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About 90 percent of the area is forested and the remainder is chiefly farm land.\r\n\r\nThe topography reflects the geologic structure and varied resistance of the bedrock to erosion. Most of the area is on the east limb of the Green Mountain \r\nanticlinorium, which is the principal structural feature of Vermont. The bedrock is predominantly sedimentary and volcanic rock that has been regionally metamorphosed. It was intruded before metamorphism by mafic and ultramafic igneous rocks, and after metamorphism by felsic and mafic igneous rocks. The metamorphosed sedimentary and volcanic rocks range in age from Cambrian(?) to Middle Silurian, the intrusive igneous rocks from probably Late Ordovician to probably late Permian. Metamorphism and principal folding in the region occurred in Middle Devonian time.\r\n\r\nThe metamorphosed sedimentary and volcanic rocks make up a section at least \r\n25,000 feet thick and can be divided into nine formations. The Hazens Notch \r\nformation of Cambrian(?) and Early Cambrian age is characterized by carbonaceous schist. It is succeeded in western parts of the area by the Jay Peak formation of Early Cambrian age, which is chiefly a schist that is distinguished by the general absence of carbonaceous zones; in central parts of the area the Hazens Notch formation is followed by the Belvidere Mountain amphibolite, probably the youngest of the formations of Early Cambrian age. The Ottauquechee formation, composed of carbonaceous phyllite and quartzite, and phyllitic graywacke, is of Middle Cambrian age. The Stowe formation of Late Cambrian(?) and Early(?) Ordovician age overlies the Ottauquechee and is predominantly noncarbonaceous schist, though it also contains greenstone and carbonaceous schist and phyllite. The Umbrella Hill formation of Middle Ordovician age is characteristically a conglomerate in which the mineral chloritoid is common. The overlying Moretown formation, also of Middle Ordovician age, contains granulite and slate, also greenstone and amphibolite of the Coburn Hill volcanic member. The Shaw Mountain formation, made up of conglomerate, phyllite, and limestone, is the oldest Silurian unit. The Shaw Mountain formation is succeeded by the Northfield slate of Middle Silurian age.\r\n\r\nThe igneous rocks of the region include various ultramafic plutonic rocks, such \r\nas dunite, peridotite, and serpentinite, probably of Late Ordovician age; sills and nearly concordant dikes of metagabbro of Late Ordovician age; biotite granite plutons or Middle or Late Devonian age, most notably on Eltey Mountain; and hypabyssallamprophyre, probably of late Permian age.\r\n\r\nMetamorphic zoning is shown by the distribution of rocks of the epidote-amphibolite facies and the greenschist facies in and near the Green Mountains, and near Coburn Hill and Eltey Mountain. Metasomatism related to regional metamorphism has produced porphyroblasts and quartz segregations in the sedimentary and volcanic rocks, and steatitization and carbonatization of serpentinite. Contact metamorphism has formed rocks of the epidote-amphibolite facies near granite plutons, and probably calc-silicate rock at the contacts of ultramafic plutons.\r\n\r\nThe axial anticline of the Green Mountain anticlinorium and other anticlines \r\nand synclines to the east are the major longitudinal structural features of the area. These structures are complicated by transverse folds, particularly a syncline in the vicinity of Tillotson Peak. Early minor cross folds that are best developed in the Hazens Notch formation are believed to be genetically related to the transverse folds. The axial planes of the cross folds are folded about the axes of the later longitudinal folds of the Green Mountain anticlinorium. The longitudinal and transverse fold systems probably formed in the same episode of defor","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Contributions to Economic Geology (1960)","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"ENGLISH","publisher":"Geological Survey (U.S.)","doi":"10.3133/b1122B","usgsCitation":"Cady, W.M., Albee, A.L., and Chidester, A., 1963, Bedrock Geology and Asbestos Deposits of the Upper Missisquoi Valley and Vicinity, Vermont: U.S. Geological Survey Bulletin 1122, Report: iv, pages B1-B78; 2 Plates - Plate 1: 36 x 25 inches, Plate 2: 10 x 14 inches, https://doi.org/10.3133/b1122B.","productDescription":"Report: iv, pages B1-B78; 2 Plates - Plate 1: 36 x 25 inches, Plate 2: 10 x 14 inches","costCenters":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":109361,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_20823.htm","linkFileType":{"id":5,"text":"html"},"description":"20823"},{"id":167327,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1122b/report-thumb.jpg"},{"id":61791,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1122b/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":61792,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1122b/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":61793,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1122b/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"62500","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -72.58333333333333,44.65 ], [ -72.58333333333333,45.016666666666666 ], [ -72.25,45.016666666666666 ], [ -72.25,44.65 ], [ -72.58333333333333,44.65 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a6be4b07f02db63db0d","contributors":{"authors":[{"text":"Cady, Wallace Martin","contributorId":98307,"corporation":false,"usgs":true,"family":"Cady","given":"Wallace","email":"","middleInitial":"Martin","affiliations":[],"preferred":false,"id":212144,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Albee, Arden Leroy","contributorId":83912,"corporation":false,"usgs":true,"family":"Albee","given":"Arden","email":"","middleInitial":"Leroy","affiliations":[],"preferred":false,"id":212143,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Chidester, A.H.","contributorId":42940,"corporation":false,"usgs":true,"family":"Chidester","given":"A.H.","email":"","affiliations":[],"preferred":false,"id":212142,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":2382,"text":"wsp1614 - 1963 - Water resources of Red River Parish, Louisiana","interactions":[],"lastModifiedDate":"2012-02-02T00:05:19","indexId":"wsp1614","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","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":"1614","title":"Water resources of Red River Parish, Louisiana","docAbstract":"Red River Parish is on the eastern flank of the Sabine uplift in northwestern Louisiana. The 'area is underlain by lignitic clay and sand of Paleocene and Eocene age which dip to the east at the rate of about 30 feet per mile. The Red River is entrenched in these rocks in the western part of the parish. Alternating valley filling and erosion during the Quaternary period have resulted in the present lowland with flanking terraces. \r\n\r\nIn the flood-plain area moderate to large quantities of very hard, iron-bearing water, suitable for irrigation, are available to wells in the alluvial sand and gravel of Quaternary age. The aquifer ranges in thickness from 20 to slightly more than 100 feet. It is recharged by downward seepage of rainfall through overlying clay and silt, by inflow from older sands adjacent to and beneath the entrenched valley, and by infiltration from the streams where the water table is below stream level during flood stages or as a result of pumping. Water levels are highest in the middle of the valley. Ground water moves mainly toward the Red River on the east and Bayou Pierre on the west, but small amounts move down the valley. Computations based on water-level and aquifer-test data indicate that the Quaternary alluvium contains more than 330 billion gallons of ground water in storage and that the maximum discharge of ground water to the streams is slightly more than 30 mgd (million gallons per day). At times of high river stage, surface water flows into the aquifer at a rate that depends in part upon the height and duration of the river stage. \r\n\r\nModerate supplies of soft, iron-bearing water may be obtained from dissected Pleistocene terrace deposits that flank the flood plains of the Red River and Black Lake Bayou. However, the quantity of water that can be pumped from these deposits varies widely from place to place because of differences in the areal extent and saturated thickness of the segments of the deposits; this extent and thickness are governed in turn by the amount of erosion the deposits have undergone. Beds of fine-grained lignitic sands of Tertiary age contain water of generally good quality to depths of 150 to 450 feet. The thinness and low permeability of the sands restrict their development to low-yield wells. Water from these sands in the western part of the parish, where they lie beneath the alluvial valley, is more mineralized than that from the younger Tertiary sands exposed in the east-central area. \r\n\r\nStreamflow records have been collected on the principal streams in Red River Parish since 1939. Additional spot low-flow data were obtained on several small streams originating within the parish for a study made in connection with the preparation of this report. Quality-of-water data for streams in the parish were collected on an occasional spot-sampling basis prior to and during this investigation. The largest source of surface water in the parish is the Red River, which drains approximately 63,400 square miles upstream from the parish. The Red River has an average flow of about 13,100 cfs (cubic feet per second), or about 8,500 mgd. Many of the streams that drain the upland area are not dependable sources of supply because their flows are not well sustained during dry seasons.\r\n\r\nThe average annual precipitation over the parish is about 52 inches, of which about 17 inches becomes runoff; this runoff is equivalent to a continuous flow of about 1.25 cfs per square mile. Seasonal and annual runoff varies, but no significant trends have been noticed.\r\n\r\nThe principal surface-water problems in the parish pertain to flood control, drainage, irrigation, and navigation. Flood problems have been alleviated considerably by the operation of Denison Dam (Lake Texoma), the completion of levees on the Red River, channel improvements on Bayou Pierre, and the completion of Wallace Lake reservoir on Cypress Bayou. There are wet lands along the Red River that would be very productive if properly drained ","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1614","usgsCitation":"Newcome, R., and Page, L.V., 1963, Water resources of Red River Parish, Louisiana: U.S. Geological Survey Water Supply Paper 1614, v, 133 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1614.","productDescription":"v, 133 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":109996,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24808.htm","linkFileType":{"id":5,"text":"html"},"description":"24808"},{"id":137824,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1614/report-thumb.jpg"},{"id":28344,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28345,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-02.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28346,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-03.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28347,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-04.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28348,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-05.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28349,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-06.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28350,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-07.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28351,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28352,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-09.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28353,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28354,"rank":410,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28355,"rank":411,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-12.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28356,"rank":412,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-13.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28357,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1614/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a16e4b07f02db603d22","contributors":{"authors":[{"text":"Newcome, Roy","contributorId":14796,"corporation":false,"usgs":true,"family":"Newcome","given":"Roy","affiliations":[],"preferred":false,"id":145113,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Page, Leland Vernon","contributorId":95450,"corporation":false,"usgs":true,"family":"Page","given":"Leland","email":"","middleInitial":"Vernon","affiliations":[],"preferred":false,"id":145114,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":14075,"text":"ofr6345 - 1963 - Preliminary interpretation of an aeromagnetic survey in north-central Iowa","interactions":[],"lastModifiedDate":"2024-07-26T22:16:42.14486","indexId":"ofr6345","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","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":"63-45","title":"Preliminary interpretation of an aeromagnetic survey in north-central Iowa","docAbstract":"Publication of Lyons' gravity map of the United States in 1950 focused attention on a spectacular geophysical feature now generally referred to as the \"midcontinent gravity high.\" This feature, the largest gravity maximum in North America, was discovered and later detailed by geophysicists at the University of Wisconsin (Woollard, 1943, 1951) and Thiel (1956). Their work reveals an essentially continuous large positive gravity anomaly extending southwestward for 800 miles from Lake Superior to the Salina Basin in Kansas. The midcontinent gravity high reaches its maximum intensity in central Iowa where the Bouguer anomaly ranges from -100 to 60 milligals.
In September-October 1961, the U. S. Geological Survey made a 5,000 square mile aeromagnetic survey in north-central Iowa in cooperation with the Iowa Geological Survey. Objectives of the investigation were to prepare and interpret a detailed aeromagnetic contour map for part of the midcontinent gravity high in Iowa. Analysis of the magnetic data could be expected to yield estimates of local thickness of the Paleozoic-Mesozoic sedimentary section and provide a basis for informed speculation about the character, configuration, and distribution of the Precambrian rocks. Such information would have obvious scientific and possible economic value in an area covered by glacial till and for which little deep subsurface knowledge was available. Interpretation of the Indiana aeromagnetic survey (Henderson and Zietz, 1958) had previously demonstrated that aeromagnetic data from the central stable region of North America would provide a significant amount of geologic information.
The 5,000 square mile area surveyed in 1961 has been combined with a previously unpublished 600 square mile aeromagnetic survey made in 1953, centered on Manson, Pocahontas Co., Iowa. The combined area is shown as the patterned area in figure 1. The unpatterned area outlined on this same figure is the additional 10,000 square mile cooperative aeromagnetic survey made in the summer of 1962 to complete coverage of the midcontinent gravity high in Iowa.
The primary purpose of this report is to make the 1953 and 1961 aeromagnetic data available to the public in advance of more formal publication. Only salient magnetic features are discussed in this preliminary presentation and in a second report on results obtained during the 1962 flying. A more complete interpretation of the entire aeromagnetic survey will be prepared.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr6345","collaboration":"Prepared in cooperation with the Iowa Geological Survey","usgsCitation":"Henderson, J.R., White, W., and Zietz, I., 1963, Preliminary interpretation of an aeromagnetic survey in north-central Iowa: U.S. Geological Survey Open-File Report 63-45, Report: 27 p.; 4 Figures: 36.03 x 23.90 inches or smaller, https://doi.org/10.3133/ofr6345.","productDescription":"Report: 27 p.; 4 Figures: 36.03 x 23.90 inches or smaller","costCenters":[],"links":[{"id":431530,"rank":7,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1963/0045/figure-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431529,"rank":6,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1963/0045/figure-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431528,"rank":5,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1963/0045/figure-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431527,"rank":4,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1963/0045/figure-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431526,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1963/0045/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":410197,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_8045.htm","linkFileType":{"id":5,"text":"html"}},{"id":146687,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1963/0045/report-thumb.jpg"}],"country":"United States","state":"Iowa","otherGeospatial":"north-central Iowa","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -95,\n 43.5\n ],\n [\n -95,\n 42.333\n ],\n [\n -92.5,\n 42.333\n ],\n [\n -92.5,\n 43.5\n ],\n [\n -95,\n 43.5\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afee4b07f02db69742d","contributors":{"authors":[{"text":"Henderson, John Richard","contributorId":52975,"corporation":false,"usgs":true,"family":"Henderson","given":"John","email":"","middleInitial":"Richard","affiliations":[],"preferred":false,"id":168890,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"White, Walter S.","contributorId":34492,"corporation":false,"usgs":true,"family":"White","given":"Walter S.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":168889,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Zietz, Isidore","contributorId":76708,"corporation":false,"usgs":true,"family":"Zietz","given":"Isidore","affiliations":[],"preferred":false,"id":168891,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":32743,"text":"pp379 - 1963 - Surficial geology and soils of the Elmira-Williamsport region, New York and Pennsylvania, with a section on forest regions and great soil groups","interactions":[],"lastModifiedDate":"2022-03-29T21:42:36.762876","indexId":"pp379","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","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":"379","title":"Surficial geology and soils of the Elmira-Williamsport region, New York and Pennsylvania, with a section on forest regions and great soil groups","docAbstract":"The Elmira-Williamsport region, lying south of the Finger Lakes in central New York and northern Pennsylvania, is part of the Appalachian Plateaus physiographic province. A small segment of the Valley and Ridge province is included near the south border. In 1953 and 1954, the authors, a geologist and a soil scientist, made a reconnaissance of about 5,000 square miles extending southward from the Finger Lakes, N.Y., to Williamsport, Pa., and eastward from Wellsboro, Pa., to Towanda, Pa. Glacial drift of Wisconsin age, covering the central and most of the northern parts of the region, belongs to the Olean substage of MacClintock and Apfel. This drift is thin and patchy, is composed of the relatively soft sandstones, siltstone, shales, and conglomerates of the plateaus, commonly has a low calcium carbonate content, and is deeply leached. Mantling its surface are extensive rubbly colluvial deposits. No conspicuous terminal moraine marks the relatively straight border of Olean drift. The Valley Heads moraine of Fairchild near the south ends of the Finger Lakes is composed of relatively thick drift containing a considerable amount of somewhat resistant sedimentary and crystalline rocks. Commonly this drift has a relatively high carbonate content and is leached to only shallow depths. The Valley Heads drift is younger than Olean, but its precise age is undetermined. The age of the Olean is perhaps between Sangamon and Farmdale, on the basis of, in part, a carbon-14 date from peat at Otto, N.Y. All differences in soil development on these two Wisconsin drifts are clearly related to the lithology of the parent material or the drainage, rather than to weathering differing in kind or in duration. The authors believe that the soils are relatively young, are in equilibrium with the present environment, and contain few, if any, features acquired during past weathering intervals. The effect of tree throw on soil profiles and the presence of soils on slopes clearly indicate that soils form rapidly. Sols Bruns Acides are the most extensive great soil group occurring throughout the region. Podzols and Gray-Brown Podzolic soils are also widespread, and on long, smooth slopes Low Humic-Gley soils are common. Organic soils are of small extent. South of the Wisconsin drift border, the surficial mantle consists chiefly of alluvial, colluvial, or residual deposits of Wisconsin or of Recent age, but there are many small isolated patches of older, strongly weathered materials of pre-Wisconsin age. Although such older materials are commonly overlain or mixed with less weathered mantle, the yellowish-red color, characteristic of the strongly weathered material, is generally not masked. Some of the older material is drift, presumed to be of Illionian age, that was probably strongly weathered to a considerable depth in Sangamon time and has been greatly eroded since the last interglacial period. No clear-cut exposure of Wisconsin drift resting on older drift or other strongly weathered mantle has been found. The old drift and the other strongly weathered materials apparently acquired their present red color in pre-Wisconsin time. Where exposed at the surface, such strongly weathered mantle is the parent material of modern Red-Yellow Podzolic soils. Sols Bruns Acides and Gray-Brown Podzolic soils, developed on slightly weathered parent materials, are found adjacent to these red soils. This suggests that these Red-Yellow Podzolic soils probably developed from strongly weathered parent materials. No buried soils were found nor were any soils recognized as relics from pre-Wisconsin time. Comparison of a map of the great soil groups with a map of the vegetation of the region, prepared by John C. Goodlett, does not reveal a close relation. Laboratory analyses of samples collected furnish data on textural, mineralogical, and chemical changes caused by weathering and soil formation. The results indicate that the amount of chemical weathering which the Wisconsin drift has undergone is slight. The Red-Yellow Podzolic soils on strongly weathered pre-Wisconsin drift have B2 horizons that have a finer texture than the A2 or C horizons. The parent materials of these soils seem to be strongly weathered because of the high chromas, reddish hues, friable condition of most rock fragments, relatively high kaolinite content, and presence of gibbsite in the clay fraction. Measurements at numerous localities show that the depth of leaching increases with decreasing carbonate content and is not a criterion of the age of the drift. Pebble counts of gravels also show that the depth of leaching of gravel is related to its limestone content. The location of the gravel deposits is probably due primarily to the presence of pebbles of resistant rock rather than to ice wastage involving abundant glacial melt water. The region is in the Susquehanna drainage basin except for its north fringe, which drains to Lake Ontario. Most of the region is a dissected plateau ranging in altitude from 700 to 2,500 feet and underlain by gently folded sedimentary rocks of Paleozoic age. Much of the region slopes moderately or steeply; the most extensive areas of gently sloping land are 011 the uplands. In the northern part are several straight and deep valleys the southern extension of the Finger Lakes basins separated by uplands with several low cuestas that face north. Similarly, some streams such as the Canisteo, Cohocton, and Chemung Rivers, and the part of the Susquehanna River that is in New York, trend at right angles to the Finger Lakes, flowing in valleys that parallel the regional strike of the bedrock. The Olean drift border is marked by a change from drift containing very few rounded or striated rock fragments to a mantle containing only angular rock fragments and traces of red, strongly weathered materials. A reconstruction of the surface of the ice sheet, at its maximum extent shows an inferred slope of its distal margin ranging from 100 to 500 feet per mile
","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/pp379","usgsCitation":"Denny, C.S., Lyford, W.H., and Goodlett, J.C., 1963, Surficial geology and soils of the Elmira-Williamsport region, New York and Pennsylvania, with a section on forest regions and great soil groups: U.S. Geological Survey Professional Paper 379, Report: iv, 59 p.; 6 Plates: 41.94 × 24.00 inches or smaller, https://doi.org/10.3133/pp379.","productDescription":"Report: iv, 59 p.; 6 Plates: 41.94 × 24.00 inches or smaller","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":60663,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0379/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60662,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0379/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60661,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0379/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60660,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0379/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60659,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0379/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60664,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0379/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60665,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0379/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":397823,"rank":9,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4377.htm"},{"id":121752,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0379/report-thumb.jpg"}],"scale":"250000","country":"United States","state":"New York, Pennsylvania","otherGeospatial":"Elmira-Williamsport region","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -77.5,\n 41.1667\n ],\n [\n -76.25,\n 41.1667\n ],\n [\n -76.25,\n 42.5\n ],\n [\n -77.5,\n 42.5\n ],\n [\n -77.5,\n 41.1667\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae2e4b07f02db688b83","contributors":{"authors":[{"text":"Denny, Charles Storrow","contributorId":86331,"corporation":false,"usgs":true,"family":"Denny","given":"Charles","email":"","middleInitial":"Storrow","affiliations":[],"preferred":false,"id":209081,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lyford, Walter Henry","contributorId":43824,"corporation":false,"usgs":true,"family":"Lyford","given":"Walter","email":"","middleInitial":"Henry","affiliations":[],"preferred":false,"id":209080,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Goodlett, J. 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Nearly 100 of these are in Alaska, and 100 in Minnesota, Wisconsin, Michigan, New York,, and Maine.
\nThirty-four fresh-water lakes, exclusive of the Great Lakes, are known to have maximum depths of 250 feet or more. Twenty of these are in Alaska, and Alaska undoubtedly has more lakes of that depth which have not been sounded.
\nThe amount of water stored in natural lakes even exclusive of the Great Lakes is much greater than the amount stored in artificial reservoirs. With the exception of the Great Lakes, however, the economic value of natural lakes is surpassed by that of artificial reservoirs. Natural lakes are best known for the recreational advantages they afford.
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water, a large sample is required to provide the 3 grams of carbon needed for a carbon-14 determination. A field procedure for isolating total dissolved-carbonate species is described. Carbon dioxide gas is evolved by adding sulfuric acid to the water sample; the gas is then collected in a sodium hydroxide trap by recycling in a closed system. The trap is then transported to the dating laboratory where the carbon-14 is counted.","language":"ENGLISH","publisher":"United States Geological Survey,","doi":"10.3133/cir480","usgsCitation":"Feltz, H., and Hanshaw, B.B., 1963, Preparation of water samples for carbon-14 dating: U.S. Geological Survey Circular 480, iii, 3 p. :ill. ;27 cm., https://doi.org/10.3133/cir480.","productDescription":"iii, 3 p. :ill. ;27 cm.","costCenters":[],"links":[{"id":123205,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1963/0480/report-thumb.jpg"},{"id":31050,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1963/0480/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a94e4b07f02db658935","contributors":{"authors":[{"text":"Feltz, H.R.","contributorId":49341,"corporation":false,"usgs":true,"family":"Feltz","given":"H.R.","email":"","affiliations":[],"preferred":false,"id":147909,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hanshaw, Bruce B.","contributorId":47350,"corporation":false,"usgs":true,"family":"Hanshaw","given":"Bruce","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":147908,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":43709,"text":"ofr63110 - 1963 - Geologic maps and sections of part of the Philipsburg district, Granite County, Montana","interactions":[{"subject":{"id":43709,"text":"ofr63110 - 1963 - Geologic maps and sections of part of the Philipsburg district, Granite County, Montana","indexId":"ofr63110","publicationYear":"1963","noYear":false,"title":"Geologic maps and sections of part of the Philipsburg district, Granite County, Montana"},"predicate":"SUPERSEDED_BY","object":{"id":35523,"text":"b1237 - 1967 - Geology and ore deposits of the Philipsburg district, Granite County, Montana","indexId":"b1237","publicationYear":"1967","noYear":false,"title":"Geology and ore deposits of the Philipsburg district, Granite County, Montana"},"id":1}],"supersededBy":{"id":35523,"text":"b1237 - 1967 - Geology and ore deposits of the Philipsburg district, Granite County, Montana","indexId":"b1237","publicationYear":"1967","noYear":false,"title":"Geology and ore deposits of the Philipsburg district, Granite County, Montana"},"lastModifiedDate":"2020-02-03T12:46:21","indexId":"ofr63110","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","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":"63-110","title":"Geologic maps and sections of part of the Philipsburg district, Granite County, Montana","docAbstract":"No abstract available.
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