Anchorage, Alaska’s largest city, is about 80 miles west-northwest of the epicenter of the March 27 earthquake. Because of its size, Anchorage bore the brunt of property damage from the quake; it sustained greater losses than all the rest of Alaska combined. Damage was caused by direct seismic vibration, by ground cracks, and by landslides. Direct seismic vibration affected chiefly multistory buildings and buildings having large floor areas, probably because of the long period and large amplitude of the seismic waves reaching Anchorage. Most small buildings were spared. Ground cracks caused capricious damage throughout the Anchorage Lowland. Cracking was most prevalent near the heads or within landslides but was also widespread elsewhere. Landslides themselves caused the most devastating damage.
Triggering of landslides by the earthquake was related to the physical-engineering properties of the Bootlegger Cove Clay, a glacial estuarine-marine deposit that underlies much of the Anchorage area. The Bootlegger Cove Clay contains zones of low shear strength, high water content, and high sensitivity that failed under the vibratory stress of the earthquake. Shear strength in sensitive zones ranged from less than 0.2 tsf to about 0.5 tsf; sensitivity ranged from about 10 to more than 40. Sensitive zones generally are centered about 10 to 20 feet above sea level, between zones of stiff insensitive clay. Many physical tests by the U.S. Army Corps of Engineers were directed toward analyzing the causes of failure in the Bootlegger Cove Clay and finding possible remedies. Strengths and sensitivities were measured directly in the field by means of vane shear apparatus. A4tterberg limits, natural water contents, triaxial shear, sensitivity, dynamic modulus, consolidation strength, and other properties were measured in the laboratory. Pulsating-load tests simulated earthquake loading.
Most of the destructive landslides in the Anchorage area moved primarily by translation rather than by rotation. Thus, all the highly damaging slides were of a single structural dynamic family despite wide variations in size, appearance, and complexity. They slid on nearly horizontal slip surfaces after loss of strength in the Bootlegger Core Clay. Same failures are attributed to spontaneous liquefaction of sand layers. All translatory slides surmounted flat-topped bluffs bounded marginally by steep slopes facing lower ground. Destructive translatory slides occurred in the downtown area (Fourth Avenue slide and L Street slide), at Government Hill, and at Turnagain Heights. Less destructive slides occurred in many other places-mostly uninhabited or undeveloped areas.
In most translatory slides, damage was greatest in graben areas at the head and in pressure-ridge areas at the toe. Many buildings inside the perimeters of slide blocks were little damaged despite horizontal translations of several feet. The large Turnagain Heights slide, however, was characterized by a complete disintegration and drastic lowering of the prequake land surface. Extensive damage back from the slide, moreover, was caused by countless tension cracks.
An approximation of the depth of failure in the Bootlegger Cove Clay in the various slides may be obtained by using a geometric relationship herein called the \"graben rule.\" Because the cross-sectional area of the graben at the head of the slide approximated the cross-sectional area of the space voided behind the slide block as the block moved outward, the depth of failure was equal to the area of the graben divided by the lateral displacement. This approximation supplements and accords with test data obtained from borings. The graben rule should apply to any translatory slide in which flowage of material from the zone of failure has not been excessive.
Geologic evidence indicates that landslides similar to those triggered by the March 27 earthquake have occurred in the Anchorage area at various times in the past.
","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/pp542A","usgsCitation":"Hansen, W.R., 1965, Effects of the earthquake of March 27, 1964, at Anchorage, Alaska: U.S. Geological Survey Professional Paper 542, Report: iv, 68 p.; 2 Plates: 50.44 x 26.21 inches and 35.05 x 10.13 inches, https://doi.org/10.3133/pp542A.","productDescription":"Report: iv, 68 p.; 2 Plates: 50.44 x 26.21 inches and 35.05 x 10.13 inches","numberOfPages":"77","additionalOnlineFiles":"Y","costCenters":[{"id":380,"text":"Menlo ParkCalif. Office-Earthquake Science Center","active":false,"usgs":true}],"links":[{"id":399840,"rank":6,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4583.htm"},{"id":170342,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0542a/report-thumb.jpg"},{"id":113265,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0542a/pp542a_plate2.pdf","size":"1792","linkFileType":{"id":1,"text":"pdf"}},{"id":113264,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0542a/pp542a_plate1.pdf","size":"7988","linkFileType":{"id":1,"text":"pdf"}},{"id":113263,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0542a/pp542a_text.pdf","size":"19635","linkFileType":{"id":1,"text":"pdf"}},{"id":111457,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pp/0542a/index.html","linkFileType":{"id":5,"text":"html"}}],"scale":"2400","country":"United States","state":"Alaska","city":"Anchorage","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -150.100708,60.999438 ], [ -150.100708,61.301243 ], [ -149.624949,61.301243 ], [ -149.624949,60.999438 ], [ -150.100708,60.999438 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a27e4b07f02db61031d","contributors":{"authors":[{"text":"Hansen, Wallace R.","contributorId":90273,"corporation":false,"usgs":true,"family":"Hansen","given":"Wallace","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":220531,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":38845,"text":"pp542B - 1965 - Effects of the earthquake of March 27, 1964, at Whittier, Alaska","interactions":[{"subject":{"id":38845,"text":"pp542B - 1965 - Effects of the earthquake of March 27, 1964, at Whittier, Alaska","indexId":"pp542B","publicationYear":"1965","noYear":false,"chapter":"B","title":"Effects of the earthquake of March 27, 1964, at Whittier, Alaska"},"predicate":"IS_PART_OF","object":{"id":70048211,"text":"pp542 - 1969 - The Alaska earthquake, March 27, 1964: Effects on communities","indexId":"pp542","publicationYear":"1969","noYear":false,"title":"The Alaska earthquake, March 27, 1964: Effects on communities"},"id":1}],"isPartOf":{"id":70048211,"text":"pp542 - 1969 - The Alaska earthquake, March 27, 1964: Effects on communities","indexId":"pp542","publicationYear":"1969","noYear":false,"title":"The Alaska earthquake, March 27, 1964: Effects on communities"},"lastModifiedDate":"2022-04-28T20:06:42.908474","indexId":"pp542B","displayToPublicDate":"1994-01-01T07:00:00","publicationYear":"1965","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":"542","chapter":"B","title":"Effects of the earthquake of March 27, 1964, at Whittier, Alaska","docAbstract":"Whittier, Alaska, lying at the western end of Passage Canal, is an ocean terminal of The Alaska Railroad. The earthquake that shook south-central Alaska at 5:36 p.m. (Alaska Standard Time) on March 27, 1964, took the lives of 13 persons and caused more than $5 million worth of damage to Government and private property at Whittier.
\n\nSeismic motion lasted only 2½-3 minutes, but when it stopped the Whittier waterfront was in shambles land the port facilities were inoperable. Damage was caused by (1) a 5.3-foot subsidence of the landmass, sufficient to put some of the developed land under water during high tides, (2) seismic shock, (3) fracturing of fill and unconsolidated sediments, (4) compaction of fill and unconsolidated deposits, (5) submarine landslides which generated waves that destroyed part of The Alaska Railroad roadbed and other property, (6) at least two, but probably three, waves generated by landslides, which completely wrecked the buildings of two lumber companies, the stub pier, the small-boat harbor, the car-barge slip dock, and several homes, and (7) fire that destroyed the fuel-storage tanks at the Whittier waterfront.
\n\nMany buildings and other facilities were totally wrecked, others were damaged to lesser degrees. For example, the 14-story reinforced concrete Hodge Building, which rests upon at least 44 feet of sandy gravel, was moderately damaged by seismic shock, but the six-story reinforced-concrete Buckner Building, which rests upon bedrock, was only slightly damaged.
","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/pp542B","usgsCitation":"Kachadoorian, R., 1965, Effects of the earthquake of March 27, 1964, at Whittier, Alaska: U.S. Geological Survey Professional Paper 542, Report: vi, 21 p.; 3 Plates: 40 x 20.5 inches or smaller, https://doi.org/10.3133/pp542B.","productDescription":"Report: vi, 21 p.; 3 Plates: 40 x 20.5 inches or smaller","numberOfPages":"29","additionalOnlineFiles":"Y","costCenters":[{"id":380,"text":"Menlo ParkCalif. Office-Earthquake Science Center","active":false,"usgs":true}],"links":[{"id":65806,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0542b/pp542b_plate2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":65805,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0542b/pp542b_plate1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":65808,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0542b/pp542b_text.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":399842,"rank":7,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4584.htm"},{"id":122275,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0542b/report-thumb.jpg"},{"id":104502,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pp/0542b/index.html","linkFileType":{"id":5,"text":"html"},"description":"4584"},{"id":65807,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0542b/pp542b_plate3.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"4800","datum":"Preearthquake Mean Sea Level","country":"United States","state":"Alaska","city":"Whittier","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -148.739934,60.765962 ], [ -148.739934,60.787502 ], [ -148.64941,60.787502 ], [ -148.64941,60.765962 ], [ -148.739934,60.765962 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a27e4b07f02db610281","contributors":{"authors":[{"text":"Kachadoorian, Reuben","contributorId":24336,"corporation":false,"usgs":true,"family":"Kachadoorian","given":"Reuben","email":"","affiliations":[],"preferred":false,"id":220532,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1810,"text":"wsp1697 - 1965 - Geology and ground water of the Tualatin Valley, Oregon","interactions":[{"subject":{"id":14012,"text":"ofr5559 - 1956 - Preliminary report on the ground-water resources of the Tualatin Valley, Oregon","indexId":"ofr5559","publicationYear":"1956","noYear":false,"title":"Preliminary report on the ground-water resources of the Tualatin Valley, Oregon"},"predicate":"SUPERSEDED_BY","object":{"id":1810,"text":"wsp1697 - 1965 - Geology and ground water of the Tualatin Valley, Oregon","indexId":"wsp1697","publicationYear":"1965","noYear":false,"title":"Geology and ground water of the Tualatin Valley, Oregon"},"id":1}],"lastModifiedDate":"2017-02-03T13:40:41","indexId":"wsp1697","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","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":"1697","title":"Geology and ground water of the Tualatin Valley, Oregon","docAbstract":"The Tualatin Valley proper consists of broad valley plains, ranging in altitude from 100 to 300 feet, and the lower mountain slopes of the drainage basin of the Tualatin River, a tributary of the Willamette River in northwestern Oregon. The valley is almost entirely farmed. Its population is increasing rapidly, partly because of the expansion of metropolitan Portland. \r\n\r\nStructurally, the bedrock of the basin is a saucer-shaped syncline almost bisected lengthwise by a ridge. The bedrock basin has been partly filled by alluvium, which underlies the valley plains. \r\n\r\nGround water occurs in the Columbia River basalt, a lava unit that forms the top several hundred feet of the bedrock, and also in the zones of fine sand in the upper part of the alluvial fill. It occurs under unconfined, confined, and perched conditions. Graphs of the observed water levels in wells show that the ground water is replenished each year by precipitation. The graphs show also that the amount and time of recharge vary in different aquifers and for different modes of ground-water occurrence. The shallower alluvial aquifers are refilled each year to a level where further infiltration recharge is retarded and water drains away as surface runoff. No occurrences of undue depletion of the ground water by pumping are known. The facts indicate that there is a great quantity of additional water available for future development. The ground water is developed for use by some spring works and by thousands of wells, most of which are of small yield. Improvements are now being made in the design of the wells in basalt and in the use of sand or gravel envelopes for wells penetrating the fine-sand aquifers. \r\n\r\nThe ground water in the basalt and the valley fill is in general of good quality, only slightly or moderately hard and of low salinity. Saline and mineralized water is present in the rocks of Tertiary age below the Columbia River basalt. Under certain structural and stratigraphic conditions this water of poor quality contaminates the fresh-water aquifers. \r\n\r\nDetailed hydrologic and geologic conditions are presented in 5 tables, 7 pictures, and 17 graphic figures and plates.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1697","usgsCitation":"Hart, D.H., and Newcomb, R.C., 1965, Geology and ground water of the Tualatin Valley, Oregon: U.S. Geological Survey Water Supply Paper 1697, v, 172 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1697.","productDescription":"v, 172 p. :ill., maps ;24 cm.","costCenters":[{"id":518,"text":"Oregon Water Science Center","active":true,"usgs":true}],"links":[{"id":26969,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1697/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26970,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1697/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26971,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1697/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26972,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1697/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137172,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1697/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adce4b07f02db68618e","contributors":{"authors":[{"text":"Hart, D. H.","contributorId":16811,"corporation":false,"usgs":true,"family":"Hart","given":"D.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":144192,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Newcomb, R. C.","contributorId":77907,"corporation":false,"usgs":true,"family":"Newcomb","given":"R.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":144193,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":15430,"text":"ofr65123 - 1965 - Veins in the northern part of the Boulder batholith, Montana","interactions":[],"lastModifiedDate":"2012-02-02T00:07:08","indexId":"ofr65123","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","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":"65-123","title":"Veins in the northern part of the Boulder batholith, Montana","docAbstract":"About 20 miles north of Butte and extending nearly to Helena, is an area of 350 square miles containing hundreds of veins and altered zones. The bedrock of the area is 1) late Cretaceous volcanic rocks, forerunners of the Boulder batholith, 2) the Boulder batholith of late Cretaceous to early Tertiary age and 3) two groups of Tertiary volcanic rocks lying on the eroded batholith. The veins are post-batholith and pre-Tertiary in age.\r\n\r\nThe veins are largely either quartz-sulfide veins of mesothermal type or chalcedony veins of epithermal type. The relations of these two types of veins have been the subject of conflicting ideas for 60 years. Three workers have proposed three different genetic classifications. This report shows that the quartz veins and the chalcedony veins are closely related parts of a strongly zoned hypogene vein system.\r\n\r\nStrong zonal patterns were established using the grain size of quartz (or pyrite vs. carbonate in one district) as well as features of the altered rocks. The scale of the zoning ranges from single veins through groups of veins or mining districts to the entire mineralized area. Single veins are zoned around a core of coarse-grained quartz; the quartz outward from the core becoming progressively finer-grained. The cores are zoned around eight major centers and several lesser ones. The centers and their nearby related veins are assigned to central, intermediate, and peripheral zones. Nearly all of the veins around the edge of the mineralized area are chalcedony.\r\n\r\nEnvelopes of altered rocks consist of seven major bands representing three major groups of constituents, aluminum silicates, iron-bearing minerals, and silica. Plagioclase altered successively to montomorillite, kaolinite, and sericite; potassium feldspar altered to sericite (aluminum silicate group). Biotite released iron which formed successively, iron oxides, iron-bearing carbonate, and pyrite (iron-bearing minerals). Excess silica formed silicified bands. Constituents for which no stable phase occurs were largely leached from the rocks.\r\n\r\nA model has been constructed showing the arrangement of zoned veins and altered rocks in which the minerals produced by alteration are arranged in bands on each side of the vein, similar to the Butte pattern. Along strike from the cores, the inner bands thin and pinch out against the vein so that the vein becomes enclosed successively in the next outer bands. The sequence of alteration minerals along the veins is sericite, kaolinite, and montmorillonite for the aluminum silicates; and pyrite, carbonate, and iron oxides for the iron-bearing minerals.\r\n\r\nAlteration is thought to be controlled by reactions between wallrock minerals and the pore solution. In the aluminum silicate reactions, H+ was added to the rock and Na+ and Ca++ were removed. Carbon and sulfur from the vein were added to iron of the wallrock to produce pyrite and iron carbonate. Carbon, sulfur, and hydrogen moved into the wallrock, while Ca++, Na+, and some SiO2 moved toward the vein along concentration or activity gradients.\r\n\r\nTemperatures during mineralization ranged from below 200? C to about 350? C.","language":"ENGLISH","publisher":"U.S. Geological Survey],","doi":"10.3133/ofr65123","usgsCitation":"Pinckney, D.M., 1965, Veins in the northern part of the Boulder batholith, Montana: U.S. Geological Survey Open-File Report 65-123, 154 p. ill. (some col.), maps (some col., some folded) ;29 cm., https://doi.org/10.3133/ofr65123.","productDescription":"154 p. ill. (some col.), maps (some col., some folded) ;29 cm.","costCenters":[],"links":[{"id":148636,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1965/0123/report-thumb.jpg"},{"id":44386,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1965/0123/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":44387,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1965/0123/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":44388,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1965/0123/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":44389,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1965/0123/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":44390,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1965/0123/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":44391,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1965/0123/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":44392,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1965/0123/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":44393,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1965/0123/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a13e4b07f02db6022ad","contributors":{"authors":[{"text":"Pinckney, D. M.","contributorId":33336,"corporation":false,"usgs":true,"family":"Pinckney","given":"D.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":171129,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1231,"text":"wsp1809D - 1965 - An evaluation of aquifer and well characteristics of municipal well fields in Los Alamos and Guaje Canyons, near Los Alamos, New Mexico","interactions":[],"lastModifiedDate":"2012-02-02T00:05:18","indexId":"wsp1809D","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","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":"1809","chapter":"D","title":"An evaluation of aquifer and well characteristics of municipal well fields in Los Alamos and Guaje Canyons, near Los Alamos, New Mexico","docAbstract":"The Jenkins-Whitesburg area includes approximately 250 square miles In Letcher and Pike Counties in the southeastern part of the Eastern Coal Field. In this area ground water is the principal source of water for nearly all rural families, most public supplies, several coal mines and coal processing plants, and one bottling plant. \r\n\r\nThe major aquifers in the Jenkins-Whitesburg area are the Breathitt and Lee Formations of Pennsylvanian age. Other aquifers range in age from Devonian to Quaternary but are not important in this area because they occur at great depth or yield little or no water. The Breathitt Formation occurs throughout the area except along the crest and slopes of Pine Mountain and where it is covered by unconsolidated material of Quaternary age. The Breathitt Formation consists of shale, sandstone, and lesser amounts of coal and associated underclay. The yield of wells penetrating the Breathitt Formation ranges from less than 1 to 330 gallons per minute. Well yield is controlled by the type and depth of well, character of the aquifer, and topography of the well site. Generally, deep wells drilled in valleys of perennial streams offer the best potential for high yields. Although enough water for a minimum domestic supply (more than 100 gallons per day) may be obtained from shale, all high-yielding wells probably obtain water from vertical joints and from bedding planes which are best developed in sandstone. About 13 percent of the wells inventoried in the Breathitt Formation failed to supply enough water for a minimum domestic supply. Most of these are shallow dug wells or drilled wells on hillsides or hilltops. Abandoned coal dunes are utilized as large infiltration galleries and furnish part of the water for several public supplies. \r\n\r\nThe chemical quality of water from the Breathitt Formation varies considerably from place to place, but the water generally is acceptable for most domestic and industrial uses. Most water is a calcium magnesium bicarbonate or sodium bicarbonate type, and nearly all sampled water contained enough iron to stain cooking and laundry utensils. The water ranged from soft to very hard, and only one well in the Breathitt Formation produced salty water. The absence of salty water may be due to abundant fractures which are associated with the Pine Mountain fault and which have allowed fresh water to enter the formation. The Lee Formation underlies the Cumberland Mountain section and is exposed along the crest and southeast slope of Pine Mountain. The Lee Formation consists of massive sandstone and conglomerate with thin beds of shale and a few thin coal seams.\r\n\r\nAlthough the Lee Formation is tapped by only a few wells in this area, it is potentially an important aquifer. Wells penetrating the Lee Formation in the Cumberland Mountain section would probably yield water under artesian pressure.\r\n\r\nUnlike most water from the Lee Formation in other part.3 of eastern Kentucky, all water from the Lee Formation in the Jenkins-Whitesburg area is fresh. All water from the Lee Formation contained more than 0.3 parts per million of iron and ranged from soft to moderately hard.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1809D","usgsCitation":"Cushman, R., 1965, An evaluation of aquifer and well characteristics of municipal well fields in Los Alamos and Guaje Canyons, near Los Alamos, New Mexico: U.S. Geological Survey Water Supply Paper 1809, v, 50 p. :ill., maps ;24 cm. + plates folded in pocket., https://doi.org/10.3133/wsp1809D.","productDescription":"v, 50 p. :ill., maps ;24 cm. + plates folded in pocket.","costCenters":[],"links":[{"id":138069,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1809d/report-thumb.jpg"},{"id":26149,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1809d/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26150,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1809d/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26151,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1809d/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26152,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1809d/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26153,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1809d/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad8e4b07f02db684a57","contributors":{"authors":[{"text":"Cushman, Robert L.","contributorId":22751,"corporation":false,"usgs":true,"family":"Cushman","given":"Robert L.","affiliations":[],"preferred":false,"id":143410,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1132,"text":"wsp1809P - 1965 - Water-supply potential from an asphalt-lined catchment near Holualoa Kona, Hawaii","interactions":[],"lastModifiedDate":"2012-02-02T00:05:18","indexId":"wsp1809P","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","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":"1809","chapter":"P","title":"Water-supply potential from an asphalt-lined catchment near Holualoa Kona, Hawaii","docAbstract":"The Jenkins-Whitesburg area includes approximately 250 square miles In Letcher and Pike Counties in the southeastern part of the Eastern Coal Field. In this area ground water is the principal source of water for nearly all rural families, most public supplies, several coal mines and coal processing plants, and one bottling plant. \r\n\r\nThe major aquifers in the Jenkins-Whitesburg area are the Breathitt and Lee Formations of Pennsylvanian age. Other aquifers range in age from Devonian to Quaternary but are not important in this area because they occur at great depth or yield little or no water. The Breathitt Formation occurs throughout the area except along the crest and slopes of Pine Mountain and where it is covered by unconsolidated material of Quaternary age. The Breathitt Formation consists of shale, sandstone, and lesser amounts of coal and associated underclay. The yield of wells penetrating the Breathitt Formation ranges from less than 1 to 330 gallons per minute. Well yield is controlled by the type and depth of well, character of the aquifer, and topography of the well site. Generally, deep wells drilled in valleys of perennial streams offer the best potential for high yields. Although enough water for a minimum domestic supply (more than 100 gallons per day) may be obtained from shale, all high-yielding wells probably obtain water from vertical joints and from bedding planes which are best developed in sandstone. About 13 percent of the wells inventoried in the Breathitt Formation failed to supply enough water for a minimum domestic supply. Most of these are shallow dug wells or drilled wells on hillsides or hilltops. Abandoned coal mines are utilized as large infiltration galleries and furnish part of the water for several public supplies. \r\n\r\nThe chemical quality of water from the Breathitt Formation varies considerably from place to place, but the water generally is acceptable for most domestic and industrial uses. Most water is a calcium magnesium bicarbonate or sodium bicarbonate type, and nearly all sampled water contained enough iron to stain cooking and laundry utensils. The water ranged from soft to very hard, and only one well in the Breathitt Formation produced salty water. The absence of salty water may be due to abundant fractures which are associated with the Pine Mountain fault and which have allowed fresh water to enter the formation. The Lee Formation underlies the Cumberland Mountain section and is exposed along the crest and southeast slope of Pine Mountain. The Lee Formation consists of massive sandstone and conglomerate with thin beds of shale and a few thin coal seams.\r\n\r\nAlthough the Lee Formation is tapped by only a few wells in this area, it is potentially an important aquifer. Wells penetrating the Lee Formation in the Cumberland Mountain section would probably yield water under artesian pressure.\r\n\r\nUnlike most water from the Lee Formation in other part.3 of eastern Kentucky, all water from the Lee Formation in the Jenkins-Whitesburg area is fresh. All water from the Lee Formation contained more than 0.3 parts per million of iron and ranged from soft to moderately hard.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1809P","usgsCitation":"Chinn, S.S., 1965, Water-supply potential from an asphalt-lined catchment near Holualoa Kona, Hawaii: U.S. Geological Survey Water Supply Paper 1809, iv, 25 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1809P.","productDescription":"iv, 25 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":137947,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1809p/report-thumb.jpg"},{"id":25912,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1809p/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e2e4b07f02db5e4bd7","contributors":{"authors":[{"text":"Chinn, Salwyn S.W.","contributorId":91082,"corporation":false,"usgs":true,"family":"Chinn","given":"Salwyn","email":"","middleInitial":"S.W.","affiliations":[],"preferred":false,"id":143231,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":12412,"text":"ofr651 - 1965 - Chemical and modal analyses of the pre-Upper Silurian quartz monzonite, and the post-Lower Devonian granodiorite, Attean quadrangle, Somerset County, Maine","interactions":[],"lastModifiedDate":"2025-06-17T18:52:19.455196","indexId":"ofr651","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","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":"65-1","title":"Chemical and modal analyses of the pre-Upper Silurian quartz monzonite, and the post-Lower Devonian granodiorite, Attean quadrangle, Somerset County, Maine","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr651","usgsCitation":"Albee, A.L., 1965, Chemical and modal analyses of the pre-Upper Silurian quartz monzonite, and the post-Lower Devonian granodiorite, Attean quadrangle, Somerset County, Maine: U.S. Geological Survey Open-File Report 65-1, 3 p., https://doi.org/10.3133/ofr651.","productDescription":"3 p.","costCenters":[],"links":[{"id":490880,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1965/0001/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":144330,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1965/0001/report-thumb.jpg"}],"country":"United States","state":"Maine","county":"Somerset County","otherGeospatial":"Attean 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\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e1e4b07f02db5e487c","contributors":{"authors":[{"text":"Albee, Arden Leroy","contributorId":83912,"corporation":false,"usgs":true,"family":"Albee","given":"Arden","email":"","middleInitial":"Leroy","affiliations":[],"preferred":false,"id":166098,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":934,"text":"wsp1809J - 1965 - Water-resources reconnaissance of the Ouachita Mountains, Arkansas","interactions":[],"lastModifiedDate":"2012-02-02T00:05:16","indexId":"wsp1809J","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","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":"1809","chapter":"J","title":"Water-resources reconnaissance of the Ouachita Mountains, Arkansas","docAbstract":"The Jenkins-Whitesburg area includes approximately 250 square miles in Letcher and Pike Counties in the southeastern part of the Eastern Coal Field. In this area ground water is the principal source of water for nearly all rural families, most public supplies, several coal mines and coal processing plants, and one bottling plant. \r\n\r\nThe major aquifers in the Jenkins-Whitesburg area are the Breathitt and Lee Formations of Pennsylvanian age. Other aquifers range in age from Devonian to Quaternary but are not important in this area because they occur at great depth or yield little or no water. The Breathitt Formation occurs throughout the area except along the crest and slopes of Pine Mountain and where it is covered by unconsolidated material of Quaternary age. The Breathitt Formation consists of shale, sandstone, and lesser amounts of coal and associated underclay. The yield of wells penetrating the Breathitt Formation ranges from less than 1 to 330 gallons per minute. Well yield is controlled by the type and depth of well, character of the aquifer, and topography of the well site. Generally, deep wells drilled in valleys of perennial streams offer the best potential for high yields. Although enough water for a minimum domestic supply (more than 100 gallons per day) may be obtained from shale, all high-yielding wells probably obtain water from vertical joints and from bedding planes which are best developed in sandstone. About 13 percent of the wells inventoried in the Breathitt Formation failed to supply enough water for a minimum domestic supply. Most of these are shallow dug wells or drilled wells on hillsides or hilltops. Abandoned coal mines are utilized as large infiltration galleries and furnish part of the water for several public supplies. \r\n\r\nThe chemical quality of water from the Breathitt Formation varies considerably from place to place, but the water generally is acceptable for most domestic and industrial uses. Most water is a calcium magnesium bicarbonate or sodium bicarbonate type, and nearly all sampled water contained enough iron to stain cooking and laundry utensils. The water ranged from soft to very hard, and only one well in the Breathitt Formation produced salty water. The absence of salty water may be due to abundant fractures which are associated with the Pine Mountain fault and which have allowed fresh water to enter the formation. The Lee Formation underlies the Cumberland Mountain section and is exposed along the crest and southeast slope of Pine Mountain. The Lee Formation consists of massive sandstone and conglomerate with thin beds of shale and a few thin coal seams.\r\n\r\nAlthough the Lee Formation is tapped by only a few wells in this area, it is potentially an important aquifer. Wells penetrating the Lee Formation in the Cumberland Mountain section would probably yield water under artesian pressure. \r\n\r\nUnlike most water from the Lee Formation in other parts of eastern Kentucky, all water from the Lee Formation in the Jenkins-Whitesburg area is fresh. All water from the Lee Formation contained more than 0.3 parts per million of iron and ranged from soft to moderately hard.","language":"ENGLISH","publisher":"United States. Government Printing Office,","doi":"10.3133/wsp1809J","usgsCitation":"Albin, D.R., 1965, Water-resources reconnaissance of the Ouachita Mountains, Arkansas: U.S. Geological Survey Water Supply Paper 1809, iii, 14 p. :maps (part fold., in pocket) ;24 cm., https://doi.org/10.3133/wsp1809J.","productDescription":"iii, 14 p. :maps (part fold., in pocket) ;24 cm.","costCenters":[],"links":[{"id":137015,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1809j/report-thumb.jpg"},{"id":25407,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1809j/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25408,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1809j/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a7ee4b07f02db6485a0","contributors":{"authors":[{"text":"Albin, Donald R.","contributorId":67486,"corporation":false,"usgs":true,"family":"Albin","given":"Donald","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":142880,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":14873,"text":"ofr65103 - 1965 - Density comparison method for the measurement of isotopic variations in prepared waters","interactions":[],"lastModifiedDate":"2024-03-27T17:36:53.195215","indexId":"ofr65103","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","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":"65-103","title":"Density comparison method for the measurement of isotopic variations in prepared waters","docAbstract":"The falling-drop method of density determination has been modified so that the densities of a standard and a sample water are compared simultaneously. A constant temperature bath that does not vary more than 0.0001°C and an accurate double micropipet are described. The method has sufficient sensitivity and precision to distinguish waters that differ in specific gravity by 0.025 micrograms per ml. The method could be applied to the measurement of small variations in the isotopic composition of prepared waters.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr65103","usgsCitation":"McCarthy, J.H., Lovering, T.S., and Lakin, H.W., 1965, Density comparison method for the measurement of isotopic variations in prepared waters: U.S. Geological Survey Open-File Report 65-103, 38 p., https://doi.org/10.3133/ofr65103.","productDescription":"38 p.","costCenters":[],"links":[{"id":427152,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1965/0103/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":147121,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1965/0103/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ab2e4b07f02db66eb93","contributors":{"authors":[{"text":"McCarthy, Joseph Howard Jr.","contributorId":46819,"corporation":false,"usgs":true,"family":"McCarthy","given":"Joseph","suffix":"Jr.","email":"","middleInitial":"Howard","affiliations":[],"preferred":false,"id":170162,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lovering, Thomas Seward","contributorId":17227,"corporation":false,"usgs":true,"family":"Lovering","given":"Thomas","email":"","middleInitial":"Seward","affiliations":[],"preferred":false,"id":170160,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Lakin, Herbert Williams","contributorId":45953,"corporation":false,"usgs":true,"family":"Lakin","given":"Herbert","email":"","middleInitial":"Williams","affiliations":[],"preferred":false,"id":170161,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":15753,"text":"ofr65141 - 1965 - Geology of the Romanzof Mountains, Brooks Range, northeastern Alaska","interactions":[{"subject":{"id":15753,"text":"ofr65141 - 1965 - Geology of the Romanzof Mountains, Brooks Range, northeastern Alaska","indexId":"ofr65141","publicationYear":"1965","noYear":false,"title":"Geology of the Romanzof Mountains, Brooks Range, northeastern Alaska"},"predicate":"SUPERSEDED_BY","object":{"id":6313,"text":"pp897 - 1977 - Geology of the western Romanzof Mountains, Brooks Range, northeastern Alaska","indexId":"pp897","publicationYear":"1977","noYear":false,"title":"Geology of the western Romanzof Mountains, Brooks Range, northeastern Alaska"},"id":1},{"subject":{"id":15754,"text":"ofr59106 - 1959 - Preliminary report on sedimentary and metamorphic rocks in part of the Romanzof Mountains, Brooks Range, northeastern Alaska","indexId":"ofr59106","publicationYear":"1959","noYear":false,"title":"Preliminary report on sedimentary and metamorphic rocks in part of the Romanzof Mountains, Brooks Range, northeastern Alaska"},"predicate":"SUPERSEDED_BY","object":{"id":15753,"text":"ofr65141 - 1965 - Geology of the Romanzof Mountains, Brooks Range, northeastern Alaska","indexId":"ofr65141","publicationYear":"1965","noYear":false,"title":"Geology of the Romanzof Mountains, Brooks Range, northeastern Alaska"},"id":2}],"supersededBy":{"id":6313,"text":"pp897 - 1977 - Geology of the western Romanzof Mountains, Brooks Range, northeastern Alaska","indexId":"pp897","publicationYear":"1977","noYear":false,"title":"Geology of the western Romanzof Mountains, Brooks Range, northeastern Alaska"},"lastModifiedDate":"2024-03-25T18:59:14.568941","indexId":"ofr65141","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","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":"65-141","title":"Geology of the Romanzof Mountains, Brooks Range, northeastern Alaska","docAbstract":"This remote 700 square mile area in the Brooks Range is topographically rugged and geologically diverse; it contains a granitic pluton, low-grade metamorphic rocks, sedimentary rocks, and mafic igneous rocks, as well as glacial features.
Rocks of sedimentary origin include from oldest to youngest:
1.Neruokpuk Formation Middle and Upper Devonian(?), more than 4000 feet thick, a variety of units which represent the greenschist facies, including quartzitic- and schistose-feldspathic graywacke; phyllite, argillite, and slate, as well as dark limestone, sandy limestone, and silicified carbonate rocks. The succession of units in parts of the area is uncertain. Correlations between these units and with others in the eastern Brooks Range are provisional.
2.Kekiktuk Conglomerate and Kayak(?) Shale (Upper Devonian(?) to Upper Mississippian), a single map unit, from absent(?) to 400+ feet thick, containing dark shale Kayak(?) in its uppermost part and quartzite, interbedded dark shale, and some pebble- to boulder-conglomerate in the locally absent lower part (Kekiktuk). The unit overlies the Neruokpuk with angular unconformity, which may reflect either a pre-Kayak(?) or pre-Kekiktuk hiatus or both.
3.Lisburne Group, almost entirely carbonate rocks, and relatively thin in this area, 600 to 800 feet thick. Alapah Limestone (Upper Mississippian), to 560 feet thick, includes gray sandy, crystalline, and cherty limestone; minor dark shale; and dark cherty carbonate rocks in the upper part. The lower contact is gradational with the Kayak(?). Wahoo(?) Limestone (Pennsylvanian(?) to Permian) conformably overlies the Alapah, is absent to 200+ feet thick, and is characterized by light-gray crinoidal limestones in its upper part.
4. Sadlerochit Formation, consisting of three intraconformable units: ferruginous sandstone member (Permian) of ironstained orthoquartzite and dark slate, 175 to 240 feet thick which unconformably overlies the Wahoo(?) and Alapah Limestones; shale member of dark shale, slate, and minor quartzite averaging 400 feet in thickness; and quartzite member (Lower(?) Triassic), 700 feet thick, mostly orthoquartzite with minor shale and conglomerate. The basal clastics were probably shed from the north.
5.Shublik Formation (Middle(?) and Upper Triassic), 600 to 700 feet thick, with the thin phosphatic sandstone member overlain by dark phosphatic limestones and limy shales of the limestone member.
6.Kingak Formation (Jurassic), more than 1000 feet thick. The siltstone member, resistant sandstone and siltstone 75 to 150 feet thick, is overlain by an undetermined thickness of black shale. The basal part contrasts sharply with the underlying Shublik, indicating possible disconformity.
7.Ignek(?) Formation (Cretaceous), represented in the foothills where lithic graywacke, shale, and coaly shale constitute the few exposures examined.
8.Glacial and glaciofluvial materials of five advances recognized on the basis of morphology and position, which are tentatively correlated with five glaciations 15 miles west of the area.
9. Recent alluvial and colluvial deposits including fans which appear to represent at least three stages of encroachment.
The Ramanzof granite, exposed in the Okpilak batholith and Jago stock, is mostly light-gray quartz monzonite to granite, and contains essential quartz, perthitic microcline, albite-oligoclase, and partly chloritized biotite. Limited modal and chemical data are presented. Three textural facies are: 1) porphyritic (marginal), with abundant large microcline megacrysts; 2) variable (middle to marginal), which exhibits textural and mineralogical banding; and 3) coarse (inner to marginal), which is gneissoid to equigranular. Facies relationships appear to be mostly gradational but may be locally intrusive. Some schistose metasedimentary(?) rock occurs in the granite. Aplite dikes, inclusions, tourmaline veins and replacements, and chlorite and quartz veins are locally common, as well as quartz monzonite and mafic igneous dikes. Contacts with Neruokpuk Formation rocks are mostly abrupt, concordant to cross-cutting, and locally adjoin tactite and hornfels of the albite-epidote-hornfels and hornblende-hornfels facies. Contacts with Kekiktuk Conglomerate are apparently gradational through a schistoze zone. Both primary and secondary structural elements are present in the Romanzof in granite. Textural and mineralogical banding and, in general, feldspar foliation are considered to be primary in origin; biotite foliation, gneissic and schistose foliation, and schistose zones are considered secondary. Lead-alpha age of zircons appears to be Late Devonian, K-Ar age of biotite is Cretaceous, possibly indicating updating by later reheating. Field age relationships are inconclusive but suggest pre-Kayak(?) (Upper Devonian) granite emplacement. The pluton is interpreted to be essentially the product of melt crystallization, synorogenically emplaced by forceful injection with minor stoping, and may include marginally granitized rock.
Mafic igneous rocks of altered basaltic composition (greenstones) include dikes in granitic and Neruokpuk Formation rocks, and volcanics(?). A late Paleozoic age is suggested for them.
Structural grain strikes east-northeast; south-dipping elements are common. Structures include the major positive nature of the area (first order), relatively broad folds (second order) which contain small tight folds (third order). Related south-dipping cleavage, schistosity, and biotite foliation in granite in the northern part of the area are cut by prominent sets of transverse joints and faults. Other features are longitudinal normal and reverse faults, at least one large-scale overthrust fault, and sheared zones in granite with possible attendant retrograde metamorphism.
Although Mesozoic and Tertiary deformational features are dominant in northern Alaska, the Romanzof area may have been part of a Late Devonian orogenic belt continuous with one in northern Canada. Three alternate trends of such a belt in northern Alaska are discussed, but evidence is inconclusive.
The mineral potential of the area is largely unknown. Minor amounts of metallic sulfides and oxides are present in granite and Neruokpuk Formation rocks. Analyses of stream silt samples suggest the possibility of tin and beryllium potential. The Shublik Formation contains rock phosphate.
Within the Mesabi-Vermilion Iron Range area, water of good quality is available from the Biwabik Iron-Formation, from stratified drift, and from lakes and streams. About 700 bgy (billion gallons a year) leaves the area as surface water, of which about one-third comes from ground water.
\nLeached, oxidized, and fractured parts of the Biwabik Iron-Formation yield as much as 1,000 gpm (gallons per minute) to wells. Much of the permeable stratified drift within the area underlies the Ice-Contact region and the Horainal and Ice-Contact region, and several wells drilled in drift have been pumped at rates of more than 1,000 gpm.
\nParts of three major drainage basins lie within the area, and lakes compose about 5 percent of the area. Low-flow and flood-frequency data have been compiled for many of the streams. Large quantities of surface water are available from the Border-Lakes region and the Morainal and Ice-Contact region.
\nThe quality of ground water from the Biwabik Iron-Formation and from the drift is similar. The water is generally moderately siliceous, hard or very hard, and contains much iron and manganese. Surface water is generally soft, contains much iron, and is highly colored.
\nLarge uses of water in the area include: taconite processing (50 bgy), wash-ore processing (19 bgy), power plants (63 bgy), municipal water supplies (3 bgy) and paper processing (1 bgy). Optimum development of the water resources might be achieved by using streamflow in the spring and stunner and ground-water and surface-water storage in the fall and winter.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, DC","doi":"10.3133/wsp1759A","collaboration":"Prepared in cooperation with the Minnesota Department of Iron Range Resources and Rehabilitation","usgsCitation":"Cotter, R.D., Young, H.L., Petri, L.R., and Prior, C.H., 1965, Ground and surface water in the Mesabi and Vermilion Iron Range area, northeastern Minnesota: U.S. Geological Survey Water Supply Paper 1759, Document: iv, 35 p.; 1 Plate: 23.00 x 17.00 inches, https://doi.org/10.3133/wsp1759A.","productDescription":"Document: iv, 35 p.; 1 Plate: 23.00 x 17.00 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science Center","active":true,"usgs":true}],"links":[{"id":400746,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24933.htm"},{"id":26060,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1759a/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26059,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1759a/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137940,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1759a/report-thumb.jpg"}],"scale":"303000","country":"United States","state":"Minnesota","otherGeospatial":"Mesabi and Vermilion Iron Range area","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -93.75,\n 48\n ],\n [\n -93.75,\n 47.089\n ],\n [\n -91.582,\n 47.089\n ],\n [\n -91.582,\n 48\n ],\n [\n -93.75,\n 48\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ab1e4b07f02db66eaed","contributors":{"authors":[{"text":"Cotter, R. D.","contributorId":89874,"corporation":false,"usgs":true,"family":"Cotter","given":"R.","email":"","middleInitial":"D.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":143330,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Young, H. L.","contributorId":23922,"corporation":false,"usgs":true,"family":"Young","given":"H.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":143327,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Petri, L. R.","contributorId":48944,"corporation":false,"usgs":true,"family":"Petri","given":"L.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":143328,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Prior, C. H.","contributorId":57827,"corporation":false,"usgs":true,"family":"Prior","given":"C.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":143329,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":6390,"text":"pp506A - 1965 - Use of analog models in the analysis of flood runoff","interactions":[],"lastModifiedDate":"2012-02-02T00:05:42","indexId":"pp506A","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","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":"506","chapter":"A","title":"Use of analog models in the analysis of flood runoff","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/pp506A","usgsCitation":"Shen, J., 1965, Use of analog models in the analysis of flood runoff: U.S. Geological Survey Professional Paper 506, p. A1-A24, https://doi.org/10.3133/pp506A.","productDescription":"p. A1-A24","costCenters":[],"links":[{"id":117613,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0506a/report-thumb.jpg"},{"id":33765,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0506a/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a18e4b07f02db604d81","contributors":{"authors":[{"text":"Shen, John","contributorId":34109,"corporation":false,"usgs":true,"family":"Shen","given":"John","email":"","affiliations":[],"preferred":false,"id":152634,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2626,"text":"wsp1810 - 1965 - Summary of floods in the United States during 1961","interactions":[],"lastModifiedDate":"2017-09-06T16:28:04","indexId":"wsp1810","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","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":"1810","title":"Summary of floods in the United States during 1961","docAbstract":"This report describes the most outstanding floods in the United States during 1961. The most damaging floods during the year were those caused by snowmelt in March and April in the upper Mississippi River basin and those accompanying Hurricane Carla in September.
Hurricane Carla traveled northward along the east edge of Texas and then northeastward through southeastern Oklahoma, northwestern Arkansas, southeastern Missouri, and central Illinois. Heavy rains and floods occurred east of the hurricane's path in Texas and west of its path for the remainder of its journey.
Mississippi, Alabama, and Georgia had moderate to severe floods in February and March from a series of large-area rainstorms. Many maximum peak discharges occurred, and streams remained at high stages for periods longer than any known before. Property damage was high and four lives were lost.
Extensive flooding took place in May from southeastern Kansas and northeastern Oklahoma through northern Arkansas, southern Missouri, northern Kentucky, and the southern parts of Illinois, Indiana, and Ohio. Maximum discharges occurred at many sites throughout the area.
Heavy flooding was experienced on Kootenai River at Bonners Ferry, Idaho, in May and June. These floods were noteworthy for their duration.
The most tragic flood of the year was in July in Charleston, W. Va. A small area cloudburst flood caused 22 deaths and damage of more than \\$1 million.
Severe flooding occurred in December in the Tombigbee River, Pearl River, and Pascagoula River basins in Mississippi, Louisiana, and Alabama. Much damage resulted, and from two to three thousand persons were evacuated from large flooded areas.
In addition to the floods mentioned above, 19 others of lesser magnitude are considered important enough to be included in this annual summary.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1810","collaboration":"Prepared in cooperation with Federal, State, and local agencies","usgsCitation":"Rostvedt, J., 1965, Summary of floods in the United States during 1961: U.S. Geological Survey Water Supply Paper 1810, vi, 123 p., https://doi.org/10.3133/wsp1810.","productDescription":"vi, 123 p.","numberOfPages":"128","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":28943,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1810/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138160,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1810/report-thumb.jpg"}],"country":"United States","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b04e4b07f02db699281","contributors":{"authors":[{"text":"Rostvedt, J.O.","contributorId":24757,"corporation":false,"usgs":true,"family":"Rostvedt","given":"J.O.","email":"","affiliations":[],"preferred":false,"id":145524,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2342,"text":"wsp1794 - 1965 - Ground-water resources of Pavant Valley, Utah","interactions":[],"lastModifiedDate":"2017-09-06T16:23:09","indexId":"wsp1794","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","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":"1794","title":"Ground-water resources of Pavant Valley, Utah","docAbstract":"Pavant Valley, in eastern Millard County in west-central Utah, is in the Great Basin section of the Basin and Range province. The area of investigation is 34 miles long from north to south and 9 miles wide from east to west and comprises about 300 square miles. Agriculture, tourist trade, and mining are the principal industries. The population of the valley is about 3,500, of which about half live in Fillmore, the county seat of Millard County.
The climate is semiarid and temperatures are moderate. Average normal annual precipitation in the lowlands is estimated to range from 10 to 14 inches. Precipitation is heaviest during the late winter and spring, January through May. The average monthly temperature at Fillmore ranges from 29°F in January to 76°F in July; the average annual temperature is 52°F.
Because of the aridity, most crops cannot be grown successfully without irrigation. Irrigation requirements were satisfied for about 60 years after the valley was settled by diverting streams tributary to the valley. Artesian water was discovered near Flowell in 1915. By 1920 flowing artesian wells supplied about 10 percent of the irrigation water used in the valley, not including water from the Central Utah Canal. The Central Utah Canal was constructed in 1916 to convey water to the Pavant Valley from the Sevier River. Especially since 1916, the quantity of surface water available each year for irrigation has changed with the vagaries of nature. The total percentage of irrigation water contributed by ground water, on the other hand, gradually increased to about 15 percent in 1945 and then increased rapidly to 45 percent in 1960; it will probably stabilize at about 50 percent.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1794","collaboration":"Prepared in cooperation with the Utah State Engineer","usgsCitation":"Mower, R.W., 1965, Ground-water resources of Pavant Valley, Utah: U.S. Geological Survey Water Supply Paper 1794, Report: v, 78 p.; 10 Plates: 36.50 x 39.00 or smaller, https://doi.org/10.3133/wsp1794.","productDescription":"Report: v, 78 p.; 10 Plates: 36.50 x 39.00 or smaller","numberOfPages":"93","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":28251,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1794/plate-06.pdf","text":"Plate 6","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map showing decline of ground-water level from March 1959 to March 1960 in Pavant Valley, Utah"},{"id":28246,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1794/plate-01.pdf","text":"Plate 1","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map of Pavant Valley, Utah, showing location of selected wells and hydrogeochemical data"},{"id":28252,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1794/plate-07.pdf","text":"Plate 7","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Hydrographs of selected observation wells in Pavant Valley, Utah, 1929-62"},{"id":28253,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1794/plate-08.pdf","text":"Plate 8","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map showing decline of ground-water level from March 1950 to March 1960 in Pavant Valley, Utah"},{"id":28254,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1794/plate-09.pdf","text":"Plate 9","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map showing areas of artesian flow and phreatophyte occupation during 1960 in Pavant Valley, Utah"},{"id":28255,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1794/plate-10.pdf","text":"Plate 10","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map showing land irrigated during 1960 in Pavant Valley, Utah"},{"id":28256,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1794/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138338,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1794/report-thumb.jpg"},{"id":28247,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1794/plate-02.pdf","text":"Plate 2","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Generalized geologic map of Pavant Valley, Utah"},{"id":28248,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1794/plate-03.pdf","text":"Plate 3","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Strip logs from drillers' logs of wells in Pavant Valley, Utah"},{"id":28249,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1794/plate-04.pdf","text":"Plate 4","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map of Pavant Valley, Utah, showing ground-water contours, March 1960"},{"id":28250,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1794/plate-05.pdf","text":"Plate 5","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map showing decline of ground-water level from March to September 1960 in Pavant Valley, Utah"}],"country":"United States","state":"Utah","county":"Millard County","otherGeospatial":"Pavant Valley","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a94e4b07f02db659403","contributors":{"authors":[{"text":"Mower, R. W.","contributorId":34898,"corporation":false,"usgs":true,"family":"Mower","given":"R.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":145050,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2771,"text":"wsp1809B - 1965 - Geology and ground-water resources of Waushara County, Wisconsin","interactions":[],"lastModifiedDate":"2015-10-02T13:14:56","indexId":"wsp1809B","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","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":"1809","chapter":"B","title":"Geology and ground-water resources of Waushara County, Wisconsin","docAbstract":"Abundant ground water for irrigation is available in the outwash deposits in western Waushara County, and many more large-capacity wells can be developed in these deposits without seriously lowering the water level. Pumping for irrigation temporarily lowers water levels in the vicinity of the wells but has not lowered regional water levels. Pumpage has probably intercepted and utilized some of the recharge that would have been rapidly discharged from the aquifer. Ground water is continuously being discharged to streams and to the atmosphere by evapotranspiration, but intermittent recharge from precipitation replaces the discharged water. Recharge and discharge are in approximate balance, maintaining about the same amount of ground water in storage. Further recharge to the aquifer is rapidly discharged to streams. The sandstones, till, and glaciolacustrine deposits in Waushara County generally yield small to moderate amounts of water to wells but do not produce enough water for irrigation ; recent alluvium may yield large quantities of water to wells. In general, the ground water is of good quality, except for hardness and local high-iron concentrations.
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Contributions to the hydrology of the United States, 1962","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1809B","collaboration":"Prepared in cooperation with the University of Wisconsin Geological and Natural History Survey","usgsCitation":"Summers, W.K., 1965, Geology and ground-water resources of Waushara County, Wisconsin: U.S. Geological Survey Water Supply Paper 1809, Report: iv, 32 p.; 3 Plates: 41.96 x 22.00 inches and 39.5 x 22.5 inches, https://doi.org/10.3133/wsp1809B.","productDescription":"Report: iv, 32 p.; 3 Plates: 41.96 x 22.00 inches and 39.5 x 22.5 inches","numberOfPages":"40","onlineOnly":"Y","additionalOnlineFiles":"Y","costCenters":[{"id":677,"text":"Wisconsin Water Science Center","active":true,"usgs":true}],"links":[{"id":29216,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1809b/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29217,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1809b/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29218,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1809b/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29219,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1809b/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138609,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1809b/report-thumb.jpg"}],"country":"United States","state":"Wisconsin","county":"Waushara County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-89.5977,44.2458],[-89.488,44.244],[-89.4835,44.244],[-89.3649,44.2439],[-89.3464,44.2439],[-89.2469,44.2438],[-89.2245,44.2433],[-89.1288,44.243],[-89.104,44.243],[-89.007,44.2426],[-88.9821,44.243],[-88.8871,44.2426],[-88.8859,44.1587],[-88.8882,44.1136],[-88.8861,44.0713],[-88.8862,43.9833],[-88.944,43.9836],[-89.0063,43.9834],[-89.1283,43.9833],[-89.1658,43.983],[-89.2472,43.9827],[-89.3654,43.9824],[-89.4823,43.982],[-89.598,43.9824],[-89.5981,44.0685],[-89.5976,44.156],[-89.5977,44.2458]]]},\"properties\":{\"name\":\"Waushara\",\"state\":\"WI\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db685374","contributors":{"authors":[{"text":"Summers, William Kelly","contributorId":69532,"corporation":false,"usgs":true,"family":"Summers","given":"William","email":"","middleInitial":"Kelly","affiliations":[],"preferred":false,"id":145756,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1062,"text":"wsp1790A - 1965 - Floods of March-April 1960 in Eastern Nebraska and adjacent states","interactions":[],"lastModifiedDate":"2012-02-02T00:05:17","indexId":"wsp1790A","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","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":"1790","chapter":"A","title":"Floods of March-April 1960 in Eastern Nebraska and adjacent states","docAbstract":"Snowmelt floods, record breaking on many streams and outstanding in terms of total area affected and runoff volumes generated, occurred in late March and early April 1960 on Missouri River tributaries in adjacent parts of six states. In order of area affected, the States are Nebraska, South Dakota, Iowa, Kansas, Minnesota, and Missouri. \r\n\r\nFive lives were lost, and the estimated damage was $14 million. Main-stem reservoirs kept Missouri River stages substantially below potential unregulated levels. Without regulation by reservoirs, the stage at Sioux City and Omaha would have been about 9 feet higher than it was and the damage would have been many millions of dollars more than actually occurred. \r\n\r\nThe floods were caused by rapid melting of an extensive snow cover of unusual depth and water equivalent, augmented by light to moderate rains. Temperatures almost continuously below normal, beginning in late December and culminating in record lows at many places during the first half of March, resulted in the retention of record snow accumulations, much later and much farther south than normal. The snowfall in eastern Nebraska from December 27 to March 26 was about twice the annual average. The excessive snowfall and below-normal temperatures produced a record-breaking 75-day period of continuous snow cover at Omaha. \r\n\r\nA rapidly rising, eastward-moving temperature pattern late in March, in combination with an easterly orientation of many Nebraska streams, tended to magnify flood peaks. The rapid temperature rise started about March 18 in western Nebraska but not until March 26 in the eastern part of the State. As a consequence, flood discharges from the headwaters, often bearing heavy ice floes, arrived in the lower reaches simultaneously with or even ahead of the breakup of the unusually heavy ice cover and caused serious jamming. Comparisons of the peak discharges of the 1960 snowmelt floods with those of previous floods reveal several interesting facts. Peak discharges on the Missouri main stem were appreciably less than those in several other years, largely because of effective reservoir control of upstream runoff, but, many tributaries throughout the report area had maximum discharges for their periods of record. Particularly significant are comparisons at some stations for which historical flood data were available. For example, the peak discharge of the Platte River at Louisville, Nebr., was the greatest since at least 1881, and the peak on the Elkhorn River at Waterloo, Nebr., was the greatest snowmelt flood since at least 1912, although it was less than half of the rain peak of June 12, 1944. \r\n\r\nFollowing a characteristic pattern for snowmelt floods, the peaks on the smaller streams generally were not unusual, but the cumulative effect of widespread high runoff throughout the stream systems caused higher and more outstanding peaks in the larger basins. Peaks due to local rains of high intensity often are more significant for small areas. \r\n\r\nSnowmelt floods occur less frequently than rainfall floods in most basins of this flood area.. Studies made for this report show that an average of only about one out of every four maximum annual flood discharges in the report area results primarily from snowmelt. But for streams flowing from north to south in South Dakota and Iowa, the ratio of snowmelt peaks to rainfall peaks is higher. \r\n\r\nComparisons of 1960 flood volumes with those for previous floods are even more striking than peak-discharge comparisons. Flood volumes at eight selected stations for the maximum 20-day period during March and April 1960 exceeded all previous 20-day volumes with only one exception; the ratios ranged from 3.11 for Vermillion River near Wakonda, S. Dak., to 0.93 for Elkhorn River at Waterloo, Nebr. The ratio of the 20-day volume to the 1960 annual runoff for the same group of stations ranged from 20 percent at Niobrara River near Spencer, Nebr., to 74 percent on the Vermillion River. For the lat","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, Geological Survey ;","doi":"10.3133/wsp1790A","usgsCitation":"Brice, H., and West, R., 1965, Floods of March-April 1960 in Eastern Nebraska and adjacent states: U.S. Geological Survey Water Supply Paper 1790, v, 144 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1790A.","productDescription":"v, 144 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":138100,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1790a/report-thumb.jpg"},{"id":25740,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1790a/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25741,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1790a/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49d9e4b07f02db5df9c2","contributors":{"authors":[{"text":"Brice, H.D.","contributorId":41406,"corporation":false,"usgs":true,"family":"Brice","given":"H.D.","email":"","affiliations":[],"preferred":false,"id":143112,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"West, R.E.","contributorId":27031,"corporation":false,"usgs":true,"family":"West","given":"R.E.","email":"","affiliations":[],"preferred":false,"id":143111,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":52503,"text":"ofr65151 - 1965 - Water resources appraisal of the Anchorage area, Alaska","interactions":[],"lastModifiedDate":"2023-10-20T20:27:13.82275","indexId":"ofr65151","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","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":"65-151","title":"Water resources appraisal of the Anchorage area, Alaska","docAbstract":"At the present, water use in the Anchorage area amounts to about 21 mgd (million gallons per day); of this amount ground water accounts for about 10 mgd. By 1980, 60 mgd may be required to meet the demand.
The greatest potential problem is overpumping the ground-water reservoir resulting in excessive declines in water levels, which, in turn, might lead to salt-water intrusion. A well-laid plan for conjunctive use of surface and ground water seems to be the most promising means of supplying the expected need of 60 mgd, and of preventing saltwater intrusion of the aquifers.
Total inflow into the Anchorage hydrologic system amounts to about 180 mgd. Of this amount Ship and South Fork Campbell Creeks contribute about 130 mgd, North Fork Campbell Creek and other streams contribute an estimated 24 mgd, and precipitation and ground-water inflow contribute an estimated 26 mgd.
Of the total outflow, which must be equivalent to the inflow, Ship and Chester Creeks contribute about 94 mgd, Campbell Creek about 25 mgd, and ground-water pumpage contributes an assumed amount of approximately 10 mgd. The difference of 50 mgd between inflow and outflow presumably is accounted for; by submarine discharge beneath Cook Inlet and evapotranspiration.
Surface and subsurface storage of excess stream discharge during periods of high flow can overcome the problem of water shortages during periods of greatest demand. Surface storage can be accomplished by construction of an additional dam on Ship Creek. Natural ground-water storage can be supplemented by spreading techniques to increase the amount of ground-water recharge. Additional recharge can be provided by returning air-conditioning water to the aquifer through recharge wells. Recharge along the coastline would be a means of maintaining a fresh-water barrier against salt-water intrusion.
The area with the greatest potential for ground-water development is along Ship Creek east and north of Mountain View. The alluvial fan east of Mountain View seems favorable for installation of deep wells; and withdrawal of ground water in this area is not likely to result in salt-water intrusion. Similar favorable conditions exist in the alluvial fan areas of North and South Forks Campbell Creek. Infiltration galleries in alluvial deposits along Ship Creek are a relatively inexpensive and convenient means of withdrawing water.
To plan for orderly and economical development of the Anchorage area's water resources, geologic and hydrologic studies are needed. An expanded network of stream-gaging stations and observation wells is needed. Deep wells near the coastline are needed to monitor any changes in chemical quality of ground water that would indicate impending salt-water intrusion. Borehole geophysical studies and pumping tests are needed to define the boundaries and hydraulic characteristics of the aquifers. The primary goal of these and other supplementing studies would be to provide the information needed to construct an electric-analog model of the Anchorage hydrologic system. Such a model would provide a means of assessing quantitatively alternative methods of water development.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr65151","usgsCitation":"Sommers, D.A., and Marcher, M.V., 1965, Water resources appraisal of the Anchorage area, Alaska: U.S. Geological Survey Open-File Report 65-151, 34 p., https://doi.org/10.3133/ofr65151.","productDescription":"34 p.","costCenters":[],"links":[{"id":422019,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1965/0151/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":177656,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1965/0151/report-thumb.jpg"}],"country":"United States","state":"Alaska","city":"Anchorage","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -150.0148756092472,\n 61.267767521656054\n ],\n [\n -150.0148756092472,\n 61.119542274353336\n ],\n [\n -149.69627209362233,\n 61.119542274353336\n ],\n [\n -149.69627209362233,\n 61.267767521656054\n ],\n [\n -150.0148756092472,\n 61.267767521656054\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a03e4b07f02db5f8302","contributors":{"authors":[{"text":"Sommers, David A.","contributorId":96761,"corporation":false,"usgs":true,"family":"Sommers","given":"David","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":245455,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Marcher, Melvin V.","contributorId":11590,"corporation":false,"usgs":true,"family":"Marcher","given":"Melvin","email":"","middleInitial":"V.","affiliations":[],"preferred":false,"id":245454,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":52470,"text":"ofr6568 - 1965 - Description and analysis of the geohydrologic system in western Pinal County, Arizona","interactions":[],"lastModifiedDate":"2012-02-02T00:11:23","indexId":"ofr6568","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","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":"65-68","title":"Description and analysis of the geohydrologic system in western Pinal County, Arizona","docAbstract":"Western Pinal County is between Phoenix and Tucson in the Basin and Range physiographic province of southern Arizona and consists of about 2,000 square miles of valley floor with low relief surrounded by mountains. It is the second largest agricultural area in the State, and about 25 percent of the ground water pumped in the State is from this area. \r\n\r\nThe study area has been divided into four parts. Three of these--the Casa Grande-Florence area, the Eloy area, and the Stanfield-Maricopa area--are in the lower Santa Cruz basin; the fourth--the Gila River area--is a long narrow strip along the Gila River from the Ashurst-Hayden Dam to the confluence of the Gila and Santa Cruz Rivers. The project was undertaken to provide a better understanding of the ground-water supply in relation to the present and potential water use in this area of extensive ground-water development. The arid climate of western Pinal County--combining high temperatures and low humidity--causes most of the precipitation to be returned to the atmosphere by evapotranspiration, which leaves only a very small part for recharge to the ground-water reservoir. The computed potential evapotranspiration--44. 97 inches--is five times greater than the average precipitation. \r\n\r\nIn general, the subsurface materials in western Pinal County are unconsolidated alluvial deposits underlain by consolidated alluvium and crystalline rocks and bounded by mountains consisting of crystalline and minor sedimentary rocks. The crystalline and sedimentary rocks of the mountains are not known to be water bearing in western Pinal County. The impermeable rocks underlying the basin are called the hydrologic bedrock unit in this report. Although the unit may consist of several different rock types, the distinction between them is relatively unimportant in this study because none of them yield appreciable amounts of water. The lower Santa Cruz basin in western Pinal County is divided into two sections by a buried ridge of the hydrologic bedrock unit, referred to in this report as the Casa Grande ridge. The ridge trends in a north-south direction from the Sacaton to the Silver Reef Mountains. \r\n\r\nThe unconsolidated deposits constitute the main storage reservoir for ground water in western Pins/ County. The deposits are divided into four units---the local gravel unit, the lower sand and gravel unit, the silt and clay unit, and the upper sand and gravel unit--all of which are major water-yielding units except the silt and clay unit. The local gravel unit, which is present only in the western section of the lower Santa Cruz basin, ranges in thickness from 0 to nearly 1,000 feet and is generally a productive aquifer. The lower sand and gravel unit, Which is a heterogeneous mixture of sand, gravel, and clay, ranges in thickness from 0 to about 500 feet. Where the lower sand and gravel unit is overlain by the silt and clay unit, it generally contains water under artesian conditions; where it is not overlain by the silt and clay unit, it is indistinguishable from the upper sand and gravel unit, and the water is under water-table conditions. The silt and clay unit is the least permeable deposit of the unconsolidated alluvium, and ranges in thickness from 0 to about 2, 000 feet. Generally it is less productive than the other units of the unconsolidated alluvium, although it yields moderate amounts of water from numerous thin stringers and lenses of highly permeable sand and gravel. The upper sand and gravel unit is at the land surface in most of the area; it ranges in thickness from less than 50 to about 600 feet. The unit has the highest average permeability of all the unconsolidated alluvial units; however, the permeability of the unit varies vertically and laterally, which results in a wide range of well yields. As of 1964, the static water levels in most wells in the basin were still in the upper sand and gravel unit. 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F.","contributorId":12455,"corporation":false,"usgs":true,"family":"Hardt","given":"W.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":245394,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Cattany, R.E.","contributorId":89967,"corporation":false,"usgs":true,"family":"Cattany","given":"R.E.","email":"","affiliations":[],"preferred":false,"id":245395,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":52501,"text":"ofr65149 - 1965 - Freshwater inflow data for Corps of Engineers model study of Houston, Texas, ship channel","interactions":[],"lastModifiedDate":"2012-02-02T00:11:41","indexId":"ofr65149","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","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":"65-149","title":"Freshwater inflow data for Corps of Engineers model study of Houston, Texas, ship channel","language":"ENGLISH","doi":"10.3133/ofr65149","usgsCitation":"Smith, R.E., and Kaminski, E., 1965, Freshwater inflow data for Corps of Engineers model study of Houston, Texas, ship channel: U.S. Geological Survey Open-File Report 65-149, 19 p., https://doi.org/10.3133/ofr65149.","productDescription":"19 p.","costCenters":[],"links":[{"id":177654,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1ae4b07f02db6a862a","contributors":{"authors":[{"text":"Smith, R. 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Mineralized water underlies large areas of the country, and its importance will grow as present supplies of fresh water are appropriated and developed. The potential uses fall in two main categories: (1) direct use in industrial processes, such as cooling, or for irrigation, where a moderate mineral content may not be a disadvantage; and (2) use after demineralization or dilution to whatever degree may be required by the intended user. It is clearly more efficient to produce and process water of moderate mineralization at points of use, where available in adequate amounts, than it is to process ocean water and pump it many miles from the sea.
\nThe Geological Survey, as a part of its responsibility to describe the water resources of the United States, has surveyed the known occurrences of mineralized ground water in the conterminous United States. The results are shown on the maps (sheets 1 and 2).
\nThis atlas was prepared to meet needs for information on the distribution and availability of mineralized water as expressed by Government agencies, private industries, and consultants. The maps are one step in providing an inventory of mineralized water of the Nation and will serve as a planning guide for further investigations and for development. They are necessarily generalized in many places owing to the complexity of the occurrence of the mineralized water, lack of detailed information for parts of the nation, and the difficulties inherent in attempts to put three-dimensional information on maps.
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\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afce4b07f02db6969e0","contributors":{"authors":[{"text":"Feth, John Henry Frederick","contributorId":37310,"corporation":false,"usgs":true,"family":"Feth","given":"John","email":"","middleInitial":"Henry Frederick","affiliations":[],"preferred":false,"id":278189,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":61616,"text":"gq409 - 1965 - Geology of the Model quadrangle in Kentucky","interactions":[],"lastModifiedDate":"2012-02-10T00:10:51","indexId":"gq409","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":316,"text":"Geologic Quadrangle","code":"GQ","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"409","title":"Geology of the Model quadrangle in Kentucky","language":"ENGLISH","doi":"10.3133/gq409","usgsCitation":"Rogers, W.B., 1965, Geology of the Model quadrangle in Kentucky: U.S. Geological Survey Geologic Quadrangle 409, 1 map :col. ;57 x 47 cm., on sheet 81 x 84 cm., folded in envelope 30 x 24 cm., https://doi.org/10.3133/gq409.","productDescription":"1 map :col. ;57 x 47 cm., on sheet 81 x 84 cm., folded in envelope 30 x 24 cm.","costCenters":[],"links":[{"id":102427,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_876.htm","linkFileType":{"id":5,"text":"html"},"description":"876"},{"id":247922,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/gq/0409/report.pdf","size":"34","linkFileType":{"id":1,"text":"pdf"}},{"id":252347,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/gq/0409/report-thumb.jpg"}],"scale":"24000","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -88,36.6175 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faulting","docAbstract":"The two principal suggested modes of facilitating overthrust faulting are (1) lubrication at the sole by evaporite beds or micaceous shales and (2) flotation due to anomalously high (> hydrostatic) pore-water pressures. Past rapid sedimentation and tectonic compression have been suggested as important causes of anomalously high water pressure (Hubbert and Rubey, 1959). We suggest osmosis as another important possibility. Field data on shale beds and experimental studies on compacted clays show that such material can act as semipermeable membranes that greatly retard passage of dissolved electrolytes relative to H2O. Equilibrium osmotic pressure, π, across an ideal membrane is given by (a, activity; VH2O01, molar volume of distilled water). At 80°C, π is 470 bars between saturated halite solution and distilled water; it is 360 bars between saturated and 10 per cent solutions. At 25°C the values are 20 per cent lower. Other dissolved components, if present in similar proportions, will enhance the effect. Anomalous water pressures of at least 400 bars above hydrostatic have been measured in oil wells; many of these wells penetrate evaporites and/or shales which separate formation waters of differing salt concentrations. These pressures are explicable by assuming osmotic equilibrium across a membrane which separates saturated halite solution from solutions up to 10 weight per cent NaCl. Thus, osmotic equilibrium may be an important mechanism for floating thrust sheets. Lubrication of thrust sheets by shales or evaporites and flotation by anomalously high pressures may be simply different manifestations of the same geologic milieu. © 1965, The Geological Society of America, Inc.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1965)76[1379:OEAOF]2.0.CO;2","issn":"00167606","usgsCitation":"Hanshaw, B., and Zen, E., 1965, Osmotic equilibrium and overthrust faulting: Geological Society of America Bulletin, v. 76, no. 12, p. 1379-1385, https://doi.org/10.1130/0016-7606(1965)76[1379:OEAOF]2.0.CO;2.","productDescription":"7 p. ","startPage":"1379","endPage":"1385","costCenters":[],"links":[{"id":370288,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"76","issue":"12","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Hanshaw, B.B.","contributorId":25928,"corporation":false,"usgs":true,"family":"Hanshaw","given":"B.B.","email":"","affiliations":[],"preferred":false,"id":777530,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Zen, E-An","contributorId":47064,"corporation":false,"usgs":true,"family":"Zen","given":"E-An","email":"","affiliations":[],"preferred":false,"id":777531,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70208785,"text":"70208785 - 1965 - Late quaternary geologic history of the lower Chippewa Valley, Wisconsin","interactions":[],"lastModifiedDate":"2020-02-28T11:01:40","indexId":"70208785","displayToPublicDate":"1965-12-31T10:55:42","publicationYear":"1965","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":5935,"text":"Bulletin of the Geological Society of America","active":true,"publicationSubtype":{"id":10}},"title":"Late quaternary geologic history of the lower Chippewa Valley, Wisconsin","docAbstract":"The lower Chippewa Valley in west-central Wisconsin extends 65 miles from the Cary terminal moraine in Chippewa County to the Mississippi River Valley. The Chippewa Valley and its tributaries were filled with a valley train of sand and gravel during the maximum stand of the Cary ice, and entrenchment of this deposit has formed the Wissota terrace, a prominent geomorphic feature that can be traced the length of the valley. Several lower terraces in the valley indicate progressive downcutting of the Wissota terrace sediments. Erosion and deposition in the Mississippi Valley are closely linked to the post-Cary history of the lower Chippewa Valley, for these factors controlled the outlet level of the Chippewa River. This outlet was substantially lower than at present throughout much of post-Cary Pleistocene and early Recent time. The modern Chippewa River has built a delta into the Mississippi Valley. The Chippewa River is aggrading the lower part of its valley, a meandering river is slowly eroding the central part; stream erosion in the upper part is restricted by sills of hard bedrock.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1965)76[113:LQGHOT]2.0.CO;2","usgsCitation":"Andrews, G., 1965, Late quaternary geologic history of the lower Chippewa Valley, Wisconsin: Bulletin of the Geological Society of America, v. 76, no. 1, p. 113-124, https://doi.org/10.1130/0016-7606(1965)76[113:LQGHOT]2.0.CO;2.","productDescription":"12 p.","startPage":"113","endPage":"124","costCenters":[],"links":[{"id":372739,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Wisconsin","otherGeospatial":"Lower Chippewa Valley","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -92.36480712890625,\n 44.22552029849434\n ],\n [\n -91.01348876953125,\n 44.22552029849434\n ],\n [\n -91.01348876953125,\n 45.14911623279028\n ],\n [\n -92.36480712890625,\n 45.14911623279028\n ],\n [\n -92.36480712890625,\n 44.22552029849434\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"76","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Andrews, George W.","contributorId":40621,"corporation":false,"usgs":true,"family":"Andrews","given":"George W.","affiliations":[],"preferred":false,"id":783380,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ]}