The Vigil Network consists of places where observations are made through time to record changes in landscape features over a long period. Resurveys will usually be made once each year or every few years and the period of observation, hopefully, will extend through and beyond the International Hydrological Decade.
Vigil Network sites will usually be chosen to represent some typical feature of a given landscape. In the example shown here, the feature is a small ephemeral channel in a basin of moderate relief underlain by silty sandstone typical of the surrounding area. Vigil sites are not protected from man's influence and indeed may be selected because of the possible or portending cultural influences. In this respect they differ from the Bench Mark Network whose purpose is to make precise observations of hydrologic factors in areas uninfluenced by and protected from man's use.
The factors which might be observed are many and varied. A few might be mentioned here, others are explained at length elsewhere (Miller and Leopold, 1963; Leopold, 1962). Streamchannel position, form, depth, and profile; vegetation in form of transects or quadrats; soil movement on slopes; rock movement on slopes or in channels. These and many more would yield valuable information on changes with time.
To assure permanence of initial field observations, including reference points, bench marks, and cross sections, brief descriptions, maps, and initial data should be filed identically in designated repositories where the data will be made available for inspection by any interested scientist. It is recommended that the designation of two such locations where records of the type here attached will be filed be taken up by the Coordinating Council of the International Hydrological Decade. In designating such repositories it should be recognized that there is no need for elaborate indexing. The main requirement is merely the maintenance of a simple file where the data are stored and can be inspected or copied by any scientist. There need be no special provision for lending or reproduction services.
The present document is an example showing what data, maps, and descriptions should be included in those permanent files at the two repositories. The material in these repositories should be sufficient to permit someone in the indefinite future to find and remeasure the same features described now. Thus the scientific value of the original surveys increases with time, - provided that the descriptions are sufficient to allow a person to find with assurance the original feature in the field.
It must be visualized that a permanent repository must economize in space. Thus, as the example here shows, the filed material is not all of the original field notes but a summary, brief but descriptive.
","language":"English","publisher":"Taylor & Francis","doi":"10.1080/02626666509493401","usgsCitation":"Leopold, L.B., and Emmett, W.W., 1965, Vigil Network sites: A sample of data for permanent filing: International Association of Scientific Hydrology - Bulletin , v. 10, no. 3, p. 12-21, https://doi.org/10.1080/02626666509493401.","productDescription":"10 p.","startPage":"12","endPage":"21","costCenters":[],"links":[{"id":480681,"rank":0,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.1080/02626666509493401","text":"Publisher Index Page"},{"id":338379,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"10","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"58da253fe4b0543bf7fda87d","contributors":{"authors":[{"text":"Leopold, Luna Bergere","contributorId":93884,"corporation":false,"usgs":true,"family":"Leopold","given":"Luna","email":"","middleInitial":"Bergere","affiliations":[],"preferred":false,"id":686308,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Emmett, William W.","contributorId":68715,"corporation":false,"usgs":true,"family":"Emmett","given":"William","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":686309,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70009989,"text":"70009989 - 1965 - Alkali content of alpine ultramafic rocks","interactions":[],"lastModifiedDate":"2020-11-24T00:39:56.572868","indexId":"70009989","displayToPublicDate":"1965-01-01T00:00:00","publicationYear":"1965","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1759,"text":"Geochimica et Cosmochimica Acta","active":true,"publicationSubtype":{"id":10}},"title":"Alkali content of alpine ultramafic rocks","docAbstract":"The lower limit of abundance of sodium and potassium in ultramafic rocks is less than the threshold amount detectable by conventional analytical methods. By a dilutionaddition modification of the flame-spectrophotometric method, sodium and potassium have been determined in 40 specimens of alpine ultramafic rocks. Samples represent six regions in the United States and one in Australia, and include dunite, peridotite, pyroxenite, and their variably serpentinized and metamorphosed derivatives.
The median value found for Na2O is 0.004 per cent, and the range of Na2O is 0.001–0.19. The median value for K2O is 0.0034 per cent and the range is 0.001–0.031 per cent. Alkali concentrations are below 0.01 per cent Na2O in 28 samples and below 0.01 per cent K2O in 35.
Derivation of basalt magma from upper-mantle material similar to such ultramafic rocks, as has been postulated, is precluded by the relative amounts of sodium and potassium, which are from 200 to 600 times more abundant in basalt than in the ultramafic rocks. Similar factors apply to a number of other elements. No reasonable process could produce such concentrations in, for example, tens of thousands of cubic miles of uniform tholeiitic basalt. The ultramafic rocks might have originated either as magmatic crystal precipitates or as mantle residues left after fusion and removal of basaltic magma. Injection of ultramafic rocks to exposed positions is tectonic rather than magmatic.
A modified Morey bomb was designed which contains a removable nichromecased 3.5-ml platinium crucible. This bomb is particularly useful for decompositions of refractory samples for micro- and semimicro-analysis. Temperatures of 400–450° and pressures estimated as great as 6000 p.s.i. were maintained in the bomb for periods as long as 24 h. Complete decompositions of rocks, garnet, beryl, chrysoberyl, phenacite, sapphirine, and kyanite were obtained with hydrofluoric acid or a mixture of hydrofluoric and sulfuric acids; the decomposition of chrome refractory was made with hydrochloric acid. Aluminum-rich samples formed difficultly soluble aluminum fluoride precipitates. Because no volatilization losses occur, silica can be determined on sample solutions by a molybdenum-blue procedure using aluminum(III) to complex interfering fluoride.
Four dredge hauls from near the crest and from the eastern flank of the seismically active Mid-Indian Ocean Ridge at 23° to 24°S, at depths of 3700 to 4300 meters, produced only low-potassium tholeiitic basalt similar in chemical and mineralogic composition to basalts characteristic of ridges and rises in the Atlantic and Pacific oceans. A fifth haul, from a depth of 4000 meters on the lower flank of a seamount on the ocean side of the Indonesian Trench, recovered tholeiitic basalt with higher concentrations of K and Ti and slightly lower amounts of Si and Ca than the typical-oceanic tholeiite of the ridge. The last sample is vesicular, suggesting depression of the area since the basalt was emplaced. Many of the rocks dredged are variously decomposed and hydrated, but there is no evidence of important chemical modification toward conversion of the lava flows to spilite during extrusion or solidification.
Fresh ground water (200 parts per million total dissolved solids and upwards) occurs in portions of Pleistocene sandstone aquifers beneath basins and wadis in north Kuwait where the mean rainfall is about five inches per year. The fresh water is surrounded and underlain by brackish water (> 4000 ppm TDS). Drilling and testing show that fresh water saturation is restricted to wadis and basin areas; in Rawdatain basin it attains a maximum thickness of about 110 feet and a lateral extent of about seven miles.
The fresh ground water represents recharge localized, during infrequent, torrential rain storms, in areas of concentrated runoff where sediments in the vadose zone are moderately permeable and depth to the water table is generally less than a hundred feet. Concentration of runoff appears to be the primary control in the localization of recharge. The fresh water percolates downward to the ground-water reservoir following rare storms, then flows in the direction of hydraulic gradient and gradually becomes brackish.
Theoretical delineation of the recharge area and ground-water flow pattern in Rawdatain was confirmed by tritium and C14 dating of the water.
Brackish ground-water conditions prevail from water table downward in areas where rainfall infiltrates essentially where it falls, permeability of sediments in the vadose zone is low, or the water table is several hundred feet below land surface. In these areas, rainfall is retained and lost within the soil zone or becomes mineralized during deep percolation.
","language":"English","publisher":"Elsevier","doi":"10.1016/0022-1694(65)90038-7","issn":"00221694","usgsCitation":"Bergstrom, R., and Aten, R., 1965, Natural recharge and localization of fresh ground water in Kuwait: Journal of Hydrology, v. 2, no. 3, p. 213-231, https://doi.org/10.1016/0022-1694(65)90038-7.","productDescription":"19 p.","startPage":"213","endPage":"231","numberOfPages":"19","costCenters":[],"links":[{"id":219390,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Kuwait","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[47.97452,29.97582],[48.18319,29.53448],[48.09394,29.3063],[48.41609,28.552],[47.70885,28.52606],[47.45982,29.00252],[46.56871,29.09903],[47.30262,30.05907],[47.97452,29.97582]]]},\"properties\":{\"name\":\"Kuwait\"}}]}","volume":"2","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a6351e4b0c8380cd7241c","contributors":{"authors":[{"text":"Bergstrom, R.E.","contributorId":66413,"corporation":false,"usgs":true,"family":"Bergstrom","given":"R.E.","email":"","affiliations":[],"preferred":false,"id":359369,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Aten, R.E.","contributorId":18105,"corporation":false,"usgs":true,"family":"Aten","given":"R.E.","email":"","affiliations":[],"preferred":false,"id":359368,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70161771,"text":"70161771 - 1964 - The role of free and bound water in irradiation preservation: Free radical damage as a function of the physical state of water","interactions":[],"lastModifiedDate":"2017-01-11T16:33:31","indexId":"70161771","displayToPublicDate":"2015-09-07T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2293,"text":"Journal of Food Science","active":true,"publicationSubtype":{"id":10}},"title":" The role of free and bound water in irradiation preservation: Free radical damage as a function of the physical state of water","docAbstract":"English sole fillets previously equilibrated with aqueous 0.1% cysteine were dehydrated by three methods to moisture levels ranging from 2 to 72%. Model systems using cellulose to replace the fish tissue were also used. The samples were irradiated at 1 Mrad in an air, nitrogen, or oxygen atmosphere. The destruction of −SH groups was measured and related to the amount and physical state of the tissue water. As free water was removed, destruction steadily increased, reaching a maximum at about 20% moisture. Destruction decreased markedly at moisture levels below 10%, and calorimetric measurements confirmed that 10% moisture was about the level of bound water in this species. These data suggest that dehydration favors the reaction of solute molecules with free radicals formed in the free water of muscle cells. At moisture levels greater than about 20%, simple free radical recombination is more likely than reaction with solute molecules, while below 20% moisture the reverse is true. The calculated α values support this conclusion, as do the results from model systems using cellulose.
","language":"English","publisher":"Institute of Food Technologists","doi":"10.1111/j.1365-2621.1964.tb00405.x","usgsCitation":"Wedemeyer, G., and Dollar, A., 1964, The role of free and bound water in irradiation preservation: Free radical damage as a function of the physical state of water: Journal of Food Science, v. 29, no. 5, p. 525-529, https://doi.org/10.1111/j.1365-2621.1964.tb00405.x.","productDescription":"5 p.","startPage":"525","endPage":"529","numberOfPages":"5","costCenters":[],"links":[{"id":313882,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"29","issue":"5","noUsgsAuthors":false,"publicationDate":"2006-08-25","publicationStatus":"PW","scienceBaseUri":"568e48cae4b0e7a44bc41815","contributors":{"authors":[{"text":"Wedemeyer, Gary gwedemeyer@usgs.gov","contributorId":5504,"corporation":false,"usgs":true,"family":"Wedemeyer","given":"Gary","email":"gwedemeyer@usgs.gov","affiliations":[],"preferred":true,"id":587723,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dollar, A.M.","contributorId":150882,"corporation":false,"usgs":false,"family":"Dollar","given":"A.M.","email":"","affiliations":[],"preferred":false,"id":587724,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70043613,"text":"70043613 - 1964 - Crustal structure between Lake Mead, Nevada, and Mono Lake, California","interactions":[],"lastModifiedDate":"2013-02-15T10:17:42","indexId":"70043613","displayToPublicDate":"2013-02-13T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":6,"text":"USGS Unnumbered Series"},"seriesTitle":{"id":355,"text":"Crustal Studies Technical Letter","active":false,"publicationSubtype":{"id":6}},"seriesNumber":"22","title":"Crustal structure between Lake Mead, Nevada, and Mono Lake, California","docAbstract":"Interpretation of a reversed seismic-refraction profile between Lake Mead, Nevada, and Mono Lake, California, indicates velocities of 6.15 km/sec for the upper layer of the crust, 7.10 km/sec for an intermediate layer, and 7.80 km/sec for the uppermost mantle. Phases interpreted to be reflections from the top of the intermediate layer and the Mohorovicic discontinuity were used with the refraction data to calculate depths. The depth to the Moho increases from about 30 km near Lake Mead to about 40 km near Mono Lake. Variations in arrival times provide evidence for fairly sharp flexures in the Moho. Offsets in the Moho of 4 km at one point and 2 1/2 km at another correspond to large faults at the surface, and it is suggested that fracture zones in the upper crust may displace the Moho and extend into the upper mantle. The phase P appears to be an extension of the reflection from the top of the intermediate layer beyond the critical angle. Bouguer gravity, computed for the seismic model of the crust, is in good agreement with the measured Bouguer gravity. Thus a model of the crustal structure is presented which is consistent with three semi-independent sources of geophysical data: seismic-refraction, seismic-reflection, and gravity.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/70043613","collaboration":"In cooperation with the Defense Advanced Research Projects Agency","usgsCitation":"Johnson, L.R., 1964, Crustal structure between Lake Mead, Nevada, and Mono Lake, California: Crustal Studies Technical Letter 22, 21 p., https://doi.org/10.3133/70043613.","productDescription":"21 p.","numberOfPages":"25","onlineOnly":"Y","costCenters":[{"id":237,"text":"Earthquake Science Center","active":true,"usgs":true},{"id":379,"text":"Menlo Park Science Center","active":false,"usgs":true}],"links":[{"id":267548,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":267546,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/misc/tl/0022/"},{"id":267547,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/misc/tl/0022/tl0022.pdf"}],"country":"United States","state":"California;Nevada","otherGeospatial":"Lake Mead;Mono Lake","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -0.01611111111111111,8.333333333333334E-4 ], [ -0.01611111111111111,8.333333333333334E-4 ], [ -0.01638888888888889,8.333333333333334E-4 ], [ -0.01638888888888889,8.333333333333334E-4 ], [ -0.01611111111111111,8.333333333333334E-4 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"511f670fe4b03b29402c5dbc","contributors":{"authors":[{"text":"Johnson, Lane R.","contributorId":19049,"corporation":false,"usgs":true,"family":"Johnson","given":"Lane","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":473970,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70040819,"text":"70040819 - 1964 - Continental crust","interactions":[],"lastModifiedDate":"2013-01-15T11:50:00","indexId":"70040819","displayToPublicDate":"2012-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":6,"text":"USGS Unnumbered Series"},"seriesTitle":{"id":355,"text":"Crustal Studies Technical Letter","active":false,"publicationSubtype":{"id":6}},"seriesNumber":"20","title":"Continental crust","docAbstract":"The structure of the Earth’s crust (the outer shell of the earth above the M-discontinuity) has been intensively studied in many places by use of geophysical methods. The velocity of seismic compressional waves in the crust and in the upper mantle varies from place to place in the conterminous United States. The average crust is thick in the eastern two-thirds of the United States, in which the crustal and upper-mantle velocities tend to be high. The average crust is thinner in the western one-third of the United States, in which these velocities tend to be low. The concept of eastern and western superprovinces can be used to classify these differences. Crustal and upper-mantle densities probably vary directly with compressional-wave velocity, leading to the conclusion that isostasy is accomplished by the variation in densities of crustal and upper-mantle rocks as well as in crustal thickness, and that there is no single, generally valid isostatic model. The nature of the M-discontinuity is still speculative.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/70040819","collaboration":"In cooperation with the Defense Advanced Research Projects Agency","usgsCitation":"Pakiser, L.C., 1964, Continental crust: Crustal Studies Technical Letter 20, iv, 24 p., https://doi.org/10.3133/70040819.","productDescription":"iv, 24 p.","numberOfPages":"28","onlineOnly":"Y","additionalOnlineFiles":"N","costCenters":[{"id":237,"text":"Earthquake Science Center","active":true,"usgs":true}],"links":[{"id":263275,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/misc/tl/0020/"},{"id":263276,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/misc/tl/0020/tl0020.pdf"},{"id":263277,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"country":"United States","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ 144.616667,13.233333 ], [ 144.616667,71.833333 ], [ -64.566667,71.833333 ], [ -64.566667,13.233333 ], [ 144.616667,13.233333 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"50abfbd3e4b0afbc75eb982c","contributors":{"authors":[{"text":"Pakiser, L. C.","contributorId":83512,"corporation":false,"usgs":true,"family":"Pakiser","given":"L.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":469080,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70189329,"text":"70189329 - 1964 - Water quality of the Swatara Creek Basin, PA","interactions":[],"lastModifiedDate":"2017-07-12T14:56:41","indexId":"70189329","displayToPublicDate":"1999-12-26T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":6,"text":"USGS Unnumbered Series"},"seriesTitle":{"id":375,"text":"Open-File Report","active":false,"publicationSubtype":{"id":6}},"title":"Water quality of the Swatara Creek Basin, PA","docAbstract":"The Swatara Creek of the Susquehanna River Basin is the farthest downstream sub-basin that drains acid water (pH of 4.5 or less) from anthracite coal mines. The Swatara Creek drainage area includes 567 square miles of parts of Schuylkill, Berks, Lebanon, and Dauphin Counties in Pennsylvania.
To learn what environmental factors and dissolved constituents in water were influencing the quality of Swatara Creek, a reconnaissance of the basin was begun during the summer of 1958. Most of the surface streams and the wells adjacent to the principal tributaries of the Creek were sampled for chemical analysis. Effluents from aquifers underlying the basin were chemically analyzed because ground water is the basic source of supply to surface streams in the Swatara Creek basin. When there is little runoff during droughts, ground water has a dominating influence on the quality of surface water. Field tests showed that all ground water in the basin was non-acidic. However, several streams were acidic. Sources of acidity in these streams were traced to the overflow of impounded water in unworked coal mines.
Acidic mine effluents and washings from coal breakers were detected downstream in Swatara Creek as far as Harper Tavern, although the pH at Harper Tavern infrequently went below 6.0. Suspended-sediment sampling at this location showed the mean daily concentration ranged from 2 to 500 ppm. The concentration of suspended sediment is influenced by runoff and land use, and at Harper Tavern it consisted of natural sediments and coal wastes. The average daily suspended-sediment discharge there during the period May 8 to September 30, 1959, was 109 tons per day, and the computed annual suspended-sediment load, 450 tons per square mile.
Only moderate treatment would be required to restore the quality of Swatara Creek at Harper Tavern for many uses. Above Ravine, however, the quality of the Creek is generally acidic and, therefore, of limited usefulness to public supplies, industries and recreation.
In general, the quality of Swatara Creek improves after it mixes with water from the Upper Little and Lower Little Swatara Creeks, which converge with the main stream near Pine Grove. Jonestown is the first downstream location where Swatara Creek contains bicarbonate ion most of the time, and for the remaining downstream length of the stream, the concentration of bicarbonate progressively increases. Before the stream enters the Susquehanna River, chemical and diluting processes contributed by tributaries change the acidic calcium sulfate water, which characterizes the upper Swatara, to a calcium bicarbonate water.
A major tributary to Swatara Creek is Quittapahilla Creek, which drains a limestone region and has alkaline characteristics. Effluents from a sewage treatment plant are discharged into this stream west of Lebanon. Adjacent to the Creek are limestone quarries and during the recovery of limestone, ground water seeps into the mining areas. This water is pumped to upper levels and flows over the land surface into Quittapahilla Creek.
As compared with the 1940's, the quality of Swatara Creek is better today, and the water is suitable for more uses. In large part, this improvement is due to curtailment of anthracite coal mining and because of the controls imposed on new mines, stripping mines, and the related coal mining operations, by the Pennsylvania Sanitary Water Board. Thus, today (1962) smaller amounts of coal mine wastes are more effectively flushed and scoured away with each successive runoff during storms that affect the drainage basin. Natural processes neutralizing acid water in the stream by infiltration of alkaline ground water through springs and through the streambed are also indicated.
","language":"English","publisher":" U.S. Geological Survey","doi":"10.3133/70189329","collaboration":"Prepared in cooperation with the Pennsylvania Department of Forests and Waters","usgsCitation":"McCarren, E.F., Wark, J., and George, J., 1964, Water quality of the Swatara Creek Basin, PA: Open-File Report, 88 p., https://doi.org/10.3133/70189329.","productDescription":"88 p.","costCenters":[],"links":[{"id":343575,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/unnumbered/70189329/report-thumb.jpg"},{"id":343749,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70189329/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Pennsylvania","otherGeospatial":"Swatara Creek Basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -75.80841064453125,\n 41.03585891144301\n ],\n [\n -75.82763671875,\n 41.03378713521864\n ],\n [\n -76.102294921875,\n 41.02964338716638\n ],\n [\n -76.70379638671874,\n 40.84498264925404\n ],\n [\n -76.81915283203125,\n 40.670222795307346\n ],\n [\n -76.84661865234375,\n 40.54511315470123\n ],\n [\n -76.89605712890625,\n 40.287906612507406\n ],\n [\n -76.871337890625,\n 40.18516846826054\n ],\n [\n -76.73126220703125,\n 40.13899044275822\n ],\n [\n -76.6790771484375,\n 40.11799004890473\n ],\n [\n -75.948486328125,\n 40.21873275657034\n ],\n [\n -75.73699951171875,\n 40.30466538259176\n ],\n [\n -75.5859375,\n 40.48455955508278\n ],\n [\n -75.62164306640625,\n 40.65563874006118\n ],\n [\n -75.65185546874999,\n 40.83874913796459\n ],\n [\n -75.74249267578125,\n 40.96952973563832\n ],\n [\n -75.80841064453125,\n 41.03585891144301\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5965e3afe4b0d1f9f05c1d98","contributors":{"authors":[{"text":"McCarren, Edward F.","contributorId":106472,"corporation":false,"usgs":true,"family":"McCarren","given":"Edward","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":704194,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wark, J.W.","contributorId":194454,"corporation":false,"usgs":false,"family":"Wark","given":"J.W.","email":"","affiliations":[],"preferred":false,"id":704195,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"George, J.R.","contributorId":15277,"corporation":false,"usgs":true,"family":"George","given":"J.R.","email":"","affiliations":[],"preferred":false,"id":704196,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":1232,"text":"wsp1752 - 1964 - Ground-water resources of north-central Connecticut","interactions":[],"lastModifiedDate":"2012-02-02T00:05:18","indexId":"wsp1752","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1752","title":"Ground-water resources of north-central Connecticut","docAbstract":"The term 'north-central Connecticut' in this report refers to an area of about 640 square miles within the central lowland of the Connecticut River basin north of Middletown. The area is mostly a broad valley floor underlain by unconsolidated deposits of Pleistocene and Recent age which mantle an erosional surface formed on consolidated rocks of pre-Triassic and Triassic age. The mean annual precipitation at Hartford, near the center of the area, is 42.83 inches and is uniformly distributed throughout the year. The average annual streamflow from the area is about 22 inches or about half the precipitation. The consolidated water-bearing formations are crystalline rocks of pre-Triassic age and sedimentary and igneous rocks of the Newark group of Triassic age. \r\n\r\nThe crystalline rocks include the Middletown gneiss, the Maromas granite gneiss, the Glastonbury granite-gneiss of Rice and Gregory (1906), and the Bolton schist which form the basement complex and the Eastern Upland of north-central Connecticut. Enough water for domestic, stock, and small commercial use generally can be obtained from the crystalline rocks. Recoverable ground water occurs in the interconnected joints and fracture zones and is yielded in amounts ranging from 29 to 35 gpm (gallons per minute) to wells ranging in depth from 29 to 550 feet. \r\n\r\nThe sedimentary rocks of Triassic age underlie all the Connecticut River Lowland and are predominantly arkosic sandstone and shale. Water supplies sufficient for domestic, stock, and small commercial use can be obtained from shallow wells penetrating these rocks, and larger supplies sufficient for industries and smaller municipalities can probably be obtained from deeper wells. \r\n\r\nReported yields range from ? to 578 gpm; the larger yields are generally obtained from wells between 300 and 600 feet in depth. Yields are larger where the overlying material is sand and gravel or where the rocks are well fractured. The igneous rocks of Triassic age are basalt and have water-bearing characteristics similar to the crystalline rocks. \r\n\r\nThe unconsolidated deposits comprise ground-moraine and drumlin deposits, ice-contact deposits, outwash-plain and valley-train deposits, and glaciolacustrine and associated delta deposits of Pleistocene age, as well as dune deposits, good-plain deposits, and swamp deposits of Recent age. Ground-moraine deposits occur throughout the area but yield only small quantities of water. \r\n\r\nThe ice-contact deposits consisting mostly of sand and gravel form kames, kame terraces, and crevasse fillings and are the surface deposits in three extensive areas along the eastern margin of the Connecticut River Lowland. The deposits in most places are saturated and, where they consist of well-sorted material, are highly permeable, yielding as much as 750 gpm to properly constructed wells. \r\n\r\nOutwash-plain and valley-train deposits and bodies of undifferentiated outwash underlie the surface in the eastern and southern parts of the area. These deposits consist of well-sorted sand and silt and some pebble gravel ranging in thickness from nearly zero to more than 225 feet in places. The thicker deposits are an important source of moderate supplies of ground water. Screened wells of moderate depth commonly yield about 150 gpm, but some yield as much as 400 gpm. Bodies of buried outwash deposits of irregular size and shape occur in the bottoms of some of the filled bedrock valleys. They seldom are more than 20-30 feet thick. Their permeability Is generally low because of the high percentage of silt; yields as much as 30 gpm to domestic wells are reported. Under most favorable conditions, these deposits yield as much as 500 gpm. The glaciolacustrine and associated delta deposits occur in nearly all parts of north-central Connecticut and are potential sources of moderate supplies of ground water. They consist of well-sorted sand which generally grades downward into varved clay and silt. The deposits of sand are thic","language":"ENGLISH","publisher":"U. S. Govt. Print. Off.,","doi":"10.3133/wsp1752","usgsCitation":"Cushman, R.V., 1964, Ground-water resources of north-central Connecticut: U.S. Geological Survey Water Supply Paper 1752, v, 96 p. :illus. maps (2 col.) ;24 cm., https://doi.org/10.3133/wsp1752.","productDescription":"v, 96 p. :illus. maps (2 col.) ;24 cm.","costCenters":[],"links":[{"id":138070,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1752/report-thumb.jpg"},{"id":26154,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1752/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26155,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1752/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26156,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1752/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26157,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1752/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a97e4b07f02db65add7","contributors":{"authors":[{"text":"Cushman, Robert Vittum","contributorId":96661,"corporation":false,"usgs":true,"family":"Cushman","given":"Robert","email":"","middleInitial":"Vittum","affiliations":[],"preferred":false,"id":143411,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2659,"text":"wsp1608F - 1964 - Cenomanian-Turonian aquifer of central Israel, its development and possible use as a storage reservoir","interactions":[],"lastModifiedDate":"2013-08-12T12:29:21","indexId":"wsp1608F","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1608","chapter":"F","title":"Cenomanian-Turonian aquifer of central Israel, its development and possible use as a storage reservoir","docAbstract":"The Cenomanian-Turonian formations constitute a highly permeable dolomite and limestone aquifer in central Israel. The aquifer is on the west limb of an anticlinorium that trends north-northeast. In places it may be as much as 800 meters thick, but in the report area, largely the foothills of the Judean-Ephraim Mountains where the water development is most intensive, its thickness is generally considerably less. In some places the aquifer occurs at or near the land surface, or it is covered by sandy and gravelly coastal-plain deposits. However, in a large part of the area, it is overlain by as much as 400 meters of relatively impermeable strata, and it is probably underlain by less permeable Lower Cretaceous strata. \n\nIn general the aquifer water is under artesian pressure. The porosity of the aquifer is characterized mainly by solution channels and cavities produced by jointing and faulting. In addition to the generally high permeability of the aquifer, some regions, which probably coincide with ancient drainage patterns and (or) fault zones, have exceptionally high permeabilities. \n\nThe source of most of the water in the aquifer is believed to be rain that falls on the foothills area. The westward movement of ground water from the mountainous outcrop areas appears to be impeded by a zone of low permeability which is related to structural and stratigraphic conditions along the western side of the mountains. \n\nGradients of the piezometric surface are small, and the net direction of water movement is westward and northwestward under natural conditions. Locally, however, the flow pattern may be in other directions owing to spatial variations in permeability in the aquifer, the location of natural discharge outlets, and the relation of the aquifer to adjacent geologic formations. There probably is also a large vertical component of flow. \n\nPumping has modified the flow pattern by producing several irregularly shaped shallow depressions in the piezometric surface although, to date, no unwatering of the aquifer has occurred. In the central part of the area, pumping has induced some infiltration from overlying coastal-plain formations. \n\nInjecting and storing surplus water seasonally in the aquifer should be feasible at almost any place. However, the movement and recovery of the injected water probably could be controlled most easily if the water were injected where depressions have been formed in the piezometric surface.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1608F","usgsCitation":"Schneider, R., 1964, Cenomanian-Turonian aquifer of central Israel, its development and possible use as a storage reservoir: U.S. Geological Survey Water Supply Paper 1608, iii, 20 p. :ill. ;24 cm. + plates folded in pocket., https://doi.org/10.3133/wsp1608F.","productDescription":"iii, 20 p. :ill. ;24 cm. + plates folded in pocket.","costCenters":[],"links":[{"id":138224,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1608f/report-thumb.jpg"},{"id":28995,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1608f/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":276493,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1608f/plate-2.pdf"},{"id":276494,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1608f/plate-3.pdf"},{"id":276492,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1608f/plate-1.pdf"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e5e4b07f02db5e6f54","contributors":{"authors":[{"text":"Schneider, Robert","contributorId":102460,"corporation":false,"usgs":true,"family":"Schneider","given":"Robert","email":"","affiliations":[],"preferred":false,"id":145569,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":12938,"text":"ofr6433 - 1964 - Geology of the Andover Granite and surrounding rocks, Massachusetts","interactions":[],"lastModifiedDate":"2012-02-02T00:06:56","indexId":"ofr6433","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","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":"64-33","title":"Geology of the Andover Granite and surrounding rocks, Massachusetts","docAbstract":"Field and petrographic studies of the Andover Granite and surrounding rocks have afforded an opportunity for an explanation of its emplacement and crystallization. The investigation has contributed secondarily to an understanding of the geologic history of southeastern New England, particularly as it is revealed in the Lawrence, Wilmington, South Groveland, and Reading quadrangles of Massachusetts. \r\n\r\nThe Andover Granite and Sharpners Pond Tonalite together comprise up to 90 percent of the Acadian(?) subalkaline intrusive series cropping out within the area of study. The subalkaline series locally invades a sequence of early to middle Paleozoic and possibly Precambrian metasedimentary and metavolcanic rocks. Much of the subalkaline series and most of the Andover Granite is confined between two prominent east-northeast trending faults or fault systems. The northern fault separates the mildly metamorphosed Middle Silurian(?) Merrimack Group on the north from a highly metamorphosed and thoroughly intruded Ordovician(?) sequence on the south. The southern 'boundary '' fault is a major structural discontinuity characterized by penetrative, diffuse shearing over a zone one-half mile or more in width. \r\n\r\nThe magmatic nature of the Andover Granite is demonstrated by: (1) sharply crosscutting relationships with surrounding rocks; (2) the occurrence of tabular-shaped xenoliths whose long directions parallel the foliation within the granite and whose internal foliation trends at a high angle to that of the granite; (3) continuity with the clearly intrusive Sharpners Pond Tonalite; (4) the compositional uniformity of the granite as contrasted with the compositional diversity of the rocks it invades; (5) its modal and normative correspondence with (a) calculated norms of salic extrusives and (b) that of the ternary (\u001Cgranite\u001D) minimum for the system NaAlSi3O8-KAlSi3O8-SiO2. \r\n\r\nOrogenic granites, as represented by the Andover, contrast with post-orogenic granites, represented locally by the Peabody Granite, in their phase composition and texture. Unlike the Peabody, the Andover Granite is thought to have been thoroughly recrystallized through the unmixing of initially homogeneous phases with the concomitant development of extremely intricate, allotriomorphic textures. Textural relationships between potassium and plagioclase feldspars and among quartz and the two feldspars, suggest that the Andover Granite has evolved through exsolution of a single hypersolvus feldspar (or two coexisting subsolvus feldspars of only slightly disparate compositions) into discrete grains of plagioclase and potassium feldspar, much along the lines proposed by Tuttle (1952). \r\n\r\nA hypothesis is proposed for the origin of myrmekite whereby it is evolved indirectly through exsolution of a homogeneous, hypersolvus, calcalkali feldspar in the presence of a silica reservoir. Where the An 'molecule' is contained in the primary mix crystal, exsolution into potassium and plagioclase feldspar phases normally requires a paired exchange between Ca-Al and K-Si. Should the silicon requirements of the developing potassium feldspar be met by the matrix silica reservoir, the concomitantly evolving plagioclase may become stoichiometrically enriched in silicon and ultimately develop into myrmekite. Discrete unmixing of pure alkali feldspar proceeds through simple alkali ion exchange; ternary compostions high in An are more apt to fall initially in the two-feldspar field, thereby reducing the unmixing potential. General restriction of myrmekite to plagioclase of calcic albite to oligoclase composition is explained accordingly.","language":"ENGLISH","publisher":"U.S. Geological Survey],","doi":"10.3133/ofr6433","usgsCitation":"Castle, R.O., 1964, Geology of the Andover Granite and surrounding rocks, Massachusetts: U.S. Geological Survey Open-File Report 64-33, 550 p. ill., maps ;29 cm., https://doi.org/10.3133/ofr6433.","productDescription":"550 p. ill., maps ;29 cm.","costCenters":[],"links":[{"id":146979,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1964/0033/report-thumb.jpg"},{"id":41382,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0033/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41383,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0033/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41384,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0033/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41385,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0033/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41386,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0033/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41387,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0033/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41388,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0033/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41389,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0033/plate-8.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41390,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0033/plate-9.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41391,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1964/0033/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad5e4b07f02db68353e","contributors":{"authors":[{"text":"Castle, Robert O.","contributorId":22741,"corporation":false,"usgs":true,"family":"Castle","given":"Robert","email":"","middleInitial":"O.","affiliations":[],"preferred":false,"id":166992,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2983,"text":"wsp1499E - 1964 - Water resources of the Flint area, Michigan","interactions":[],"lastModifiedDate":"2017-02-06T15:45:12","indexId":"wsp1499E","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1499","chapter":"E","title":"Water resources of the Flint area, Michigan","docAbstract":"This report describes the water resources of Genesee County, Mich., whose principal city is Flint. The sources of water available to the county are the Flint and Shiawassee Rivers and their tributaries, inland lakes, ground water, and Lake Huron. The withdrawal use of water in the county in 1958 amounted to about 45 mgd. Of this amount, 36 mgd was withdrawn from the Flint River by the Flint public water-supply system. The rest was supplied by wells. At present (1959) the Shiawassee River and its tributaries and the inland lakes are not used for water supply.
Flint River water is used for domestic, industrial, and waste-dilution requirements in Flint. About 60 percent of the water supplied by the Flint public water system is used by Flint industry. At least 30 mgd of river water is needed for waste dilution in the Flint River during warm weather.
Water from Holloway Reservoir, which has a storage capacity of 5,760 million gallons, is used to supplement low flows in the Flint River to meet water-supply and waste-dilution requirements. About 650 million gallons in Kearsley Reservoir, on a Flint River tributary, is held in reserve for emergency use. Based on records for the lowest flows during the period 1930-52, the Flint River system, with the two reservoirs in operation, is capable of supplying about 60 mgd at Flint, less evaporation and seepage losses. The 1958 water demands exceeded this amount. Development of additional storage in the Flint River basin is unlikely because of lack of suitable storage sites. Plans are underway to supply Flint and most of Genesee County with water from Lake Huron.
The principal tributaries of the Flint River in and near Flint could furnish small supplies of water. Butternut Creek, with the largest flow of those studied, has an estimated firm yield of 0.054 mgd per sq mi for 95 percent of the time. The Shiawassee River at Byron is capable of supplying at least 29 mgd for 95 percent of the time.
Floods are a serious problem in Flint. The April 1947 flood, the largest on record, caused nearly $4 million flood damage in Flint. A proposed flood-control plan for Flint calls for channel, floodwall, and levee improvements and the removal or modification of some bridges.
Analyses of water samples taken from selected streams and lakes in the Flint area indicate that the waters are of the calcium bicarbonate type and generally hard to very hard. Flint River water is relatively uniform in quality although a progressive increase in iron, sodium, and chloride concentrations was noted between Otisville and Montrose. Downstream from Flint, the dissolved oxygen
content may be low during low flows. At times, concentrations of iron, manganese, phenols, color, and turbidity in Flint River water exceed the limits recommended in drinking water standards. Water temperatures ranged from freezing to 86°F in a 4-year period. The finished water supplied by the Flint water-treatment plant is fairly uniform in quality, moderately soft, alkaline, and low in color and turbidity. The pH is nearly always above 10. Further softening and removal of iron and related minerals would be desirable for certain industrial uses.
The quality of the water sampled in the Flint River tributaries was generally similar to that of the Flint River. However, no phenols or oils and waxes were found. Softening and other treatment dependent upon use would be required if these streams were developed for water supply.
Waters sampled in the Shiawassee River and selected lakes were generally less mineralized than Flint River water. Water from the lakes showed the lowest concentrations of dissolved solids. Softening would be required for nearly all uses. Additional treatment would depend upon contemplated use.
Shallow deposits of sand and gravel deposited as outwash along glacial meltwater streams and as deltas in the glacial lakes that covered the northwestern part of the county are sources of water to moderate- and large-capacity wells. Thick deposits of sand and gravel also fill some of the valleys in the bedrock surface and yield moderate to large supplies of water. Production from public supply wells tapping the drift aquifers in the area ranges from about 50 to 1,200 gpm. The water from the drift aquifer is hard or very hard and commonly contains objectionable amounts of iron.
The Saginaw formation is a source of water to wells supplying some of the small communities and industries in the county. The Saginaw, which is the uppermost bedrock formation in the area, underlies most of the county. It is composed of layers of sandstone, shale, and limestone and some beds of coal. The formation is composed principally of sandstone in some areas of the county, and shale in others. Production from wells tapping the Saginaw ranges from a few to about 500 gpm. The water produced is generally moderately hard or hard and commonly contains objectionable amounts of chloride. The quality of the water limits its development for water supply. Overdrafts from the Saginaw result in a lowering of the piezometric surface and commonly cause an upward migration of water high in chloride.
The Michigan and Marshall formations are generally not sources of fresh water where they are overlain by the Saginaw formation. In the southern and eastern parts of the county where they are overlain by glacial deposits, they are a source of water of good quality. The quantity of water obtainable from these formations is not fully known. However, the Marshall may be a source of large supplies of water in the southeastern part of the county.
An ample supply of water is available in lakes, ponds, and streams in the metropolitan area of Flint to meet requirements for domestic, sanitary, and firefighting use in civil defense emergencies. The extent of emergency use of water from these sources would depend upon the pumping, distribution, and treatment facilities available. Enough private industrial and commercial, and public wells are present in the area normally supplied by the Flint public water system to meet emergency requirements for domestic and sanitary use. Use of these wells would also depend upon available pumping and distribution facilities. Water from many of these wells contains objectionable amounts of chloride, but it could be used without treatment in an emergency.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1499E","usgsCitation":"Wiitala, S.W., Vanlier, K., and Krieger, R.A., 1964, Water resources of the Flint area, Michigan: U.S. Geological Survey Water Supply Paper 1499, Document: viii, 86 p.; 6 Plates: 20.00 x 18.29 inches or smaller, https://doi.org/10.3133/wsp1499E.","productDescription":"Document: viii, 86 p.; 6 Plates: 20.00 x 18.29 inches or smaller","costCenters":[{"id":382,"text":"Michigan Water Science Center","active":true,"usgs":true}],"links":[{"id":139431,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1499e/report-thumb.jpg"},{"id":29743,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499e/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29744,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499e/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29745,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499e/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29746,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499e/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29747,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499e/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29748,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499e/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29749,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1499e/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Michigan","county":"Genesee County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-83.4607,43.2235],[-83.4593,43.1425],[-83.4589,43.1365],[-83.455,42.9681],[-83.4553,42.9617],[-83.4546,42.8798],[-83.4541,42.8766],[-83.5737,42.8744],[-83.6902,42.871],[-83.6863,42.7822],[-83.9225,42.7812],[-83.928,42.8677],[-83.9309,42.9574],[-83.9283,43.0451],[-83.9294,43.1334],[-83.9318,43.2204],[-83.8154,43.2212],[-83.694,43.2223],[-83.5809,43.2226],[-83.4607,43.2235]]]},\"properties\":{\"name\":\"Genesee\",\"state\":\"MI\"}}]}\n","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a14e4b07f02db602df3","contributors":{"authors":[{"text":"Wiitala, Sulo Werner","contributorId":20315,"corporation":false,"usgs":true,"family":"Wiitala","given":"Sulo","email":"","middleInitial":"Werner","affiliations":[],"preferred":false,"id":146097,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Vanlier, K.E.","contributorId":24332,"corporation":false,"usgs":true,"family":"Vanlier","given":"K.E.","affiliations":[],"preferred":false,"id":146098,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Krieger, Robert A.","contributorId":99954,"corporation":false,"usgs":true,"family":"Krieger","given":"Robert","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":146099,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":14683,"text":"ofr64103 - 1964 - The geology, mineralogy and paragenesis of the Castrovirreyna lead-zinc-silver deposits, Peru","interactions":[],"lastModifiedDate":"2012-02-02T00:07:06","indexId":"ofr64103","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","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":"64-103","title":"The geology, mineralogy and paragenesis of the Castrovirreyna lead-zinc-silver deposits, Peru","docAbstract":"The Castrovirreyna mining district lies in the Andean Cordillera of South Central Peru, and has been worked sporadically since its discovery in 1591. Supergene silver ores were first mined. Currently the district produces about 20,000 tons of lead-zinc ore and 5000 tons of silver ore annually.\r\n\r\nThe district is underlain by Tertiary andesitic rocks interbedded with basalts and intruded by small bodies of quartz latite porphyry. The terrane reflects recent glaciation and is largely covered by glacial debris.\r\n\r\nThe ore deposits are steeply dipping veins that strike N. 60? E. to S. 50? E., and average 60 centimeters wide and 300 meters long. The principal veins are grouped around three centers, lying 5 kilometers apart along a line striking N. 55? E. They are, from east to west: San Genaro, Caudalosa, and La Virreyna. A less important set of veins, similarly aligned, lies 2 kilometers to the north. Most of the veins were worked to depths of about 30 meters, the limit of supergene enrichment; but in the larger veins hypogene ores have been worked to depths of over 150 meters.\r\n\r\nGalena, sphalerite, chalcopyrite, and tetrahedrite are common to all veins, but are most abundant in the westernmost veins at La Virreyna. In the center of the district, around Caudalosa, land sulfantimonides are the commonest ore minerals, and at the eastern end, around San Genaro and Astohuaraca, silver sulfosalts predominate.\r\n\r\nSupergene enrichment of silver is found at shallow depths in all deposits. Silver at San Genaro, however, was concentrated towards the surface by migration along hypogene physico-chemical gradients in time and space, as vein material was reworked by mineralizing fluids. The pattern of wallrock alteration throughout the district grades from silicification and scricitization adjacent to the veins, through argillization and propylitization, to widespread chloritization farther away.\r\n\r\nMineralization can be divided into three stages:\r\n\r\n1) Preparatory stage, characterized by silicification and pyritization;\r\n\r\n2) Depositional stage, characterized by the deposition of base-metal sulfides; and\r\n\r\n3) Reworking stage, characterized by the formation of lead sulfantimonides from galena at Caudalosa, and the deposition of silver sulfide and sulfosalts at San Genaro.\r\n\r\nMaximum temperatures, indicated by the wurtzite-sphalerite, famatinite-energite and chalcopyrite-sphalerite assemblages, did not exceed 350? C. The low iron content of sphalerite suggests that most of the base-metal sulfides were deposited below 250? C. The colloidal habits of pyrite and quartz in the preparatory and reworking stages imply relatively low temperatures of deposition, probably between 50? C and 100? C.\r\n\r\nMineralization was shallow and pressures ranged from 17 atmospheres in the silver deposits to over 45 atmospheres in the lead sulfantimonide deposits.\r\n\r\nMineralization at Castrovirreyna represents an open chemical system in which mineralizing fluids constantly modified the depositional environment while they themselves underwent modification. The deposits formed under nonequilibrium conditions from fluids containing complex ions and colloids. Reworking and migration along persistent physico-chemical gradients in time and space, from a deep source to the west concentrated base-metal sulfides in the western half, lead-antimony minerals in the center, and silver-antimony minerals in the eastern part of the district. Silver, antimony, and bismuth were kept in solution as complex ions until low temperature and pressure prevailed. They document in situ reworking by reacting with existing minerals.\r\n\r\nPhysico-chemical gradients controlled the type of minerals deposited, whereas vein structure controlled the quantity deposited.\r\n\r\nVein fissures formed by the equivalent of from east-west compression during Andean orogenesis and mineralization probably came from the underlying Andean Batholith.","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/ofr64103","usgsCitation":"Lewis, R.W., 1964, The geology, mineralogy and paragenesis of the Castrovirreyna lead-zinc-silver deposits, Peru: U.S. Geological Survey Open-File Report 64-103, 265 p. ill., maps ;29 cm., https://doi.org/10.3133/ofr64103.","productDescription":"265 p. ill., maps ;29 cm.","costCenters":[],"links":[{"id":149029,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1964/0103/report-thumb.jpg"},{"id":43451,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1964/0103/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43433,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0103/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43434,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0103/plate-02.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43435,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0103/plate-03.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43436,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0103/plate-04.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43437,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0103/plate-05.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43438,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0103/plate-06.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43439,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0103/plate-07.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43440,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0103/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43441,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0103/plate-09.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43442,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0103/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43443,"rank":410,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0103/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43444,"rank":411,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0103/plate-12.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43445,"rank":412,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0103/plate-13.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43446,"rank":413,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0103/plate-14.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43447,"rank":414,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0103/plate-15.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43448,"rank":415,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0103/plate-16.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43449,"rank":416,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0103/plate-17.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43450,"rank":417,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0103/plate-18.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9ae4b07f02db65d603","contributors":{"authors":[{"text":"Lewis, Richard Wheatley Jr.","contributorId":58656,"corporation":false,"usgs":true,"family":"Lewis","given":"Richard","suffix":"Jr.","email":"","middleInitial":"Wheatley","affiliations":[],"preferred":false,"id":169841,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":16256,"text":"ofr64151 - 1964 - Magnetic properties of Pd, Pd-H and Pd-D from 300 degrees K to 4.2 degrees K","interactions":[],"lastModifiedDate":"2024-08-05T20:04:29.494955","indexId":"ofr64151","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","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":"64-151","title":"Magnetic properties of Pd, Pd-H and Pd-D from 300 degrees K to 4.2 degrees K","docAbstract":"The magnetic properties of many substances first studied seriously by Faraday have played an important role in our modern technology. In particular, the magnetic properties of the transition elements are of great importance in the understanding of the electronic band form of these elements. Once the electronic band form is known, many of the physical properties may be predicted. Although many investigations have been made of the magnetic properties of palladium, no recent measurements have been reported at temperatures lower than 20° K.
There is some discrepancy between the earlier work of Onnes and Oosterhuis (1913, 1914) and the later work of Hoare and Matthews (1952). There is reason to believe that the later work is correct because of the purity of the samples, but the data indicate a necessity for measurements at temperatures below 20° K.
Palladium adsorbs enormous amounts of hydrogen and a study of this effect could lead to information which would be valuable in the interpretation of the magnetic properties of palladium. The magnetic susceptibility of hydrogenized palladium was studied first by Graham (1869). Since that time it has been shown by Svensson (1953) that the susceptibility of palladium diminishes linearly with increasing hydrogen content and finally reaches a value just below zero for a H/pd volume ratio of 800/1. This same effect was shown to occur by Sieverts and Danz (1937) when deuterium is substituted for hydrogen. Recently, Wucher (1952) has made a study of the variation of the susceptibility of hydrogenized palladium with temperature from -98.6° C to 16.3° C. However, later measurements of the resistivity and thermoelectric power of hydrogenized palladium by Schindler and Smith (1979) indicate that there might be a magnetic anomaly in hydrogenized palladium at 40° K.
The purpose of this work is to extend the previous measurements down to 4.2° K, but measurements will be made on desorbed as well as adsorbed samples of hydrogenized and deuterized palladium. The results on the desorbed samples turned out to be quite interesting and suggest further experiments.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr64151","usgsCitation":"Thorpe, A.N., 1964, Magnetic properties of Pd, Pd-H and Pd-D from 300 degrees K to 4.2 degrees K: U.S. Geological Survey Open-File Report 64-151, 56 p., https://doi.org/10.3133/ofr64151.","productDescription":"56 p.","costCenters":[],"links":[{"id":148285,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1964/0151/report-thumb.jpg"},{"id":432173,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1964/0151/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a80e4b07f02db649328","contributors":{"authors":[{"text":"Thorpe, Arthur N.","contributorId":52591,"corporation":false,"usgs":true,"family":"Thorpe","given":"Arthur","email":"","middleInitial":"N.","affiliations":[],"preferred":false,"id":172505,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1021,"text":"wsp1536I - 1964 - Methods of determining permeability, transmissibility and drawdown","interactions":[{"subject":{"id":51650,"text":"ofr5480 - 1954 - The \"slug test\" for estimating transmissibility","indexId":"ofr5480","publicationYear":"1954","noYear":false,"title":"The \"slug test\" for estimating transmissibility"},"predicate":"SUPERSEDED_BY","object":{"id":1021,"text":"wsp1536I - 1964 - Methods of determining permeability, transmissibility and drawdown","indexId":"wsp1536I","publicationYear":"1964","noYear":false,"chapter":"I","title":"Methods of determining permeability, transmissibility and drawdown"},"id":1},{"subject":{"id":51779,"text":"ofr54310 - 1954 - Estimating transmissibility from specific capacity","indexId":"ofr54310","publicationYear":"1954","noYear":false,"title":"Estimating transmissibility from specific capacity"},"predicate":"SUPERSEDED_BY","object":{"id":1021,"text":"wsp1536I - 1964 - Methods of determining permeability, transmissibility and drawdown","indexId":"wsp1536I","publicationYear":"1964","noYear":false,"chapter":"I","title":"Methods of determining permeability, transmissibility and drawdown"},"id":2}],"lastModifiedDate":"2012-02-02T00:05:16","indexId":"wsp1536I","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1536","chapter":"I","title":"Methods of determining permeability, transmissibility and drawdown","docAbstract":"If the Theis graphical method is used for determining the hydraulic constants of an aquifer under water-table conditions, the observed drawdowns should be corrected for the decrease in saturated thickness. This is especially true if the drawdown is a large fraction of the original saturated thickness, for then the computed coefficient of permeability is highly inaccurate if based on observed, rather than corrected, water levels. Wenzel's limiting formula, a modification of the Theis graphical method, is useful where u=r2s/4Tt is less than about 0.01. However, a shorter procedure for determination of the coefficient of transmissibility, as well as the coefficient of storage, consists of plotting the values of the corrected drawdowns against the values of the logarithm of r. \r\n\r\nWenzel (1942) suggested that observation wells be situated on lines that extend upgradient and downgradient from the pumped well. However, a detailed analysis of aquifer-test results indicates that such a restriction is unnecessary. The gradient method for determining permeability should yield the same results as the Thies method. The former, when applied for a distance within the range of applicability of the latter, is merely a duplication of effort or, at best, a crude check. Because of the limitations of accuracy in plotting, the gradient method is much less satisfactory. That Wenzel (1942) obtained identical results from the two methods is regarded as a coincidence. \r\n\r\nFailure to take into consideration the fact that the pumped well does not tap the full thickness of the aquifer leads to an apparent coefficient of permeability that is much too low, especially if the aquifer consists of stratified sediments. The average coefficient of permeability computed from uncorrected drawdowns may be only a little more than half of the true value.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1536I","usgsCitation":"Bentall, R., 1964, Methods of determining permeability, transmissibility and drawdown: U.S. Geological Survey Water Supply Paper 1536, vi, 99 p. :ill. ;24 cm., https://doi.org/10.3133/wsp1536I.","productDescription":"vi, 99 p. :ill. ;24 cm.","costCenters":[],"links":[{"id":137921,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1536i/report-thumb.jpg"},{"id":25635,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1536i/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a54e4b07f02db62bcc6","contributors":{"authors":[{"text":"Bentall, Ray","contributorId":78711,"corporation":false,"usgs":true,"family":"Bentall","given":"Ray","email":"","affiliations":[],"preferred":false,"id":143040,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1154,"text":"wsp1779S - 1964 - Evaluation of hydrogeology and hydrogeochemistry of Truckee Meadows area, Washoe County, Nevada","interactions":[],"lastModifiedDate":"2012-02-02T00:05:12","indexId":"wsp1779S","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1779","chapter":"S","title":"Evaluation of hydrogeology and hydrogeochemistry of Truckee Meadows area, Washoe County, Nevada","docAbstract":"Practically all the ground water of economic importance in the Truckee Meadows area, an alluviated intermontane basin in western Nevada is in the valley fill, which consists of unconsolidated and partially consolidated sedimentary deposits. The Mesozoic and Cenozoic consolidated rocks of the mountains bordering the valley contain some water in fractures and other openings, but they have virtually no interstitial permeability. The permeability of the valley fill is extremely variable. The Truckee Formation, which is the oldest deposit of the valley fill, yields very little water to wells. Permeable lenses of sand and gravel in the valley fill that are younger than the Truckee Formation yield moderate to large amounts of water to wells. \r\n\r\nThe estimated average annual recharge to and discharge from the groundwater reservoir is 35,000 acre-feet. About 25,000 acre-feet of the recharge is from the infiltration of irrigation water diverted from the Truckee River. Most of the discharge is by evapotranspiration and by seepage to ditches and streams. \r\n\r\nSome water in the area is unsuitable for many uses because of its poor chemical quality. Water in the Steamboat Springs area is hot and has high concentrations of chloride and dissolved solids. Both water draining areas of bleached rock and ground water downgradient from areas of leached rock have high concentrations of sulfate and dissolved solids. Surface water of low dissolved-solids content mixes with and dilutes some highly mineralized ground water. \r\n\r\nIncreased pumping in discharge areas will help to alleviate waterlogged conditions and will decrease ground-water losses by evapotranspiration. Increased pumping near the Truckee River may induce recharge from the river to the ground-water system.","language":"ENGLISH","publisher":"U.S. Government Printing Office,","doi":"10.3133/wsp1779S","usgsCitation":"Cohen, P.M., and Loeltz, O.J., 1964, Evaluation of hydrogeology and hydrogeochemistry of Truckee Meadows area, Washoe County, Nevada: U.S. Geological Survey Water Supply Paper 1779, v, 63 p. :ill., maps ;23 cm., https://doi.org/10.3133/wsp1779S.","productDescription":"v, 63 p. :ill., maps ;23 cm.","costCenters":[],"links":[{"id":137311,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1779s/report-thumb.jpg"},{"id":25954,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1779s/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25955,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1779s/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25956,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1779s/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25957,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1779s/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4ae4b07f02db6250cd","contributors":{"authors":[{"text":"Cohen, Philip M.","contributorId":67860,"corporation":false,"usgs":true,"family":"Cohen","given":"Philip","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":143269,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Loeltz, Omar J.","contributorId":86312,"corporation":false,"usgs":true,"family":"Loeltz","given":"Omar","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":143270,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1989,"text":"wsp1776 - 1964 - Geology and ground-water resources of Washington, D.C., and vicinity, with a section on chemical quality of the water","interactions":[{"subject":{"id":52182,"text":"ofr6179 - 1961 - Basic data, ground-water resources and geology of Washington, D. C., and vicinity","indexId":"ofr6179","publicationYear":"1961","noYear":false,"title":"Basic data, ground-water resources and geology of Washington, D. C., and vicinity"},"predicate":"SUPERSEDED_BY","object":{"id":1989,"text":"wsp1776 - 1964 - Geology and ground-water resources of Washington, D.C., and vicinity, with a section on chemical quality of the water","indexId":"wsp1776","publicationYear":"1964","noYear":false,"title":"Geology and ground-water resources of Washington, D.C., and vicinity, with a section on chemical quality of the water"},"id":1}],"lastModifiedDate":"2023-11-02T21:05:20.22677","indexId":"wsp1776","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1776","title":"Geology and ground-water resources of Washington, D.C., and vicinity, with a section on chemical quality of the water","docAbstract":"The area of this report includes 436 square miles centered about the District of Columbia.
The area contains parts of two distinctly different physiographic provinces-the Piedmont and the Coastal Plain. The Fall Line, which separates the Piedmont province on the west from the Coastal Plain Province on the east, bisects the area diagonally from northeast to southwest. Northwest of the Fall Line, deeply weathered igneous and metamorphic rocks are exposed ; to the southeast, these rocks are covered by Coastal Plain sediments; the nonconformity between crystalline rock and sediments dips southeast at an average rate of about 125 feet per mile.
The rocks of the Piedmont include: (1) schist, phyllite, and quartzite of the Wissahickon Formation; (2) altered mafic rocks such as greenstone and serpentine; (3) the Laurel Gneiss of Chapman, 1942, and the Sykesville Formation of Jonas, 1928--both probably derived from the Wissahickon ; and (4) later granitic intrusive rocks.
Lying upon this basement of hard rocks east of the Fall Line are the generally unconsolidated sediments of the Coastal Plain, which include gravel, sand, and clay, ranging in age from Cretaceous to Recent. These sediments measure only a few inches at their western extremity but thicken to 1,800 feet at the southeast corner of the mapped area.
Owing to the great diversity in the geology of the two provinces, the waterbearing characteristics of the rocks also vary greatly. In the Piedmont, ground water occurs under unconfined or water-table conditions in openings and fissures in the hard rocks or in the residual weathered blanket that overlies them. In the Coastal Plain, the shallow wells tap unconfined water, but beneath the upper clay layers the water is contained in the sand and gravel under artesian pressure and must be recovered by deep drilled wells.
Wells are of three types--drilled, bored, and dug. Drilled wells furnish a permanent water supply and are the least subject to pollution when properly constructed. Bored or dug wells allow greater storage capacity and are satisfactory for domestic supplies in some locations, but they are polluted easily. If not properly constructed or of sufficient depth, they may fail in dry weather.
Ground-water supplies for domestic use, 5 to 10 gpm (gallons per minute), are obtainable in most places. In the Piedmont, recorded yields in drilled wells range from 0.2 to 212 gpm. In the Coastal Plain, wells yield from 1 to 800 gpm.
The quality of the ground water in the report area is generally satisfactory for domestic, industrial, and irrigation use. High iron content and corrosiveness are troublesome in places. The water is soft to moderately hard--2 to 175 ppm (parts per million). Water in the Piedmont province is. dominantly the calcium and bicarbonate type; in the Coastal Plain most water is of calcium-magnesium bicarbonate type.
In the Piedmont, careful location of wells with respect to the geology (rock type and structure) and to topography usually results in higher yields and may mean the difference between success and failure. In the Coastal Plain, drilled artesian wells are not affected by topography, but the yield obtained depends upon the penetration of a water-bearing sand or gravel bed at sufficient depth.
The early settlers obtained water from the springs and streams, and later from dug wells. After Washington was established as the Capital in 1800, water was obtained from public and privately owned wells. Water was piped from some of the springs to government buildings and to private homes and business houses. In 1863 a diversion dam was completed in the Potomac above Great Falls and a conduit was built into the city to furnish a public water supply. This system with modifications has been in use ever since. A new diversion dam and pumping station at Little Falls was put into service in the summer of 1959.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1776","usgsCitation":"Johnston, P.M., Weaver, D.E., and Siu, L., 1964, Geology and ground-water resources of Washington, D.C., and vicinity, with a section on chemical quality of the water: U.S. Geological Survey Water Supply Paper 1776, Report: vi, 97 p.; 2 Plates: 34.50 x 26.60 inches and 21.00 x 28.60 inches, https://doi.org/10.3133/wsp1776.","productDescription":"Report: vi, 97 p.; 2 Plates: 34.50 x 26.60 inches and 21.00 x 28.60 inches","costCenters":[],"links":[{"id":422360,"rank":5,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_16352.htm","linkFileType":{"id":5,"text":"html"}},{"id":27381,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1776/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27382,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1776/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138471,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1776/report-thumb.jpg"},{"id":27380,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1776/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"District of Columbia","city":"Washington D.C.","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-77.038598,38.791513],[-77.038898,38.800813],[-77.035798,38.814913],[-77.038098,38.815613],[-77.039098,38.821413],[-77.038098,38.828612],[-77.039199,38.832212],[-77.041199,38.833712],[-77.042599,38.833812],[-77.043499,38.833212],[-77.044899,38.834712],[-77.044999,38.838512],[-77.044489,38.839595],[-77.044199,38.840212],[-77.041699,38.840212],[-77.032798,38.841712],[-77.031698,38.850512],[-77.039299,38.864312],[-77.038899,38.865812],[-77.039099,38.868112],[-77.040599,38.871212],[-77.043299,38.874012],[-77.045399,38.875212],[-77.046599,38.874912],[-77.045599,38.873012],[-77.046299,38.871312],[-77.049099,38.870712],[-77.051299,38.873212],[-77.051099,38.875212],[-77.054099,38.879112],[-77.055199,38.880012],[-77.058254,38.880069],[-77.063499,38.888611],[-77.067299,38.899211],[-77.068199,38.899811],[-77.070099,38.900711],[-77.0822,38.901911],[-77.0902,38.904211],[-77.0937,38.905911],[-77.1012,38.911111],[-77.1034,38.912911],[-77.1063,38.919111],[-77.1134,38.925211],[-77.1166,38.928911],[-77.1179,38.932411],[-77.119857,38.93427],[-77.1199,38.934311],[-77.1045,38.94641],[-77.1007,38.94891],[-77.0915,38.95651],[-77.054299,38.98511],[-77.040999,38.99511],[-77.036299,38.99171],[-77.015598,38.97591],[-77.013798,38.97441],[-77.008298,38.97011],[-77.002636,38.965521],[-77.002498,38.96541],[-76.941519,38.918276],[-76.935096,38.913311],[-76.909395,38.892812],[-76.910795,38.891712],[-76.919295,38.885112],[-76.920195,38.884412],[-76.949696,38.861312],[-76.953696,38.858512],[-76.979497,38.837812],[-76.992697,38.828213],[-76.999997,38.821913],[-77.001397,38.821513],[-77.024392,38.80297],[-77.038598,38.791513]]]},\"properties\":{\"name\":\"District of Columbia\",\"nation\":\"USA \"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db685810","contributors":{"authors":[{"text":"Johnston, Paul McKelvey","contributorId":8828,"corporation":false,"usgs":true,"family":"Johnston","given":"Paul","email":"","middleInitial":"McKelvey","affiliations":[],"preferred":false,"id":144482,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Weaver, D. E.","contributorId":51718,"corporation":false,"usgs":true,"family":"Weaver","given":"D.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":887473,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Siu, Leonard","contributorId":331349,"corporation":false,"usgs":false,"family":"Siu","given":"Leonard","email":"","affiliations":[],"preferred":false,"id":887474,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":1122,"text":"wsp1773 - 1964 - Geology and ground-water resources of the Anchorage area, Alaska","interactions":[],"lastModifiedDate":"2012-02-02T00:05:17","indexId":"wsp1773","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1773","title":"Geology and ground-water resources of the Anchorage area, Alaska","docAbstract":"The Anchorage area, at the head of Cook Inlet in south-central Alaska, \r\noccupies 150 square miles of a glaciated lowland and lies between two estuaries and the Chugach Mountains. Two military bases are in the area; \r\nAnchorage is the largest city in Alaska and the chief transportation center \r\nfor this part of the State. \r\nThe bedrock in the Anchorage area is chiefly Tertiary shale in the lowland \r\nand metamorphic rocks of Mesozoic age beneath the adjacent mountain \r\nslopes. Glacial drift which underlies nearly the entire area has an average \r\nthickness of several hundred feet and appears to include at least five sheets \r\nof deposits, two of which are exposed. The drift consists of till, outwash stream and lake deposits (sand and gravel), and estuarine (and lake) deposits \r\n(clay and silt). The stratigraphy and lateral distribution of the deposits are \r\ncomplex, but data at hand s, how that the thickest deposits, including all the \r\nestuarine and lake sediment and most of the stream-deposited sediment, \r\nare beneath the lowland away from the mountain wall, and that the deposits \r\nnear the mountains are till and subordinate outwash sediments. \r\nDeposits of sand and gravel laid down by outwash streams in channels and \r\non outwash plains are the most important aquifers, and the only \r\nones which yield large quantities of ground water from single beds. Thin \r\nlayers of sandy or gravelly material in till are also important aquifers although they yield relatively small quantities of water. Bedded sand and \r\nsilt associated with the estuarine and lake(?) clay commonly becomes unstable during drilling and pumping, and has been successfully developed in \r\nonly a few wells. Unconfined aquifers are extensive, but permeable saturated \r\nmaterial is thin in many places and water supplies available from them are \r\nsmall or undependable in those places. The most important aquifers are confined or artesian. Clay and till form the confining beds: the till is somewhat 'leaky' in many places. Near Anchorage the buried water-bearing \r\nbeds appear to be interconnected and to form a single artesian system. The \r\nwater table and piezometric surface slope from the mountain wall of the \r\nlowland toward the estuaries, and the flow of the ground water is in that \r\ndirection. The aquifers are recharged by the infiltration of precipitation \r\nat the land surface and of surface water through stream beds: near the mountains the artesian aquifers are probably recharged in part by percolation from \r\nthe water-table aquifer, and far from the mountains the water-table aquifer \r\nis probably recharged in part by upward flow from the underlying artesian \r\naquifers. In several valleys and in a few other places, in the lowland, artesian wells flow at the land surface. \r\nThe outwash sand and gravel are moderately to very permeable; most \r\nof the other water-bearing material are much less permeable. The co- efficient of transmissibility for some single beds of sandy gravel is as high \r\nas 60,000 to I00,000 gpd per ft (gallons per day per foot); for the entire \r\nsection of glacial drift at and near Anchorage it is believed to be of the \r\norder of 200,000 gpd per ft. Calculations based on this value for the total \r\nsection and on the slope of the piezometric surface indicate that in the \r\nimmediate vicinity of Anchorage about 5 million gpd flows through each \r\nmile-wide section of the drift (measured in a northeast-southwest direction, perpendicular to the direction of flow), under normal (nonpumping) conditions. Under conditions of continuous heavy pumping the slope of the piezometric surface is steepened, flow is increased, and additional recharge is induced. \r\n\r\nThe highest yield reported from a well in this area is 2.600 gpm (gallons per minute) with 35 feet of drawdown: the highest reported specific capacity is 180 gpm per ft of drawdown, for a well pumped at. 270 gpm. \r\n\r\nOnly a few wells in the area have been developed for high yields. Well screens have been used ","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1773","usgsCitation":"Cederstrom, D.J., Trainer, F.W., and Waller, R.M., 1964, Geology and ground-water resources of the Anchorage area, Alaska: U.S. Geological Survey Water Supply Paper 1773, vi, 108 p. :illus., maps (1 col.) diagrs., tables. ;24 cm., https://doi.org/10.3133/wsp1773.","productDescription":"vi, 108 p. :illus., maps (1 col.) diagrs., tables. ;24 cm.","costCenters":[],"links":[{"id":138014,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1773/report-thumb.jpg"},{"id":25887,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1773/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25888,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1773/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25889,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1773/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25890,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1773/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25891,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1773/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db6855f4","contributors":{"authors":[{"text":"Cederstrom, Dagfin John","contributorId":90287,"corporation":false,"usgs":true,"family":"Cederstrom","given":"Dagfin","email":"","middleInitial":"John","affiliations":[],"preferred":false,"id":143212,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Trainer, Frank W.","contributorId":103655,"corporation":false,"usgs":true,"family":"Trainer","given":"Frank","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":143213,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Waller, Roger Milton","contributorId":22320,"corporation":false,"usgs":true,"family":"Waller","given":"Roger","email":"","middleInitial":"Milton","affiliations":[],"preferred":false,"id":143211,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":1054,"text":"wsp1695 - 1964 - Geology and ground-water resources of southeastern New Hampshire","interactions":[{"subject":{"id":51806,"text":"ofr5516 - 1955 - Preliminary report on the investigation of ground-water resources of the seacoast region of New Hampshire","indexId":"ofr5516","publicationYear":"1955","noYear":false,"title":"Preliminary report on the investigation of ground-water resources of the seacoast region of New Hampshire"},"predicate":"SUPERSEDED_BY","object":{"id":1054,"text":"wsp1695 - 1964 - Geology and ground-water resources of southeastern New Hampshire","indexId":"wsp1695","publicationYear":"1964","noYear":false,"title":"Geology and ground-water resources of southeastern New Hampshire"},"id":1}],"lastModifiedDate":"2012-02-02T00:05:17","indexId":"wsp1695","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1695","title":"Geology and ground-water resources of southeastern New Hampshire","docAbstract":"The continued growth and development of southeastern New Hampshire, an area of about 390 square miles adjacent to the Atlantic Ocean, will depend partly on effectively satisfying the demand for water, which has increased rapidly since World War II. \r\n\r\nThe report identifies and describes the principal geologic units with respect to the occurrence of ground water. These units include bedrock and the various unconsolidated deposits that mantle the bedrock surface discontinuously throughout the area. \r\n\r\nThe bedrock formations, consisting of igneous and metamorphic rocks, chiefly of Paleozoic age, form a single water-bearing unit. Ground water is in joints and fractures. The fractures are small and scattered and therefore impart only a low permeability to the rocks. Wells in the bedrock commonly produce small but reliable supplies of ground water at depths of less than 150 feet. The yields of about 80 wells inventoried for this report ranged from 1? to 100 gpm (gallons per minute) and the median was 912 gpm. Depths ranged from 45 to 600 feet. The unconsolidated deposits consist of glacial drift of Pleistocene age; swamp deposits, alluvium, and beach deposits of Recent age; and eolian deposits of Pleistocene -and Recent age. For this report the glacial drift is divided into till, ice-contact deposits, marine deposits, and outwash and shore deposits. Glacial till forms a discontinuous blanket, commonly less than 15 but in some hills (drumlins) as much as about 200 feet thick. It has a low permeability but, because of its widespread outcrop area, it has been utilized as a source of water for numerous domestic supplies. Because most wells in till are shallow, many fail to meet modern demands during dry summers. \r\n\r\nIce-contact deposits locally form kames, kame terraces, kame plains, and ice-channel fillings throughout the area. They overlie bedrock and till and range in thickness from less than 1 foot to as much as 190 feet. In general, the ice-contact deposits are coarse textured and permeable, but variations in- the physical and hydrologic properties of a single deposit and from deposit to deposit are common. Ice-contact deposits are the source of the larger ground-water supplies in southeastern New Hampshire. \r\n\r\nMarine deposits underlie lowlands and valleys to a distance of about 20 miles inland from the present coastline. They commonly overlie bedrock and till and at places overlie or are interbedded with ice-contact deposits. Marine deposits range in thickness from less than 1 foot to possibly 75 feet. They are fine textured and impermeable; they do not yield water to wells in southeastern New Hampshire but generally act as a barrier to ground-water movement. Outwash and shore deposits form broad sand plains or gently sloping terraces of small extent. At most places the outwash and shore deposits, which range in thickness from less than 1 foot to about 50 feet, overlie marine deposits, but at some places they overlie bedrock, till, or ice-contact deposits. The outwash and shore deposits are fine textured and moderately permeable. They commonly yield enough ground water to meet the needs of farms, homes, and small industries. Alluvium underlies the flood plains and channels of the principal streams and overlies bedrock and older unconsolidated deposits wherever streams cross the older units. The alluvium generally is not tapped by wells. \r\n\r\nBeach deposits occupy areas along the Atlantic Ocean between promontories of bedrock or till. In general beach deposits are permeable and are a source of water supplies for domestic use. Yields of wells are limited, however, by the danger of drawing in salty water. \r\n\r\nRecharge in southeastern New Hampshire is derived principally from precipitation on outcrop areas of ice-contact deposits and outwash and shore deposits during the nongrowing season. Ground water is discharged naturally by springs, by effluent seepage to streams and other bodies of surface water, and by evapotranspiration. It ","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1695","usgsCitation":"Bradley, E., 1964, Geology and ground-water resources of southeastern New Hampshire: U.S. Geological Survey Water Supply Paper 1695, v, 80 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1695.","productDescription":"v, 80 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":25720,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1695/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25721,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1695/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25722,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1695/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25723,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1695/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25724,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1695/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25725,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1695/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25726,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1695/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25727,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1695/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137945,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1695/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db685601","contributors":{"authors":[{"text":"Bradley, Edward","contributorId":67071,"corporation":false,"usgs":true,"family":"Bradley","given":"Edward","email":"","affiliations":[],"preferred":false,"id":143098,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1258,"text":"wsp1618 - 1964 - Use of ground-water reservoirs for storage of surface water in the San Joaquin Valley, California","interactions":[],"lastModifiedDate":"2012-02-02T00:05:13","indexId":"wsp1618","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1618","title":"Use of ground-water reservoirs for storage of surface water in the San Joaquin Valley, California","docAbstract":"The San Joaquin Valley includes roughly the southern two-thirds of the Central Valley of California, extending 250 miles from Stockton on the north to Grapevine at the foot of the Tehachapi Mountains. The valley floor ranges in width from 25 miles near Bakersfield to about 55 miles near Visalia; it has a surface area of about 10,000 square miles. More than one-quarter of all the ground water pumped for irrigation in the United States is used in this highly productive valley. Withdrawal of ground water from storage by heavy pumping not only provides a needed irrigation water supply, but it also lowers the ground-water level and makes storage space available in which to conserve excess water during periods of heavy runoff. A storage capacity estimated to be 93 million acre-feet to a depth of 200 feet is available in this ground-water reservoir. This is about nine times the combined capacity of the existing and proposed surface-water reservoirs in the San Joaquin Valley under the California Water Plan.\r\n\r\nThe landforms of the San Joaquin Valley include dissected uplands, low plains and fans, river flood plains and channels, and overflow lands and lake bottoms. Below the land surface, unconsolidated sediments derived from the surrounding mountain highlands extend downward for hundreds of feet. These unconsolidated deposits, consisting chiefly of alluvial deposits, but including some widespread lacustrine sediments, are the principal source of ground water in the valley. Ground water occurs under confined and unconfined conditions in the San Joaquin Valley. In much of the western, central, and southeastern parts of the valley, three distinct ground-water reservoirs are present. In downward succession these are 1) a body of unconfined and semiconfined fresh water in alluvial deposits of Recent, Pleistocene, and possibly later Pliocene age, overlying the Corcoran clay member of the Tulare formation; 2) a body of fresh water confined beneath the Corcoran clay member, which occurs in alluvial and lacustrine deposits of late Pliocene age or older; and 3) a body of saline connate water contained in marine sediments of middle Pliocene or older age, which underlies the fresh-water body throughout the area. In much of the eastern part of the valley, especially in the areas of the major streams, the Corcoran clay member is not present and ground water occurs as one fresh-water body to considerable depth.\r\n\r\nThe ground-water body is replenished by infiltration of rainfall, by infiltration from streams, canals, and ditches, by underflow entering the valley from tributary stream canyons, and by infiltration of excess irrigation water. In much of the valley, however, the annual rainfall is so low that little penetrates deeply, and soil-moisture deficiency is perennial. Infiltration from stream channels and canals and from irrigated fields are the principal sources of groundwater recharge. The ground-water storage capacity of the San Joaquin Valley has been estimated in an earlier report (Davis and others, 1959) as 93 million acre-feet. This is the quantity of water that would drain by gravity from the valley deposits if the regional water level were lowered from 10 to 200 feet below the land surface. Storage capacity was estimated for only the part of the valley considered to be potentially usable as a ground-water reservoir. In this study, a 200foot depth was selected as a practical valley-wide depth limit for unwatering \r\n\r\nunder full utilization of the ground-water reservoir, even though in localized areas sections in excess of 350 feet in depth have already been dewatered. Some of the factors that locally limit the utilization of the ground-water reservoir are inferior water quality, relatively impermeable surface soils, and relatively impermeable subsurface deposits. On the basis of a detailed analysis of la peg model, the subsurface geology of the San Joaquin Valley was subdivided into predominantly permeable and impermeable zones in the 1","language":"ENGLISH","publisher":"United States Govt. Print. Off.,","doi":"10.3133/wsp1618","usgsCitation":"Davis, G.H., Lofgren, B.E., and Mack, S., 1964, Use of ground-water reservoirs for storage of surface water in the San Joaquin Valley, California: U.S. Geological Survey Water Supply Paper 1618, vii, 125 p. :illus., maps, diagrs., tables. and portfolio ;24 cm., https://doi.org/10.3133/wsp1618.","productDescription":"vii, 125 p. :illus., maps, diagrs., tables. and portfolio ;24 cm.","costCenters":[],"links":[{"id":137412,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1618/report-thumb.jpg"},{"id":26195,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26196,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-02.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26197,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-03.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26198,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-04.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26199,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-05.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26200,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-06.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26201,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-07.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26202,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26203,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-09.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26204,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26205,"rank":410,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26206,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1618/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a17e4b07f02db604592","contributors":{"authors":[{"text":"Davis, G. H.","contributorId":40963,"corporation":false,"usgs":true,"family":"Davis","given":"G.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":143449,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lofgren, B. E.","contributorId":42579,"corporation":false,"usgs":true,"family":"Lofgren","given":"B.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":143450,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Mack, Seymour","contributorId":101247,"corporation":false,"usgs":true,"family":"Mack","given":"Seymour","email":"","affiliations":[],"preferred":false,"id":143451,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":2253,"text":"wsp1777 - 1964 - Geology and ground-water resources of Washington County, Colorado","interactions":[],"lastModifiedDate":"2012-02-02T00:05:19","indexId":"wsp1777","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1777","title":"Geology and ground-water resources of Washington County, Colorado","docAbstract":"Washington County, in northeastern Colorado, has an area of 2,520 square miles. The eastern two-thirds of the county, part of the High Plains physiographic section, is relatively flat and has been moderately altered by the deposition of loess and dune sand, and by stream erosion. The western one-third is a part of the South Platte River basin and has been deeply dissected by tributary streams. The soils and climate of the county are generally suited for agriculture, which is the principal industry. \r\n\r\nThe rocks that crop out in the county influence the availability of ground water. The Pierre Shale, of Late Cretaceous age, underlies the entire area and ranges in thickness from 2,000 to 4,500 feet. This dense shale is a barrier to the downward movement of water and yields little or no water to wells. The Chadron Formation, of Oligocene age, overlies the Pierre Shale in the northern and central parts of the area. The thickness of the formation ranges from a few feet to about 300 feet. Small to moderate quantities of water are available from the scattered sand lenses and from the highly fractured zones of the siltstone. The Ogallala Formation, of Pliocene age, overlies the Chadron Formation and in Washington County forms the High Plains section of the Great Plains province. The thickness of the Ogallala Formation ranges from 0 to about 400 feet, and the yield from wells ranges from a few gallons per hour to about 1,500 gpm. Peorian loess, of Pleistocene age, and dune sand, of Pleistocene to Recent age, mantle a large pan of the county and range in thickness from a few inches to about 120 feet Although the loess and dune sand yield little water to wells, they absorb much of the precipitation and conduct the water to underlying formations. Alluvium, of Pleistocene and Recent age, occupies most of the major stream valleys in thicknesses of a few feet to about 250 feet. The yield of wells tapping the alluvium ranges from a few gallons per minute to about 3,000 gpm, according to the thickness of saturated material. \r\n\r\nDevelopment of ground water for irrigation has been generally restricted to the South Platte, Arikaree, and Beaver valleys. There were 134 irrigation wells, 3 industrial wells, and 10 municipal wells in the county in 1959. The annual ground-water pumpage from Washington County is estimated to be 18,000 acre-ft; about 10,000 acre-ft is from the High Plains ground-water province. Although some ground water enters the county as underflow, most of the recharge to ground-water reservoirs is from precipitation on the land surface. Recharge to the Ogallala Formation in the county is assumed to be approximately equal to the natural discharge from the county by underflow because ground-water withdrawals are from storage, and no other significant amount of natural discharge is apparent. Undertow in the Ogallala was calculated to be 83,000 acre-ft per year and the rate of recharge from precipitation to be about 0.95 inch per year. Neither recharge nor discharge was calculated for that part of the county in the South Platte River basin. \r\n\r\nAll ground water in Washington County has a high proportion of carbonate and is classed as hard to very hard. The sodium-adsorption-ratio for all samples analyzed was below the limit recommended for irrigation water. All the water from the Ogallala Formation and most of the water from the Chadron Formation is suitable for domestic use. Some water from the alluvial deposits overlying the Pierre Shale was exceptionally high in calcium, magnesium, and sodium sulfates. \r\n\r\nGround water has been heavily developed for irrigation in the South Platte valley and in some parts of the Beaver and Arikaree valleys. Some additional areas, however, could be developed in the latter two valleys. Large quantities of ground water in the Ogallala Formation are available for future development. The quantity of water in storage in the High Plains ground-water province in Washington County is about 6.5 million acre-f","language":"ENGLISH","publisher":"U. S. Govt. Print. Off.,","doi":"10.3133/wsp1777","usgsCitation":"McGovern, H.E., 1964, Geology and ground-water resources of Washington County, Colorado: U.S. Geological Survey Water Supply Paper 1777, iv, 46 p. :illus., maps (4 fold. 1 col., in pocket) ;24 cm., https://doi.org/10.3133/wsp1777.","productDescription":"iv, 46 p. :illus., maps (4 fold. 1 col., in pocket) ;24 cm.","costCenters":[],"links":[{"id":110015,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24953.htm","linkFileType":{"id":5,"text":"html"},"description":"24953"},{"id":137835,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1777/report-thumb.jpg"},{"id":28024,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1777/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28025,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1777/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28026,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1777/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28027,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1777/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28028,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1777/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db68580b","contributors":{"authors":[{"text":"McGovern, Harold E.","contributorId":9634,"corporation":false,"usgs":true,"family":"McGovern","given":"Harold","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":144901,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":5714,"text":"pp360 - 1964 - Geology and quicksilver deposits of the New Almaden district, Santa Clara County, California","interactions":[{"subject":{"id":12513,"text":"ofr5027 - 1950 - Some exploration possibilities at the New Almaden quicksilver mine, Santa Clara County, California","indexId":"ofr5027","publicationYear":"1950","noYear":false,"title":"Some exploration possibilities at the New Almaden quicksilver mine, Santa Clara County, California"},"predicate":"SUPERSEDED_BY","object":{"id":5714,"text":"pp360 - 1964 - Geology and quicksilver deposits of the New Almaden district, Santa Clara County, California","indexId":"pp360","publicationYear":"1964","noYear":false,"title":"Geology and quicksilver deposits of the New Almaden district, Santa Clara County, California"},"id":1},{"subject":{"id":46936,"text":"ofr529 - 1952 - Eleven maps of the New Almanden quicksilver mine area, California","indexId":"ofr529","publicationYear":"1952","noYear":false,"title":"Eleven maps of the New Almanden quicksilver mine area, California"},"predicate":"SUPERSEDED_BY","object":{"id":5714,"text":"pp360 - 1964 - Geology and quicksilver deposits of the New Almaden district, Santa Clara County, California","indexId":"pp360","publicationYear":"1964","noYear":false,"title":"Geology and quicksilver deposits of the New Almaden district, Santa Clara County, California"},"id":2},{"subject":{"id":50893,"text":"ofr4919 - 1949 - The New Almaden quicksilver mine, Santa Clara County, California","indexId":"ofr4919","publicationYear":"1949","noYear":false,"title":"The New Almaden quicksilver mine, Santa Clara County, California"},"predicate":"SUPERSEDED_BY","object":{"id":5714,"text":"pp360 - 1964 - Geology and quicksilver deposits of the New Almaden district, Santa Clara County, California","indexId":"pp360","publicationYear":"1964","noYear":false,"title":"Geology and quicksilver deposits of the New Almaden district, Santa Clara County, California"},"id":3},{"subject":{"id":55325,"text":"ofr4474 - 1941 - The Harry area, New Almaden mine, Santa Clara County, California","indexId":"ofr4474","publicationYear":"1941","noYear":false,"title":"The Harry area, New Almaden mine, Santa Clara County, California"},"predicate":"SUPERSEDED_BY","object":{"id":5714,"text":"pp360 - 1964 - Geology and quicksilver deposits of the New Almaden district, Santa Clara County, California","indexId":"pp360","publicationYear":"1964","noYear":false,"title":"Geology and quicksilver deposits of the New Almaden district, Santa Clara County, California"},"id":4}],"lastModifiedDate":"2013-06-24T14:10:22","indexId":"pp360","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","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":"360","title":"Geology and quicksilver deposits of the New Almaden district, Santa Clara County, California","docAbstract":"The New Almaden district, situated a few miles south of San Jose in Santa Clara County, Calif., has yielded nearly 40 percent of the quicksilver produced in the United States. The area mapped as the district for this report includes about 80 square miles, extending south from the flat Santa Clara Valley across the moderately low foothills containing the mines to the more rugged crest of the California Coast Ranges.","language":"ENGLISH","publisher":"United States Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/pp360","usgsCitation":"Bailey, E.H., and Everhart, D.L., 1964, Geology and quicksilver deposits of the New Almaden district, Santa Clara County, California: U.S. Geological Survey Professional Paper 360, viii, 206 p., https://doi.org/10.3133/pp360.","productDescription":"viii, 206 p.","costCenters":[],"links":[{"id":104440,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4358.htm","linkFileType":{"id":5,"text":"html"},"description":"4358"},{"id":139893,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0360/report-thumb.jpg"},{"id":268949,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0360/report.pdf"}],"country":"United States","state":"California","county":"Santa Clara County","otherGeospatial":"New Almaden District","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -124,36 ], [ -124,39.5 ], [ -120,39.5 ], [ -120,36 ], [ -124,36 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad6e4b07f02db6842a3","contributors":{"authors":[{"text":"Bailey, Edgar Herbert","contributorId":85179,"corporation":false,"usgs":true,"family":"Bailey","given":"Edgar","email":"","middleInitial":"Herbert","affiliations":[],"preferred":false,"id":151475,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Everhart, Donald Lough","contributorId":40108,"corporation":false,"usgs":true,"family":"Everhart","given":"Donald","email":"","middleInitial":"Lough","affiliations":[],"preferred":false,"id":151474,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ]}