During the early 1990s (but echoing studies by S.T. Harding at the University of California, from as early as the 1930s), several lines of paleoclimate evidence in and around the Sierra Nevada Range have provided the water community in California with some real horror stories. By studying ancient tree stumps submerged in Lake Tahoe and Tenaya Lake, stumps that were emerging from Mono Lake during its recent decline, and stumps that were exhumed in the Walker River bed during the floods of 1997, paleoclimatologists like Scott Stine of California State University, Hayward, assembled a picture of epic droughts in the central Sierra Nevada during the medieval period. These droughts had to be severe to drop water levels in the lakes and rivers low enough for the trees to grow in the first place, and then had to last for hundreds of years to explain tree-ring counts in these sizeable stumps. Worse yet, the evidence suggested at least two such epic droughts, one ending close to 1100 and the other close to 1350. These epic droughts challenged paleoclimatologists, as well as modern climatologists and hydrologists, to understand and, ultimately, to determine the likelihood that such droughts might recur in the foreseeable future. The first challenge, however, was to verify that such droughts were more than local events and as extreme as suggested. At this year’s Pacific Climate (PACLIM) Workshop, held March 18–21, 2001, at Asilomar (Pacific Grove, Calif.), special sessions brought together scientists to compare paleoclimatic reconstructions of ancient droughts and pluvial (wet) epidodes to try to determine the nature of decadal and centennial climate fluctuations in western North America, with emphasis on California. A companion session brought together modern climatologists to report on the latest explanations (and evidence) for decadal climate variations during the instrumental era of the 20th century.
","language":"English","publisher":"Interagency","usgsCitation":"Dettinger, M.D., 2001, Droughts, epic droughts and droughty centuries - lessons from a California paleoclimatic record: a PACLIM 2001 meeting report: Interagency Ecological Program Newsletter, v. 14, no. 3, p. 51-53.","productDescription":"3 p.","startPage":"51","endPage":"53","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":552,"text":"San Francisco Bay-Delta","active":false,"usgs":true},{"id":5079,"text":"Pacific Regional Director's Office","active":true,"usgs":true}],"links":[{"id":325161,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":325160,"rank":1,"type":{"id":15,"text":"Index Page"},"url":"https://www.water.ca.gov/iep/newsletters/2001/IEPNewsletterSummer2001.pdf"}],"volume":"14","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"579b2caee4b0589fa1c9809d","contributors":{"authors":[{"text":"Dettinger, M. D. 0000-0002-7509-7332","orcid":"https://orcid.org/0000-0002-7509-7332","contributorId":93069,"corporation":false,"usgs":false,"family":"Dettinger","given":"M.","middleInitial":"D.","affiliations":[{"id":16196,"text":"Scripps Institution of Oceanography, La Jolla, CA","active":true,"usgs":false}],"preferred":false,"id":642308,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":30897,"text":"wri014014 - 2001 - Analysis of borehole-radar reflection logs from selected HC boreholes at the Project Shoal area, Churchill County, Nevada","interactions":[],"lastModifiedDate":"2019-10-15T11:28:55","indexId":"wri014014","displayToPublicDate":"2001-09-01T00:00:00","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":"2001-4014","title":"Analysis of borehole-radar reflection logs from selected HC boreholes at the Project Shoal area, Churchill County, Nevada","docAbstract":"Single-hole borehole-radar reflection logs were collected and interpreted in support of a study to characterize ground-water flow and transport at the Project Shoal Area (PSA) in Churchill County, Nevada. Radar logging was conducted in six boreholes using 60-MHz omni-directional electric-dipole antennas and a 60-MHz magnetic-dipole directional receiving antenna.Radar data from five boreholes were interpreted to identify the location, orientation, estimated length, and spatial continuity of planar reflectors present in the logs. The overall quality of the radar data is marginal and ranges from very poor to good. Twenty-seven reflectors were interpreted from the directional radar reflection logs. Although the range of orientation interpreted for the reflectors is large, a significant number of reflectors strike northeast-southwest and east-west to slightly northwest-southeast. Reflectors are moderate to steeply dipping and reflector length ranged from less than 7 m to more than 133 m.Qualitative scores were assigned to each reflector to provide a sense of the spatial continuity of the reflector and the characteristics of the field data relative to an ideal planar reflector (orientation score). The overall orientation scores are low, which reflects the general data quality, but also indicates that the properties of most reflectors depart from the ideal planar case. The low scores are consistent with reflections from fracture zones that contain numerous, closely spaced, sub-parallel fractures.Interpretation of borehole-radar direct-wave velocity and amplitude logs identified several characteristics of the logged boreholes: (1) low-velocity zones correlate with decreased direct-wave amplitude, indicating the presence of fracture zones; (2) direct-wave amplitude increases with depth in three of the boreholes, suggesting an increase in electrical resistivity with depth resulting from changes in mineral assemblage or from a decrease in the specific conductance of ground water; and (3) an increase in primary or secondary porosity and an associated change in mineral assemblage, or decrease in ground water specific conductance, was characterized in two of the boreholes below 300 m.The results of the radar reflection logging indicate that even where data quality is marginal, borehole-radar reflection logging can provide useful information for ground-water characterization studies in fractured rock and insights into the nature and extent of fractures and fracture zones in and near boreholes.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri014014","usgsCitation":"Lane, J., Joesten, P., Pohll, G., and Mihevic, T., 2001, Analysis of borehole-radar reflection logs from selected HC boreholes at the Project Shoal area, Churchill County, Nevada: U.S. Geological Survey Water-Resources Investigations Report 2001-4014, iv, 23 p. , https://doi.org/10.3133/wri014014.","productDescription":"iv, 23 p. ","costCenters":[{"id":493,"text":"Office of Ground Water","active":true,"usgs":true}],"links":[{"id":160124,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":2835,"rank":100,"type":{"id":11,"text":"Document"},"url":"https://water.usgs.gov/ogw/bgas/publications/wri014014/wri014014.pdf","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Nevada","county":"Churchill County","otherGeospatial":"Project 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J.W. Jr.","contributorId":66723,"corporation":false,"usgs":true,"family":"Lane","given":"J.W.","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":204306,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Joesten, P. K.","contributorId":62818,"corporation":false,"usgs":true,"family":"Joesten","given":"P. K.","affiliations":[],"preferred":false,"id":204304,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Pohll, G.M.","contributorId":65261,"corporation":false,"usgs":true,"family":"Pohll","given":"G.M.","email":"","affiliations":[],"preferred":false,"id":204305,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Mihevic, Todd","contributorId":87416,"corporation":false,"usgs":true,"family":"Mihevic","given":"Todd","email":"","affiliations":[],"preferred":false,"id":204307,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":30896,"text":"wri014012 - 2001 - Summary of and factors affecting pesticide concentrations in streams and shallow wells of the lower Susquehanna River basin, Pennsylvania and Maryland, 1993-95","interactions":[],"lastModifiedDate":"2018-02-26T15:58:23","indexId":"wri014012","displayToPublicDate":"2001-09-01T00:00:00","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":"2001-4012","title":"Summary of and factors affecting pesticide concentrations in streams and shallow wells of the lower Susquehanna River basin, Pennsylvania and Maryland, 1993-95","docAbstract":"This report presents the detection frequency of 83 analyzed pesticides, describes the concentrations of those pesticides measured in water from streams and shallow wells, and presents conceptual models of the major factors affecting seasonal and areal patterns of pesticide concentrations in water from streams and shallow wells in the Lower Susquehanna River Basin. Seasonal and areal patterns of pesticide concentrations were observed in 577 samples and nearly 40,000 pesticide analyses collected from 155 stream sites and 169 shallow wells from 1993 to 1995. For this study, shallow wells were defined as those generally less than 200 feet deep.
The most commonly detected pesticides were agricultural herbicides?atrazine, metolachlor, simazine, prometon, alachlor, and cyanazine. Atrazine and metolachlor are the two most-used agricultural pesticides in the Lower Susquehanna River Basin. Atrazine was detected in 92 percent of all the samples and in 98 percent of the stream samples. Metolachlor was detected in 83 percent of all the samples and in 95 percent of the stream samples. Nearly half of all the analyzed pesticides were not detected in any sample. Of the 45 pesticides that were detected at least once, the median concentrations of 39 of the pesticides were less than the detection limit for the individual compounds, indicating that for at least 50 percent of the samples collected, those pesticides were not detected. Only 10 (less than 0.025 percent) of the measured concentrations exceeded any established drinking-water standards; 25 concentrations exceeded 2 mg/L (micrograms per liter) and 55 concentrations exceeded 1 mg/L. None of the elevated concentrations were measured in samples collected from streams that are used for public drinking-water supplies, and 8 of the 10 were measured in storm-affected samples.
The timing and rate of agricultural pesticide applications affect the seasonal and areal concentration patterns of atrazine, simazine, chlorpyrifos, and diazinon observed in water from wells and streams in the Lower Susquehanna River Basin. Average annual pesticide use for agricultural purposes and nonagricultural pesticide use indicators were used to explain seasonal and areal patterns. Elevated concentrations of some pesticides in streams during base-flow and storm-affected conditions were related to the seasonality of agricultural-use applications and local climate conditions. Agricultural-use patterns affected areal concentration patterns for the high-use pesticides, but indicators of nonagricultural use were needed to explain concentration patterns of pesticides with smaller amounts used for agricultural purposes.
Bedrock type influences the movement and discharge of ground water, which in turn affects concentration patterns of pesticides. The ratio of atrazine concentrations in stream base flow to concentrations in shallow wells varied among the different general rock types found in the Lower Susquehanna River Basin. Median concentrations of atrazine in well water and stream base flow tended to be similar in individual areas underlain by carbonate bedrock, indicating the connectivity of water in streams and shallow wells in these areas. In areas underlain by noncarbonate bedrock, median concentrations of atrazine tended to be significantly higher in stream base flow than in well water. This suggests a deep ground-water system that delivers water to shallow wells and a near-surficial system that supplies base-flow water to streams. In addition to the presence or absence of carbonate bedrock, pesticide leaching potential and persistence, soil infiltration capacity, and agricultural land use affected areal patterns in detection frequency and concentration differences between samples collected from streams during base-flow conditions and shallow wells.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri014012","usgsCitation":"Hainly, R.A., Zimmerman, T.M., Loper, C.A., and Lindsey, B., 2001, Summary of and factors affecting pesticide concentrations in streams and shallow wells of the lower Susquehanna River basin, Pennsylvania and Maryland, 1993-95: U.S. Geological Survey Water-Resources Investigations Report 2001-4012, viii, 75 p., https://doi.org/10.3133/wri014012.","productDescription":"viii, 75 p.","onlineOnly":"Y","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":351012,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2001/4012/wri20014012.pdf","text":"Report","size":"4.79 MB","linkFileType":{"id":1,"text":"pdf"},"description":"WRI 2001-4012"},{"id":160118,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/2001/4012/coverthb.jpg"}],"contact":"Director, Pennsylvania Water Science Center
U.S. Geological Survey
215 Limekiln Road
New Cumberland, PA 17070
During 1997–98, the U.S. Geological Survey, in cooperation with the Houston-Galveston Area Council, collected stream-habitat and benthic macroinvertebrate data for 31 reaches on abovetidal streams in the Council service area near Houston, Texas. Stream-habitat, land-use and population, and benthic aquatic insect metrics were determined for the 31 reaches. Statistical analyses were used to determine the stream-habitat, land-use and population, and aquatic insect variables that are strongly intercorrelated and that explain the greatest amount of variation between the reaches.
Comparison of stream-habitat and biological integrity scores computed for each of the 31 reaches indicated (1) reaches generally had larger stream-habitat integrity scores in drainage areas that were heavily forested and had fewer people per square mile, (2) larger biological integrity scores were significantly correlated with larger stream-habitat integrity scores, and (3) urban reaches generally had more simplified streamhabitat conditions and smaller biological integrity scores.
Seven reaches in the study area were selected as reference reaches on the basis of high streamhabitat integrity and high biological integrity. The reference-reaches median biological integrity score was equaled or exceeded by three reaches (one on Spring Creek and two on Cypress Creek) that are on the State of Texas 303(d) list of threatened or impaired waters with respect to aquatic life. This indicates that direct measures of biological integrity could be used to supplement surrogatebased designations of biological integrity such as the State list.
A statistically significant multipleregression model was developed that uses independent variables that can be obtained without fieldintensive studies to predict the biological integrity score for a reach. The deviation from the model’s predicted score with the score based on biological sampling can be used to interpret the degree of biological impairment in a reach. Data from reaches outside the group of reaches used in this study are needed to test the validity of the multipleregression model.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri014010","usgsCitation":"Moring, J., 2001, Influence of stream habitat and land use on benthic macroinvertebrate indicators of stream quality of selected above-tidal streams in the Houston-Galveston Area Council service area, Texas, 1997–98: U.S. Geological Survey Water-Resources Investigations Report 2001-4010, 22 p., https://doi.org/10.3133/wri014010.","productDescription":"22 p.","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":160117,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/wri014010.PNG"},{"id":393816,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_38857.htm"},{"id":328037,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/wri014010/pdf/01-4010.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":2833,"rank":99,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri014010/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Texas","city":"Galveston, Houston","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -95.8062744140625,\n 29.19532826709913\n ],\n [\n -94.669189453125,\n 29.19532826709913\n ],\n [\n -94.669189453125,\n 30.244831915307145\n ],\n [\n -95.8062744140625,\n 30.244831915307145\n ],\n [\n -95.8062744140625,\n 29.19532826709913\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49c2e4b07f02db5d3acf","contributors":{"authors":[{"text":"Moring, J. Bruce","contributorId":53372,"corporation":false,"usgs":true,"family":"Moring","given":"J. Bruce","affiliations":[],"preferred":false,"id":204299,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":30887,"text":"wri20004266 - 2001 - Simulation of flow in the upper North Coast Limestone Aquifer, Manati-Vega Baja area, Puerto Rico","interactions":[],"lastModifiedDate":"2012-03-08T17:16:16","indexId":"wri20004266","displayToPublicDate":"2001-09-01T00:00:00","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":"2000-4266","title":"Simulation of flow in the upper North Coast Limestone Aquifer, Manati-Vega Baja area, Puerto Rico","docAbstract":"A two-dimensional computer ground-water model was constructed of the Manati-Vega Baja area to improve the understanding of the unconfined upper aquifer within the North Coast Province of Puerto Rico. The modeled area covers approximately 79 square miles within the municipios of Manati and Vega Baja and small portions of Vega Alta and Barceloneta. \r\n\r\nSteady-state two-dimensional ground-water simulations were correlated to conditions prior to construction of the Laguna Tortuguero outlet channel in 1940 and calibrated to the observed potentiometric surface in March 1995. At the regional scale, the unconfined Upper North Coast Limestone aquifer is a diffuse ground-water flow system through the Aguada and Aymamon limestone units. The calibrated model input parameters for aquifer recharge varied from 2 inches per year in coastal areas to 18 inches per year in the upland areas south of Manati and Vega Baja. The calibrated transmissivity values ranged from less than 500 feet squared per day in the upland areas near the southern boundary to 70,000 feet squared per day in the areas west of Vega Baja. Increased ground-water withdrawals from 1.0 cubic foot per second for 1940 conditions to 26.3 cubic feet per second in 1995, has reduced the natural ground-water discharge to springs and wetland areas, and induced additional recharge from the rivers. The most important regional drainage feature is Laguna Tortuguero, which is the major ground-water discharge body for the upper aquifer, and has a drainage area of approximately 17 square miles. The discharge to the sea from Laguna Tortuguero through the outlet channel has been measured on a bi-monthly basis since 1974. The outflow represents a combination of ground- and surface-water discharge over the drainage area. \r\n\r\nHydrologic conditions, prior to construction of the Laguna Tortuguero outlet channel in 1943, can be considered natural conditions with minimal ground-water pumpage (1.0 cubic foot per second), and heads in the lagoon were 2.4 feet higher. The model was calibrated to March 1995 conditions during a dry period of minimal aquifer recharge and relatively constant water levels in the upper aquifer. For the steady-state 1995 model simulation, however, ground-water pumpage had been increased to 26.3 cubic foot per second, due to increased demand for public water supply, the heads at 0.9 feet, and the outflow to the sea at Laguna Tortuguero had been lowered considerably. Simulated ground-water inflow for 1940 hydrologic conditions included 35.9 cubic feet per second from areal recharge, contributions from streamflow along the southern boundary of 1.6 cubic feet per second, and streamflow infiltration to the upper aquifer of 4.2 cubic feet per second. Simulated ground-water outflow for 1940 hydrologic conditions are discharge to springs of 17.4 cubic feet per second, total ground-water withdrawals of 1.0 cubic feet per second, and aquifer contribution to streamflow or wetland areas of 23.4 cubic feet per second. \r\n\r\nSimulated ground-water inflow for hydrologic conditions of March 1995 include d contributions from streamflow along the southern boundary of 1.6 cubic feet per second, areal recharge of 35.9 cubic feet per second, and streamflow infiltration to the upper aquifer of 11 cubic feet per second. Simulated ground-water outflow for hydrologic conditions of March 1995 are ground-water withdrawals of 26.3 cubic feet per second, discharge from springs of 7.3 cubic feet per second, and aquifer contribution to streamflow or wetland areas of 14 .9 cubic feet per second. The overall ground-water budget increased from 41.8 cubic feet per second for 1940 conditions to 48.6 cubic feet per second for the hydrologic conditions of March 1995. The increase in ground-water budget is a direct result of increased ground-water withdrawals, which induced greater streamflow infiltration. \r\n\r\nSimulated ground-water flux to Laguna Tortuguero for 1940 conditions was 11 cubic feet per second, which drop","language":"ENGLISH","doi":"10.3133/wri20004266","collaboration":"In cooperation with the\r\nPUERTO RICO DEPARTMENT OF NATURAL AND ENVIRONMENTAL RESOURCES and the PUERTO RICO INDUSTRIAL DEVELOPMENT CORPORATION","usgsCitation":"Cherry, G.S., 2001, Simulation of flow in the upper North Coast Limestone Aquifer, Manati-Vega Baja area, Puerto Rico: U.S. Geological Survey Water-Resources Investigations Report 2000-4266, vi, 82 p. , https://doi.org/10.3133/wri20004266.","productDescription":"vi, 82 p. ","costCenters":[{"id":156,"text":"Caribbean Water Science Center","active":true,"usgs":true}],"links":[{"id":160993,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":9217,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/wri/wri00-4266/","linkFileType":{"id":5,"text":"html"}}],"geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -66.61777777777777,18.366944444444446 ], [ -66.61777777777777,18.5 ], [ -66.25,18.5 ], [ -66.25,18.366944444444446 ], [ -66.61777777777777,18.366944444444446 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a7ee4b07f02db6485ff","contributors":{"authors":[{"text":"Cherry, Gregory S. 0000-0002-5567-1587 gccherry@usgs.gov","orcid":"https://orcid.org/0000-0002-5567-1587","contributorId":1567,"corporation":false,"usgs":true,"family":"Cherry","given":"Gregory","email":"gccherry@usgs.gov","middleInitial":"S.","affiliations":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true},{"id":316,"text":"Georgia Water Science Center","active":true,"usgs":true}],"preferred":true,"id":204276,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":30885,"text":"wri004250 - 2001 - Source identification and fish exposure for polychlorinated biphenyls using congener analysis from passive water samplers in the Millers River basin, Massachusetts","interactions":[],"lastModifiedDate":"2012-02-02T00:09:12","indexId":"wri004250","displayToPublicDate":"2001-09-01T00:00:00","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":"2000-4250","title":"Source identification and fish exposure for polychlorinated biphenyls using congener analysis from passive water samplers in the Millers River basin, Massachusetts","docAbstract":"Measurements of elevated concentrations of polychlorinated biphenyls (PCBs) in fish and in streambed sediments of the Millers River Basin, Massachusetts and New Hampshire, have been reported without evidence of the PCB source. In 1999, an investigation was initiated to determine the source(s) of the elevated PCB concentrations observed in fish and to establish the extent of fish exposure to PCBs along the entire main stems of the Millers River and one of its tributaries, the Otter River. \r\n\r\nPassive samplers deployed for 2-week intervals in the water-column at 3 1 stations, during summer and fall 1999, were used to assess PCB concentrations in the Millers River Basin. The samplers concentrate PCBs, which diffuse from the water column through a polyethylene membrane to hexane (0.200 liters) contained inside the samplers. Only dissolved PCBs (likely equivalent to the bioavailable fraction) are subject to diffusion through the membrane. The summed concentrations of all targeted PCB congeners (summed PCB) retrieved from the samplers ranged from 1 to 8,000 nanograms per hexane sample. Concentration and congener-pattern comparisons indicated that the historical release of PCBs in the Millers River Basin likely occurred on the Otter River at the upstream margin of Baldwinville, Mass. Elevated water-column concentrations measured in a wetland reach on the Otter River downstream from Baldwinville were compatible with a conceptual model for a present-day (1999) source in streambed sediments, to which the PCBs partitioned after their original introduction into the Otter River and from which PCBs are released to the water now that the original discharge has ceased or greatly decreased. \r\n\r\nTwo four-fold decreases in summed PCB concentrations in the Millers River, by comparison with the highest concentration on the Otter River, likely were caused by (1) dilution with water from the relatively uncontaminated upstream Millers River and (2) volatilization of PCBs from the Millers River in steep-gradient reaches. A relatively constant concentration of summed PCBs in the reach of the Millers River from river mile 20 to river mile 10 was likely a consequence of a balance between decreased volatilization rates in that relatively low-gradient reach and resupply of PCBs to the water column from contaminated streambed sediments. A second high-gradient reach from river mile 10 to the confluence of the Millers River with the Connecticut River also was associated with a decrease in concentration of water-column summed PCBs. Volatilization as a loss mechanism was supported by evidence in the form of slight changes of the congener pattern in the reaches where decreases occurred. \r\n\r\nExposure of fish food webs to concentrations of dissolved PCBs exceeded the U.S. Environmental Protection Agency's water-quality criterion for PCBs throughout most of the Millers River and Otter River main stems. Because the apparent source of PCBs discharged was upstream on the Otter River, a large number of river miles downstream (more than 30 mi) had summer water-column PCB concentrations that would likely lead to high concentrations of PCBs in fish.","language":"ENGLISH","doi":"10.3133/wri004250","usgsCitation":"Colman, J.A., 2001, Source identification and fish exposure for polychlorinated biphenyls using congener analysis from passive water samplers in the Millers River basin, Massachusetts: U.S. Geological Survey Water-Resources Investigations Report 2000-4250, 44 p. , https://doi.org/10.3133/wri004250.","productDescription":"44 p. ","costCenters":[],"links":[{"id":2792,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri004250/","linkFileType":{"id":5,"text":"html"}},{"id":161470,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e6e4b07f02db5e774a","contributors":{"authors":[{"text":"Colman, John A. 0000-0001-9327-0779 jacolman@usgs.gov","orcid":"https://orcid.org/0000-0001-9327-0779","contributorId":2098,"corporation":false,"usgs":true,"family":"Colman","given":"John","email":"jacolman@usgs.gov","middleInitial":"A.","affiliations":[{"id":466,"text":"New England Water Science Center","active":true,"usgs":true},{"id":376,"text":"Massachusetts Water Science Center","active":true,"usgs":true}],"preferred":true,"id":204273,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":33065,"text":"b2201D - 2001 - Petroleum geology and resources of the North Ustyurt Basin, Kazakhstan and Uzbekistan","interactions":[],"lastModifiedDate":"2024-10-11T10:57:00.043534","indexId":"b2201D","displayToPublicDate":"2001-09-01T00:00:00","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":"2201","chapter":"D","title":"Petroleum geology and resources of the North Ustyurt Basin, Kazakhstan and Uzbekistan","docAbstract":"The triangular-shaped North Ustyurt basin is located between the Caspian Sea and the Aral Lake in Kazakhstan and Uzbekistan and extends offshore both on the west and east. Along all its sides, the basin is bounded by the late Paleozoic and Triassic foldbelts that are partially overlain by Jurassic and younger rocks. The basin formed on a cratonic microcontinental block that was accreted northward to the Russian craton in Visean or Early Permian time. Continental collision and deformation\r\nalong the southern and eastern basin margins occurred in Early Permian time. In Late Triassic time, the basin was subjected\r\nto strong compression that resulted in intrabasinal thrusting\r\nand faulting.\r\nJurassic-Tertiary, mostly clastic rocks several hundred meters to 5 km thick overlie an older sequence of Devonian?Middle Carboniferous carbonates, Upper Precambrian massifs and deformed Caledonian foldbelts. The\r\nCarboniferous?Lower Permian clastics, carbonates, and volca-basement is at depths from 5.5 km on the highest uplifts to 11\r\nnics, and Upper Permian?Triassic continental clastic rocks, pri-km in the deepest depressions.\r\nmarily red beds. Paleogeographic conditions of sedimentation, Three total petroleum systems are identified in the basin.\r\nthe distribution of rock types, and the thicknesses of pre-Triassic Combined volumes of discovered hydrocarbons in these sysstratigraphic\r\nunits are poorly known because the rocks have been tems are nearly 2.4 billion barrels of oil and 2.4 trillion cubic\r\npenetrated by only a few wells in the western and eastern basin feet of gas. Almost all of the oil reserves are in the Buzachi Arch\r\nareas. The basement probably is heterogeneous; it includes and Surrounding Areas Composite Total Petroleum System in\r\n2 Petroleum Geology, Resources?North Ustyurt Basin, Kazakhstan and Uzbekistan\r\nthe western part of the basin. Oil pools are in shallow Jurassic and Neocomian sandstone reservoirs, in structural traps. Source rocks are absent in the total petroleum system area; therefore, the oil could have migrated from the adjacent North Caspian basin.\r\nThe North Ustyurt Jurassic Total Petroleum System encompasses\r\nthe rest of the basin area and includes Jurassic and younger rocks. Several oil and gas fields have been discovered in this total petroleum system. Oil accumulations are in Jurassic clastic reservoirs, in structural traps at depths of 2.5?3 km. Source rocks for the oil are lacustrine beds and coals in the continental\r\nJurassic sequence. Gas fields are in shallow Eocene sandstones in the northern part of the total petroleum system. The origin of the gas is unknown.\r\nThe North Ustyurt Paleozoic Total Petroleum System stratigraphically underlies the North Ustyurt Jurassic system and occupies the same geographic area. The total petroleum system is almost unexplored. Two commercial flows of gas and several oil and gas shows have been tested in Carboniferous shelf carbonates\r\nin the eastern part of the total petroleum system. Source rocks probably are adjacent Carboniferous deep-water facies interpreted from seismic data. The western extent of the total petroleum system is conjectural.\r\nAlmost all exploration drilling in the North Ustyurt basin has been limited to Jurassic and younger targets. The underlying Paleozoic-Triassic sequence is poorly known and completely unexplored. No wells have been drilled in offshore parts of the basin.\r\nEach of three total petroleum systems was assessed as a single assessment unit. Undiscovered resources of the basin are small to moderate. Most of the undiscovered oil probably will be discovered in Jurassic and Neocomian stratigraphic and structural\r\ntraps on the Buzachi arch, especially on its undrilled off-shore extension. Most of the gas discoveries are expected to be in Paleozoic carbonate reservoirs in the eastern part of the basin.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/b2201D","usgsCitation":"Ulmishek, G.F., 2001, Petroleum geology and resources of the North Ustyurt Basin, Kazakhstan and Uzbekistan (Version 1.0): U.S. Geological Survey Bulletin 2201, 14 p., https://doi.org/10.3133/b2201D.","productDescription":"14 p.","costCenters":[],"links":[{"id":161251,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":3238,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/bul/2201/D/index.html","linkFileType":{"id":5,"text":"html"}},{"id":462802,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/2201/D/b2201-d.pdf","text":"Report","size":"1.03 MB","linkFileType":{"id":1,"text":"pdf"}}],"edition":"Version 1.0","contact":"","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b15e4b07f02db6a4c95","contributors":{"authors":[{"text":"Ulmishek, Gregory F.","contributorId":48971,"corporation":false,"usgs":true,"family":"Ulmishek","given":"Gregory","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":209808,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":30846,"text":"wri894131 - 2001 - Hydrogeology and ground-water flow in the Memphis and Fort Pillow aquifers in the Memphis area, Tennessee","interactions":[],"lastModifiedDate":"2012-02-02T00:09:04","indexId":"wri894131","displayToPublicDate":"2001-09-01T00:00:00","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":"89-4131","title":"Hydrogeology and ground-water flow in the Memphis and Fort Pillow aquifers in the Memphis area, Tennessee","docAbstract":"On the basis of known hydrogeology of the Memphis and Fort Pillow aquifers in the Memphis area, a three-layer, finite-difference numerical model was constructed and calibrated as the primary tool to refine understanding of flow in the aquifers. The model was calibrated and tested for accuracy in simulating measured heads for nine periods of transient flow from 1886-1985. Testing and sensitivity analyses indicated that the model accurately simulated observed heads areally as well as through time.\r\n\r\nThe study indicates that the flow system is currently dominated by the distribution of pumping in relation to the distribution of areally variable confining units. Current withdrawal of about 200 million gallons per day has altered the prepumping flow paths, and effectively captured most of the water flowing through the aquifers. Ground-water flow is controlled by the altitude and location of sources of recharge and discharge, and by the hydraulic characteristics of the hydrogeologic units.\r\n\r\nLeakage between the Fort Pillow aquifer and Memphis aquifer, and between the Memphis aquifer and the water-table aquifers (alluvium and fluvial deposits) is a major component of the hydrologic budget. The study indicates that more than 50 percent of the water withdrawn from the Memphis aquifer in 1980 is derived from vertical leakage across confining units, and the leakage from the shallow aquifer (potential source of contamination) is not uniformly distributed. Simulated leakage was concentrated along the upper reaches of the Wolf and Loosahatchie Rivers, along the upper reaches of Nonconnah Creek, and the surficial aquifer of the Mississippi River alluvial plain. These simulations are supported by the geologic and geophysical evidence suggesting relatively thin or sandy confining units in these general locations. Because water from surficial aquifers is inferior in quality and more susceptible to contamination than water in the deeper aquifers, high rates of leakage to the Memphis aquifer may be cause for concern.\r\n\r\nA significant component of flow (12 percent) discharging from the Fort Pillow aquifer was calculated as upward leakage to the Memphis aquifer. This upward leakage was generally limited to areas near major pumping centers in the Memphis aquifer, where heads in the Memphis aquifer have been drawn significantly below heads in the Fort Pillow aquifer. Although the Fort Pillow aquifer is not capable of producing as much water as the Memphis aquifer for similar conditions, it is nonetheless a valuable resource throughout the area.","language":"ENGLISH","doi":"10.3133/wri894131","usgsCitation":"Brahana, J., and Broshears, R.E., 2001, Hydrogeology and ground-water flow in the Memphis and Fort Pillow aquifers in the Memphis area, Tennessee: U.S. Geological Survey Water-Resources Investigations Report 89-4131, 56 p., https://doi.org/10.3133/wri894131.","productDescription":"56 p.","costCenters":[],"links":[{"id":124933,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/wri_89_4131.jpg"},{"id":2728,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri89-4131","linkFileType":{"id":5,"text":"html"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4de4b07f02db6274b1","contributors":{"authors":[{"text":"Brahana, J. V.","contributorId":32926,"corporation":false,"usgs":true,"family":"Brahana","given":"J. V.","affiliations":[],"preferred":false,"id":204190,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Broshears, R. E.","contributorId":75552,"corporation":false,"usgs":true,"family":"Broshears","given":"R.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":204191,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":28584,"text":"wri004239 - 2001 - Hydrologic and water-quality characterization and modeling of the Chenoweth Run basin, Jefferson County, Kentucky","interactions":[],"lastModifiedDate":"2023-01-06T22:18:41.147137","indexId":"wri004239","displayToPublicDate":"2001-09-01T00:00:00","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":"2000-4239","title":"Hydrologic and water-quality characterization and modeling of the Chenoweth Run basin, Jefferson County, Kentucky","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri004239","usgsCitation":"Martin, G.R., Zarriello, P.J., and Shipp, A.A., 2001, Hydrologic and water-quality characterization and modeling of the Chenoweth Run basin, Jefferson County, Kentucky: U.S. Geological Survey Water-Resources Investigations Report 2000-4239, xi, 197 p., https://doi.org/10.3133/wri004239.","productDescription":"xi, 197 p.","costCenters":[{"id":354,"text":"Kentucky Water Science Center","active":true,"usgs":true},{"id":376,"text":"Massachusetts Water Science Center","active":true,"usgs":true},{"id":49157,"text":"Rocky Mountain Regional Office","active":true,"usgs":true}],"links":[{"id":119775,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/wri_2000_4239.jpg"},{"id":411530,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_34833.htm","linkFileType":{"id":5,"text":"html"}},{"id":264508,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2000/4239/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Kentucky","county":"Jefferson County","otherGeospatial":"Chenoweth Run basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -85.5,\n 38.242\n ],\n [\n -85.5,\n 38.125\n ],\n [\n -85.583,\n 38.125\n ],\n [\n -85.583,\n 38.242\n ],\n [\n -85.5,\n 38.242\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a29e4b07f02db61178c","contributors":{"authors":[{"text":"Martin, Gary R. 0000-0002-3274-5846 grmartin@usgs.gov","orcid":"https://orcid.org/0000-0002-3274-5846","contributorId":3413,"corporation":false,"usgs":true,"family":"Martin","given":"Gary","email":"grmartin@usgs.gov","middleInitial":"R.","affiliations":[{"id":354,"text":"Kentucky Water Science Center","active":true,"usgs":true}],"preferred":true,"id":200068,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Zarriello, Phillip J. 0000-0001-9598-9904 pzarriel@usgs.gov","orcid":"https://orcid.org/0000-0001-9598-9904","contributorId":1868,"corporation":false,"usgs":true,"family":"Zarriello","given":"Phillip","email":"pzarriel@usgs.gov","middleInitial":"J.","affiliations":[{"id":376,"text":"Massachusetts Water Science Center","active":true,"usgs":true}],"preferred":true,"id":200067,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Shipp, Allison A. 0000-0003-2927-8893 aashipp@usgs.gov","orcid":"https://orcid.org/0000-0003-2927-8893","contributorId":338,"corporation":false,"usgs":true,"family":"Shipp","given":"Allison","email":"aashipp@usgs.gov","middleInitial":"A.","affiliations":[{"id":49157,"text":"Rocky Mountain Regional Office","active":true,"usgs":true}],"preferred":true,"id":200066,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":28935,"text":"wri20004244 - 2001 - Analytical versus numerical estimates of water-level declines caused by pumping, and a case study of the Iao Aquifer, Maui, Hawaii","interactions":[],"lastModifiedDate":"2023-04-06T19:59:38.937721","indexId":"wri20004244","displayToPublicDate":"2001-09-01T00:00:00","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":"2000-4244","title":"Analytical versus numerical estimates of water-level declines caused by pumping, and a case study of the Iao Aquifer, Maui, Hawaii","docAbstract":"Comparisons were made between model-calculated water levels from a one-dimensional analytical model referred to as RAM (Robust Analytical Model) and those from numerical ground-water flow models using a sharp-interface model code. RAM incorporates the horizontal-flow assumption and the Ghyben-Herzberg relation to represent flow in a one-dimensional unconfined aquifer that contains a body of freshwater floating on denser saltwater. RAM does not account for the presence of a low-permeability coastal confining unit (caprock), which impedes the discharge of fresh ground water from the aquifer to the ocean, nor for the spatial distribution of ground-water withdrawals from wells, which is significant because water-level declines are greatest in the vicinity of withdrawal wells. Numerical ground-water flow models can readily account for discharge through a coastal confining unit and for the spatial distribution of ground-water withdrawals from wells.\r\n\r\nFor a given aquifer hydraulic-conductivity value, recharge rate, and withdrawal rate, model-calculated steady-state water-level declines from RAM can be significantly less than those from numerical ground-water flow models. The differences between model-calculated water-level declines from RAM and those from numerical models are partly dependent on the hydraulic properties of the aquifer system and the spatial distribution of ground-water withdrawals from wells. RAM invariably predicts the greatest water-level declines at the inland extent of the aquifer where the freshwater body is thickest and the potential for saltwater intrusion is lowest. For cases in which a low-permeability confining unit overlies the aquifer near the coast, however, water-level declines calculated from numerical models may exceed those from RAM even at the inland extent of the aquifer.\r\n\r\nSince 1990, RAM has been used by the State of Hawaii Commission on Water Resource Management for establishing sustainable-yield values for the State?s aquifers. Data from the Iao aquifer, which lies on the northeastern flank of the West Maui Volcano and which is confined near the coast by caprock, are now available to evaluate the predictive capability of RAM for this system. In 1995 and 1996, withdrawal from the Iao aquifer reached the 20 million gallon per day sustainable-yield value derived using RAM. However, even before 1996, water levels in the aquifer had declined significantly below those predicted by RAM, and continued to decline in 1997. To halt the decline of water levels and to preclude the intrusion of salt-water into the four major well fields in the aquifer, it was necessary to reduce withdrawal from the aquifer system below the sustainable-yield value derived using RAM. \r\n\r\nIn the Iao aquifer, the decline of measured water levels below those predicted by RAM is consistent with the results of the numerical model analysis. Relative to model-calculated water-level declines from numerical ground-water flow models, (1) RAM underestimates water-level declines in areas where a low-permeability confining unit exists, and (2) RAM underestimates water-level declines in the vicinity of withdrawal wells.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri20004244","usgsCitation":"Oki, D.S., and Meyer, W., 2001, Analytical versus numerical estimates of water-level declines caused by pumping, and a case study of the Iao Aquifer, Maui, Hawaii: U.S. Geological Survey Water-Resources Investigations Report 2000-4244, iv, 31 p., https://doi.org/10.3133/wri20004244.","productDescription":"iv, 31 p.","costCenters":[{"id":525,"text":"Pacific Islands Water Science Center","active":true,"usgs":true}],"links":[{"id":124608,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/wri_2000_4244.jpg"},{"id":415376,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_34827.htm","linkFileType":{"id":5,"text":"html"}},{"id":13744,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/wri/wri00-4244/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Hawaii","otherGeospatial":"Iao aquifer, Maui","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -156.598,\n 20.94\n ],\n [\n -156.598,\n 20.838\n ],\n [\n -156.465,\n 20.838\n ],\n [\n -156.465,\n 20.94\n ],\n [\n -156.598,\n 20.94\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4acce4b07f02db67e459","contributors":{"authors":[{"text":"Oki, Delwyn S. 0000-0002-6913-8804 dsoki@usgs.gov","orcid":"https://orcid.org/0000-0002-6913-8804","contributorId":1901,"corporation":false,"usgs":true,"family":"Oki","given":"Delwyn","email":"dsoki@usgs.gov","middleInitial":"S.","affiliations":[{"id":525,"text":"Pacific Islands Water Science Center","active":true,"usgs":true}],"preferred":true,"id":200644,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Meyer, William","contributorId":87538,"corporation":false,"usgs":true,"family":"Meyer","given":"William","affiliations":[],"preferred":false,"id":200645,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":30905,"text":"wri014040 - 2001 - Pond-aquifer interaction at South Pond of Lake Cochituate, Natick, Massachusetts","interactions":[],"lastModifiedDate":"2012-02-02T00:09:07","indexId":"wri014040","displayToPublicDate":"2001-09-01T00:00:00","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":"2001-4040","title":"Pond-aquifer interaction at South Pond of Lake Cochituate, Natick, Massachusetts","docAbstract":"A U.S. Army facility on a peninsula in South Pond of Lake Cochituate was designated a Superfund site by the U.S. Environmental Protection Agency in 1994 because contaminated ground water was detected at the facility, which is near the Natick Springvale public-supply wellfield. The interaction between South Pond and the underlying aquifer controls ground-water flow patterns near the pond and determines the source of water withdrawn from the wellfield.A map of the bathymetry and the thickness of fine-grained pond-bottom sediments was prepared on the basis of fathometer, ground-penetrating radar, and continuous seismic-reflection surveys. The geophysical data indicate that the bottom sediments are fine grained toward the middle of the pond but are coarse grained in shoreline areas. Natick Springvale wellfield, which consists of three active public-supply wells adjacent to South Pond, is 2,200 feet downgradient from the boundary of the Army facility. That part of South Pond between the Natick Springvale wellfield and the Army facility is 18 feet deep with at least 14 feet of fine-grained sediment beneath the pond-bottom. Water levels from the pond and underlying sediments indicate a downward vertical gradient and the potential for infiltration of pond water near the wellfield. Head differences between the pond and the wellfield ranged from 1.66 to 4.41 feet during this study. The velocity of downward flow from South Pond into the pond-bottom sediments, determined on the basis of temperature profiles measured over a diurnal cycle at two locations near the wellfield, was 0.5 and 1.0 feet per day. These downward velocities resulted in vertical hydraulic conductivities of 1.1 and 2.9 feet per day for the pond-bottom sediments.Naturally occurring stable isotopes of oxygen and hydrogen were used as tracers of pond water and ground water derived from recharge of precipitation, two potential sources of water to a well in a pond-aquifer setting. The isotopic composition of pond water varied seasonally and was distinctly different from the isotopic composition of ground water. The isotopic composition of shallow water beneath and adjacent to South Pond near the wellfield corresponds to the temporal variation of pond water, indicating that nearly all water at shallow depths was derived from pond water. A two-component mixing model based on the average stable isotope values of the source waters indicated that 64 ?15 percent at the 95-percent confidence interval of the water withdrawn at the public-supply wells was derived from the pond; pond water accounted for most of the uncertainty in the result. The rate of infiltration of pond water into the aquifer and discharging to the wellfield was 1.0 million gallons per day at the average pumping rate.","language":"ENGLISH","doi":"10.3133/wri014040","usgsCitation":"Friesz, P.J., and Church, P.E., 2001, Pond-aquifer interaction at South Pond of Lake Cochituate, Natick, Massachusetts: U.S. Geological Survey Water-Resources Investigations Report 2001-4040, 42 p., 1 over-size sheet. , https://doi.org/10.3133/wri014040.","productDescription":"42 p., 1 over-size sheet. ","costCenters":[],"links":[{"id":2840,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri014040","linkFileType":{"id":5,"text":"html"}},{"id":160730,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad7e4b07f02db68437a","contributors":{"authors":[{"text":"Friesz, Paul J. 0000-0002-4660-2336 pfriesz@usgs.gov","orcid":"https://orcid.org/0000-0002-4660-2336","contributorId":1075,"corporation":false,"usgs":true,"family":"Friesz","given":"Paul","email":"pfriesz@usgs.gov","middleInitial":"J.","affiliations":[{"id":466,"text":"New England Water Science Center","active":true,"usgs":true}],"preferred":true,"id":204327,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Church, Peter E.","contributorId":99178,"corporation":false,"usgs":true,"family":"Church","given":"Peter","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":204328,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":30902,"text":"wri014026 - 2001 - Historical trends and concentrations of fecal coliform bacteria in the Brandywine Creek basin, Chester County, Pennsylvania","interactions":[],"lastModifiedDate":"2018-02-26T15:57:29","indexId":"wri014026","displayToPublicDate":"2001-09-01T00:00:00","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":"2001-4026","title":"Historical trends and concentrations of fecal coliform bacteria in the Brandywine Creek basin, Chester County, Pennsylvania","docAbstract":"The Brandywine Creek in Chester County is used for recreation and as an important source of drinking water. For this study, 40 sites were established for collection of water samples for analysis of fecal coliform and Escherichia coli bacteria in 1998-99. Samples were collected during base-flow conditions and during five storms in which rainfall exceeded 0.5 inch. During base- flow conditions, the median concentrations of fecal coliform bacteria exceeded 200 col/100 mL at 26 of the 40 sites (65 percent). During stormflow conditions, the median concentration of fecal coliform bacteria exceeded the Pennsylvania Department of Environmental Protection (PaDEP) criterion of 200 col/100 mL at 30 of 33 sites sampled (91 percent). Trends in fecal coliform bacteria concentrations were downward for the period 1973-99 at three long-term water-quality monitor stations, the result of upgrades in wastewater treatment plants, decreases in point-source discharges, and a decrease in agricultural land. A positive relation exists between streamflow and concentrations of fecal coliform bacteria at two of the long-term stations, but concentrations are elevated in base flow and stormflow at all three stations.
Factors affecting bacteria concentrations in the Brandywine Creek Basin include nonpoint-source contaminants, reservoirs, seasonality, and stormflow. Nonpoint sources of bacterial contamination in the basin include, but are not limited to, land-surface runoff, urbanization, agricultural processes, groundwater contamination, and wildlife. Bacteria concentrations in streams that flow directly from the reservoirs are much lower than the concentrations in the streams flowing into the reservoirs. During March, April, May, October, and November, the Brandywine Creek tends to have lower water temperatures and bacteria concentrations than during June, July, August, and September. The 10-year median concentrations of bacteria at West Branch Brandywine Creek at Modena and East Branch Brandywine Creek below Downingtown exceed the criterion of 200 col/100 mL established by the PaDEP during the swimming season. The 10-year median concentrations of bacteria at Brandywine Creek at Chadds Ford exceed the criterion of 200 col/100 mL only during June. None of the stations exceed the criterion of 2,000 col/100 mL as established by the PaDEP for the remainder of the year.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri014026","collaboration":"Prepared in cooperation with the Chester Counter Water Resources Authority; Chester County Health Department","usgsCitation":"Town, D., 2001, Historical trends and concentrations of fecal coliform bacteria in the Brandywine Creek basin, Chester County, Pennsylvania: U.S. Geological Survey Water-Resources Investigations Report 2001-4026, vi, 46 p., https://doi.org/10.3133/wri014026.","productDescription":"vi, 46 p.","onlineOnly":"Y","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":125062,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/2001/4026/coverthb.jpg"},{"id":2838,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2001/4026/wri20014026.pdf","text":"Report","size":"1 MB","linkFileType":{"id":1,"text":"pdf"},"description":"WRI 2001-4026"}],"contact":"Director, Pennsylvania Water Science Center
U.S. Geological Survey
215 Limekiln Road
New Cumberland, PA 17070
The Hudson River is being considered for use as a supplemental source of water supply for New York City during droughts. One proposal entails withdrawal of Hudson River water from locations near Newburgh, Chelsea, or Kingston, but the extent to which this could cause the salt front to advance upstream to points where it could adversely affect community water supplies is unknown. The U.S. Geological Survey (USGS) one-dimensional Branch-Network Dynamic Flow model (BRANCH) was used in conjunction with the USGS one-dimensional Branched Lagrangian Solute-Transport Model (BLTM) to simulate the effect of five water-withdrawal scenarios on the salt-front location.
The modeled reach contains 132 miles of the lower Hudson River between the Federal Dam at Troy and Hastings-on-Hudson (near New York City). The BRANCH model was calibrated and verified to 19 tidal-cycle discharge measurements made at 11 locations by conventional and acoustic Doppler current-profiler methods. Maximum measured instantaneous tidal flow ranged from 20,000 ft3/s (cubic feet per second) at Albany to 368,000 ft3/s at Tellers Point; daily-mean flow at Green Island near Troy ranged from 3,030 ft3/s to 45,000 ft3/s during the flow measurements. Successive ebb- and flood-flow volumes were measured and compared with computed volumes; daily-mean bias was -1.6 percent (range from -21.0 to +23.7 percent; 13.5 percent mean absolute error). Daily-mean deviation between simulated and measured stage at eight locations (from Bowline Point to Albany) over the 19 tidal-cycle measurements averaged +0.06 ft (range from -0.31 to +0.40 ft; 0.21 ft root mean square error, RMSE). These results indicate that the model can accurately simulate flow in the Hudson River under a wide range of flow, tide, and meteorological conditions.
The BLTM was used to simulate chloride transport in the 61-mi reach from Turkey Point to Bowline Point under two seasonal conditions in 1990.one representing spring conditions of high inflow and low salinity (April-June), the other representing typical summer conditions of low inflow and high salinity (July-August). Measured chloride concentrations at Bowline Point were used to drive the BLTM simulations, and data collected at West Point were used for calibration. Mean bias in simulated chloride concentration for the April-June 1990 (high flow) data (observed range from 12 to 201 mg/L [milligrams per liter]; 30 mg/L RMSE) was .16 mg/L, and mean bias for the July-August 1990 (low flow) data (observed range from 31 to 2,000 mg/L; 535 mg/ L RMSE) was +126 mg/L. The salt front (saltwater/ freshwater interface) on the Hudson River was defined as the furthest upstream location where the chloride concentration exceeded 100 mg/L. Data from August 1991 were used to evaluate solute transport between West Point and Poughkeepsie because a chloride concentration of 100 mg/L was not observed at Clinton Point in 1990. The BLTM then was used to simulate chloride concentrations at Chelsea Pump Station and Clinton Point. Regression equations, based on daily mean values of specific conductance measured at West Point, were used to estimate daily mean chloride concentrations at Chelsea Pump Station and Clinton Point for model analysis. Mean biases in BLTM-simulated daily mean chloride concentrations for August 1991 were .38 mg/L at Chelsea Pump Station (range from 189 to 551 mg/L; 103 mg/L RMSE) and .9 mg/L at Clinton Point (range from 53 to 264 mg/L; 62 mg/L RMSE).
Hypothetical withdrawals at (1) Newburgh, (2) Chelsea, (3) Chelsea and Newburgh, (4) Chelsea and Kingston, and (5) Kingston and Newburgh, were simulated to compute the effects of withdrawals on salt-front movement. Withdrawals of 300 Mgal/d from any combination of Chelsea or Newburgh could result in upstream movement of the salt front of as much as 1.0 mi, given an initial salt-front location between West Point and Rogers Point. Scenarios that included withdrawals at Kingston caused the greatest upstream salt-front movement. Simulation of a 90-day April-June high-flow period during which discharges at Green Island averaged 25,200 ft3/s indicated that withdrawals of 1,939 Mgal/d (million gallons per day) at Chelsea Pump Station would not measureably increase chloride concentrations at Chelsea Pump Station under normal tidal and meteorological conditions, but withdrawals at twice that rate (3,878 Mgal/d) could increase the chloride concentration at Chelsea Pump Station to 250 mg/L.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri994024","collaboration":"Prepared in cooperation with the New York City Department of Environmental ProtectionDirector, New York Water Science Center
U.S. Geological Survey
425 Jordan Rd
Troy, NY 12180
(518) 285-5695
http://ny.water.usgs.gov/
Suspended sediment has long been recognized as an important contaminant affecting water resources. Besides its direct role in determining water clarity, bridge scour and reservoir storage, sediment serves as a vehicle for the transport of many binding contaminants, including nutrients, trace metals, semi-volatile organic compounds, a nd numerous pesticides (U.S. Environmental Protection Agency, 2000a). Recent efforts to addr ess water-quality concerns through the Total Maximum Daily Load (TMDL) process have iden tified sediment as the single most prevalent cause of impairment in the Nation’s streams a nd rivers (U.S. Environmental Protection Agency, 2000b). Moreover, sediment has been identified as a medium for the tran sport and sequestration of organic carbon, playing a potentia lly important role in understa nding sources and sinks in the global carbon budget (Stallard, 1998).
A comprehensive understanding of sediment fate a nd transport is considered essential to the design and implementation of effective plans for sediment management (Osterkamp and others, 1998, U.S. General Accounting Office, 1990). An exte nsive literature addr essing the problem of quantifying sediment transport has produced a nu mber of methods for estimating its flux (see Cohn, 1995, and Robertson and Roerish, 1999, for us eful surveys). The accuracy of these methods is compromised by uncertainty in the concentration measurements and by the highly episodic nature of sediment movement, particul arly when the methods are applied to smaller basins. However, for annual or decadal flux es timates, the methods are generally reliable if calibrated with extended periods of data (Robertson and Roerish, 1999). A substantial literature also supports the Universal Soil Loss Equation (U SLE) (Soil Conservation Service, 1983), an engineering method for estimating sheet and rill erosion, although the empirical credentials of the USLE have recently been questioned (Tri mble and Crosson, 2000). Conversely, relatively little direct evidence is available concerning the fate of sediment. The common practice of quantifying sediment fate with a sediment deliv ery ratio, estimated from a simple empirical relation with upstream basin area, does not artic ulate the relative importance of individual storage sites within a basin (Wolman, 1977). Rates of sediment deposition in reservoirs and flood plains can be determined from empirical measurement s , but only a limited number of sites have been monitored, and net rates of deposition or loss from other potential sinks and sources is largely unknown (Stallard, 1998). In particular, little is known about how much sediment loss from fields ultimately makes its way to stream channels, and how much sediment is subsequently stored in or lost from th e streambed (Meade and Parker, 1985, Trimble and Crosson, 2000).
This paper reports on recent progress made to a ddress empirically the question of sediment fate and transport on a national scale. The model pres ented here is based on the SPAtially Referenced Regression On Watershed attr ibutes (SPARROW) methodology, fi rst used to estimate the distribution of nutrients in str eams and rivers of the United Stat es, and subsequently shown to describe land and stream processes affecting the delivery of nutrients (Smith and others, 1997, Alexander and others, 2000, Preston and Brakeb ill, 1999). The model makes use of numerous spatial datasets, available at the national level, to explain long-term sediment water-quality conditions in major streams and rivers throughou t the United States. Sediment sources are identified using sediment erosion rates from the National Resources I nventory (NRI) (Natural Resources Conservation Service, 2000) and apportioned over the landscape according to 30- meter resolution land-use information from th e National Land Cover Data set (NLCD) (U.S. Geological Survey, 2000a). More than 76,000 reservoirs from the National Inventory of Dams (NID) (U.S. Army Corps of Engin eers, 1996) are identified as pot ential sediment sinks. Other, non-anthropogenic sources and sinks are identified using soil in formation from the State Soil Survey Geographic (STATSGO) data base (Schwarz and Alexander, 1995) and spatial coverages representing surficial rock t ype and vegetative cover. The SPA RROW model empirically relates these diverse spatial datasets to estimates of long-term, mean annual sediment flux computed from concentration and flow measurements co llected over the period 1985 -95 from more than 400 monitoring stations maintained by the Na tional Stream Quality Accounting Network (Alexander and others, 1998), the National Wa ter Quality Assessment Program, and U.S. Geological Survey District offices (Turcios and Gray, in press). Th e calibrated model is used to estimate sediment flux for over 60,000 stream segments included in the River Reach File 1 (RF1) stream network (Alexander and others, 1999).
SPARROW uses statis tical methods to calibrate a simple, structural model of riverine water quality, one that imposes mass ba lance in accounting for changes in contaminant flux. As applied here, the mass-balance approach facilitates the interpretation of model results in terms of physical processes affecting sediment transport, and makes possible the estimation of various rates of sediment generation and loss associated with stream channels and features of the landscape. The statistical approach provides a basi s for assessing the error of these inferred rates and of the error in extrapolated estimates of sediment flux made for streams in the RF1 network. An important implication of the holistic modeling approach adopted in this analysis is that estimates of sediment production and loss ar e based on, and therefore consistent with, measurements of in-stream flux. Other ancillary information, such as direct measurements of long-term sediment storage and release from rese rvoirs (Steffen, 1996), is incorporated into the analysis by specifying additional equations expl aining these ancillary variables. The imposition of cross-equation constraints affords this info rmation a statistically consistent weight in explaining in-stream sediment flux. Thus, the me thodology described here represents a general framework for synthesizing a wide spectrum of available information relevant to the understanding of sediment fate and transport.
","largerWorkType":{"id":4,"text":"Book"},"largerWorkTitle":"Proceedings of the Seventh Federal Interagency Sedimentation Conference, March 25 to 29, 2001, Reno, Nevada","largerWorkSubtype":{"id":12,"text":"Conference publication"},"conferenceTitle":"7th Federal Interagency Sedimentation Conference","conferenceDate":"Mar 25-29, 2001","conferenceLocation":"Reno, NV","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","usgsCitation":"Schwarz, G., Smith, R.A., Alexander, R.B., and Gray, J.R., 2001, A spatially referenced regression model (SPARROW) for suspended sediment in streams of the Conterminous U.S., in Proceedings of the Seventh Federal Interagency Sedimentation Conference, March 25 to 29, 2001, Reno, Nevada, v. II, Reno, NV, Mar 25-29, 2001, p. 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]\n}","volume":"II","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53ef1ec1e4b0bfa1f993eece","contributors":{"authors":[{"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":451,"text":"National Water Quality Assessment Program","active":true,"usgs":true},{"id":5067,"text":"Northeast Regional Director's Office","active":true,"usgs":true}],"preferred":false,"id":498327,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Smith, Richard A. 0000-0003-2117-2269 rsmith1@usgs.gov","orcid":"https://orcid.org/0000-0003-2117-2269","contributorId":580,"corporation":false,"usgs":true,"family":"Smith","given":"Richard","email":"rsmith1@usgs.gov","middleInitial":"A.","affiliations":[{"id":37778,"text":"WMA - Integrated Modeling and Prediction Division","active":true,"usgs":true},{"id":503,"text":"Office of Water Quality","active":true,"usgs":true},{"id":451,"text":"National Water Quality Assessment Program","active":true,"usgs":true}],"preferred":true,"id":498328,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Alexander, Richard B. 0000-0001-9166-0626 ralex@usgs.gov","orcid":"https://orcid.org/0000-0001-9166-0626","contributorId":541,"corporation":false,"usgs":true,"family":"Alexander","given":"Richard","email":"ralex@usgs.gov","middleInitial":"B.","affiliations":[{"id":503,"text":"Office of Water Quality","active":true,"usgs":true},{"id":451,"text":"National Water Quality Assessment Program","active":true,"usgs":true}],"preferred":true,"id":498326,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Gray, John R. 0000-0002-8817-3701 jrgray@usgs.gov","orcid":"https://orcid.org/0000-0002-8817-3701","contributorId":1158,"corporation":false,"usgs":true,"family":"Gray","given":"John","email":"jrgray@usgs.gov","middleInitial":"R.","affiliations":[{"id":5058,"text":"Office of the Chief Scientist for Water","active":true,"usgs":true}],"preferred":true,"id":498329,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":58061,"text":"wri014138 - 2001 - Mountain Island Lake, North Carolina: Analysis of ambient conditions and simulation of hydrodynamics, constituent transport, and water-quality characteristics, 1996–97","interactions":[],"lastModifiedDate":"2024-06-27T21:43:47.104333","indexId":"wri014138","displayToPublicDate":"2001-08-01T00:00:00","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":"2001-4138","title":"Mountain Island Lake, North Carolina: Analysis of ambient conditions and simulation of hydrodynamics, constituent transport, and water-quality characteristics, 1996–97","docAbstract":"Mountain Island Lake is an impoundment of the Catawba River in North Carolina and supplies drinking water to more than 600,000 people in Charlotte, Gastonia, Mount Holly, and several other communities. The U.S. Geological Survey, in cooperation with the Charlotte-Mecklenburg Utilities, conducted an investigation of the reservoir to characterize hydrologic and water-quality conditions and to develop and apply a simulation model to predict the response of the reservoir to changes in constituent loadings or the flow regime.
During 1996–97, flows into Mountain Island Lake were dominated by releases from Cowans Ford Dam on Lake Norman, with more than 85 percent of the total inflow to the reservoir coming from Lake Norman. Riverbend Steam Station discharges accounted for about 12 percent of the inflows to the reservoir, and inflows from tributary streams contributed less than 1.5 percent of the total inflows. Releases through Mountain Island Dam accounted for about 81 percent of outflows from the reservoir, while Riverbend Steam Station withdrawals, which were equal to discharge from the facility, constituted about 13 percent of the reservoir withdrawals. About 5.5 percent of the withdrawals from the reservoir were for water supply.
Strong thermal stratification was seldom observed in Mountain Island Lake during April 1996-September 1997. As a result, dissolved-oxygen concentrations were only infrequently less than 4 milligrams per liter, and seldom less than 5 milligrams per liter throughout the entire reservoir, including the coves. The Riverbend Steam Station thermal discharge had a pronounced effect on surface-water temperatures near the outfall.
McDowell Creek, which drains to McDowell Creek cove, receives treated wastewater from a large municipal facility and has exhibited signs of poor water-quality conditions in the past. During April 1996-September 1997, concentrations of nitrate, ammonia, total phosphorus, and chlorophyll a were higher in McDowell Creek cove than elsewhere throughout the reservoir. Nevertheless, the highest chlorophyll a concentration measured during the study was 13 micrograms per liter—well below the North Carolina ambient water-quality standard of 40 micrograms per liter. In the mainstem of the reservoir, near-bottom ammonia concentrations occasionally were greater than near-surface concentrations. However, the relatively large top-to-bottom differences in ammonia and phosphorus that have been observed in other Catawba River reservoirs were not present in Mountain Island Lake.
External loadings of suspended solids, nitrogen, phosphorus, and biochemical oxygen demand were determined for May 1996-April 1997. Flows through Cowans Ford Dam contributed more than 80 percent of the biochemical oxygen demand and nitrogen load to the reservoir, with McDowell Creek contributing about 15 percent of the biochemical oxygen demand load. In contrast, McDowell Creek contributed about half of the phosphorus load to the reservoir, while inflows through Cowans Ford Dam contributed about one-fourth of the phosphorus load, and the McDowell Creek wastewater-treatment plant contributed about 15 percent of the total phosphorus load. The remainder of the phosphorus loadings came from Gar Creek and the discharge from the Riverbend ash settling pond.
Mountain Island Lake is a relatively small (11.3-square-kilometer surface area) impoundment. An area of 181 square kilometers drains directly to the reservoir, but much of this area is undergoing development. In addition, the reservoir receives treated effluent from a municipal wastewater-treatment facility.
The two-dimensional, laterally averaged model CE-QUAL-W2 was applied to Mountain Island Lake. The model was configured to simulate water level, water temperature, and 12 water-quality constituents. The model included the mainstem, four coves, three point-source discharges, and three withdrawals.
Simulated water levels generally were within 10 centimeters of measured values, indicating a good calibration of the water balance for the reservoir. The root-mean-square difference between measured and simulated water temperatures was about 1 to 1.5 degrees Celsius, and vertical distributions of water temperature were accurately simulated in both the mainstem and coves.
Seasonal and spatial patterns of nitrate, ammonia, orthophosphorus, and chlorophyll a were reasonably reproduced by the water-quality model. Because of the absence of the denitrification process in the model formulation, nitrate concentrations typically were overpredicted. Simulated and measured ammonia concentrations seldom differed by more than 0.01 milligram per liter, and simulations of seasonal fluctuations in chlorophyll a were representative of measured conditions. The root mean square of the difference between measured and simulated dissolved-oxygen concentrations was about 1 milligram per liter.
The calibrated water-quality model was applied to evaluate (1) the movement of a conservative, neutrally buoyant material, or tracer, through the reservoir for several sets of conditions; (2) the effects of the Riverbend thermal discharge on water temperature in the reservoir; (3) the effects of changes in water-supply withdrawal rates on water-quality conditions; and (4) changes in reservoir water quality in response to changes in point- and nonpoint-source loadings. In general, dissolved material entering Mountain Island Lake from both Cowans Ford Dam and McDowell Creek during the summer moves along the bottom of the lake toward Mountain Island Dam, with little mixing of dissolved material into the surface layers. Simulations suggest that dissolved material can move upstream in the reservoir when flows from Cowans Ford Dam are near zero. Dissolved material can remain in Mountain Island Lake for a period far in excess of the theoretical retention time of 12 days.
Simulations indicated that the Riverbend thermal discharge increases water temperature in the surface layers of the downstream part of the reservoir by as much as 5 degrees Celsius. However, the discharge has little effect on near-bottom water temperature.
Based on model simulations, a proposed doubling of the water-supply withdrawals from Mountain Island Lake has no readily apparent effect on water quality in the reservoir. The increased withdrawal rate may have some localized effects on circulation in the reservoir, but a more detailed model of the intake zone would be required to identify those effects.
The effects of a 20-percent increase in water-chemistry loadings through Cowans Ford Dam and from McDowell Creek were simulated separately. Increased loadings from Cowans Ford Dam had about the same effect on water-quality conditions near Mountain Island Dam as did increased loadings from McDowell Creek. Maintaining good water quality in Mountain Island Lake depends on maintaining good water quality in Lake Norman as well as in the inflows from the McDowell Creek watershed.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri014138","collaboration":"Prepared in cooperation with the Charlotte-Mecklenburg Utilities","usgsCitation":"Bales, J.D., Sarver, K.M., and Giorgino, M.J., 2001, Mountain Island Lake, North Carolina: Analysis of ambient conditions and simulation of hydrodynamics, constituent transport, and water-quality characteristics, 1996–97: U.S. Geological Survey Water-Resources Investigations Report 2001-4138, viii, 85 p., https://doi.org/10.3133/wri014138.","productDescription":"viii, 85 p.","costCenters":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true}],"links":[{"id":430579,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_42928.htm","linkFileType":{"id":5,"text":"html"}},{"id":184151,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/2001/4138/coverthb.jpg"},{"id":5988,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2001/4138/wri20014138.pdf","text":"Report","linkFileType":{"id":1,"text":"pdf"},"description":"WRI 2001-4138"}],"country":"United States","state":"North Carolina","otherGeospatial":"Catawba River, Mountain Island Lake","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -80.8319091796875,\n 34.164090803573124\n ],\n [\n -80.5517578125,\n 34.23451236236987\n ],\n [\n -80.45013427734375,\n 34.277644878733824\n ],\n [\n -80.43365478515625,\n 34.397844946449865\n ],\n [\n -80.5078125,\n 34.655803905058974\n ],\n [\n -80.58746337890625,\n 34.836349990763864\n ],\n [\n -80.67535400390625,\n 35.05248370662468\n ],\n [\n -80.738525390625,\n 35.69745580725804\n ],\n [\n -80.74127197265625,\n 35.72421761691415\n ],\n [\n -80.96649169921875,\n 35.909073928771534\n ],\n [\n -81.5625,\n 35.875698032496665\n ],\n [\n -81.85638427734375,\n 35.88014896488361\n ],\n [\n -82.02667236328125,\n 35.79108281624994\n ],\n [\n -82.09259033203125,\n 35.68853320738875\n ],\n [\n -82.01019287109375,\n 35.60818490437746\n ],\n [\n -81.80419921875,\n 35.634976650677295\n ],\n [\n -81.73278808593749,\n 35.628279555648845\n ],\n [\n -81.70257568359375,\n 35.567980458012094\n ],\n [\n -81.55975341796875,\n 35.58138418324621\n ],\n [\n -81.5020751953125,\n 35.564629176277855\n ],\n [\n -81.50482177734375,\n 35.496456056584165\n ],\n [\n -81.49932861328125,\n 35.07271701786369\n ],\n [\n -81.42379760742188,\n 34.95349314197422\n ],\n [\n -81.331787109375,\n 34.92197103616377\n ],\n [\n -81.1669921875,\n 34.807038111521614\n ],\n [\n -81.03790283203125,\n 34.52918706954935\n ],\n [\n -80.98846435546875,\n 34.3774457585774\n ],\n [\n -80.8319091796875,\n 34.164090803573124\n ]\n ]\n ]\n }\n }\n ]\n}","contact":"Director, South Atlantic Water Science Center
U.S. Geological Survey
720 Gracern Road
Columbia, SC 29210
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":31233,"text":"ofr0173 - 2001 - Summary of trends and status analysis for flow, nutrients, and sediments at selected nontidal sites, Chesapeake Bay basin, 1985-99","interactions":[],"lastModifiedDate":"2018-02-09T09:13:28","indexId":"ofr0173","displayToPublicDate":"2001-08-01T00:00:00","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":"2001-73","title":"Summary of trends and status analysis for flow, nutrients, and sediments at selected nontidal sites, Chesapeake Bay basin, 1985-99","docAbstract":"Water-quality and flow data from 31 sites in nontidal portions of the Chesapeake Bay Basin were analyzed to document annual nutrient and sediment loads and trends for the period 1985 through 1999 as part of an annual reevaluation and reporting for the Chesapeake Bay Program. Annual loads were estimated by use of the U.S. Geological Survey ESTIMATOR model. Trends were estimated using linear regression. Trends were reported for monthly mean flow, monthly load, flow-adjusted concentration, and flow-weighted concentration. Median yields and concentrations were calculated to help facilitate comparisons between basins. The drought of 1999 had pronounced effects on trend results. The trend in flow increased at 4 of the 31 sites, 8 fewer sites than in 1998. Ten less significant trends were estimated for nutrient and sediment loads compared to 1985-98. Trends in flow-weighted and flow-adjusted concentrations varied little by nutrient species and geographic location. Trends were generally downward or not significant for both the nitrogen and phosphorus species throughout the Chesapeake Bay Basin. Trends in flow-adjusted concentration indicated downward trends at most sites for nutrients and about half the sites for sediments, an indication that management actions are reducing nutrient and sediment concentrations.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr0173","usgsCitation":"Langland, M., Edwards, R.E., Sprague, L., and Yochum, S., 2001, Summary of trends and status analysis for flow, nutrients, and sediments at selected nontidal sites, Chesapeake Bay basin, 1985-99: U.S. Geological Survey Open-File Report 2001-73, 49 p., https://doi.org/10.3133/ofr0173.","productDescription":"49 p.","onlineOnly":"Y","additionalOnlineFiles":"N","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":160559,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/2001/0073/coverthb.jpg"},{"id":2802,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2001/0073/ofr20010073.pdf","text":"Report","size":"1.81 MB","linkFileType":{"id":1,"text":"pdf"},"description":"OFR 2001-0073"}],"contact":"Director, Pennsylvania Water Science Center
U.S. Geological Survey
215 Limekiln Road
New Cumberland, PA 17070
What is the Advanced National Seismic System? The Advanced National Seismic System (ANSS) is designed to organize, modernize, and standardize operations of seismic networks in the United States to improve the Nation’s ability to respond effectively to damaging earthquakes, volcanoes, and tsunamis. To achieve this, the ANSS will link more than 7,000 national, regional and urban monitoring stations in real time
","language":"English","doi":"10.3133/fs04501","usgsCitation":"Benz, H., Shedlock, K.M., and Buland, R., 2001, The Advanced National Seismic System; management and implementation: U.S. Geological Survey Fact Sheet 045-01, 2 p., https://doi.org/10.3133/fs04501.","productDescription":"2 p.","costCenters":[],"links":[{"id":121414,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/fs/2001/0045/report-thumb.jpg"},{"id":2572,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/fs/fs-0045-01/","linkFileType":{"id":5,"text":"html"}},{"id":59474,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/fs/2001/0045/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad5e4b07f02db683559","contributors":{"authors":[{"text":"Benz, H.M.","contributorId":21594,"corporation":false,"usgs":true,"family":"Benz","given":"H.M.","email":"","affiliations":[],"preferred":false,"id":203825,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Shedlock, K. M.","contributorId":72805,"corporation":false,"usgs":true,"family":"Shedlock","given":"K.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":203826,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Buland, R.P.","contributorId":85233,"corporation":false,"usgs":true,"family":"Buland","given":"R.P.","email":"","affiliations":[],"preferred":false,"id":203827,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":38271,"text":"pp1629 - 2001 - Estimation of hydraulic parameters from an unconfined aquifer test conducted in a glacial outwash deposit, Cape Cod, Massachusetts","interactions":[],"lastModifiedDate":"2020-02-23T17:08:16","indexId":"pp1629","displayToPublicDate":"2001-08-01T00:00:00","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":"1629","title":"Estimation of hydraulic parameters from an unconfined aquifer test conducted in a glacial outwash deposit, Cape Cod, Massachusetts","docAbstract":"An aquifer test conducted in a sand and gravel, glacial outwash deposit on Cape Cod, Massachusetts was analyzed by means of a model for flow to a partially penetrating well in a homogeneous, anisotropic unconfined aquifer. The model is designed to account for all significant mechanisms expected to influence drawdown in observation piezometers and in the pumped well. In addition to the usual fluid-flow and storage processes, additional processes include effects of storage in the pumped well, storage in observation piezometers, effects of skin at the pumped-well screen, and effects of drainage from the zone above the water table.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/pp1629","usgsCitation":"Moench, A.F., Garabedian, S.P., and LeBlanc, D.R., 2001, Estimation of hydraulic parameters from an unconfined aquifer test conducted in a glacial outwash deposit, Cape Cod, Massachusetts: U.S. Geological Survey Professional Paper 1629, 69 p., https://doi.org/10.3133/pp1629.","productDescription":"69 p.","costCenters":[{"id":589,"text":"Toxic Substances Hydrology Program","active":true,"usgs":true}],"links":[{"id":122522,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/pp_1629.jpg"},{"id":3500,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pp/pp1629/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Massachusetts ","otherGeospatial":"Cape Cod","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -70.68603515625,\n 41.566141964768384\n ],\n [\n -69.873046875,\n 41.566141964768384\n ],\n [\n -69.873046875,\n 42.09007006868398\n ],\n [\n -70.68603515625,\n 42.09007006868398\n ],\n [\n -70.68603515625,\n 41.566141964768384\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0ae4b07f02db5fb2b6","contributors":{"authors":[{"text":"Moench, Allen F. afmoench@usgs.gov","contributorId":3903,"corporation":false,"usgs":true,"family":"Moench","given":"Allen","email":"afmoench@usgs.gov","middleInitial":"F.","affiliations":[],"preferred":true,"id":219477,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Garabedian, Stephen P.","contributorId":91090,"corporation":false,"usgs":true,"family":"Garabedian","given":"Stephen","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":219478,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"LeBlanc, Denis R. 0000-0002-4646-2628 dleblanc@usgs.gov","orcid":"https://orcid.org/0000-0002-4646-2628","contributorId":1696,"corporation":false,"usgs":true,"family":"LeBlanc","given":"Denis","email":"dleblanc@usgs.gov","middleInitial":"R.","affiliations":[{"id":466,"text":"New England Water Science Center","active":true,"usgs":true}],"preferred":true,"id":219476,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":30904,"text":"wri014035 - 2001 - Hydrogeology, model description, and flow analysis of the Mississippi River alluvial aquifer in northwestern Mississippi","interactions":[],"lastModifiedDate":"2018-03-29T08:27:01","indexId":"wri014035","displayToPublicDate":"2001-08-01T00:00:00","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":"2001-4035","title":"Hydrogeology, model description, and flow analysis of the Mississippi River alluvial aquifer in northwestern Mississippi","docAbstract":"The Mississippi River alluvial aquifer underlies a 7,000-square-mile area of the Mississippi River alluvial plain in northwestern Mississippi, an area locally known as the Delta. The alluvial aquifer is the most heavily pumped aquifer in Mississippi, and wells yielding more than 2,000 gallons per minute are common. About 98 percent of the pumpage from the alluvial aquifer is for agriculture. The sand and gravel that form the alluvial aquifer averages about 110 feet in thickness. The aquifer is confined over most of the Delta, and the upper confining unit averages about 25 feet in thickness. The average depth to water in the alluvial aquifer during fall 1999 was about 25 feet. The alluvial aquifer receives lateral recharge at the western boundary from the Mississippi River and at the eastern boundary from aquifers that directly underlie the Bluff Hills. The alluvial aquifer receives water vertically from precipitation, internal streams and lakes, and locally from the Cockfield and Sparta aquifers where they directly underlie the alluvial aquifer. The alluvial aquifer also discharges water to the underlying aquifers, and during extended periods with no surface runoff, to the Mississippi River and to the internal streams and lakes. The magnitude of recharge from the Mississippi River, precipitation, and internal lakes and streams can vary greatly depending upon hydrologic and climatic conditions. The U.S. Geological Survey modular threedimensional finite-difference ground-water flow model, MODFLOW, was used to simulate the Mississippi River alluvial aquifer flow system in northwestern Mississippi. The model uses one layer with a rectangular-grid and 1-mile square cells to represent the alluvial aquifer. The model was calibrated and verified by using spring and fall water-level measurements from January 1988 through December 1996. The values of selected model calibration-derived parameters for the alluvial aquifer are hydraulic conductivity, 425 feet per day; specific yield, 0.32; and storage coefficient, 0.016. The model showed that the aquifer lost water from storage at an average rate of 404 cubic feet per second during the 9-year simulation period. During this period, the average pumpage rate was 1,270 million gallons per day (1,980 cubic feet per second). Simulated areal recharge from precipitation averaged 2.6 inches per year (1,360 cubic feet per second). Vertical recharge from the internal streams and lakes and lateral recharge from aquifers underlying the Bluff Hills averaged 113 and 108 cubic feet per second, respectively. Model results indicated that net recharge from the Mississippi River and from aquifers directly underlying the alluvial aquifer was small. ","language":"English","doi":"10.3133/wri014035","usgsCitation":"Arthur, J.K., 2001, Hydrogeology, model description, and flow analysis of the Mississippi River alluvial aquifer in northwestern Mississippi: U.S. Geological Survey Water-Resources Investigations Report 2001-4035, 47 p., https://doi.org/10.3133/wri014035.","productDescription":"47 p.","costCenters":[],"links":[{"id":160835,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":352893,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://permanent.access.gpo.gov/LPS104393/LPS104393/ms.water.usgs.gov/ms_proj/reports/WRIR_01-4035.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":2839,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://ms.water.usgs.gov/ms_proj/reports/WRIR_01-4035.pdf ","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Mississippi","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -90.263671875,\n 35.06597313798418\n ],\n [\n -90.7470703125,\n 34.903952965590065\n ],\n [\n -91.25244140624999,\n 33.99802726234877\n ],\n [\n -91.40625,\n 33.00866349457558\n ],\n [\n -91.16455078125,\n 32.24997445586331\n ],\n [\n -90.81298828125,\n 32.30570601389429\n ],\n [\n -90.966796875,\n 33.43144133557529\n ],\n [\n -90.90087890624999,\n 33.90689555128866\n ],\n [\n -90.59326171875,\n 34.27083595165\n ],\n [\n -90.263671875,\n 35.06597313798418\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e479fe4b07f02db492f52","contributors":{"authors":[{"text":"Arthur, J. K.","contributorId":56223,"corporation":false,"usgs":true,"family":"Arthur","given":"J.","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":204326,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":22947,"text":"ofr00415 - 2001 - A Microsoft Windows version of the MARK3 Monte Carlo resource simulator","interactions":[],"lastModifiedDate":"2025-12-10T18:34:41.903203","indexId":"ofr00415","displayToPublicDate":"2001-08-01T00:00:00","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":"2000-415","title":"A Microsoft Windows version of the MARK3 Monte Carlo resource simulator","docAbstract":"This publication includes a version of the MARK3 Monte Carlo resource simulator that will run under Microsoft Windows 98, NT, and 2000. The disc also includes grade and tonnage information and related deposit model files that allow the user to calculate probability curves for mineral resources. A total of 113 deposit models are included on the disc although some of them are subsets of others. In most cases the list of deposits with associated grade and tonnage data are also present. Ten of the models contain proprietary information and the grade and tonnage for those are not included. The program also includes an extensive help file that provides information about the program and about the concepts that are the basis of the program and about this method for estimating quantitative mineral resources.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr00415","issn":"0094-9140","isbn":"0607965185","usgsCitation":"Duval, J.S., 2001, A Microsoft Windows version of the MARK3 Monte Carlo resource simulator: U.S. Geological Survey Open-File Report 2000-415, 1 CD-ROM, https://doi.org/10.3133/ofr00415.","productDescription":"1 CD-ROM","costCenters":[],"links":[{"id":1396,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2000/of00-415/index.htm","linkFileType":{"id":5,"text":"html"}},{"id":154202,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53cd495be4b0b290850ef181","contributors":{"authors":[{"text":"Duval, Joseph S.","contributorId":22314,"corporation":false,"usgs":true,"family":"Duval","given":"Joseph","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":189175,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ]}