Irondequoit Creek drains 169 square miles in the eastern part of Monroe County. Nutrients transported by Irondequoit Creek to Irondequoit Bay on Lake Ontario have contributed to the eutrophication of the Bay. Sewage-treatment-plant effluent, a major source of nutrients to the creek and its tributaries, was eliminated from the basin in 1979 by diversion to a regional wastewater-treatment facility, but sediment and contaminants from nonpoint sources continue to enter the creek and Irondequoit Bay.
This report analyzes data from five surface-water monitoring sites in the Irondequoit Creek basin. Irondequoit Creek at Railroad Mills, East Branch Allen Creek at Pittsford, Allen Creek near Rochester, Irondequoit Creek at Blossom Road, and Irondequoit Creek at Empire Boulevard. It is the third in a series of reports that present interpretive analyses of the hydrologic data collected in Monroe County since 1984. Also included are data from a site on Northrup Creek, which drains a 23.5-square-mile basin west of the Genesee River in western Monroe County, to provide information on surface-water quality in a stream west of the Genesee River and on loads of nutrients delivered to Long Pond, a small eutrophic embayment of Lake Ontario, and data from the Genesee River for comparison of historical water-quality conditions with 1994-96 conditions. Water-level and water-quality data from nine observation wells in Ellison Park, and atmospheric-deposition data from Mendon Ponds, also are included.
Average annual yields of chemical constituents from atmospheric deposition for 1994-96 were generally similar to those for the previous 10 years (1984-93), except for dissolved sodium, dissolved potassium, total phosphorus, and orthophosphate, which ranged from 42 percent (dissolved sodium) to 275 percent (dissolved potassium) greater than during 1984-93, and dissolved sulfate and ammonia, which were about 30 percent less than in 1984-93.
Loads of all nutrients deposited in the Irondequoit Creek basin from atmospheric sources during water years 1994-96 exceeded those removed by Irondequoit Creek at Blossom Road—ammonia by 5,600 percent, orthophosphate by 2,500 percent, ammonia + organic nitrogen by 350 percent, total phosphorus by 300 percent and nitrite + nitrate by 140 percent. Average yields of dissolved chloride and dissolved sulfate from atmospheric deposition were much less than those transported in streamflow—yields of dissolved chloride from atmospheric sources were only 1.9 percent, and yields of sulfate were only 9.2 percent, of those transported in streamflow at Blossom Road.
Concentrations of several chemical constituents in streams of the Irondequoit Creek basin showed statistically significant trends from the beginning of their period of record through 1996. The constituents that showed the greatest number of statistically significant trends were dissolved chloride, ammonia, and ammonia + organic nitrogen. Dissolved chloride showed an upward trend at Blossom Road, Allen Creek, and Empire Boulevard and a downward trend at Railroad Mills. Ammonia showed downward trends at Allen Creek, Blossom Road and Railroad Mills. Ammonia + organic nitrogen showed a downward trend at Allen Creek, Blossom Road, and Empire Boulevard. Nitrite + nitrate showed a downward trend at Allen Creek, and orthophosphate showed an upward trend at that site. Turbidity and total suspended solids showed a downward trend at Empire Boulevard. Neither total phosphorus nor volatile suspended solids showed statistically significant trends in concentration at any of the Irondequoit basin sites.
Northrup Creek showed a downward trend in total suspended solids and ammonia + organic nitrogen, and an upward trend in dissolved chloride. The Genesee River showed a downward trend in ammonia + organic nitrogen and chloride, and an upward trend in orthophosphate.
Most constituents for the 1994-96 water years showed lower average yields at Blossom Road than for the 1989-93 water years, but dissolved chloride showed higher yields for the 1994-96 water years at all sites except Blossom Road. Ammonia + organic nitrogen and total phosphorus showed a decrease in yield at all sites after 1993, and nitrite + nitrate showed slightly higher yields for 1994-96 at the upstream, predominantly rural sites, and lower yields at the downstream, more urban sites, than during 1989-93.
The trends and changes in surface-water quality after 1993 can be attributed to several factors within the basin, including land-use changes, annual and seasonal variations in streamflow, and year-to-year variations in the application of deicing salts on area roads. Statistical analyses of long-term (9 years or more) streamflow records of three unregulated streams in Monroe County indicate that annual mean flows for water years 1994-96 were in the normal range (75th to 25th percentile), although Allen Creek showed a statistically significant downward trend in monthly mean streamflow over the 1984-96 water years.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri004201","collaboration":"Prepared in cooperation with the Monroe County Department of Health","usgsCitation":"Sherwood, D.A., 2001, Water resources of Monroe County, New York, water years 1994-96, with emphasis on water quality in the Irondequoit Creek basin: Atmospheric deposition, ground water, streamflow, trends in water quality, and chemical loads to Irondequoit Bay: U.S. Geological Survey Water-Resources Investigations Report 2000-4201, vi, 39 p., https://doi.org/10.3133/wri004201.","productDescription":"vi, 39 p.","onlineOnly":"N","costCenters":[{"id":474,"text":"New York Water Science Center","active":true,"usgs":true}],"links":[{"id":401888,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_37344.htm","linkFileType":{"id":5,"text":"html"}},{"id":324245,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2000/4201/wri20004201.pdf","text":"Report","linkFileType":{"id":1,"text":"pdf"},"description":"WRI 2000-4201"},{"id":161468,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/2000/4201/coverthb.jpg"}],"country":"United States","state":"New York","county":"Monroe County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-77.3792,43.2748],[-77.3756,43.1898],[-77.3731,43.1221],[-77.3719,43.0329],[-77.4866,43.0321],[-77.4822,42.9431],[-77.5805,42.9438],[-77.635,42.9443],[-77.6374,42.9397],[-77.7582,42.9404],[-77.7602,42.9426],[-77.7583,42.9445],[-77.7527,42.9455],[-77.747,42.9438],[-77.7378,42.9476],[-77.7321,42.9449],[-77.7309,42.9468],[-77.7343,42.9549],[-77.7311,42.9554],[-77.7279,42.9532],[-77.7244,42.9592],[-77.7265,42.9655],[-77.7235,42.9719],[-77.7185,42.9715],[-77.718,42.9738],[-77.7213,42.9797],[-77.7326,42.9818],[-77.731,42.9882],[-77.9101,42.9877],[-77.9098,43.0141],[-77.9068,43.0369],[-77.9527,43.0392],[-77.9083,43.132],[-77.9981,43.1321],[-77.9985,43.2818],[-77.9959,43.3656],[-77.9921,43.3657],[-77.9877,43.3662],[-77.9827,43.3677],[-77.9771,43.3687],[-77.9701,43.3679],[-77.9562,43.3668],[-77.9365,43.3626],[-77.9327,43.3604],[-77.9251,43.3587],[-77.9168,43.3575],[-77.908,43.3572],[-77.9004,43.3565],[-77.8985,43.3551],[-77.894,43.3534],[-77.8902,43.3526],[-77.8737,43.3501],[-77.8592,43.3486],[-77.8523,43.3487],[-77.8333,43.3458],[-77.8149,43.343],[-77.7909,43.3398],[-77.7827,43.3394],[-77.777,43.34],[-77.7733,43.341],[-77.7702,43.3415],[-77.7677,43.3424],[-77.7645,43.3425],[-77.7594,43.3412],[-77.755,43.339],[-77.7486,43.3355],[-77.7409,43.3329],[-77.7339,43.3316],[-77.725,43.3277],[-77.7186,43.3255],[-77.7148,43.3233],[-77.7128,43.3202],[-77.7121,43.3179],[-77.712,43.3161],[-77.712,43.3147],[-77.7126,43.3147],[-77.7145,43.3147],[-77.7152,43.3165],[-77.7178,43.3183],[-77.7216,43.3191],[-77.7247,43.3186],[-77.7278,43.3176],[-77.7291,43.3172],[-77.7284,43.3158],[-77.7252,43.3154],[-77.7214,43.3145],[-77.7189,43.3137],[-77.7176,43.3123],[-77.7181,43.3105],[-77.7181,43.3092],[-77.7105,43.3079],[-77.7079,43.307],[-77.7074,43.3084],[-77.7087,43.3102],[-77.7081,43.3107],[-77.7049,43.3098],[-77.6953,43.3041],[-77.676,43.2916],[-77.6619,43.2832],[-77.6555,43.2797],[-77.6479,43.2775],[-77.639,43.275],[-77.6243,43.2679],[-77.6166,43.2635],[-77.6032,43.256],[-77.5821,43.2463],[-77.5643,43.2393],[-77.5535,43.2367],[-77.5428,43.2351],[-77.539,43.2356],[-77.5359,43.2356],[-77.5272,43.2385],[-77.5135,43.2451],[-77.508,43.2479],[-77.5055,43.2489],[-77.5017,43.2494],[-77.4973,43.249],[-77.4873,43.2505],[-77.4779,43.2538],[-77.4717,43.2562],[-77.4586,43.2587],[-77.4448,43.2616],[-77.4318,43.2673],[-77.4262,43.2701],[-77.4199,43.2697],[-77.4105,43.2703],[-77.403,43.2713],[-77.3961,43.2746],[-77.3886,43.2761],[-77.3792,43.2748]]]},\"properties\":{\"name\":\"Monroe\",\"state\":\"NY\"}}]}","contact":"Director, New York Water Science Center
U.S. Geological Survey
425 Jordan Rd
Troy, NY 12180
(518) 285-5695
http://ny.water.usgs.gov/
The stage of Lake Brooklyn, in southwestern Clay County, Florida, has varied over a range of 27 feet since measurements by the U.S. Geological Survey began in July 1957. The large stage changes have been attributed to the relation between highly transient surface-water inflow to the lake and subsurface conduits of karstic origin that permit a high rate of leakage from the lake to the Upper Floridan aquifer. After the most recent and severe stage decline (1990-1994), the U.S. Geological Survey began a study that entailed the use of numerical ground-water flow models to simulate the interaction of the lake with the Upper Floridan aquifer and the large fluctuations of stage that were a part of that process. A package (set of computer programs) designed to represent lake/aquifer interaction in the U.S. Geological Survey Modular Finite-Difference Ground-Water Flow Model (MODFLOW-96) and the Three-Dimensional Method-of-Characteristics Solute-Transport Model (MOC3D) simulators was prepared as part of this study, and a demonstration of its capability was a primary objective of the study. (Although the official names are Brooklyn Lake and Magnolia Lake (Florida Geographic Names), in this report the local names, Lake Brooklyn and Lake Magnolia, are used.)
In the simulator of lake/aquifer interaction used in this investigation, the stage of each lake in a simulation is updated in successive time steps by a budget process that takes into account ground-water seepage, precipitation upon and evaporation from the lake surface, stream inflows and outflows, overland runoff inflows, and augmentation or depletion by artificial means. The simulator was given the capability to simulate both the division of a lake into separate pools as lake stage falls and the coalescence of several pools into a single lake as the stage rises. This representational capability was required to simulate Lake Brooklyn, which can divide into as many as 10 separate pools at sufficiently low stage.
In the first of two calibrated models, recharge to the water table, specified as a monthly rate, was set equal to 40 percent of the monthly rainfall rate. The specified rate of inflow to the uppermost stream segment was set equal to outflows from Lake Lowry estimated from lake stage and the 1994-97 rating table. Leakage to the intermediate and Upper Floridan aquifers was assumed to occur from the surficial aquifer system through the confining layers directly beneath deeper parts of the lake bottom. A leakance coefficient value of 0.001 feet per day per foot of thickness was used beneath Lake Magnolia, and a value of 0.005 feet per day per foot of thickness was used beneath most of Lake Brooklyn. With these values, the conductance through the confining layers beneath Lake Brooklyn was about 19 times that beneath Lake Magnolia.
The simulated stages of Lake Brooklyn matched the measured stages reasonably well in the early (1957-72) and later (1990-98) parts of the simulation time period, but the match was unsatisfactory in an intermediate time period (1973-89). To resolve this discrepancy, the hypothesis was proposed that undocumented losses of water from Alligator Creek upstream from Lake Brooklyn or from the lake itself occurred between 1973 and 1989 when there was sufficient streamflow. The resulting simulation of lake stages matched the measured lake stages accurately during the entire simulation time period. The model was then revised to incorporate the assumption that only 20 percent of precipitation recharged the water table (the second calibrated model). Recalibration of the model required that leakance values for the confining units under deeper parts of the lakes also be reduced by nearly 50 percent. The stages simulated with the new parameter assumptions, but retaining the assumption of surface-water losses, were an excellent match of the measured values. The stage of Lake Magnolia was also simulated accurately. The results of sensitivity analyses show that simulated streamflow between Lakes Magnolia and Brooklyn tends to be water-budget controlled, and is not appreciably affected by the specified outflow altitude or channel characteristics of the receiving stream.
To match heads measured in observation wells of the surficial aquifer network, the assigned hydraulic conductivity values were zoned, and ranged from a minimum of 4 feet per day to a maximum of 400 feet per day in the first calibrated model. These values were reduced by about 50 percent in the second calibrated model. Differences between observation wells were noted in the abruptness of changes of measured head values, and in the relation of the timing of peak measured heads and simulated peak heads. These differences seemed to be correlated with the depth of the water table below land surface. Spatially uniform values of transmissivity were specified for the intermediate (10,000 feet squared per day) and Upper Floridan (100,000 feet squared per day) aquifers. Simulated heads in the Upper Floridan aquifer layer follow the trend of the heads measured in a long-term observation well with data beginning in 1960. This result suggests that the observed head decline could be explained entirely in terms of the stage decline in Lake Brooklyn and may not indicate a regional trend.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri004204","usgsCitation":"Merritt, M.L., 2001, Simulation of the interaction of karstic lakes Magnolia and Brooklyn with the upper Floridan Aquifer, southwestern Clay County, Florida: U.S. Geological Survey Water-Resources Investigations Report 2000-4204, vi, 62 p., https://doi.org/10.3133/wri004204.","productDescription":"vi, 62 p.","costCenters":[],"links":[{"id":161469,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":415188,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_37335.htm","linkFileType":{"id":5,"text":"html"}},{"id":2785,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri00-4204/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Florida","county":"Clay County","otherGeospatial":"Lake Brooklyn, Lake Magnolila","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -82.0833,\n 29.833\n ],\n [\n -82.0833,\n 29.783\n ],\n [\n -82,\n 29.783\n ],\n [\n -82,\n 29.833\n ],\n [\n -82.0833,\n 29.833\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f7e4b07f02db5f1fcd","contributors":{"authors":[{"text":"Merritt, M. L.","contributorId":47401,"corporation":false,"usgs":true,"family":"Merritt","given":"M.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":204252,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":31212,"text":"ofr0135 - 2001 - Hydraulic and mechanical properties affecting ground-water flow and aquifer-system compaction, San Joaquin Valley, California","interactions":[],"lastModifiedDate":"2012-02-02T00:09:06","indexId":"ofr0135","displayToPublicDate":"2001-07-01T00:00:00","publicationYear":"2001","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":"2001-35","title":"Hydraulic and mechanical properties affecting ground-water flow and aquifer-system compaction, San Joaquin Valley, California","docAbstract":"This report summarizes hydraulic and mechanical properties affecting ground-water flow and aquifer-system compaction in the San Joaquin Valley, a broad alluviated intermontane structural trough that constitutes the southern two-thirds of the Central Valley of California. These values will be used to constrain a coupled ground-water flow and aquifer-system compaction model of the western San Joaquin Valley called WESTSIM. A main objective of the WESTSIM model is to evaluate potential future land subsidence that might occur under conditions in which deliveries of imported surface water for agricultural use are reduced and ground-water pumping is increased. Storage values generally are components of the total aquifer-system storage and include inelastic and elastic skeletal storage values of the aquifers and the aquitards that primarily govern the potential amount of land subsidence. Vertical hydraulic conductivity values generally are for discrete thicknesses of sediments, usually aquitards, that primarily govern the rate of land subsidence. The data were compiled from published sources and include results of aquifer tests, stress-strain analyses of borehole extensometer observations, laboratory consolidation tests, and calibrated models of aquifer-system compaction.","language":"ENGLISH","doi":"10.3133/ofr0135","usgsCitation":"Sneed, M., 2001, Hydraulic and mechanical properties affecting ground-water flow and aquifer-system compaction, San Joaquin Valley, California: U.S. Geological Survey Open-File Report 2001-35, 26 p., https://doi.org/10.3133/ofr0135.","productDescription":"26 p.","costCenters":[],"links":[{"id":2745,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/ofr01035","linkFileType":{"id":5,"text":"html"}},{"id":160887,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a51e4b07f02db629b78","contributors":{"authors":[{"text":"Sneed, Michelle 0000-0002-8180-382X micsneed@usgs.gov","orcid":"https://orcid.org/0000-0002-8180-382X","contributorId":155,"corporation":false,"usgs":true,"family":"Sneed","given":"Michelle","email":"micsneed@usgs.gov","affiliations":[{"id":154,"text":"California Water Science Center","active":true,"usgs":true}],"preferred":true,"id":205335,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":30906,"text":"wri014041 - 2001 - Modeling water quality in the Tualatin River, Oregon, 1991-1997","interactions":[],"lastModifiedDate":"2017-02-07T09:12:57","indexId":"wri014041","displayToPublicDate":"2001-07-01T00:00:00","publicationYear":"2001","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2001-4041","title":"Modeling water quality in the Tualatin River, Oregon, 1991-1997","docAbstract":"The calibration of a model of flow, temperature, and water quality in the Tualatin River, Oregon, originally calibrated for the summers of 1991 through 1993, was extended to the summers of 1991 through 1997. The model is now calibrated for a total period of 42 months during the May through October periods of 7 hydrologically distinct years. Based on a modified version of the U.S. Army Corps of Engineers model CE-QUAL-W2, this model provides a good fit to the measured data for streamflow, water temperature, and water quality constituents such as chloride, ammonia, nitrate, total phosphorus, orthophosphate, phytoplankton, and dissolved oxygen. In particular, the model simulates ammonia concentrations and the effects of instream ammonia nitrification very well, which is critical to ongoing efforts to revise ammonia regulations for the Tualatin River. In addition, the model simulates the timing, duration, and relative size of algal blooms with sufficient accuracy to provide important insights for regulators and managers of this river.Efforts to limit the size of algal blooms through phosphorus control measures are apparent in the model simulations, which show this limitation on algal growth. Such measures are largely responsible for avoiding violations of the State of Oregon maximum pH standard of 8.5 in recent years, but they have not yet reduced algal biomass levels below the State of Oregon nuisance phytoplankton growth guideline of 15 ?g/L chlorophyll-a.Most of the dynamics of the instream dissolved oxygen concentrations are captured by the model. About half of the error in the simulated dissolved oxygen concentrations is directly attributable to error in the size of the simulated phytoplankton population. To achieve greater accuracy in simulating dissolved oxygen, therefore, it will be necessary to increase accuracy in the simulation of Tualatin River phytoplankton.Future efforts may include the introduction of multiple algal groups in the model. This model of the Tualatin River continues to be used as a quantitative tool to aid in the management of this important resource.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Portland, OR","doi":"10.3133/wri014041","collaboration":"Prepared in cooperation with the Unified Sewerage Agency of Washington County, Oregon","usgsCitation":"Rounds, S.A., and Wood, T.M., 2001, Modeling water quality in the Tualatin River, Oregon, 1991-1997: U.S. Geological Survey Water-Resources Investigations Report 2001-4041, v, 53 p., https://doi.org/10.3133/wri014041.","productDescription":"v, 53 p.","numberOfPages":"60","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":518,"text":"Oregon Water Science Center","active":true,"usgs":true}],"links":[{"id":160731,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/wri014041.PNG"},{"id":311371,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2001/4041/report.pdf","text":"Report","linkFileType":{"id":1,"text":"pdf"},"description":"Report"}],"country":"United States","state":"Oregon","otherGeospatial":"Tualaltin River","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -91.1700439453125,\n 32.55144352864431\n ],\n [\n -91.1700439453125,\n 32.55144352864431\n ],\n [\n -91.16455078125,\n 32.55144352864431\n ],\n [\n -91.16455078125,\n 32.55144352864431\n ],\n [\n -91.1700439453125,\n 32.55144352864431\n ]\n ]\n ]\n }\n },\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -123.57421875,\n 45.00365115687189\n ],\n [\n -123.57421875,\n 45.85176048817254\n ],\n [\n -122.178955078125,\n 45.85176048817254\n ],\n [\n -122.178955078125,\n 45.00365115687189\n ],\n [\n -123.57421875,\n 45.00365115687189\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b05e4b07f02db699763","contributors":{"authors":[{"text":"Rounds, Stewart A. 0000-0002-8540-2206 sarounds@usgs.gov","orcid":"https://orcid.org/0000-0002-8540-2206","contributorId":905,"corporation":false,"usgs":true,"family":"Rounds","given":"Stewart","email":"sarounds@usgs.gov","middleInitial":"A.","affiliations":[{"id":518,"text":"Oregon Water Science Center","active":true,"usgs":true}],"preferred":true,"id":204329,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wood, Tamara M. 0000-0001-6057-8080 tmwood@usgs.gov","orcid":"https://orcid.org/0000-0001-6057-8080","contributorId":1164,"corporation":false,"usgs":true,"family":"Wood","given":"Tamara","email":"tmwood@usgs.gov","middleInitial":"M.","affiliations":[{"id":518,"text":"Oregon Water Science Center","active":true,"usgs":true}],"preferred":true,"id":204330,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":31229,"text":"ofr0167 - 2001 - A comparative analysis of hazard models for predicting debris flows in Madison County, Virginia","interactions":[],"lastModifiedDate":"2021-12-01T22:24:22.681164","indexId":"ofr0167","displayToPublicDate":"2001-07-01T00:00:00","publicationYear":"2001","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":"2001-67","title":"A comparative analysis of hazard models for predicting debris flows in Madison County, Virginia","docAbstract":"During the rainstorm of June 27, 1995, roughly 330-750 mm of rain fell within a sixteen-hour period, initiating floods and over 600 debris flows in a small area (130 km2) of Madison County, Virginia. Field studies showed that the majority (70%) of these debris flows initiated with a thickness of 0.5 to 3.0 m in colluvium on slopes from 17 o to 41 o (Wieczorek et al., 2000). This paper evaluated and compared the approaches of SINMAP, LISA, and Iverson's (2000) transient response model for slope stability analysis by applying each model to the landslide data from Madison County. Of these three stability models, only Iverson's transient response model evaluated stability conditions as a function of time and depth. Iverson?s model would be the preferred method of the three models to evaluate landslide hazards on a regional scale in areas prone to rain-induced landslides as it considers both the transient and spatial response of pore pressure in its calculation of slope stability. The stability calculation used in SINMAP and LISA is similar and utilizes probability distribution functions for certain parameters. Unlike SINMAP that only considers soil cohesion, internal friction angle and rainfall-rate distributions, LISA allows the use of distributed data for all parameters, so it is the preferred model to evaluate slope stability over SINMAP. Results from all three models suggested similar soil and hydrologic properties for triggering the landslides that occurred during the 1995 storm in Madison County, Virginia. The colluvium probably had cohesion of less than 2KPa. The root-soil system is above the failure plane and consequently root strength and tree surcharge had negligible effect on slope stability. The result that the final location of the water table was near the ground surface is supported by the water budget analysis of the rainstorm conducted by Smith et al. (1996).","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr0167","usgsCitation":"Morrissey, M.M., Wieczorek, G.F., and Morgan, B.A., 2001, A comparative analysis of hazard models for predicting debris flows in Madison County, Virginia (Version 1.0): U.S. Geological Survey Open-File Report 2001-67, HTML Document; CD-ROM, https://doi.org/10.3133/ofr0167.","productDescription":"HTML Document; CD-ROM","costCenters":[],"links":[{"id":161344,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":392351,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_37337.htm"},{"id":2799,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2001/ofr-01-0067/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Virginia","county":"Madison County","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -78.5,\n 38.333\n ],\n [\n -78.333,\n 38.333\n ],\n [\n -78.333,\n 38.55\n ],\n [\n -78.5,\n 38.55\n ],\n [\n -78.5,\n 38.333\n ]\n ]\n ]\n }\n }\n ]\n}","edition":"Version 1.0","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53cd4993e4b0b290850ef46c","contributors":{"authors":[{"text":"Morrissey, Meghan M.","contributorId":98765,"corporation":false,"usgs":true,"family":"Morrissey","given":"Meghan","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":205390,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wieczorek, Gerald F.","contributorId":81889,"corporation":false,"usgs":true,"family":"Wieczorek","given":"Gerald","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":205389,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Morgan, Benjamin A.","contributorId":32158,"corporation":false,"usgs":true,"family":"Morgan","given":"Benjamin","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":205388,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":31252,"text":"ofr01102 - 2001 - Vegetative resistance to flow in South Florida: Summary of vegetation sampling in Taylor Slough, Everglades National Park, September 1997–July 1998","interactions":[],"lastModifiedDate":"2025-04-23T15:55:32.798402","indexId":"ofr01102","displayToPublicDate":"2001-07-01T00:00:00","publicationYear":"2001","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":"2001-102","title":"Vegetative resistance to flow in South Florida: Summary of vegetation sampling in Taylor Slough, Everglades National Park, September 1997–July 1998","docAbstract":"The U.S. Geological Survey is one of many agencies providing scientific support to the effort to restore the South Florida Everglades. In September and November 1997 and July 1998, vegetation was sampled at selected sites in the Everglades as part of a study to quantify vegetative resistance to flow. The objectives of the vegetation sampling are (1) to provide detailed information on species composition, vegetation characteristics, and biomass for quantification of the effect of vegetation on water flow, and (2) to use these data in the future to infer flow resistance from vegetation information. Forty-two vegetation quadrats were sampled in Taylor Slough to determine the number and width of stems and leaves and the biomass of live and dead standing sawgrass, rush, and other plants, and the biomass of dead litter and periphyton. The samples were grouped into ten vegetation classes based on species composition and total biomass minus periphyton biomass.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr01102","productDescription":"vii, 59 p.","costCenters":[{"id":27821,"text":"Caribbean-Florida Water Science Center","active":true,"usgs":true}],"links":[{"id":391837,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_40461.htm"},{"id":160866,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/2001/0102/report-thumb.jpg"},{"id":59712,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2001/0102/report.pdf","text":"Report","size":"9 MB","linkFileType":{"id":1,"text":"pdf"},"description":"OFR 2001-102"}],"country":"United States","state":"Florida","otherGeospatial":"Everglades National Park, Taylor Slough","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -80.833,\n 25.167\n ],\n [\n -80.467,\n 25.167\n ],\n [\n -80.467,\n 25.417\n ],\n [\n -80.833,\n 25.417\n ],\n [\n -80.833,\n 25.167\n ]\n ]\n ]\n }\n }\n ]\n}","contact":"Caribbean-Florida Water Science Center
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As of September 30, 1999, the surface-water data-collection network of Texas (table 1) included 321 continuous-record streamflow stations (D), 20 continuous-record gage-height only stations (G), 24 crest-stage partial-record stations (C), 40 floodhydrograph partial-record stations (H), 25 low-flow partial-record stations (L), 1 continuous-record temperature station (M1), 25 continuous-record temperature and specific conductance stations (M2), 17 continuous-record temperature, specific conductance, dissolved oxygen, and pH stations (M4), 4 daily water-quality stations (Qd), 115 periodic water-quality stations (Qp), 17 reservoir/lake surveys for water quality stations (Qs), 85 continuous or daily reservoircontent stations (R), and 10 daily precipitation stations (Pd). Plate 1 identifies the major river basins in Texas and shows the location of the stations listed in table 1.
Table 1 shows the station number and name, latitude and longitude, type of station, and office responsible for the collection of the data and maintenance of the record. An 8-digit permanent numerical designation for all gaging stations has been adopted on a nationwide basis; stations are numbered and listed in downstream order. In the downstream direction along the main stem, all stations on a tributary entering between two main-stem stations are listed between these two stations. A similar order is followed in listing stations by first rank, second rank, and other ranks of tributaries. The rank of any tributary, with respect to the stream to which it is an immediate tributary, is indicated by an indention in the table. Each indention represents one rank. This downstream order and system of indention shows which gaging stations are on tributaries between any two stations on a main stem and the rank of the tributary on which each gaging station is situated.
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\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49fae4b07f02db5f4253","contributors":{"compilers":[{"text":"Gandara, Susan C.","contributorId":178740,"corporation":false,"usgs":true,"family":"Gandara","given":"Susan","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":662860,"contributorType":{"id":3,"text":"Compilers"},"rank":1},{"text":"Barbie, Dana L.","contributorId":64632,"corporation":false,"usgs":true,"family":"Barbie","given":"Dana","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":662861,"contributorType":{"id":3,"text":"Compilers"},"rank":2}]}} ,{"id":30861,"text":"wri004070 - 2001 - Use of borehole and surface geophysics to investigate ground-water quality near a road-deicing salt-storage facility, Valparaiso, Indiana","interactions":[],"lastModifiedDate":"2019-04-15T09:01:17","indexId":"wri004070","displayToPublicDate":"2001-06-01T00:00:00","publicationYear":"2001","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2000–4070","displayTitle":"Use of borehole and surface geophysics to investigate ground-water quality near a road-deicing salt-storage facility, Valparaiso, Indiana","title":"Use of borehole and surface geophysics to investigate ground-water quality near a road-deicing salt-storage facility, Valparaiso, Indiana","docAbstract":"Borehole and surface geophysics were used to investigate ground-water quality affected by a road-deicing salt-storage facility located near a public water-supply well field. From 1994 through 1998, borehole geophysical logs were made in an existing network of monitoring wells completed near the bottom of a thick sand aquifer. Logs of natural gamma activity indicated a uniform and negligible contribution of clay to the electromagnetic conductivity of the aquifer so that the logs of electromagnetic conductivity primarily measured the amount of dissolved solids in the ground water near the wells. Electromagnetic-conductivity data indicated the presence of a saltwater plume near the bottom of the aquifer. Increases in electromagnetic conductivity, observed from sequential logging of wells, indicated the saltwater plume had moved north about 60 to 100 feet per year between 1994 and 1998. These rates were consistent with estimates of horizontal ground-water flow based on velocity calculations made with hydrologic data from the study area.
Ratios of chloride to bromide concentrations in water samples were used to distinguish sources of chloride in the ground water?whether from road-deicing salt, domestic wastewater, or natural occurrences. Water samples identified with the chloride/bromide ratios as being affected by road-deicing salt had concentrations of dissolved solids, chloride, and sodium many times the background levels for the study area. The largest concentrations were in water from wells near the salt-storage facility?12,400 to 12,800 milligrams per liter (mg/L) dissolved solids, 6,730 to 7,230 mg/L chloride, and 3,690 to 4,400 mg/L sodium.
A conceptual, multi-layer model was developed to describe the vertical extent of the saltwater plume in the vicinity of the monitoring wells. A relation was derived between average borehole electromagnetic conductivity in the screened interval of the wells in the saltwater plume and concentrations of dissolved solids in water samples from those wells. This relation was used in the model to show borehole electromagnetic conductivity in transects of wells as a zone of saline water overlain by zones of brackish water and freshwater. The thickness and altitude of the zones of saline and brackish water decreased with increased distance from the salt-storage facility.
Two surface surveys of terrain electromagnetic conductivity were used to map the horizontal extent of the saltwater plume in areas without monitoring wells. Background values of terrain conductivity were measured in an area where water-quality and borehole geophysical data did not indicate saline or brackish water. Based on a guideline from previous case studies, the boundaries of the saltwater plume were mapped where terrain conductivity was 1.5 times background. The extent of the saltwater plume, based on terrain conductivity, generally was consistent with the available water-quality and borehole electromagnetic-conductivity data and with directions of ground-water flow determined from water-level altitudes.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Indianapolis, IN","doi":"10.3133/wri004070","usgsCitation":"Risch, M., and Robinson, B., 2001, Use of borehole and surface geophysics to investigate ground-water quality near a road-deicing salt-storage facility, Valparaiso, Indiana: U.S. Geological Survey Water-Resources Investigations Report 2000–4070, Report: vi, 63 p., https://doi.org/10.3133/wri004070.","productDescription":"Report: vi, 63 p.","numberOfPages":"71","onlineOnly":"Y","additionalOnlineFiles":"N","costCenters":[{"id":346,"text":"Indiana Water Science Center","active":true,"usgs":true}],"links":[{"id":2737,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2000/4070/wri20004070.pdf","text":"Report","size":"4.04 MB","linkFileType":{"id":1,"text":"pdf"},"description":"WRI 2000-4070"},{"id":160294,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/2000/4070/coverthb.jpg"}],"country":"United States","state":"Indiana","county":"Porter County","city":"Valparaiso","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-85.9369,39.9272],[-85.9379,39.87],[-85.9541,39.8696],[-85.9518,39.6969],[-85.9523,39.638],[-86.248,39.6335],[-86.3268,39.6318],[-86.3281,39.8526],[-86.328,39.8662],[-86.325,39.8662],[-86.3267,39.9238],[-86.2967,39.9246],[-86.2757,39.925],[-86.2385,39.9259],[-85.9801,39.9269],[-85.9411,39.9272],[-85.9369,39.9272]]]},\"properties\":{\"name\":\"Marion\",\"state\":\"IN\"}}]}","contact":"Director, Indiana Water Science Center
U.S. Geological Survey
5957 Lakeside Blvd.
Indianapolis, IN 46278
Caribbean-Florida Water Science Center
U.S. Geological Survey
3321 College Avenue
Davie, FL 33314
The collection of nine papers that follow continue the series of U.S. Geological Survey (USGS) investigative reports in Alaska under the broad umbrella of the geologic sciences. The series presents new and sometimes preliminary findings that are of interest to earth scientists in academia, government, and industry; to land and resource managers; and to the general public. Reports presented in Geologic Studies in Alaska cover a broad spectrum of topics from various parts of the State (fig. 1), serving to emphasize the diversity of USGS efforts to meet the Nation's needs for earth-science information in Alaska.
\nThe papers in this volume are organized under the topics: Hazards, Geologic Framework, Environment and Climate, and Resources. This organization is intended to reflect the scope and objectives of USGS geologic programs currently active in Alaska. The two Hazards studies discuss volcano-related topics in the seismically active southcentral Alaska region. The first paper revisits the eruptive events of Redoubt Volcano that occurred more than a decade ago and the subsequent development of the Alaska Volcano Observatory (AVO). This treatise documents the historic impact of this eruption and briefly summarizes the state of our knowledge of the other Cook Inlet, Alaska Peninsula, and Aleutian Island volcanoes. Finally, it discusses the recent role that AVO has had in seismic station installation and hazard assessment at volcanically active sites throughout the world. The second paper discusses the eruptive history of Snowy Mountain in the upper Alaska Peninsula. Because subsets of its 25-30 lava flows erupted as packages in short episodes, calculation of the volcano's lifetime average volumetric eruption rate is problematic. A portion of the cone was hydrothermally weakened and collapsed in the late Holocene producing a 22-km2 debris avalanche.
\nGeologic Framework studies provide background information that is the scientific basis for present and future earth science investigations. The first paper compares and contrasts the Insular-Intermontane suture zone (IISZ) of southeast Alaska with the Adria-Europe suture zone (AESZ) of Switzerland and Hungary. The study develops the hypothesis that the zones have distinct differences as well as similarities and neither is a simple lithotectonic terrane boundary. The second paper discusses the relation among volcanic, glacial, and tectonic activity in the Cold Bay and False Pass 1 :250,000-scale quadrangles on the Alaska Peninsula. During Pleistocene time, continental-shelf glaciations and two massive volcanic centers were the dominant controls over landscape development. The third paper gives detailed geologic information for Paleozoic rocks within the Taylor Mountains D-1 quadrangle portion of the Holitna Lowland of southwestern Alaska. Because of the excellent preservation of megafossils, these Silurian and Ordovician strata lend themselves to detailed statigraphic investigations. Further, low thermal alteration indices of this area have made them a potential target of petroleum exploration. The final report in this section discusses the development of a new spectral enhancement approach for interpreting Multispectral Scanner (MSS) and Thematic Mapper (TM) satellite images. This technique enhances the use of remote sensing data in identifying geologic units in areas that have been poorly investigated. This study used this technique to better define the distribution of a JMtu (mafic, ultramafic, and sedimentary) unit and a PzZrqs (pelitic and quartzitic schist) unit.
\nEnvironment and climate studies are the emphasis of two papers. One presents the first radiocarbon-dated postglacial vegetation history of the Kenai Mountains of southcentral Alaska. This reconstruction is the result of the analysis of pollen assemblages and peat from sediments collected in Tern Lake and presents a minimum age for deglaciation of these interior valleys at 9,31 0±200 yr B .P. Current vegetation, however, developed within the past ca. 2,500 years. A second study discusses the cycling of arsenic and cadmium in sub-arctic boreal forest ecosystems typical of interior Alaska and defines the importance of various natural (geogenic) sources. The transport and uptake into vegetation of these elements from soils developed from loess as well as soils developed from the major rock units is presented. The bioaccumulation of cadmium in willow (Salix sp.) and its potential consequence to the health of browsing animals is discussed.
\nPapers related to resource issues comprise the topic of the final report. This paper presents a brief statistical summary of the geochemistry of rock samples collected in the east-central portion of the Eagle 1 :250,000-scale quadrangle. This study helps define the rock unit source of both resource- and environmental-based chemical elements of interest in the Fortymile mining district.
\nTwo bibliographies at the end of the volume list reports covering Alaska earth science topics in USGS publications during 1999 and reports about Alaska by USGS authors in non-USGS publications during the same period.
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\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adee4b07f02db6874a1","contributors":{"editors":[{"text":"Gough, Larry P. lgough@usgs.gov","contributorId":1230,"corporation":false,"usgs":true,"family":"Gough","given":"Larry","email":"lgough@usgs.gov","middleInitial":"P.","affiliations":[],"preferred":true,"id":544579,"contributorType":{"id":2,"text":"Editors"},"rank":1},{"text":"Wilson, Frederic H. 0000-0003-1761-6437 fwilson@usgs.gov","orcid":"https://orcid.org/0000-0003-1761-6437","contributorId":67174,"corporation":false,"usgs":true,"family":"Wilson","given":"Frederic","email":"fwilson@usgs.gov","middleInitial":"H.","affiliations":[{"id":119,"text":"Alaska Science Center Geology Minerals","active":true,"usgs":true},{"id":114,"text":"Alaska Science Center","active":true,"usgs":true}],"preferred":true,"id":544580,"contributorType":{"id":2,"text":"Editors"},"rank":2}]}} ,{"id":38273,"text":"pp1636 - 2001 - Numerical-simulation and conjunctive-management models of the Hunt-Annaquatucket-Pettaquamscutt stream-aquifer system, Rhode Island","interactions":[],"lastModifiedDate":"2023-01-04T20:31:55.742573","indexId":"pp1636","displayToPublicDate":"2001-04-01T00:00:00","publicationYear":"2001","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"1636","title":"Numerical-simulation and conjunctive-management models of the Hunt-Annaquatucket-Pettaquamscutt stream-aquifer system, Rhode Island","docAbstract":"Numerical-simulation and optimization techniques were used to evaluate alternatives for the conjunctive management of ground- and surface-water resources of the Hunt-Annaquatucket-Pettaquamscutt stream-aquifer system in central Rhode Island. Ground-water withdrawals from the Hunt-Annaquatucket-Pettaquamscutt aquifer exceeded 8 million gallons per day during months of peak water use during 199398, and additional withdrawals have been proposed to meet growing demands from within and outside of the system boundary. The system is defined by the Hunt-Annaquatucket-Pettaquamscutt aquifer, which is composed of glacial stratified deposits, and the network of rivers, brooks, and ponds that overlie and are in hydraulic connection with the aquifer. Nearly all of the water withdrawn, however, is derived from depletions of flow in the rivers, brooks, and ponds that overlie the aquifer. Streamflow depletions are of concern to environmental agencies because of the adverse effects that reductions in streamflow can have on aquatic and riparian ecosystems.
A conjunctive-management model of the stream-aquifer system was developed to simultaneously address the water-demand and streamflow-depletion issues. The objective of the model was to maximize total ground-water withdrawal from the aquifer during July, August, and September. These three months are generally the time of year when water-supply demands are largest and streamflows are simultaneously lowest. Total withdrawal from the aquifer was limited by a set of constraints specified in the model. These constraints were (1) maximum rates of streamflow depletion in the Hunt, Annaquatucket, and Pettaquamscutt Rivers; (2) minimum monthly water demands of each of three water-supply systems that withdraw water from the aquifer; and (3) minimum and maximum withdrawal rates at each supply well.
The conjunctive-management model was formulated mathematically as a linear program. The model was solved by a response-matrix technique that incorporates the results of transient, numerical simulation of the stream-aquifer system into the constraint set of the linear program. The basis of the technique was the assumption that streamflow-depletion rates in each river were a linear function of ground-water-withdrawal rates at each well. This assumption was shown to be valid for the conditions evaluated in this study, primarily because of the very high transmissivity of the aquifer near many of the wells pumped for water supply. A transient, numerical model of the system was developed to simulate an average annual cycle of monthly withdrawal and hydrologic conditions representative of the 56-year period 194196. The transient model was used to generate characteristic streamflow-depletion responses in each river to simulated withdrawals at each well; these characteristic responses, or response coefficients, were then incorporated directly into the streamflow-depletion constraints of the linear program.
Four sets of applications of the conjunctive-management model were made to determine whether total ground-water withdrawal from the aquifer during July, August, and September could be increased over the current total withdrawal for alternative definitions of the maximum rates of streamflow depletion allowed in the Hunt, Annaquatucket, and Pettaquamscutt Rivers. Current conditions were defined as the average monthly withdrawal rates at each supply well, water demands of each of the three water-supply systems, and estimated streamflow-depletion rates during the 6-year period 199398. Total withdrawal from all wells in the system from July through September during 199398 was 506.5 million gallons. Estimated streamflow-depletion rates for 199398 were calculated by use of the transient model, with the 199398 average monthly withdrawal rates specified at each supply well. Streamflow-depletion rates calculated for July, August, and September averaged 25 percent of the model-calculated pre-withdrawal streamflow rates for the Hunt River, 19 percent for the Annaquatucket River, and 7 percent for the Pettaquamscutt River.
The first set of applications of the model were made with the current estimated rates of streamflow depletion in the Hunt, Annaquatucket, and Pettaquamscutt Rivers. Results of these applications indicated that total withdrawal from the aquifer during July, August, and September could be increased from about 8 to 18 percent (from 546.0 to 596.3 million gallons) over the current total withdrawal. The increased withdrawal would require modifications to the current annual withdrawal schedule of each supply well and, for the 18-percent increase, a modified network of supply wells that would include two new wells in the Annaquatucket River Basin. A second set of model applications then was made to determine if current estimated rates of streamflow depletion in the Hunt River could be reduced without increasing current estimated rates of streamflow depletion in the Annaquatucket or Pettaquamscutt Rivers. Decreases in the current rates of streamflow depletion in the Hunt River would result in increased streamflow in the river during these three months. Results showed that current rates of streamflow depletion in the Hunt River during July, August, and September could be decreased from 5 to 15 percent, depending on whether the existing or modified well network was used.
Subsequent model applications indicated that substantial increases in total ground-water withdrawal from the aquifer are possible, but would require increased rates of streamflow depletion in the Annaquatucket and Pettaquamscutt Rivers. Maximum increases in the July through September withdrawal from the aquifer of about 39 to 50 percent (from 705.1 to 760.3 million gallons) over the current total withdrawal were calculated when streamflow-depletion rates in the Annaquatucket and Pettaquamscutt Rivers were allowed to increase from current estimated rates to a maximum of 25 percent of the model-calculated pre-withdrawal streamflow for each river during July, August, and September. Alternatively, it was shown that current estimated rates of streamflow depletion in the Hunt River during July, August, and September could be reduced by as much as 35 percent for the maximum allowed increases in streamflow depletion in the Annaquatucket and Pettaquamscutt Rivers; maximum increased withdrawal from the aquifer, however, would range from 8 to 18 percent over the current total withdrawal for the 35-percent reduction in streamflow-depletion rates in the Hunt River.
Results of the different applications of the model demonstrate the usefulness of coupling numerical-simulation and optimization techniques for regional-scale evaluation of water-resource management alternatives. The results of the evaluation must be viewed, however, within the limitations of the quality of data available for the Hunt-Annaquatucket-Pettaquamscutt stream-aquifer system and representation of the system by a simulation model. An additional limitation of the analysis was the use of an average annual cycle of monthly withdrawal and hydrologic conditions. Ground-water withdrawal strategies may need to be modified to meet streamflow-depletion constraints during extreme hydrologic events, such as droughts.
Contributing areas and sources of water to the supply wells also were delineated by use of a steady-state model of the stream-aquifer system. The model was developed to simulate long-term-average ground-water flow and ground-water/ surface-water interactions in the system during the 56-year period 194196. Sources of water to the wells consisted of precipitation and wastewater recharge to the aquifer, streamflow leakage from natural stream-channel losses, streamflow leakage caused by induced infiltration, and lateral ground-water inflow from till and bedrock upland areas.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/pp1636","usgsCitation":"Barlow, P.M., and Dickerman, D.C., 2001, Numerical-simulation and conjunctive-management models of the Hunt-Annaquatucket-Pettaquamscutt stream-aquifer system, Rhode Island: U.S. Geological Survey Professional Paper 1636, Report: vi, 88 p.; 1 Plate: 8.00 x 10.74 inches, https://doi.org/10.3133/pp1636.","productDescription":"Report: vi, 88 p.; 1 Plate: 8.00 x 10.74 inches","costCenters":[{"id":493,"text":"Office of Ground Water","active":true,"usgs":true}],"links":[{"id":411376,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_37347.htm","linkFileType":{"id":5,"text":"html"}},{"id":162711,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":3502,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pp/pp1636/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Rhode Island","otherGeospatial":"Hunt-Annaquatucket-Pettaquamscutt stream-aquifer system","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -71.53278939505572,\n 41.672256551048775\n ],\n [\n -71.53278939505572,\n 41.46679169393127\n ],\n [\n -71.42248696957856,\n 41.46679169393127\n ],\n [\n -71.42248696957856,\n 41.672256551048775\n ],\n [\n -71.53278939505572,\n 41.672256551048775\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afce4b07f02db696840","contributors":{"authors":[{"text":"Barlow, Paul M. 0000-0003-4247-6456 pbarlow@usgs.gov","orcid":"https://orcid.org/0000-0003-4247-6456","contributorId":1200,"corporation":false,"usgs":true,"family":"Barlow","given":"Paul","email":"pbarlow@usgs.gov","middleInitial":"M.","affiliations":[{"id":493,"text":"Office of Ground Water","active":true,"usgs":true}],"preferred":true,"id":219481,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dickerman, David C.","contributorId":41047,"corporation":false,"usgs":true,"family":"Dickerman","given":"David","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":219482,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":67545,"text":"i2740 - 2001 - Geologic map of Colorado National Monument and adjacent areas, Mesa County, Colorado","interactions":[],"lastModifiedDate":"2023-01-17T19:29:09.263641","indexId":"i2740","displayToPublicDate":"2001-04-01T00:00:00","publicationYear":"2001","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":320,"text":"IMAP","code":"I","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2740","subseriesTitle":"GIS","title":"Geologic map of Colorado National Monument and adjacent areas, Mesa County, Colorado","docAbstract":"New 1:24,000-scale geologic mapping in the Colorado National Monument Quadrangle and adjacent areas, in support of the USGS Western Colorado I-70 Corridor Cooperative Geologic Mapping Project, provides new interpretations of and data for the stratigraphy, structure, geologic hazards in the area from the Colorado River in Grand Valley onto the Uncompahgre Plateau. The plateau drops abruptly along northwest-trending structures toward the northeast 800 m to the Redlands area and the Colorado River in Grand Valley. In addition to common alluvial and colluvial deposits, surficial deposits include Holocene and late Pleistocene charcoal-bearing valley-fill deposits, late to middle Pleistocene river-gravel terrace deposits, Holocene to middle Pleistocene younger, intermediate, and old fan-alluvium deposits, late to middle Pleistocene local gravel deposits, Holocene to late Pleistocene rock-fall deposits, Holocene to middle Pleistocene young and old landslide deposits, Holocene to late Pleistocene sheetwash deposits and eolian deposits, and Holocene Cienga-type deposits. Only the lowest part of the Upper Cretaceous Mancos Shale is exposed in the map area near the Colorado River. The Upper and Lower? Cretaceous Dakota Formation and the Lower Cretaceous Burro Canyon Formation form resistant dipslopes in the Grand Valley and a prominent ridge on the plateau. Less resistant strata of the Upper Jurassic Morrison Formation consisting of the Brushy Basin, Salt Wash, and Tidwell Members form slopes on the plateau and low areas below the mountain front of the plateau. The Middle Jurassic Wanakah Formation nomenclature replaces the previously used Summerville Formation. Because an upper part of the Middle Jurassic Entrada Formation is not obviously correlated with strata found elsewhere, it is therefore not formally named; however, the lower rounded cliff former Slickrock Member is clearly present. The Lower Jurassic silica-cemented Kayenta Formation forms the cap rock for the Lower Jurassic carbonate-cemented Wingate Sandstone, which forms the impressive cliffs of the monument. The Upper Triassic Chinle Formation was deposited on the eroded and weathered Middle Proterozoic meta-igneous gneiss, pegmatite dikes, and migmatitic gneiss. Structurally the area is deceptively challenging. Nearly flat-lying strata on the plateau are folded by northwest-trending fault-propagation folds into at least two S-shaped folds along the mountain front of the plateau. Strata under Grand Valley dip at about 6 degrees to the northeast. In the absence of local evidence, the uplifted plateau is attributed to Laramide deformation by dated analogous structures elsewhere in the Colorado Plateau. The major exposed fault records high-angle reverse relationships in the basement rocks but dissipates strain as a triangular zone of distributed microfractures and cataclastic flow into overlying Mesozoic strata that absorb the fault strain, leaving only folds. Evidence for younger, probably late Pliocene or early Pleistocene, uplift does exist at the antecedent Unaweep Canyon south and east of the map area. To what degree this younger deformation affected the map area is unknown. Several geologic hazards affect the area. Middle and late Pleistocene landslides involving the smectite-bearing Brushy Basin Member of the Morrison Formation are extensive on the plateau and common in the Redlands below the plateau. Expansive clay in the Brushy Basin and other strata create foundation stability problems for roads and homes. Flash floods create a serious hazard to people on foot in narrow canyons in the monument and to homes close to water courses downstream from narrow restrictions close to the monument boundary.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/i2740","usgsCitation":"Scott, R.B., Harding, A.E., Hood, W.C., Cole, R.D., Livaccari, R.F., Johnson, J.B., Shroba, R.R., and Dickerson, R.P., 2001, Geologic map of Colorado National Monument and adjacent areas, Mesa County, Colorado (Version 1.0): U.S. Geological Survey IMAP 2740, Report: iv, 40 p.; 1 Plate: 56.00 x 39.50 inches; Metadata, https://doi.org/10.3133/i2740.","productDescription":"Report: iv, 40 p.; 1 Plate: 56.00 x 39.50 inches; Metadata","costCenters":[],"links":[{"id":110180,"rank":5,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_38261.htm","linkFileType":{"id":5,"text":"html"},"description":"38261"},{"id":189086,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/imap/2740/report-thumb.jpg"},{"id":91696,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/imap/2740/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":91697,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/imap/2740/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":6157,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/imap/i-2740/","linkFileType":{"id":5,"text":"html"}}],"scale":"24000","country":"United States","state":"Colorado","county":"Mesa County","otherGeospatial":"Colorado National Monument","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -108.756,\n 38.976\n ],\n [\n -108.756,\n 39.125\n ],\n [\n -108.621,\n 39.125\n ],\n [\n -108.621,\n 38.976\n ],\n [\n -108.756,\n 38.976\n ]\n ]\n ]\n }\n }\n ]\n}","edition":"Version 1.0","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b12e4b07f02db6a2a3a","contributors":{"authors":[{"text":"Scott, Robert B. rbscott@usgs.gov","contributorId":766,"corporation":false,"usgs":true,"family":"Scott","given":"Robert","email":"rbscott@usgs.gov","middleInitial":"B.","affiliations":[],"preferred":true,"id":276629,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Harding, Anne E.","contributorId":106554,"corporation":false,"usgs":true,"family":"Harding","given":"Anne","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":276636,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hood, William C.","contributorId":100946,"corporation":false,"usgs":true,"family":"Hood","given":"William","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":276635,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Cole, Rex D.","contributorId":50979,"corporation":false,"usgs":true,"family":"Cole","given":"Rex","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":276632,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Livaccari, Richard F.","contributorId":65548,"corporation":false,"usgs":true,"family":"Livaccari","given":"Richard","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":276634,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Johnson, James B.","contributorId":55088,"corporation":false,"usgs":true,"family":"Johnson","given":"James","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":276633,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Shroba, Ralph R. 0000-0002-2664-1813 rshroba@usgs.gov","orcid":"https://orcid.org/0000-0002-2664-1813","contributorId":1266,"corporation":false,"usgs":true,"family":"Shroba","given":"Ralph","email":"rshroba@usgs.gov","middleInitial":"R.","affiliations":[{"id":318,"text":"Geosciences and Environmental Change Science Center","active":true,"usgs":true}],"preferred":true,"id":276630,"contributorType":{"id":1,"text":"Authors"},"rank":7},{"text":"Dickerson, Robert P.","contributorId":6461,"corporation":false,"usgs":true,"family":"Dickerson","given":"Robert","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":276631,"contributorType":{"id":1,"text":"Authors"},"rank":8}]}} ,{"id":59158,"text":"mf2349 - 2001 - Geologic map and map database of the Spreckels 7.5-minute Quadrangle, Monterey County, California","interactions":[],"lastModifiedDate":"2018-06-14T13:18:58","indexId":"mf2349","displayToPublicDate":"2001-03-01T00:00:00","publicationYear":"2001","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":325,"text":"Miscellaneous Field Studies Map","code":"MF","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2349","title":"Geologic map and map database of the Spreckels 7.5-minute Quadrangle, Monterey County, California","docAbstract":"Introduction\r\n\r\nThe Spreckels quadrangle lies at the north end of the Sierra de Salinas and extends from the Salinas Valley on the northeast across Los Laurelles Ridge south to Carmel Valley, an intermontane valley that separates the Santa Lucia Range from the Sierra de Salinas (fig. 1). The Toro Regional Park occupies the east-central part of the quadrangle, whereas the former Fort Ord Military Reservation covers the northwestern part of the area and is the probable locus of future development. Subdivisions largely occupy the older floodplain of Toro Creek and the adjacent foothills, with less dense development along the narrower canyons of Corral de Tierra and San Benancio Gulch to the south. The foothills southwest of the Salinas River are the site of active residential development. \r\n\r\nGeologically, the study area has a crystalline basement of Upper Cretaceous granitic rocks of the Salinian block and older metasedimentary rocks of the schist of the Sierra de Salinas of probable Cretaceous age. Resting nonconformably upon these basement rocks is a sedimentary section that ranges in age from middle Miocene to Holocene and has a composite thickness of as much as 1,200 m. One of the purposes of the present study was to investigate the apparent lateral variation of the middle to upper Miocene sections from the typical porcelaneous and diatomaceous Monterey Formation of the Monterey and Seaside quadrangles to the west (Clark and others, 1997) to a thick marine sandstone section in the eastern part of the Spreckels quadrangle. \r\n\r\nLiquefaction, which seriously affected the Spreckels area in the 1906 San Francisco earthquake (Lawson, 1908), and landsliding are the two major geological hazards of the area. The landslides consist mainly of older large slides in the southern and younger debris flows in the northern part of the quadrangle.\r\n\r\nThis digital map database, compiled from previously published and unpublished data, and new mapping by the authors, represents the general distribution of bedrock and surficial deposits in the mapped area. Together with the accompanying text file (skmf.txt, skmf.pdf, or skmf.ps), it provides current information on the geologic structure and stratigraphy of the area covered. The database delineates map units that are identified by general age and lithology following the stratigraphic nomenclature of the U.S. Geological Survey. The scale of the source maps limits the spatial resolution (scale) of the database to 1:24,000 or smaller.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/mf2349","usgsCitation":"Clark, J., Brabb, E.E., Rosenberg, L.I., Goss, H.V., and Watkins, S.E., 2001, Geologic map and map database of the Spreckels 7.5-minute Quadrangle, Monterey County, California (Online Version 1.0): U.S. Geological Survey Miscellaneous Field Studies Map 2349, Map (31 x 32 inches); Pamphlet (22 p.); Metadata, https://doi.org/10.3133/mf2349.","productDescription":"Map (31 x 32 inches); Pamphlet (22 p.); Metadata","additionalOnlineFiles":"Y","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true},{"id":647,"text":"Western Earth Surface Processes","active":false,"usgs":true}],"links":[{"id":180194,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":9536,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/mf/2001/2349/","linkFileType":{"id":5,"text":"html"}},{"id":110148,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_34798.htm","linkFileType":{"id":5,"text":"html"},"description":"34798"}],"scale":"24000","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -121.75,36.5 ], [ -121.75,36.6175 ], [ -121.61749999999999,36.6175 ], [ -121.61749999999999,36.5 ], [ -121.75,36.5 ] ] ] } } ] }","edition":"Online Version 1.0","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1ae4b07f02db6a8669","contributors":{"authors":[{"text":"Clark, Joseph C.","contributorId":101663,"corporation":false,"usgs":true,"family":"Clark","given":"Joseph C.","affiliations":[],"preferred":false,"id":261547,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Brabb, Earl E.","contributorId":48939,"corporation":false,"usgs":true,"family":"Brabb","given":"Earl","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":261546,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Rosenberg, Lewis I.","contributorId":12073,"corporation":false,"usgs":true,"family":"Rosenberg","given":"Lewis","email":"","middleInitial":"I.","affiliations":[],"preferred":false,"id":261543,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Goss, Heather V.","contributorId":32776,"corporation":false,"usgs":true,"family":"Goss","given":"Heather","email":"","middleInitial":"V.","affiliations":[],"preferred":false,"id":261545,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Watkins, Sarah E.","contributorId":23234,"corporation":false,"usgs":true,"family":"Watkins","given":"Sarah","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":261544,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":66252,"text":"i2684 - 2001 - Geologic Map of the Lavinia Planitia Quadrangle (V-55), Venus","interactions":[],"lastModifiedDate":"2016-12-28T14:12:05","indexId":"i2684","displayToPublicDate":"2001-03-01T00:00:00","publicationYear":"2001","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":320,"text":"IMAP","code":"I","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2684","subseriesTitle":"GIS","title":"Geologic Map of the Lavinia Planitia Quadrangle (V-55), Venus","docAbstract":"Introduction\r\n\r\nThe Lavinia Planitia quadrangle (V-55) is in the southern hemisphere of Venus and extends from 25 to 50 south latitude and from 330 to 360 longitude. It covers the central and northern part of Lavinia Planitia and parts of its margins. Lavinia Planitia consists of a centralized, deformed lowland flooded by volcanic deposits and surrounded by Dione Regio to the west (Keddie and Head, 1995), Alpha Regio tessera (Bindschadler and others, 1992a) and Eve Corona (Stofan and others, 1992) to the northeast, itself an extensive rift zone and coronae belt to the east and south (Baer and others, 1994; Magee and Head, 1995), Mylitta Fluctus to the south (Magee Roberts and others, 1992), and Helen Planitia to the southwest (Senske and others, 1991). In contrast to other areas on Venus, the Lavinia Planitia area is one of several large, relatively equidimensional lowlands (basins) and as such is an important region for the analysis of processes of basin formation and volcanic flooding. \r\n\r\nBefore the Magellan mission, Lavinia Planitia was known on the basis of Pioneer-Venus altimetry to be a lowland area (Pettengill and others, 1980);. Arecibo radar images showed that Lavinia Plaitia was surrounded by several corona-like features and rift-like fractures parallel to the basin margin to the east and south (Senske and others, 1991; Campbell and others, 1990). Arecibo data further revealed that the interior contained complex patterns of deformational features in the form of belts and volcanic plains, and several regions along the margins were seen to be the sources of extensive outpourings of digitate lava flows into the interior (Senske and others, 1991; Campbell and others, 1990). Early Magellan results showed that the ridge belts are composed of complex structures of both extensional and contractional origin (Squyres and others, 1992; Solomon and others, 1992) and that the complex lava flows (fluctus) along the margins (Magee Roberts and others, 1992) emanated from a variety of sources ranging from volcanoes to coronae (Magee and Head, 1995; Keddie and Head, 1995). In addition, global analysis of the distribution of volcanic features revealed that Lavinia Planitia is an area deficient in the distribution of distinctive volcanic sources and corona-like features (Head and others, 1992; Crumpler and others, 1993). \r\n\r\nLavinia Planitia gravity and geoid data show that the lowland is characterized by a -30 mGal gravity anomaly and a -10 m geoid anomaly, centered on eastern Lavinia (Bindschadler and others, 1992b; Konopliv and Sjogren, 1994). Indeed, the characteristics and configuration of Lavinia Planitia have been cited as evidence for the region being the site of large-scale mantle down welling (Bindschadler and others, 1992b). Thus, this region is a laboratory for the study of the formation of lowlands, the emplacement of volcanic plains, the formation of associated tectonic features, and their relation to mantle processes. These questions and issues are the basis for our geologic mapping analysis. \r\n\r\nIn our analysis we have focused on the geologic mapping of the Lavinia Planitia quadrangle using traditional methods of geologic unit definition and characterization for the Earth (for example, American Commission on Stratigraphic Nomenclature, 1961) and planets (for example, Wilhelms, 1990) appropriately modified for radar data (Tanaka, 1994). We defined units and mapped key relations using the full resolution Magellan synthetic aperture radar (SAR) data (mosaiced full resolution basic image data records, C1-MIDR's, F-MIDR's, and F-Maps) and transferred these results to the base map compiled at a scale of 1:5 million. In addition to the SAR image data, we incorporated into our analyses digital versions of Magellan altimetry, emissivity, Fresnel reflectivity, and roughness data (root mean square, rms, slope). The background for our unit definition and characterization is described in Tanaka (1994), Basilevsky and Head (1995a, b)","language":"ENGLISH","publisher":"Geological Survey (U.S.)","doi":"10.3133/i2684","isbn":"0607945052","usgsCitation":"Ivanov, M.A., and Head, J.W., 2001, Geologic Map of the Lavinia Planitia Quadrangle (V-55), Venus: U.S. Geological Survey IMAP 2684, 1 remote-sensing image :col. ;54 x 62 cm., on sheet 101 x 112 cm., folded in envelope 30 x 24 cm., https://doi.org/10.3133/i2684.","productDescription":"1 remote-sensing image :col. ;54 x 62 cm., on sheet 101 x 112 cm., folded in envelope 30 x 24 cm.","costCenters":[{"id":131,"text":"Astrogeology Science Center","active":true,"usgs":true}],"links":[{"id":438885,"rank":101,"type":{"id":30,"text":"Data Release"},"url":"https://doi.org/10.5066/P9F4Z1WM","text":"USGS data release","linkHelpText":"Geologic Map of the Lavinia Planitia Quadrangle (V-55), Venus"},{"id":187584,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":9384,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/imap/i2684/","linkFileType":{"id":5,"text":"html"}}],"scale":"4711886","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1ae4b07f02db6a84b9","contributors":{"authors":[{"text":"Ivanov, Mikhail A.","contributorId":25245,"corporation":false,"usgs":true,"family":"Ivanov","given":"Mikhail","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":274246,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Head, James W. III","contributorId":102954,"corporation":false,"usgs":true,"family":"Head","given":"James","suffix":"III","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":274247,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":33088,"text":"b2064GG - 2001 - Geochemical results of a hydrothermally altered area at Baker Creek, Blaine County, Idaho","interactions":[],"lastModifiedDate":"2012-02-02T00:09:17","indexId":"b2064GG","displayToPublicDate":"2001-03-01T00:00:00","publicationYear":"2001","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2064","chapter":"GG","title":"Geochemical results of a hydrothermally altered area at Baker Creek, Blaine County, Idaho","docAbstract":"The area immediately east of Baker Creek, Blaine County, Idaho, is underlain by a thick section of mafic to intermediate lava flows of the Eocene Challis Volcanic Group. Widespread propylitic alteration surrounds a zone of argillic alteration and an inner core of phyllic alteration.\r\n\r\nSilicified breccia is present along an east-trending fault within the zone of phyllic alteration. As part of a reconnaissance geochemical survey, soils and plants were sampled. Several species of plants (Douglas-fir [ Pseudotsuga menziesii ], mountain big sagebrush [ Artemisia tridentata ssp. vaseyana ], and elk sedge [ Carex geyerii ]) were collected from 10 upland localities and stream sediments, panned concentrates, and aquatic mosses were collected from 16 drainage basin localities all of which were generally within the area of alteration.\r\n\r\nGeochemical results yielded anomalous concentrations of molybenum, zinc, silver, and lead in at least half of the seven different sample media and of gold, thallium, arsenic, antimony, manganese, boron, cadmium, bismuth, copper, and beryllium in from one to four of the various media. Part of this suite of elements? silver, gold, arsenic, antimony, thallium, and manganese? suggests that the mineralization in the area is epithermal. Barite and pyrite (commonly botryoidal-framboidal) are widespread throughout the area sampled. Visible gold and pyromorphite (a secondary lead mineral) were identified in only one small drainage basin, but high levels of gold were detected in aquatic mosses over a larger area.\r\n\r\nData from the upland and stream sampling indicate two possible mineralized areas. The first mineralized area was identified by a grab sample from an outcrop of quartz stockwork that contained 50 ppb Au, 1.5 ppm Ag, and 50 ppm Mo. Although the soil and plant species that were sampled in the area indicated mineralized bedrock, the Douglas-fir samples were the best indicators of the silver anomaly. The second possible mineralized area centers on the fault-controlled silicified breccia that is most likely the source of anomalous silver and molybdenum levels identified in the soils; silver, molybdenum, and manganese in stream sediments; thallium in Douglas-fir; bismuth and silver in concentrates; and gold, silver, arsenic, antimony, and molybdenum and lead in aquatic mosses.\r\n\r\nAn interpretation of regional aeromagnetic data delineated the subsurface extent of shallow, steeply dipping magnetic sources inferred to be shallower parts of an Eocene batholith thought to underlie much of the Baker Creek area. The Eocene intrusive event(s) may have served as the heat source(s) that caused the hydrothermal alteration.\r\n\r\nExamination of core from a 1,530-ft-deep (466 m) hole drilled in 1982 confirmed a bedrock source for the anomalous silver and base-metal suite at the quartz stockwork location, and indicated subeconomic levels of molybdenum.","language":"ENGLISH","doi":"10.3133/b2064GG","usgsCitation":"Erdman, J.A., Moye, F.J., Theobald, P., McCafferty, A.E., and Larsen, R.K., 2001, Geochemical results of a hydrothermally altered area at Baker Creek, Blaine County, Idaho (Version 1.0): U.S. Geological Survey Bulletin 2064, 21 p., https://doi.org/10.3133/b2064GG.","productDescription":"21 p.","costCenters":[],"links":[{"id":163360,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":3288,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/bul/b2064-gg/","linkFileType":{"id":5,"text":"html"}}],"edition":"Version 1.0","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b23e4b07f02db6ade17","contributors":{"authors":[{"text":"Erdman, James A.","contributorId":37748,"corporation":false,"usgs":true,"family":"Erdman","given":"James","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":209863,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Moye, Falma J.","contributorId":104113,"corporation":false,"usgs":true,"family":"Moye","given":"Falma","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":209865,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Theobald, Paul K.","contributorId":45361,"corporation":false,"usgs":true,"family":"Theobald","given":"Paul K.","affiliations":[],"preferred":false,"id":209864,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"McCafferty, Anne E. 0000-0001-5574-9201 anne@usgs.gov","orcid":"https://orcid.org/0000-0001-5574-9201","contributorId":1120,"corporation":false,"usgs":true,"family":"McCafferty","given":"Anne","email":"anne@usgs.gov","middleInitial":"E.","affiliations":[{"id":211,"text":"Crustal Geophysics and Geochemistry Science Center","active":true,"usgs":true},{"id":35995,"text":"Geology, Geophysics, and Geochemistry Science Center","active":true,"usgs":true}],"preferred":true,"id":209861,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Larsen, Richard K.","contributorId":22402,"corporation":false,"usgs":true,"family":"Larsen","given":"Richard","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":209862,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":45064,"text":"wri004251 - 2001 - Simulation of ground-water discharge to Biscayne Bay, southeastern Florida","interactions":[],"lastModifiedDate":"2022-01-04T18:43:24.622742","indexId":"wri004251","displayToPublicDate":"2001-01-01T21:40:00","publicationYear":"2001","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2000-4251","displayTitle":"Simulation of Ground-Water Discharge to Biscayne Bay, Southeastern Florida","title":"Simulation of ground-water discharge to Biscayne Bay, southeastern Florida","docAbstract":"As part of the Place-Based Studies Program, the U.S. Geological Survey initiated a project in 1996, in cooperation with the U.S. Army Corps of Engineers, to quantify the rates and patterns of submarine ground-water discharge to Biscayne Bay. Project objectives were achieved through field investigations at three sites (Coconut Grove, Deering Estate, and Mowry Canal) along the coastline of Biscayne Bay and through the development and calibration of variable-density, ground-water flow models. Two-dimensional, vertical cross-sectional models were developed for steady-state conditions for the Coconut Grove and Deering Estate transects to quantify local-scale ground-water discharge patterns to Biscayne Bay. A larger regional-scale model was developed in three dimensions to simulate submarine ground-water discharge to the entire bay. The SEAWAT code, which is a combined version of MODFLOW and MT3D, was used to simulate the complex variable-density flow patterns. Field data suggest that ground-water discharge to Biscayne Bay relative to the shoreline is restricted to within 300 meters at Coconut Grove, 600 to 1,000 meters at Deering Estate, and 100 meters at Mowry Canal. The vertical cross-sectional models, which were calibrated to the field data using the assumption of steady state, tend to focus ground-water discharge to within 50 to 200 meters of the shoreline. With homogeneous distributions for aquifer parameters and a constant-concentration boundary for Biscayne Bay, the numerical models could not reproduce the lower ground-water salinities observed beneath the bay, which suggests that further research may be necessary to improve the accuracy of the numerical simulations. Results from the cross-sectional models, which were able to simulate the approximate position of the saltwater interface, suggest that longitudinal dispersivity ranges between 1 and 10 meters, and transverse dispersivity ranges from 0.1 to 1 meter for the Biscayne aquifer. The three-dimensional, regional-scale model was calibrated to ground-water heads, canal baseflow, and the general position of the saltwater interface for nearly a 10-year period from 1989 to 1998. The mean absolute error between observed and simulated head values is 0.15 meter. The mean absolute error between observed and simulated baseflow is 3 x 105 cubic meters per day. The position of the simulated saltwater interface generally matches the position observed in the field, except for areas north of the Miami Canal where the simulated saltwater interface is located about 5 kilometers inland of the observed saltwater interface. Results from the regional-scale model suggest that the average rate of fresh ground-water discharge to Biscayne Bay for the 10-year period (1989-98) is about 2 x 105 cubic meters per day for 100 kilometers of coastline. This simulated discharge rate is about 6 percent of the measured surface-water discharge to Biscayne Bay for the same period. The model also suggests that nearly 100 percent of the fresh ground-water discharge is to the northern half of Biscayne Bay, north of the Cutler Drain Canal. South of the Cutler Drain Canal, coastal lowlands prevent the water table from rising high enough to drive measurable quantities of ground water to Biscayne Bay. Annual variations in sea-level elevation, which can be as large as 0.3 meter, have a substantial effect on rates of ground-water discharge. During 1989-98, simulated rates of ground-water discharge to Biscayne Bay generally are highest when sea level is relatively low.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri004251","collaboration":"Prepared in cooperation with the U.S. Army Corps of Engineers","usgsCitation":"Langevin, C.D., 2001, Simulation of ground-water discharge to Biscayne Bay, southeastern Florida: U.S. Geological Survey Water-Resources Investigations Report 2000-4251, Report: vi, 127 p.; 3 Plates: 8.5 x 11 in, https://doi.org/10.3133/wri004251.","productDescription":"Report: vi, 127 p.; 3 Plates: 8.5 x 11 in","costCenters":[{"id":27821,"text":"Caribbean-Florida Water Science Center","active":true,"usgs":true}],"links":[{"id":99370,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/2000/4251/wri004251_plate3.pdf","text":"Plate 3","size":"1.06 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 3"},{"id":99369,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/2000/4251/wri004251_plate2.pdf","text":"Plate 2","size":"0.98 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 2"},{"id":167923,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/2000/4251/report-thumb.jpg"},{"id":99367,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2000/4251/wri004251.pdf","text":"Report","size":"8.79 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":99368,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/2000/4251/wri004251_plate1.pdf","text":"Plate 1","size":"820 KB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 1"}],"country":"United States","state":"Florida","otherGeospatial":"Biscayne Bay","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -81.134033203125,\n 25.44823489808649\n ],\n [\n -80.255126953125,\n 25.030861410390447\n ],\n [\n -80.03814697265625,\n 26.125850185680356\n ],\n [\n -80.79620361328125,\n 26.480407161007275\n ],\n [\n -81.134033203125,\n 25.44823489808649\n ]\n ]\n ]\n }\n }\n ]\n}","contact":"Caribbean-Florida Water Science Center
U.S. Geological Survey
3321 College Avenue
Davie, FL 33314
The regional, confined Atlantic City 800-foot sand is the principal source of water supply for coastal communities of southern New Jersey. In response to extensive use of the aquifer--nearly 21 million gallons per day in 1986--water levels have declined to about 100 feet below sea level near Atlantic City and remain below sea level throughout the coastal areas of southern New Jersey, raising concerns about the potential for saltwater intrusion into well fields.
\nWater levels in the Atlantic City 800-foot sand have declined in response to pumping from the aquifer since the 1890's. Water levels in the first wells drilled into the Atlantic City 800-foot sand were above land surface, and water flowed continuously from the wells. By 1986, water levels were below sea level throughout most of the coastal areas. Under current conditions, wells near the coast derive most of their supply from lateral flow contributed from the unconfined part of the aquifer northwest of the updip limit of the confining unit that overlies the Atlantic City 800- foot sand. Ground water also flows laterally from offshore areas and leaks vertically through the overlying and underlying confining units into the Atlantic City 800-foot sand. The decline in water levels upsets the historical equilibrium between freshwater and ancient saltwater in offshore parts of the aquifer and permits the lateral movement of saltwater toward pumping centers. The rate of movement is accelerated as the decline in water levels increases. The chloride concentration of aquifer water 5.3 miles offshore of Atlantic City was measured as 77 mg/L (milligrams per liter) in 1985 at a U.S. Geological Survey observation well. Salty water has also moved toward wells in Cape May County. The confined, regional nature of the Atlantic City 800-foot sand permits water levels in Cape May County to decline in response to pumping in Atlantic County and vice versa. Historically, chloride concentrations as great as 1 ,510 mg/L have been reported for water in a former supply well in southern Cape May County. These data indicate that salty water has moved inland in Cape May County. Analysis of the chloride-concentration data indicates that ground water with a chloride concentration of 250 mg/L is within 4 miles of supply wells in Stone Harbor, Cape May County, and is about 10 miles offshore of supply wells near Atlantic City.
\nResults of numerical simulations of ground-water flow were analyzed to determine the effects of four water-supply alternatives on water levels, the flow budget, and potential saltwater movement toward pumping centers during 1986-2040. In the supply alternatives, pumpage is (1) held constant at 1986 rates of pumpage; (2) increased by 35 percent at 1986 locations; (3) increased by 35 percent, but with relocation of some supply wells further inland; and (4) increased by 35 percent but with some of the increase derived from inland wells tapping the Kirkwood-Cohansey aquifer system rather than the Atlantic City 800-foot sand. Inland relocation of supply wells closer to the updip limit of the overlying confining unit results in the smallest decline in water levels and the smallest rate of ground-water flow between the offshore location of salty water and coastal supply wells. Increased pumpage from coastal supply wells results in the greatest water-level declines and the greatest increase in the rate of ground-water flow from offshore to coastal wells.
\nFlow of undesirable salty ground water from offshore locations remains nearly the same as for current (1986) conditions when pumping rates do not change, and the flow-rate increase is smallest for the relocated pumpage (fourth) alternative. In comparing the two conditions of a 35-percent increase in pumpage, the flow from undesirable salty water positions is lessened and flow from the unconfined aquifer is increased when some of the pumping centers are relocated farther inland. Ground water from the 250-mg/L isochlor position does not reach supply wells during any simulated conditions predicted for 1986-2040. The analysis of the simulation, however, includes only advective freshwater flow from an estimated 250-mg/L isochlor position and does not include density effects. A chloride concentration data-collection network could be designed to monitor for saltwater intrusion and serve as an early warning system for the communities of southern Cape May County and the coastal communities near Atlantic City. Data from existing offshore wells could continue to serve as an early warning system for the Atlantic City area; however, observation wells south of Stone Harbor, in the Wildwood area, would be useful as an early warning system for southern Cape May County.
","language":"English","publisher":"New Jersey Department of Environmental Protection, Division of Science, Research and Technology, Geological Survey","publisherLocation":"Trenton, NJ","collaboration":"Prepared by the United States Geological Survey in cooperation with the New Jersey Department of Environmental Protection, Division of Science, Research and Technology, Geological Survey","usgsCitation":"McAuley, S.D., Barringer, J., Paulachok, G.N., Clark, J.S., and Zapecza, O.S., 2001, Ground-water flow and quality in the Atlantic City 800-foot sand, New Jersey: New Jersey Geological Survey Report GSR 41, vi, 86 p.","productDescription":"vi, 86 p.","numberOfPages":"94","costCenters":[],"links":[{"id":290121,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":290120,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70114185/report.pdf"}],"projection":"Universal Transverse Mercator Projection, Zone 18","country":"United States","state":"New Jersey","city":"Atlantic City","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -75.4266,38.7969 ], [ -75.4266,40.246 ], [ -73.7842,40.246 ], [ -73.7842,38.7969 ], [ -75.4266,38.7969 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53aa9df2e4b065055fab1669","contributors":{"authors":[{"text":"McAuley, Steven D.","contributorId":81895,"corporation":false,"usgs":true,"family":"McAuley","given":"Steven","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":495260,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Barringer, Julia L.","contributorId":59419,"corporation":false,"usgs":true,"family":"Barringer","given":"Julia L.","affiliations":[],"preferred":false,"id":495259,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Paulachok, Gary N. gnpaulac@usgs.gov","contributorId":3500,"corporation":false,"usgs":true,"family":"Paulachok","given":"Gary","email":"gnpaulac@usgs.gov","middleInitial":"N.","affiliations":[],"preferred":true,"id":495257,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Clark, Jeffrey S.","contributorId":85222,"corporation":false,"usgs":true,"family":"Clark","given":"Jeffrey","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":495261,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Zapecza, Otto S. ozapecza@usgs.gov","contributorId":3687,"corporation":false,"usgs":true,"family":"Zapecza","given":"Otto","email":"ozapecza@usgs.gov","middleInitial":"S.","affiliations":[],"preferred":true,"id":495258,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":45030,"text":"wri20004292 - 2001 - A field and statistical modeling study to estimate irrigation water use at Benchmark Farms study sites in southwestern Georgia, 1995-96","interactions":[],"lastModifiedDate":"2023-04-06T18:27:35.321456","indexId":"wri20004292","displayToPublicDate":"2001-01-01T00:00:00","publicationYear":"2001","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2000-4292","title":"A field and statistical modeling study to estimate irrigation water use at Benchmark Farms study sites in southwestern Georgia, 1995-96","docAbstract":"A benchmark irrigation monitoring network of farms located in a 32-county area in southwestern Georgia was established in 1995 to improve estimates of irrigation water use. A stratified random sample of 500 permitted irrigators was selected from a data base--maintained by the Georgia Department of Natural Resources, Georgia Environmental Protection Division, Water Resources Management Branch--to obtain 180 voluntary participants in the study area. Site-specific irrigation data were collected at each farm using running-time totalizers and noninvasive flowmeters. Data were collected and compiled for 50 farms for 1995 and 130 additional farms for the 1996 growing season--a total of 180 farms. Irrigation data collected during the 1996 growing season were compiled for 180 benchmark farms and used to develop a statistical model to estimate irrigation water use in 32 counties in southwestern Georgia. The estimates derived were developed from using a statistical approach know as \"bootstrap analysis\" that allows for the estimation of precision. Five model components--whether-to-irrigate, acres irrigated, crop selected, seasonal-irrigation scheduling, and the amount of irrigation applied--compose the irrigation model and were developed to reflect patterns in the data collected at Benchmark Farms Study area sites. The model estimated that peak irrigation for all counties in the study area occurred during July with significant irrigation also occurring during May, June, and August. Irwin and Tift were the most irrigated and Schley and Houston were the least irrigated counties in the study area. High irrigation intensity primarily was located along the eastern border of the study area; whereas, low irrigation intensity was located in the southwestern quadrant where ground water was the dominant irrigation source. Crop-level estimates showed sizable variations across crops and considerable uncertainty for all crops other than peanuts and pecans. Counties having the most irrigated acres showed higher variations in annual irrigation than counties having the least irrigated acres. The Benchmark Farms Study model estimates were higher than previous irrigation estimates, with 20 percent of the bias a result of underestimating irrigation acreage in earlier studies. Model estimates showed evidence of an upward bias of about 15 percent with the likely cause being a misrepresented inches-applied model. A better understanding of the causes of bias in the model could be determined with a larger irrigation sample size and increased substantially by automating the reporting of monthly totalizer amounts.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri20004292","usgsCitation":"Fanning, J.L., Schwarz, G., and Lewis, W., 2001, A field and statistical modeling study to estimate irrigation water use at Benchmark Farms study sites in southwestern Georgia, 1995-96: U.S. Geological Survey Water-Resources Investigations Report 2000-4292, vii, 32 p., https://doi.org/10.3133/wri20004292.","productDescription":"vii, 32 p.","temporalStart":"1995-01-01","temporalEnd":"1996-12-31","costCenters":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true}],"links":[{"id":135730,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":415362,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_37101.htm","linkFileType":{"id":5,"text":"html"}},{"id":8948,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/wri/wri00-4292/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Georgia","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -85.111083984375,\n 32.69486597787505\n ],\n [\n -85.089111328125,\n 32.59773394005744\n ],\n [\n -85.0286865234375,\n 32.532920675187846\n ],\n [\n -84.9737548828125,\n 32.47269502206151\n ],\n [\n -84.96826171874999,\n 32.393877575286446\n ],\n [\n -84.990234375,\n 32.375322284319346\n ],\n [\n -85.01220703125,\n 32.32427558887655\n ],\n [\n -84.96826171874999,\n 32.310348764525806\n ],\n [\n -84.9298095703125,\n 32.287132632616384\n ],\n [\n -84.891357421875,\n 32.25926542645933\n ],\n [\n -84.92431640625,\n 32.24068253457369\n ],\n [\n -84.9627685546875,\n 32.217448573031014\n ],\n [\n -84.9957275390625,\n 32.19885712788488\n ],\n [\n -85.0396728515625,\n 32.17096283641326\n ],\n [\n -85.0726318359375,\n 32.13375715632646\n ],\n [\n -85.0506591796875,\n 32.10118973232094\n ],\n [\n -85.0506591796875,\n 32.05930026106166\n ],\n [\n -85.067138671875,\n 31.994100723260804\n ],\n [\n -85.0946044921875,\n 31.914867503276223\n ],\n [\n -85.1385498046875,\n 31.863562548378965\n ],\n [\n -85.1385498046875,\n 31.812229022640704\n ],\n [\n -85.1275634765625,\n 31.737511125687828\n ],\n [\n -85.111083984375,\n 31.686107579079483\n ],\n [\n -85.0946044921875,\n 31.63467554954133\n ],\n [\n -85.067138671875,\n 31.606609719226917\n ],\n [\n -85.045166015625,\n 31.58321506275729\n ],\n [\n -85.05615234375,\n 31.522361470421437\n ],\n [\n -85.0836181640625,\n 31.42866311735861\n ],\n [\n -85.0946044921875,\n 31.330178972184655\n ],\n [\n -85.10009765625,\n 31.264465555752835\n ],\n [\n -85.11657714843749,\n 31.208103321325254\n ],\n [\n -85.1055908203125,\n 31.156408414557\n ],\n [\n -85.05615234375,\n 31.123496964067325\n ],\n [\n -85.0067138671875,\n 31.038815104128687\n ],\n [\n -85.0067138671875,\n 30.963479049959364\n ],\n [\n -84.957275390625,\n 30.90222470517144\n ],\n [\n -84.9407958984375,\n 30.826780904779774\n ],\n [\n -84.9078369140625,\n 30.746556862773616\n ],\n [\n -84.8638916015625,\n 30.69933500437198\n ],\n [\n -83.1500244140625,\n 30.62845887475364\n ],\n [\n -83.133544921875,\n 32.74570253945518\n ],\n [\n -85.111083984375,\n 32.69486597787505\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b24e4b07f02db6aeadf","contributors":{"authors":[{"text":"Fanning, Julia L.","contributorId":73981,"corporation":false,"usgs":true,"family":"Fanning","given":"Julia","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":230956,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Schwarz, Gregory E. 0000-0002-9239-4566 gschwarz@usgs.gov","orcid":"https://orcid.org/0000-0002-9239-4566","contributorId":543,"corporation":false,"usgs":true,"family":"Schwarz","given":"Gregory E.","email":"gschwarz@usgs.gov","affiliations":[{"id":5067,"text":"Northeast Regional Director's Office","active":true,"usgs":true},{"id":451,"text":"National Water Quality Assessment Program","active":true,"usgs":true}],"preferred":false,"id":230954,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Lewis, William C.","contributorId":50878,"corporation":false,"usgs":true,"family":"Lewis","given":"William C.","affiliations":[],"preferred":false,"id":230955,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70023687,"text":"70023687 - 2001 - Elevated carbon dioxide flux at the Dixie Valley geothermal field, Nevada; relations between surface phenomena and the geothermal reservoir","interactions":[],"lastModifiedDate":"2012-03-12T17:20:02","indexId":"70023687","displayToPublicDate":"2001-01-01T00:00:00","publicationYear":"2001","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1213,"text":"Chemical Geology","active":true,"publicationSubtype":{"id":10}},"title":"Elevated carbon dioxide flux at the Dixie Valley geothermal field, Nevada; relations between surface phenomena and the geothermal reservoir","docAbstract":"In the later part of the 1990s, a large die-off of desert shrubs occurred over an approximately 1 km2 area in the northwestern section of the Dixie Valley (DV) geothermal field. This paper reports results from accumulation-chamber measurements of soil CO2 flux from locations in the dead zone and stable isotope and chemical data on fluids from fumaroles, shallow wells, and geothermal production wells within and adjacent to the dead zone. A cumulative probability plot shows three types of flux sites within the dead zone: Locations with a normal background CO2 flux (7 g m-2 day-1); moderate flux sites displaying \"excess\" geothermal flux; and high flux sites near young vents and fumaroles. A maximum CO2 flux of 570 g m-2 day-1 was measured at a location adjacent to a fumarole. Using statistical methods appropriate for lognormally distributed populations of data, estimates of the geothermal flux range from 7.5 t day-1 from a 0.14-km2 site near the Stillwater Fault to 0.1 t day-1 from a 0.01 -km2 location of steaming ground on the valley floor. Anomalous CO2 flux is positively correlated with shallow temperature anomalies. The anomalous flux associated with the entire dead zone area declined about 35% over a 6-month period. The decline was most notable at a hot zone located on an alluvial fan and in the SG located on the valley floor. Gas geochemistry indicates that older established fumaroles along the Stillwater Fault and a 2-year-old vent in the lower section of the dead zone discharge a mixture of geothermal gases and air or gases from air-saturated meteoric water (ASMW). Stable isotope data indicate that steam from the smaller fumaroles is produced by ??? 100??C boiling of these mixed fluids and reservoir fluid. Steam from the Senator fumarole (SF) and from shallow wells penetrating the dead zone are probably derived by 140??C to 160??C boiling of reservoir fluid. Carbon-13 isotope data suggest that the reservoir CO2 is produced mainly by thermal decarbonation of hydrothermal calcite in veins that cut reservoir rocks. Formation of the dead zone is linked to the reservoir pressure decline caused by continuous reservoir drawdown from 1986 to present. These reservoir changes have restricted flow and induced boiling in a subsurface hydrothermal outflow plume extending from the Stillwater Fault southeast toward the DV floor. We estimate that maximum CO2 flux in the upflow zone along the Stillwater Fault in 1998 was roughly seven to eight times greater than the pre-production flux in 1986. The eventual decline in CO2 flux reflects the drying out of the outflow plume. Published by Elsevier Science B.V.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Chemical Geology","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","doi":"10.1016/S0009-2541(00)00381-8","issn":"00092541","usgsCitation":"Bergfeld, D., Goff, F., and Janik, C.J., 2001, Elevated carbon dioxide flux at the Dixie Valley geothermal field, Nevada; relations between surface phenomena and the geothermal reservoir: Chemical Geology, v. 177, no. 1-2, p. 43-66, https://doi.org/10.1016/S0009-2541(00)00381-8.","startPage":"43","endPage":"66","numberOfPages":"24","costCenters":[],"links":[{"id":207367,"rank":9999,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1016/S0009-2541(00)00381-8"},{"id":232264,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"177","issue":"1-2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a08c7e4b0c8380cd51c7f","contributors":{"authors":[{"text":"Bergfeld, D.","contributorId":58053,"corporation":false,"usgs":true,"family":"Bergfeld","given":"D.","email":"","affiliations":[],"preferred":false,"id":398451,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Goff, F.","contributorId":53408,"corporation":false,"usgs":true,"family":"Goff","given":"F.","email":"","affiliations":[],"preferred":false,"id":398450,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Janik, C. J.","contributorId":10795,"corporation":false,"usgs":true,"family":"Janik","given":"C.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":398449,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70180468,"text":"70180468 - 2001 - Quaternary geology, Cold Bay and False Pass quadrangles, Alaska Peninsula","interactions":[{"subject":{"id":70180468,"text":"70180468 - 2001 - Quaternary geology, Cold Bay and False Pass quadrangles, Alaska Peninsula","indexId":"70180468","publicationYear":"2001","noYear":false,"title":"Quaternary geology, Cold Bay and False Pass quadrangles, Alaska Peninsula"},"predicate":"IS_PART_OF","object":{"id":38272,"text":"pp1633 - 2001 - Geologic studies in Alaska by the U.S. Geological Survey, 1999","indexId":"pp1633","publicationYear":"2001","noYear":false,"title":"Geologic studies in Alaska by the U.S. Geological Survey, 1999"},"id":1}],"isPartOf":{"id":38272,"text":"pp1633 - 2001 - Geologic studies in Alaska by the U.S. Geological Survey, 1999","indexId":"pp1633","publicationYear":"2001","noYear":false,"title":"Geologic studies in Alaska by the U.S. Geological Survey, 1999"},"lastModifiedDate":"2021-08-30T21:03:50.009945","indexId":"70180468","displayToPublicDate":"2001-01-01T00:00:00","publicationYear":"2001","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"subseriesTitle":"1633","title":"Quaternary geology, Cold Bay and False Pass quadrangles, Alaska Peninsula","docAbstract":"Recent mapping and interpretation of Quaternary geologic features has improved our understanding of the interaction between volcanic, glacial, and tectonic activity in the Cold Bay and False Pass 1:250,000-scale quadrangles on the Alaska Peninsula. The glacial and volcanic record of the map area strongly suggests that continental-shelf glaciations and two massive volcanic centers were the dominant controls over landscape development during Pleistocene time. Ancestral Morzhovoi and Emmons Volcanoes were major impediments to flow of shelf glaciers during much of the Pleistocene. Our mapping suggests that the area around Emmons Volcano may have also been an important source area for glaciers during this period. Our data further indicate that Frosty Volcano developed late in the Pleistocene, having had no apparent impact on early Brooks Lake glacial advances but serving as a source area for later glacial advances during late Brooks Lake time. We also believe that major Holocene eruptions of Frosty Volcano have yielded multiple debris and ash flows resulting in the construction of a new south summit cone that filled an earlier crater. Frosty Volcano was the source area for multiple Holocene glacial advances, and its flanks preserve the best record of Neoglacial activity in the map area.
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Geologic studies in Alaska by the U.S. Geological Survey, 1999","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Denver, CO","doi":"10.3133/70180468","usgsCitation":"Wilson, F.H., and Weber, F.R., 2001, Quaternary geology, Cold Bay and False Pass quadrangles, Alaska Peninsula: U.S. Geological Survey Professional Paper, 21 p., https://doi.org/10.3133/70180468.","productDescription":"21 p.","startPage":"51","endPage":"71","numberOfPages":"21","costCenters":[{"id":114,"text":"Alaska Science Center","active":true,"usgs":true}],"links":[{"id":334364,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":334363,"rank":1,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/1633/pp1633_report.pdf#page=59","text":"Start page in larger work"}],"country":"United States","state":"Alaska","otherGeospatial":"Alaska Peninsula, Cold Bay quadrangle, False Pass quadrangle","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -153.72070312499997,\n 59.17592824927136\n ],\n [\n -157.060546875,\n 58.768200159239576\n ],\n [\n -159.609375,\n 56.70450561416937\n ],\n [\n -163.388671875,\n 55.32914440840507\n ],\n [\n -162.158203125,\n 54.67383096593114\n ],\n [\n -157.85156249999997,\n 55.97379820507658\n ],\n [\n -153.6328125,\n 58.722598828043374\n ],\n [\n -153.72070312499997,\n 59.17592824927136\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"58905ef4e4b072a7ac0cad53","contributors":{"authors":[{"text":"Wilson, Frederic H. 0000-0003-1761-6437 fwilson@usgs.gov","orcid":"https://orcid.org/0000-0003-1761-6437","contributorId":67174,"corporation":false,"usgs":true,"family":"Wilson","given":"Frederic","email":"fwilson@usgs.gov","middleInitial":"H.","affiliations":[{"id":114,"text":"Alaska Science Center","active":true,"usgs":true},{"id":119,"text":"Alaska Science Center Geology Minerals","active":true,"usgs":true}],"preferred":true,"id":661721,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Weber, Florence R.","contributorId":17621,"corporation":false,"usgs":true,"family":"Weber","given":"Florence","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":661722,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70023242,"text":"70023242 - 2001 - Seismic tomography shows that upwelling beneath Iceland is confined to the upper mantle","interactions":[],"lastModifiedDate":"2012-03-12T17:19:59","indexId":"70023242","displayToPublicDate":"2001-01-01T00:00:00","publicationYear":"2001","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1803,"text":"Geophysical Journal International","active":true,"publicationSubtype":{"id":10}},"title":"Seismic tomography shows that upwelling beneath Iceland is confined to the upper mantle","docAbstract":"We report the results of the highest-resolution teleseismic tomography study yet performed of the upper mantle beneath Iceland. The experiment used data gathered by the Iceland Hotspot Project, which operated a 35-station network of continuously recording, digital, broad-band seismometers over all of Iceland 1996-1998. The structure of the upper mantle was determined using the ACH damped least-squares method and involved 42 stations, 3159 P-wave, and 1338 S-wave arrival times, including the phases P, pP, sP, PP, SP, PcP, PKIKP, pPKIKP, S, sS, SS, SKS and Sdiff. Artefacts, both perceptual and parametric, were minimized by well-tested smoothing techniques involving layer thinning and offset-and-averaging. Resolution is good beneath most of Iceland from ??? 60 km depth to a maximum of ??? 450 km depth and beneath the Tjornes Fracture Zone and near-shore parts of the Reykjanes ridge. The results reveal a coherent, negative wave-speed anomaly with a diameter of 200-250 km and anomalies in P-wave speed, Vp, as strong as -2.7 per cent and in S-wave speed, Vs, as strong as -4.9 per cent. The anomaly extends from the surface to the limit of good resolution at ??? 450 km depth. In the upper ??? 250 km it is centred beneath the eastern part of the Middle Volcanic Zone, coincident with the centre of the ??? 100 mGal Bouguer gravity low over Iceland, and a lower crustal low-velocity zone identified by receiver functions. This is probably the true centre of the Iceland hotspot. In the upper ??? 200 km, the low-wave-speed body extends along the Reykjanes ridge but is sharply truncated beneath the Tjornes Fracture Zone. This suggests that material may flow unimpeded along the Reykjanes ridge from beneath Iceland but is blocked beneath the Tjornes Fracture Zone. The magnitudes of the Vp, Vs and Vp/Vs anomalies cannot be explained by elevated temperature alone, but favour a model of maximum temperature anomalies <200 K, along with up to ??? 2 per cent of partial melt in the depth range ??? 100-300 km beneath east-central Iceland. The anomalous body is approximately cylindrical in the top 250 km but tabular in shape at greater depth, elongated north-south and generally underlying the spreading plate boundary. Such a morphological change and its relationship to surface rift zones are predicted to occur in convective upwellings driven by basal heating, passive upwelling in response to plate separation and lateral temperature gradients. Although we cannot resolve structure deeper than ??? 450 km, and do not detect a bottom to the anomaly, these models suggest that it extends no deeper than the mantle transition zone. Such models thus suggest a shallow origin for the Iceland hotspot rather than a deep mantle plume, and imply that the hotspot has been located on the spreading ridge in the centre of the north Atlantic for its entire history, and is not fixed relative to other Atlantic hotspots. The results are consistent with recent, regional full-thickness mantle tomography and whole-mantle tomography images that show a strong, low-wave-speed anomaly beneath the Iceland region that is confined to the upper mantle and thus do not require a plume in the lower mantle. Seismic and geochemical observations that are interpreted as indicating a lower mantle, or core-mantle boundary origin for the North Atlantic Igneous Province and the Iceland hotspot should be re-examined to consider whether they are consistent with upper mantle processes.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Geophysical Journal International","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","doi":"10.1046/j.0956-540X.2001.01470.x","issn":"0956540X","usgsCitation":"Foulger, G., Pritchard, M., Julian, B., Evans, J., Allen, R.M., Nolet, G., Morgan, W.J., Bergsson, B.H., Erlendsson, P., Jakobsdottir, S., Ragnarsson, S., Stefansson, R., and Vogfjord, K., 2001, Seismic tomography shows that upwelling beneath Iceland is confined to the upper mantle: Geophysical Journal International, v. 146, no. 2, p. 504-530, https://doi.org/10.1046/j.0956-540X.2001.01470.x.","startPage":"504","endPage":"530","numberOfPages":"27","costCenters":[],"links":[{"id":478974,"rank":10000,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.1046/j.0956-540x.2001.01470.x","text":"Publisher Index Page"},{"id":207314,"rank":9999,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1046/j.0956-540X.2001.01470.x"},{"id":232159,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"146","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505b8b6fe4b08c986b31781e","contributors":{"authors":[{"text":"Foulger, G.R.","contributorId":14439,"corporation":false,"usgs":false,"family":"Foulger","given":"G.R.","email":"","affiliations":[],"preferred":false,"id":396984,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Pritchard, M.J.","contributorId":102656,"corporation":false,"usgs":true,"family":"Pritchard","given":"M.J.","email":"","affiliations":[],"preferred":false,"id":396993,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Julian, B.R.","contributorId":101272,"corporation":false,"usgs":true,"family":"Julian","given":"B.R.","email":"","affiliations":[],"preferred":false,"id":396992,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Evans, J.R.","contributorId":50526,"corporation":false,"usgs":true,"family":"Evans","given":"J.R.","email":"","affiliations":[],"preferred":false,"id":396988,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Allen, R. M.","contributorId":36170,"corporation":false,"usgs":false,"family":"Allen","given":"R.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":396987,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Nolet, G.","contributorId":26448,"corporation":false,"usgs":true,"family":"Nolet","given":"G.","email":"","affiliations":[],"preferred":false,"id":396986,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Morgan, W. J.","contributorId":10573,"corporation":false,"usgs":false,"family":"Morgan","given":"W.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":396981,"contributorType":{"id":1,"text":"Authors"},"rank":7},{"text":"Bergsson, B. H.","contributorId":19320,"corporation":false,"usgs":false,"family":"Bergsson","given":"B.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":396985,"contributorType":{"id":1,"text":"Authors"},"rank":8},{"text":"Erlendsson, P.","contributorId":95638,"corporation":false,"usgs":true,"family":"Erlendsson","given":"P.","email":"","affiliations":[],"preferred":false,"id":396991,"contributorType":{"id":1,"text":"Authors"},"rank":9},{"text":"Jakobsdottir, S.","contributorId":64828,"corporation":false,"usgs":true,"family":"Jakobsdottir","given":"S.","email":"","affiliations":[],"preferred":false,"id":396989,"contributorType":{"id":1,"text":"Authors"},"rank":10},{"text":"Ragnarsson, S.","contributorId":12644,"corporation":false,"usgs":true,"family":"Ragnarsson","given":"S.","email":"","affiliations":[],"preferred":false,"id":396982,"contributorType":{"id":1,"text":"Authors"},"rank":11},{"text":"Stefansson, R.","contributorId":81650,"corporation":false,"usgs":true,"family":"Stefansson","given":"R.","email":"","affiliations":[],"preferred":false,"id":396990,"contributorType":{"id":1,"text":"Authors"},"rank":12},{"text":"Vogfjord, K.","contributorId":13768,"corporation":false,"usgs":true,"family":"Vogfjord","given":"K.","email":"","affiliations":[],"preferred":false,"id":396983,"contributorType":{"id":1,"text":"Authors"},"rank":13}]}} ,{"id":70174307,"text":"70174307 - 2001 - Time series of suspended-solids concentration, salinity, temperature, and total mercury concentration in San Francisco Bay during water year 1998","interactions":[],"lastModifiedDate":"2016-07-27T13:18:41","indexId":"70174307","displayToPublicDate":"1999-12-31T00:00:00","publicationYear":"2001","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":9,"text":"Other Report"},"title":"Time series of suspended-solids concentration, salinity, temperature, and total mercury concentration in San Francisco Bay during water year 1998","docAbstract":"Many physical processes affect how constituents within San Francisco Bay vary. Processes and their associated time scales include turbulence (seconds), semidiurnal and diurnal tides (hours), the spring-neap tidal cycle (days), freshwater flow (weeks), seasonal winds (months), ecological and climatic changes (years), and geologic changes (thousands of years). Continuous time series of data on basic state variables of the bay, such as suspended-solids concentration (SSC), salinity, and water temperature, provide insight on the effect and relative importance of physical processes on the bay. SSC time series and Regional Monitoring Program (RMP) water-quality data can be used to calculate time series of some traceelement concentrations (Schoellhamer, 1997a, 1997b). The purpose of this chapter is to describe qualitatively time series of SSC, salinity, water temperature, and mercury during water year 1998 (October 1997 through September 1998).
\nSalinity, temperature, and sediment are important components of the San Francisco Bay estuarine system. Salinity and temperature affect the hydrodynamics (Monismith et al., 1996; Schoellhamer and Burau, 1998), geochemistry (Kuwabara et al., 1989), and ecology (Cloern, 1984; Nichols et al., 1986; Jassby et al., 1995) of the bay. Suspended sediments limit light availability in the bay, which, in turn, limits primary production (Cloern, 1987; Cole and Cloern, 1987), and thus food for higher trophic levels. Sediments deposit in ports and shipping channels, which must be dredged to maintain navigation (U.S. Environmental Protection Agency, 1992). Potentially toxic substances, such as metals and pesticides, adsorb to sediment particles (Kuwabara et al., 1989; Domagalski and Kuivila, 1993; Flegal et al., 1996; Schoellhamer, 1997a, 1997b).
\nThe transport and fate of suspended sediments are important factors in determining the transport and fate of constituents adsorbed on the sediments. For example, the concentration of suspended particulate chromium in the bay appears to be controlled primarily by sediment resuspension (Abu-Saba and Flegal, 1995). Concentrations of dissolved trace elements are greater in South Bay than elsewhere in San Francisco Bay, and bottom sediments are believed to be a significant source (Flegal et al., 1991). The sediments on the bay bottom provide habitat for benthic communities that can ingest these substances and introduce them into the food web (Luoma et al., 1985; Brown and Luoma, 1995, Luoma 1996). Bottom sediments also are a reservoir of nutrients that contribute to the maintenance of estuarine productivity (Hammond et al., 1985).
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