{"pageNumber":"401","pageRowStart":"10000","pageSize":"25","recordCount":10951,"records":[{"id":2040,"text":"wsp1798F - 1969 - Sedimentation in upper Stony Creek basin, eastern flank of the Coast Ranges of northern California","interactions":[],"lastModifiedDate":"2021-12-23T19:46:43.776282","indexId":"wsp1798F","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","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":"1798","chapter":"F","title":"Sedimentation in upper Stony Creek basin, eastern flank of the Coast Ranges of northern California","docAbstract":"

No abstract available.

","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Sedimentation in small drainage basins","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/wsp1798F","usgsCitation":"Knott, J.M., and Dunnam, C., 1969, Sedimentation in upper Stony Creek basin, eastern flank of the Coast Ranges of northern California: U.S. Geological Survey Water Supply Paper 1798, iv, 35 p., https://doi.org/10.3133/wsp1798F.","productDescription":"iv, 35 p.","costCenters":[],"links":[{"id":388910,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24989.htm"},{"id":137707,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1798f/report-thumb.jpg"},{"id":27530,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1798f/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"California","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -122.3330,\n 39.7170\n ],\n [\n -122.8330,\n 39.7170\n ],\n [\n -122.8330,\n 39.2500\n ],\n [\n -122.3330,\n 39.2500\n ],\n [\n -122.3330,\n 39.7170\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9ee4b07f02db66055b","contributors":{"authors":[{"text":"Knott, J. M.","contributorId":77909,"corporation":false,"usgs":true,"family":"Knott","given":"J.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":144573,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dunnam, C.A.","contributorId":56200,"corporation":false,"usgs":true,"family":"Dunnam","given":"C.A.","email":"","affiliations":[],"preferred":false,"id":144572,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":34608,"text":"b1291 - 1969 - The Geologic Story of the Uinta Mountains","interactions":[],"lastModifiedDate":"2017-02-09T12:59:04","indexId":"b1291","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1291","title":"The Geologic Story of the Uinta Mountains","docAbstract":"The opening of the West after the Civil War greatly stimulated early geologic exploration west of the 100th Meridian. One of the areas first studied, the Uinta Mountains region, gained wide attention as a result of the explorations of three Territorial Surveys, one headed by John Wesley Powell, one by Clarence King, and one by Ferdinand V. Hayden. Completion of the Union Pacific Railroad across southern Wyoming 100 years ago, in 1869, materially assisted geologic exploration, and the railheads at Green River and Rock Springs greatly simplified the outfitting of expeditions into the mountains.\r\n\r\nThe overlap of the Powell, King, and Hayden surveys in the Uinta Mountains led to efforts that were less concerted than competitive and not without acrimony. Many parts of the area were seen by all three parties at almost the same time. Duplication was inevitable, of course, but all three surveys contributed vast quantities of new knowledge to the storehouse of geology, and many now-basic concepts arose from their observations.\r\n\r\nPowell's area of interest extended mainly southward from the Uinta Mountains to the Grand Canyon, including the boundless plateaus and canyons of southern Utah and northern Arizona. King's survey extended eastward from the High Sierra in California to Cheyenne, Wyoming, and encompassed a swath of country more than 100 miles wide. Hayden's explorations covered an immense region of mountains and basins from Yellowstone Park in Wyoming southeast throughout most of Colorado.\r\n\r\nPowell first entered the Uinta Mountains in the fall of 1868, having traveled north around the east end of the range from the White River country to Green River, Wyoming, then south over a circuitous route to Flaming Gorge and Browns Park, and finally back to the White River, where he spent the winter. In 1869, after reexamining much of the area visited the previous season, Powell embarked on his famous 'first boat trip' down the Green and Colorado Rivers. This trip was more exploratory than scientific; his second, more scientific trip was made 2 years later. Powell revisited the Uinta Mountains in 1874 and 1875 to complete the studies begun 6 years earlier. His classic 'Report on the Geology of the Eastern Portion of the Uinta Mountains and a Region of Country Adjacent Thereto' was published in 1876.\r\n\r\nKing's survey?officially 'The United States Geological Exploration of the Fortieth Parallel'?is better known simply as the '40th Parallel Survey.' King began working eastward from California in 1867. The Uinta Mountains region, however, was mapped by S. F. Emmons, under the supervision of King, in the summers of 1869 and 1871. Emmons' work was monumental, and although he emphasized in his letter of transmittal to King the exploratory nature of the work?as the formal title of the report indicates?his maps, descriptions, and conclusions reflect a comprehensive understanding of the country and its rocks. The 40th Parallel report contains the best, most complete early descriptions of the Uinta Mountains. It, indeed, is a treasurechest of information and a landmark contribution to the emerging science of geology.\r\n\r\nHayden visited the Uinta Mountains in 1870, descending the valley of Henrys Fork to Flaming Gorge in the fall after having earlier examined the higher part of the range to the west. Most of Hayden's observations were cursory, and he repeatedly expressed regret at having insufficient time for more detailed studies. In reference to the area between Clay Basin and Browns Park, he remarked (Hayden, 1871, p. 67) somewhat dryly that 'the geology of this portion of the Uinta range is very complicated and interesting. To have solved the problem to my entire satisfaction would have required a week or two.' Eighty-odd years later I spent several months there?looking at the same rocks.\r\n\r\nPowell was perhaps more creative?more intuitive?than either King or Hayden, and his breadth of interest in the fields of geology, physiography, ethnology, an","language":"ENGLISH","publisher":"U.S. Geological Survey","doi":"10.3133/b1291","usgsCitation":"Hansen, W.R., 1969, The Geologic Story of the Uinta Mountains: U.S. Geological Survey Bulletin 1291, 144 p, https://doi.org/10.3133/b1291.","productDescription":"144 p","costCenters":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":92845,"rank":299,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1291/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":163008,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1291/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c61d","contributors":{"authors":[{"text":"Hansen, Wallace R.","contributorId":90273,"corporation":false,"usgs":true,"family":"Hansen","given":"Wallace","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":213255,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":16403,"text":"ofr69309 - 1969 - An analysis of gravity data in Area 12, Nevada Test Site","interactions":[],"lastModifiedDate":"2025-07-28T20:08:52.024588","indexId":"ofr69309","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","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":"69-309","title":"An analysis of gravity data in Area 12, Nevada Test Site","docAbstract":"The gravity data available from Healey and Miller (1963a) were augmented by new observations along three profiles through two new drill holes in Area 12; UEI2t #1 and UEI2p #1. The data were interpreted to allow evaluation of the geologic structure prior to the planning and excavation of two proposed tunnel complexes, Ul2t and Ul2p.\r\n\r\nDensity values for each of six rock units were determined to allow a two-dimensional analysis of the gravity data along the above-mentioned profiles. The surficial rocks of Quaternary and Tertiary age and the Tertiary volcanic rocks have a weighted average density of 1.86 gm/cc. The density of the caprock at Rainier and Aqueduct Mesas ranges from 2.17 gm/cc at UEI2p #1 to 2.27 gm/cc at UEI2t #1. The Gold Meadows stock and the associated Precambrian quartzite have an arithmetic average density of 2.60 gm/cc for all samples measured. The middle Paleozoic dolomite in Area 12 has an arithmetic average density of 2.75 gm/cc. The clastic rocks of Paleozoic age have an arithmetic average density of 2.60 gm/cc. \r\n\r\nInterpretation of the residual gravity data indicates a maximum thickness of about 2,800 feet for all Tertiary volcanic rocks. A normal fault striking N. 30 ? E. disrupts the pre-Cenozoic surface at UEI2p #1 and 0.4 mile east of UEI2t #1. The throw within rock of Paleozoic age is about 400-500 feet. Another normal fault that strikes about N. 20 ? E. is located about 1.5 miles east of UEI2p #1. The throw of this fault is at least 1,100 feet in rocks of pre-Cenozoic age.\r\n\r\nElevation contours representing the pre-Cenozoic surface in Area 12 show a maximum relief of about 2,000 feet.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr69309","usgsCitation":"Wahl, R.R., 1969, An analysis of gravity data in Area 12, Nevada Test Site: U.S. Geological Survey Open-File Report 69-309, Report: iii, 23 p.; 3 Plates: 42.76 x 29.41 inches or smaller, https://doi.org/10.3133/ofr69309.","productDescription":"Report: iii, 23 p.; 3 Plates: 42.76 x 29.41 inches or smaller","costCenters":[],"links":[{"id":493049,"rank":6,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_8426.htm","linkFileType":{"id":5,"text":"html"}},{"id":45377,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1969/0309/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":45376,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0309/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":45375,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0309/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":45374,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0309/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":147470,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1969/0309/report-thumb.jpg"}],"country":"United States","state":"Nevada","otherGeospatial":"Area 12, Nevada Test Site","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -116.25,\n 37.265\n ],\n [\n -116.25,\n 37.164\n ],\n [\n -116.083,\n 37.164\n ],\n [\n -116.083,\n 37.265\n ],\n [\n -116.25,\n 37.265\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adbe4b07f02db685a2a","contributors":{"authors":[{"text":"Wahl, R. R.","contributorId":27462,"corporation":false,"usgs":true,"family":"Wahl","given":"R.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":172787,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":38817,"text":"pp543I - 1969 - Tectonics of the March 27, 1964, Alaska earthquake","interactions":[{"subject":{"id":38817,"text":"pp543I - 1969 - Tectonics of the March 27, 1964, Alaska earthquake","indexId":"pp543I","publicationYear":"1969","noYear":false,"chapter":"I","title":"Tectonics of the March 27, 1964, Alaska earthquake"},"predicate":"IS_PART_OF","object":{"id":70048225,"text":"pp543 - 1966 - The Alaska earthquake, March 27, 1964: regional effects","indexId":"pp543","publicationYear":"1966","noYear":false,"title":"The Alaska earthquake, March 27, 1964: regional effects"},"id":1}],"isPartOf":{"id":70048225,"text":"pp543 - 1966 - The Alaska earthquake, March 27, 1964: regional effects","indexId":"pp543","publicationYear":"1966","noYear":false,"title":"The Alaska earthquake, March 27, 1964: regional effects"},"lastModifiedDate":"2022-06-28T18:18:07.763935","indexId":"pp543I","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"543","chapter":"I","title":"Tectonics of the March 27, 1964, Alaska earthquake","docAbstract":"The March 27, 1964, earthquake was accomp anied by crustal deformation-including warping, horizontal distortion, and faulting-over probably more than 110,000 square miles of land and sea bottom in south-central Alaska. Regional uplift and subsidence occurred mainly in two nearly parallel elongate zones, together about 600 miles long and as much as 250 miles wide, that lie along the continental margin. From the earthquake epicenter in northern Prince William Sound, the deformation extends eastward 190 miles almost to long 142° and southwestward slightly more than 400 miles to about long 155°. It extends across the two zones from the chain of active volcanoes in the Aleutian Range and Wrangell Mountains probably to the Aleutian Trench axis.\n\nUplift that averages 6 feet over broad areas occurred mainly along the coast of the Gulf of Alaska, on the adjacent Continental Shelf, and probably on the continental slope. This uplift attained a measured maximum on land of 38 feet in a northwest-trending narrow belt less than 10 miles wide that is exposed on Montague Island in southwestern Prince William Sound. Two earthquake faults exposed on Montague Island are subsidiary northwest-dipping reverse faults along which the northwest blocks were relatively displaced a maximum of 26 feet, and both blocks were upthrown relative to sea level. From Montague Island, the faults and related belt of maximum uplift may extend southwestward on the Continental Shelf to the vicinity of the Kodiak group of islands. To the north and northwest of the zone of uplift, subsidence forms a broad asymmetrical downwarp centered over the Kodiak-Kenai-Chugach Mountains that averages 2½ feet and attains a measured maximum of 7½ feet along the southwest coast of the Kenai Peninsula. Maximum indicated uplift in the Alaska and Aleutian Ranges to the north of the zone of subsidence was l½ feet. Retriangulation over roughly 25,000 square miles of the deformed region in and around Prince William Sound shows that vertical movements there were accompanied by horizontal distortion, involving systematic shifts of about 64 feet in a relative seaward direction. Comparable horizontal movements are presumed to have affected those parts of the major zones of uplift and subsidence for which retriangulation data are unavailable.\n\nRegional vertical deformation generated a train of destructive long-period seismic sea waves in the Gulf of Alaska as well as unique atmospheric and ionospheric disturbances that were recorded at points far distant from Alaska. Warping resulted in permanent tilt of larger lake basins and temporary reductions in discharge of some major rivers. Uplift and subsidence relative to sea level caused profound modifications in shoreline morphology with attendant catastrophic effects on the nearshore biota and costly damage to coasta1 installations. Systematic horizontal movements of the land relative to bodies of confined or semiconfined water may have caused unexplained short-period waves—some of which were highly destructive—observed during or immediately after the earthquake at certain coastal localities and in Kenai Lake. Porosity increases, probably related to horizontal displacements in the zone of subsidence, were reflected in lowered well-water levels and in losses of surface water.\n\nThe primary fault, or zone of faults, along which the earthquake occurred is not exposed at the surface on land. Focal-mechanism studies, when considered in conjunction with the pattern of deformation and seismicity, suggest that it was a complex thrust fault (megathrust) dipping at a gentle angle beneath the continental margin from the vicinity of the Aleutian Trench. Movement on the megathrust was accompanied by subsidiary reverse faulting, and perhaps wrench faulting, within the upper plate. Aftershock distribution suggests movement on a segment of the megathrust, some 550–600 miles long and 110–180 miles wide, that underlies most of the major zone of uplift and the seaward part of the major zone of subsidence.\n\nAccording to the postulated model, the observed and inferred tectonic displacements that accompanied the earthquake resulted primarily from (1) relative seaward displacement and uplift of the seaward part of the block by movement along the dipping megathrust and subsidiary faults that break through the upper plate to the surface, and (2) simultaneous elastic horizontal extension and vertical attenuation (subsidence) of the crustal slab behind the upper plate. Slight uplift inland from the major zones of deformation presumably was related to elastic strain changes resulting from the overthrusting; however, the data are insufficient to permit conclusions regarding its cause.\n\nThe belt of seismic activity and major zones of tectonic deformation associated with the 1964 earthquake, to a large extent, lie between and parallel to the Aleutian Volcanic Arc and the Aleutian Trench, and are probably genetically related to the arc. Geologic data indicate that the earthquake-related tectonic movements were but the most recent pulse in an episode of deformation that probably began in late Pleistocene time and has continued intermittently to the present. Evidence for progressive coastal submergence in the deformed region for several centuries preceding the earthquake, in combin1ation with transverse horizontal shortening indicated by the retriangulation data, suggests pre-earthquake strain directed at a gentle angle downward beneath the arc. The duration of strain accumulation in the epicentral region, as interpreted from the time interval during which the coastal submergence occurred, probably is 930–1,360 years.","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"The Alaska earthquake, March 27, 1964: Regional effects (Professional Paper 543)","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/pp543I","usgsCitation":"Plafker, G., 1969, Tectonics of the March 27, 1964, Alaska earthquake: U.S. Geological Survey Professional Paper 543, Report: viii, 74 p.; 2 Plates: 27.08 x 21.87 inches and 16.09 x 20.66 inches, https://doi.org/10.3133/pp543I.","productDescription":"Report: viii, 74 p.; 2 Plates: 27.08 x 21.87 inches and 16.09 x 20.66 inches","numberOfPages":"88","costCenters":[{"id":380,"text":"Menlo ParkCalif. Office-Earthquake Science Center","active":false,"usgs":true}],"links":[{"id":402614,"rank":6,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4593.htm","linkFileType":{"id":5,"text":"html"}},{"id":277849,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pp/0543i/index.html"},{"id":65741,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0543i/pp543i_text.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":264156,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0543i/pp543i_plate2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":264155,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0543i/pp543i_plate1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":122539,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0543i/report-thumb.jpg"}],"country":"United States","state":"Alaska","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -141.2,51.8 ], [ -141.2,64.0 ], [ -174.1,64.0 ], [ -174.1,51.8 ], [ -141.2,51.8 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db6858cd","contributors":{"authors":[{"text":"Plafker, George","contributorId":3920,"corporation":false,"usgs":false,"family":"Plafker","given":"George","email":"","affiliations":[],"preferred":false,"id":220493,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":68445,"text":"ha311 - 1969 - Hydrology of a part of the Big Sioux drainage basin, eastern South Dakota","interactions":[],"lastModifiedDate":"2022-02-03T21:34:22.779976","indexId":"ha311","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":318,"text":"Hydrologic Atlas","code":"HA","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"311","title":"Hydrology of a part of the Big Sioux drainage basin, eastern South Dakota","docAbstract":"

In 1960 the U.S. Geological Survey, in cooperation with the South Dakota State Water Resources Commission and the South Dakota State Geological Survey, started a program for the hydrogeologic investigation of glacial drift in selected drainage basins in eastern South Dakota. This program was designed to delineate water-bearing deposits of glacial-outwash sand and gravel, and to determine their water-yielding characteristics, particularly with regard to irrigation and industrial use. Investigations of this type will aid in planning the use and conservation of ground water for future agricultural and industrial growth in South Dakota.

\n

This report describes the part of the Big Sioux River drainage basin from Sioux Falls north to a U.S. Geological Survey gaging station 9M miles southeast of Brookings (see fig. 1).

\n

The drainage area, about 675 square miles, is in the southwestern part of the Coteau des Prairies section of the Central Lowland physiographic province, as defined by Flint (1955, p. 5). It includes the Big Sioux River valley in Moody and north-central Minnehaha Counties, and the uplands that drain into the valley, from Brookings, Lake, Moody, and Minnehaha Counties, South Dakota, and Pipestone and Lincoln Counties, Minnesota.

\n

This report is based on data from field and laboratory studies and from published and unpublished records of State and Federal agencies. The investigations included: (1) Delineating area of water-bearing glacial outwash deposits; (2) inventorying wells to locate areas of greatest ground-water potential; (3) examining samples from auger holes to define thickness, extent, and character of water-bearing deposits; (4) determining the altitudes of selected test holes and wells for use in preparing cross sections and watertable maps; (5) collecting and analyzing water samples to determine the chemical character of water; and (6) testing aquifers to determine the hydrologic properties of the water-bearing deposits.

\n

Data consisting of logs of wells and test holes, waterlevel measurements, chemical analyses of water, stream-runoff measurements, and determinations of the hydrologic properties of aquifers are contained in a separate report by Ellis and Adolphson (1968).

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ha311","usgsCitation":"Ellis, M.J., Adolphson, D.G., and West, R.E., 1969, Hydrology of a part of the Big Sioux drainage basin, eastern South Dakota: U.S. Geological Survey Hydrologic Atlas 311, Report: 5 p.; 1 Plate: 41.0 x 51.0 inches, https://doi.org/10.3133/ha311.","productDescription":"Report: 5 p.; 1 Plate: 41.0 x 51.0 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":562,"text":"South Dakota Water Science Center","active":true,"usgs":true},{"id":34685,"text":"Dakota Water Science Center","active":true,"usgs":true}],"links":[{"id":89976,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/ha/311/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":89977,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/ha/311/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":395411,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_15684.htm"},{"id":186197,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/ha/311/report-thumb.jpg"}],"scale":"125000","country":"United States","state":"South Dakota","otherGeospatial":"Big Sioux drainage basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -97.37182617187499,\n 43.50872101129684\n ],\n [\n -97.37182617187499,\n 44.3002644115815\n ],\n [\n -95.833740234375,\n 44.3002644115815\n ],\n [\n -95.833740234375,\n 43.50872101129684\n ],\n [\n -97.37182617187499,\n 43.50872101129684\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a17e4b07f02db604747","contributors":{"authors":[{"text":"Ellis, Michael J.","contributorId":40360,"corporation":false,"usgs":true,"family":"Ellis","given":"Michael","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":278232,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Adolphson, Donald G.","contributorId":53872,"corporation":false,"usgs":true,"family":"Adolphson","given":"Donald","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":278233,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"West, Robert E.","contributorId":10101,"corporation":false,"usgs":true,"family":"West","given":"Robert","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":278231,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":63797,"text":"gp653 - 1969 - Aeromagnetic map of the Thompson quadrangle and part of the East Killingly quadrangle, Connecticut and Rhode Island","interactions":[],"lastModifiedDate":"2025-06-20T16:53:08.829303","indexId":"gp653","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":317,"text":"Geophysical Investigations Map","code":"GP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"653","title":"Aeromagnetic map of the Thompson quadrangle and part of the East Killingly quadrangle, Connecticut and Rhode Island","docAbstract":"

No abstract available.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/gp653","usgsCitation":"Water Resources Division, U.S. Geological Survey, 1969, Aeromagnetic map of the Thompson quadrangle and part of the East Killingly quadrangle, Connecticut and Rhode Island: U.S. Geological Survey Geophysical Investigations Map 653, 1 Plate: 21.84 x 33.91 inches, https://doi.org/10.3133/gp653.","productDescription":"1 Plate: 21.84 x 33.91 inches","costCenters":[],"links":[{"id":491041,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_6020.htm","linkFileType":{"id":5,"text":"html"}},{"id":250011,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/gp/0653/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":253488,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/gp/0653/report-thumb.jpg"},{"id":250010,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/gp/0653/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"24000","country":"United States","state":"Connecticut, Rhode Island","otherGeospatial":"Thompson quadrangle and part of the East Killingly quadrangle","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -71.875,\n 42\n ],\n [\n -71.875,\n 41.875\n ],\n [\n -71.75,\n 41.875\n ],\n [\n -71.75,\n 42\n ],\n [\n -71.875,\n 42\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae7e4b07f02db68c3e1","contributors":{"authors":[{"text":"Water Resources Division, U.S. Geological Survey","contributorId":128075,"corporation":true,"usgs":false,"organization":"Water Resources Division, U.S. Geological Survey","id":533266,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":63954,"text":"gp651 - 1969 - Aeromagnetic map of the Eastford quadrangle and part of the Hampton quadrangle, Tolland and Windham Counties, Connecticut","interactions":[],"lastModifiedDate":"2025-06-20T16:43:17.070372","indexId":"gp651","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":317,"text":"Geophysical Investigations Map","code":"GP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"651","title":"Aeromagnetic map of the Eastford quadrangle and part of the Hampton quadrangle, Tolland and Windham Counties, Connecticut","docAbstract":"

No abstract available.

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The Buffalo River watershed includes two general physiographic areas – a glacial lake plain and an glacial moraine.

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The lake plain, which was formed by Glacial lake Agassiz more than 9,000 years ago, is extremely flat – sloping only a few feet per mile westward near the Red River of the North. The moraine is largely an area of gently rolling hills, but in the eastern “tail” of the watershed the relief locally is over two hundred feet.

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The watershed has an area of about 1,690 square miles and includes most of Clay County and parts of Wilkin, Otter Tail, Becker, and Norman Counties. The population of the area is about 45,500 – 31,000 urban and 14,500 rural.

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The economy is largely agricultural. Sugar beet and wheat farming are dominant in the areas of clay and silt; potato farming is confined mainly to the sandy areas. Dairying and stock raising is important in the morainal area. The larger industries are located in Moorhead and consist of sugar beet, potato, and dairy product processing.

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Water-based recreation consists mostly of fishing in the larger lakes in the morainal area, and water-fowl hunting in the area of prairie potholes – the western part of the morainal area.

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This is the fourth report on the extent and frequency of inundation prepared for the Delaware River Basin Commission. The first of these reports covered floods on the Delaware River in the vicinity of Easton, Pennsylvania and Phillipsburg, New Jersey. The second covered a reach of the Schuylkill River from Conshohocken to Philadelphia. The third was for the Delaware River in the vicinity of Belvidere, New Jersey. The first and third reports were written by George M. Farlekas of the Trenton district, and the second was written by Arthur T. Alter of the Harrisburg district. Specific information as to the areal extent and contents of these studies can be obtained from the Delaware River Basin Commission, P.O. Box 360, Trenton, New Jersey.

This flood inundation study is part of an investigative program financed through a cooperative agreement between the U.S. Geological Survey and the Delaware River Basin Commission. The report was prepared under the direction of Norman H. Beamer, District, Chief, U.S. Geological Survey, Harrisburg, Pennsylvania.

The streamflow data for Perkiomen Creek at Graterford were collected by the Pennsylvania Department of Forests and Waters from 1914 to 1931. Since 1931 the data have been collected under a cooperative agreement between the U.S. Geological Survey and the Department of Forests and Waters. Data on high-water marks and areas inundated in past periods of flooding have been obtained from many local residents of Montgomery County. The Reading Company cooperated by allowing survey crews to work on their right-of-way. The author is grateful to Mr. John W. Buchanan for surveys, Mr. Lewis C. Shaw for illustrations and to Mrs. Joan C. King for typing.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr6929","collaboration":"Prepared in cooperation with Delaware River Basin Commission","usgsCitation":"Busch, W.F., 1969, Extent and frequency of inundation on the Perkiomen Creek flood plain from Green Lane Reservoir to the Schuylkill River (near Oaks, Pennsylvania): U.S. Geological Survey Open-File Report 69-29, vii, 27 p., https://doi.org/10.3133/ofr6929.","productDescription":"vii, 27 p.","costCenters":[],"links":[{"id":343692,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1969/0029/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":181532,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1969/0029/report-thumb.jpg"}],"country":"United States","state":"Pennsylvania","otherGeospatial":"Green Lane Reservoir, Perkiomen Creek flood plain, Schuylkill River","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -75.48912048339844,\n 40.42917828232078\n ],\n [\n -75.50148010253906,\n 40.43440488077008\n ],\n [\n -75.53443908691405,\n 40.42708752919884\n ],\n [\n -75.55572509765625,\n 40.41611000901211\n ],\n [\n -75.56465148925781,\n 40.391011807973285\n ],\n [\n -75.55641174316406,\n 40.360672330668166\n ],\n [\n -75.52963256835938,\n 40.334506645085234\n ],\n [\n -75.50628662109375,\n 40.256996734279234\n ],\n [\n -75.49942016601562,\n 40.20300156544074\n ],\n [\n -75.49736022949219,\n 40.142139942215415\n ],\n [\n -75.4877471923828,\n 40.1095880747414\n ],\n [\n -75.46440124511717,\n 40.09803366543276\n ],\n [\n -75.43212890625,\n 40.108537754986166\n ],\n [\n -75.42045593261719,\n 40.150537893668925\n ],\n [\n -75.41015624999999,\n 40.18359473454382\n ],\n [\n -75.41976928710938,\n 40.22554847206815\n ],\n [\n -75.42388916015625,\n 40.280049508234804\n ],\n [\n -75.42800903320312,\n 40.329795743702064\n ],\n [\n -75.45204162597656,\n 40.37584377696013\n ],\n [\n -75.46989440917969,\n 40.406176423413704\n ],\n [\n -75.48912048339844,\n 40.42917828232078\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a06e4b07f02db5f8ab3","contributors":{"authors":[{"text":"Busch, William F.","contributorId":96959,"corporation":false,"usgs":true,"family":"Busch","given":"William","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":254424,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":63955,"text":"gp661 - 1969 - Aeromagnetic map of the Easthampton quadrangle, Hampshire and Hampden Counties, Massachusetts","interactions":[],"lastModifiedDate":"2025-06-20T18:42:43.920707","indexId":"gp661","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":317,"text":"Geophysical Investigations Map","code":"GP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"661","title":"Aeromagnetic map of the Easthampton quadrangle, Hampshire and Hampden Counties, Massachusetts","docAbstract":"

No abstract available.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/gp661","usgsCitation":"Water Resources Division, U.S. Geological Survey, 1969, Aeromagnetic map of the Easthampton quadrangle, Hampshire and Hampden Counties, Massachusetts: U.S. Geological Survey Geophysical Investigations Map 661, 1 Plate: 19.17 x 32.33 inches, https://doi.org/10.3133/gp661.","productDescription":"1 Plate: 19.17 x 32.33 inches","costCenters":[],"links":[{"id":491052,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_6028.htm","linkFileType":{"id":5,"text":"html"}},{"id":250315,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/gp/0661/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":253805,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/gp/0661/report-thumb.jpg"},{"id":250314,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/gp/0661/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"24000","country":"United States","state":"Massachusetts","county":"Hampshire County, Hampden County","otherGeospatial":"Easthampton quadrangle","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -72.625,\n 42.25\n ],\n [\n -72.625,\n 42.375\n ],\n [\n -72.75,\n 42.375\n ],\n [\n -72.75,\n 42.25\n ],\n [\n -72.625,\n 42.25\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afce4b07f02db696789","contributors":{"authors":[{"text":"Water Resources Division, U.S. Geological Survey","contributorId":128075,"corporation":true,"usgs":false,"organization":"Water Resources Division, U.S. Geological Survey","id":533424,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":47220,"text":"ofr6924 - 1969 - Geologic map of the Park City East Quadrangle, Summit and Wasatch Counties, Utah","interactions":[{"subject":{"id":47220,"text":"ofr6924 - 1969 - Geologic map of the Park City East Quadrangle, Summit and Wasatch Counties, Utah","indexId":"ofr6924","publicationYear":"1969","noYear":false,"title":"Geologic map of the Park City East Quadrangle, Summit and Wasatch Counties, Utah"},"predicate":"SUPERSEDED_BY","object":{"id":63302,"text":"gq852 - 1971 - Geologic map of the Park City East quadrangle, Summit and Wasatch Counties, Utah","indexId":"gq852","publicationYear":"1971","noYear":false,"title":"Geologic map of the Park City East quadrangle, Summit and Wasatch Counties, Utah"},"id":1}],"supersededBy":{"id":63302,"text":"gq852 - 1971 - Geologic map of the Park City East quadrangle, Summit and Wasatch Counties, Utah","indexId":"gq852","publicationYear":"1971","noYear":false,"title":"Geologic map of the Park City East quadrangle, Summit and Wasatch Counties, Utah"},"lastModifiedDate":"2022-04-27T22:09:58.193311","indexId":"ofr6924","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","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":"69-24","title":"Geologic map of the Park City East Quadrangle, Summit and Wasatch Counties, Utah","docAbstract":"

No abstract available. 

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr6924","usgsCitation":"Bromfield, C., and Crittenden, M.D., 1969, Geologic map of the Park City East Quadrangle, Summit and Wasatch Counties, Utah: U.S. Geological Survey Open-File Report 69-24, 2 Plates: 21.13 x 28.59 inches and 23.77 x 21.65 inches, https://doi.org/10.3133/ofr6924.","productDescription":"2 Plates: 21.13 x 28.59 inches and 23.77 x 21.65 inches","costCenters":[],"links":[{"id":168716,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1969/0024/report-thumb.jpg"},{"id":399769,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0024/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":399770,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0024/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"24000","country":"United States","state":"Utah","county":"Summit County, Wasatch County","otherGeospatial":"Park City East Quadrangle","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -111.5,40.6175 ], [ -111.5,40.75 ], [ -111.36749999999999,40.75 ], [ -111.36749999999999,40.6175 ], [ -111.5,40.6175 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4af5e4b07f02db6924de","contributors":{"authors":[{"text":"Bromfield, Calvin S.","contributorId":98690,"corporation":false,"usgs":true,"family":"Bromfield","given":"Calvin S.","affiliations":[],"preferred":false,"id":234848,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Crittenden, Max D. Jr.","contributorId":28951,"corporation":false,"usgs":true,"family":"Crittenden","given":"Max","suffix":"Jr.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":234847,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":68642,"text":"ha360 - 1969 - Water resources of Wisconsin: Rock-Fox River basin","interactions":[],"lastModifiedDate":"2024-02-28T23:08:39.564696","indexId":"ha360","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":318,"text":"Hydrologic Atlas","code":"HA","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"360","title":"Water resources of Wisconsin: Rock-Fox River basin","docAbstract":"

PURPOSE AND SCOPE

\n

The purpose of this report is to describe the physical environment, availability, distribution, characteristics, movement, quality, water problems, and use of water within the Rock-Fox River basin in order to aid in planning future water management within the basin.

\n

This report presents general information on the basin that was derived from data obtained from Federal, State, and local agencies. In addition, new data were collected from areas where available data were scarce. The reader is referred to the section entitled “Agencies Having Additional Information” and to the list of selected references (sheet 4) for sources of more detailed information.

\n

This atlas is one of a series of 12 river-basin studies designed to describe in general terms the water resources of the State. More detailed studies of problem areas will be required in the future as the need for additional information increases.

\n

LOCATION AND EXTENT

\n

The Rock-Fox River basin in Wisconsin, covers about 4,750 square miles in the southeastern part of the State. It includes all or parts of the following 13 counties: Columbia, Dane, Dodge, Fond du Lac, Green Lake, Jefferson, Kenosha, Milwaukee, Racine, Rock, Walworth, Washington, and Waukesha. It includes the area drained by the Rock, Fox, and Des Plaines Rivers within the State of Wisconsin.

\n

Although the basin boundary is the topographic divide, part of the streamflow is derived from ground water that drains from an area similar to, but not having the same boundaries as, the topographic basin. The ground-water basin covers about 4,350 square miles, 400 square miles less than the topographic basin. Most of the reduction in basin area is along the eastern side of the basin.

\n

 

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ha360","usgsCitation":"Cotter, R.D., Hutchinson, R.D., Skinner, E., and Wentz, D., 1969, Water resources of Wisconsin: Rock-Fox River basin: U.S. Geological Survey Hydrologic Atlas 360, 4 Plates: 41.00 x 31.84 inches or smaller, https://doi.org/10.3133/ha360.","productDescription":"4 Plates: 41.00 x 31.84 inches or smaller","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":677,"text":"Wisconsin Water Science Center","active":true,"usgs":true}],"links":[{"id":426094,"rank":6,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_15738.htm","linkFileType":{"id":5,"text":"html"}},{"id":186591,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":90314,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/ha/360/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":90313,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/ha/360/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":90316,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/ha/360/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":90315,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/ha/360/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"1000000","country":"United States","state":"Wisconsin","county":"Columbia County, Dane County, Dodge County, Fond du Lac County, Green Lake County, Jefferson County, Kenosha County, Milwaukee County, Racine County, Rock County, Walworth County, Washington County, Waukesha County","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -89.45068359374999,\n 42.52879629320373\n ],\n [\n -89.45068359374999,\n 43.691707903073805\n ],\n [\n -87.945556640625,\n 43.691707903073805\n ],\n [\n -87.945556640625,\n 42.52879629320373\n ],\n [\n -89.45068359374999,\n 42.52879629320373\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f4e4b07f02db5f06c6","contributors":{"authors":[{"text":"Cotter, R. D.","contributorId":89874,"corporation":false,"usgs":true,"family":"Cotter","given":"R.","email":"","middleInitial":"D.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":278625,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hutchinson, R. D.","contributorId":99112,"corporation":false,"usgs":true,"family":"Hutchinson","given":"R.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":895565,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Skinner, E.L.","contributorId":53412,"corporation":false,"usgs":true,"family":"Skinner","given":"E.L.","email":"","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":895566,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Wentz, D.A.","contributorId":85206,"corporation":false,"usgs":true,"family":"Wentz","given":"D.A.","email":"","affiliations":[],"preferred":false,"id":895567,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":53421,"text":"ofr69328 - 1969 - Geology, hydrology, and water quality in the Fresno area, California","interactions":[],"lastModifiedDate":"2024-08-01T13:34:45.292576","indexId":"ofr69328","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","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":"69-328","title":"Geology, hydrology, and water quality in the Fresno area, California","docAbstract":"

The Fresno area comprises about 1.400 square miles lying west of the foothills of the Sierra Nevada and east of the trough of the San Joaquin Valley. The rainfall averages less than 10 inches per year causing agricultural development to depend mainly on surface-water deliveries and ground-water pumpage. Surface-water deliveries and ground-water pumpage, however, vary considerably from year to year. For example, in agricultural year 1958 (April 1, 1958-March 31, 1959) surface-water deliveries were about 1,340,000 acre-feet and agricultural ground-water pumpage was about 1,740,000 acre-feet, but in agricultural year 1960 deliveries were only about 560,000 acre-feet and pumpage was about 2,520,000 acre-feet.

Alluvial fans are the dominant geomorphic features in the area. Small alluvial fans have been formed near the foothills by the deposits from the numerous intermittent streams that lie both north and south of the Kings River. Thicker and much more extensive alluvial fans have been formed under most of the area by deposits from the San Joaquin and Kings Rivers.

Geologic units in the area consist of consolidated rocks and unconsolidated deposits. In turn, consolidated rocks consist of basement complex of pre-Tertiary age and marine and continental sedimentary rocks of Cretaceous and Tertiary age. Unconsolidated deposits are of both Tertiary and Quaternary age. Most of the geologic units dip gently southwestward approximately paralleling the back slope of the Sierra Nevada. Although some of these geologic units are faulted, especially in the deep subsurface, faulting has not affected the occurrence and movement of fresh ground water.

The basement complex crops out along the eastern border of the area and yields only small amounts of water to wells; the marine and continental sedimentary rocks do not crop out in the area and do not yield any water to wells.

The unconsolidated deposits are divided into an older series of Tertiary and Quaternary age, and a younger series of Quaternary age. The continental deposits of Tertiary and Quaternary age crop out beneath the extreme southeastern part of the area and yield small amounts of water to wells, and the deposits of Quaternary age crop out over most of the area and yield more than 90 percent of the water pumped from wells.

The deposits of Quaternary age in turn are divided into older alluvium, lacustrine and marsh deposits, younger alluvium, flood-basin deposits. and sand dunes.

The older alluvium is by far the most important aquifer in the Fresno area. It consists of intercalated lenses of clay, silt, silty and sandy clay, clayey and silty sand, sand, gravel, cobbles, and boulders, and in general it is fine grained near the trough of the valley and beneath the alluvial fans of intermittent streams.

In the older alluvium, yields to wells range from less than 20 gpm (gallons per minute) to more than 3,000 gpm.

The lacustrine and marsh deposits occur only in the subsurface in the western part of the area. Consisting mostly of silt and clay, they are virtually impermeable and thus restrict the vertical movement of water. These deposits from oldest to youngest are designated the E-clay, the C-clay, and the A-clay. The E-clay is the thickest and most extensive of all the lacustrine and marsh deposits.

Because the clays tend to confine ground water in the Fresno area, five water bodies are recognized. These are the unconfined water body, the shallow water body, the confined water body below the A-clay, the confined water body below the C-clay, and the confined water body below the E-clay. The unconfined water body underlies most of the Fresno area. The shallow and confined water bodies underlie parts of the extreme western part of the area. There, heads in successively underlying water bodies are less than those in overlying water bodies, indicating that some ground water moves slowly downward through the clays.

From agricultural years 1957 to 1962, outflow in the area exceeded inflow. As a result, for this period, the Fresno area had a net deficit of about 2,890,000 acre-feet. This deficit was made up for mostly by a decline in ground water stored.

Water levels in all water bodies have been declining over the years, yet when streamflow and canal deliveries are large they show a general rise.

The general movement of ground water in the Fresno area is toward the southwest, although pumping depressions near Fresno and near the western part of the area, cause ground water to move northward, southward, and westward toward them.

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R.A.","contributorId":69223,"corporation":false,"usgs":true,"family":"LeBlanc","given":"R.A.","email":"","affiliations":[],"preferred":false,"id":247559,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":68495,"text":"ha330 - 1969 - Ground water in the Ogallala formation in the southern high plains of Texas and New Mexico","interactions":[],"lastModifiedDate":"2016-08-16T16:38:08","indexId":"ha330","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":318,"text":"Hydrologic Atlas","code":"HA","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"330","title":"Ground water in the Ogallala formation in the southern high plains of Texas and New Mexico","docAbstract":"

The Ogallala Formation of Tertiary (Pliocene) age is the principal aquifer in the Southern High Plains of western Texas and eastern New Mexico. This heavily pumped aquifer supplies practically all the water used for irrigation, municipal, industrial (except oil-field repressuring), and domestic purposes.

\n

Although the ground water in the Ogallala Formation in the Southern High Plains is common to both Texas and New Mexico, the State laws concerning ownership of the water are different. The New Mexico statutes provide that all underground waters of the State belong to the public and are subject to appropriation for beneficial use (Reynolds, 1961, p. 79). Under conditions specified in the law, the State Engineer may declare certain areas as underground water basins in which the State Engineer has jurisdiction over the drilling of wells. The approximate boundaries of two such basins in New Mexico are shown on the maps. In Texas, the landowner owns the underground water. Under a law passed by the Texas State Legislature in 1949, underground water conservation districts may be formed with the authority to make rules and regulations for the conservation of ground waters, such as rules governing the minimum spacing of wells, and rules for the prevention of waste and contamination of fresh water, and other practices for the conservation of ground water. The approximate boundaries of two underground water conservation districts in Texas are shown on the maps.

","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/ha330","usgsCitation":"Cronin, J., 1969, Ground water in the Ogallala formation in the southern high plains of Texas and New Mexico: U.S. Geological Survey Hydrologic Atlas 330, Document: 9 p.; 4 Plates: 29.50 x 40.79 inches or smaller, https://doi.org/10.3133/ha330.","productDescription":"Document: 9 p.; 4 Plates: 29.50 x 40.79 inches or smaller","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":90050,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/ha/330/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":90051,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/ha/330/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":90052,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/ha/330/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":90053,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/ha/330/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":90054,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/ha/330/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":185976,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/ha/330/report-thumb.jpg"}],"scale":"500000","country":"United States","state":"New Mexico, Texas","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-101.6243,35.6186],[-101.6244,35.6249],[-101.0862,35.6238],[-101.0862,35.6211],[-101.0862,35.1826],[-101.0873,34.7476],[-100.943,34.7466],[-100.9472,34.3132],[-100.5121,34.315],[-100.5206,33.835],[-100.5194,33.3966],[-101.0406,33.3962],[-101.0371,32.9701],[-101.1733,32.9627],[-101.1738,32.9627],[-101.176,32.5272],[-101.1776,32.4871],[-101.1739,32.0897],[-101.2626,32.0896],[-101.2654,31.6522],[-101.777,31.6521],[-102.2897,31.6533],[-102.3171,31.6527],[-102.769,31.6512],[-102.7986,31.6513],[-102.7982,32.0871],[-103.0641,32.0856],[-103.0642,31.9996],[-103.3084,32.0006],[-103.3265,32.0007],[-103.3394,32.0008],[-103.3781,32.0008],[-103.3954,32.0008],[-103.7164,32.0015],[-103.7162,32.0631],[-103.716,32.0918],[-103.716,32.1666],[-103.7161,32.1817],[-103.7157,32.2546],[-103.7158,32.2692],[-103.7154,32.3385],[-103.7155,32.3535],[-103.7156,32.4278],[-103.7157,32.4429],[-103.7165,32.4916],[-103.7165,32.5085],[-103.7166,32.524],[-103.7194,32.524],[-103.7493,32.5242],[-103.7716,32.5246],[-103.789,32.5245],[-103.8096,32.5249],[-103.8097,32.5399],[-103.81,32.6101],[-103.8101,32.6247],[-103.8103,32.6971],[-103.8105,32.7122],[-103.8112,32.7823],[-103.8114,32.7974],[-103.8112,32.8429],[-103.8114,32.8575],[-103.8115,32.8725],[-103.8116,32.8876],[-103.8112,32.903],[-103.8111,32.9663],[-103.7651,32.9668],[-103.765,33.0096],[-103.7646,33.0232],[-103.7625,33.2722],[-103.7623,33.3173],[-103.7611,33.3973],[-103.7155,33.3973],[-103.7149,33.4547],[-103.7151,33.4683],[-103.7146,33.4847],[-103.7143,33.5147],[-103.7139,33.5284],[-103.7127,33.5702],[-103.5738,33.571],[-103.5396,33.5712],[-103.506,33.5713],[-103.5043,33.6591],[-103.6091,33.6595],[-103.6466,33.6603],[-103.6637,33.6606],[-103.7144,33.6612],[-103.716,33.7208],[-103.7159,33.8186],[-103.8385,33.8219],[-103.8396,34.0843],[-103.945,34.0848],[-103.9419,34.2625],[-103.9475,34.2621],[-103.9457,34.6056],[-104.1266,34.6059],[-104.1268,34.7817],[-104.1282,34.9553],[-104.1226,34.9561],[-104.123,35.1427],[-104.016,35.1927],[-103.8564,35.2641],[-103.8561,35.2424],[-103.6927,35.2409],[-103.6352,35.2406],[-103.6357,35.3894],[-103.586,35.3913],[-103.4799,35.3914],[-103.3992,35.391],[-103.3919,35.3922],[-103.3774,35.4032],[-103.3789,35.6524],[-103.3746,35.6525],[-103.3744,35.7398],[-103.0409,35.7408],[-103.0409,35.7394],[-103.0409,35.6225],[-102.1624,35.6277],[-102.1625,35.6203],[-101.768,35.6197],[-101.6927,35.619],[-101.656,35.6186],[-101.6514,35.6187],[-101.6463,35.6187],[-101.6356,35.6184],[-101.6243,35.6186]]]},\"properties\":{\"name\":\"Curry\",\"state\":\"NM\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ab0e4b07f02db66d8e0","contributors":{"authors":[{"text":"Cronin, J.G.","contributorId":47769,"corporation":false,"usgs":true,"family":"Cronin","given":"J.G.","email":"","affiliations":[],"preferred":false,"id":278327,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":12939,"text":"ofr6936 - 1969 - Recent surface movements in the Baldwin Hills, Los Angeles County, California","interactions":[{"subject":{"id":12939,"text":"ofr6936 - 1969 - Recent surface movements in the Baldwin Hills, Los Angeles County, California","indexId":"ofr6936","publicationYear":"1969","noYear":false,"title":"Recent surface movements in the Baldwin Hills, Los Angeles County, California"},"predicate":"SUPERSEDED_BY","object":{"id":5758,"text":"pp882 - 1976 - Recent surface movements in the Baldwin Hills, Los Angeles County, California","indexId":"pp882","publicationYear":"1976","noYear":false,"title":"Recent surface movements in the Baldwin Hills, Los Angeles County, California"},"id":1}],"supersededBy":{"id":5758,"text":"pp882 - 1976 - Recent surface movements in the Baldwin Hills, Los Angeles County, California","indexId":"pp882","publicationYear":"1976","noYear":false,"title":"Recent surface movements in the Baldwin Hills, Los Angeles County, California"},"lastModifiedDate":"2024-05-24T19:53:10.458712","indexId":"ofr6936","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","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":"69-36","title":"Recent surface movements in the Baldwin Hills, Los Angeles County, California","docAbstract":"

The Baldwin Hills are located in the northwest part of the densely populated Los Angeles basin. They comprise one of several groups of isolated hills that extend along the northwest-trending Newport-Inglewood zone of folds and faults, a structural lineament identified with a series of very productive oil fields. In addition to being the site of the Inglewood oil field, these hills are the site of surface deformation that has been monitored for over 35 years. This record of deformation, which includes differential subsidence, horizontal displacements, and surface rupturing, forms one of the best documented examples of oilfield-associated surface deformation yet recognized. The deformation is described in detail, analyzed as to cause(s), and finally attributed largely or essentially entirely to the exploitation of the spatially-associated Inglewood oil field.

The Baldwin Hills are underlain by gently to moderately arched and conspicuously faulted Cenozoic sedimentary and volcanic rocks that overlie crystalline basement rocks at a depth of more than 10,000 feet. The Inglewood fault, a part of the northwest-trending Newport-Inglewood zone, diagonally transects the hills. Right-lateral displacements of 3,000-4,000 feet since middle or late Pliocene time and 1,500-2,000 feet during Quaternary time are indicated by offset structural and physio-graphic features; indications of vertical separations of up to about 200 feet during late Quaternary time occur locally.

Evidence of continuing deformation includes recognized seismicity and regional elevation changes. The M5-5 1/2 Inglewood earthquake of 1920, the largest local earthquake of record, is believed to have originated immediately southeast of the Baldwin Hills; it was apparently unassociated with surficial fault displacements. Leveling in and around the west and central Los Angeles basin has shown that lowland stations have been consistently subsiding, whereas foothill stations commonly have been rising. Several seemingly persistent basins of differential subsidence and a zone of positive movement, roughly coincident with the Newport-Inglewood zone, have also been identified in the northwest part of the basin.

A prominent, elliptically-shaped, northwest-trending subsidence bowl encompassing the northwest part of the Baldwin Hills, has been defined by repeated level circuits. Partial reconstruction of selected level circuits with respect to a common, relatively stable control point (Hollywood E-11), located on the edge of the subsidence bowl, has permitted evaluation of the subsidence since 1910 and 1911 at two points near the center of the bowl. Thus bench mark PBM 67 is estimated to have subsided approximately 4.324 feet between June 1910 and February 1963; and bench mark PBM 68 (the only bench mark within the subsidence bowl that was leveled prior to 1926 and has been repeatedly leveled since) subsided 3.846 feet between November 1911 and June 1962. Analysis of the available data indicates little if any elevation change at PBM 68 (or elsewhere throughout the Baldwin Hills-Inglewood area) associated with the Inglewood earthquake of 1920. Maximum subsidence of PBM 122 (which has remained very close to the center of subsidence since at . least 1950) between 1911 and 1963 is calculated to have been 5.67 feet.

Horizontal displacements (with respect to a north-south base line about 3 miles east of the hills) of six triangulation points within the subsidence bowl have been measured for various periods between 1934 and 1963. Displacements have been generally toward the center of subsidence and almost precisely perpendicular to the immediately adjacent isobases of equal elevation change. Maximum movement has been recorded at triangulation point Baldwin Aux, which was displaced 2.21 feet between 1934 and 1961; horizontal displacements of three additional points ranged from 0.95 foot to 1.85 feet between 1936 and 1961. Displacements of 0.10-0.29 foot were recorded at all six monuments during the period 1961-1963.

\"Earth cracks\" and surficial fault displacements were recognized in the Baldwin Hills at least as early as 1957. The cracks are relatively straight, generally continuous fractures confined to the structural block east of the Inglewood fault; they are concentrated in two areas centering on (1) the Baldwin Hills Reservoir and (2) the Stocker Street-LaBrea Avenue-Overhill Drive intersection. The cracks trend north to north-northeast and are nearly everywhere parallel to or coincident with minor faults and joints, and are generally orthogonal to radii emanating from the center of subsidence. Differential movement along the cracks has been almost entirely dip slip along steep to nearly vertical surfaces, and generally down-dropped toward the center of subsidence. Cumulative displacements have been as much as 6 or 7 inches. Rates of displacement have ranged widely, and the movement has generally occurred as creep or very small discrete jumps. A probable exception is the several inches of differential movement that is believed to have occurred along a crack through the floor of the Baldwin Hills Reservoir on or about December 14, 1963.

The contemporary surface movements are attributable to one or more of the following phenomena: (1). exploitation of the Inglewood oil field; (2) changes in the ground-water regimen; (3) compaction of sedimentary materials in response to surface loading; (4) tectonic activity.

The following considerations indicate that the differential subsidence is attributable largely or entirely to exploitation of the underlying Inglewood oil field: (1) the coincidence of the centers of the oil field, the producing structure, and the subsidence bowl; (2) the general correspondence between the pattern of subsidence and the outlines of the oil field; (3) the approximate coincidence between the initiation of production and the initiation of subsidence; (4) the generally linear relations between various measures of subsidence and liquid production from both the field as a whole and the exceptionally prolific Vickers zone in particular; (5) the sharp deceleration of subsidence in the eastern block of the field coincident with the initiation of full-scale water flooding there; (6) the many examples of oil fields In which both spatial and temporal associations between production and subsidence are recognized; (7) the many similarities of the subsidence-production relations in the Inglewood field to those in the Wilmington field, where the subsidence has been authoritatively attributed to oilfield operations; (8) the theoretical relation between subsidence or a tendency toward subsidence and increased effective pressure associated with underground fluid extraction.

Consideration of six possible explanations for the increasing rather than decreasing or constant rate of subsidence with respect to reservoir fluid pressure decline suggests that measured or calculated down-hole reservoir fluid pressure decline is non-representative of average or real fluid pressure decline away from producing wells. The near-linear relations between net-liquid production and subsidence are explained through analogy with a tightly confined artesian system of infinite areal extent, where production must derive from liquid expansion and/or reservoir compaction. Test data from compaction studies in two other oil fields yield estimates of ultimate compaction of the Vickers zone resulting from a total loss of fluid pressure; these estimates range over an order of magnitude. The best estimate, based on these data and considerations of late Cenozoic history in the Baldwin Hills area, is about 10 feet.

The centripetally-directed horizontal movements are considered attributable to exploitation of the Inglewood oil field on the basis of:
(1) their well-defined symmetrical and geometrical association with the differential subsidence; (2) the similarities between these associations and those developed in and around other subsiding oil fields; and (3) the mechanical compatibility of these movements with subsidence induced by the extraction of subsurface materials.

The earth cracks and surficial fault displacements are considered largely or entirely attributable to the exploitation of the Inglewood oil field on the basis of: (1) their spatial and temporal relations to both oil-field operations and the differential subsidence; (2) the similarities of these cracks and displacements to those generated in and around other oil fields and areas of subsurface materials extraction; and (3) surface strain patterns predicted from the measured vertical and horizontal surface movements. The cracks and displacements can i)e explained by an exploitation-based, elastic-rebound model which requires elastic compression of the sedimentary section in response to compaction-induced downdrag within those blocks around the periphery of the subsidence bowl. The measured displacements have been about one-quarter to one-half those predicted for a purely elastic system.

Analysis of: (1) the history of ground-water extraction within and around the Baldwin Hills; and (2) subsidence associated with water-level declines in sediments comparable with those in the Baldwin Hills, indicate that the surface movements can be no more than incidentally attributed to changes in ground-water conditions. Similarly, analysis of the history of natural and artificial changes in surface loading indicate that these movements are generally unassociated with changes in surface loading conditions.

Considerations of local geologic history and various tectonic associations indicate that it is very unlikely that the differential subsidence and horizontal movements are due to tectonic downwarping. There exists a far stronger prima facie argument for tectonic involvement in the earth cracking and associated fault displacements. This argument is disputed by; (1) the spatial and temporal relations of the earth cracks to, and their mechanical compatibility with, the nontectonic differential subsidence; (2) the absence of displacements on the Inglewood fault in conjunction with those along the conjugate earth cracks; (3) the probability that purely tectonic displaceMents would be characterized by oblique or strike slip; and (4) the absence of any clear temporal relation between crack growth and local seismicity, However, because as much as 10 percent of the local isobase gradient may be unexplained' by oil-field exploitation, a small fraction of this gradient, and thus the displacements among the southern group of cracks, may be attributable to tectonic activity. This fraction should have been insignificant in the presence of the strain pattern produced by nontectonic compaction of the underlying oil measures.

Because nearly all of the observed and measured surface movements can be fully explained as the products of oil-field operations, yet can be no more than incidentally attributed to changes in ground-water conditions, surface loading, or tectonic activity, we conclude that these movements are attributable largely or essentially entirely to the exploitation of the Inglewood oil field.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr6936","usgsCitation":"Castle, R.O., and Yerkes, R.F., 1969, Recent surface movements in the Baldwin Hills, Los Angeles County, California: U.S. Geological Survey Open-File Report 69-36, xviii, 185 p., https://doi.org/10.3133/ofr6936.","productDescription":"xviii, 185 p.","costCenters":[],"links":[{"id":429278,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1969/0036/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":146998,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1969/0036/report-thumb.jpg"}],"country":"United States","state":"California","county":"Los Angeles County","otherGeospatial":"Baldwin Hills","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -118.38187677397389,\n 34.0348739886972\n ],\n [\n -118.38187677397389,\n 33.97553856602411\n ],\n [\n -118.30144514525205,\n 33.97553856602411\n ],\n [\n -118.30144514525205,\n 34.0348739886972\n ],\n [\n -118.38187677397389,\n 34.0348739886972\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a7ee4b07f02db648569","contributors":{"authors":[{"text":"Castle, Robert O.","contributorId":22741,"corporation":false,"usgs":true,"family":"Castle","given":"Robert","email":"","middleInitial":"O.","affiliations":[],"preferred":false,"id":166993,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Yerkes, R. F.","contributorId":24754,"corporation":false,"usgs":true,"family":"Yerkes","given":"R.","middleInitial":"F.","affiliations":[],"preferred":false,"id":166994,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70207551,"text":"70207551 - 1969 - Kilauea Volcano: The 1967-68 summit eruption","interactions":[],"lastModifiedDate":"2019-12-24T10:04:52","indexId":"70207551","displayToPublicDate":"1969-12-23T12:12:58","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3338,"text":"Science","active":true,"publicationSubtype":{"id":10}},"title":"Kilauea Volcano: The 1967-68 summit eruption","docAbstract":"

On 5 November 1967 Kilauea volcano began erupting lava from vents on the floor of its summit pit crater. Halemaumau, 170 meters deep. This eruption ended nearly 2 years of the quiescence that followed a short lived eruption on the east  rift zone of Kilauea in December 1965 (1). The 1967-68 eruption was the first activity in Halemaumau since July 1961 (2). The eruption ceased on 13 July 1968 following 31 separate phases of fountaining separated by short periods of quiescence. Six weeks after the  end of the summit eruption, a short eruption occurred on the upper east rift zone of Kilauea. As the article goes to press there have been four eruptions, all of the upper east rift zone. The last of the four began  in May 1969 and have just completed its seventh phase. The article summarizes the eruption in Halemanumau and complements an article Fiske and Kinoshita on the deformation that preceded the eruption (3). The methods of study and the instrumentation used during the eruption are the same as those discussed in the earlier article. The locations of all seismographs tiltmeter stations and bench marks are shown in Fig. 1. 

","language":"English","publisher":"AAAS","doi":"10.1126/science.166.3904.459","usgsCitation":"Kinoshita, W.T., Koyanagi, R.Y., Wright, T., and Fiske, R.S., 1969, Kilauea Volcano: The 1967-68 summit eruption: Science, v. 166, no. 3904, p. 459-468, https://doi.org/10.1126/science.166.3904.459.","productDescription":"10 p.","startPage":"459","endPage":"468","costCenters":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"links":[{"id":370651,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Hawaii","otherGeospatial":"Kilauea Volcano","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -155.36659240722656,\n 19.276146935787732\n ],\n [\n -155.1372528076172,\n 19.276146935787732\n ],\n [\n -155.1372528076172,\n 19.475655495911568\n ],\n [\n -155.36659240722656,\n 19.475655495911568\n ],\n [\n -155.36659240722656,\n 19.276146935787732\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"166","issue":"3904","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Kinoshita, Willie Tomoni","contributorId":87148,"corporation":false,"usgs":true,"family":"Kinoshita","given":"Willie","email":"","middleInitial":"Tomoni","affiliations":[],"preferred":false,"id":778439,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Koyanagi, R. Y.","contributorId":35719,"corporation":false,"usgs":true,"family":"Koyanagi","given":"R.","email":"","middleInitial":"Y.","affiliations":[],"preferred":false,"id":778440,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Wright, Thomas L. twright@usgs.gov","contributorId":3890,"corporation":false,"usgs":true,"family":"Wright","given":"Thomas L.","email":"twright@usgs.gov","affiliations":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"preferred":true,"id":778441,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Fiske, Richard S.","contributorId":17984,"corporation":false,"usgs":true,"family":"Fiske","given":"Richard","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":778442,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70223877,"text":"70223877 - 1969 - Mesozoic California and the underflow of Pacific mantle","interactions":[],"lastModifiedDate":"2021-09-10T20:41:55.668543","indexId":"70223877","displayToPublicDate":"1969-12-01T15:32:51","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Mesozoic California and the underflow of Pacific mantle","docAbstract":"

The Mesozoic evolution of California is interpreted as dominated by the underflow of oceanic mantle beneath the continental margin. Underflow during part of Late Cretaceous time of more than 2000 km of the eastern Pacific plate seems required by the marine magnetic data. Correspondingly, varied oceanic environments—abyssal hill, island arc, trench, oceanic crust, and upper mantle, perhaps also continental rise and abyssal plain—appear to be represented in the eugeosynclinal terranes of California. The rock juxtapositions accord with the concept that these materials were scraped off against the continent as the oceanic plate slid beneath it along Mesozoic Benioff seismic zones, which are now seen as serpentine belts separating profoundly different rock assemblages.

The chaotic Franciscan Formation of coastal California consists of deep-ocean Late Jurassic to Late Cretaceous sedimentary, volcanic, crustal, and mantle materials. As open-ocean abyssal oozes and the oceanic crust beneath them were swept into the Benioff-zone trench at the continental margin, they were covered by terrigenous clastic sediments, and the entire complex was carried beneath the correlative continental-shelf and continental-slope deposits (Great Valley sequence) and the older Mesozoic complexes.

The other eugeosynclinal terranes of California can be interpreted, albeit with less confidence, in similar terms of underflow of Pacific mantle. In the Klamath Mountains and northern Sierra Nevada, for example, Ordovician and Silurian ocean-floor materials, overlain by or juxtaposed against an Upper Silurian to Permian island arc, were swept in first to the continent, along with a large fragment of oceanic crust and mantle and another fragment of an old orogenic belt. This debris was followed by Permian and Triassic ocean-floor deposits. Late Triassic and Jurassic volcanic products from stocks and batholiths forming in the welded complexes lapped across both landward and oceanward sides of the region.

Reversal of Cenozoic extension, strike-slip faulting, and volcanic crustal growth in the western United States reveals a Cretaceous tectonic pattern strikingly like the modern pattern of the Andes, so the paleotectonic setting of North America can be inferred from the South American present. The Mesozoic batholiths of North America, like the late Cenozoic volcanic belt of the central Andes, are products of the same rapid motion of oceanic plates that carried oceanic sediments against the continent to form eugeosynclinal terranes. Magmas generated in the Benioff zones formed the batholiths and the volcanic fields which initially capped them.

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1969)80[2409:MCATUO]2.0.CO;2","usgsCitation":"Hamilton, W., 1969, Mesozoic California and the underflow of Pacific mantle: Geological Society of America Bulletin, v. 80, no. 12, p. 2409-2429, https://doi.org/10.1130/0016-7606(1969)80[2409:MCATUO]2.0.CO;2.","productDescription":"21 p.","startPage":"2409","endPage":"2429","costCenters":[],"links":[{"id":389117,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"East Pacific Rise, Franciscan Formation, Klamath Mountains, North American continental plate, Pacific Ocean, Pacific plate, Sierra 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\"}}]}","volume":"80","issue":"12","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Hamilton, Warren","contributorId":14819,"corporation":false,"usgs":true,"family":"Hamilton","given":"Warren","affiliations":[],"preferred":false,"id":823056,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70224559,"text":"70224559 - 1969 - Mean streamflow from discharge measurements","interactions":[],"lastModifiedDate":"2021-09-27T17:22:47.671228","indexId":"70224559","displayToPublicDate":"1969-12-01T07:44:09","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":5334,"text":"International Association of Scientific Hydrology - Bulletin ","onlineIssn":"2150-3435","printIssn":"0262-6667","active":false,"publicationSubtype":{"id":10}},"title":"Mean streamflow from discharge measurements","docAbstract":"

Mean flow of a stream is usually computed from a continuous record of flow ai a gaging station. A less costly method consists of (1) estimating 12 individual monthly flows from one discharge measurement per month and a concurrent gaging station record on a nearby stream, using a different relation for each month, (2) computing the annual mean from the estimated monthly means, and (3) using a relation based on gaging station records to estimate the long-term mean from the one annual mean. An annual mean can be estimated within about 10 percent of its measured value even though both the gaged and ungaged streams are affected by diversions and have different runoff characteristics. The method has greatest utility in regions where mean runoff is not closely related to drainage area.

","language":"English","publisher":"Taylor & Francis","doi":"10.1080/02626666909493757","usgsCitation":"Riggs, H.C., 1969, Mean streamflow from discharge measurements: International Association of Scientific Hydrology - Bulletin , v. 14, no. 4, p. 95-110, https://doi.org/10.1080/02626666909493757.","productDescription":"16 p.","startPage":"95","endPage":"110","costCenters":[],"links":[{"id":480298,"rank":0,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.1080/02626666909493757","text":"Publisher Index Page"},{"id":389820,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Idaho, Nevada, Washington","city":"Contact, Elk City, Three Creek, Yellow Pine","otherGeospatial":"East Fork Bruneau River, East Fork Jarbidge River, Fish Creek, Johnson Creek, Salmon Falls Creek, South Fork Clearwater River, Tailholt Creek","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -113.45581054687499,\n 46.66451741754235\n ],\n [\n -108.226318359375,\n 46.66451741754235\n ],\n [\n -108.226318359375,\n 48.99463598353405\n ],\n [\n -113.45581054687499,\n 48.99463598353405\n ],\n [\n -113.45581054687499,\n 46.66451741754235\n ]\n ]\n ]\n }\n },\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -117.9107666015625,\n 41.017210578228436\n ],\n [\n -112.91748046874999,\n 41.017210578228436\n ],\n [\n -112.91748046874999,\n 43.13306116240612\n ],\n [\n -117.9107666015625,\n 43.13306116240612\n ],\n [\n -117.9107666015625,\n 41.017210578228436\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"14","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Riggs, H. C.","contributorId":17210,"corporation":false,"usgs":true,"family":"Riggs","given":"H.","email":"","middleInitial":"C.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":824055,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70048802,"text":"70048802 - 1969 - Great Salt Lake, Utah: Chemical and physical variations of the brine, 1963-1966","interactions":[],"lastModifiedDate":"2017-09-06T17:24:08","indexId":"70048802","displayToPublicDate":"1969-11-05T16:15:00","publicationYear":"1969","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":2,"text":"State or Local Government Series"},"seriesTitle":{"id":5485,"text":"Utah Geological and Mineralogical Survey Water-Resources Bulletin","active":false,"publicationSubtype":{"id":2}},"seriesNumber":"12","title":"Great Salt Lake, Utah: Chemical and physical variations of the brine, 1963-1966","docAbstract":"

Great Salt Lake is a shallow, closed-basin lake in northern Utah. Its surface area and concentration of dissolved solids vary in response to both annual and long-term climatic changes. The lake gains water mainly as streamflow from mountains to the east and loses water through evaporation. In 1965, at a lake-surface altitude of 4,194 feet, the surface area was about 1,000 square miles, and the maximum measured depth was 27 feet.

Studies to define the variations in chemical and physical characteristics of the brine began in 1963, and detailed sampling of the lake at 29 sites was made in October 1965 and May 1966. Data resulting from concurrent sampling of the 29 sites indicated that four types of brine coexist in the lake.

","language":"English","publisher":"Utah Geological and Mineralogical Survey","publisherLocation":"Salt Lake City, UT","collaboration":"Prepared in cooperation with the Utah Geological and Mineralogical Survey","usgsCitation":"Hahl, D.C., and Handy, A., 1969, Great Salt Lake, Utah: Chemical and physical variations of the brine, 1963-1966: Utah Geological and Mineralogical Survey Water-Resources Bulletin 12, 33 p.","productDescription":"33 p.","numberOfPages":"36","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":278873,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":333160,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://ugspub.nr.utah.gov/publications/water_resources_bulletins/WRB-12.pdf"}],"country":"United States","state":"Utah","otherGeospatial":"Great Salt Lake","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -113.131714,40.634799 ], [ -113.131714,41.71393 ], [ -111.860046,41.71393 ], [ -111.860046,40.634799 ], [ -113.131714,40.634799 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"527b731fe4b0a7295d9b8630","contributors":{"authors":[{"text":"Hahl, D. C.","contributorId":57436,"corporation":false,"usgs":true,"family":"Hahl","given":"D.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":485674,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Handy, A.H.","contributorId":104493,"corporation":false,"usgs":true,"family":"Handy","given":"A.H.","email":"","affiliations":[],"preferred":false,"id":485675,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70224249,"text":"70224249 - 1969 - Fission-track ages of accessory minerals from granitic rocks of the central Sierra Nevada batholith, California","interactions":[],"lastModifiedDate":"2021-09-15T16:22:04.699773","indexId":"70224249","displayToPublicDate":"1969-11-01T09:52:34","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Fission-track ages of accessory minerals from granitic rocks of the central Sierra Nevada batholith, California","docAbstract":"

Ages of apatite, sphene, allanite, epidote, and garnet from plutonic rocks of the central Sierra Nevada and Inyo Mountains have been determined by the fission-track method.

Ages of 44 specimens of apatite range from 54 to 128 m.y. Oldest apatites generally occur in rocks from the western portion of the batholith; youngest are from granitic rocks along the eastern slope of the Sierra Nevada.

Thirty-four specimens of sphene have been dated and range in age from 71 to 118 m.y. Within experimental error, all sphenes are as old as, or older than, coexisting apatites. The oldest sphene is from granitic rock of the Inyo Mountains; however, sampled rocks from the western Sierra Nevada do not contain sphene. The youngest sphenes are generally from rocks slightly west of the Sierran crest.

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1969)80[2201:FAOAMF]2.0.CO;2","usgsCitation":"Naeser, C.W., and Dodge, F.C., 1969, Fission-track ages of accessory minerals from granitic rocks of the central Sierra Nevada batholith, California: Geological Society of America Bulletin, v. 80, no. 11, p. 2201-2211, https://doi.org/10.1130/0016-7606(1969)80[2201:FAOAMF]2.0.CO;2.","productDescription":"11 p.","startPage":"2201","endPage":"2211","costCenters":[],"links":[{"id":389270,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Sierra Nevada","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -120.62988281249999,\n 39.138581990583525\n ],\n [\n -120.091552734375,\n 38.03078569382294\n ],\n [\n -120.10253906249999,\n 37.54457732085582\n ],\n [\n -119.20166015625,\n 36.55377524336089\n ],\n [\n -118.861083984375,\n 35.82672127366604\n ],\n [\n -118.65234374999999,\n 35.38904996691167\n ],\n [\n -117.23510742187501,\n 34.985003130171066\n ],\n [\n -116.861572265625,\n 35.209721645221386\n ],\n [\n -118.05908203124999,\n 36.59788913307022\n ],\n [\n -118.23486328125,\n 37.16907157713011\n ],\n [\n -118.6083984375,\n 38.013476231041935\n ],\n [\n -119.981689453125,\n 38.98503278695909\n ],\n [\n -120.003662109375,\n 39.36827914916014\n ],\n [\n -120.62988281249999,\n 39.138581990583525\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"80","issue":"11","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Naeser, C. W.","contributorId":17582,"corporation":false,"usgs":true,"family":"Naeser","given":"C.","middleInitial":"W.","affiliations":[],"preferred":false,"id":823354,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dodge, F. C. W.","contributorId":18755,"corporation":false,"usgs":true,"family":"Dodge","given":"F.","email":"","middleInitial":"C. W.","affiliations":[],"preferred":false,"id":823355,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70223907,"text":"70223907 - 1969 - The U.S. Geological Survey's gravity program in California","interactions":[],"lastModifiedDate":"2021-09-13T17:45:08.832973","indexId":"70223907","displayToPublicDate":"1969-10-01T12:38:16","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":7458,"text":"Eos Science News","active":true,"publicationSubtype":{"id":10}},"title":"The U.S. Geological Survey's gravity program in California","docAbstract":"

Since the 1963 gravity symposium, the U.S. Geological Survey has entered into a cooperative program with the California Division of Mines and Geology, the Army Map Service, and several universities for the purpose of completing a 5-mgal Bouguer gravity map of the entire State of California at a scale of 1:250,000 by 1970. The areal division of responsibility within the program is shown on a map of California by Chapman (p. 542).

It is evident from a plot of existing stations that considerably more data are required in the eastern Mojave Desert located in the southeastern corner of the state, and in the Sierra Nevada north of Lake Tahoe. Additional fill-in work is needed in nearly all parts of the state. The data requirements vary for a 5-mgal contour map depending on the local complexity of the gravity field; but in general, we are obtaining gravity stations at an interval of about 3 km along roads, trails, and rivers, and 5 to 8 km between these access routes by cross-country jeep, horseback, or helicopter if necessary. About 6000 new stations were obtained in California by the Geological Survey during 1968 and we expect to obtain about 3000 more in 1969.

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\"}}]}","volume":"50","issue":"10","noUsgsAuthors":false,"publicationDate":"2011-06-03","publicationStatus":"PW","contributors":{"authors":[{"text":"Oliver, Howard W.","contributorId":78704,"corporation":false,"usgs":true,"family":"Oliver","given":"Howard W.","affiliations":[],"preferred":false,"id":823228,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70224621,"text":"70224621 - 1969 - The structure and tectonic history of the eastern Aleutian Trench","interactions":[],"lastModifiedDate":"2021-09-30T17:34:49.906947","indexId":"70224621","displayToPublicDate":"1969-10-01T12:24:36","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"The structure and tectonic history of the eastern Aleutian Trench","docAbstract":"

The tectonic character of the eastern Aleutian Trench and some major events in its geologic history can be estimated from nine continuous seismic reflection records. A section of pre-trench, deep oceanic sediments rests on the down-warped crust that forms the trench. Nearly horizontal undeformed strata that unconformably overlie this deep oceanic section partially fill the trench. The trench fill is thickest near present sediment sources. A Pliocene age for development of the eastern Aleutian Trench is estimated from the thickness of deep oceanic sediment that accumulated after the trench began to fill. The eastern Aleutian Trench thus appears younger than the central Aleutian Trench—a relation which helps to explain the distribution of sediment along the two trench segments.

Depression of the eastern Aleutian Trench diminished or virtually ended soon after the trench began to fill. The undeformed fill provides no evidence for a large thrust fault zone at the base of the continental slope. Nor is there any evidence that oceanic sediments have disappeared beneath the continents in late Tertiary time. These observations are difficult to reconcile with the simple model of a continental margin advanced in the hypothesis of plate tectonics.

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1969)80[1889:TSATHO]2.0.CO;2","usgsCitation":"von Huene, R.E., and Shor, G.G., 1969, The structure and tectonic history of the eastern Aleutian Trench: Geological Society of America Bulletin, v. 80, no. 10, p. 1889-1902, https://doi.org/10.1130/0016-7606(1969)80[1889:TSATHO]2.0.CO;2.","productDescription":"16 p.","startPage":"1889","endPage":"1902","costCenters":[],"links":[{"id":390048,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"Aleutian Trench, Gulf of Alaska","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -169.3212890625,\n 52.855864177853974\n ],\n [\n -169.0576171875,\n 52.07950600379697\n ],\n [\n -153.80859375,\n 55.89995614406812\n ],\n [\n -144.580078125,\n 60.673178565817715\n ],\n [\n -150.205078125,\n 61.75233128411639\n ],\n [\n -169.365234375,\n 53.85252660044951\n ],\n [\n -169.3212890625,\n 52.855864177853974\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"80","issue":"10","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"von Huene, Roland E. 0000-0003-1301-3866 rvonhuene@usgs.gov","orcid":"https://orcid.org/0000-0003-1301-3866","contributorId":191070,"corporation":false,"usgs":true,"family":"von Huene","given":"Roland","email":"rvonhuene@usgs.gov","middleInitial":"E.","affiliations":[{"id":237,"text":"Earthquake Science Center","active":true,"usgs":true},{"id":7065,"text":"USGS emeritus","active":true,"usgs":false}],"preferred":false,"id":824385,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Shor, George G. Jr.","contributorId":266140,"corporation":false,"usgs":false,"family":"Shor","given":"George","suffix":"Jr.","email":"","middleInitial":"G.","affiliations":[{"id":16196,"text":"Scripps Institution of Oceanography, La Jolla, CA","active":true,"usgs":false}],"preferred":false,"id":824386,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70224597,"text":"70224597 - 1969 - The ground-water situation in Ohio","interactions":[],"lastModifiedDate":"2021-09-29T15:41:00.579479","indexId":"70224597","displayToPublicDate":"1969-09-01T10:35:01","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3825,"text":"Groundwater","active":true,"publicationSubtype":{"id":10}},"title":"The ground-water situation in Ohio","docAbstract":"

Present ground-water use in Ohio, approximately 650mgd (million gallons per day) amounts to about 5 percent of the water that enters the ground-water reservoirs. The largest ground-water supplies are developed where natural concentrations of water occur, chiefly in the watercourse aquifers, which consist of sand and gravel of glacial origin (outwash) in the valleys of the major streams. Other important aquifers are glacial outwash in upland areas and in the buried Teays Valley system, the limestone and dolomite aquifers in western Ohio, and sandstone and shale aquifers in the eastern half of the State.

Future outlook is that more of the increasing water demand will be met from ground-water sources. Ground-water supplies will be developed at many new sites, and aquifers in areas already heavily pumped will be made to yield more water by the drilling of additional wells and recharging the aquifers artificially. Large quantities of ground water in storage, virtually unexploited, could be used for temporary low-flow augmentation of streams. Management of ground-water resources will be needed to help solve supply and distribution problems, and to resolve conflicts between users. Among future problems will be those arising from underground disposal of wastes, a practice which is expected to grow substantially from enforcement of water-quality standards for streams, set under the Federal Water Quality Act of 1965.

","language":"English","publisher":"National Ground Water Association","doi":"10.1111/j.1745-6584.1969.tb01294.x","usgsCitation":"Norris, S., 1969, The ground-water situation in Ohio: Groundwater, v. 7, no. 5, p. 25-33, https://doi.org/10.1111/j.1745-6584.1969.tb01294.x.","productDescription":"9 p.","startPage":"25","endPage":"33","costCenters":[],"links":[{"id":389963,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United 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\"}}]}","volume":"7","issue":"5","noUsgsAuthors":false,"publicationDate":"2006-07-06","publicationStatus":"PW","contributors":{"authors":[{"text":"Norris, Stanley E.","contributorId":63844,"corporation":false,"usgs":true,"family":"Norris","given":"Stanley E.","affiliations":[],"preferred":false,"id":824239,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70225040,"text":"70225040 - 1969 - Aeromagnetic investigation of crustal structure for a strip across the western United States","interactions":[],"lastModifiedDate":"2021-10-13T15:28:52.927166","indexId":"70225040","displayToPublicDate":"1969-09-01T09:46:26","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Aeromagnetic investigation of crustal structure for a strip across the western United States","docAbstract":"

This report represents part of a larger study undertaken to interpret the gross features of the earth's crust by aeromagnetic methods. The larger survey covers a 100-mile-wide strip along a great circle arc from Washington, D.C., to San Francisco, California. The area considered extends from about 200 miles east of the Rocky Mountains to 150 miles west of the coast of the Pacific Ocean. Inferences on gross structure and lithology are made from the magnetic patterns and trends shown on the map.

At the continental margin, the magnetic data strongly suggest that the oceanic crust becomes much more deeply buried as the continent is approached.

A large magnetic anomaly extending northwestward along the center of the Great Valley is probably caused by mafic intrusive rocks.

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1969)80[1703:AIOCSF]2.0.CO;2","usgsCitation":"Zietz, I., Bateman, P.C., Case, J.E., Crittenden, M.D., Griscom, A., King, E.R., Roberts, R., and Lorentzen, G.R., 1969, Aeromagnetic investigation of crustal structure for a strip across the western United States: Geological Society of America Bulletin, v. 80, no. 9, p. 1703-1714, https://doi.org/10.1130/0016-7606(1969)80[1703:AIOCSF]2.0.CO;2.","productDescription":"13 p.","startPage":"1703","endPage":"1714","costCenters":[],"links":[{"id":390468,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California, Colorado, Kansas, Nebraska, Nevada, Utah, Wyoming","otherGeospatial":"Cedar Mountains, Colorado Plateau, Front Range, Great Plains, Great Salt Lake Desert, Kern Mountains, Laramie Range, Medicine Bow Range, Oquirrh Mountains, Park Range, Rocky Mountains, Sheeprock Mountains, Sierra Nevada, Stansbury Mountains, Tintic Mountains, Uinta Mountains, Wasatch Mountains","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -124.38720703124999,\n 40.16208338164617\n ],\n [\n -123.94775390625,\n 39.70718665682654\n ],\n [\n -124.01367187499999,\n 39.35129035526705\n ],\n [\n -123.85986328124999,\n 38.736946065676\n ],\n [\n -120.58593749999999,\n 34.252676117101515\n ],\n [\n -114.01611328125,\n 37.03763967977139\n ],\n [\n -101.3818359375,\n 37.00255267215955\n ],\n [\n -96.21826171874999,\n 37.00255267215955\n ],\n [\n -99.49218749999999,\n 42.98857645832184\n ],\n [\n -111.02783203125,\n 42.01665183556825\n ],\n [\n -120.21240234375001,\n 41.96765920367816\n ],\n [\n -124.38720703124999,\n 40.16208338164617\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"80","issue":"9","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Zietz, Isidore","contributorId":76708,"corporation":false,"usgs":true,"family":"Zietz","given":"Isidore","affiliations":[],"preferred":false,"id":825133,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bateman, Paul C.","contributorId":18377,"corporation":false,"usgs":true,"family":"Bateman","given":"Paul","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":825134,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Case, James E.","contributorId":68702,"corporation":false,"usgs":true,"family":"Case","given":"James","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":825135,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Crittenden, M. D. Jr.","contributorId":43421,"corporation":false,"usgs":true,"family":"Crittenden","given":"M.","suffix":"Jr.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":825136,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Griscom, Andrew","contributorId":23520,"corporation":false,"usgs":true,"family":"Griscom","given":"Andrew","email":"","affiliations":[],"preferred":false,"id":825137,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"King, Elizabeth R.","contributorId":40990,"corporation":false,"usgs":true,"family":"King","given":"Elizabeth","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":825138,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Roberts, R. J.","contributorId":267486,"corporation":false,"usgs":false,"family":"Roberts","given":"R. J.","affiliations":[],"preferred":false,"id":825139,"contributorType":{"id":1,"text":"Authors"},"rank":7},{"text":"Lorentzen, George R.","contributorId":267487,"corporation":false,"usgs":false,"family":"Lorentzen","given":"George","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":825140,"contributorType":{"id":1,"text":"Authors"},"rank":8}]}} ,{"id":70223878,"text":"70223878 - 1969 - Cretaceous, Tertiary, and early Pleistocene rocks from the continental margin in the Bering Sea","interactions":[],"lastModifiedDate":"2021-09-10T21:03:56.525131","indexId":"70223878","displayToPublicDate":"1969-08-01T15:45:29","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Cretaceous, Tertiary, and early Pleistocene rocks from the continental margin in the Bering Sea","docAbstract":"

Rocks dredged from the continental margin in eastern Bering Sea in and near the Pribilof Canyon indicate that the acoustic basement represents the upper surface of thoroughly lithified turbidite beds of graywacke and siltstone of Late Cretaceous age. The stratified sequence covering the acoustic basement is gently deformed and includes marine clastic and diatomaceous sediments ranging in age from middle or late Miocene through early Pleistocene. Dense argillite, siltstone, and calcareous sandstone of early Tertiary age in and near the Zhemchug Canyon probably represent an older part of this sequence. The main layered sequence accumulated above the acoustic basement in shallow water, and, because the older beds now lie as much as 1000 m below sea level, the continental margin must have undergone considerable subsidence during late Tertiary and Quaternary time. A rich pollen flora indicates that the shoreline lay only a few tens of kilometers away from the site of the Pribilof Canyon during late Miocene time.

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1969)80[1471:CTAEPR]2.0.CO;2","usgsCitation":"Hopkins, D., Scholl, D.W., Addicott, W.O., Pierce, R.L., Smith, P.B., Wolfe, J.A., Gershanovich, D., Kotenev, B., Lohman, K.E., Lipps, J.H., and Obradovich, J.D., 1969, Cretaceous, Tertiary, and early Pleistocene rocks from the continental margin in the Bering Sea: Geological Society of America Bulletin, v. 80, no. 8, p. 1471-1480, https://doi.org/10.1130/0016-7606(1969)80[1471:CTAEPR]2.0.CO;2.","productDescription":"12 p.","startPage":"1471","endPage":"1480","costCenters":[],"links":[{"id":389121,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"Bering Sea, Pribilof Canyon, Zhemchug Canyon","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -174.517822265625,\n 54.99022172004893\n ],\n [\n -164.520263671875,\n 54.99022172004893\n ],\n [\n -164.520263671875,\n 58.21123794344608\n ],\n [\n -174.517822265625,\n 58.21123794344608\n ],\n [\n -174.517822265625,\n 54.99022172004893\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"80","issue":"8","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Hopkins, David M.","contributorId":37409,"corporation":false,"usgs":true,"family":"Hopkins","given":"David M.","affiliations":[],"preferred":false,"id":823057,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Scholl, David W. 0000-0001-6500-6962 dscholl@usgs.gov","orcid":"https://orcid.org/0000-0001-6500-6962","contributorId":3738,"corporation":false,"usgs":true,"family":"Scholl","given":"David","email":"dscholl@usgs.gov","middleInitial":"W.","affiliations":[{"id":186,"text":"Coastal and Marine Geology Program","active":true,"usgs":true},{"id":520,"text":"Pacific Coastal and Marine Science Center","active":true,"usgs":true}],"preferred":true,"id":823058,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Addicott, Warren O.","contributorId":80668,"corporation":false,"usgs":true,"family":"Addicott","given":"Warren","email":"","middleInitial":"O.","affiliations":[],"preferred":false,"id":823059,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Pierce, Richard L.","contributorId":265588,"corporation":false,"usgs":false,"family":"Pierce","given":"Richard","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":823060,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Smith, Patsy Beckstead","contributorId":69135,"corporation":false,"usgs":true,"family":"Smith","given":"Patsy","email":"","middleInitial":"Beckstead","affiliations":[],"preferred":false,"id":823061,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Wolfe, Jack A.","contributorId":102474,"corporation":false,"usgs":true,"family":"Wolfe","given":"Jack","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":823062,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Gershanovich, David","contributorId":265589,"corporation":false,"usgs":false,"family":"Gershanovich","given":"David","email":"","affiliations":[],"preferred":false,"id":823063,"contributorType":{"id":1,"text":"Authors"},"rank":7},{"text":"Kotenev, Boris","contributorId":265590,"corporation":false,"usgs":false,"family":"Kotenev","given":"Boris","email":"","affiliations":[],"preferred":false,"id":823064,"contributorType":{"id":1,"text":"Authors"},"rank":8},{"text":"Lohman, Kenneth E.","contributorId":265591,"corporation":false,"usgs":false,"family":"Lohman","given":"Kenneth","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":823065,"contributorType":{"id":1,"text":"Authors"},"rank":9},{"text":"Lipps, Jere H.","contributorId":174189,"corporation":false,"usgs":false,"family":"Lipps","given":"Jere","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":823066,"contributorType":{"id":1,"text":"Authors"},"rank":10},{"text":"Obradovich, John D.","contributorId":84361,"corporation":false,"usgs":true,"family":"Obradovich","given":"John","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":823067,"contributorType":{"id":1,"text":"Authors"},"rank":11}]}} ]}