stream diversions in the Nā Wai ‘Ehā area have a combined capacity exceeding at least 75 million gallons per day and are capable of diverting all or nearly all of the dry-weather flows of these streams, leaving some downstream reaches dry. Hourly photographs collected during 2006–2008 indicate that some stream reaches downstream of diversions are dry more than 50 percent of the time. Many of these reaches would be perennial or nearly perennial in the absence of diversions.
A lack of sufficient streamflow downstream of existing diversions has led to recent conflicts between those currently diverting or using the water and those desiring sufficient instream flows for protection of traditional and customary Hawaiian rights (including the cultivation of taro), maintenance of habitat for native stream fauna, recreation, aesthetics, and groundwater recharge from loss of water through the streambed. In response to a need for additional information, the U.S. Geological Survey (USGS) undertook the present investigation to characterize the effects of existing surface-water diversions on (1) streamflow, (2) potential groundwater recharge from the streams to the underlying groundwater body, (3) physical habitat for native stream fauna (fish, shrimp, and snails), and (4) instream temperatures.
Information collected for this study includes discharge measurements under different streamflow conditions to characterize streamflow and seepage losses, hourly photographs of stream conditions from mounted cameras, snorkel surveys of stream fauna, measurements of microhabitat (depth, velocity, and substrate) under different flow conditions, and measurements of water temperatures. Families of curves were developed to show the relations between surface-water diversion intake capacity (the maximum rate that an intake can divert) and (1) selected duration discharges for sites near the coast; (2) selected duration discharges for the diversions; (3) groundwater-recharge reduction; and (4) physical-habitat reduction for native stream fauna. These curves may be used by water managers to evaluate the effects of different diversion intake capacities on streamflow, water available for offstream use, groundwater recharge, and habitat for native stream fauna.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/sir20105011","collaboration":"Prepared in Cooperation with the County of Maui Office of Economic Development, County of Maui Department of Water Supply, State of Hawai`i Commission on Water Resource Management, State of Hawai`i Office of Hawaiian Affairs","usgsCitation":"Oki, D.S., Wolff, R.H., and Perreault, J.A., 2010, Effects of surface-water diversion on streamflow, recharge, physical habitat, and temperature, Na Wai Eha, Maui, Hawai'i: U.S. Geological Survey Scientific Investigations Report 2010-5011, Report: xviii, 138 p.; Table Folder, https://doi.org/10.3133/sir20105011.","productDescription":"Report: xviii, 138 p.; Table Folder","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[{"id":525,"text":"Pacific Islands Water Science Center","active":true,"usgs":true}],"links":[{"id":424247,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_93243.htm","linkFileType":{"id":5,"text":"html"}},{"id":13655,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2010/5011/","linkFileType":{"id":5,"text":"html"}},{"id":125402,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2010_5011.jpg"}],"scale":"24000","country":"United States","state":"Hawaii","otherGeospatial":"Maui, Nā Wai ‘Ehā","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -156.61734491035466,\n 20.77964772031042\n ],\n [\n -156.6117081382047,\n 20.984212083071995\n ],\n [\n -156.45681014971802,\n 20.982896272637973\n ],\n [\n -156.45365279711842,\n 20.774040548992517\n ],\n [\n -156.61734491035466,\n 20.77964772031042\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4ae4b07f02db624b9f","contributors":{"authors":[{"text":"Oki, Delwyn S. 0000-0002-6913-8804 dsoki@usgs.gov","orcid":"https://orcid.org/0000-0002-6913-8804","contributorId":1901,"corporation":false,"usgs":true,"family":"Oki","given":"Delwyn","email":"dsoki@usgs.gov","middleInitial":"S.","affiliations":[{"id":525,"text":"Pacific Islands Water Science Center","active":true,"usgs":true}],"preferred":true,"id":305217,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wolff, Reuben H.","contributorId":35020,"corporation":false,"usgs":true,"family":"Wolff","given":"Reuben","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":305218,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Perreault, Jeff A.","contributorId":333052,"corporation":false,"usgs":false,"family":"Perreault","given":"Jeff","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":305219,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":98388,"text":"sir20105076 - 2010 - Polychlorinated Biphenyls in suspended-sediment samples from outfalls to Meandering Road Creek at Air Force Plant 4, Fort Worth, Texas, 2003-08","interactions":[],"lastModifiedDate":"2016-08-11T16:32:48","indexId":"sir20105076","displayToPublicDate":"2010-05-15T00:00:00","publicationYear":"2010","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":334,"text":"Scientific Investigations Report","code":"SIR","onlineIssn":"2328-0328","printIssn":"2328-031X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2010-5076","title":"Polychlorinated Biphenyls in suspended-sediment samples from outfalls to Meandering Road Creek at Air Force Plant 4, Fort Worth, Texas, 2003-08","docAbstract":"Meandering Road Creek is an intermittent stream and tributary to Lake Worth, a reservoir on the West Fork Trinity River on the western edge of Fort Worth, Texas. U.S. Air Force Plant 4 (AFP4) is on the eastern shore of Woods Inlet, an arm of Lake Worth. Meandering Road Creek gains inflow from several stormwater outfalls as it flows across AFP4. Several studies have characterized polychlorinated biphenyls (PCBs) in the water and sediments of Lake Worth and Meandering Road Creek; sources of PCBs are believed to originate primarily from AFP4. Two previous U.S. Geological Survey (USGS) reports documented elevated PCB concentrations in surficial sediment samples from Woods Inlet relative to concentrations in surficial sediment samples from other parts of Lake Worth. The second of these two previous reports also identified some of the sources of PCBs to Lake Worth. These reports were followed by a third USGS report that documented the extent of PCB contamination in Meandering Road Creek and Woods Inlet and identified runoff from outfalls 4 and 5 at AFP4 as prominent sources of these PCBs. This report describes the results of a fourth study by the USGS, in cooperation with the Lockheed Martin Corporation, to investigate PCBs in suspended-sediment samples in storm runoff from outfalls 4 and 5 at AFP4 following the implementation of engineering controls designed to potentially alleviate PCB contamination in the drainage areas of these outfalls. Suspended-sediment samples collected from outfalls 4 and 5 during storms on March 2 and November 10, 2008, were analyzed for selected PCBs. Sums of concentrations of 18 reported PCB congeners (Sigma PCBc) in suspended-sediment samples collected before and after implementation of engineering controls are compared. At both outfalls, the Sigma PCBc before engineering controls was higher than the Sigma PCBc after engineering controls. The Sigma PCBc in suspended-sediment samples collected at AFP4 before and after implementation of engineering controls also is compared to the threshold effect concentration (TEC), the concentration below which adverse effects to benthic biota rarely occur. Sigma PCBc exceeded the TEC for 75 percent of the samples collected at outfall 4 and 67 percent of the samples collected at outfall 5 before the implementation of engineering controls. Sigma PCBc did not exceed the TEC in samples collected at either outfall 4 or outfall 5 after the implementation of engineering controls. The relative prominence of 10 selected PCB congeners was evaluated by graphical analysis of ratios of individual concentrations of the 10 PCB congeners to the sum of these PCB congeners. An overall decrease in concentrations of PCB congeners at outfalls 4 and 5 after implementation of engineering controls, as well as a shift in prominence from lighter, less chlorinated congeners to a heavier, more chlorinated congener might have resulted from the implementation of engineering controls. Because of the small number of samples collected and lack of runoff and precipitation data to evaluate comparability of sampling conditions before and after implementation of engineering controls, all conclusions are preliminary.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, Virginia","doi":"10.3133/sir20105076","collaboration":"In cooperation with the Lockheed Martin Corporation","usgsCitation":"Braun, C.L., and Wilson, J.T., 2010, Polychlorinated Biphenyls in suspended-sediment samples from outfalls to Meandering Road Creek at Air Force Plant 4, Fort Worth, Texas, 2003-08: U.S. Geological Survey Scientific Investigations Report 2010-5076, vi, 20 p. , https://doi.org/10.3133/sir20105076.","productDescription":"vi, 20 p. ","onlineOnly":"N","additionalOnlineFiles":"N","temporalStart":"2008-03-02","temporalEnd":"2010-11-10","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":126290,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2010_5076.jpg"},{"id":13639,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2010/5076/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Texas","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -97.45083333333334,32.75 ], [ -97.45083333333334,32.78388888888889 ], [ -97.40138888888889,32.78388888888889 ], [ -97.40138888888889,32.75 ], [ -97.45083333333334,32.75 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad5e4b07f02db683992","contributors":{"authors":[{"text":"Braun, Christopher L. 0000-0002-5540-2854 clbraun@usgs.gov","orcid":"https://orcid.org/0000-0002-5540-2854","contributorId":925,"corporation":false,"usgs":true,"family":"Braun","given":"Christopher","email":"clbraun@usgs.gov","middleInitial":"L.","affiliations":[{"id":48595,"text":"Oklahoma-Texas Water Science Center","active":true,"usgs":true}],"preferred":true,"id":305158,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wilson, Jennifer T. 0000-0003-4481-6354 jenwilso@usgs.gov","orcid":"https://orcid.org/0000-0003-4481-6354","contributorId":1782,"corporation":false,"usgs":true,"family":"Wilson","given":"Jennifer","email":"jenwilso@usgs.gov","middleInitial":"T.","affiliations":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"preferred":true,"id":305159,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":98378,"text":"sir20095256 - 2010 - Outcrops, fossils, geophysical logs, and tectonic interpretations of the Upper Cretaceous Frontier Formation and contiguous strata in the Bighorn Basin, Wyoming and Montana","interactions":[],"lastModifiedDate":"2023-01-09T22:59:55.116163","indexId":"sir20095256","displayToPublicDate":"2010-05-13T00:00:00","publicationYear":"2010","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":334,"text":"Scientific Investigations Report","code":"SIR","onlineIssn":"2328-0328","printIssn":"2328-031X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2009-5256","title":"Outcrops, fossils, geophysical logs, and tectonic interpretations of the Upper Cretaceous Frontier Formation and contiguous strata in the Bighorn Basin, Wyoming and Montana","docAbstract":"In the Bighorn Basin of north-central Wyoming and south-central Montana, the Frontier Formation of early Late Cretaceous age consists of siliciclastic, bentonitic, and carbonaceous beds that were deposited in marine, brackish-water, and continental environments. Most lithologic units are laterally discontinuous. The Frontier Formation conformably overlies the Mowry Shale and is conformably overlain by the Cody Shale. Molluscan fossils collected from outcrops of these formations and listed in this report are mainly of marine origin and of Cenomanian, Turonian, and Coniacian ages. \r\n\r\nThe lower and thicker part of the Frontier in the Bighorn Basin is of Cenomanian age and laterally equivalent to the Belle Fourche Member of the Frontier in central Wyoming. Near the west edge of the basin, these basal strata are disconformably overlain by middle Turonian beds that are the age equivalent of the Emigrant Gap Member of the Frontier in central Wyoming. The middle Turonian beds are disconformably overlain by lower Coniacian strata. Cenomanian strata along the south and east margins of the basin are disconformably overlain by upper Turonian beds in the upper part of the Frontier, as well as in the lower part of the Cody; these are, in turn, conformably overlain by lower Coniacian strata. \r\n\r\nThicknesses and ages of Cenomanian strata in the Bighorn Basin and adjoining regions are evidence of regional differential erosion and the presence of an uplift during the early Turonian centered in northwestern Wyoming, west of the basin, probably associated with a eustatic event. The truncated Cenomanian strata were buried by lower middle Turonian beds during a marine transgression and possibly during regional subsidence and a eustatic rise. An uplift in the late middle Turonian, centered in north-central Wyoming and possibly associated with a eustatic fall, caused the erosion of lower middle Turonian beds in southern and eastern areas of the basin as well as in an adjoining region of north-central Wyoming. Similarly, in east-central Wyoming and an adjacent area to the south, Cenomanian strata are disconformably overlain by upper middle and lower upper Turonian strata that probably reflect uplift and erosion in that region during the interim period of middle Turonian time. \r\n\r\nDuring later subsidence and a marine transgression, upper Turonian deposits buried Cenomanian beds in areas along the south and east margins of the Bighorn Basin and buried lower middle Turonian beds in much of northern Wyoming. Upper Turonian and lower Coniacian strata are apparently conformable in eastern and southern areas of the basin as well as near Riverton, Kaycee, and Casper in central Wyoming. Upper Turonian strata are absent on the west flank of the Bighorn Basin and in outcrops west of the basin, where middle Turonian beds are disconformably overlain by lower Coniacian beds . The conformable upper Turonian and lower Coniacian beds apparently transgressed an eroded middle Turonian surface in the region, but only Coniacian strata overlie middle Turonian beds on the west side of the basin and areas farther west. Coniacian strata onlap the truncated lower middle Turonian surface west of the basin, indicating a region that had higher elevation possibly resulting from tectonic uplift. \r\n\r\nIn east-central Wyoming and an adjoining region to the south, upper middle Turonian and lower upper Turonian strata are disconformably overlain by lower and middle Coniacian beds. That region apparently was uplifted and eroded during the latest Turonian.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/sir20095256","usgsCitation":"Merewether, E., Cobban, W.A., and Tillman, R.W., 2010, Outcrops, fossils, geophysical logs, and tectonic interpretations of the Upper Cretaceous Frontier Formation and contiguous strata in the Bighorn Basin, Wyoming and Montana: U.S. Geological Survey Scientific Investigations Report 2009-5256, iv, 49 p., https://doi.org/10.3133/sir20095256.","productDescription":"iv, 49 p.","onlineOnly":"N","costCenters":[{"id":164,"text":"Central Energy Resources Science Center","active":true,"usgs":true}],"links":[{"id":125393,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2009_5256.jpg"},{"id":411600,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_93117.htm","linkFileType":{"id":5,"text":"html"}},{"id":13628,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2009/5256/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Montana, Wyoming","otherGeospatial":"Big Horn Basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -109.3942,\n 43.3822\n ],\n [\n -109.3942,\n 45.5033\n ],\n [\n -107.75,\n 45.5033\n ],\n [\n -107.75,\n 43.3822\n ],\n [\n -109.3942,\n 43.3822\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae4e4b07f02db68a385","contributors":{"authors":[{"text":"Merewether, E.A.","contributorId":32517,"corporation":false,"usgs":true,"family":"Merewether","given":"E.A.","affiliations":[],"preferred":false,"id":305131,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Cobban, W. A.","contributorId":21577,"corporation":false,"usgs":true,"family":"Cobban","given":"W.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":305130,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Tillman, R. W.","contributorId":88848,"corporation":false,"usgs":true,"family":"Tillman","given":"R.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":305132,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":98380,"text":"sir20095267 - 2010 - Methods for estimating flow-duration and annual mean-flow statistics for ungaged streams in Oklahoma","interactions":[],"lastModifiedDate":"2012-12-17T09:21:20","indexId":"sir20095267","displayToPublicDate":"2010-05-13T00:00:00","publicationYear":"2010","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":334,"text":"Scientific Investigations Report","code":"SIR","onlineIssn":"2328-0328","printIssn":"2328-031X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2009-5267","title":"Methods for estimating flow-duration and annual mean-flow statistics for ungaged streams in Oklahoma","docAbstract":"Flow statistics can be used to provide decision makers with surface-water information needed for activities such as water-supply permitting, flow regulation, and other water rights issues. Flow statistics could be needed at any location along a stream. Most often, streamflow statistics are needed at ungaged sites, where no flow data are available to compute the statistics. Methods are presented in this report for estimating flow-duration and annual mean-flow statistics for ungaged streams in Oklahoma. \n\nFlow statistics included the (1) annual (period of record), (2) seasonal (summer-autumn and winter-spring), and (3) 12 monthly duration statistics, including the 20th, 50th, 80th, 90th, and 95th percentile flow exceedances, and the annual mean-flow (mean of daily flows for the period of record). Flow statistics were calculated from daily streamflow information collected from 235 streamflow-gaging stations throughout Oklahoma and areas in adjacent states.\n\nA drainage-area ratio method is the preferred method for estimating flow statistics at an ungaged location that is on a stream near a gage. The method generally is reliable only if the drainage-area ratio of the two sites is between 0.5 and 1.5. \n\nRegression equations that relate flow statistics to drainage-basin characteristics were developed for the purpose of estimating selected flow-duration and annual mean-flow statistics for ungaged streams that are not near gaging stations on the same stream. Regression equations were developed from flow statistics and drainage-basin characteristics for 113 unregulated gaging stations. \n\nSeparate regression equations were developed by using U.S. Geological Survey streamflow-gaging stations in regions with similar drainage-basin characteristics. These equations can increase the accuracy of regression equations used for estimating flow-duration and annual mean-flow statistics at ungaged stream locations in Oklahoma. Streamflow-gaging stations were grouped by selected drainage-basin characteristics by using a k-means cluster analysis. Three regions were identified for Oklahoma on the basis of the clustering of gaging stations and a manual delineation of distinguishable hydrologic and geologic boundaries: Region 1 (western Oklahoma excluding the Oklahoma and Texas Panhandles), Region 2 (north- and south-central Oklahoma), and Region 3 (eastern and central Oklahoma). \n\nA total of 228 regression equations (225 flow-duration regressions and three annual mean-flow regressions) were developed using ordinary least-squares and left-censored (Tobit) multiple-regression techniques. These equations can be used to estimate 75 flow-duration statistics and annual mean-flow for ungaged streams in the three regions. Drainage-basin characteristics that were statistically significant independent variables in the regression analyses were (1) contributing drainage area; (2) station elevation; (3) mean drainage-basin elevation; (4) channel slope; (5) percentage of forested canopy; (6) mean drainage-basin hillslope; (7) soil permeability; and (8) mean annual, seasonal, and monthly precipitation. \n\nThe accuracy of flow-duration regression equations generally decreased from high-flow exceedance (low-exceedance probability) to low-flow exceedance (high-exceedance probability) . This decrease may have happened because a greater uncertainty exists for low-flow estimates and low-flow is largely affected by localized geology that was not quantified by the drainage-basin characteristics selected.\n\nThe standard errors of estimate of regression equations for Region 1 (western Oklahoma) were substantially larger than those standard errors for other regions, especially for low-flow exceedances. These errors may be a result of greater variability in low flow because of increased irrigation activities in this region.\n\nRegression equations may not be reliable for sites where the drainage-basin characteristics are outside the range of values of independent vari","language":"ENGLISH","publisher":"U.S. Geological Survey","doi":"10.3133/sir20095267","collaboration":"Prepared in cooperation with the Oklahoma Water Resources Board","usgsCitation":"Esralew, R.A., and Smith, S.J., 2010, Methods for estimating flow-duration and annual mean-flow statistics for ungaged streams in Oklahoma: U.S. Geological Survey Scientific Investigations Report 2009-5267, vi, 53 p.; Tables, https://doi.org/10.3133/sir20095267.","productDescription":"vi, 53 p.; Tables","onlineOnly":"N","costCenters":[{"id":516,"text":"Oklahoma Water Science Center","active":true,"usgs":true}],"links":[{"id":125390,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2009_5267.jpg"},{"id":13630,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2009/5267/","linkFileType":{"id":5,"text":"html"}}],"geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -103.66666666666667,34 ], [ -103.66666666666667,38 ], [ -94,38 ], [ -94,34 ], [ -103.66666666666667,34 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4acce4b07f02db67e80d","contributors":{"authors":[{"text":"Esralew, Rachel A.","contributorId":104862,"corporation":false,"usgs":true,"family":"Esralew","given":"Rachel","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":305136,"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":305135,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":98371,"text":"ofr20091268 - 2010 - Temporal chemical data for sediment, water, and biological samples from the Lava Cap Mine Superfund site, Nevada County, California— 2006–2008","interactions":[],"lastModifiedDate":"2021-08-31T21:28:00.198834","indexId":"ofr20091268","displayToPublicDate":"2010-05-08T00:00:00","publicationYear":"2010","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2009-1268","title":"Temporal chemical data for sediment, water, and biological samples from the Lava Cap Mine Superfund site, Nevada County, California— 2006–2008","docAbstract":"The Lava Cap Mine is located about 6 km east of the city of Grass Valley, Nevada County, California, at an elevation of about 900 m. Gold was hosted in quartz-carbonate veins typical of the Sierran Gold Belt, but the gold grain size was smaller and the abundance of sulfide minerals higher than in typical deposits. The vein system was discovered in 1860, but production was sporadic until the 1930s when two smaller operations on the site were consolidated, a flotation mill was built, and a 100-foot deep adit was driven to facilitate drainage and removal of water from the mine workings, which extended to 366 m. Peak production at the Lava Cap occurred between 1934 and 1943, when about 90,000 tons of ore per year were processed. To facilitate removal of the gold and accessory sulfide minerals, the ore was crushed to a very fine sand or silt grain size for processing. Mining operations at Lava Cap ceased in June 1943 due to War Production Board Order L-208 and did not resume after the end of World War II.
Two tailings retention structures were built at the Lava Cap Mine. The first was a log dam located about 0.4 km below the flotation mill on Little Clipper Creek, and the second, built in 1938, was a larger earth fill and rip-rap structure constructed about 2 km downstream, which formed the water body now called Lost Lake. The log dam failed during a storm that began on December 31, 1996, and continued into January 1997; an estimated 8,000-10,000 m3 of tailings were released into Little Clipper Creek during this event. Most of the fine tailings were deposited in Lost Lake, dramatically increasing its turbidity and resulting in a temporary 1-1.5 m rise in lake level due to debris blocking the dam spillway. When the blockage was cleared, the lake level quickly lowered, leaving a \"bathtub ring\" of very fine tailings deposited substantially above the water line. The U.S. Environmental Protection Agency (EPA) initiated emergency action in late 1997 at the mine site to reduce the possibility of future movement of tailings, and began an assessment of the risks posed by physical and chemical hazards at the site.
The EPA's assessment identified arsenic (As) as the primary hazard of concern. Three main exposure routes were identified: inhalation/ingestion of mine tailings, dermal absorption/ingestion of As in lake water from swimming, and ingestion of As-contaminated ground water or surface water. Lost Lake is a private lake which is completely surrounded by low-density residential development. Prior to the dam failure, the lake was used by the local residents for swimming and boating. An estimated 1,776 people reside within one mile of the lake, and almost all residents of the area use potable groundwater for domestic use. Risk factors for human exposure to As derived from mine wastes were high enough to merit placement of the mine site and surrounding area on the National Priority List (commonly called \"Superfund\").
The Lava Cap Mine Superfund site (LCMS) encompasses approximately 33 acres that include the mine site, the stretch of Little Clipper Creek between the mine and Lost Lake, the lake itself, and the area between the lake and the confluence of Little Clipper Creek with its parent stream, Clipper Creek. The area between the two creeks is named the \"deposition area\" due to the estimated 24 m thick layer of tailings that were laid down there during and after active mining. The lobate structure of Lost Lake is also due to deposition in this area. The deposition area and Lost Lake are together estimated to contain 382,277 m3 of tailings.
The primary goals of the EPA have been to minimize tailings movement downstream of Lost Lake and to ensure that residents in the area have drinking water that meets national water quality standards. EPA has officially decided to construct a public water supply line to deliver safe water to affected residences, since some residential wells in the area have As concentrations above the current drinking water standard (10 ppb). However, some deeper monitoring wells in the deposition
area have As concentrations that are as much as 100 times the As drinking water standard (EPA, 2001). Fracture-dominated groundwater flowpaths complicate measurement of the rate and direction of groundwater flow in the area. Investigations of groundwater movement at the LCMS are planned by the EPA, but have not been undertaken at the time of this writing.
Pollen analysis of two cores with discontinuous records from a peat bog near Girdwood, in south-central Alaska, provides the basis for reconstructing the first radiocarbon-dated outline of postglacial history of vegetation in the upper Turnagain Arm area of Cook Inlet. Pollen data from clayey silt underlying peat at one site indicate that the earliest known vegetation in the Girdwood area was shrub–herb tundra. Tundra vegetation developed by ∼13 800 cal years BP, soon after local retreat of glacial ice from the maximum position of the Elmendorf glacial advance (∼15 000 – 11 000 cal years BP). By ∼10 900 cal years BP, the tundra vegetation became shrubbier as Betula nana, Salix, and Ericales increased, and scattered Alnus shrubs began to colonize Turnagain Arm. By ∼9600 cal years BP, Alnus thickets with Polypodiaceae ferns became the dominant vegetation. By ∼6600 cal years BP, birch trees (Betula neoalaskana, B. kenaica) from the Anchorage and Kenai lowlands began to spread eastward into eastern Turnagain Arm. Mountain hemlock (Tsuga mertensiana) began to colonize the Girdwood area by ∼3400 cal years BP, followed soon after by Sitka spruce (Picea sitchensis), both Pacific coastal forest species that spread westward from Prince William Sound after a long migration from southeastern Alaska. For at least the past 2700 cal years, Pacific coastal forest composed mostly of Tsuga mertensiana, Picea sitchensis, and Alnus has been the dominant vegetation of eastern Turnagain Arm.
","language":"English","publisher":"Canadian Science Publishing","doi":"10.1139/E10-020","usgsCitation":"Ager, T.A., Carrara, P.E., and McGeehin, J., 2010, Ecosystem development in the Girdwood area, south-central Alaska, following late Wisconsin glaciation: Canadian Journal of Earth Sciences, v. 47, no. 7, p. 971-985, https://doi.org/10.1139/E10-020.","productDescription":"15 p.","startPage":"971","endPage":"985","costCenters":[{"id":318,"text":"Geosciences and Environmental Change Science Center","active":true,"usgs":true}],"links":[{"id":374502,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"Girdwood south-central Alaska","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -152.0068359375,\n 60.457217797743944\n ],\n [\n -148.0517578125,\n 60.457217797743944\n ],\n [\n -148.0517578125,\n 61.85614879566797\n ],\n [\n -152.0068359375,\n 61.85614879566797\n ],\n [\n -152.0068359375,\n 60.457217797743944\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"47","issue":"7","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Ager, T. A.","contributorId":88386,"corporation":false,"usgs":true,"family":"Ager","given":"T.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":788604,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Carrara, Paul E. pcarrara@usgs.gov","contributorId":1342,"corporation":false,"usgs":true,"family":"Carrara","given":"Paul","email":"pcarrara@usgs.gov","middleInitial":"E.","affiliations":[{"id":318,"text":"Geosciences and Environmental Change Science Center","active":true,"usgs":true}],"preferred":true,"id":788605,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"McGeehin, John mcgeehin@usgs.gov","contributorId":167455,"corporation":false,"usgs":true,"family":"McGeehin","given":"John","email":"mcgeehin@usgs.gov","affiliations":[{"id":242,"text":"Eastern Geographic Science Center","active":true,"usgs":true},{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true}],"preferred":true,"id":788606,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70044293,"text":"70044293 - 2010 - Fluvial processes and vegetation - Glimpses of the past, the present, and perhaps the future.","interactions":[],"lastModifiedDate":"2019-08-27T08:01:24","indexId":"70044293","displayToPublicDate":"2010-05-01T00:00:00","publicationYear":"2010","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1801,"text":"Geomorphology","active":true,"publicationSubtype":{"id":10}},"title":"Fluvial processes and vegetation - Glimpses of the past, the present, and perhaps the future.","docAbstract":"\"Most research before 1960 into interactions among fluvial processes, resulting landforms, and vegetation was descriptive. Since then, however, research has become more detailed and quantitative permitting numerical modeling and applications including agricultural-erosion abatement and rehabilitation of altered\nbottomlands. Although progress was largely observational, the empiricism increasingly yielded to objective recognition of how vegetation interacts with and influences geomorphic process. A review of advances relating fluvial processes and vegetation during the last 50 years centers on hydrologic reconstructions from\ntree rings, plant indicators of flow- and flood-frequency parameters, hydrologic controls on plant species, regulation of sediment movement by vegetation, vegetative controls on mass movement, and relations between plant cover and sediment movement. Extension of present studies of vegetation as a regulator of bottomland hydrologic and geomorphic processes may become markedly more sophisticated and widespread than at present. Research emphases that are\nlikely to continue include vegetative considerations for erosion modeling, response of riparian-zone forests to disturbance such as dams and water diversion, the effect of vegetation on channel and bottomland dynamics, and rehabilitation of stream corridors. Research topics that presently are receiving attention are the effect of woody vegetation on the roughness of stream corridors and, hence, processes of flood conveyance and flood-plain sedimentation, the development of a theoretical basis for rehabilitation projects as opposed to fully empirical approaches, the effect of invasive plant species on the dynamics of bottomland vegetation, the quantification of below-surface biomass and related soil-stability factors for use in erosion prediction models, and the effect of impoundments on downstream narrowing of channels and accompanying encroachment of vegetation. Bottomland vegetation partially controls and is controlled by fluvial-geomorphic processes. The purposes of this paper are to identify and review investigations that have related vegetation to bottomland features and\nprocesses, to distinguish the present status of these investigations, and to anticipate future research into how hydrologic and fluvial-geomorphic processes of bottomlands interact with vegetation.\"","language":"English","publisher":"Elsevier","doi":"10.1016/j.geomorph.2009.11.018","usgsCitation":"Osterkamp, W.R., and Hupp, C.R., 2010, Fluvial processes and vegetation - Glimpses of the past, the present, and perhaps the future.: Geomorphology, v. 116, p. 274-285, https://doi.org/10.1016/j.geomorph.2009.11.018.","productDescription":"12 p.","startPage":"274","endPage":"285","numberOfPages":"12","ipdsId":"IP-013235","costCenters":[{"id":436,"text":"National Research Program - Eastern Branch","active":true,"usgs":true}],"links":[{"id":270789,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":270788,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1016/j.geomorph.2009.11.018"}],"country":"United States","volume":"116","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"516689e3e4b0bba30b388bda","contributors":{"authors":[{"text":"Osterkamp, Waite R.","contributorId":8505,"corporation":false,"usgs":true,"family":"Osterkamp","given":"Waite","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":475247,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hupp, Cliff R. 0000-0003-1853-9197 crhupp@usgs.gov","orcid":"https://orcid.org/0000-0003-1853-9197","contributorId":2344,"corporation":false,"usgs":true,"family":"Hupp","given":"Cliff","email":"crhupp@usgs.gov","middleInitial":"R.","affiliations":[{"id":436,"text":"National Research Program - Eastern Branch","active":true,"usgs":true},{"id":37277,"text":"WMA - Earth System Processes Division","active":true,"usgs":true}],"preferred":true,"id":475246,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":98351,"text":"sir20095250 - 2010 - Techniques for Estimating the Magnitude and Frequency of Peak Flows on Small Streams in Minnesota Based on Data through Water Year 2005","interactions":[],"lastModifiedDate":"2012-03-08T17:16:29","indexId":"sir20095250","displayToPublicDate":"2010-04-28T00:00:00","publicationYear":"2010","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":334,"text":"Scientific Investigations Report","code":"SIR","onlineIssn":"2328-0328","printIssn":"2328-031X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2009-5250","title":"Techniques for Estimating the Magnitude and Frequency of Peak Flows on Small Streams in Minnesota Based on Data through Water Year 2005","docAbstract":"Knowledge of the peak flow of floods of a given recurrence interval is essential for regulation and planning of water resources and for design of bridges, culverts, and dams along Minnesota's rivers and streams. Statistical techniques are needed to estimate peak flow at ungaged sites because long-term streamflow records are available at relatively few places. Because of the need to have up-to-date peak-flow frequency information in order to estimate peak flows at ungaged sites, the U.S. Geological Survey (USGS) conducted a peak-flow frequency study in cooperation with the Minnesota Department of Transportation and the Minnesota Pollution Control Agency.\r\n\r\nEstimates of peak-flow magnitudes for 1.5-, 2-, 5-, 10-, 25-, 50-, 100-, and 500-year recurrence intervals are presented for 330 streamflow-gaging stations in Minnesota and adjacent areas in Iowa and South Dakota based on data through water year 2005. The peak-flow frequency information was subsequently used in regression analyses to develop equations relating peak flows for selected recurrence intervals to various basin and climatic characteristics. Two statistically derived techniques-regional regression equation and region of influence regression-can be used to estimate peak flow on ungaged streams smaller than 3,000 square miles in Minnesota. Regional regression equations were developed for selected recurrence intervals in each of six regions in Minnesota: A (northwestern), B (north central and east central), C (northeastern), D (west central and south central), E (southwestern), and F (southeastern). The regression equations can be used to estimate peak flows at ungaged sites. The region of influence regression technique dynamically selects streamflow-gaging stations with characteristics similar to a site of interest. Thus, the region of influence regression technique allows use of a potentially unique set of gaging stations for estimating peak flow at each site of interest. Two methods of selecting streamflow-gaging stations, similarity and proximity, can be used for the region of influence regression technique.\r\n\r\nThe regional regression equation technique is the preferred technique as an estimate of peak flow in all six regions for ungaged sites. The region of influence regression technique is not appropriate for regions C, E, and F because the interrelations of some characteristics of those regions do not agree with the interrelations throughout the rest of the State. Both the similarity and proximity methods for the region of influence technique can be used in the other regions (A, B, and D) to provide additional estimates of peak flow. The peak-flow-frequency estimates and basin characteristics for selected streamflow-gaging stations and regional peak-flow regression equations are included in this report.\r\n","language":"ENGLISH","publisher":"U.S. Geological Survey","doi":"10.3133/sir20095250","collaboration":"Prepared in cooperation with the Minnesota Department of Transportation and the Minnesota Pollution Control Agency","usgsCitation":"Lorenz, D.L., Sanocki, C.A., and Kocian, M.J., 2010, Techniques for Estimating the Magnitude and Frequency of Peak Flows on Small Streams in Minnesota Based on Data through Water Year 2005: U.S. Geological Survey Scientific Investigations Report 2009-5250, iv, 54 p. , https://doi.org/10.3133/sir20095250.","productDescription":"iv, 54 p. ","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science Center","active":true,"usgs":true}],"links":[{"id":125896,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2009_5250.jpg"},{"id":13600,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2009/5250/","linkFileType":{"id":5,"text":"html"}}],"projection":"Universal Transverse Mercator","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -98,43 ], [ -98,50 ], [ -89,50 ], [ -89,43 ], [ -98,43 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adbe4b07f02db6860bb","contributors":{"authors":[{"text":"Lorenz, David L. 0000-0003-3392-4034 lorenz@usgs.gov","orcid":"https://orcid.org/0000-0003-3392-4034","contributorId":1384,"corporation":false,"usgs":true,"family":"Lorenz","given":"David","email":"lorenz@usgs.gov","middleInitial":"L.","affiliations":[{"id":392,"text":"Minnesota Water Science Center","active":true,"usgs":true}],"preferred":true,"id":305057,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Sanocki, Christopher A. 0000-0001-6714-5421 sanocki@usgs.gov","orcid":"https://orcid.org/0000-0001-6714-5421","contributorId":3142,"corporation":false,"usgs":true,"family":"Sanocki","given":"Christopher","email":"sanocki@usgs.gov","middleInitial":"A.","affiliations":[{"id":37947,"text":"Upper Midwest Water Science Center","active":true,"usgs":true}],"preferred":true,"id":305058,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Kocian, Matthew J.","contributorId":19654,"corporation":false,"usgs":false,"family":"Kocian","given":"Matthew","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":305059,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":98336,"text":"ofr20101081 - 2010 - Nitrogen Loads in Groundwater Entering Back Bays and Ocean from Fire Island National Seashore, Long Island, New York","interactions":[],"lastModifiedDate":"2012-03-08T17:16:29","indexId":"ofr20101081","displayToPublicDate":"2010-04-22T00:00:00","publicationYear":"2010","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2010-1081","title":"Nitrogen Loads in Groundwater Entering Back Bays and Ocean from Fire Island National Seashore, Long Island, New York","docAbstract":"Fire Island is a barrier island that lies south of central Long Island, N.Y. It is about 60 km (37 mi) long and 0.5 km (1/4 mi) wide and is bounded by the Great South Bay, Narrow Bay, and Moriches Bay estuaries to the north; by the Atlantic Ocean to the south; by Fire Island Inlet to the west; and by Moriches Inlet to the east (fig. 1). Fire Island National Seashore (FIIS) encompasses a 42-km (26-mi) length of Fire Island that is bordered by Robert Moses State Park to the west and Smith Point County Park to the east (fig. 2). Interspersed throughout FIIS are 17 residential beach communities that together contain about 4,100 homes.\r\n\r\nThe barrier island's summer population increases 50-fold through the arrival of summer residents and vacationers. The National Park Service (NPS) has established several facilities on the island to accommodate visitors to FIIS. About 2.2 million people visit at least one of the 17 communities and (or) Smith Point County Park, the waterways surrounding Fire Island, or a FIIS facility annually (National Park Service, 2007). Combined visitation on a peak-season weekend day can be as high as 100,000 (National Park Service, 2002).\r\n\r\nMost homes and businesses in the 17 barrier-island communities discharge untreated wastewater directly to the shallow (water-table) aquifer through private septic systems and cesspools; the NPS facilities discharge wastewater to this aquifer through leach fields and cesspools. (The community of Ocean Beach (fig. 2) has a treatment plant that discharges to tidewater.) Contaminants in sewage entering the shallow groundwater move through the flow system and are ultimately discharged to adjacent marine surface waters, where they can pose a threat to coastal habitats. A contaminant of major concern is nitrogen, which is derived from fertilizers and human waste. The continuous inflow of nitrogen to surface-water bodies can lead to increased production of phytoplankton and macroalgae, which in turn can cause oxygen depletion, decreases in size of estuarine fish and shellfish communities, and loss of submerged seagrass habitat through light limitation (Valiela and others, 1992).\r\n\r\nThe FIIS boundary extends roughly 1.2 km (0.8 mi) into the back-barrier estuaries of Great South Bay, Narrow Bay, and Moriches Bay (fig. 1). Within this estuarine zone are extensive areas of seagrass, shellfish, and finfish habitat, as well as intense recreational activity (Bokuniewicz and others, 1993). Management strategies for protection of these habitats require data on (1) concentrations and movement of nutrients and other human-derived contaminants that enter the groundwater system from on-site septic systems, and (2) aquifer characteristics and groundwater flow patterns. These data can then be used in three-dimensional flow models of the shallow aquifer system to predict the rates of groundwater discharge to the marine surface waters that bound Fire Island and the concentrations of nitrogen entering these water bodies from the aquifer's discharge zones.\r\n\r\nIn 2004, the U.S. Geological Survey (USGS), in cooperation with the NPS, began a 3-year investigation to (1) measure groundwater levels within four local study areas at FIIS, (2) collect groundwater samples from these areas for nutrient (nitrogen) analysis, (3) develop a three-dimensional model of the hydrologic system and adjacent saltwater bodies for groundwater-flow delineation and particle tracking, and (4) apply the results of groundwater-discharge simulations to calculate the annual nitrogen loads in these discharges, particularly those entering Great South Bay, which together with the other back bays receives an estimated 80 percent of the total groundwater discharge from Fire Island.\r\n\r\nThe four areas on which the investigation focused were the communities of Kismet and Robbins Rest, the NPS Visitor Center at Watch Hill, and the undeveloped Otis Pike Fire Island High Dune Wilderness (shown in panels A, B, C, and D in fig. 2); these were","language":"ENGLISH","publisher":"U.S. Geological Survey","doi":"10.3133/ofr20101081","collaboration":"Prepared in cooperation with the National Park Service","usgsCitation":"Schubert, C., deVries, M.P., and Finch, A.J., 2010, Nitrogen Loads in Groundwater Entering Back Bays and Ocean from Fire Island National Seashore, Long Island, New York: U.S. Geological Survey Open-File Report 2010-1081, 16 p., https://doi.org/10.3133/ofr20101081.","productDescription":"16 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":474,"text":"New York Water Science Center","active":true,"usgs":true}],"links":[{"id":125893,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr_2010_1081.jpg"},{"id":13584,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2010/1081/","linkFileType":{"id":5,"text":"html"}}],"geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -73.33333333333333,40.53333333333333 ], [ -73.33333333333333,40.85 ], [ -72.76666666666667,40.85 ], [ -72.76666666666667,40.53333333333333 ], [ -73.33333333333333,40.53333333333333 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a51e4b07f02db629c59","contributors":{"authors":[{"text":"Schubert, Christopher 0000-0003-0705-3933 schubert@usgs.gov","orcid":"https://orcid.org/0000-0003-0705-3933","contributorId":1243,"corporation":false,"usgs":true,"family":"Schubert","given":"Christopher","email":"schubert@usgs.gov","affiliations":[{"id":474,"text":"New York Water Science Center","active":true,"usgs":true}],"preferred":false,"id":305026,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"deVries, M. Peter pdevries@usgs.gov","contributorId":1555,"corporation":false,"usgs":true,"family":"deVries","given":"M.","email":"pdevries@usgs.gov","middleInitial":"Peter","affiliations":[],"preferred":true,"id":305027,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Finch, Anne J.","contributorId":102494,"corporation":false,"usgs":true,"family":"Finch","given":"Anne","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":305028,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":98333,"text":"sir20105014 - 2010 - Potentiometric Surfaces and Water-Level Trends in the Cockfield (Upper Claiborne) and Wilcox (Lower Wilcox) Aquifers of Southern and Northeastern Arkansas, 2009","interactions":[],"lastModifiedDate":"2012-02-10T00:11:53","indexId":"sir20105014","displayToPublicDate":"2010-04-21T00:00:00","publicationYear":"2010","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":334,"text":"Scientific Investigations Report","code":"SIR","onlineIssn":"2328-0328","printIssn":"2328-031X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2010-5014","title":"Potentiometric Surfaces and Water-Level Trends in the Cockfield (Upper Claiborne) and Wilcox (Lower Wilcox) Aquifers of Southern and Northeastern Arkansas, 2009","docAbstract":"Eocene-age sand beds near the base of the Cockfield Formation of Claiborne Group constitute the aquifer known locally as the Cockfield aquifer. Upper-Paleocene age sand beds within the lower parts of the Wilcox Group constitute the aquifer known locally as the Wilcox aquifer. In 2005, reported water withdrawals from the Cockfield aquifer in Arkansas totaled 16.1 million gallons per day, while reported water withdrawals from the Wilcox aquifer in Arkansas totaled 27.0 million gallons per day. Major withdrawals from these units were for industrial and public water supplies with lesser but locally important withdrawals for commercial, domestic, and agricultural uses. \r\n\r\nDuring February 2009, 56 water-level measurements were made in wells completed in the Cockfield aquifer and 57 water-level measurements were made in wells completed in the Wilcox aquifer. The results from the 2009 water-level measurements are presented in potentiometric-surface maps and in combination with previous water-level measurements. \r\n\r\nTrends in water-level change over time within the two aquifers are investigated using water-level difference maps and well hydrographs. Water-level difference maps were constructed for each aquifer using the difference between depth to water measurements made in 2003 to 2009. Well hydrographs for each aquifer were constructed for wells with 20 or more years of historical water-level data. The hydrographs were evaluated individually using linear regression to calculate the annual rise or decline in water levels, and by aggregating the regression results by county and statistically summarizing for the range, mean, and median water-level change in each county.\r\n\r\nThe 2009 potentiometric surface of the Cockfield aquifer map indicates the regional direction of groundwater flow generally towards the east and southeast, except in two areas of intense groundwater withdrawals that have developed into cones of depression. The lowest water-level altitude measured was 43 feet and the highest water-level altitude measured was 351 feet. \r\n\r\nA water-level difference map was constructed from 54 wells completed in the Cockfield aquifer within Arkansas. The largest rise in water level was 14.9 feet and the largest decline was 27.4 feet. Seven wells had a rise in water level, and the remaining 47 wells had a decline in water level. \r\n\r\nHydrographs for 33 wells completed in the Cockfield aquifer were developed. Hydrographs indicate water-level changes in individual wells ranged from rises of 0.33 feet per year to declines of 1.21 feet per year over the 20-year period (1990-2009). County summaries of the linear regression analysis indicate Cleveland and Columbia Counties have mean annual rises. Arkansas, Ashley, Bradley, Calhoun, Chicot, Desha, Drew, Lincoln, and Union Counties have mean annual declines. \r\n\r\nThe potentiometric surface for the Wilcox aquifer is presented using two maps, one for a southern area and another for a northeastern area, because of the absence of water-level data in the central part of the State. The direction of groundwater flow in the southern area is generally the east, except around two cones of depression and around two mounds of elevated water levels. Water-level altitudes in the southern area range from 147 feet to 400 feet. The direction of groundwater flow in the northeastern area is generally to the south and southeast except in an area of intense groundwater withdrawals that has altered the flow to a westerly direction.\r\n\r\nTwo water-level difference maps were constructed using water-level altitudes measured in 2003 to 2009 from 53 wells completed in the Wilcox aquifer within southern and northeastern Arkansas. In the southern area the largest rise in water level was 16.0 feet and the largest decline was 17.7 feet. Eight wells in the southern area had rising water levels and the remaining five wells had declining water levels. In the northeastern area, the largest rise in water level was 1.3 feet and the larg","language":"ENGLISH","publisher":"U.S. Geological Survey","doi":"10.3133/sir20105014","collaboration":"Prepared in cooperation with the Arkansas Natural Resources Commission and the Arkansas Geological Survey","usgsCitation":"Pugh, A., 2010, Potentiometric Surfaces and Water-Level Trends in the Cockfield (Upper Claiborne) and Wilcox (Lower Wilcox) Aquifers of Southern and Northeastern Arkansas, 2009: U.S. Geological Survey Scientific Investigations Report 2010-5014, v, 47 p. , https://doi.org/10.3133/sir20105014.","productDescription":"v, 47 p. ","onlineOnly":"N","additionalOnlineFiles":"N","temporalStart":"2003-01-01","temporalEnd":"2009-12-31","costCenters":[{"id":129,"text":"Arkansas Water Science Center","active":true,"usgs":true}],"links":[{"id":118633,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2010_5014.jpg"},{"id":13582,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2010/5014/","linkFileType":{"id":5,"text":"html"}}],"geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -94.7,33 ], [ -94.7,36.5 ], [ -89.68333333333334,36.5 ], [ -89.68333333333334,33 ], [ -94.7,33 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a1ae4b07f02db606677","contributors":{"authors":[{"text":"Pugh, Aaron L. apugh@usgs.gov","contributorId":2480,"corporation":false,"usgs":true,"family":"Pugh","given":"Aaron L.","email":"apugh@usgs.gov","affiliations":[{"id":129,"text":"Arkansas Water Science Center","active":true,"usgs":true}],"preferred":true,"id":305019,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70209979,"text":"70209979 - 2010 - Holocene stratigraphy and chronology of the Casper Dune Field, Casper, Wyoming, USA","interactions":[],"lastModifiedDate":"2020-05-07T17:58:02.635462","indexId":"70209979","displayToPublicDate":"2010-04-20T12:52:34","publicationYear":"2010","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1905,"text":"Holocene","active":true,"publicationSubtype":{"id":10}},"title":"Holocene stratigraphy and chronology of the Casper Dune Field, Casper, Wyoming, USA","docAbstract":"Activation chronologies of dune fields within the North American Great Plains are significant sources of paleoclimate information. Although many regional chronologies exist, several dune fields have been understudied, including the Casper Dune Field of central Wyoming. This study investigated aeolian dune sediment and buried soils of the Casper Dune Field. Complex parabolic and hairpin parabolic dunes dominate the eastern dune field, while simple parabolic and linear dunes dominate the western dune field. Buried soils are found throughout the dune field, though their distribution and degree of development varies. Buried soils in the eastern dune field are weakly developed with typical A-C profiles, whereas soils in the western dune field typically exhibit A-Bt-C profiles. Optically stimulated luminescence (OSL) and radiocarbon ages were used to provide a chronology of dune field activation that spans most of the Holocene. At the onset of the Holocene, alluvium was deposited first, followed by widespread dune activity ~ 10.0—6.2 ka. Following activity, the dune field stabilized until about 4.1 ka. During this stabilization period, however, reactivation occurred in at least one locality within the dune field at 5.1 ka. Subsequent aeolian activity occurred at 4.1 ka and between 1.0 ka and 0.4 ka. The resulting activation chronology is compared with those obtained from elsewhere in Wyoming and from other west-central Great Plains dune fields.
","language":"English","publisher":"Sage","doi":"10.1177/0959683610362812","usgsCitation":"Halfen, A.F., Fredlund, G.G., and Mahan, S.A., 2010, Holocene stratigraphy and chronology of the Casper Dune Field, Casper, Wyoming, USA: Holocene, v. 20, no. 5, p. 773-783, https://doi.org/10.1177/0959683610362812.","productDescription":"11 p.","startPage":"773","endPage":"783","costCenters":[{"id":318,"text":"Geosciences and Environmental Change Science Center","active":true,"usgs":true}],"links":[{"id":374546,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Wyoming","city":"Caspar","otherGeospatial":"Caspar Dune Field","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -108.028564453125,\n 42.71473218539458\n ],\n [\n -104.1888427734375,\n 42.71473218539458\n ],\n [\n -104.1888427734375,\n 43.92559366355069\n ],\n [\n -108.028564453125,\n 43.92559366355069\n ],\n [\n -108.028564453125,\n 42.71473218539458\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"20","issue":"5","noUsgsAuthors":false,"publicationDate":"2010-04-23","publicationStatus":"PW","contributors":{"authors":[{"text":"Halfen, Alan F.","contributorId":224604,"corporation":false,"usgs":false,"family":"Halfen","given":"Alan","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":788676,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Fredlund, G. G.","contributorId":53568,"corporation":false,"usgs":true,"family":"Fredlund","given":"G.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":788677,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Mahan, Shannon A. 0000-0001-5214-7774 smahan@usgs.gov","orcid":"https://orcid.org/0000-0001-5214-7774","contributorId":147159,"corporation":false,"usgs":true,"family":"Mahan","given":"Shannon","email":"smahan@usgs.gov","middleInitial":"A.","affiliations":[{"id":318,"text":"Geosciences and Environmental Change Science Center","active":true,"usgs":true}],"preferred":true,"id":788678,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70198317,"text":"70198317 - 2010 - Enhancement of the volcanogenic \"bromine explosion\" via reactive nitrogen chemistry (Kīlauea volcano, Hawai'i)","interactions":[],"lastModifiedDate":"2019-12-30T09:36:02","indexId":"70198317","displayToPublicDate":"2010-04-20T09:43:41","publicationYear":"2010","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":923,"text":"Atmospheric Chemistry and Physics Discussions","active":true,"publicationSubtype":{"id":10}},"title":"Enhancement of the volcanogenic \"bromine explosion\" via reactive nitrogen chemistry (Kīlauea volcano, Hawai'i)","docAbstract":"Since the first detection of bromine monoxide in volcanic plumes attention has focused on the atmospheric synthesis and impact of volcanogenic reactive halogens. We report here new measurements of BrO in the volcanic plume emitted from Kīlauea volcano – the first time reactive halogens have been observed in emissions from a hotspot volcano. Observations were carried out by ground-based Differential Optical Absorption Spectroscopy in 2007 and 2008 at Pu'u'O'o crater, and at the 2008 magmatic vent that opened within Halema'uma'u crater. BrO was readily detected in the Halema'uma'u plume (average column amount of 3×1015 molec cm−2) and its abundance was strongly correlated with that of SO2. However, anticorrelation between NO2 and SO2 (and BrO) abundances in the same plume strongly suggest an active role of NOx in reactive halogen chemistry. The calculated SO2/BrO molar ratio of ~1600 is comparable to observations at other volcanoes, although the BrO mixing ratio is roughly double that observed elsewhere. While BrO was not observed in the Pu'u'O'o plume this was probably merely a result of the detection limit of our measurements and based on understanding of the Summit and East Rift magmatic system we expect reactive halogens to be formed also in the Pu'u'O'o emissions. If this is correct then based on the long term SO2 flux from Pu'u'O'o we calculate that Kīlauea emits ~480 Mg yr−1 of reactive bromine and may thus represent an important source to the tropical Pacific troposphere.
","language":"English","publisher":"EGU","doi":"10.5194/acpd-10-10313-2010","usgsCitation":"Salerno, G.G., Oppenheimer, C., Tsanev, V., Sutton, A., Roberts, T., and Elias, T., 2010, Enhancement of the volcanogenic \"bromine explosion\" via reactive nitrogen chemistry (Kīlauea volcano, Hawai'i): Atmospheric Chemistry and Physics Discussions, v. 10, p. 10313-10334, https://doi.org/10.5194/acpd-10-10313-2010.","productDescription":"22 p.","startPage":"10313","endPage":"10334","costCenters":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"links":[{"id":475734,"rank":0,"type":{"id":41,"text":"Open Access External Repository Page"},"url":"https://doi.org/10.5194/acpd-10-10313-2010","text":"External Repository"},{"id":356047,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Hawaii","otherGeospatial":"Kilauea Volcano ","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -155.3528594970703,\n 19.329286698998818\n ],\n [\n -155.17501831054688,\n 19.329286698998818\n ],\n [\n -155.17501831054688,\n 19.46400263520258\n ],\n [\n -155.3528594970703,\n 19.46400263520258\n ],\n [\n -155.3528594970703,\n 19.329286698998818\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"10","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5b98b794e4b0702d0e844eb1","contributors":{"authors":[{"text":"Salerno, G. G.","contributorId":206547,"corporation":false,"usgs":false,"family":"Salerno","given":"G.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":741016,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Oppenheimer, C.","contributorId":69767,"corporation":false,"usgs":true,"family":"Oppenheimer","given":"C.","email":"","affiliations":[],"preferred":false,"id":741017,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Tsanev, V.","contributorId":40417,"corporation":false,"usgs":true,"family":"Tsanev","given":"V.","affiliations":[],"preferred":false,"id":741018,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Sutton, A.J. ajsutton@usgs.gov","contributorId":3584,"corporation":false,"usgs":true,"family":"Sutton","given":"A.J.","email":"ajsutton@usgs.gov","affiliations":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"preferred":false,"id":741019,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Roberts, T.J.","contributorId":198344,"corporation":false,"usgs":false,"family":"Roberts","given":"T.J.","email":"","affiliations":[],"preferred":false,"id":741020,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Elias, T. 0000-0002-9592-4518","orcid":"https://orcid.org/0000-0002-9592-4518","contributorId":71195,"corporation":false,"usgs":true,"family":"Elias","given":"T.","affiliations":[],"preferred":false,"id":741021,"contributorType":{"id":1,"text":"Authors"},"rank":6}]}} ,{"id":98328,"text":"ds501 - 2010 - Seasonal and Spatial Distribution of Freshwater Flow and Salinity in the Ten Thousand Islands Estuary, Florida, 2007-2009","interactions":[],"lastModifiedDate":"2019-11-08T06:32:08","indexId":"ds501","displayToPublicDate":"2010-04-15T00:00:00","publicationYear":"2010","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":310,"text":"Data Series","code":"DS","onlineIssn":"2327-638X","printIssn":"2327-0271","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"501","title":"Seasonal and Spatial Distribution of Freshwater Flow and Salinity in the Ten Thousand Islands Estuary, Florida, 2007-2009","docAbstract":"The watershed of the Ten Thousand Islands (TTI) estuary has been substantially altered through the construction of canals and roads for the Southern Golden Gate Estates (SGGE), Barron River Canal, and U.S. 41 (Tamiami Trail). Two restoration projects designed to improve freshwater delivery to the estuary are the Picayune Strand Restoration Project, which includes the Southern Golden Gate Estates, and the Tamiami Trail Culverts Project; both are part of the Comprehensive Everglades Restoration Plan. To address hydrologic information needs critical for monitoring the effects of these restoration projects, the U.S. Geological Survey initiated a study in October 2006 to characterize freshwater outflows from the rivers, internal circulation and mixing within the estuary, and surface-water exchange between the estuary and Gulf of Mexico. The effort is conducted in cooperation with the South Florida Water Management District and complemented by monitoring performed by the Rookery Bay National Estuarine Research Reserve. \r\n\r\nSurface salinity was measured during moving boat surveys using a flow-through system that operated at planing speeds averaging 20 miles per hour. The data were logged every 10 seconds by a data recorder that simultaneously logged location information from a Global Positioning System. The major rivers, bays, and nearshore Gulf of Mexico region of the TTI area were surveyed in approximately 5 hours by two boats traversing about 200 total miles. Salinity and coordinate data were processed using inverse distance weighted interpolation to create salinity contour maps of the entire TTI region. \r\n\r\nTen maps were created from salinity surveys performed between May 2007 and May 2009 and illustrate the dry season, transitional, and wet season salinity patterns of the estuarine rivers, inner bays, mangrove islands, and Gulf of Mexico boundary. The effects of anthropogenic activities are indicated by exceptionally low salinities associated with point discharge into the estuary from the Faka Union Canal and Barron River during the wet season. Low salinities in Faka Union Bay may cause reduced diversity and density of submerged aquatic vegetation, fish, and benthic organisms compared with neighboring Fakahatchee Bay. The Faka Union Canal System reduced the size of the watershed for the western TTI estuary, resulting in increased wet season salinities compared to those for the eastern TTI estuary, the watershed of which is composed of the relatively pristine Fakahatchee Strand Preserve State Park. Minimal river discharge and high evaporation caused hypersaline conditions to develop throughout the entire TTI region during the dry season. The 2007-2008 drought and passage of Tropical Storm Fay on August 18-19, 2008, demonstrated the effects of seasonal rainfall on salinity patterns, with substantially higher salinities observed during the 2007 wet season compared to those for the 2008 wet season. The salinity maps, coupled with data from the monitoring stations, provide baseline information of seasonal and spatial distribution of freshwater flow and salinity in the TTI estuary, and a means of monitoring the effects of restoration in improving freshwater delivery to the estuary. \r\n","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ds501","collaboration":"Prepared in cooperation with South Florida Water Management District","usgsCitation":"Soderqvist, L.E., and Patino, E., 2010, Seasonal and Spatial Distribution of Freshwater Flow and Salinity in the Ten Thousand Islands Estuary, Florida, 2007-2009: U.S. Geological Survey Data Series 501, vi, 24 p., https://doi.org/10.3133/ds501.","productDescription":"vi, 24 p.","onlineOnly":"N","temporalStart":"2007-05-01","temporalEnd":"2009-05-31","costCenters":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":118621,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ds_501.jpg"},{"id":13577,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/ds/501/","linkFileType":{"id":5,"text":"html"}}],"geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -81.62155151367188,\n 25.977181684362176\n ],\n [\n -81.69261932373047,\n 25.857060917861336\n ],\n [\n -81.42345428466797,\n 25.759082934951692\n ],\n [\n -81.35890960693358,\n 25.90185031509369\n ],\n [\n -81.62155151367188,\n 25.977181684362176\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0ce4b07f02db5fc42b","contributors":{"authors":[{"text":"Soderqvist, Lars E.","contributorId":92358,"corporation":false,"usgs":true,"family":"Soderqvist","given":"Lars","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":305007,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Patino, Eduardo 0000-0003-1016-3658 epatino@usgs.gov","orcid":"https://orcid.org/0000-0003-1016-3658","contributorId":1743,"corporation":false,"usgs":true,"family":"Patino","given":"Eduardo","email":"epatino@usgs.gov","affiliations":[{"id":270,"text":"FLWSC-Tampa","active":true,"usgs":true},{"id":269,"text":"FLWSC-Ft. Lauderdale","active":true,"usgs":true}],"preferred":true,"id":305006,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":98327,"text":"sir20095266 - 2010 - Status and understanding of groundwater quality in the central-eastside San Joaquin Basin, 2006: California GAMA Priority Basin Project","interactions":[],"lastModifiedDate":"2024-10-30T20:14:13.008933","indexId":"sir20095266","displayToPublicDate":"2010-04-14T00:00:00","publicationYear":"2010","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":334,"text":"Scientific Investigations Report","code":"SIR","onlineIssn":"2328-0328","printIssn":"2328-031X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2009-5266","title":"Status and understanding of groundwater quality in the central-eastside San Joaquin Basin, 2006: California GAMA Priority Basin Project","docAbstract":"Groundwater quality in the approximately 1,695-square-mile Central Eastside San Joaquin Basin (Central Eastside) study unit was investigated as part of the Priority Basin Project (PBP) of the Groundwater Ambient Monitoring and Assessment (GAMA) Program. The GAMA PBP was developed in response to the California Groundwater Quality Monitoring Act of 2001, and is being conducted by the California State Water Resources Control Board in collaboration with the U.S. Geological Survey and the Lawrence Livermore National Laboratory. The GAMA Central Eastside study unit was designed to provide a spatially unbiased assessment of untreated-groundwater quality, as well as a statistically consistent basis for comparing water quality throughout California. During March through June 2006, samples were collected from 78 wells in Stanislaus and Merced Counties, 58 of which were selected using a spatially distributed, randomized grid-based method to provide statistical representation of the study unit (grid wells), and 20 of which were sampled to evaluate changes in water chemistry along groundwater-flow paths (understanding wells). Water-quality data from the California Department of Public Health (CDPH) database also were used for the assessment.
An assessment of the current status of the groundwater quality included collecting samples from wells for analysis of anthropogenic constituents such as volatile organic compounds (VOCs) and pesticides, as well as naturally occurring constituents such as major ions and trace elements. The assessment of status is intended to characterize the quality of untreated-groundwater resources within the primary aquifer system, not the treated drinking water delivered to consumers by water purveyors. The primary aquifer system (hereinafter, primary aquifer) is defined as that part of the aquifer corresponding to the perforation interval of wells listed in the CDPH database for the Central Eastside study unit. The quality of groundwater in shallower or deeper water-bearing zones may differ from that in the primary aquifer; shallower groundwater may be more vulnerable to surficial contamination. The primary aquifer is represented by the grid wells, of which 90 percent had depths to the tops of their perforations of about 80 to 330 feet and depths to bottom of about 100 to 670 feet. Relative-concentrations (sample concentration divided by benchmark concentration) were used as the primary metric for assessing the status of water quality for those constituents that have Federal and (or) California human health or aesthetic benchmarks. A relative-concentration greater than (>) 1.0 indicates a concentration above a benchmark, and less than or equal to (≤) 1.0 indicates a concentration equal to or below a benchmark. For organic and special interest constituents, relative-concentrations were classified as high (>1.0), moderate (≤1.0 and >0.1), or low (≤0.1). For inorganic constituents, relative-concentrations were classified as high (>1.0), moderate (≤1.0 and >0.5), or low (≤0.5). The threshold between low and moderate classifications was lower for organic and special interest constituents than for inorganic constituents because organic constituents generally are less prevalent and have smaller relative-concentrations than inorganic constituents.
Grid-based and spatially-weighted approaches, the latter incorporating data from all CDPH wells, were used to evaluate the proportion of the primary aquifer (aquifer-scale proportions) with high, moderate, or low relative-concentrations. For individual constituents or classes of constituents, the aquifer-scale high proportion is the percentage of the area of the study unit having high relative-concentrations within the depth-zones of the primary aquifer. Aquifer-scale moderate and low proportions are defined similarly. Spatially-weighted aquifer-scale high proportions nearly always fell within the 90-percent confidence interval of grid-based aquifer-scale high proportions, indicating that the grid-based approach yielded statistically equivalent results to the spatially-weighted approach incorporating CDPH data.
The status assessment for inorganic constituents showed that inorganic constituents (one or more) were high, relative to human-health benchmarks, in 18.0 percent of the primary aquifer, moderate in 44.0 percent, and low in 38.0 percent. Of inorganic constituents with human-health benchmarks, arsenic, vanadium, and nitrate were detected at high relative-concentrations in 15.6 percent, 3.6 percent, and 2.1 percent, respectively, of the primary aquifer. Of inorganic constituents with secondary maximum contaminant levels (SMCL), manganese, iron, and TDS were detected at high relative-concentrations in 4.5 percent, 2.2 percent, and 1.7 percent, respectively, of the primary aquifer.
The status assessment for organic constituents showed that organic constituents (one or more) were high, relative to human-health benchmarks, in a smaller proportion of the primary aquifer (1.2 percent) than inorganic constituents (18.0 percent). Organic constituents had moderate relative-concentrations in 14.3 percent, and had low relative-concentrations or were not detected in 84.5 percent, of the primary aquifer. The proportion of the primary aquifer with high relative-concentrations of organic constituents reflected high proportions of the discontinued soil fumigant 1,2-dibromo-3-chlororopane (DBCP; 1.0 percent) and the solvent tetrachloroethene (PCE; 0.2 percent). Most of the organic and special interest constituents detected in groundwater in the Central Eastside study unit have human-health benchmarks. Of the 205 organic and special interest constituents analyzed for, 36 constituents were detected. Of these constituents, 32 were detected only at low relative-concentrations. Four constituents, chloroform, carbon tetrachloride, DBCP, and perchlorate, were detected at moderate relative-concentrations in grid wells. Nine organic and special-interest constituents were detected frequently (detected in greater than 10 percent of samples): the trihalomethanes chloroform, bromoform, bromodichloromethane, and dibromochloromethane; the solvent PCE; the herbicides atrazine, simazine, and metolachlor, and special-interest constituent perchlorate.
An assessment of understanding of the groundwater quality included sampling of understanding wells, some of which were perforated in shallower or deeper portions of the aquifer system than the primary aquifer, and analysis of correlations of groundwater quality with land use, depth, age classification, and other potential explanatory factors.
The understanding assessment indicated that the concentrations of many constituents were related to depth and groundwater age. However, concentrations of individual constituents or constituent classes also were sometimes related to geochemical conditions, lateral position in the flow system, or land use.
High and moderate relative-concentrations of uranium, nitrate, and total dissolved solids (TDS) were detected in some wells where the tops of perforations are within the upper 200 feet of the aquifer system. In wells with the depth to the top of perforations below this depth, concentrations were low. A similar pattern occurred for the sum of herbicide concentrations. These vertical water-chemistry patterns are consistent with the hydrogeologic setting, in which return flows from agricultural and urban land use are the major source of recharge, and withdrawals for irrigation and urban supply are the major source of discharge, resulting in substantial vertical components of groundwater flow.
The decrease in concentrations of many constituents with depth reflects in part that groundwater gets older with depth. Tritium, helium-isotopes, and carbon-14 data were used to classify the predominant age of groundwater samples into three categories: modern (water that has entered the aquifer in the last 50 years), pre-modern (water that entered the aquifer more than 50 years, up to tens of thousands of years, ago), and mixed (mixtures of waters with modern and pre-modern ages). Uranium, nitrate, and herbicide concentrations were significantly higher in groundwater having modern- and mixed-ages than pre-modern ages, indicating that these constituents may be affected by anthropogenic activities in the last 50 years.
Other patterns in the distribution of nitrate, uranium, and TDS are evident. Isotopic and geochemical data are consistent with partial denitrification of nitrate in some reducing groundwaters in the western and deeper parts of the flow system. Uranium and TDS concentrations increase from east to west across the valley, along the direction of regional lateral groundwater flow.
High and moderate relative-concentrations of arsenic can be attributed to reductive dissolution of manganese or iron oxides, or to desorption by high pH waters. Arsenic concentrations also increased with increasing depth and groundwater age. High to moderate relative-concentrations of vanadium primarily are related to high pH under oxic conditions.
The frequency of detections of DBCP was greater in areas with orchard-vineyard land use >40 percent and at depths <200 feet. THMs and solvents were correlated positively with percent urban land use. Herbicide concentrations were correlated negatively with percent natural land use. Perchlorate concentrations were significantly greater in waters having modern and mixed ages than waters having pre-modern ages and were significantly and positively correlated with two land uses—percent orchard/vineyard land use and percent urban land use.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/sir20095266","collaboration":"Prepared in cooperation with the California State Water Resources Control Board","usgsCitation":"Landon, M.K., Belitz, K., Jurgens, B., Kulongoski, J., and Johnson, T., 2010, Status and understanding of groundwater quality in the central-eastside San Joaquin Basin, 2006: California GAMA Priority Basin Project: U.S. Geological Survey Scientific Investigations Report 2009-5266, xii, 97 p., https://doi.org/10.3133/sir20095266.","productDescription":"xii, 97 p.","numberOfPages":"113","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":154,"text":"California Water Science Center","active":true,"usgs":true}],"links":[{"id":13576,"rank":3,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2009/5266/","linkFileType":{"id":5,"text":"html"}},{"id":463447,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_92511.htm","linkFileType":{"id":5,"text":"html"}},{"id":125892,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.er.usgs.gov/thumbnails/sir_2009_5266.jpg"},{"id":339724,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/sir/2009/5266/pdf/sir20095266.pdf","linkFileType":{"id":1,"text":"pdf"}}],"projection":"Albers Equal Area Conic","country":"United States","state":"California","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -121.41666666666667,37 ], [ -121.41666666666667,38 ], [ -119,38 ], [ -119,37 ], [ -121.41666666666667,37 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49dbe4b07f02db5e0eb8","contributors":{"authors":[{"text":"Landon, Matthew K. 0000-0002-5766-0494 landon@usgs.gov","orcid":"https://orcid.org/0000-0002-5766-0494","contributorId":392,"corporation":false,"usgs":true,"family":"Landon","given":"Matthew","email":"landon@usgs.gov","middleInitial":"K.","affiliations":[{"id":154,"text":"California Water Science Center","active":true,"usgs":true}],"preferred":true,"id":305001,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Belitz, Kenneth 0000-0003-4481-2345 kbelitz@usgs.gov","orcid":"https://orcid.org/0000-0003-4481-2345","contributorId":442,"corporation":false,"usgs":true,"family":"Belitz","given":"Kenneth","email":"kbelitz@usgs.gov","affiliations":[{"id":27111,"text":"National Water Quality Program","active":true,"usgs":true},{"id":503,"text":"Office of Water Quality","active":true,"usgs":true},{"id":466,"text":"New England Water Science Center","active":true,"usgs":true},{"id":376,"text":"Massachusetts Water Science Center","active":true,"usgs":true},{"id":451,"text":"National Water Quality Assessment Program","active":true,"usgs":true}],"preferred":true,"id":305002,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Jurgens, Bryant C. 0000-0002-1572-113X","orcid":"https://orcid.org/0000-0002-1572-113X","contributorId":22454,"corporation":false,"usgs":true,"family":"Jurgens","given":"Bryant C.","affiliations":[],"preferred":false,"id":305003,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Kulongoski, Justin T. 0000-0002-3498-4154","orcid":"https://orcid.org/0000-0002-3498-4154","contributorId":59909,"corporation":false,"usgs":true,"family":"Kulongoski","given":"Justin T.","affiliations":[],"preferred":false,"id":305004,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Johnson, Tyler D. 0000-0002-7334-9188","orcid":"https://orcid.org/0000-0002-7334-9188","contributorId":64366,"corporation":false,"usgs":true,"family":"Johnson","given":"Tyler D.","affiliations":[],"preferred":false,"id":305005,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":98311,"text":"sim3119 - 2010 - Reconnaissance geologic map of the Hayfork 15' quadrangle, Trinity County, California","interactions":[],"lastModifiedDate":"2022-04-14T21:25:57.250117","indexId":"sim3119","displayToPublicDate":"2010-04-08T00:00:00","publicationYear":"2010","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":"3119","title":"Reconnaissance geologic map of the Hayfork 15' quadrangle, Trinity County, California","docAbstract":"The Hayfork 15' quadrangle is located just west of the Weaverville 15' quadrangle in the southern part of the Klamath Mountains geologic province of northern California. It spans parts of six generally north-northwest-trending tectonostratigraphic terranes that are, from east to west, the Eastern Klamath, Central Metamorphic, North Fork, Eastern Hayfork, Western Hayfork, and Rattlesnake Creek terranes. Remnants of a once-widespread postaccretionary overlap assemblage, the Cretaceous Great Valley sequence, crop out at three localities in the southern part of the Hayfork quadrangle. The Tertiary fluvial and lacustrine Weaverville Formation occupies a large, shallow, east-northeast-trending graben in the south half of the quadrangle. \r\n\r\nThe small area of Eastern Klamath terrane is part of the Oregon Mountain outlier, which is more widely exposed to the east in the Weaverville 15' quadrangle. It was originally mapped as a thrust plate of Bragdon(?) Formation, but it is now thought by some to be part of an outlier of Yreka terrane that has been dislocated 60 km southward by the La Grange Fault. The Central Metamorphic terrane, which forms the footwall of the La Grange Fault, was formed by the eastward subduction of oceanic crustal basalt (the Salmon Hornblende Schist) and its overlying siliceous sediments with interbedded limestone (the Abrams Mica Schist) beneath the Eastern Klamath terrane. Rb-Sr analysis of the Abrams Mica Schist indicates a Middle Devonian metamorphic age of approximately 380 Ma, which probably represents the age of subduction. \r\n\r\nThe North Fork terrane, which is faulted against the western boundary of the Central Metamorphic terrane, consists of the Permian(?) North Fork ophiolite and overlying broken formation and melange of Permian to Early Jurassic (Pliensbachian) marine metasedimentary and metavolcanic rocks. The ophiolite, which crops out along the western border of the terrane, is thrust westward over the Eastern Hayfork terrane. \r\n\r\nThe Eastern Hayfork terrane is a broken formation and melange of volcanic and sedimentary rocks, including chert and blocks of amphibolite, limestone, and serpentinized ultramafic rocks. The chert contains radiolarians of Permian and Triassic ages, but none of clearly Jurassic age. In contrast, the cherts of the North Fork terrane contain Early and Middle Jurassic radiolarians in addition to those of Permian and Triassic ages; also, some limestones of the Eastern Hayfork terrane contain fossil faunas of Tethyan affinity, but those of the North Fork terrane do not. \r\n\r\nThe Western Hayfork terrane is an andesitic volcanic arc that was accreted to the Eastern Hayfork terrane. It consists mainly of metavolcaniclastic andesitic agglomerate and tuff, as well as argillite and chert, and it includes the dioritic Ironside Mountain batholith, which intruded during Middle Jurassic time. Two large patches of Western Hayfork terrane mapped in the central part of the Eastern Hayfork terrane may be exposed through windows in the Eastern Hayfork terrane, although the structural relation is not clear. \r\n\r\nThe Rattlesnake Creek terrane is a melange that occupies only a small area in the southwest corner of the Hayfork quadrangle; however, it is a major unit in the Hyampom 15' quadrangle to the west. It consists mainly of broken and sheared ophiolitic rocks of probable Permian or early Mesozoic age. \r\n\r\nThe Cretaceous Great Valley sequence overlap assemblage here postdates the Early Cretaceous (approximately 136 Ma) emplacement of the Shasta Bally batholith, which is widely exposed to the east in the Weaverville 15' quadrangle. The Great Valley sequence once covered much of the southern Klamath Mountains; however, in the Hayfork quadrangle, only three small patches remain near its southern boundary. \r\n\r\nWeakly consolidated nonmarine sedimentary rocks of the Weaverville Formation of mid-Tertiary age, which contain abundant fossil plants, occupy a large, shallow, east-northeast-trending graben","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/sim3119","usgsCitation":"Irwin, W., 2010, Reconnaissance geologic map of the Hayfork 15' quadrangle, Trinity County, California: U.S. Geological Survey Scientific Investigations Map 3119, Report: 1 p.; 1 Plate: 40.85 x 28.36 inches; GIS Sources, https://doi.org/10.3133/sim3119.","productDescription":"Report: 1 p.; 1 Plate: 40.85 x 28.36 inches; GIS Sources","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[{"id":235,"text":"Earthquake Hazards Program - Northern California","active":false,"usgs":true},{"id":300,"text":"Geologic Hazards Science Center","active":true,"usgs":true}],"links":[{"id":118613,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sim_3119.jpg"},{"id":398786,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_92496.htm"},{"id":13564,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sim/3119/","linkFileType":{"id":5,"text":"html"}}],"scale":"50000","country":"United States","state":"California","county":"Trinity County","otherGeospatial":"Hayfork 15' quadrangle","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -123.25,\n 40.75\n ],\n [\n -123,\n 40.75\n ],\n [\n -123,\n 40.5\n ],\n [\n -123.25,\n 40.5\n ],\n [\n -123.25,\n 40.75\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a74e4b07f02db64442e","contributors":{"authors":[{"text":"Irwin, William P.","contributorId":12889,"corporation":false,"usgs":true,"family":"Irwin","given":"William P.","affiliations":[],"preferred":false,"id":304973,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70236358,"text":"70236358 - 2010 - Multiple phases of basin formation along the Stateline fault system in the Pahrump and Mesquite Valleys, Nevada and California","interactions":[],"lastModifiedDate":"2022-09-02T19:48:01.910987","indexId":"70236358","displayToPublicDate":"2010-04-01T14:41:09","publicationYear":"2010","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1820,"text":"Geosphere","active":true,"publicationSubtype":{"id":10}},"title":"Multiple phases of basin formation along the Stateline fault system in the Pahrump and Mesquite Valleys, Nevada and California","docAbstract":"Two phases of deformation are needed to describe the Cenozoic tectonic evolution of the Pahrump and Mesquite basins in the southern Great Basin and eastern Mojave Desert, United States. By interpreting seismic reflection and gravity observations along with bedrock and surficial mapping, we infer an extensional phase of basin formation followed by a transtensional phase, in this area straddling the border of southern Nevada and southeastern California. We reprocessed ∼220 line km of industry seismic reflection data from the Pahrump and Mesquite Valleys to emphasize reflections in the basin fill, and combined these results with analysis of gravity data. The seismic lines portray the complex geometry of the Stateline fault system, a major Neogene dextral strike-slip system that passes through these valleys, and provide evidence for multiple ages of faulting along structures that bound the Pahrump basin. Locally thick sequences of preextensional Tertiary sedimentary rocks are cut by large-offset, relatively high-angle normal faults that record a phase of extensional basin formation that preceded transtension. The existence of preextensional basins beneath the Pahrump and Mesquite Valleys bears on tectonic reconstruction of the region and suggests that tilted ranges blocks to the west of these valleys need not restore to positions immediately adjacent to the Spring Mountains to the east. Subsequent dextral offset on the Stateline fault system resulted in the formation of steep-sided basins, local arching and tectonic inversion, and the burial of earlier-formed normal faults with coarse clastic detritus. Gravity models that are constrained to match the basin architecture observed in the seismic lines require lateral variations in basin-fill and bedrock density, and they confirm that the Paleozoic outcrop of Black Butte, a topographic high separating the Pahrump and Mesquite Valleys, is unrooted to underlying bedrock.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/GES00520.1","usgsCitation":"Scheirer, D., Sweetkind, D.S., and Miller, J.J., 2010, Multiple phases of basin formation along the Stateline fault system in the Pahrump and Mesquite Valleys, Nevada and California: Geosphere, v. 6, no. 2, p. 93-129, https://doi.org/10.1130/GES00520.1.","productDescription":"37 p.","startPage":"93","endPage":"129","costCenters":[],"links":[{"id":475737,"rank":0,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.1130/ges00520.1","text":"Publisher Index Page"},{"id":406178,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California, Nevada","otherGeospatial":"Mesquite Valley, Pahrump Valley","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -115.48553466796874,\n 35.634976650677295\n ],\n [\n -115.52947998046874,\n 35.94688293218141\n ],\n [\n -115.58990478515625,\n 36.089060460282006\n ],\n [\n -115.70251464843749,\n 36.089060460282006\n ],\n [\n -115.76568603515624,\n 36.20882309283712\n ],\n [\n -115.8673095703125,\n 36.20439070158873\n ],\n [\n -115.85906982421874,\n 36.31733823488624\n ],\n [\n -116.01287841796874,\n 36.48976535146369\n ],\n [\n -116.28204345703124,\n 36.28856319836237\n ],\n [\n -116.25457763671875,\n 36.20217441183449\n ],\n [\n -116.16668701171875,\n 36.16005298551354\n ],\n [\n -116.0870361328125,\n 36.00911716117325\n ],\n [\n -116.08154296875001,\n 35.86902116501695\n ],\n [\n -115.94696044921875,\n 35.81558597375359\n ],\n [\n -115.71075439453125,\n 35.7286770448517\n ],\n [\n -115.65856933593749,\n 35.66622234103479\n ],\n [\n -115.48553466796874,\n 35.634976650677295\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"6","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Scheirer, Daniel S. dscheirer@usgs.gov","contributorId":2325,"corporation":false,"usgs":true,"family":"Scheirer","given":"Daniel S.","email":"dscheirer@usgs.gov","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":850772,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Sweetkind, Donald S. 0000-0003-0892-4796 dsweetkind@usgs.gov","orcid":"https://orcid.org/0000-0003-0892-4796","contributorId":139913,"corporation":false,"usgs":true,"family":"Sweetkind","given":"Donald","email":"dsweetkind@usgs.gov","middleInitial":"S.","affiliations":[{"id":318,"text":"Geosciences and Environmental Change Science Center","active":true,"usgs":true}],"preferred":true,"id":850773,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Miller, John J. 0000-0002-9098-0967 jmiller@usgs.gov","orcid":"https://orcid.org/0000-0002-9098-0967","contributorId":3785,"corporation":false,"usgs":true,"family":"Miller","given":"John","email":"jmiller@usgs.gov","middleInitial":"J.","affiliations":[{"id":164,"text":"Central Energy Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":850774,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70155081,"text":"70155081 - 2010 - Abandoned mine drainage in the Swatara Creek Basin, southern anthracite coalfield, Pennsylvania, USA: 1. stream quality trends coinciding with the return of fish","interactions":[],"lastModifiedDate":"2015-07-29T10:43:45","indexId":"70155081","displayToPublicDate":"2010-04-01T00:00:00","publicationYear":"2010","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2745,"text":"Mine Water and the Environment","active":true,"publicationSubtype":{"id":10}},"title":"Abandoned mine drainage in the Swatara Creek Basin, southern anthracite coalfield, Pennsylvania, USA: 1. stream quality trends coinciding with the return of fish","docAbstract":"Acidic mine drainage (AMD) from legacy anthracite mines has contaminated Swatara Creek in eastern Pennsylvania. Intermittently collected base-flow data for 1959–1986 indicate that fish were absent immediately downstream from the mined area where pH ranged from 3.5 to 7.2 and concentrations of sulfate, dissolved iron, and dissolved aluminum were as high as 250, 2.0, and 4.7 mg/L, respectively. However, in the 1990s, fish returned to upper Swatara Creek, coinciding with the implementation of AMD treatment (limestone drains, limestone diversion wells, limestone sand, constructed wetlands) in the watershed. During 1996–2006, as many as 25 species of fish were identified in the reach downstream from the mined area, with base-flow pH from 5.8 to 7.6 and concentrations of sulfate, dissolved iron, and dissolved aluminum as high as 120, 1.2, and 0.43 mg/L, respectively. Several of the fish taxa are intolerant of pollution and low pH, such as river chub (Nocomis icropogon) and longnose dace (Rhinichthys cataractae). Cold-water species such as brook trout (Salvelinus fontinalis) and warm-water species such as rock bass (Ambloplites rupestris) varied in predominance depending on stream flow and stream temperature. Storm flow data for 1996–2007 indicated pH, alkalinity, and sulfate concentrations decreased as the stream flow and associated storm-runoff component increased, whereas iron and other metal concentrations were poorly correlated with stream flow because of hysteresis effects (greater metal concentrations during rising stage than falling stage). Prior to 1999, pH\\5.0 was recorded during several storm events; however, since the implementation of AMD treatments, pH has been maintained near neutral. Flow-adjusted trends for1997–2006 indicated significant increases in calcium; decreases in hydrogen ion, dissolved aluminum, dissolved and total manganese, and total iron; and no change in sulfate or dissolved iron in Swatara Creek immediately downstream from the mined area. The increased pH and calcium from limestone in treatment systems can be important for mitigating toxic effects of dissolved metals. Thus, treatment of AMD during the 1990s improved pH buffering, reduced metals transport, and helped to decrease metals toxicity to fish.
","language":"English","publisher":"Springer","doi":"10.1007/s10230-010-0112-6","usgsCitation":"Cravotta, C., Brightbill, R.A., and Langland, M.J., 2010, Abandoned mine drainage in the Swatara Creek Basin, southern anthracite coalfield, Pennsylvania, USA: 1. stream quality trends coinciding with the return of fish: Mine Water and the Environment, v. 29, no. 3, p. 176-199, https://doi.org/10.1007/s10230-010-0112-6.","productDescription":"24 p.","startPage":"176","endPage":"199","onlineOnly":"N","additionalOnlineFiles":"N","ipdsId":"IP-005668","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":306225,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Pennsylvania","otherGeospatial":"Swatara Creek basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -76.62757873535156,\n 40.42499671108253\n ],\n [\n -76.62757873535156,\n 40.58162765924269\n ],\n [\n -76.32064819335938,\n 40.58162765924269\n ],\n [\n -76.32064819335938,\n 40.42499671108253\n ],\n [\n -76.62757873535156,\n 40.42499671108253\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"29","issue":"3","publishingServiceCenter":{"id":10,"text":"Baltimore PSC"},"noUsgsAuthors":false,"publicationDate":"2010-04-22","publicationStatus":"PW","scienceBaseUri":"55b98fb7e4b08f6647be5168","contributors":{"authors":[{"text":"Cravotta, Charles A. III 0000-0003-3116-4684 cravotta@usgs.gov","orcid":"https://orcid.org/0000-0003-3116-4684","contributorId":138829,"corporation":false,"usgs":true,"family":"Cravotta","given":"Charles A.","suffix":"III","email":"cravotta@usgs.gov","affiliations":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"preferred":false,"id":564782,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Brightbill, Robin A. 0000-0003-4683-9656 rabright@usgs.gov","orcid":"https://orcid.org/0000-0003-4683-9656","contributorId":618,"corporation":false,"usgs":true,"family":"Brightbill","given":"Robin","email":"rabright@usgs.gov","middleInitial":"A.","affiliations":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"preferred":true,"id":564783,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Langland, Michael J. 0000-0002-8350-8779 langland@usgs.gov","orcid":"https://orcid.org/0000-0002-8350-8779","contributorId":2347,"corporation":false,"usgs":true,"family":"Langland","given":"Michael","email":"langland@usgs.gov","middleInitial":"J.","affiliations":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"preferred":true,"id":564784,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70157566,"text":"70157566 - 2010 - Stratigraphy, age, and depositional setting of the Miocene Barstow Formation at Harvard Hill, central Mojave Desert, California","interactions":[],"lastModifiedDate":"2023-05-24T13:21:36.133472","indexId":"70157566","displayToPublicDate":"2010-04-01T00:00:00","publicationYear":"2010","noYear":false,"publicationType":{"id":24,"text":"Conference Paper"},"publicationSubtype":{"id":19,"text":"Conference Paper"},"title":"Stratigraphy, age, and depositional setting of the Miocene Barstow Formation at Harvard Hill, central Mojave Desert, California","docAbstract":"New detailed geologic mapping and geochronology of the Barstow Formation at Harvard Hill, 30 km east of Barstow, CA, help to constrain Miocene paleogeography and tectonics of the central Mojave Desert. A northern strand of the Quaternary ENE-striking, sinistral Manix fault divides the Barstow Formation at Harvard Hill into two distinct lithologic assemblages. Strata north of the fault consist of: a green rhyolitic tuff, informally named the Shamrock tuff; lacustrine sandstone; partially silicified thin-bedded to massive limestone; and alluvial sandstone to pebble conglomerate. Strata south of the fault consist of: lacustrine siltstone and sandstone; a rhyolitic tuff dated at 19.1 Ma (U-Pb); rock-avalanche breccia deposits; partially silicified well-bedded to massive limestone; and alluvial sandstone and conglomerate. Our U-Pb zircon dating of the Shamrock tuff by SHRIMP-RG yields a peak probability age of 18.7 ± 0.1 Ma. Distinctive outcrop characteristics, mineralogy, remanent magnetization, and zircon geochemistry (Th/U) suggest that the Shamrock tuff represents a lacustrine facies of the regionally extensive Peach Spring Tuff (PST). Here we compare zircon age and geochemical analyses from the Shamrock tuff with those of the PST at Stoddard Wash and provide new insight into the age of zircon crystallization in the PST rhyolite. Results of our field studies show that Miocene strata at Harvard Hill mostly accumulated in a lacustrine environment, although depositional environments varied from a relatively deep lake to a very shallow lake or even onshore setting. Rock-avalanche breccias and alluvial deposits near the base of the exposed section indicate proximity to a steep basin margin and detrital studies suggest a southern source for coarse-grained deposits; therefore, we may infer a southern basin-margin setting at Harvard Hill during the early Miocene. Our geochronology demonstrates that deposition of the Barstow Formation at Harvard Hill extended from before ~19.1 Ma until well after ~18.7 Ma, similar to timing of Barstow Formation lake deposition in the Calico Mountains but at least 3 million years older than comparable lacustrine facies in the Mud Hills type section. These observations are consistent with either of two paleogeographic models: westward transgression of lacustrine environments within a single large basin, or sequential development of geographically distinct eastern and western sub-basins.
","largerWorkType":{"id":4,"text":"Book"},"largerWorkTitle":"Overboard in the Mojave: 20 million years of lakes and wetlands","largerWorkSubtype":{"id":12,"text":"Conference publication"},"conferenceTitle":"2010 Desert Symposium","conferenceDate":"April, 2010","language":"English","publisher":"California State University Desert Studies Consortium","usgsCitation":"Leslie, S.R., Miller, D., Wooden, J., and Vazquez, J.A., 2010, Stratigraphy, age, and depositional setting of the Miocene Barstow Formation at Harvard Hill, central Mojave Desert, California, in Overboard in the Mojave: 20 million years of lakes and wetlands, April, 2010, 20 p.","productDescription":"20 p.","onlineOnly":"N","additionalOnlineFiles":"N","ipdsId":"IP-021102","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":308665,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Harvard Hill, Mojave Desert","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -116.66628115139929,\n 34.93378658494973\n ],\n [\n -116.66540100503497,\n 34.934596132280205\n ],\n [\n -116.66527220312803,\n 34.935370474424644\n ],\n [\n -116.66557274091105,\n 34.93593362775644\n ],\n [\n -116.66683929299616,\n 34.93538807302471\n ],\n [\n -116.66829904794145,\n 34.934772119773186\n ],\n [\n -116.66628115139929,\n 34.93378658494973\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"560a64ede4b058f706e536f6","contributors":{"authors":[{"text":"Leslie, Shannon R.","contributorId":148038,"corporation":false,"usgs":false,"family":"Leslie","given":"Shannon","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":573654,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Miller, David M. 0000-0003-3711-0441 dmiller@usgs.gov","orcid":"https://orcid.org/0000-0003-3711-0441","contributorId":1707,"corporation":false,"usgs":true,"family":"Miller","given":"David M.","email":"dmiller@usgs.gov","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":false,"id":573655,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Wooden, Joseph L.","contributorId":32209,"corporation":false,"usgs":true,"family":"Wooden","given":"Joseph L.","affiliations":[],"preferred":false,"id":573656,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Vazquez, Jorge A. 0000-0003-2754-0456 jvazquez@usgs.gov","orcid":"https://orcid.org/0000-0003-2754-0456","contributorId":4458,"corporation":false,"usgs":true,"family":"Vazquez","given":"Jorge","email":"jvazquez@usgs.gov","middleInitial":"A.","affiliations":[{"id":5056,"text":"Office of the AD Energy and Minerals, and Environmental Health","active":true,"usgs":true},{"id":615,"text":"Volcano Hazards Program","active":true,"usgs":true},{"id":617,"text":"Volcano Science Center","active":true,"usgs":true},{"id":501,"text":"Office of Science Quality and Integrity","active":true,"usgs":true}],"preferred":true,"id":573657,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70155086,"text":"70155086 - 2010 - Abandoned mine drainage in the Swatara Creek Basin, southern anthracite coalfield, Pennsylvania, USA: 2. performance of treatment systems","interactions":[],"lastModifiedDate":"2015-07-29T11:13:09","indexId":"70155086","displayToPublicDate":"2010-04-01T00:00:00","publicationYear":"2010","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2745,"text":"Mine Water and the Environment","active":true,"publicationSubtype":{"id":10}},"title":"Abandoned mine drainage in the Swatara Creek Basin, southern anthracite coalfield, Pennsylvania, USA: 2. performance of treatment systems","docAbstract":"A variety of passive and semi-passive treatment systems were constructed by state and local agencies to neutralize acidic mine drainage (AMD) and reduce the transport of dissolved metals in the upper Swatara Creek Basin in the Southern Anthracite Coalfield in eastern Pennsylvania. To evaluate the effectiveness of selected treatment systems installed during 1995–2001, the US Geological Survey collected water-quality data at upstream and downstream locations relative to each system eight or more times annually for a minimum of 3 years at each site during 1996–2007. Performance was normalized among treatment types by dividing the acid load removed by the size of the treatment system. For the limestone sand, open limestone channel, oxic limestone drain, anoxic limestone drain (ALD), and limestone diversion well treatment systems, the size was indicated by the total mass of limestone; for the aerobic wetland systems, the size was indicated by the total surface area of ponds and wetlands. Additionally, the approximate cost per tonne of acid treated over an assumed service life of 20 years was computed. On the basis of these performance metrics, the limestone sand, ALD, oxic limestone drain, and limestone diversion wells had similar ranges of acid-removal efficiency and cost efficiency. However, the open limestone channel had lower removal efficiency and higher cost per ton of acid treated. The wetlands effectively attenuated metals transport but were relatively expensive considering metrics that evaluated acid removal and cost efficiency. Although the water-quality data indicated that all treatments reduced the acidity load from AMD, the ALD was most effective at producing near-neutral pH and attenuating acidity and dissolved metals. The diversion wells were effective at removing acidity and increasing pH of downstream water and exhibited unique potential to treat moderate to high flows associated with storm flow conditions.
","language":"English","publisher":"Springer","doi":"10.1007/s10230-010-0113-5","usgsCitation":"Cravotta, C., 2010, Abandoned mine drainage in the Swatara Creek Basin, southern anthracite coalfield, Pennsylvania, USA: 2. performance of treatment systems: Mine Water and the Environment, v. 29, no. 3, p. 200-216, https://doi.org/10.1007/s10230-010-0113-5.","productDescription":"17 p.","startPage":"200","endPage":"216","onlineOnly":"N","additionalOnlineFiles":"N","ipdsId":"IP-013771","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":306227,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":305713,"type":{"id":15,"text":"Index Page"},"url":"https://link.springer.com/article/10.1007/s10230-010-0113-5"}],"country":"United States","state":"Pennsylvania","otherGeospatial":"Swatara Creek Basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -76.62757873535156,\n 40.42499671108253\n ],\n [\n -76.62757873535156,\n 40.58162765924269\n ],\n [\n -76.32064819335938,\n 40.58162765924269\n ],\n [\n -76.32064819335938,\n 40.42499671108253\n ],\n [\n -76.62757873535156,\n 40.42499671108253\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"29","issue":"3","publishingServiceCenter":{"id":10,"text":"Baltimore PSC"},"noUsgsAuthors":false,"publicationDate":"2010-04-30","publicationStatus":"PW","scienceBaseUri":"55b98fb9e4b08f6647be516b","contributors":{"authors":[{"text":"Cravotta, Charles A. III 0000-0003-3116-4684 cravotta@usgs.gov","orcid":"https://orcid.org/0000-0003-3116-4684","contributorId":138829,"corporation":false,"usgs":true,"family":"Cravotta","given":"Charles A.","suffix":"III","email":"cravotta@usgs.gov","affiliations":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"preferred":false,"id":564788,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70156704,"text":"70156704 - 2010 - Correlation of the Miocene Peach Spring Tuff with the geomagnetic polarity time scale and new constraints on tectonic rotations in the Mojave Desert, California","interactions":[],"lastModifiedDate":"2023-05-24T13:22:17.707589","indexId":"70156704","displayToPublicDate":"2010-04-01T00:00:00","publicationYear":"2010","noYear":false,"publicationType":{"id":24,"text":"Conference Paper"},"publicationSubtype":{"id":19,"text":"Conference Paper"},"title":"Correlation of the Miocene Peach Spring Tuff with the geomagnetic polarity time scale and new constraints on tectonic rotations in the Mojave Desert, California","docAbstract":"We report new paleomagnetic results and 40Ar/39Ar ages from the Peach Spring Tuff (PST), a key marker bed that occurs in the desert region between Barstow, California, and Peach Springs, Arizona. The 40Ar/39Ar ages were determined using individual hand-picked sanidine crystals from ash-flow specimens used in previous paleomagnetic studies at eight sites correlated by mineralogy, stratigraphic position, and magnetic inclination. Site-mean ages, which range from 18.43 Ma to 18.78 Ma with analytical precision (1 s.d.) typically 0.04 Ma, were obtained from areas near Fort Rock, AZ; McCullough Mts, NV; Cima Dome, Parker Dam, Danby, Ludlow, Kane Walsh, and Stoddard Wash, CA. The regional mean age determination is 18.71 ± 0.13 Ma, after the data were selected for sanidine crystals that yielded greater than 90% radiogenic argon (N=40). This age determination is compatible with previous 40Ar/39Ar dating of the PST after taking various neutron-flux monitor calibrations into account. We report paleomagnetic results from eight new sites that bear on reconstructions of the Miocene basins associated with the Hector Formation, Barstow Formation, and similar fine-grained sedimentary deposits in the Barstow region. Key findings of the new paleomagnetic study pertain to age control of the Hector Formation and clockwise rotation of the Northeast Mojave Domain. Our study of a rhyolitic ash flow at Baxter Wash, northern Cady Mountains, confirms the correlation of the PST within the Hector Formation and prompts reinterpretation of the previously determined magnetostratigraphy. Our model correlates the PST to the normal-polarity zone just below the C6-C5E boundary (18.748 Ma) of the astronomically tuned Geomagnetic Polarity Time Scale. After emplacement of the Peach Spring Tuff at Alvord Mountain and the Cady Mountains, the southern part of the Northeast Mojave Domain (between Cady and Coyote Lake faults) underwent clockwise rotation of 30°–55°. Clockwise rotations increase with distance northward from the Cady fault and may reflect Late Miocene and younger accommodation of right-lateral motion across the Eastern California Shear Zone. The new results also expand the area known to be affected by the Peach Springs eruption, and confirm that a pink ash-flow tuff surrounding Daggett Ridge near Barstow is part of the PST.
","largerWorkType":{"id":4,"text":"Book"},"largerWorkTitle":"Overboard in the Mojave: 20 million years of lakes and wetlands","largerWorkSubtype":{"id":12,"text":"Conference publication"},"conferenceTitle":"Overboard in the Mojave: 20 million years of lakes and wetlands","conferenceDate":"April, 2010","conferenceLocation":"Fullerton, CA","language":"English","publisher":"California State University Desert Studies Consortium","usgsCitation":"Hillhouse, J.W., Miller, D., and Turrin, B., 2010, Correlation of the Miocene Peach Spring Tuff with the geomagnetic polarity time scale and new constraints on tectonic rotations in the Mojave Desert, California, in Overboard in the Mojave: 20 million years of lakes and wetlands, Fullerton, CA, April, 2010, p. 105-121.","productDescription":"17 p.","startPage":"105","endPage":"121","onlineOnly":"N","additionalOnlineFiles":"N","ipdsId":"IP-021139","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":307553,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":307552,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://biology.fullerton.edu/facilities/dsc/school/symposium.html"}],"country":"United States","state":"Arizona, California, Nevada","otherGeospatial":"Mojave Desert","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -117.476806640625,\n 34.016241889667015\n ],\n [\n -111.939697265625,\n 34.016241889667015\n ],\n [\n -111.939697265625,\n 37.53586597792038\n ],\n [\n -117.476806640625,\n 37.53586597792038\n ],\n [\n -117.476806640625,\n 34.016241889667015\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"55dee32ee4b0518e354e0801","contributors":{"authors":[{"text":"Hillhouse, John W. 0000-0002-1371-4622 jhillhouse@usgs.gov","orcid":"https://orcid.org/0000-0002-1371-4622","contributorId":2618,"corporation":false,"usgs":true,"family":"Hillhouse","given":"John","email":"jhillhouse@usgs.gov","middleInitial":"W.","affiliations":[],"preferred":true,"id":570165,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Miller, David M. 0000-0003-3711-0441 dmiller@usgs.gov","orcid":"https://orcid.org/0000-0003-3711-0441","contributorId":1707,"corporation":false,"usgs":true,"family":"Miller","given":"David M.","email":"dmiller@usgs.gov","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":false,"id":570166,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Turrin, Brent D.","contributorId":89867,"corporation":false,"usgs":true,"family":"Turrin","given":"Brent D.","affiliations":[],"preferred":false,"id":570167,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ]}