An investigation begun in 1937 by the United States and the Oklahoma Geological Surveys, has shown that the depth to the water table in the Oklahoma Panhandle ranges from less than 25 feet in parts of major valleys to about 3oo feet in parts of the uplands. In 8 upland areas the depth is between 50 and 100 feet. The thi kness of the zone of saturation differs widely in these areas, the most promising of which totals about 80 square miles in northeastern Texas County. The pervious sands and gravels of the Ogallala formation, of Pliocene age, furnish most of the ground water, and one well yielding 960 gallons a minute from them has been used for irrigation since x937. The formation ranges from less than xoo to more than 500 feet thick, the differences being due to relief on the pre-Ogallala topography and to post-Ogallala erosion. The alluvium is also an important source of water, as are the Dakota and Cheyenne sandstones, of Cretaceous age. A few wells yield water of variable quality from Jurassic and Triassic rocks, and many wells in the valleys of the eastern part of the area yield small supplies of highly mineralized water from Permian red beds. © 1940 Society of Economic Geologists, Inc
","language":"English","publisher":"Society of Economic Geologists ","doi":"10.2113/gsecongeo.35.4.534","issn":"03610128","usgsCitation":"Schoff, S., 1940, Ground water in the Oklahoma Panhandle: Economic Geology, v. 35, no. 4, p. 534-545, https://doi.org/10.2113/gsecongeo.35.4.534.","productDescription":"12 p. ","startPage":"534","endPage":"545","costCenters":[],"links":[{"id":370293,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States ","state":"Oklahoma","otherGeospatial":"Panhandle ","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-100.9441,36.9988],[-100.6337,36.9986],[-100.1079,36.9983],[-100.0902,36.9983],[-100.0024,36.9985],[-100.004,36.8538],[-100.0044,36.76],[-100.0045,36.5917],[-100.0044,36.5849],[-100.0038,36.4998],[-100.1458,36.4998],[-100.3204,36.4999],[-100.5459,36.4994],[-100.7022,36.5],[-100.8939,36.4998],[-100.9524,36.4998],[-101.0908,36.5003],[-101.6255,36.5025],[-101.87,36.5034],[-102.1618,36.5004],[-103.0007,36.5013],[-103.0007,36.5905],[-103.0007,36.6732],[-103.0007,36.7643],[-103.0008,36.9341],[-103.0009,36.999],[-102.7973,36.9988],[-102.7859,36.9988],[-102.7808,36.9986],[-102.7016,36.9958],[-102.6943,36.9957],[-102.6757,36.9956],[-102.5627,36.9962],[-102.5372,36.9963],[-102.5034,36.9963],[-102.4775,36.9963],[-102.4577,36.9961],[-102.3931,36.9955],[-102.351,36.9951],[-102.3247,36.9948],[-102.0423,36.9922],[-102.0417,36.9922],[-102.0281,36.9925],[-101.9881,36.9925],[-101.918,36.9929],[-101.5552,36.9951],[-101.544,36.9952],[-101.2679,36.9967],[-101.0671,36.9978],[-100.9536,36.9988],[-100.9441,36.9988]]]},\"properties\":{\"name\":\"Beaver\",\"state\":\"OK\"}}]}","volume":"35","issue":"4","noUsgsAuthors":false,"publicationDate":"1940-06-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Schoff, S.L.","contributorId":107365,"corporation":false,"usgs":true,"family":"Schoff","given":"S.L.","email":"","affiliations":[],"preferred":false,"id":777542,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70161774,"text":"70161774 - 1940 - Geology and ground-water resources of the islands of Lanai and Kahoolawe, Hawaii","interactions":[],"lastModifiedDate":"2016-01-06T10:46:49","indexId":"70161774","displayToPublicDate":"1940-01-01T10:30:00","publicationYear":"1940","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":4,"text":"Other Government Series"},"seriesTitle":{"id":242,"text":"Bulletin","active":false,"publicationSubtype":{"id":4}},"seriesNumber":"6","title":"Geology and ground-water resources of the islands of Lanai and Kahoolawe, Hawaii","docAbstract":"Lanai lies 59 miles southeast of Honolulu, Oahu, has an area of 141 square miles, and is 3,370 feet high. (See fig. 1 and pl. 1.) Lanai City is the only town of importance. The island produces pineapples and cattle. The surface above about 1,200 feet is generally covered with lateritic soil, which reaches a maximum depth of about 50 feet. Below this level the island is partly devoid of vegetation and is strewn with boulders, the result of having been once submerged by the ocean to this depth. Traces of various emerged and submerged shore lines are described, the highest fossiliferous marine deposits being 1,070 feet above sea level. Lanai is an eroded extinct basaltic volcano built during one period of activity. No secondary eruptions occurred as on most of the other islands. It has three rift zones and a summit caldera. The summit plateau has resulted from collapse along the northwest rift zone. Elsewhere there is much evidence of faulting. About 100 faults and 275 dikes were recorded, but they are so close together in places that it was not possible to show them all on the map.
The climate is semitropical, the mean annual temperature of Lanai City, altitude 1,620 feet, being 68° F. Because Lanai lies to the lee of Maui Island it is dry. The mean annual rainfall ranges from 38 inches on the summit to less than 10 inches on the coast. The windward (northeast) side is carved by streams into deep canyons. Maunalei Gulch has the only perennial stream, and it does not reach the sea. Ground water, the lifeblood of Lanai is scarce. Lanai City obtains some of its water supply by a tunnel from gravel in Maumalei Gulch. This water apparently rises from the dike complex in this gulch. The rest of the supply comes from a recently constructed shaft tapping the dike complex not far downstream. The total quantity of high-level ground water discharged by springs and tunnels ranges from about 600,000 gallons a day in wet weather to about 250,000 gallons a day in dry weather. The basal water, although potable, is fairly high in salt. Several sites are recommended for developing and conserving ground water.
Kahoolawe Island is 11 miles long, 6 miles wide, 1,491 feet high, covers 45 square miles, and lies 94 miles southeast of Honolulu and 6 3/4 miles southwest of Maui. It is a shield-shaped extinct volcano composed chiefly of thin flows of primitive basalt poured in rapid succession from three rift zones and a vent at their intersection. At one stage the volcano was indented with a caldera about 3 miles across which was later completely filled. A graben led southwestward from it. The rocks are divided into Late Tertiary (?) or early Pleistocene(?) pre-caldera basalts, caldera-filling basalts and basaltic andesites, post-caldera basalts and andesites, and Recent post erosional basalts. A few thin vitric tuff beds and cinder cones were found. Marine erosion has cut cliffs as high as 800 feet along the east and south shores and exposed a cross section of the caldera. Only shallow ephemeral gulches exist. The entire summit has been eroded to a hard-pan surface by the wind as a result of the vegetation being destroyed by livestock.
The island is semi-arid and well water is needed for stook: \"The stook is now supplied entirely from storage of rain and flood waters. During droughts water is hauled by boat from the island of Maui. All the wells dug so far yield water that is too brackish for stock except at the fairly inaccessible south side of Kanapou Bay. The resistivity survey indicates a water table 1.5 feet or less above sea level for 2.25 miles inland. A few sites for wells are recommended in the dike complex where small supplies of water suitable for stock might be found.
Petrographic studies by Gordon A. Macdonald indicate that the pre-caldera and caldera-filling lavas are largely normal olivine basalt of the type which forms the bulk of all Hawaiian volcanoes thus far investigated. It represents the undifferentiated magma of the Hawaiian petrographic province. Toward the close of the caldera-filling epoch the vent became less active, and magmatic differentiation produced basaltic andesites, which are interbedded with normal basalts. The post-caldera lavas are largely basaltic andesites and andesites. The much younger lavas, erupted after a period of extensive erosion, are olivine basalts similar in composition to the pre-caldera flows. The mineralogy of the Kahoolawe rocks is described in detail.
Special Chapters:
\nA total of 2,902 Lake Michigan fish was tagged and released, 48.8 per cent of which were lake trout and 85 per cent lake trout, lake herring, and whitefish. A total of 388 fish or 13.4 per cent was recaptured. The percentages of returns indicated a tremendous fishing intensity for lake trout, whitefish, and sturgeon. About 81 per cent of the recaptured fish were retaken within a radius of 25 miles from the port of tagging (Port Washington, Wisconsin). Lake trout, rainbow trout, and sturgeon were found to be extensive travelers; lake herring, whitefish, chubs, pilots, and perhaps perch did not migrate so extensively. Lake trout, herring, and whitefish tended to move in a northerly direction, perch in a southerly, and rainbow trout in all easterly, toward the Michigan shore. Sturgeon apparently roam all over the lake. Fifty-three per cent of the recovered lake trout were recaptured within one year of release, 73 per cent within 25 miles from Port Washington. It required three years for the trout to become fairly well scattered throughout the lake. With the attainment of adulthood lake trout moved in all directions from the port of release, although nearly 50 per cent of the adults were retaken within 25 miles from this port. Fish moved across state boundaries. Data are given on the growth and estimated age of the tagged lake trout, rainbow trout, whitefish, and sturgeon. The minimum size limits of lake trout and whitefish on the Great Lakes are economically unsound–they are too low–because they permit the capture of these species at a time of most rapid increase in weight.
","language":"English","publisher":"Taylor & Francis","doi":"10.1577/1548-8659(1939)69[63:TEWLTW]2.0.CO;2","usgsCitation":"Smith, O.H., and Van Oosten, J., 1940, Tagging experiments with lake trout, whitefish, and other species of fish from Lake Michigan: Transactions of the American Fisheries Society, v. 69, no. 1, p. 63-84, https://doi.org/10.1577/1548-8659(1939)69[63:TEWLTW]2.0.CO;2.","productDescription":"22 p.","startPage":"63","endPage":"84","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":324,"text":"Great Lakes Science Center","active":true,"usgs":true}],"links":[{"id":129185,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"69","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afee4b07f02db697664","contributors":{"authors":[{"text":"Smith, Oliver H.","contributorId":107648,"corporation":false,"usgs":true,"family":"Smith","given":"Oliver","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":308474,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Van Oosten, John","contributorId":23479,"corporation":false,"usgs":true,"family":"Van Oosten","given":"John","email":"","affiliations":[],"preferred":false,"id":308473,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":35448,"text":"b922N - 1940 - Chromite deposits of the eastern part of the Stillwater complex, Stillwater County, Montana","interactions":[{"subject":{"id":55442,"text":"ofr4321 - 1943 - Chromite deposits in the Stillwater complex, Montana","indexId":"ofr4321","publicationYear":"1943","noYear":false,"title":"Chromite deposits in the Stillwater complex, Montana"},"predicate":"SUPERSEDED_BY","object":{"id":35448,"text":"b922N - 1940 - Chromite deposits of the eastern part of the Stillwater complex, Stillwater County, Montana","indexId":"b922N","publicationYear":"1940","noYear":false,"chapter":"N","title":"Chromite deposits of the eastern part of the Stillwater complex, Stillwater County, Montana"},"id":1}],"lastModifiedDate":"2023-01-06T12:07:53.00597","indexId":"b922N","displayToPublicDate":"1940-01-01T00:00:00","publicationYear":"1940","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":"922","chapter":"N","title":"Chromite deposits of the eastern part of the Stillwater complex, Stillwater County, Montana","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/b922N","usgsCitation":"Peoples, J.W., and Howland, A.L., 1940, Chromite deposits of the eastern part of the Stillwater complex, Stillwater County, Montana: U.S. Geological Survey Bulletin 922, Report: 52 p.; 1 Plate: 36.88 × 14.99 inches, https://doi.org/10.3133/b922N.","productDescription":"Report: 52 p.; 1 Plate: 36.88 × 14.99 inches","costCenters":[],"links":[{"id":93331,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/0922n/plate-64.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":93333,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/0922n/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":167113,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/0922n/report-thumb.jpg"}],"country":"United States","state":"Montana","county":"Stillwater County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-108.9239,46.1328],[-108.924,46.0476],[-108.9208,45.961],[-108.9005,45.9613],[-108.9002,45.7842],[-108.9034,45.7842],[-108.9052,45.6831],[-108.885,45.6829],[-108.8844,45.6536],[-108.8642,45.6534],[-108.8639,45.6392],[-108.8417,45.6394],[-108.8431,45.611],[-108.8606,45.6145],[-108.8679,45.6086],[-108.8823,45.6051],[-108.8921,45.6052],[-108.9032,45.6031],[-108.9181,45.6065],[-108.9337,45.6048],[-108.9518,45.611],[-108.9758,45.6163],[-108.9851,45.6091],[-109.0092,45.6093],[-109.0197,45.603],[-109.0415,45.5905],[-109.0723,45.5816],[-109.0865,45.5841],[-109.1074,45.5834],[-109.1229,45.5881],[-109.1274,45.5891],[-109.1288,45.5228],[-109.1893,45.5229],[-109.1904,45.464],[-109.3548,45.4627],[-109.3551,45.449],[-109.4161,45.4486],[-109.4157,45.4345],[-109.4332,45.4346],[-109.4335,45.4186],[-109.4789,45.418],[-109.4805,45.4025],[-109.5006,45.4027],[-109.5014,45.3903],[-109.5189,45.3904],[-109.5198,45.3758],[-109.5425,45.3764],[-109.5434,45.3605],[-109.559,45.3601],[-109.5591,45.3469],[-109.5643,45.3474],[-109.5652,45.3314],[-109.5872,45.332],[-109.587,45.3046],[-109.6058,45.3038],[-109.6072,45.2896],[-109.6069,45.2686],[-109.607,45.2613],[-109.6549,45.2612],[-109.6797,45.2472],[-109.6875,45.2444],[-109.6904,45.1668],[-109.7977,45.1665],[-109.7977,45.1729],[-110.059,45.1758],[-110.0565,45.3476],[-109.9314,45.3471],[-109.9305,45.3727],[-109.9314,45.4198],[-109.9317,45.4646],[-109.9318,45.5222],[-109.8057,45.5216],[-109.8053,45.5645],[-109.683,45.5643],[-109.6824,45.6087],[-109.5574,45.6088],[-109.5594,45.6952],[-109.5628,45.7826],[-109.5471,45.7829],[-109.5472,45.8708],[-109.5073,45.8714],[-109.5073,45.9602],[-109.4222,45.96],[-109.4215,46.0447],[-109.4201,46.1312],[-109.4036,46.1324],[-109.2927,46.132],[-109.275,46.1323],[-108.9239,46.1328]]]},\"properties\":{\"name\":\"Stillwater\",\"state\":\"MT\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49dbe4b07f02db5e0f93","contributors":{"authors":[{"text":"Peoples, Joe Webb","contributorId":78343,"corporation":false,"usgs":true,"family":"Peoples","given":"Joe","email":"","middleInitial":"Webb","affiliations":[],"preferred":false,"id":214656,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Howland, Arthur Lloyd","contributorId":75606,"corporation":false,"usgs":true,"family":"Howland","given":"Arthur","email":"","middleInitial":"Lloyd","affiliations":[],"preferred":false,"id":214655,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1238,"text":"wsp842 - 1939 - Floods in the Canadian and Pecos River basins of New Mexico, May and June 1937","interactions":[],"lastModifiedDate":"2022-01-31T22:12:44.831439","indexId":"wsp842","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1939","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":"842","title":"Floods in the Canadian and Pecos River basins of New Mexico, May and June 1937","docAbstract":"In May and June floods occurred in the Canadian and Pecos River Basins of New Mexico that were unusually high and in many places were record breaking. \r\n\r\nThe floods were caused by heavy rains that occurred over the eastern part of the State from May 23 to June 4 in a series of intense and intermittent storms. During these storms of the cloudburst type as much as 12 inches of rain fell in the 13-day period, and a fall of 7 inches in 2 hours and 40 minutes was reported from the vicinity of Clayton. Heavy rains also fell in the mountainous region west of Roswell, amounting to as much as l0 inches at some places. Much of the region that had excessive rainfall is relatively flat and has no well-defined drainage system. From these areas there was very little run-off and practically no water was contributed to the major streams. \r\n\r\nHail fell at many places in eastern New Mexico, causing damage to crops, livestock, and other property. Hail fell somewhere in the Canadian and Pecos River Basins almost every day during the storm period, but the duration of the fall was generally short. The largest hailstones were reported from Clayton, where one stone measured 8 inches in circumference and weighed 9 ounces; at Centerville, where reports state that some stones were 9 to 10 inches in circumference; and near Roswell, where it was reported that six stones would fill a gallon bucket. The Canadian River flood reached a peak at Logan of 110,000 second-feet, which has been exceeded in this century only by the floods of 1904, 1909, and 1914. The total run-off at Logan for the flood period has been computed as 653,800 acre-feet. \r\n\r\nAt Santa Rosa the Pecos River reached a maximum discharge of 88,200 second-feet, which is greater than any previously recorded. This flood was partly stored in the Alamogordo Reservoir; the peak below the reservoir was only 25,200 second-feet. \r\n\r\nThe Pecos River flood at Roswell reached a maximum discharge of more than 80,000 second-feet. This water came mostly from tributaries that have .their sources in the mountainous area west of Roswell. The Cienaga del Macho, ordinarily a small dry creek, discharged about 49,800 second-feet at its peak. The Rio Hondo experienced several flood peaks, the largest at Roswell probably being near 20,000 second-feet. Berrendo Creek, which enters the Rio Hondo near Roswell, had a computed peak discharge of 37,700 second-feet. \r\n\r\nRoswell was subjected to several floods that inundated large areas of the town. Considerable damage was done by the water, which covered nearly all the area occupied by the town. \r\n\r\nLake McMillan, an artificial reservoir on the Pecos River about 12 miles above Carlsbad, was put to a severe strain by the large quantity of water passing through it, but no serious damage resulted. The capacity of the lake at spillway level is about 39,000 acre-feet, but at the peak of the flood the lake held about 86,000 acre-feet. The total quantity of water passing through the lake during the flood period was more than 440,000 acre-feet. \r\n\r\nThis report presents data pertinent to the floods of May and June 1937, including results of peak discharge determinations made at about 14 miscellaneous places, records of peak stages and discharges and of mean daily discharges during the flood period at 23 regular river-measurement stations, records of rainfall at about 190 places, an isohyetal map showing rainfall over the entire State and two isohyetal maps showing rainfall over the Canadian and Pecos River Basins, and a discussion of the weather conditions during the flood period, including an upper-air wind and pressure chart of the United States for May 28, 1937. In addition to the information listed above the report includes a summary of records of past floods at all places in New Mexico at which authentic records were available.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp842","usgsCitation":"Dalrymple, T., 1939, Floods in the Canadian and Pecos River basins of New Mexico, May and June 1937: U.S. Geological Survey Water Supply Paper 842, iv, 68 p., https://doi.org/10.3133/wsp842.","productDescription":"iv, 68 p.","costCenters":[],"links":[{"id":395197,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24657.htm"},{"id":26167,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/0842/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138090,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/0842/report-thumb.jpg"}],"country":"United States","state":"New Mexico","otherGeospatial":"Canadian and Pecos River basins","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -109,\n 32\n ],\n [\n -103,\n 32\n ],\n [\n -103,\n 37\n ],\n [\n -109,\n 37\n ],\n [\n -109,\n 32\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b28e4b07f02db6b1170","contributors":{"authors":[{"text":"Dalrymple, Tate","contributorId":59420,"corporation":false,"usgs":true,"family":"Dalrymple","given":"Tate","email":"","affiliations":[],"preferred":false,"id":143423,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2501,"text":"wsp780 - 1939 - Geology and ground-water hydrology of the Mokelumne area, California","interactions":[],"lastModifiedDate":"2018-12-17T09:45:46","indexId":"wsp780","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1939","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":"780","title":"Geology and ground-water hydrology of the Mokelumne area, California","docAbstract":"The Mokelumne River basin of central California comprises portions of the \nCalifornia Trough and the Sierra Nevada section of the Pacific Mountain system. \nThe California Trough is divisible into four subsections-the Delta tidal plain, \nthe Victor alluvial plain, tlie river flood plains and channels, and the Arroyo Seco \ndissected pediment. These four subsections comprise the land forms produced \nby the Mokelumne River and other streams since the Sierra Nevada attained its \npresent height in the Pleistocene epoch. \nThe Victor alluvial plain rises eastward from the Delta plain and abuts on the \ndissected Arroyo Seco pediment; in the Mokelumne area it is 12 to 16 miles wide \nand slopes between 5 and 8 feet in a mile. It includes relatively extensive tracts \nthat are intensively cultivated and irrigated with water pumped from wells. The \nVictor plain has been compounded of overlapping alluvial fans along the western \nbase of the Sierra Nevada. It is prolonged eastward into the pediment by tongues \nof alluvium along several of the present streams; thus it seems likely that the \npresent stream pattern in the eastern part of the area has been fixed since dissection of the pediment began. \nThree of the four major streams-the Mokelumne and Cosumnes Rivers and \nDry Creek-traverse the Victor plain in trenches which are 15 to 40 feet deep \nat the heads of their respective alluvial fans but which die out toward the west. \nThe floors of these trenches, the historic flood plains, are from 100 yards to a mile \nwide. The exceptional major stream, which has not entrenched itself, is the \nCalaveras River. \nThe Arroyo Seco pediment, which lies east of the Victor plain, was initially at \nleast 8 to 15 miles wide and lay along the western foot of the Sierra Nevada entirely \n.across the Mokelumne area. Its numerous remnants decline 15 to 35 feet in a \nmile toward the west. \nThe Sierra Nevada section adjoins and lies east of the California Trough. Its \nmajor ridge crests define a volcanic plain whose westward slope is' inferred to have \nbeen initially about 90 feet in a mile but is now about 180 feet in a mile, owing to \ntilting of the Sierra Nevada block in Pleistocene time. \nIn and near the Mokelumne area the Sierra Nevada and California Trough \ntogether are roughly coextensive with a single structural unit. The Sierra \nNevada constitutes a block that has risen with respect to adjoini;ng valley areas \n'by simple rotation or tilting toward the west; it has not been warped or faulted \n-extensively. It is inferred that this block extends westward beneath the thick \nalluvial deposits of the trough without material warping or faulting. \nThe oldest rocks of the Mokelumne region are the Carboniferous and Jurassic \n-rocks that compose the crystalline core of the Sierra Nevada. These are overlain \nunconformably by sediments of Tertiary age--in upward succession the lone, \nValley Springs, Mehrten, and J.Jaguna formations. Of these formations all except \nthe lone are newly discriminated, and type sections are described in the full text. \nThese Tertiary sediments form a great wedge, thinnest along the mountain front \nto the east, where they have been truncated by erosion. They dip about 2° W. \nThe lone formation (Eocene) consists chiefly of sandstone, clay, and shale; its \nmaximum thickness is 450 feet. \nThe Valley Springs formation (middle? Miocene) overlies the lone formation \nunconformably. It is composed largely of greenish-gray clay, shale, and sandstone derived from rhyolitic ejectamenta. These rhyolitic deposits are confined \nto narrow channels in the higher part of the Sierra Nevada, but they \nspread fanlike over the lower western edge of the mountain block, where they \nattain a maximum thickness of 525 feet. \nThe Mehrten formation (upper? Miocene and lower Pliocene?) comprises the \nandesitic rocks that constructed the Sierran volcanic plain. In the Mokelumne \narea it consists chiefly of sandstone and siltstone but includes, as a minor though \nconspicuous part of the formation, layers and tongues of resistant breccia or agglomerate, which are presumed to have originated as mud flows. Nonfragmental \nandesite is not known to occur in the Mokelumne area, although several possible \nvents occur farther east. In the eastern part of the area the Mehrten formation \ntruncates in turn the Valley Springs and lone formations and the pre-Cretaceous \nrocks; in the western part the Mehrten formation (andesitic) interfingers with the \nunderlying Valley Springs formation (rhyolitic). Its maximum measured thickness is 400 feet. Few of the irrigation wells are so deep that they can be said \nwith assurance to reach the Mehrten formation. \nThe Laguna formation (Pliocene? and possibly lower Pleistocene) comprises \npoorly sorted, nonandesitic fluviatile sedimentary that overlie the \nMehrten formation. It is inferred to be essentially parallel to and tilted equally \nwith the Mehrten formation and to be about 400 feet thick. \nThe Arroyo Seco gravel (presumably middle Pleistocene) veneers the Arroyo \nSeco pediment. At its easternmost outcrops the formation is composed of \npebbles, cobbles, and boulders in a matrix of brick-red sand and silt; farther west, \ndown the slope of the pediment, it becomes pr9gressively finer. It is inferred \nthat the Arroyo Seco gravel is a coarse fraction of the rock waste that was transported from the Sierra Nevada after the Sierran.block was tilted in Pleistocene \ntime. It is inferred further that the correlative of the Arroyo Seco gravel in the \nCalifornia Trough is a wedge-shaped mass of sediments whose base is the \ntilted Laguna formation and whose top can be interpolated by projecting a \nhypothetical surface through the remnants of the pediment. \nThe Victor formation comprises the fluviatile sand, silt, and gravel that built \nthe Victor alluvial plain over the hypothetical equivalent of the Arroyo' Seco \ngravel along the axis of the California Trough and against the western front of \nthe dissected pediment to the east. The formation is thought to be about 100 \nfeet thick along the western margin of the Mokelumne area, according to an \nestimate based upon projecting the slope of the Arroyo Seco pediment westward \nbeneath the Victor plain. \nThe Mokelumne area lies on the fertile central plain along the Mokelumne \nRiver about the city of Lodi, in northern San Joaquin County, and has been \nintensively developed for the cultivation of grapes, deciduous fruits, and other \ncrops. Of necessity its great productiveness is maintained by irrigation. Extensive irrigation from wells began about 1907 and has increased steadily until in \n1932 about 50,000 acres (80 percent of the area) was watered in that manner. \nThe specific question at issue is the extent to which the supply of ground water \nand hence the productiveness of the area are dependent upon the water flowing \nin the Mokelumne River and the extent to which that productiveness may be \ninfluenced by regulation of the stream--:in particular, by the substantial regulation of the river that is accomplished by the Pardee Dam of the East Bay Municipal Utility District, which began to function in March 1929. \nThe depth of 1,447 irrigation wells in five townships in the central part of the \narea (T. 3 N., Rs. 6 and 7 E., and T. 4 N., Rs. 6 to 8 E.) ranges from 20 to 910 \nfeet. About half the wells bottom within a 100-foot zone whose base is 75 feet \nbelow the projected Arroyo Seco pediment; essentially that zone constitutes the \nVictor formation. Only 6 percent of the wells bottom within the next lower 25-\nfoot zone, but the percentage increases sharply for depths still greater; it is inferred \nthat impervious strata are relatively persistent between 75 and 100 feet below \nthe projected pediment and that these are the uppermost part of the Arroyo Seco \ngravel. Of 580 observation wells known to bottom in the Victor formation, essentially all appear to indicate a regional water-table stage; thus the water is essentially unconfined. On the other hand, nearly all wells so deep that they reach the \nArroyo Seco gravel or some underlying formation tap confined water. Near the \nMokelumne River the water levels in these deep wells stand below the water \ntable, which is semiperched. In most deep wells remote from the river the water \nlevel stands above the water table except during the pumping season. \nFluctuations of ground-water levels are ascribed to moving or changing load on \nthe land surface, earthquakes, variation of barometic pressure, ground-water \ndraft by vegetation, infiltration of rain and certain indirect effects of rainfall, infiltration of water applied to the land for irrigation, variation in the discharge of \nstreams, and pumping from wells. \nIn the eastern part of the central district, between Clements and the vicinity of \nLockeford, it is inferred that (1) the river and the water in the alluvium of the \nflood plain are not insulated from the water in the sediments that form the adjacent Victor plain; (2) locally if not generally, however, there are discontinuities \nin pervious strata along the outer margin of the flood plain, where the water table \npasses from the alluvium into the enclosing sediments, so that percolation of \nground water is impeded materially at that margin; (3) rising river stages set up \nground-water waves that store relatively large volumes of water in the alluvium \nclose to the river, whereas falling stages cause much of that stored water to percolate back into the river, weeks and even months lapsing before the ground-water \nstage becomes steady within the flood plain; and (4) seepage loss from the river \ninto the alluvium tends to be intermittent and to alternate with seepage gain, the \nrate of loss or gain lagging weeks or months behind the fluctuations of river stage \nand lagging more for moderate changes at low stage. However, in the succeeding \nreach downstream as far as Woodbridge, it is inferred that percolation of ground \nwater is not impeded generally along the outer margin of the flood plain and that \nthe river tends to lose almost continuously by seepage rather than intermittently, \nalthough the rate of loss fluctuates somewhat in response to changing river stage. \nThe yearly pumpage for irrigation has been as much as 114,600 acre-feet (1928-\n29), and there have been as many as 2,500 wells equipped with irrigation pumping plants (1931). Commonly the wells are pumped only in daylight and are \nidle over week-ends and holidays, also during and after protracted rainstorms in \nthe early part of the season. In a small district near Victor pumping in recent \nyears has begun in January or February, has reached its height in March, and \nlargely has passed by April. In outlying districts general pumping has begun as \nlate as May, reached its height in June or July, and waned by September. \nSince 1907 the water table appears to have declined steadily in most of the \nMokelumne area except along the river. The decline was least in the Woodbridge Irrigation District, where in four typical wells. the average decline from 1907 \nto 1937 was 3 feet, or 0.15 foot a year. Among 18 shallow wells in the district of \nmost intensive pumping the average recession of the water table from 1907 to 1927 \nwas 11 feet, or 0.55 foot a year; the greatest measured recession was 15 feet, or \n0.75 foot a year. From 1927 to 1933 the water table declined 5 feet or more over \nmost of the central pumping district except within 2 miles of the Mokelumne \nRiver, and the greatest measured decline was 9 feet. The area of material \nrecession ,extends 4 to 7 miles eastward beyond the central pumping district, \nwhence it is inferred that pumping has drawn gradually on remote ground-water \nstorage. \nIt is inferred that the Mokelumne River ordinarily has been a losing stream \nbetween the Mehrten dam site, near Clements, and the Woodbridge Dam, the \narea that received the percolate having been triangular with its upstream \nand having included about 5,200 acres of the flood plain and 36,500 acres in outlying districts to the north and to the south. \nMean fluctuations of the water table within the area receiving percolate from \nihe river are believed to indicate that relatively little water is drawn from outside \nthe area. Accordingly, simple storage methods are competent for a ground-water \ninventory. It is inferred that the rate of seepage loss from the river depends \njointly upon river discharge, stage in the Woodbridge Reservoir, and groundwater pumpage. \nThe foregoing inferences lead to the following conclusions with respect to \nground-water replenishment by seepage loss from the river in the intensively \ncultivated district about Lodi: (1) The annual replenishment has tended to increase \nfor at least two decades, owing to the gradual increase in head between surface \nwater and ground water as ground-water levels have been lowered progressively \nby pumping; (2) annual replenishment has tended to increase, especially in recent \nyears, owing to gradually prolonged use of the Woodbridge Reservoir, for thereby \na relatively large wetted area and great differential head have been maintained \nfor an increasing term; (3) the rate of replenishment tends to be greater under \nregulation than under the so-called natural regimen, to the extent that regulation \nhas maintained a moderately large wetted area and stage in the river through \nthe later part ·of each pumping season, whi1e the ground-water levels have been \nlowest. Moreover, for any particular yearly run-off below the Mehrten dam site, \nthe replenishment by seepage would tend to be greater under the regulated \nregimen to the extent that fluctuations in discharge were suppressed, for the \ngreatest yearly mean stage and mean wetted area would be afforded by constant \ndischarge. -Thus, diverting water out of the Mokelumne River Basin at the \nPardee Dam does not necessari1y-entail a diminution in ground-water replenishment by seepage loss along the lower reach of the stream, at least in the replenishment beneath the Victor plain above the gaging station at Woodbridge. Rather. \nthe Pardee Dam affords a means for so regulating the discharge as to effect a \nmaximum ground-water replenishment with-a given run-off in the natural channel. \nBodies of ground water perched above the regional water table are common in \nthe Laguna formation, especially in its lower part. Conspicuous bodies occur \nabout 3 miles south of Clay, in a district between 1 mile and 5 miles south of \nClements, and along Dry Creek in T. 5 N., Rs. 7 and 8 E. \nFrom the relation between the water table and the piezometric surface for water \nconfined in deep aquifers, the area receiving percolate from the Mokelumne River \nmay be divided roughly into (1) a central area, extending not :p1ore than half a \nmi1e beyond the flood plain, in which the piezometric surface is inferred to have \nstood below the water table throughout the term of the investigation and hence \nin which the difference in head has favored the percolation of water from shallow \nbeds into deep beds in all seasons, and (2) an outlying area in which the difference \nin head likewise favors downward percolation into deep beds during the pumping \nseason but favors upward percolation during the nonpumping season. This outlying area includes about 75 percent of the segment of the Victor plain that receives percolate from the river. \nFrom 1927 to 1933 the subartesian head that existed during the nonpumping \nseason in the area remote from the river tended to increase; it is therefore inferred \nthat the relative opportunity for seasonal recharge of the shallow water-bearing \nbeds by underfeeding has likewise tended to increase. On the other hand, the \nnegative differential head in wells near the river also has tended to increase; thus \nin this central area the opportunity for discharge of water from shallow beds by \ndownward percolation has probably tended to increase. \nIt is believed that ground-water storage within the area near the river is not \ndecreased materially by\" discharge westward through deep pervious beds, also \nthat the yearly addition to ground-water storage in the outlying area by deep \npercolation from a remote easterly source is scant and for all practical purposes is \noffset by downward percolation along the river.","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington","doi":"10.3133/wsp780","usgsCitation":"Piper, A.M., Gale, H.S., Thomas, H.E., and Robinson, T.W., 1939, Geology and ground-water hydrology of the Mokelumne area, California: U.S. Geological Survey Water Supply Paper 780, Report: vii, 230 p.; 8 Plates: 52.32 x 43.46 and smaller, https://doi.org/10.3133/wsp780.","productDescription":"Report: vii, 230 p.; 8 Plates: 52.32 x 43.46 and smaller","numberOfPages":"257","costCenters":[{"id":154,"text":"California Water Science Center","active":true,"usgs":true}],"links":[{"id":138771,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/0780/report-thumb.jpg"},{"id":278843,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/0780/plate-10.pdf"},{"id":278841,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/0780/report.pdf"},{"id":278842,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/0780/plate-09.pdf"},{"id":277927,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/0780/plate-08.pdf"},{"id":28624,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/0780/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28625,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/0780/plate-02.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28626,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/0780/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28627,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/0780/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28628,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/0780/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"500000","country":"United States","state":"California","otherGeospatial":"Calaveras River;California Trough;Cosumnes River;Dry Creek;Mokelumne River;Sierra Nevada","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -122.5,37.5 ], [ -122.5,39.25 ], [ -119.5,39.25 ], [ -119.5,37.5 ], [ -122.5,37.5 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adce4b07f02db6864a1","contributors":{"authors":[{"text":"Piper, A. M.","contributorId":102865,"corporation":false,"usgs":true,"family":"Piper","given":"A.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":145299,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Gale, H. S.","contributorId":102040,"corporation":false,"usgs":true,"family":"Gale","given":"H.","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":145298,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Thomas, H. E.","contributorId":12829,"corporation":false,"usgs":true,"family":"Thomas","given":"H.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":145296,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Robinson, T. W.","contributorId":82285,"corporation":false,"usgs":true,"family":"Robinson","given":"T.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":145297,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":45282,"text":"b900B - 1939 - Subsurface geology and oil and gas resources of Osage County, Oklahoma. Part 2, Townships 22 and 23 north, ranges 8 and 9 east","interactions":[{"subject":{"id":45282,"text":"b900B - 1939 - Subsurface geology and oil and gas resources of Osage County, Oklahoma. Part 2, Townships 22 and 23 north, ranges 8 and 9 east","indexId":"b900B","publicationYear":"1939","noYear":false,"chapter":"B","title":"Subsurface geology and oil and gas resources of Osage County, Oklahoma. Part 2, Townships 22 and 23 north, ranges 8 and 9 east"},"predicate":"IS_PART_OF","object":{"id":33723,"text":"b900 - 1942 - Subsurface geology and oil and gas resources of Osage county, Oklahoma","indexId":"b900","publicationYear":"1942","noYear":false,"title":"Subsurface geology and oil and gas resources of Osage county, Oklahoma"},"id":1}],"isPartOf":{"id":33723,"text":"b900 - 1942 - Subsurface geology and oil and gas resources of Osage county, Oklahoma","indexId":"b900","publicationYear":"1942","noYear":false,"title":"Subsurface geology and oil and gas resources of Osage county, Oklahoma"},"lastModifiedDate":"2021-09-01T12:35:13.290702","indexId":"b900B","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1939","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":"900","chapter":"B","title":"Subsurface geology and oil and gas resources of Osage County, Oklahoma. Part 2, Townships 22 and 23 north, ranges 8 and 9 east","docAbstract":"This report on the subsurface geology of Osage County, Okla., describes the structural features, the character of the oil- and gas-producing beds, and the localities where additional oil and gas may be found. It embodies a part of the results of a subsurface geologic investigation of the Osage Indian Reservation, which coincides in area with Osage County. The investigation was conducted by a field party of the Geological Survey of the United States Department of the Interior from 1934 to 1937 and involved the study of the records of about 17,000 wells that have been drilled in Osage County. Funds for the investigation were allotted to the Geological Survey by the Public Works Administration. The primary purpose of the examination was to obtain geologic data for use in the administration of the Indian lands. The results of the inquiry have shown that many localities in Osage County outside the present producing oil fields are worthy of prospecting for oil and gas and that additional oil and gas can be found also by exploring deeply buried beds in old producing fields.
All townships in Osage County that contain many wells are described; the information furnished by such townships is ample for drawing detailed subsurface structure-contour maps. The descriptions of several contiguous townships are combined in separate reports, which are issued as parts of a single bulletin. No edition of the consolidated volume will be published, but the several parts can be bound together if desired.
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N. W.","contributorId":104867,"corporation":false,"usgs":true,"family":"Bass","given":"N. W.","affiliations":[],"preferred":false,"id":231351,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Kennedy, L. E.","contributorId":26271,"corporation":false,"usgs":true,"family":"Kennedy","given":"L.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":231348,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Dillard, W. R.","contributorId":25906,"corporation":false,"usgs":true,"family":"Dillard","given":"W.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":231347,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Leatherock, Otto","contributorId":103645,"corporation":false,"usgs":true,"family":"Leatherock","given":"Otto","email":"","affiliations":[],"preferred":false,"id":231350,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Hengst, J. H.","contributorId":54960,"corporation":false,"usgs":true,"family":"Hengst","given":"J.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":231349,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":1740,"text":"wsp838 - 1938 - Floods of Ohio and Mississippi Rivers, January-February 1937, with a section on the Flood deposits of the Ohio River, January-February 1937","interactions":[],"lastModifiedDate":"2016-05-24T11:12:48","indexId":"wsp838","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1938","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":"838","title":"Floods of Ohio and Mississippi Rivers, January-February 1937, with a section on the Flood deposits of the Ohio River, January-February 1937","docAbstract":"In January and February 1937 the Ohio and mid-Mississippi Rivers experienced floods which, over reaches many hundreds of miles in length, exceeded all previously recorded stages. When measured by the loss of life and property, extent of damage, and general disruption of human activities, these floods constituted a major catastrophe.
\nThe floods were caused by a succession of heavy rainstorms that began late in December 1936 and continued nearly to the end of the following January. Although the storms covered a considerable part of the lower Mississippi River Basin and almost the entire Ohio River Basin, the center of heaviest precipitation was in the middle and lower portions of the Ohio River Valley.
\nThe total storm period can be subdivided into several individual storms, which were more or less clearly demarked by short intervening periods of little or no precipitation. Although the individual storm periods were the same or nearly the same over wide areas, their subdivisions were somewhat different in the most widely separated parts of the affected areas, with intermediate gradations in the intervening areas. The heaviest rainfall--that of January 20 to 25--was centered in the lower Ohio Valley, and, falling as it did upon a region with soil saturated and waterways already running full, it had the effect of producing extreme floods.
\nThe small quantity of snow on the ground over the higher eastern parts of the area at the beginning of the storm period disappeared in a short time. Some of the precipitation occurred in the form of snow, but this snow and the associated cold weather were much less significant in their influence on the floods than in the misery and discomfort they caused to ill-sheltered flood refugees and flood-bound people.
\nSequence and time of the storms were such that in the upper and smaller tributary basins the associated flood rises tended to clear to a notable degree before the-next flood rises came; hence many of these tributaries were at no time in extreme flood. In the lower reaches of the largest tributaries, and especially on the middle and lower reaches of the Ohio River, there were extreme and almost continuously increasing accumulations of run-off, which culminated in the region of Louisville, Ky., in stages 10 or 11 feet higher than any previously known.
\nThe precipitation was heaviest in the Ohio River Basin, and the flood in the Mississippi River, like other notable floods of the past, was caused largely by the extraordinary contributions from the Ohio River. The river stages exceeded those previously recorded for the lower 700 miles on the Ohio River and for 250 miles .on the Mississippi River below the Ohio. At Cairo, Ill., at the mouth Of the Ohio River, the river stage was higher for a period of 19 days, from January 24 to February 11, than at any previous time on record. The height above previous flood stages diminished materially as the flood progressed down the Mississippi.
\nThe mean precipitation ever the Ohio River Basin during the storm period was. 12.85 inches. The snow on the ground at the beginning of the period is estimated to have been equivalent to a mean depth of 0.10 inch of water over the basin. Out of the total precipitation 8.9 inches appeared as flood flow. On January 26 the computed volume of water in the stream channels of the Ohio River Basin was 56,000,000 acre-feet, equivalent to a depth of 5.1 inches over the drainage basin. The maximum discharge of the Ohio River at its mouth was 1,880,000 second-feet on February 1. On February 2, the day of the crest stage at the mouth of the Ohio, the computed volume of water on the surface channel system was equivalent to a depth of 3.7 inches over the drainage basin, of which 2.4 inches was in the 337-mile reach of the Ohio River between Louisville, Ky., and the mouth.
\nThis water-supply paper presents records of stage and discharge for the period including the floods at about 250 measurement stations, records of stage and discharge for the period including the floods at about 250 measurement stations, records of storage in many reservoirs, a summary of peak discharges with comparative data for other floods at about 470 measurement points, and tables
showing crest stages along an aggregate length of stream channel for 5,000 miles. The report also includes basic information in regard to the
weather associated with the floods, results of detailed studies of the rainfall and run-off, analyses of the volume of flood waters'in the surface
channel systems during the progress of the floods, and many other kinds of flood information.
Following the main flood report is a brief report entitled \"Flood\" deposits of the Ohio River, January-February 1937, a study of sedimentation.\"
An abstract of that report is presented on page 693.
No abstract available.
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","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/b875","usgsCitation":"Moore, B.N., 1937, Nonmetallic mineral resources of eastern Oregon: U.S. Geological Survey Bulletin 875, Report: viii, 180 p.; 4 Plates: 14.84 x 18.27 inches or smaller, https://doi.org/10.3133/b875.","productDescription":"Report: viii, 180 p.; 4 Plates: 14.84 x 18.27 inches or smaller","costCenters":[],"links":[{"id":485869,"rank":12,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_21053.htm","text":"pumice deposits in Klamath and Deschutes Counties","linkFileType":{"id":5,"text":"html"}},{"id":485868,"rank":11,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_21052.htm","text":"limestone deposit at Lime","linkFileType":{"id":5,"text":"html"}},{"id":485867,"rank":10,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_21051.htm","text":"diatomite in Otis basin area","linkFileType":{"id":5,"text":"html"}},{"id":485866,"rank":9,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_21050.htm","text":"Wallowa Mountains limestone","linkFileType":{"id":5,"text":"html"}},{"id":485865,"rank":8,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_21049.htm","text":"Klamath diatomite district","linkFileType":{"id":5,"text":"html"}},{"id":485864,"rank":7,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_21048.htm","text":"Harper diatomite district","linkFileType":{"id":5,"text":"html"}},{"id":93269,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/0875/plate-16.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":93268,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/0875/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":93266,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/0875/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":93270,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/0875/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":167096,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/0875/report-thumb.jpg"},{"id":93267,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/0875/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Oregon","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -116.4302394922459,\n 46.09256722139355\n ],\n [\n -120.5124247413606,\n 46.09256722139355\n ],\n [\n -120.5124247413606,\n 41.9405979285178\n ],\n [\n -116.4302394922459,\n 41.9405979285178\n ],\n [\n -116.4302394922459,\n 46.09256722139355\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afde4b07f02db696ebf","contributors":{"authors":[{"text":"Moore, Bernard Nettleton","contributorId":85647,"corporation":false,"usgs":true,"family":"Moore","given":"Bernard","email":"","middleInitial":"Nettleton","affiliations":[],"preferred":false,"id":214378,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2100,"text":"wsp796D - 1937 - Geology and ground-water resources of Ogden Valley, Utah","interactions":[],"lastModifiedDate":"2017-09-07T15:18:03","indexId":"wsp796D","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1937","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":"796","chapter":"D","title":"Geology and ground-water resources of Ogden Valley, Utah","docAbstract":"Ogden Valley is a fault trough bounded on both the east and west by faults that dip toward the middle of the valley. This fault trough contains unconsolidated deposits of clay, sand, and gravel, whose thickness is more than 600 feet. These materials are stream and lake deposits and in places are well sorted and stratified. The lake sediments were laid down in a small lake that occupied Ogden Valley and that was connected with glacial Lake Bonneville at its high stage by an arm of water that occupied Ogden Canyon. During this stage of Lake Bonneville the Ogden Valley was completely filled with lake sediments up to an altitude of about 4,900 feet. These sediments include about 70 feet of clay, sand, and gravel in alternating layers, below which is a bed of varved clay whose maximum thickness is about 70 feet. This clay is continuous under the lower parts of the valley and is the confining bed that produces the artesian conditions. Below the varved clay is a deposit of silt, sand, and gravel of unknown thickness, most of which is believed to be pre-Bonneville alluvium.
In most summers the streams entering Ogden Valley are diverted for irrigation, and the upper parts of their channels are generally dry during the irrigation season. Lower down in the valley seepage water appears in the channels, and below these points there is continuous flow. The flow of the Ogden River increases as it passes through Ogden Canyon. This gain in flow is believed to be derived chiefly from ground-water seepage from the canyon walls, although there is probably some groundwater underflow from Ogden Valley at the head of Ogden Canyon. Some of the gain is also due to leakage from pipe lines in the canyon.
Of the 146 wells whose records are given in this report, 70 are flowing wells.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp796D","collaboration":"Prepared in cooperation with the City of Ogden","usgsCitation":"Leggette, R., and Taylor, G., 1937, Geology and ground-water resources of Ogden Valley, Utah: U.S. Geological Survey Water Supply Paper 796, iv, p. 63 p.; 6 Plates: 23.50 x 18.50 inches or smaller, https://doi.org/10.3133/wsp796D.","productDescription":"iv, p. 63 p.; 6 Plates: 23.50 x 18.50 inches or smaller","startPage":"99","endPage":"161","numberOfPages":"67","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":247109,"rank":410,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/0796d/plate-39.pdf","text":"Plate 39","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Stream flow in Ogden valley, 1933-34"},{"id":247108,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/0796d/plate-38.pdf","text":"Plate 38","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Hydrographs of observation wells in Ogden valley and the flow of south fork of Ogden River"},{"id":247110,"rank":411,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/0796d/plate-40.pdf","text":"Plate 40","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Well logs, Ogden Valley, Utah"},{"id":138192,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/0796d/report-thumb.jpg"},{"id":27674,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/0796d/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":247105,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/0796d/plate-35.pdf","text":"Plate 35","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Annual cumulative departure from normal precipitation at Ogden, Utah, and annual precipitation at Ogden and Huntsville, Utah"},{"id":247106,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/0796d/plate-36.pdf","text":"Plate 36","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map of a part of Ogden Valley, Weber County, Utah"},{"id":247107,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/0796d/plate-37.pdf","text":"Plate 37","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Graphs of the flow of south fork of Ogden river, the precipitation at Ogden, the withdrawal of ground water at Artesian park, and the water levels in five observation wells in Ogden valley, 1932-35"}],"country":"United States","state":"Utah","county":"Weber County","otherGeospatial":"Ogden Valley","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adbe4b07f02db6859d7","contributors":{"authors":[{"text":"Leggette, R.M.","contributorId":87525,"corporation":false,"usgs":true,"family":"Leggette","given":"R.M.","email":"","affiliations":[],"preferred":false,"id":144675,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Taylor, G.H.","contributorId":85158,"corporation":false,"usgs":true,"family":"Taylor","given":"G.H.","email":"","affiliations":[],"preferred":false,"id":144674,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":493,"text":"wsp782 - 1937 - Surface water supply of the United States, 1935, Part II, South Atlantic slope and eastern Gulf of Mexico basins","interactions":[],"lastModifiedDate":"2012-02-02T00:05:10","indexId":"wsp782","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1937","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":"782","title":"Surface water supply of the United States, 1935, Part II, South Atlantic slope and eastern Gulf of Mexico basins","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp782","usgsCitation":"Water Resources Division, U.S. Geological Survey, 1937, Surface water supply of the United States, 1935, Part II, South Atlantic slope and eastern Gulf of Mexico basins: U.S. Geological Survey Water Supply Paper 782, 233 p. ;23 cm., https://doi.org/10.3133/wsp782.","productDescription":"233 p. ;23 cm.","costCenters":[],"links":[{"id":135991,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/0782/report-thumb.jpg"},{"id":25056,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/0782/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afee4b07f02db6976f9","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":527465,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":3153,"text":"wsp679B - 1937 - Thermal springs in the United States","interactions":[],"lastModifiedDate":"2024-02-01T22:18:55.044119","indexId":"wsp679B","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1937","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":"679","chapter":"B","title":"Thermal springs in the United States","docAbstract":"The earliest extensive studies of thermal springs in the United States were made by physicians. In 1831 Dr. John Bell issued a book entitled \"Baths and Mineral Waters\" in which he listed 21 spring localities. In the edition of his work published in 1855 the number was increased to 181. The earliest report on a geologic study of thermal springs was that of W. B, Rogers in 1840 on the thermal springs of Virginia. In 1875 G. K. Gilbert published a map and table showing thermal springs in the United States and pointed out that they are present chiefly in the mountainous areas of folded and faulted rocks. Early geologic study of them was principally inspired by the information which they afford at a few places on the deposition of minerals. The relation of hot springs to volcanic action has been studied in the Yellowstone National Park and near Lassen Peak in California. Studies in recent years have been concerned with the source of the water as well as of its heat.
All the notable thermal springs in the eastern United States are in the Appalachian Highlands, principally in the region of folded rocks. The Atlantic Coastal Plain contains no appreciably warm springs. In Florida there are large springs whose water rises from a depth of a few hundred feet and is about 5° above the mean annual temperature, but they are not usually classed as thermal.
The only warm springs in the great Interior Plains region are at and near Hot Springs, S. Dak., in the vicinity of the Black Hills uplift of crystalline rocks. In the Interior Highlands thermal springs occur only in the Ozark region, the largest group being at Hot Springs, Ark.
The Rocky Mountain System includes the Yellowstone National Park, with its world-famous hot springs and geysers (see pis. 7,12), and there are many other hot springs within this great mountainous region. In the Intermontane areas of great lava plains and faulted lava mountains in Utah, Nevada, southern Idaho, and eastern Oregon there are many hot springs, closely associated with the larger faults. In the Pacific Mountain System, including the Cascade Range and Sierra Nevada, there are many warm and hot springs, some of which issue in areas of granite, and others in areas of lava. In the Coast Ranges of California many thermal springs issue from different geologic formations.
Of the total of more than 1,000 thermal-spring localities listed in this paper more than half are situated in the three States of Idaho, California, and Nevada, each of which contains more than 150 thermal-spring localities. Wyoming, including the Yellowstone National Park, contains more than 100 hot-spring localities. Oregon, Utah, Colorado, Montana, and New Mexico contain several dozen thermal springs each, of which the principal ones are developed as resorts. The other thermal springs are scattered through 12 States, of which Massachusetts, New York, Pennsylvania, and North Carolina contain one spring or group each. More than half of the total number are developed as resorts or used for irrigation or water supply, but many have remained undeveloped because they are not easily accessible.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp679B","usgsCitation":"Stearns, N., Stearns, H.T., and Waring, G.A., 1937, Thermal springs in the United States: U.S. Geological Survey Water Supply Paper 679, Report: iv, 147 p.; 1 Plate: 29.00 x 20.00 inches, https://doi.org/10.3133/wsp679B.","productDescription":"Report: iv, 147 p.; 1 Plate: 29.00 x 20.00 inches","startPage":"59","endPage":"206","numberOfPages":"175","costCenters":[{"id":154,"text":"California Water Science Center","active":true,"usgs":true},{"id":610,"text":"Utah Water Science 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],\n [\n -97.22872,\n 49.0007\n ],\n [\n -95.15907,\n 49\n ],\n [\n -95.15609,\n 49.38425\n ],\n [\n -94.81758,\n 49.38905\n ]\n ]\n ]\n ]\n },\n \"properties\": {\n \"name\": \"United States\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a56e4b07f02db62dc25","contributors":{"authors":[{"text":"Stearns, Norah D.","contributorId":25549,"corporation":false,"usgs":true,"family":"Stearns","given":"Norah D.","affiliations":[],"preferred":false,"id":146340,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Stearns, Harold T.","contributorId":65831,"corporation":false,"usgs":true,"family":"Stearns","given":"Harold","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":146341,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Waring, Gerald A.","contributorId":100365,"corporation":false,"usgs":true,"family":"Waring","given":"Gerald","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":146342,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70212780,"text":"70212780 - 1937 - Ground‐water in Utah","interactions":[],"lastModifiedDate":"2020-08-27T18:28:31.097458","indexId":"70212780","displayToPublicDate":"1937-08-27T13:18:40","publicationYear":"1937","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1578,"text":"Eos, Transactions, American Geophysical Union","onlineIssn":"2324-9250","printIssn":"0096-394","active":true,"publicationSubtype":{"id":10}},"title":"Ground‐water in Utah","docAbstract":"In common with many of the arid and semiarid States, the prosperity of Utah probably is more dependent upon the amount of water available than upon any other natural resource. Although only about four per cent of the State is irrigated, a shortage of water for irrigation becomes a major calamity. A large part of the water‐supply for the State is derived from surface‐streams, but a most valuable supplement to this supply is the water available from underground sources. Ground‐water is used extensively for domestic, stock‐watering, and industrial purposes as well as for irrigation. The primary source of the municipal water‐supply for Salt Lake City is from streams entering the Jordan River Valley from the western slope of the Wasatch Mountains. However, since the drought‐year of 1931, a supplementary municipal supply has been obtained from ground‐water, and, among the 17 wells developed by the City during the extreme drought of 1934, one—yielding about ten cubic feet per second, or 4500 gallons a minute—is probably the largest in the State. Ogden, the second largest city in Utah, with a population of about 40,000, obtains the major part of its municipal water‐supply from a group of artesian wells in Ogden Valley about 12 miles east of the City. A considerable part of the water‐supply for the City of Brigham is obtained from wells. Springs constitute the source of most of the water‐supply for Logan, Provo, and many smaller towns and localities in the State. In nearly every developed area of the State ground‐water is used for some purpose, and in some areas the water‐supply is obtained almost entirely from wells.
","language":"English","publisher":"American Geophysical Union","doi":"10.1029/TR018i002p00536","usgsCitation":"Taylor, G.H., 1937, Ground‐water in Utah: Eos, Transactions, American Geophysical Union, v. 18, no. 2, p. 536-541, https://doi.org/10.1029/TR018i002p00536.","productDescription":"6 p.","startPage":"536","endPage":"541","costCenters":[],"links":[{"id":377954,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Utah","otherGeospatial":"Ground Water Provinces","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -113.84033203125,\n 38.272688535980976\n ],\n [\n -113.51074218749999,\n 37.3002752813443\n ],\n [\n -112.3681640625,\n 37.64903402157866\n ],\n [\n -111.29150390625,\n 39.977120098439634\n ],\n [\n -109.423828125,\n 40.12849105685408\n ],\n [\n -110.74218749999999,\n 40.64730356252251\n ],\n [\n -111.4453125,\n 40.863679665481676\n ],\n [\n -111.15966796875,\n 41.95131994679697\n ],\n [\n -113.99414062499999,\n 41.78769700539063\n ],\n [\n -113.84033203125,\n 40.730608477796636\n ],\n [\n -112.8076171875,\n 40.16208338164617\n ],\n [\n -113.13720703125,\n 39.13006024213511\n ],\n [\n -113.84033203125,\n 38.272688535980976\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"18","issue":"2","noUsgsAuthors":false,"publicationDate":"2014-08-18","publicationStatus":"PW","contributors":{"authors":[{"text":"Taylor, George H.","contributorId":24386,"corporation":false,"usgs":true,"family":"Taylor","given":"George","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":797455,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70212777,"text":"70212777 - 1937 - Extraordinary topaz‐replacement body in the Brewer Mine, South Carolina","interactions":[],"lastModifiedDate":"2020-08-28T12:46:30.919473","indexId":"70212777","displayToPublicDate":"1937-08-27T13:00:29","publicationYear":"1937","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1578,"text":"Eos, Transactions, American Geophysical Union","onlineIssn":"2324-9250","printIssn":"0096-394","active":true,"publicationSubtype":{"id":10}},"title":"Extraordinary topaz‐replacement body in the Brewer Mine, South Carolina","docAbstract":"A large body of massive topaz forms a part of the gold‐bearing lode at the Brewer Mine, South Carolina. This gold‐mine was opened 100 years ago and merits the distinction of being one of the early gold‐discoveries of the Southern Appalachian Region. The Brewer Mine is located near Jefferson, in Chesterfield County, near the northern boundary of South Carolina, and on the eastern edge of the Piedmont Province.
The country rock is described by J. T. Pardee and C. F. Park, Jr., (Gold‐deposits of the Southern Appalachians, U. S. Geol. Surv. Prof. Paper, in preparation) as a quartz‐sericite schist that locally preserves the structure of a fine‐grained, waterlaid tuff, probably a rhyolite,from which it was derived. Exposures of granite that intrude the schist appear on the north and west at distances of a mile to a mile and a half.
","language":"English","publisher":"American Geophysical Union","doi":"10.1029/TR018i001p00243","usgsCitation":"Glass, J.J., 1937, Extraordinary topaz‐replacement body in the Brewer Mine, South Carolina: Eos, Transactions, American Geophysical Union, v. 18, no. 1, p. 243-246, https://doi.org/10.1029/TR018i001p00243.","productDescription":"4 p.","startPage":"243","endPage":"246","costCenters":[],"links":[{"id":377976,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"South Carolina","city":"Jefferson","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -80.42953491210938,\n 34.616256875628956\n ],\n [\n -80.34576416015625,\n 34.616256875628956\n ],\n [\n -80.34576416015625,\n 34.6704879985043\n ],\n [\n -80.42953491210938,\n 34.6704879985043\n ],\n [\n -80.42953491210938,\n 34.616256875628956\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"18","issue":"1","noUsgsAuthors":false,"publicationDate":"2014-08-18","publicationStatus":"PW","contributors":{"authors":[{"text":"Glass, Jewell J.","contributorId":106948,"corporation":false,"usgs":true,"family":"Glass","given":"Jewell","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":797453,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70039566,"text":"70039566 - 1936 - Stream flow, suspended, and dissolved matter in streams on and near soil conservation project, La Crosse, WI","interactions":[],"lastModifiedDate":"2012-08-12T01:01:45","indexId":"70039566","displayToPublicDate":"2012-01-01T23:11:52","publicationYear":"1936","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":6,"text":"USGS Unnumbered Series"},"title":"Stream flow, suspended, and dissolved matter in streams on and near soil conservation project, La Crosse, WI","docAbstract":"Measurements of stream flow and movement of suspended natter have been obtained at stations on the La Crosse project as indicated below: Little La Crosse River near Leon, Wis. Drainage area 77.1 square miles. The station is in sec. 3, T. 16 N., R. 4 W., 2 miles northwest of Leon, Monroe County; established March 14, 1934; suspended matter determined from April 1, 1934. Coon Creek at Coon Valley, Wis. Drainage area 77.2 square miles. The station is in sec. 7, T. 14 N., R. 5 W., in the village of Coon Valley, Vernon County; established March 16, 1934; suspended matter determined from April 6, 1934. Coon Creek near Stoddard, Wis. Drainage area 115 square miles. The station is in sec. 25, T. 14 N., R. 7 W., 3 1/4 miles east of Stoddard, Vernon County; established March 28, 1934; suspended matter determined from April 6, 1934.","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/70039566","collaboration":"Prepared in cooperation with the Soil Conservation Service, U.S. Department of Agriculture","usgsCitation":"Grover, N., 1936, Stream flow, suspended, and dissolved matter in streams on and near soil conservation project, La Crosse, WI, 21 p., *66 p.; Tables; Worksheets, https://doi.org/10.3133/70039566.","productDescription":"21 p., *66 p.; Tables; Worksheets","numberOfPages":"109","costCenters":[],"links":[{"id":261079,"rank":800,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70039566/report.pdf"},{"id":261080,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/unnumbered/70039566/report-thumb.jpg"}],"country":"United States","state":"Wisconsin","city":"La Crosse","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505b9a72e4b08c986b31c946","contributors":{"authors":[{"text":"Grover, N.C.","contributorId":65453,"corporation":false,"usgs":true,"family":"Grover","given":"N.C.","email":"","affiliations":[],"preferred":false,"id":466490,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":485,"text":"wsp757 - 1936 - Surface water supply of the United States, 1934, Part II, South Atlantic slope and eastern Gulf of Mexico basins","interactions":[],"lastModifiedDate":"2012-02-02T00:05:07","indexId":"wsp757","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1936","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":"757","title":"Surface water supply of the United States, 1934, Part II, South Atlantic slope and eastern Gulf of Mexico basins","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp757","usgsCitation":"Water Resources Division, U.S. Geological Survey, 1936, Surface water supply of the United States, 1934, Part II, South Atlantic slope and eastern Gulf of Mexico basins: U.S. Geological Survey Water Supply Paper 757, vii, 216 p. ;23 cm., https://doi.org/10.3133/wsp757.","productDescription":"vii, 216 p. ;23 cm.","costCenters":[],"links":[{"id":136647,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/0757/report-thumb.jpg"},{"id":25048,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/0757/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afee4b07f02db697756","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":527457,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2137,"text":"wsp773D - 1936 - Ground-water resources of Kleberg County, Texas","interactions":[],"lastModifiedDate":"2016-08-16T11:38:47","indexId":"wsp773D","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1936","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":"773","chapter":"D","title":"Ground-water resources of Kleberg County, Texas","docAbstract":"Abundant supplies of fresh water are obtained from deep artesian wells In all parts of Kleberg County. The water is derived from a stratum of sand, 10 to 150 feet thick, which usually has been referred to the Goliad sand but possibly may be at the base of the LIssie formation. The top of the sand Is reached at depths of around 400 feet In the western part of the county, 600 to 700 feet In the locality of Klngsville, and 1,250 to 1,450 feet In the eastern part of the county. Small supplies of fairly good water are obtained from shallow wells In very sandy areas in the eastern and southern parts of the county, but with this exception, so far as known, no good water has been obtained In the county either above or below the artesian fresh-water horizon.
\nThe fresh artesian water Is supplied by percolation from the outcrop of the water-bearing sands, which is many miles to the west In Jim Wells, Brooks, and Duval Counties. The estimated average replenishment from the outcrop to the wells of Kleberg County is 3,000,000 gallons a day.
\nAvailable Information regarding most of the wells of the county Is given in the table of well records. Of the 43V wells listed 34 are not In use, and the water supplies from the others are used as follows: , Entirely for stock, 151; domestic use and stock, 241; public supply, 3; Industrial supply, 2; Irrigation, 4; railroad supply, 1; unrecorded, 1. About 80 are flowing wells In the southern and eastern parts of the county.
\nIt is concluded that the total withdrawal from those wells averages about 4,000,000 gallons a day. Some water is wasted, but the amount is not very great.
\nThere has been a general decline In the artesian head throughout the county. The largest decline has been in the western part of the county and In the vicinity of Klngsville, where the water level is now 15 to 45 feet below the surface in wells that once had a strong flow. Wells continue to flow in the southern and eastern parts of the county, but under less head than formerly. There was a small net loss in head in most parts of the county between the winters of 1932-33 and 1934-35, indicating that the decline is slowly continuing. Originally the artesian pressure In the fresh-water sands was much higher than the pressure In the overlying saltwater sands, but this relation has been reversed in the western part of the county and In the district around Klngsville, as a result of the decline in artesian head.
\nWater obtained from the fresh-water horizon is comparatively fresh in the western and central parts of the county but contains a somewhat higher proportion of chlorides toward the Gulf. Samples obtained from about 100 wells, located for the most part in the central part of the county, showed a. higher chloride content than is normal for the freshwater beds in the area. These wells are believed in large part to be defective and to be admitting salt water. This was demonstrated and the leaks located in several wells that were tested. No evidence was found of salt-water contamination by percolation through the formations, however. The leaky wells should be repaired, If practicable, or sealed to prevent them from contaminating the fresh-water sand. The chances of leaks developing can be largely eliminated If the wells are properly drilled and provided with casing of good grade, and the casing is adequately seated.
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Contributions to the hydrology of the United States","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp773D","usgsCitation":"Livingston, P.P., and Bridges, T.W., 1936, Ground-water resources of Kleberg County, Texas: U.S. Geological Survey Water Supply Paper 773, 197-232 p., https://doi.org/10.3133/wsp773D.","productDescription":"197-232 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":137791,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/0773d/report-thumb.jpg"},{"id":27737,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/0773d/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aa7e4b07f02db666fca","contributors":{"authors":[{"text":"Livingston, Penn Poore","contributorId":79452,"corporation":false,"usgs":true,"family":"Livingston","given":"Penn","email":"","middleInitial":"Poore","affiliations":[],"preferred":false,"id":144722,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bridges, Thomas W.","contributorId":106870,"corporation":false,"usgs":true,"family":"Bridges","given":"Thomas","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":144723,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":45772,"text":"pp185I - 1936 - Geomorphology of the north flank of the Uinta Mountains","interactions":[],"lastModifiedDate":"2018-01-29T11:20:29","indexId":"pp185I","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1936","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":"185","chapter":"I","title":"Geomorphology of the north flank of the Uinta Mountains","docAbstract":"The Uinta Mountains, whose northern margin is almost coincident with the southern boundary of Wyoming, extend from the Wasatch Range eastward across the northern part of Utah into northwestern Colorado. They were carved out of a large, simple anticlinal fold of sedimentary rocks arched up into essentially their present attitude at the end of the Cretaceous period. The Uinta Mountain group (Uinta quartzite of previous reports) a series of brick-red to purplish-red quartzite and sandstone beds of pre-Cambrian age, aggregating more than 12,000 feet in thickness, makes up the central mass of the range. Flanking the quartzite core and sharing its anticlinal structure are beds of limestone, sandstone, and shale ranging in age from Upper or Middle Cambrian to Upper Cretaceous. These rocks, which have a total thickness of about 15,000 feet, have been eroded from the higher part of the range, so the upturned edges of the harder\nbeds now form hogbacks ranked along the sides of the fold. In places large faults, approximating the regional strike, cut these steeply inclined beds. Gently warped Tertiary sediments, mostly of Eocene age, fill the large Green River Basin, which lies north of the range, to a depth of several thousand feet and lap up on the flanks of the mountains, from which they were chiefly derived.","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Shorter contributions to general geology, 1934-35","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"United States Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/pp185I","usgsCitation":"Bradley, W.H., 1936, Geomorphology of the north flank of the Uinta Mountains: U.S. Geological Survey Professional Paper 185, Report: iv, 47 p.; 1 Plate, https://doi.org/10.3133/pp185I.","productDescription":"Report: iv, 47 p.; 1 Plate","startPage":"163","endPage":"199","numberOfPages":"52","costCenters":[],"links":[{"id":271147,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0185i/plate-34.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":266797,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0185i/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":169521,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0185i/report-thumb.jpg"}],"country":"United States","state":"Colorado, Idaho, Utah, Wyoming","otherGeospatial":"Uinta Mountains","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -0.01638888888888889,38.5 ], [ -0.01638888888888889,0.0011111111111111111 ], [ -0.016666666666666666,0.0011111111111111111 ], [ -0.016666666666666666,38.5 ], [ -0.01638888888888889,38.5 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c493","contributors":{"authors":[{"text":"Bradley, W. 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