Eclogites are divisible into three groups based on mode of occurrence: Group A, inclusions in kimberlites, basalts, or layers in ultramafic rocks; Group B, bands or lenses within migmatite gneissic terrains; Group C, bands or lenses within alpine-type metamorphic rocks. The compositions range from olivine basalt for Group A to tholeiitic basalts for Group C. New analytical data on six eclogites from glaucophane schist terrains in California and New Caledonia now permit comparisons among the three eclogite types. The pyrope content of the garnets is distinctive for each group as follows: Group A, greater than 55 per cent py; Group B, 30–55 per cent py; Group C, less than 30 percent py. Pyroxenes coexisting with these garnets also reflect a compositional change related to their occurrence. The jadeite content progressively increases from Group A through Group B, whereas the diopside content decreases. A comparison of eclogites from different geologic occurrences but with similar bulk compositions demonstrates variation in Ca-Mg partition between coexisting garnet and pyroxene. The Ca/Mg ratio increases in garnet and decreases in pyroxene from Group A through Group B eclogites. This obvious difference in the Ca-Mg partition between coexisting garnet-pyroxene in eclogites of the same bulk composition indicates a broad range of pressure-temperature conditions obtained during crystallization. Experimental synthesis of eclogite-like material at high pressures and temperatures demonstrates that some eclogites may form in the earth's mantle, but naturally occurring Group C eclogites have coexisting garnet-pyroxene with distinct Ca/Mg ratios when compared to Group A or B eclogites of similar bulk composition. This difference in the Ca/Mg ratio must reflect the pressure-temperature conditions characterizing the glaucophane schist facies.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1965)76[483:EAETDA]2.0.CO;2","usgsCitation":"Coleman, R.G., Lee, D., Beatty, L.B., and Brannock, W.W., 1965, Eclogites and eclogites: Their differences and similarities: GSA Bulletin, v. 76, no. 5, p. 483-508, https://doi.org/10.1130/0016-7606(1965)76[483:EAETDA]2.0.CO;2.","productDescription":"26 p.","startPage":"483","endPage":"508","costCenters":[],"links":[{"id":387678,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"76","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Coleman, R. G.","contributorId":75170,"corporation":false,"usgs":true,"family":"Coleman","given":"R.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":820546,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lee, Donald E.","contributorId":11615,"corporation":false,"usgs":true,"family":"Lee","given":"Donald E.","affiliations":[],"preferred":false,"id":820547,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Beatty, L. B.","contributorId":261744,"corporation":false,"usgs":false,"family":"Beatty","given":"L.","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":820548,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Brannock, W. W.","contributorId":74504,"corporation":false,"usgs":true,"family":"Brannock","given":"W.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":820549,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70222060,"text":"70222060 - 1965 - Investigation of initial Sr87/Sr86 ratios in the Sierra Nevada Plutonic Province","interactions":[],"lastModifiedDate":"2021-07-16T13:00:54.153796","indexId":"70222060","displayToPublicDate":"1965-07-16T07:58:20","publicationYear":"1965","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1723,"text":"GSA Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Investigation of initial Sr87/Sr86 ratios in the Sierra Nevada Plutonic Province","docAbstract":"One to three whole-rock samples from each of more than a dozen discrete plutonic intrusions in the east-central Sierra Nevada batholith have been analyzed for Sr87/Sr86 and Rb/Sr ratios to obtain information on initial Sr87 abundances.
The initial Sr87/Sr86 ratios in the rock magmas forming this province appear to have been in the range 0.7073 ± .0010 in the majority of cases. This range is definitely higher than that found for modern alkali-type and tholeiite-type basalt magmas of oceanic regions, which commonly range between 0.703 and 0.705. However, it is much lower than the average Sr87/Sr86 ratios found in Precambrian sialic regions which range from 0.71 to 0.73. It seems clear therefore that the Sierra Nevada magmas were not derived solely either from the typical source regions of oceanic basalt or from the melting of ancient crustal sial. It is possible that these magmas represent a mixture of oceanic basalt and crustal sial, as would be the case of anatexis in a geosyncline containing much volcanic material of fairly recent origin and some terrigenous sialic detritus. They may instead be of mantle derivation with admixtures of crustal material assimilated during their rise.
The whole-rock Rb-Sr age results derivec from the study indicate that the Lamarck and Mount Givens Granodiorites and the alaskite of Evolution Basin and porphyritic biotite granite of Dinkey Lakes form a younger group of intrusive rocks of 90 ± 10 m.y. Although the sampling was not designed for isochron age studies, it appears that most of the remaining rock units are considerably older.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1965)76[165:IOISSR]2.0.CO;2","usgsCitation":"Hurley, P., Bateman, P.C., Fairbairn, H., and Pinson, W., 1965, Investigation of initial Sr87/Sr86 ratios in the Sierra Nevada Plutonic Province: GSA Bulletin, v. 76, no. 2, p. 165-174, https://doi.org/10.1130/0016-7606(1965)76[165:IOISSR]2.0.CO;2.","productDescription":"10 p.","startPage":"165","endPage":"174","costCenters":[],"links":[{"id":387213,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"76","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Hurley, P.M.","contributorId":258271,"corporation":false,"usgs":false,"family":"Hurley","given":"P.M.","email":"","affiliations":[],"preferred":false,"id":819351,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bateman, P. C.","contributorId":27851,"corporation":false,"usgs":true,"family":"Bateman","given":"P.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":819352,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Fairbairn, H.W.","contributorId":88609,"corporation":false,"usgs":true,"family":"Fairbairn","given":"H.W.","email":"","affiliations":[],"preferred":false,"id":819353,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Pinson, W.H.","contributorId":237001,"corporation":false,"usgs":false,"family":"Pinson","given":"W.H.","email":"","affiliations":[{"id":12444,"text":"Massachusetts Institute of Technology","active":true,"usgs":false}],"preferred":false,"id":819354,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":1001418,"text":"1001418 - 1965 - An automatic camera device for measuring waterfowl use","interactions":[],"lastModifiedDate":"2025-02-07T16:35:25.540112","indexId":"1001418","displayToPublicDate":"1965-07-02T00:00:00","publicationYear":"1965","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2508,"text":"Journal of Wildlife Management","active":true,"publicationSubtype":{"id":10}},"title":"An automatic camera device for measuring waterfowl use","docAbstract":"A Yashica Sequelle camera was modified and equipped with a timing device so that it would take pictures automatically at 15-minute intervals. Several of these cameras were used to photograph randomly selected quadrats located in different marsh habitats. The number of birds photographed in the different areas was used as an index of waterfowl use.","language":"English","publisher":"Wiley","doi":"10.2307/3798066","usgsCitation":"Cowardin, L.M., and Ashe, J., 1965, An automatic camera device for measuring waterfowl use: Journal of Wildlife Management, v. 29, no. 3, p. 636-640, https://doi.org/10.2307/3798066.","productDescription":"5 p.","startPage":"636","endPage":"640","costCenters":[{"id":480,"text":"Northern Prairie Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":133814,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"29","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad9e4b07f02db684cee","contributors":{"authors":[{"text":"Cowardin, Lewis M.","contributorId":34574,"corporation":false,"usgs":true,"family":"Cowardin","given":"Lewis","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":311008,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Ashe, J.E.","contributorId":6417,"corporation":false,"usgs":true,"family":"Ashe","given":"J.E.","email":"","affiliations":[],"preferred":false,"id":311007,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70221197,"text":"70221197 - 1965 - Natural controls involved in shallow aquifer contamination","interactions":[],"lastModifiedDate":"2021-06-04T21:03:19.909849","indexId":"70221197","displayToPublicDate":"1965-07-01T16:00:52","publicationYear":"1965","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3825,"text":"Groundwater","active":true,"publicationSubtype":{"id":10}},"title":"Natural controls involved in shallow aquifer contamination","docAbstract":"Shallow aquifers, commonly the most important sources of ground water, are also those most susceptible to contamination. The mode of entry of contaminants to shallow aquifers is (1) directly, via wells or secondary openings in consolidated rocks, (2) percolation through the zone of aeration, (3) induced infiltration through the zone of saturation, and (4) interaquifer leakage or flow through open holes. Natural removal or degradation of contaminants is by filtration, dispersion, sorption, ion exchange, oxidation, and various biochemical processes. These phenomena are controlled by the physical environment, structure; mineralogy, and hydraulic characteristics of the earth materials contacted by the liquid wastes. When liquid wastes enter an aquifer directly, there is little or no natural treatment by filtration, sorption, or oxidation. Purification is only by those processes that operate within the aquifer under anaerobic conditions. Contaminants from natural sources that enter aquifers under saturated‐flow conditions are degraded primarily by dilution. The natural processes effective in reducing contamination from surface‐water sources depend on the hydraulic regimen involved, which vary with individual cases. Liquid wastes percolating through the zone of aeration are those most likely to be purified by natural environment processes. Natural processes, however, do not effectively remove or degrade all contaminants, especially some of the many highly stable compounds that have gained widespread use in recent years, such as synthetic detergents. Comprehensive interdisciplinary research into the ability of various earth materials to remove many types of contaminants under varying hydrologic conditions is needed.
","language":"English","publisher":"Wiley Blackwell","doi":"10.1111/j.1745-6584.1965.tb01219.x","usgsCitation":"Deutsch, M., 1965, Natural controls involved in shallow aquifer contamination: Groundwater, v. 3, no. 3, p. 37-40, https://doi.org/10.1111/j.1745-6584.1965.tb01219.x.","productDescription":"4 p.","startPage":"37","endPage":"40","costCenters":[],"links":[{"id":386242,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"3","issue":"3","noUsgsAuthors":false,"publicationDate":"2006-07-06","publicationStatus":"PW","contributors":{"authors":[{"text":"Deutsch, M.","contributorId":19707,"corporation":false,"usgs":true,"family":"Deutsch","given":"M.","email":"","affiliations":[],"preferred":false,"id":817035,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70207282,"text":"70207282 - 1965 - Relation of carbon 14 concentrations to saline water contamination of coastal aquifers","interactions":[],"lastModifiedDate":"2019-12-17T07:00:43","indexId":"70207282","displayToPublicDate":"1965-03-31T16:24:40","publicationYear":"1965","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3721,"text":"Water Resources Management","onlineIssn":"1573-1650","printIssn":"0920-4741","active":true,"publicationSubtype":{"id":10}},"title":"Relation of carbon 14 concentrations to saline water contamination of coastal aquifers","docAbstract":"Naturally occurring stable or radioactive isotopes may be used in some places to identify the origin of saline water that contaminates some coastal aquifers. In a recent study to determine the origin of saline water in the Ocala Limestone aquifer near Brunswick, Georgia, the following sources were analyzed for C14 and deuterium concentrations: potable water from the Ocala Limestone, contaminated water from the Ocala Limestone, saune water from the underlying Claiborne Group, and nearby ocean water. The chloride concentration of the groundwater ranges from about 25 ppm in the potable water to more than 2000 ppm in the deeper part of the Claiborne Group. From an interpretation of piezometric maps and other hydrologic data, previous investigators had concluded that the source of the contaminating water was the Claiborne Group and not the nearby ocean. The essentially uniform range of low values of −965 to −987‰ of the modern standard (National Bureau Standard C14 oxalic acid) for the C14 activity of the groundwater samples (regardless of the degree of contamination) is in agreement with this conclusion. If recent ocean water, which had a C14 value of +285‰, were the source of contamination, the contaminated water would have had a C14 activity higher than the activity of the fresh water. Deuterium analyses are not inconsistent with the interpretation that water from the Claiborne Group, rather than recent ocean water, is the source of the contaminating water. The concurrence of the hydrologic and the isotopic data in this area where the hydrology is well known suggests that isotopic analysis may be used to identify the origin of water in different portions of a hydrologic environment.
","language":"English","publisher":"American Geophysical Union","doi":"10.1029/WR001i001p00109","issn":"00431397","usgsCitation":"Hanshaw, B., Back, W., Rubin, M., and Wait, R.L., 1965, Relation of carbon 14 concentrations to saline water contamination of coastal aquifers: Water Resources Management, v. 1, no. 1, p. 109-114, https://doi.org/10.1029/WR001i001p00109.","productDescription":"6 p. ","startPage":"109","endPage":"114","costCenters":[],"links":[{"id":370289,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Georgia","county":"Glynn County","city":"Brunswick","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -81.73828125,\n 30.92107637538488\n ],\n [\n -81.221923828125,\n 30.92107637538488\n ],\n [\n -81.221923828125,\n 31.39115752282472\n ],\n [\n -81.73828125,\n 31.39115752282472\n ],\n [\n -81.73828125,\n 30.92107637538488\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"1","issue":"1","noUsgsAuthors":false,"publicationDate":"2010-07-09","publicationStatus":"PW","contributors":{"authors":[{"text":"Hanshaw, B.B.","contributorId":25928,"corporation":false,"usgs":true,"family":"Hanshaw","given":"B.B.","email":"","affiliations":[],"preferred":false,"id":777532,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Back, W.","contributorId":33839,"corporation":false,"usgs":true,"family":"Back","given":"W.","email":"","affiliations":[],"preferred":false,"id":777533,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Rubin, Meyer","contributorId":107283,"corporation":false,"usgs":true,"family":"Rubin","given":"Meyer","email":"","affiliations":[],"preferred":false,"id":777690,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Wait, Robert L.","contributorId":12839,"corporation":false,"usgs":true,"family":"Wait","given":"Robert","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":777691,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70199507,"text":"70199507 - 1965 - Mathematical models of catchment behavior","interactions":[],"lastModifiedDate":"2025-02-27T18:37:54.196925","indexId":"70199507","displayToPublicDate":"1965-01-01T16:01:10","publicationYear":"1965","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2550,"text":"Journal of the Hydraulics Division","active":true,"publicationSubtype":{"id":10}},"title":"Mathematical models of catchment behavior","docAbstract":"After an examination of trends in the modeling of hydrologic systems, a review of some recent studies is given. The authors' preliminary studies on the feasibility and efficiency of the automatic evaluation of catchment model parameters by use of a digital computer are described and some results presented.
","language":"English","publisher":"American Society of Civil Engineers","doi":"10.1061/JYCEAJ.0001271","usgsCitation":"Dawdy, D.R., and O’Donnell, T., 1965, Mathematical models of catchment behavior: Journal of the Hydraulics Division, v. 91, no. 4, p. 123-137, https://doi.org/10.1061/JYCEAJ.0001271.","productDescription":"15 p.","startPage":"123","endPage":"137","costCenters":[{"id":154,"text":"California Water Science Center","active":true,"usgs":true}],"links":[{"id":357514,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"91","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Dawdy, David R.","contributorId":75125,"corporation":false,"usgs":true,"family":"Dawdy","given":"David","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":745630,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"O’Donnell, Terence","contributorId":208019,"corporation":false,"usgs":false,"family":"O’Donnell","given":"Terence","email":"","affiliations":[],"preferred":false,"id":745631,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70221186,"text":"70221186 - 1965 - Ages of minerals from metamorphic and igneous rocks near Iron Mountain, Michigan","interactions":[],"lastModifiedDate":"2021-06-04T18:07:07.223979","indexId":"70221186","displayToPublicDate":"1965-01-01T13:01:22","publicationYear":"1965","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2420,"text":"Journal of Petrology","active":true,"publicationSubtype":{"id":10}},"title":"Ages of minerals from metamorphic and igneous rocks near Iron Mountain, Michigan","docAbstract":"More than 100 independent isotopic ages have been determined for minerals from an area in northern Michigan about 35 miles square. Granites, pegmatites, and metamorphosed sedimentary and volcanic rocks have yielded Rb-Sr ages for feldspar, muscovite, and biotite, K-Ar ages for hornblende, muscovite, biotite, and feldspar, and U-Pb and Th-Pb ages for zircon. It was anticipated that we would learn from the measurements both the intrusive and metamorphic history of the area and would be able to place limits on the age of the Precambrian sediments in this area. The conclusions may be summarized as follows: (1) Granites and pegmatites with approximate ages of 2,700 and 1,900 m.y. have been found. (2) The major mineral-forming metamorphic event occurred between 1,800 and 2,000 m.y. ago. (3) The Precambrian sedimentary rocks called Animikie are older than 1, 900 m.y. and younger than 2,700 m.y. (4) Biotite Rb-Sr and K-Ar ages and muscovite K-Ar ages were strongly modified by the equivalent of a rise in temperature approximately 1,350 m.y. ago, although no mineral-forming event in this interval has been observed. (5) The K-Ar system was further affected by a thermal rise at about 1,100 m.y. This later event is probably recorded geologically by a few diabase dikes.The resistance to post-formation thermal events shown by the various minerals and decay systems tested may be classified as follows (lowest to highest): feldspar K-Ar, biotite K-Ar, muscovite K-Ar, biotite Rb-Sr, zircon U238-Pb206, zircon Th-Pb208, zircon U235-Pb207, muscovite Rb-Sr, feldspar Rb-Sr. The few hornblende K-Ar measurements indicate that the resistance of this system is about comparable to that of muscovite and feldspar Rb-Sr. The Pb207-Pb206 age derived from the two U-Pb ages is somewhat more resistant to change than the feldspar Rb-Sr ages.
","language":"English","publisher":"Oxford University Press","doi":"10.1093/petrology/6.3.445","usgsCitation":"Aldrich, L.T., Davis, G., and James, H.L., 1965, Ages of minerals from metamorphic and igneous rocks near Iron Mountain, Michigan: Journal of Petrology, v. 6, no. 3, p. 445-472, https://doi.org/10.1093/petrology/6.3.445.","productDescription":"28 p.","startPage":"445","endPage":"472","costCenters":[],"links":[{"id":386231,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Michigan","city":"Iron Mountain","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -88.13232421875,\n 45.75219336063106\n ],\n [\n -87.7587890625,\n 45.75219336063106\n ],\n [\n -87.7587890625,\n 45.9511496866914\n ],\n [\n -88.13232421875,\n 45.9511496866914\n ],\n [\n -88.13232421875,\n 45.75219336063106\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"6","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Aldrich, Lyman Thomas","contributorId":108105,"corporation":false,"usgs":true,"family":"Aldrich","given":"Lyman","email":"","middleInitial":"Thomas","affiliations":[],"preferred":false,"id":817016,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Davis, G.L.","contributorId":259301,"corporation":false,"usgs":false,"family":"Davis","given":"G.L.","email":"","affiliations":[],"preferred":false,"id":817017,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"James, H. L.","contributorId":96732,"corporation":false,"usgs":true,"family":"James","given":"H.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":817018,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70048263,"text":"70048263 - 1965 - Directional hydraulic behavior of a fractured-shale aquifer in New Jersey","interactions":[],"lastModifiedDate":"2021-02-17T22:57:35.415612","indexId":"70048263","displayToPublicDate":"1965-01-01T09:15:00","publicationYear":"1965","noYear":false,"publicationType":{"id":24,"text":"Conference Paper"},"publicationSubtype":{"id":19,"text":"Conference Paper"},"title":"Directional hydraulic behavior of a fractured-shale aquifer in New Jersey","docAbstract":"The principal source of ground water throughout a large part of central and northeastern New Jersey is the aquifer in the Brunswick Shale -- the youngest unity of the Newark Group of Triassic Age. Large-diameter public-supply and industrial wells tapping the Brunswick Shale commonly yield several hundred gallons per minute each. Virtually all ground water in this aquifer occurs in interconnecting fractures; the formation has practically no effective primary porosity. Numerous pumping tests have shown that the aquifer exhibits directional, rather than isotropic, hydraulic behavior. Water levels in wells alined along the strike of the formation show greater magnitude of interference than those in wells alined in transverse directions. Drawdown data evaluated by standard time-drawdown methods indicate computed coefficient of transmissibility in all cases is least in the direction of strike. Because of the distribution of observation wells available for the tests, distance-drawdown methods of evaluation could be used in only one instance -- for just one direction; the computed coefficient compared favorably with that calculated from the time-drawdown method. Computed values of transmissibility may be unreliable owing to the departure of the aquifer from the ideal model. It is even possible that the direction of minimum computed transmissiblity is actually indicative of the alinement of fractures with the greatest permeability. However, the relation of the directional behavior to the structure of the formation has practical significance when locating the new wells near existing wells. Well interference can be greatly minimized, generally, by alining wells perpendicular to the strike.","largerWorkTitle":"Proceedings of the international symposium on hydrology of fractured rocks","conferenceTitle":"International Symposium on Hydrology of Fractured Rocks","conferenceDate":"October 1965","conferenceLocation":"Dubrovnik, Croatia","language":"English","publisher":"International Association of Scientific Hydrology","usgsCitation":"Vecchioli, J., 1965, Directional hydraulic behavior of a fractured-shale aquifer in New Jersey, in Proceedings of the international symposium on hydrology of fractured rocks, Dubrovnik, Croatia, October 1965, 9 p.","productDescription":"9 p.","numberOfPages":"9","costCenters":[],"links":[{"id":277842,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"New Jersey","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -75.2082,40.2451 ], [ -75.2082,41.3574 ], [ -73.9931,41.3574 ], [ -73.9931,40.2451 ], [ -75.2082,40.2451 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"523c1ce6e4b024b60d4072a3","contributors":{"authors":[{"text":"Vecchioli, John","contributorId":36113,"corporation":false,"usgs":true,"family":"Vecchioli","given":"John","email":"","affiliations":[],"preferred":false,"id":484210,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70010658,"text":"70010658 - 1965 - Natural recharge and localization of fresh ground water in Kuwait","interactions":[],"lastModifiedDate":"2020-11-24T00:17:46.668516","indexId":"70010658","displayToPublicDate":"1965-01-01T00:00:00","publicationYear":"1965","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2342,"text":"Journal of Hydrology","active":true,"publicationSubtype":{"id":10}},"title":"Natural recharge and localization of fresh ground water in Kuwait","docAbstract":"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":70010782,"text":"70010782 - 1965 - Solution of rocks and refractory minerals by acids at high temperatures and pressures. Determination of silica after decomposition with hydrofluoric acid","interactions":[],"lastModifiedDate":"2020-11-24T00:11:38.14032","indexId":"70010782","displayToPublicDate":"1965-01-01T00:00:00","publicationYear":"1965","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":760,"text":"Analytica Chimica Acta","active":true,"publicationSubtype":{"id":10}},"title":"Solution of rocks and refractory minerals by acids at high temperatures and pressures. Determination of silica after decomposition with hydrofluoric acid","docAbstract":"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.
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.
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":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":"2026-05-08T13:41:14.407157","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":267546,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/misc/tl/0022/"},{"id":267547,"rank":1,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/misc/tl/0022/tl0022.pdf"},{"id":504098,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_98164.htm","linkFileType":{"id":5,"text":"html"}},{"id":267548,"rank":3,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"country":"United States","state":"California, Nevada","otherGeospatial":"Lake Mead, Mono Lake","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -119.1732667158729,\n 38.15329669327568\n ],\n [\n -114.04842885902873,\n 38.15329669327568\n ],\n [\n -114.04842885902873,\n 35.91035825172828\n ],\n [\n -119.1732667158729,\n 35.91035825172828\n ],\n [\n -119.1732667158729,\n 38.15329669327568\n ]\n ]\n ]\n }\n }\n ]\n}","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":12572,"text":"ofr6410 - 1964 - Lower Permian stratigraphy of east-central Nevada and adjacent Utah","interactions":[],"lastModifiedDate":"2026-01-20T18:51:18.957146","indexId":"ofr6410","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":"64-10","title":"Lower Permian stratigraphy of east-central Nevada and adjacent Utah","docAbstract":"The Permian section near Ely, Nevada, consists of, in ascending order: Riepe Spring Limestone, a bluff-forming limestone with abundant corals, and Reipetown Sandstone, a buff to red very coarse-grained siltstone with minor carbonates, both formations of Steele (1960); Arcturus Formation, divisible into a Lower Member composed of alternating medium-bedded limestone and buff siltstone, and an Upper Member composed of alternating thin-bedded limestone and buff to red siltstone and gypsum; and Kaibab Limestone, a massive bioclastic limestone. The Wolfcamp-Leonard boundary occurs within the Arcturus Formation. West of Ely the Riepe Spring Limestone and Reipetown Sandstone thin and change into thin-bedded cherty limestone. These beds, plus the basal part of the Arcturus Formation, form the Carbon Ridge Formation at Dry Mountain at Eureka. At Dry Mountain, minor clastic chert occurs in the Arcturus Formation, and beyond to the west clastic chert replaces most of the limestone to form the conglomeratic Garden Valley Formation. The cherty limestone at the base of the Garden Valley is apparently equivalent to the upper part of the Carbon Ridge Formation at Carbon Ridge. Eastward in Utah the Riepe Spring Limestone is recognizable in the Confusion Range, but is almost unrecognizable in the Needle Range. The dolomite content in the Reipetown Sandstone usually increases to 25 percent of the formation in the Confusion and Needle ranges. The Arcturus Formation thins and undergoes moderate lithologic changes. It is equivalent to the rocks above a horizon 300 feet below Bed A of the Arcturus Formation as mapped in the Confusion Range by Hose and Repenning (1959, 1963).
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr6410","usgsCitation":"Barosh, P.J., 1964, Lower Permian stratigraphy of east-central Nevada and adjacent Utah: U.S. Geological Survey Open-File Report 64-10, Report: 144 p.; 10 Plates: 79.84 x 42.75 inches ; 3 Tables, https://doi.org/10.3133/ofr6410.","productDescription":"Report: 144 p.; 10 Plates: 79.84 x 42.75 inches ; 3 Tables","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":311529,"rank":15,"type":{"id":27,"text":"Table"},"url":"https://pubs.usgs.gov/of/1964/0010/table-03.pdf","text":"Table 3","linkFileType":{"id":1,"text":"pdf"}},{"id":311527,"rank":13,"type":{"id":27,"text":"Table"},"url":"https://pubs.usgs.gov/of/1964/0010/table-01.pdf","text":"Table 1","linkFileType":{"id":1,"text":"pdf"}},{"id":311526,"rank":12,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0010/plate-12.pdf","text":"Plate 12","linkFileType":{"id":1,"text":"pdf"}},{"id":311525,"rank":11,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0010/plate-11.pdf","text":"Plate 11","linkFileType":{"id":1,"text":"pdf"}},{"id":311524,"rank":10,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0010/plate-10.pdf","text":"Plate 10","linkFileType":{"id":1,"text":"pdf"}},{"id":498785,"rank":16,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_119130.htm","linkFileType":{"id":5,"text":"html"}},{"id":311523,"rank":9,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0010/plate-09.pdf","text":"Plate 9","linkFileType":{"id":1,"text":"pdf"}},{"id":311522,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0010/plate-08.pdf","text":"Plate 8","linkFileType":{"id":1,"text":"pdf"}},{"id":311528,"rank":14,"type":{"id":27,"text":"Table"},"url":"https://pubs.usgs.gov/of/1964/0010/table-02.pdf","text":"Table 2","linkFileType":{"id":1,"text":"pdf"}},{"id":311521,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0010/plate-07.pdf","text":"Plate 7","linkFileType":{"id":1,"text":"pdf"}},{"id":311520,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0010/plate-06.pdf","text":"Plate 6","linkFileType":{"id":1,"text":"pdf"}},{"id":311519,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0010/plate-05.pdf","text":"Plate 5","linkFileType":{"id":1,"text":"pdf"}},{"id":311518,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0010/plate-04.pdf","text":"Plate 4","linkFileType":{"id":1,"text":"pdf"}},{"id":146246,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1964/0010/report-thumb.jpg"},{"id":40963,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1964/0010/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":311517,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0010/plate-03.pdf","text":"Plate 3","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Nevada, Utah","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -116.2,\n 39.9\n ],\n [\n -116.2,\n 38.7\n ],\n [\n -113.5,\n 38.7\n ],\n [\n -113.5,\n 39.9\n ],\n [\n -116.2,\n 39.9\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a7fe4b07f02db648961","contributors":{"authors":[{"text":"Barosh, Patrick James","contributorId":42184,"corporation":false,"usgs":true,"family":"Barosh","given":"Patrick","email":"","middleInitial":"James","affiliations":[],"preferred":false,"id":166359,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"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":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":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":975,"text":"wsp1653 - 1964 - Ground-water resources of the lower Rio Grande Valley area, Texas","interactions":[],"lastModifiedDate":"2016-08-22T11:21:21","indexId":"wsp1653","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":"1653","title":"Ground-water resources of the lower Rio Grande Valley area, Texas","docAbstract":"The report contains information about the occurrence, quality, and use of ground water in the Lower Rio Grande Valley area which consists of Cameron, Hidalgo, Starr, and Willacy Counties in southern Texas.
\nThe principal use of water in the area is for irrigation. The principal irrigated crops are cotton, winter vegetables, and citrus fruits. In southeastern Starr County, southern Hidalgo County, and western Cameron County, the main source of water is the Rio Grande. The greatest development of ground water in this area was after 1948 when ground water was needed to supplement water from the river.
\nThe Lower Rio Grande Valley area has four major ground-water reservoirs. Because of the uncertainty in mapping the stratigraphic units and because some of the ground-water reservoirs are composed of parts of two or more formations, three of the ground-water reservoirs have been given names in this report. The major ground-water reservoirs are: the Oakville sandstone, an important source of water for industrial use in northeastern Stair County; the Linn-Faysville ground-water reservoir, which supplies irrigation water in the Linn-Faysville area in central Hidalgo County; and the Rio Grande ground-water reservoir and the Mercedes-Sebastian shallow ground-water reservoir, both of which supply considerable irrigation water in southeastern Starr, southern Hidalgo, western Cameron, and southwestern Willacy Counties.
\nThe quality of water differs considerably from place to place in the Lower Rio Grande Valley area. In most of the area, water is available that can be used for domestic or public supply, but it generally is slightly saline. In most of the area, the ground water is unsuitable for irrigation .particularly if used exclusively. Water of the best quality in the area is from the Rio Grande groundwater reservoir near the Rio Grande at depths of less than 75 feet in southeastern Stair County, between 50 and 250 feet in southern Hidalgo County, and between 100 and 300 feet in western Cameron County. At progressively greater distances from the Rio Grande, the ground water at these depths tends to be more mineralized. Also at some places at depths greater than those indicated, the water tends to be more mineralized. In the Linn-Faysville area the ground water from the Linn-Faysville ground-water reservoir is moderately mineralized and ranges from fair to unsuitable for irrigation.
\nIn western Cameron County, water levels in some wells tapping the Rio Grande ground-water reservoir declined about 10 feet from 1954 to 1957. In 1959 the water levels stood higher than in 1954. The water levels in most wells tapping the Linn-Faysville ground-water reservoir declined 10 feet or more from 1948 to 1958. In some wells the decline was more than 15 feet.
\nThe available information indicates that in some localities the Rio Grande ground-water reservoir may be nearly filled to capacity, and waterlogging will occur during periods of above-normal precipitation. During protracted periods of below-normal precipitation, the available water in the ground-water reservoir may be depleted.
\nFurther studies should be made in the area to correct important deficiencies in available information. A continuing program is recommended because information such as fluctuations in water levels and the amount and distribution of pumping can be obtained only on a current basis.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1653","usgsCitation":"Baker, R.C., and Dale, O., 1964, Ground-water resources of the lower Rio Grande Valley area, Texas: U.S. Geological Survey Water Supply Paper 1653, Report: v, 56 p.; 5 Plates, https://doi.org/10.3133/wsp1653.","productDescription":"Report: v, 56 p.; 5 Plates","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":25537,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1653/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137059,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1653/report-thumb.jpg"},{"id":25532,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1653/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25533,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1653/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25534,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1653/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25535,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1653/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25536,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1653/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e48cde4b07f02db54492c","contributors":{"authors":[{"text":"Baker, R. C.","contributorId":79084,"corporation":false,"usgs":true,"family":"Baker","given":"R.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":142951,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dale, O.C.","contributorId":28583,"corporation":false,"usgs":true,"family":"Dale","given":"O.C.","email":"","affiliations":[],"preferred":false,"id":142950,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":972,"text":"wsp1694 - 1964 - Geology and ground-water conditions in the Wilmington-Reading area, Massachusetts","interactions":[],"lastModifiedDate":"2012-02-02T00:05:16","indexId":"wsp1694","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":"1694","title":"Geology and ground-water conditions in the Wilmington-Reading area, Massachusetts","docAbstract":"The Wilmington-Reading area, as defined for this report, contains the headwaters of the Ipswich River in northeastern Massachusetts. Since World War II the growth of communities in this area and the change in character of some of them from rural to suburban have created new water problems and intensified old ones. The purpose of this report on ground-water conditions is to provide information that will aid in understanding and resolving some of these problems. \r\n\r\nThe regional climate, which is humid and temperate, assures the area an ample natural supply of water. At the current stage of water-resources development a large surplus of water drains from the area by way of the Ipswich River during late autumn, winter, and spring each year and is unavailable for use during summer and early autumn, when during some years there is a general water deficiency. \r\n\r\nGround water occurs both in bedrock and in the overlying deposits of glacial drift. The bedrock is a source of small but generally reliable supplies of water throughout the area. Glacial till also is a source of small supplies of water, but wells in till often fail to meet modern demands. Stratified glacial drift, including ice-contact deposits and outwash, yields small to large supplies of water. \r\n\r\nStratified glacial drift forms the principal ground-water reservoir. It partly fills a system of preglacial valleys corresponding roughly to the valleys of the present Ipswich River system and is more than 100 feet thick at places. The ice-contact deposits generally are more permeable than the outwash deposits. Ground water occurs basically under water-table conditions. \r\n\r\nRecharge in the Wilmington-Reading area is derived principally from precipitation on outcrop areas of ice-contact deposits and outwash during late autumn, winter. and spring. It is estimated that the net annual recharge averages about 10 inches and generally ranges from 5 inches during unusually dry years to 15 inches during unusually wet years. Ground water withdrawn largely by municipal wells supplies the towns of North Reading, Reading, and Wilmington. In 1957 the average daily withdrawal from these wells was about 2.5 million gallons, of which about half was used outside the Ipswich River drainage basin. \r\n\r\nThe chemical quality of the ground water is generally satisfactory except for local excessive concentrations of iron. \r\n\r\nThe storage capacity of the ground-water reservoir and recharge in the Wilmington-Reading area are large enough to sustain a total withdrawal of ground water at several times the current rate, but the use of the reservoir probably will be limited by the extent to which wells of moderate or large capacity can be dispersed. This will depend upon the distribution of areas of thick permeable materials. Conditions in the Martins Brook-Skug River drainage basin seem generally favorable for increased development of water supplies. In the rest of the Wilmington-Reading area the chances of finding substantial bodies of thick permeable materials probably are small, but further exploration is desirable. \r\n\r\nMeasures proposed to drain swampland by deepening and straightening the Ipswich River and its tributaries will have some effect upon the ground-water conditions. Probably the most obvious effect will be a lowering of water levels in wells near improved reaches of channel. Also important will b the effect of changes in low streamflow conditions on wells that induce infiltration from streams and the effect on well yields of an improved hydraulic connection between streams and the ground-water body. \r\n\r\nThe Reading 100-acre well field, which derives part of its supply by inducing recharge from the Ipswich River, would be affected by the drainage measures. During a dry summer, such as that of 1957, the flow of the Ipswich is fully diverted by pumping at this well field, and drawdowns at some of the wells approach half the saturated thickness of the aquifer there. If the drainage measures are","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1694","usgsCitation":"Baker, J.A., Healy, H., and Hackett, O.M., 1964, Geology and ground-water conditions in the Wilmington-Reading area, Massachusetts: U.S. Geological Survey Water Supply Paper 1694, v, 80 p. :ill., maps (1 col.) ;24 cm., https://doi.org/10.3133/wsp1694.","productDescription":"v, 80 p. :ill., maps (1 col.) ;24 cm.","costCenters":[],"links":[{"id":137045,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1694/report-thumb.jpg"},{"id":25518,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1694/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25519,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1694/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25520,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1694/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25521,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1694/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25522,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1694/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25523,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1694/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adbe4b07f02db6860c9","contributors":{"authors":[{"text":"Baker, John Augustus","contributorId":48159,"corporation":false,"usgs":true,"family":"Baker","given":"John","email":"","middleInitial":"Augustus","affiliations":[],"preferred":false,"id":142946,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Healy, H.G.","contributorId":72776,"corporation":false,"usgs":true,"family":"Healy","given":"H.G.","email":"","affiliations":[],"preferred":false,"id":142947,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hackett, O. M.","contributorId":38527,"corporation":false,"usgs":true,"family":"Hackett","given":"O.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":142945,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ]}