The 1964 earthquake caused wide-spread damage to inhabited places throughout more than 60,000 square miles of south-central Alaska. This report describes damage to all communities in the area except Anchorage, Whittier, Homer, Valdez, Seward, the communities of the Kodiak group of islands, and communities in the Copper River Basin; these were discussed in previous chapters of the Geological Survey's series of reports on the earthquake. At the communities discussed herein, damage resulted primarily from sea waves of diverse origins, displacements of the land relative to sea level, and seismic shaking. Waves took all of the 31 lives lost at those communities; physical damage was primarily from the waves and vertical displacements of the land relative to sea level.
\n\nDestructive waves of local origin struck during or immediately after the earthquake throughout much of Prince William Sound, the southern Kenai Peninsula, and the shores of Kenai Lake. In Prince William Sound, waves demolished all but one home at the native village of Chenega, destroyed homesites at Point Nowell and Anderson Bay, and caused varying amounts of damage to waterfront facilities at Sawmill Bay, Latouche, Port Oceanic, Port Nellie Juan, Perry Island, and western Port Valdez. The local waves, which ran up as high as 70 feet above tide level at Chenega and more than 170 feet in several uninhabited parts of the Sound, took nearly all of the lives lost by drowning at these communities. Destructive local waves that devastated shores of Anderson Bay and adjacent parts of western Port Valdez probably were generated primarily by massive submarine slides of glacial and fluvioglacial deposits ; the origin of the waves that caused damage at most of the other communities and at extensive uninhabited segments of shoreline is not known. At these places the most probable generative mechanisms are: unidentified submarine slides of unconsolidated deposits, and (or) the horizontal tectonic displacements, of 20 to more than 60 feet, that occurred in the Prince William Sound region during the earthquake.
\n\nA train of long-period seismic sea waves that began about 20 minutes after the start of the earthquake inundated shores along the Gulf of Alaska coast to a maximum height of 35 feet above tide level. At the communities described, they virtually destroyed two logging camps at Whidbey Bay and Puget Bay on the south coast of the Kenai Peninsula, caused moderate damage to boat harbors and docks at Seldovia and Cordova, floated away some beach cabins in the Cordova area, and drowned two people, one at Point Whitshed near Cordora and one at the Cape Saint Elias Light Station. The seismic sea waves were generated by regional tectonic uplift of the sea floor on the Continental Shelf.
\n\nVertical tectonic displacements of the land relative to sea level that accompanied the earthquake affected virtually all the coastal communities. Tectonic subsidence of 5 to 6 feet, augmented locally by surficial subsidence of unconsolidated deposits required either the relocation or raising of structures at Portage, Girdwood, and Hope on Turnagain Arm. Shoreline submergence resulting from about 3½ feet of tectonic subsidence at Seldovia necessitated raising all waterfront facilities and the airstrip above the level of high tides. On the other hand, tectonic uplift of the land in the Prince Williams Sound region required deepening of the small-boat harbors at Cordora and Tatitlek, dredging of the waterways in the Cordova area, and lengthening of some docks or piers at Cordova, the Cape Hinchinbrook Light Station, and in Sawmill Bay.
\n\nSignificant structural damage from direct seismic shaking was largely confined to fluid containers and a pier facility near Kenai. Indirect damage from fissuring and differential settling of foundation mterials in the vicinity of the Cordova airfield mused damage to a building, underground utilities, an airfield fill, and the highway. Minor amounts of direct and indirect damage from seismic vibrations were sustained by most of the communities situated on unconsolidated deposits as far east as Yakutat, north to Fairbanks, and west to King Salmon. Except for a few cracked or toppled chimney, all the damage from shaking was confined to areas of thick, unconsolidated deposits. Foundation damage was almost entirely restricted to water-saturated unconsolidated deposits which, when liquefied by seismic shaking, could spread laterally toward free faces and (or) settle differentially through compaction.
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"The Alaska earthquake, March 27, 1964: Effects on communities (Professional Paper 542)","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, DC","doi":"10.3133/pp542G","usgsCitation":"Plafker, G., Kachadoorian, R., Eckel, E.B., and Mayo, L.R., 1969, Effects of the earthquake of March 27, 1964, on various communities: U.S. Geological Survey Professional Paper 542, Report: vi, 50 p.; 2 Plates: 47 x 35 inches and 41.96 x 37 inches, https://doi.org/10.3133/pp542G.","productDescription":"Report: vi, 50 p.; 2 Plates: 47 x 35 inches and 41.96 x 37 inches","numberOfPages":"61","additionalOnlineFiles":"Y","costCenters":[{"id":380,"text":"Menlo ParkCalif. Office-Earthquake Science Center","active":false,"usgs":true}],"links":[{"id":399843,"rank":6,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4589.htm"},{"id":33598,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0542g/pp542g_text.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":33597,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0542g/pp542g_plate2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":33596,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0542g/pp542g_plate1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":117253,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0542g/report-thumb.jpg"},{"id":104505,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pp/0542g/index.html","linkFileType":{"id":5,"text":"html"},"description":"4589"}],"scale":"2500000","datum":"Mean Sea Level","country":"United States","state":"Alaska","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -168,\n 52\n ],\n [\n -130,\n 52\n ],\n [\n -130,\n 66.5\n ],\n [\n -168,\n 66.5\n ],\n [\n -168,\n 52\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c82f","contributors":{"authors":[{"text":"Plafker, George","contributorId":3920,"corporation":false,"usgs":false,"family":"Plafker","given":"George","email":"","affiliations":[],"preferred":false,"id":152485,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Kachadoorian, Reuben","contributorId":24336,"corporation":false,"usgs":true,"family":"Kachadoorian","given":"Reuben","email":"","affiliations":[],"preferred":false,"id":152486,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Eckel, Edwin B.","contributorId":26680,"corporation":false,"usgs":true,"family":"Eckel","given":"Edwin","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":152487,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Mayo, Lawrence R.","contributorId":98344,"corporation":false,"usgs":true,"family":"Mayo","given":"Lawrence","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":152488,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":53593,"text":"ofr69207 - 1969 - An iterative digital model for aquifer evaluation","interactions":[],"lastModifiedDate":"2012-02-02T00:11:24","indexId":"ofr69207","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":"69-207","title":"An iterative digital model for aquifer evaluation","language":"ENGLISH","doi":"10.3133/ofr69207","usgsCitation":"Pinder, G.F., 1969, An iterative digital model for aquifer evaluation: U.S. Geological Survey Open-File Report 69-207, 35 leaves : ill. ; 28 cm., https://doi.org/10.3133/ofr69207.","productDescription":"35 leaves : ill. ; 28 cm.","costCenters":[],"links":[{"id":178361,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1969/0207/report-thumb.jpg"},{"id":87479,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1969/0207/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad6e4b07f02db6842aa","contributors":{"authors":[{"text":"Pinder, George Francis","contributorId":99964,"corporation":false,"usgs":true,"family":"Pinder","given":"George","email":"","middleInitial":"Francis","affiliations":[],"preferred":false,"id":247868,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2234,"text":"wsp1879H - 1969 - Water quality and discharge of streams in the Lehigh River Basin, Pennsylvania","interactions":[],"lastModifiedDate":"2017-06-21T11:04:08","indexId":"wsp1879H","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":"1879","chapter":"H","title":"Water quality and discharge of streams in the Lehigh River Basin, Pennsylvania","docAbstract":"The Lehigh River, 100 miles long, is the second largest tributary to the Delaware River. It drains 1,364 square miles in four physiographic provinces. The Lehigh River basin includes mountainous and forested areas, broad agricultural valleys and areas of urban and industrial development. In the headwaters the water is of good quality and has a low concentration of solutes. Downstream, some tributaries receive coal-mine drainage and become acidic; others drain areas underlain by limestone and acquire alkaline characteristics. The alkaline streams neutralize and dilute the acid mine water where they mix. The dissolved-oxygen content of river water, which is high in the upper reaches of the stream, is reduced in the lower reaches because of lower turbulence, higher temperature, and the respiration of organisms. The Lehigh is used for public supply, recreation, waterpower, irrigation, and mining and other industrial purposes.\r\n\r\n Because the river is shallow in its upper reaches, most of the water comes in contact with the atmosphere as it churns over rocks and around islets and large boulders. Aeration of the water is rapid. When water that was low in dissolved-oxygen concentration was released from the lower strata of the Francis E. Walter Reservoir in June 1966, it quickly became aerated in the Lehigh River, and for 40 miles downstream from the dam the water was nearly saturated with oxygen.\r\n\r\n Most of the river water requires only moderate treatment for industrial use and public distribution throughout the Lehigh River valley. At times, however, some segments of the main river and its tributaries transport industrial wastes and acid coal-mine drainage. Usually the relatively high concentrations of solutes in water and the ensuing damage caused to quality by such waste discharges are more extensive and prolonged during droughts and other periods of low streamflow.\r\n\r\n For many years the Lehigh River flow has been continuously measured and its water chemically analyzed. Since May 1966 an instrument installed by the U.S. Geological Survey at Easton, Pa., has continuously recorded such water-quality parameters as specific conductance, temperature, and dissolved oxygen content.","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/wsp1879H","usgsCitation":"McCarren, E.F., and Keighton, W.B., 1969, Water quality and discharge of streams in the Lehigh River Basin, Pennsylvania: U.S. Geological Survey Water Supply Paper 1879, iv, 48 p., https://doi.org/10.3133/wsp1879H.","productDescription":"iv, 48 p.","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":137749,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1879h/report-thumb.jpg"},{"id":27993,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1879h/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a08e4b07f02db5f9c5d","contributors":{"authors":[{"text":"McCarren, Edward F.","contributorId":106472,"corporation":false,"usgs":true,"family":"McCarren","given":"Edward","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":144865,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Keighton, Walter B.","contributorId":81877,"corporation":false,"usgs":true,"family":"Keighton","given":"Walter","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":144864,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":5673,"text":"pp666 - 1969 - Magnetic fields for a 4x6 prismatic model","interactions":[],"lastModifiedDate":"2012-02-02T00:05:54","indexId":"pp666","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":"666","title":"Magnetic fields for a 4x6 prismatic model","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/pp666","usgsCitation":"Andreasen, G., and Zietz, I., 1969, Magnetic fields for a 4x6 prismatic model: U.S. Geological Survey Professional Paper 666, 9 p., https://doi.org/10.3133/pp666.","productDescription":"9 p.","costCenters":[],"links":[{"id":118034,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0666/report-thumb.jpg"},{"id":32192,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0666/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a80e4b07f02db6492ea","contributors":{"authors":[{"text":"Andreasen, Gordon E.","contributorId":94272,"corporation":false,"usgs":true,"family":"Andreasen","given":"Gordon E.","affiliations":[],"preferred":false,"id":151409,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Zietz, Isidore","contributorId":76708,"corporation":false,"usgs":true,"family":"Zietz","given":"Isidore","affiliations":[],"preferred":false,"id":151408,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":13486,"text":"ofr6987 - 1969 - Evaluation of core data, physical properties, and oil yield USBM/AEC Colorado Core Hole no. 3 (Bronco BR-1)","interactions":[],"lastModifiedDate":"2012-02-02T00:06:37","indexId":"ofr6987","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":"69-87","title":"Evaluation of core data, physical properties, and oil yield USBM/AEC Colorado Core Hole no. 3 (Bronco BR-1)","docAbstract":"USBM/AEC Colorado Core Hole No. 3 (Bronco BR-1) is located in the SW1/4SW1/4SW1/4 sec. 14, T. 1 N., R. 98 W., Rio Blanco County, Colorado. The collar is at a ground elevation of 6,356 feet. The hole was core drilled between depths of 964 and 3,325 feet with a total depth of 3,797 feet. The hole was drilled to investigate geologic, geophysical and hydrological conditions at a possible in situ oil-shale retorting experiment site. The drill hole passed through 1,157 feet of alluvium and the Evacuation Creek Member of the Green River Formation, 1,603 feet of the Parachute Creek Member and penetrated into the Garden Gulch Member of the Green River Formation. In-bole density log/oil yield ratio interpretation indicates that two oil-shale zones exist which yield more than 20 gallons of shale oil per ton of rock; an upper zone lying between 1,271 and 1,750 feet in depth and a lower zone lying between 1,900 and 2,964 feet. Halite (sodium chloride salt) is found between 2,140 and 2,185 feet and nahcolite (sodium bicarbonate salt) between 2,195 and 2,700 feet. Nahcolite was present at one time above 2,195 feet but has been subsequently dissolved out by ground water. The core can be divided into six structural units based upon degree of fracturing. A highly fractured interval is found between 1,646 and 1,899 feet, which coincides with the dissolution or leached nahcolite zone. Physical property tests made on core samples between 1,356 and 3,253 feet give average values of 11,988 psi for uniaxial compressive strength, 1.38 X 10[superscript]6[superscript] psi for static Young's modulus and 11,809 fps for compressional velocity.","language":"ENGLISH","publisher":"U.S. Geological Survey],","doi":"10.3133/ofr6987","usgsCitation":"Ege, J.R., Carroll, R.D., Way, R., and Magner, J.E., 1969, Evaluation of core data, physical properties, and oil yield USBM/AEC Colorado Core Hole no. 3 (Bronco BR-1): U.S. Geological Survey Open-File Report 69-87, 25 p. ill. (some folded, col.), map ;29 cm., https://doi.org/10.3133/ofr6987.","productDescription":"25 p. ill. (some folded, col.), map ;29 cm.","costCenters":[],"links":[{"id":144724,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1969/0087/report-thumb.jpg"},{"id":41955,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0087/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41956,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0087/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41960,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0087/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41961,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0087/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41962,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1969/0087/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41957,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0087/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41958,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0087/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41959,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0087/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a09e4b07f02db5fae72","contributors":{"authors":[{"text":"Ege, John R.","contributorId":69534,"corporation":false,"usgs":true,"family":"Ege","given":"John","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":167874,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Carroll, R. D.","contributorId":53373,"corporation":false,"usgs":true,"family":"Carroll","given":"R.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":167873,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Way, R.J.","contributorId":17238,"corporation":false,"usgs":true,"family":"Way","given":"R.J.","email":"","affiliations":[],"preferred":false,"id":167872,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Magner, J. E.","contributorId":87131,"corporation":false,"usgs":true,"family":"Magner","given":"J.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":167875,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":1078,"text":"wsp1859F - 1969 - Geohydrology and water utilization in the Willcox Basin, Graham and Cochise Counties, Arizona","interactions":[],"lastModifiedDate":"2012-02-02T00:05:18","indexId":"wsp1859F","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":"1859","chapter":"F","title":"Geohydrology and water utilization in the Willcox Basin, Graham and Cochise Counties, Arizona","docAbstract":"The Willcox basin is an area of interior drainage in the northern part of Sulphur Springs Valley, Cochise and Graham Counties, Ariz. The basin comprises about 1,500 square miles, of which the valley floor occupies about 950 square miles. \r\n\r\nThe basin probably formed during middle and late Tertiary time, when the area was subjected to large-scale faulting accompanied by the uplift of the mountain ranges that presently border it. During and after faulting, large quantities of alluvium were deposited in the closed basin. \r\n\r\nThe rocks in the basin are divided into two broad groups--the rocks of the mountain blocks, of Precambrian through Tertiary age, and the rocks of the basin, of Tertiary and Quaternary age. The mountain blocks consist of igneous, metamorphic, and sedimentary rocks; the water-bearing characteristics of these rocks depend primarily on their degree of weathering and fracturing. Even in areas where these rocks are fractured and jointed, only small amounts of water have been developed. The rocks of the basin consist of moderately consolidated alluvium, poorly consolidated alluvium, and unconsolidated alluvium. The water-bearing characteristics of the moderately and poorly consolidated alluvium are not well known. The unconsolidated alluvium underlies most of the valley floor and consists of two facies, stream deposits and lake beds associated with the old playa. The lenticular sand and gravel layers interbedded in silt- and clay-size material of the unconsolidated alluvium constitute the principal aquifer in the basin. The other aquifers, which yield less water, consist of beds of poorly to moderately consolidated sand- and gravel-size material; these beds occur in both the poorly consolidated and moderately consolidated alluvium. \r\n\r\nIn the Stewart area the median specific capacity of wells per 100 feet of saturated unconsolidated alluvium was 20 gallons per minute, and in the Kansas Settlement area the specific capacity of wells penetrating the poorly and moderately consolidated alluvium, undifferentiated, was only 7.4 gallons per minute per 100 feet of saturated material penetrated. The aquifer in the Kansas Settlement area is much less permeable but more homogeneous than the aquifer in the Stewart area. The coefficient of transmissibility of the aquifers, which was estimated from the specific-capacity data, ranged from 58,000 to 160,000 gal. tons per day per foot. \r\n\r\nPrior to extensive ground-water pumpage, the ground-water system probably was in equilibrium, with discharge equaling recharge. At that time, ground water moved toward the playa, where it was discharged by transpiration and evaporation. The estimate of the evapotranspiration in the playa area before large-scale development was about 75,000 acre-feet per year. On the basis of estimates of coefficients of transmissibility of the aquifer and on the basis of the water-table configuration, underflow toward the playa was computed to be about 54,000 acre-feet per year. \r\n\r\nBy 1963, large-scale pumping had caused marked changes in the shape of the piezometric surface; large cones of depression had developed, and ground-water movement was toward the centers of pumping. The cones of depression caused by large-scale pumping have since expanded, and water-level declines have been measured in the recharge areas along the mountain fronts. \r\n\r\nGround water has been used for irrigation since 1910. In 1928, about 4,000 acre-feet of ground water was pumped, and by 1963 180,000 acre-feet per year was being pumped. An estimated 1,860,000 acre-feet of water has been pumped for irrigation in the Willcox basin through 1963; 680,000 acre-feet from the Stewart area, 990,000 acre-feet from the Kansas Settlement area, and 190,000 acre-feet from the Pearce-Cochise area. In the Sierra Bonita Ranch area and the north playa area, ground-water withdrawal for irrigation through 1963 was small. From the spring of 1952 to the spring of 1964 water-level declines resulting from the ","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1859F","usgsCitation":"Brown, S., and Schumann, H.H., 1969, Geohydrology and water utilization in the Willcox Basin, Graham and Cochise Counties, Arizona: U.S. Geological Survey Water Supply Paper 1859, 32 p. :maps (3 fold. in pocket), https://doi.org/10.3133/wsp1859F.","productDescription":"32 p. :maps (3 fold. in pocket)","costCenters":[],"links":[{"id":138054,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1859f/report-thumb.jpg"},{"id":25785,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1859f/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25786,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1859f/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25787,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1859f/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25788,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1859f/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1be4b07f02db6a8b50","contributors":{"authors":[{"text":"Brown, S. G.","contributorId":46914,"corporation":false,"usgs":true,"family":"Brown","given":"S. G.","affiliations":[],"preferred":false,"id":143141,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Schumann, Herbert H.","contributorId":30964,"corporation":false,"usgs":true,"family":"Schumann","given":"Herbert","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":143140,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":4919,"text":"pp606 - 1969 - Revision of some of Girty's invertebrate fossils from the Fayetteville Shale (Mississippian) of Arkansas and Oklahoma","interactions":[],"lastModifiedDate":"2015-10-21T10:16:21","indexId":"pp606","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":"606","title":"Revision of some of Girty's invertebrate fossils from the Fayetteville Shale (Mississippian) of Arkansas and Oklahoma","docAbstract":"J.n 1910, G. H. Girty published a paper on the fauna of the Fayetteville Shale of northern Arkansas and northeastern Oklahoma in which he described 110 new taxa of fossil invertebrates. He did not, however, designate any type specimens or divulge the localities at which •the fossils were collected, nor did he illustrate the species. The present study is designed to fill the gaps in information on some of these species and to bring them as far as possible up to date and in line with the modern scheme of classification.
\nThis report deals with the corals, pelecypods, _gastropods, trilobites, and ostracodes. It does not include the brachiopods and bryozoans. The study has been performed by specialists of the U.S. Geological Survey who are contributing separate parts to the volume.
\n","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/pp606","usgsCitation":"Gordon, M., Sando, W.J., Pojeta, J., Yochelson, E.L., and Sohn, I.G., 1969, Revision of some of Girty's invertebrate fossils from the Fayetteville Shale (Mississippian) of Arkansas and Oklahoma: U.S. Geological Survey Professional Paper 606, iii, 59 p.; 8 Plates; 1 Map: 21.62 x 12.87 inches, https://doi.org/10.3133/pp606.","productDescription":"iii, 59 p.; 8 Plates; 1 Map: 21.62 x 12.87 inches","numberOfPages":"94","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":251792,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0606/report-thumb.jpg"},{"id":247317,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0606/report.pdf","size":"9886","linkFileType":{"id":1,"text":"pdf"}},{"id":310255,"rank":301,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0606/plate-9.pdf","text":"Plate 9","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Arkansas, Oklahoma","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -97.1630859375,\n 35.65729624809628\n ],\n [\n -97.1630859375,\n 37.00255267215955\n ],\n [\n -92.6806640625,\n 37.00255267215955\n ],\n [\n -92.6806640625,\n 35.65729624809628\n ],\n [\n -97.1630859375,\n 35.65729624809628\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a14e4b07f02db602b54","contributors":{"authors":[{"text":"Gordon, Mackenzie Jr.","contributorId":13225,"corporation":false,"usgs":true,"family":"Gordon","given":"Mackenzie","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":576292,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Sando, William J.","contributorId":47851,"corporation":false,"usgs":true,"family":"Sando","given":"William","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":576293,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Pojeta, John Jr.","contributorId":44514,"corporation":false,"usgs":true,"family":"Pojeta","given":"John","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":576294,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Yochelson, Ellis L.","contributorId":90802,"corporation":false,"usgs":true,"family":"Yochelson","given":"Ellis","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":576295,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Sohn, I. G.","contributorId":70751,"corporation":false,"usgs":true,"family":"Sohn","given":"I.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":576296,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":17964,"text":"ofr699 - 1969 - Preliminary geologic interpretation of aeromagnetic data in the Nixon Fork district, Alaska","interactions":[{"subject":{"id":17964,"text":"ofr699 - 1969 - Preliminary geologic interpretation of aeromagnetic data in the Nixon Fork district, Alaska","indexId":"ofr699","publicationYear":"1969","noYear":false,"title":"Preliminary geologic interpretation of aeromagnetic data in the Nixon Fork district, Alaska"},"predicate":"SUPERSEDED_BY","object":{"id":39568,"text":"pp700D - 1970 - Geological Survey research 1970, Chapter D","indexId":"pp700D","publicationYear":"1970","noYear":false,"chapter":"D","title":"Geological Survey research 1970, Chapter D"},"id":1}],"supersededBy":{"id":39568,"text":"pp700D - 1970 - Geological Survey research 1970, Chapter D","indexId":"pp700D","publicationYear":"1970","noYear":false,"title":"Geological Survey research 1970, Chapter D"},"lastModifiedDate":"2024-01-17T19:39:16.691625","indexId":"ofr699","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":"69-9","title":"Preliminary geologic interpretation of aeromagnetic data in the Nixon Fork district, Alaska","docAbstract":"
An aeromagnetic map covering 480 square miles was compiled for the Nixon Fork district, which is located approximately 35 miles northeast of McGrath, Alaska. The survey was flown in search of concealed intrusive rocks which may have produced contact metamorphic deposits in limestone similar to the known lode deposits which have been the principal source of gold in the district.
The exposed quartz monzonite stocks with which the lode deposits are associated produce negative magnetic anomalies. Slight to moderately strong positive anomalies correlate with granitic intrusives in contact with Upper Cretaceous rocks in the Iditarod-Nixon Fork fault zone. No significant mineral deposits have been found in conjunction with these granitic bodies.
Positive anomalies, delineating buried intrusives, occur near the east and west boundaries of the mapped area. The nature of the westernmost intrusive is unknown.
An area of possible economic interest lies between Limestone Mountain and Whirlwind-Canyon Creeks in the eastern sector of the mapped area. An elliptical positive anomaly is superimposed on an elongate, slightly negative anomaly. This negative anomaly may represent an intrusive similar to the quartz monzonite with which the lode deposits are affiliated. The positive anomaly may be a near-vertical mafic dike intruded to within 50 feet of the surface of a limestone ridge. Limestone in the vicinity of the dike may be a favorable area for prospecting for lode deposits similar to the known gold-producing deposits of the district.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr699","usgsCitation":"Anderson, L.A., Reed, B.L., and Johnson, G.R., 1969, Preliminary geologic interpretation of aeromagnetic data in the Nixon Fork district, Alaska: U.S. Geological Survey Open-File Report 69-9, Report: ii, 6 p.; 1 Plate: 40.63 x 31.55 inches, https://doi.org/10.3133/ofr699.","productDescription":"Report: ii, 6 p.; 1 Plate: 40.63 x 31.55 inches","costCenters":[],"links":[{"id":149186,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1969/0009/report-thumb.jpg"},{"id":424516,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0009/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":424515,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1969/0009/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Alaska","otherGeospatial":"Nixon Fork district","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -156.21098975436422,\n 64.39363688486736\n ],\n [\n -156.0545619009912,\n 64.39363688486736\n ],\n [\n -156.0545619009912,\n 64.40237470471484\n ],\n [\n -156.21098975436422,\n 64.40237470471484\n ],\n [\n -156.21098975436422,\n 64.39363688486736\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n },\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -158.14993847514128,\n 64.4117874414261\n ],\n [\n -158.14993847514128,\n 63.40759602117143\n ],\n [\n -150.94307945964977,\n 63.40759602117143\n ],\n [\n -150.94307945964977,\n 64.4117874414261\n ],\n [\n -158.14993847514128,\n 64.4117874414261\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c2e1","contributors":{"authors":[{"text":"Anderson, Lennart A.","contributorId":106111,"corporation":false,"usgs":true,"family":"Anderson","given":"Lennart","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":178293,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Reed, Bruce L.","contributorId":19928,"corporation":false,"usgs":true,"family":"Reed","given":"Bruce","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":178294,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Johnson, Gordon R.","contributorId":90725,"corporation":false,"usgs":true,"family":"Johnson","given":"Gordon","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":178295,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":32678,"text":"pp543H - 1969 - Erosion and deposition on a beach raised by the 1964 earthquake Montague Island, Alaska","interactions":[{"subject":{"id":32678,"text":"pp543H - 1969 - Erosion and deposition on a beach raised by the 1964 earthquake Montague Island, Alaska","indexId":"pp543H","publicationYear":"1969","noYear":false,"chapter":"H","title":"Erosion and deposition on a beach raised by the 1964 earthquake Montague Island, Alaska"},"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":"2022-02-16T20:17:09.532739","indexId":"pp543H","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":"H","title":"Erosion and deposition on a beach raised by the 1964 earthquake Montague Island, Alaska","docAbstract":"During the 1964 Alaska earthquake, tectonic deformation uplifted the southern end of Montague Island as much as 33 feet or more. The uplifted shoreline is rapidly being modified by subaerial and marine processes. The new raised beach is formed in bedrock, sand, gravel, and deltaic bay-head deposits, and the effect of each erosional process was measured in each material. Fieldwork was concentrated in two areas—MacLeod Harbor on the northwest side and Patton Bay on the southeast side of Montague Island. In the unconsolidated deltaic deposits of MacLeod Harbor, 97 percent of the erosion up to June 1965, 15 months after the earthquake, was fluvial, 2.2 percent was by rainwash, and only 0.8 percent was marine; 52 percent of the total available raised beach material had already been removed. The volume removed by stream erosion was proportional to low-flow discharge raised to the power of 0.75 to 0.95, and this volume increased as the bed material became finer. Stream response to the relative fall in base level was very rapid, most of the downcutting in unconsolidated materials occurring within 48 hours of the uplift for streams with low flows greater than 10 cubic feet per second. Since then, erosion by these streams has been predominantly lateral. Streams with lower discharges, in unconsolidated materials, still had knickpoints after 15 months. No response to uplift could be detected in stream courses above the former preearthquake sea level.\n\nWhere the raised beach is in bedrock, it is being destroyed principally by marine action but at such a low rate that no appreciable erosion of bedrock was found 15 months after the earthquake. A dated rock platform raised earlier has eroded at a mean rate of 0.49 foot per year. In this area the factor limiting the rate of erosion was rock resistance rather than the transporting capacity of the waves.\n\nThe break in slope between the top of the raised beach and the former seacliff is being obliterated by debris which is accumulating at the base of the cliffs and which is no longer being removed by the sea. Current cliff retreat by rockfall, mudflows, and landslides was estimated at 0.7 to 2.0 feet per year, and in parts of Patton Bay the accumulation of debris has obliterated 78 percent of the original break in slope in 15 months.\n\nEvidence of two relative sea-level changes before 1964 was found in Patton Bay. At a high stand of sea level lasting until about 2000 B.P. (before present), an older raised beach was formed which, over a distance of 5 miles, shows 40 feet of deformation relative to the present sea level. Peat deposits exposed by the 1964 uplift also record a low sea level that lasted until at least 600 B.P.\n\nThe 1964 raised beach was used to test the accuracy of identification of former sea-level elevations from raised beach features. The Pre-1964 sea level could be accurately determined from the height of the former barnacle line, so an independent check on high-water level was available. The most reliable topographic indicator was the elevation of the break in slope at the top of a beach between a bedrock platform and a cliff. Even here, the former sea level could only be identified within 5 feet. The breaks in slope at the top of gravel beaches were found to be poor indicators of former sea level.\n\nOn Montague Island, evidence of former high sea levels appeared to be best preserved (1) as raised bedrock platforms on rocks of moderate resistance in slightly sheltered locations and (2) as raised storm beaches where the relief immediately inland was very low.","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/pp543H","usgsCitation":"Kirkby, M.J., and Kirkby, A.V., 1969, Erosion and deposition on a beach raised by the 1964 earthquake Montague Island, Alaska: U.S. Geological Survey Professional Paper 543, vi, 41 p., https://doi.org/10.3133/pp543H.","productDescription":"vi, 41 p.","numberOfPages":"49","costCenters":[{"id":380,"text":"Menlo ParkCalif. Office-Earthquake Science Center","active":false,"usgs":true}],"links":[{"id":277846,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pp/0543h/index.html"},{"id":60590,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0543h/pp543h_text.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":126481,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0543h/report-thumb.jpg"},{"id":396031,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_99031.htm"}],"country":"United States","state":"Alaska","otherGeospatial":"Montague Island","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -147.923,59.7643 ], [ -147.923,60.3825 ], [ -146.9077,60.3825 ], [ -146.9077,59.7643 ], [ -147.923,59.7643 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0ee4b07f02db5fe045","contributors":{"authors":[{"text":"Kirkby, M. J.","contributorId":55322,"corporation":false,"usgs":true,"family":"Kirkby","given":"M.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":208911,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Kirkby, Anne V.","contributorId":108013,"corporation":false,"usgs":true,"family":"Kirkby","given":"Anne","email":"","middleInitial":"V.","affiliations":[],"preferred":false,"id":208912,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":34790,"text":"b1271E - 1969 - Pecos National Monument, New Mexico: Its geologic setting","interactions":[],"lastModifiedDate":"2021-09-22T21:27:07.716549","indexId":"b1271E","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":"1271","chapter":"E","title":"Pecos National Monument, New Mexico: Its geologic setting","docAbstract":"The ruins of the pueblos and missions of Pecos lie on the east bank of Glorieta Creek near its junction with the Pecos River at the south end of the Sangre de Cristo Mountains in north-central New Mexico. Here the Pecos River and Glorieta Creek have formed a broad rolling valley in which the red adobe walls of the mission church stand as a striking monument to a historic past.\r\n\r\nThis is beautiful country; the bright hues of red rocks are complemented by the varied greens of the junipers, pi?ons, and ponderosa pines. Northward the Sangre de Cristo Mountains stretch for miles in a blue mist toward the Truchas Peaks and forests of the Pecos Wilderness. A few miles south of the ruins the steep high escarpment of Glorieta Mesa marks, in a general way, the southern termination of the Rocky Mountain System, which here is represented by the Sangre de Cristos.\r\n\r\nThe escarpment of Glorieta Mesa has been formed largely by the Pecos River and its tributaries eroding the soft sedimentary layers. The Pecos flows southward from the high mountains in the north, parallels the mesa escarpment for 15 miles, and breaches the mesa near San Jose. About 1-1/2 miles southwest of the Pecos ruins at Cerro de Escobas is the highest point on Glorieta Mesa. It is the most conspicuous feature of the local landscape and rises to an elevation of 8,212 feet - 1,270 feet above the ruins. The slope of the escarpment here is very steep, rising 6 feet in every 10 horizontal feet.\r\n\r\nAlong the north side of the Glorieta Mesa escarpment is a 30-mile-long natural pass around the south end of the Sangre de Cristos that extends from Canoncito on the west to Starvation Peak on the east (fig. 1). The elevation of the pass is greater than 6,000 feet at all places, and it reaches its summit of 7,432 feet near the village of Glorieta near the west end of the pass. This pass has been used as a major travel route for more than 800 years by the Indians, Spanish, and Americans. The famous Santa Fe Trail passed through here and was superseded by the railroad, whose main-line tracks closely parallel the traces of the old wagon ruts. The modern four-lane divided highway, Interstate Highway I-25, carries high-speed automotive traffic through Glorieta Pass alongside the Santa Fe Railway. Glorieta Pass has been the locale of many important historical events, including the passage of Coronado's expedition in 1540-41; the construction of the two large mission churches at Pecos Pueblo; the capture and imprisonment of the men of the Texas Expedition in 1841; the passage of the American Army under General Kearny on its way to Santa Fe, Chihuahua, and California in 1846; and the Civil War Battle of Glorieta Pass in 1862.","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Contributions to general geology, 1968","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/b1271E","usgsCitation":"Johnson, R.B., 1969, Pecos National Monument, New Mexico: Its geologic setting: U.S. Geological Survey Bulletin 1271, Report: iii, 11 p.; 1 Plate: 12.00 × 10.00 inches, https://doi.org/10.3133/b1271E.","productDescription":"Report: iii, 11 p.; 1 Plate: 12.00 × 10.00 inches","costCenters":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":109683,"rank":699,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_21363.htm","linkFileType":{"id":5,"text":"html"},"description":"21363"},{"id":62688,"rank":299,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1271e/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":62687,"rank":399,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1271e/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":167645,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1271e/report-thumb.jpg"}],"country":"United States","state":"New Mexico","otherGeospatial":"Pecos National Monument","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -105.7170,\n 35.5137842234445\n ],\n [\n -105.64453124999999,\n 35.5137842234445\n ],\n [\n -105.64453124999999,\n 35.56853899134082\n ],\n [\n -105.7170,\n 35.56853899134082\n ],\n [\n -105.7170,\n 35.5137842234445\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad4e4b07f02db682ef5","contributors":{"authors":[{"text":"Johnson, Ross Byron","contributorId":37339,"corporation":false,"usgs":true,"family":"Johnson","given":"Ross","email":"","middleInitial":"Byron","affiliations":[],"preferred":false,"id":213590,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1223,"text":"wsp1879D - 1969 - Water resources of the Salmon Falls Creek basin, Idaho-Nevada","interactions":[],"lastModifiedDate":"2013-11-26T15:56:40","indexId":"wsp1879D","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":"1879","chapter":"D","title":"Water resources of the Salmon Falls Creek basin, Idaho-Nevada","docAbstract":"The northern part of the Salmon Falls Creek basin, referred to as the Salmon Falls tract, contains a large acreage of good agricultural land, but the surface-water supply is inadequate to develop the area fully. Attempts to develop ground water for irrigation have been successful only locally. Specific capacities of wells drilled for irrigation and for test purposes ranged from less than 0.5 to 70 gallons per minute per foot of drawdown. The surface-water supply averages 107,000 acre-feet annually, of which about 76,000 acre-feet is diverted for irrigation. \n\nThe Idavada Volcanics, the most widespread and oldest water-bearing formation in the Salmon Falls tract, consists of massive, dense, thick flows and blankets of welded silicic tuff with associated fine- to coarse-grained ash, clay, silt, sand, and gravel. Fault zones and jointed rock yield large amounts of water to wells, but massive nonjointed units yield little water. Sand, tuff, and ash beds yield moderate quantities of water. Clay, sandy clay, sand, and pea gravel occur in topographic lows on the Idavada Volcanics. The finegrained sediments yield little water to wells, but the gravel yields moderate quantities. \n\nVesicular porphyritic irregularly jointed olivine basalt flows, which overlie the Idavada Volcanics, underlie almost all the Salmon Falls tract. Lenticular fine-grained sedimentary beds as much as 15 feet thick separate some of the flows. Joints and contacts between flows yield small to moderate amounts of water to wells. \n\nAlluvial and windblown deposits blanket most of the tract. Where they occur below the water table, the alluvial deposits yield adequate supplies for stock and domestic wells. Perched water in the alluvium along Deep Creek supplies some stock and domestic wells during most years. \n\nGround-water supplies adequate for domestic and stock use can be obtained everywhere in the tract, but extensive exploration has discovered only five local areas where pumping ground water for irrigation is presently economically feasible. About 8,000 acre-feet was withdrawn for all uses in 1960.\n\nNatural discharge of ground water is northward -- toward the Twin Falls South Side Project and the Snake River--and is provisionally estimated to be 115,000 acre-feet annually. \n\nGround water in the Salmon Falls tract has a medium- to high salinity hazard and a low sodium hazard. The salinity does not appear to affect crops presently grown in the tract. \n\nThe southern part of the Salmon Falls Creek basin, referred to as the upper drainage basin, has little agricultural development and is used mostly for grazing livestock. Silicic volcanic rocks and tuffaceous sedimentary rocks of Tertiary age and alluvial deposits yield water to livestock, domestic, and commercial wells.","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1879D","usgsCitation":"Crosthwaite, E., 1969, Water resources of the Salmon Falls Creek basin, Idaho-Nevada: U.S. Geological Survey Water Supply Paper 1879, iv, 33 p. :ill. ;24 cm., https://doi.org/10.3133/wsp1879D.","productDescription":"iv, 33 p. :ill. ;24 cm.","costCenters":[{"id":343,"text":"Idaho Water Science Center","active":true,"usgs":true}],"links":[{"id":137893,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1879d/report-thumb.jpg"},{"id":26139,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1879d/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Idaho;Nevada","otherGeospatial":"Salmon Falls Creek","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f2e4b07f02db5eee85","contributors":{"authors":[{"text":"Crosthwaite, E. G.","contributorId":83098,"corporation":false,"usgs":true,"family":"Crosthwaite","given":"E. G.","affiliations":[],"preferred":false,"id":143396,"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":23859,"text":"ofr70209 - 1969 - Perspective center determination","interactions":[],"lastModifiedDate":"2012-02-02T00:08:07","indexId":"ofr70209","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":"70-209","title":"Perspective center determination","docAbstract":"This program determines coordinates of the perspective center of a stereoplotter projector by bringing two bundles of rays into a best fit coincidence in a space-resection solution. One of the bundles of rays is defined by the perspective center and the grid intersections on a grid plate. The other bundle of rays is defined by the perspective center and the projected grid intersections in the model space. \r\n\r\nThe program is used with the independent-model method of semianalytlcal aerotriangulation, which requires the coordinates of perspective centers. It may also be used in checking the calibration of stereoplotters.","language":"ENGLISH","publisher":"U.S. Geological Survey, Topographic Division,","doi":"10.3133/ofr70209","issn":"0094-9140","usgsCitation":"McLaurin, J., 1969, Perspective center determination: U.S. Geological Survey Open-File Report 70-209, 41 p. :ill. ;28 cm., https://doi.org/10.3133/ofr70209.","productDescription":"41 p. :ill. ;28 cm.","costCenters":[],"links":[{"id":155699,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1970/0209/report-thumb.jpg"},{"id":53079,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1970/0209/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b20e4b07f02db6abb09","contributors":{"authors":[{"text":"McLaurin, J.D.","contributorId":68348,"corporation":false,"usgs":true,"family":"McLaurin","given":"J.D.","email":"","affiliations":[],"preferred":false,"id":190871,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":3658,"text":"cir608 - 1969 - Scientific or rule-of-thumb techniques of ground-water management--Which will prevail?","interactions":[],"lastModifiedDate":"2017-06-25T13:03:53","indexId":"cir608","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":307,"text":"Circular","code":"CIR","onlineIssn":"2330-5703","printIssn":"1067-084X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"608","title":"Scientific or rule-of-thumb techniques of ground-water management--Which will prevail?","docAbstract":"Emphasis in ground-water development, once directed largely to quantitatively minor (but sociologically vital) service of human and stock needs, is shifting: aquifers are treated as possible regulating reservoirs managed conjunctively with surface water. Too, emphasis on reducing stream pollution is stimulating interest in aquifers as possible waste-storage media. \r\n\r\nSuch management of aquifers requires vast amounts of data plus a much better understanding of aquifer-system behavior than now exists. Implicit in this deficiency of knowledge is a need for much new research, lest aquifers be managed according to ineffective rule-of-thumb standards, or even abandoned as unmanageable. \r\n\r\nThe geohydrologist's task is to define both internal and boundary characteristics of aquifer systems. Stratigraphy is a primary determinant of these characteristics, but stratigraphically minor features may make aquifers transcend stratigraphic boundaries. For example, a structurally insignificant fracture may carry more water than a major fault; a minor stratigraphic discontinuity may be a major hydrologic boundary. Hence, there is a need for ways of defining aquifer boundaries and quantifying aquifer and confining-bed characteristics that are very different from ordinary stratigraphic techniques. Among critical needs are techniques for measuring crossbed permeability; for extrapolating and interpolating point data on direction and magnitude of permeability in defining aquifer geometry; and for accurately measuring geochemical properties of water and aquifer material, and interpreting those measurements in terms of source of water, rate of movement, and waste-sorbing capacities of aquifers and of confining beds--in general, techniques adequate for predicting aquifer response to imposed forces whether static, hydraulic, thermal, or chemical. Only when such predictions can be made routinely can aquifer characteristics be inserted into a master model that incorporates both the hydrologic and the socioeconomic facts necessary to intelligent social actions involving water.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/cir608","usgsCitation":"McGuinness, C.L., 1969, Scientific or rule-of-thumb techniques of ground-water management--Which will prevail?: U.S. Geological Survey Circular 608, iii, 8 p. ;26 cm., https://doi.org/10.3133/cir608.","productDescription":"iii, 8 p. ;26 cm.","costCenters":[],"links":[{"id":30699,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1969/0608/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":124739,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1969/0608/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0ce4b07f02db5fceba","contributors":{"authors":[{"text":"McGuinness, Charles Lee","contributorId":101249,"corporation":false,"usgs":true,"family":"McGuinness","given":"Charles","email":"","middleInitial":"Lee","affiliations":[],"preferred":false,"id":147357,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1676,"text":"wsp1757K - 1969 - A ground-water reconnaissance of the Republic of Ghana, with a description of geohydrologic provinces","interactions":[],"lastModifiedDate":"2012-02-02T00:05:23","indexId":"wsp1757K","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":"1757","chapter":"K","title":"A ground-water reconnaissance of the Republic of Ghana, with a description of geohydrologic provinces","docAbstract":"This report gives a general summary of the availability and use of ground water and describes the occurrence of ground water in five major geohydrologic provinces lying in the eight administrative regions of Ghana. The identification and delineation of the geohydrologic provinces are based on their distinctive characteristics with respect to the occurrence and availability of ground water. \r\n\r\nThe Precambrian province occupies the southern, western, and northern parts of Ghana and is underlain largely by intrusive crystalline and metasedimentary rocks. The Voltaian province includes that part of the Voltaian sedimentary basin in central Ghana and is underlain chiefly by consolidated sandstone, mudstone, and shale. Narrow discontinuous bands of consolidated Devonian and Jurassic sedimentary rocks near the coast constitute the Coastal Block Fault province. \r\n\r\nThe Coastal Plain province includes semiconsolidated to unconsolidated sediments of Cretaceous to Holocene age that underlie coastal plain areas in southwestern and southeastern Ghana. The Alluvial province includes the Quaternary alluvial deposits in the principal river valleys and on the delta of the Volta River. Because of the widespread distribution of crystalline and consolidated sedimentary rocks of low permeability in the Precambrian, Voltaian, and Coastal Block Fault provinces, it is difficult to develop large or event adequate groundwater supplies in much of Ghana. On the other hand, small (1 to 50 gallons per minute) supplies of water of usable quality are available from carefully sited boreholes in most parts of the country. Also, moderate (50 to 200 gpm) supplies of water are currently (1964) obtained from small-diameter screened boreholes tapping sand and limestone aquifers in the Coastal Plain province in southwestern and southeastern Ghana, but larger supplies could be obtained through properly constructed boreholes. In the Alluvial province, unconsolidated deposits in the larger stream valleys that are now largely undeveloped offer desirable locations for shallow vertical or horizontal wells, which can induce infiltration from streams and yield moderate to large water supplies. \r\n\r\nThe principal factors that limit development of ground-water supplies in Ghana are (1) prevailing low permeability and water-yielding potential of the crystalline and consolidated sedimentary rocks that underlie most of the country, (2) highly mineralized ground water which appears to be widely distributed in the northern part of the Voltaian province, and (3) potential problems of salt-water encroachment in the Coastal Plain province in the Western Region and in the Keta area. \r\n\r\nOn the other hand, weathering has increased porosity and has thus substantially increased the water-yielding potential of the crystalline and consolidated sedimentary rocks in much of central and northern Ghana. Also, with proper construction and development, much larger yields than those now (1964) prevalent could be obtained from boreholes tapping sand and limestone aquifers in the Coastal Plain province.","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1757K","usgsCitation":"Gill, H., 1969, A ground-water reconnaissance of the Republic of Ghana, with a description of geohydrologic provinces: U.S. Geological Survey Water Supply Paper 1757, iii, 38 p., https://doi.org/10.3133/wsp1757K.","productDescription":"iii, 38 p.","costCenters":[],"links":[{"id":138253,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1757k/report-thumb.jpg"},{"id":26751,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1757k/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26752,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1757k/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26753,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1757k/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b32e4b07f02db6b45c0","contributors":{"authors":[{"text":"Gill, H.E.","contributorId":24330,"corporation":false,"usgs":true,"family":"Gill","given":"H.E.","email":"","affiliations":[],"preferred":false,"id":143958,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":15426,"text":"ofr69205 - 1969 - Meteoritic origin and consequent endogenic modification of large lunar craters - a study in analytic geomorphology","interactions":[],"lastModifiedDate":"2012-02-02T00:07:08","indexId":"ofr69205","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":"69-205","title":"Meteoritic origin and consequent endogenic modification of large lunar craters - a study in analytic geomorphology","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/ofr69205","usgsCitation":"Pike, R.J., 1969, Meteoritic origin and consequent endogenic modification of large lunar craters - a study in analytic geomorphology: U.S. Geological Survey Open-File Report 69-205, 404 p. ill. ;29 cm., https://doi.org/10.3133/ofr69205.","productDescription":"404 p. ill. ;29 cm.","costCenters":[],"links":[{"id":148632,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4fe4b07f02db6288e0","contributors":{"authors":[{"text":"Pike, Richard J. rpike@usgs.gov","contributorId":5753,"corporation":false,"usgs":true,"family":"Pike","given":"Richard","email":"rpike@usgs.gov","middleInitial":"J.","affiliations":[],"preferred":true,"id":171121,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":38830,"text":"pp529D - 1969 - Atlantic continental shelf and slope of the United States - Color of marine sediments","interactions":[],"lastModifiedDate":"2024-10-25T14:43:46.753707","indexId":"pp529D","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":"529","chapter":"D","title":"Atlantic continental shelf and slope of the United States - Color of marine sediments","docAbstract":"A systematic examination of the regional color distribution of the upper sediment layer on the Atlantic continental margin between Nova Scotia and southern Florida reveals that brown, dark green, and yellow predominate on the shelf north of Cape Hatteras, whereas olive, gray, and yellow predominate to the south. Color is affected by composition. texture, physiography, and geological events in the recent past. Many of the color patterns on the shelf are more closely related to Pleistocene and Holocene sedimentary events than to modern dispersal processes. Relict color patterns occur in areas such as Georges and Browns Banks, which were exposed during lower stands of sea level. Linear but discontinuous belts of yellow sediment on the outer shelf and along the shelf break south of Cape Hatteras are probably also related to strandline features formed during the Pleistocene low stands of sea level and during the transgressive advance of the Holocene sea.
Color patterns on the continental slope and rise and on the Blake Plateau, unlike those on the shelf, are arranged in linear belts that trend parallel or subparallel to the shelf break. Major trends vary di redly with depth, ranging from olive and green at the top of the slope, through light gray and pale yellowish brown, to brown and yellow at. the top of the continental rise. These trends are probably related to the oxidation-reduction Potential of the environment, which results from a balance between the rate of deposition and the rate of bacterial decomposition of organic matter deposited with the sediment. Isolated areas of color on the slope and rise seem to be due to the slumping of sediment masses downslope and to the exposure of pre-Holocene outcrops. Red Pleistocene till masses, which were once exposed on the Scotian Shelf during the glacial epoch, may have been reworked during the Holocene rise in sea level. This may explain why 'brown and reddish-brown sediments are found at progressively shallower depths northeastward on the rise and slope off the Gulf of Maine and Nova Scotia.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/pp529D","usgsCitation":"Stanley, D., 1969, Atlantic continental shelf and slope of the United States - Color of marine sediments: U.S. Geological Survey Professional Paper 529, Report: iii, 15 p.; 1 Plate: 18.50 x 33.00 inches, https://doi.org/10.3133/pp529D.","productDescription":"Report: iii, 15 p.; 1 Plate: 18.50 x 33.00 inches","costCenters":[],"links":[{"id":120116,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0529d/report-thumb.jpg"},{"id":65761,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0529d/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":65762,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0529d/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","otherGeospatial":"Atlantic continental shelf","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -61.951131406124944,\n 44.656140898792216\n ],\n [\n -65.03271055868028,\n 46.6747751769158\n ],\n [\n -68.09301659384751,\n 48.53700763232774\n ],\n [\n -85.39748164610373,\n 28.3802471692038\n ],\n [\n -80.39211999326048,\n 23.782933097067072\n ],\n [\n -61.951131406124944,\n 44.656140898792216\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aaee4b07f02db66c7bf","contributors":{"authors":[{"text":"Stanley, D.J.","contributorId":107356,"corporation":false,"usgs":true,"family":"Stanley","given":"D.J.","email":"","affiliations":[],"preferred":false,"id":220508,"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":1690,"text":"wsp1898A - 1969 - Stage-discharge characteristics of a Weir in a sand-channel stream","interactions":[],"lastModifiedDate":"2012-02-02T00:05:14","indexId":"wsp1898A","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":"1898","chapter":"A","title":"Stage-discharge characteristics of a Weir in a sand-channel stream","docAbstract":"A unique relation between water-surface elevation and water discharge usually does not exist for sand-channel streams. The relation is affected by changes in bed roughness and changes in bed elevation because of scour and fill. An artificial control on a sand-channel stream must control both the resistance to flow and the bed elevation in order to stabilize the relation between water-surface elevation and water discharge. \r\n\r\nThe weir (control structure) in the Rio Grande conveyance channel near Bernardo, N. Mex., was designed on the basis of a model study and field data (Harris and Richardson, 1964). About 72 percent of the measurements used to define the base relation between water-surface elevation and water discharge falls within plus or minus 5 percent of the mean relation for the prototype. The stage-discharge relation is not affected by backwater for values of submergence less than 90 percent. There is no consistent relation between the ratio of measured discharge to rated discharge and submergence for values of submergence greater than 90 percent. \r\n\r\nThe control does not restrict the channel capacity to less than the stated design capacity of 2,000 cubic feet per second. When the control is drowned out, or ineffective, the relation of water-surface elevation to water discharge is virtually the same as that prior to construction of the control for discharges greater than 1,500 cubic feet per second. When the control is not drowned out--that is, free-fall conditions exist--the water-surface elevation for a discharge of 2,000 cubic feet per second is greater than the minimum elevation, but is less than the maximum elevation that occurred at that discharge prior to construction. \r\n\r\nThe model study was only partially successful in predicting the operating characteristics of the prototype. Some of the differences between prototype operation and model predictions may exist because the prototype was not built exactly as recommended on the basis of the model study. In general, the prototype has operated somewhat better than the model predicted.","language":"ENGLISH","publisher":"U. S. Govt. Print. Off.,","doi":"10.3133/wsp1898A","usgsCitation":"Gonzalez, D.D., Scott, C., and Culbertson, J.K., 1969, Stage-discharge characteristics of a Weir in a sand-channel stream: U.S. Geological Survey Water Supply Paper 1898, iii, 29 p., https://doi.org/10.3133/wsp1898A.","productDescription":"iii, 29 p.","costCenters":[],"links":[{"id":137040,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1898a/report-thumb.jpg"},{"id":26775,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1898a/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e478fe4b07f02db48a1b7","contributors":{"authors":[{"text":"Gonzalez, Don D.","contributorId":49774,"corporation":false,"usgs":true,"family":"Gonzalez","given":"Don","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":143978,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Scott, C.H.","contributorId":101634,"corporation":false,"usgs":true,"family":"Scott","given":"C.H.","email":"","affiliations":[],"preferred":false,"id":143979,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Culbertson, James K.","contributorId":31371,"corporation":false,"usgs":true,"family":"Culbertson","given":"James","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":143977,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":1143,"text":"wsp1608L - 1969 - Evaluation and control of corrosion and encrustation in tube wells of the Indus Plains, West Pakistan","interactions":[{"subject":{"id":22722,"text":"ofr6436 - 1964 - Preliminary evaluation of corrosion and encrustation mechanisms in tube wells of the Indus Plains, West Pakistan","indexId":"ofr6436","publicationYear":"1964","noYear":false,"title":"Preliminary evaluation of corrosion and encrustation mechanisms in tube wells of the Indus Plains, West Pakistan"},"predicate":"SUPERSEDED_BY","object":{"id":1143,"text":"wsp1608L - 1969 - Evaluation and control of corrosion and encrustation in tube wells of the Indus Plains, West Pakistan","indexId":"wsp1608L","publicationYear":"1969","noYear":false,"chapter":"L","title":"Evaluation and control of corrosion and encrustation in tube wells of the Indus Plains, West Pakistan"},"id":1},{"subject":{"id":52566,"text":"ofr6745 - 1967 - Evaluation and control of corrosion and encrustation in tube wells of the Indus Plain, West Pakistan","indexId":"ofr6745","publicationYear":"1967","noYear":false,"title":"Evaluation and control of corrosion and encrustation in tube wells of the Indus Plain, West Pakistan"},"predicate":"SUPERSEDED_BY","object":{"id":1143,"text":"wsp1608L - 1969 - Evaluation and control of corrosion and encrustation in tube wells of the Indus Plains, West Pakistan","indexId":"wsp1608L","publicationYear":"1969","noYear":false,"chapter":"L","title":"Evaluation and control of corrosion and encrustation in tube wells of the Indus Plains, West Pakistan"},"id":2}],"lastModifiedDate":"2012-02-02T00:05:18","indexId":"wsp1608L","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":"1608","chapter":"L","title":"Evaluation and control of corrosion and encrustation in tube wells of the Indus Plains, West Pakistan","docAbstract":"Seepage from rivers and irrigation canals has contributed to waterlogging and soil salinization problems in much of the Indus Plains of West Pakistan. These problems are being overcome in part by tube-well dewatering and deep leaching of salinized soils. The ground waters described here are anaerobic and some are supersaturated with troublesome minerals such as calcium carbonate (calcite) and iron carbonate (siderite). These waters are moderately corrosive to steel. Some wells contain sulfate-reducing bacteria, which catalyze corrosion, and pH-electrode potential relationships favorable to the solution of iron also are rather common. Corrosion is concentrated in the relatively active (anodic) saw slots of water-well filter pipes (screens), where metal loss is least tolerable. Local changes in chemical properties of the water, because of corrosion, apparently cause deposition of calcium carbonate, iron carbonate, and other minerals which clog the filter pipes. In some places well capacities are seriously reduced in very short periods of time. There appears to be no practicable preventive treatment for corrosion and encrustation in these wells. Even chemical sterilization for bacterial control has yielded poor results. Periodic rehabilitation by down-hole blasting or by other effective mechanical or chemical cleaning methods will prolong well life. It may be possible to repair severely damaged well screens by inserting perforated sleeves of plastic or other inert material. \r\n\r\nThe most promising approach to future, well-field development is to use filter pipes of epoxy-resin-bonded fiber glass, stainless steel, or other inert material which minimizes both corrosion and corrosion-catalyzed encrustation. Fiberglass plastic pipe appears to be the most economically practicable construction material at this time and already is being used with promising results.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1608L","usgsCitation":"Clarke, F., and Barnes, I., 1969, Evaluation and control of corrosion and encrustation in tube wells of the Indus Plains, West Pakistan: U.S. Geological Survey Water Supply Paper 1608, vi, 63 p. : ill., maps ;22 cm., https://doi.org/10.3133/wsp1608L.","productDescription":"vi, 63 p. : ill., maps ;22 cm.","costCenters":[],"links":[{"id":137622,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1608l/report-thumb.jpg"},{"id":25924,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1608l/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a50e4b07f02db629652","contributors":{"authors":[{"text":"Clarke, Frank Eldridge","contributorId":107255,"corporation":false,"usgs":true,"family":"Clarke","given":"Frank Eldridge","affiliations":[],"preferred":false,"id":143250,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Barnes, Ivan","contributorId":56619,"corporation":false,"usgs":true,"family":"Barnes","given":"Ivan","email":"","affiliations":[],"preferred":false,"id":143249,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":3207,"text":"wsp1591D - 1969 - Considerations involved in evaluating mathematical modeling of urban hydrologic systems","interactions":[],"lastModifiedDate":"2012-02-02T00:05:25","indexId":"wsp1591D","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":"1591","chapter":"D","title":"Considerations involved in evaluating mathematical modeling of urban hydrologic systems","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1591D","usgsCitation":"Dawdy, D.R., 1969, Considerations involved in evaluating mathematical modeling of urban hydrologic systems: U.S. Geological Survey Water Supply Paper 1591, 1 v. (issued as seperate chapters) :ill. ;24 cm. ;18 p., https://doi.org/10.3133/wsp1591D.","productDescription":"1 v. (issued as seperate chapters) :ill. ;24 cm. ;18 p.","costCenters":[],"links":[{"id":138134,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1591d/report-thumb.jpg"},{"id":30197,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1591d/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b12e4b07f02db6a2f95","contributors":{"authors":[{"text":"Dawdy, David R.","contributorId":75125,"corporation":false,"usgs":true,"family":"Dawdy","given":"David","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":146432,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":55893,"text":"ofr6953 - 1969 - Digital computer modeling for estimating mine-drainage problems, Piceance Creek basin, northwestern Colorado","interactions":[],"lastModifiedDate":"2014-07-15T11:30:30","indexId":"ofr6953","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":"69-53","title":"Digital computer modeling for estimating mine-drainage problems, Piceance Creek basin, northwestern Colorado","docAbstract":"No abstract available.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/ofr6953","usgsCitation":"Coffin, D.L., and Bredehoeft, J.D., 1969, Digital computer modeling for estimating mine-drainage problems, Piceance Creek basin, northwestern Colorado: U.S. Geological Survey Open-File Report 69-53, 20 p., https://doi.org/10.3133/ofr6953.","productDescription":"20 p.","numberOfPages":"20","costCenters":[],"links":[{"id":181535,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b32e4b07f02db6b464c","contributors":{"authors":[{"text":"Coffin, Donald L.","contributorId":90696,"corporation":false,"usgs":true,"family":"Coffin","given":"Donald","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":254429,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bredehoeft, John D.","contributorId":86747,"corporation":false,"usgs":true,"family":"Bredehoeft","given":"John","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":254428,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70112275,"text":"70112275 - 1969 - The geographic applications program of the U. S. Geological Survey","interactions":[],"lastModifiedDate":"2017-03-27T13:58:42","indexId":"70112275","displayToPublicDate":"1990-06-12T11:43:00","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3051,"text":"Photogrammetric Engineering","active":true,"publicationSubtype":{"id":10}},"title":"The geographic applications program of the U. S. Geological Survey","docAbstract":"The fundamental objective of modern Geography is to improve man's level of living through a better understanding of man-environment inter actions. Related goals of the USGS program for applications of remote sensor data to Geographical research are: (1) the analysis and improvement of land use, with special emphasis on urban problems; and (2) more effective use of the total available energy budget, including insolation, mineral fuels, atomic energy, human resources, and mental energy, all of which are integrated into man-environment interactions. The collection of data through remote sensors in air craft and spacecraft is financed largely by funds from NASA, and is part of the much broader EROS Program of the Department of the Interior. Results to date have achieved much toward the identification of remote sensor signatures for Earth features and human activities, and toward evaluation of instruments for collecting essential information.
","language":"English","publisher":"American Society of Photogrammetry","publisherLocation":"Falls Church, VA","usgsCitation":"Gerlach, A.C., 1969, The geographic applications program of the U. S. Geological Survey: Photogrammetric Engineering, v. 35, no. 1, p. 58-60.","productDescription":"3 p.","startPage":"58","endPage":"60","numberOfPages":"3","costCenters":[{"id":222,"text":"Earth Resources Observation and Science (EROS) Center","active":true,"usgs":true}],"links":[{"id":288477,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"35","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"539acc58e4b0e83db6d0902b","contributors":{"authors":[{"text":"Gerlach, Arch C.","contributorId":78249,"corporation":false,"usgs":true,"family":"Gerlach","given":"Arch","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":494608,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70207466,"text":"70207466 - 1969 - Interstitial water studies on small core samples, Deep Sea Drilling Project, Leg 1","interactions":[],"lastModifiedDate":"2019-12-19T16:46:01","indexId":"70207466","displayToPublicDate":"1969-12-31T16:41:16","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1997,"text":"Initial reports of the Deep Sea Drilling Project","active":true,"publicationSubtype":{"id":10}},"title":"Interstitial water studies on small core samples, Deep Sea Drilling Project, Leg 1","docAbstract":"The most dramatic variations in pore water composition occurred in Holes 2 and 3 in the Gulf of Mexico. Both holes showed a strong increase in salinity with depth, evidently owing to diffusion from underlying salt bodies. However, on Challenger Knoll (Hole 2) a sharp drop in salinity was observed in the cap rock of the salt dome in which chloride fell to only 4.8 percent. The drop is attributed to production of fresh water during the formation of native sulfur.
Outside of the Gulf of Mexico, changes in total salinity with depth did not exceed a few percent, but differences in diagenetic modification of the ionic ratios of sea water were pronounced. In nondiapiric strata in the Gulf of Mexico (Hole 1) both magnesium and potassium were depleted in the pore waters, whereas in the open ocean holes (4, 5, 6, and 7), potassium appeared in excess. Water content (porosity) of the cores was irregular.
","language":"English","publisher":"National Science Foundation","doi":"10.2973/dsdp.proc.1.120.1969","usgsCitation":"Manheim, F.T., and Sayles, F., 1969, Interstitial water studies on small core samples, Deep Sea Drilling Project, Leg 1: Initial reports of the Deep Sea Drilling Project, v. 1, p. 403-410, https://doi.org/10.2973/dsdp.proc.1.120.1969.","productDescription":"11 p.","startPage":"403","endPage":"410","costCenters":[{"id":678,"text":"Woods Hole Coastal and Marine Science Center","active":true,"usgs":true}],"links":[{"id":488839,"rank":0,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.2973/dsdp.proc.1.120.1969","text":"Publisher Index Page"},{"id":370524,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"1","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Manheim, Frank T. 0000-0003-4005-4524","orcid":"https://orcid.org/0000-0003-4005-4524","contributorId":20770,"corporation":false,"usgs":true,"family":"Manheim","given":"Frank","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":778156,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Sayles, F.L.","contributorId":77657,"corporation":false,"usgs":true,"family":"Sayles","given":"F.L.","email":"","affiliations":[],"preferred":false,"id":778157,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70207273,"text":"70207273 - 1969 - The relationship between fluids in some fresh alpine-type ultramafics and possible modern serpentinization, western United States","interactions":[],"lastModifiedDate":"2019-12-15T13:35:58","indexId":"70207273","displayToPublicDate":"1969-12-31T13:35:23","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 relationship between fluids in some fresh alpine-type ultramafics and possible modern serpentinization, western United States","docAbstract":"Calcium hydroxide waters issue from four partly serpentinized Alpine-type ultramafic bodies in the western United States. The occurrence of calcium-hydroxide-type water is restricted to fresh Alpine-type ultramafic rocks. The calcium hydroxide waters are unsaturated with Mg end-member olivine and pyroxene but supersaturated with Mg end-member brucite and serpentine and thus have chemical potentials to cause Serpentinization. The calcium hydroxide waters are isotopically similar to the common magnesium bicarbonate meteoric waters peculiar to ultramafic rocks and serpentinites. Some Serpentinization is apparently a near-surface phenomenon occurring at present. The Serpentinization takes place at nearly constant composition, except for loss of CaO. © 1969, The Geological Society of America, Inc.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1969)80[1947:TRBFIS]2.0.CO;2","issn":"00167606","usgsCitation":"Barnes, I., and O’Neil, J.R., 1969, The relationship between fluids in some fresh alpine-type ultramafics and possible modern serpentinization, western United States: Geological Society of America Bulletin, v. 80, no. 10, p. 1947-1960, https://doi.org/10.1130/0016-7606(1969)80[1947:TRBFIS]2.0.CO;2.","productDescription":"14 p. ","startPage":"1947","endPage":"1960","costCenters":[],"links":[{"id":370279,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"80","issue":"10","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Barnes, I.","contributorId":23678,"corporation":false,"usgs":true,"family":"Barnes","given":"I.","affiliations":[],"preferred":false,"id":777511,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"O’Neil, J. R.","contributorId":111576,"corporation":false,"usgs":true,"family":"O’Neil","given":"J.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":777512,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ]}