The Lake Mary quadrangle is in eastern Iron County, in the west part of the Upper Peninsula of Michigan. The quadrangle is underlain by Lower and Middle Precambrian rocks, formerly designated Archean and Algonkian rocks, and is extensively covered by Pleistocene glacial deposits. A few Upper Precambrian (Keweenawan) diabase dikes and two remnants of sandstone and dolomite of early Paleozoic age are also found in the area.
The major structural feature is the Holmes Lake anticline, the axis of which strikes northwest through the northeast part of the quadrangle. Most of the quadrangle, therefore, is underlain by rock of the west limb of the anticline. To the northwest along the fold axis, the Holmes Lake anticline is separated from the Amasa oval by a saddle of transverse folds in the vicinity of Michigamme Mountain in the Kiernan quadrangle.
The Lower Precambrian rocks are represented by the Dickinson group and by porphyritic red granite whose relation to the Dickinson group is uncertain, but which may be older. The rocks of the Dickinson group are chiefly green to black metavolcanic schist and red felsite, some of the latter metarhyolite. The dark schist is commonly magnetic. The Dickinson group underlies the core area of the Holmes Lake anticline, which is flanked by steeply dipping Middle Precambrian formations of the Animikie series.
A major unconformity separates the Lower Precambrian rocks from the overlying Middle Precambrian rocks. In ascending order the formations of the Middle Precambrian are the Randville dolomite, the Hemlock formation, which includes the Mansfield iron-bearing slate member, and the Michigamme slate. An unconformity occurs between the Hemlock formation and Michigamme slate. The post-Hemlock unconformity is thought to be represented in the Lake Mary quadrangle by the absence of iron-formation of the Amasa formation, which is known to lie between the Hemlock and the Michigamme to the northwest of the Lake Mary quadrangle in the Crystal Falls quadrangle. Post-Hemlock erosion may account also for the absence of iron-formation of the Fence River formation on the east limb of the Holmes Lake anticline within the Lake Mary quadrangle.
The Randville dolomite is not exposed and is known only from diamond drilling in the northeast part of the area where it occurs in the east and west limbs of the Holmes Lake anticline. The formation has a maximum thickness of about 2,100 feet; this includes a lower arkosic phase, some of which is quartz pebble conglomerate, a medial dolomitic phase, and an upper slate phase. The triad is gradational. Included within the formation are a few beds of chloritic schist thought to be of volcanic origin. An unconformity between the Randville and the succeeding Hemlock is not indicated in the quadrangle, but is probably present.
The Hemlock formation is best exposed in the northwest and south-central parts of the area. The apparent thickness of the formation is 10,000- 17,000 feet. It is composed mainly of mafic metavolcanic rocks and intercalated slate and iron-formation. In the north part of the quadrangle the volcanic rocks are greenstone, which includes altered basaltic flow rocks, volcanic breccia, tuff, and slate. Pillow structures are common in the metabasalt. It is not certain if any Hemlock rocks are present in the east limb of the Holmes Lake anticline. In the south part of the quadrangle, the rocks of the Hemlock are chiefly chlorite and hornblende schist and hornfels. Pyroxene hornfels is sparingly present.
At least two sedimentary slate belts are included in the Hemlock formation. One of these, the Mansfield iron-bearing slate member, includes in its upper part an altered chert-siderite iron-formation 30 to over 150 feet thick from which iron ore has been mined at the Mansfield location. The position of the iron-bearing rocks has been determined magnetically, and past explorations for iron ore are discussed.
Though probably; unconformable, the contact between the Hemlock and the Michigamme formations appears conformable. The Michigamme slate consists of at least 4,000 feet of interbedded mica schist and granulite, the altered equivalents of the slate and graywacke characteristic of the Michigamme in adjacent areas. The Michigamme rocks are best exposed in the south part of the quadrangle in the vicinity of Peavy Pond.
Two periods of regional metamorphism have resulted in the alteration of almost all of the rocks of the quadrangle. The Lower Precambrian rocks underwent at least one period of metamorphism, uplift, and erosion before the deposition of the Randville dolomite. After the deposition of the Michigamme slate, a post-Middle Precambrian period of regional metamorphism occurred with attending deformation and igneous intrusion. The grade of metamorphism rises toward the south in the area. The rocks in the northern two-thirds of the quadrangle are representative of greenschist facies of regional metamorphism, whereas the rocks in the southern onethird of the quadrangle are representative of the albite-epidote-amphibolite, the amphibolite, and the pyroxene hornfels facies, the metamorphic node centering about the intrusive Peavy Pond complex in the Peavy Pond area.
The Precambrian sedimentary and volcanic rocks are cut by intrusive igneous rocks of different types and several different ages. Gabbroic sills and dikes invaded the Hemlock rocks at some time after the Hemlock was deposited and before the post-Middle Precambrian orogeny and metamorphism. Some contact metamorphism attended the intrusion of the major sills. One of the sills, the West Kiernan sill, is well differentiated. A syntectonic igneous body, composed of gabbro and minor ultramafic parts and fringed with intermediate and felsic differentiates and hybrids, the Peavy; Pond complex, was intruded into the Hemlock and Michigamme formations during the post-Middle Precambrian orogeny. The complex is situated in the Peavy Pond area at the crest of the regional metamorphic node. Contact-altered sedimentary and volcanic rocks margin the complex.
The effects of regional metamorphism have been superposed on the contact metamorphic rocks peripheral to the complex and on the igneous rocks of the complex as well. The mafic augite-bearing rocks of the complex emplaced early in the orogeny were deformed by granulation at the peak of the deformation and subsequently metamorphosed to hornblende rocks. Some of the intermediate and felsic rocks of the complex were foliated by the deformation, while the more fluid, felsic parts of the complex were intruded under orogenic stress and crystallized after the peak of deformation. The deformation culminated in major faulting during which the formations were dislocated, and some of the granite of the complex was extremely brecciated.
A few diabase dikes, probably of Keweenawan age, have intruded the deformed and altered Animikie rocks.
The only known metallic resource is iron ore. The Mansfield mine produced 1¥2 million tons of high-grade iron ore between the years 1890 and 1913. Sporadic exploration since 1913 has failed to reveal other ore deposits of economic importance.
","language":"English","publisher":"U. S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/b1077","collaboration":"Prepared in cooperation with the Geological Survey Division Michigan Department of Conservation","usgsCitation":"Bayley, R.W., 1959, Geology of the Lake Mary quadrangle, Iron County, Michigan: U.S. Geological Survey Bulletin 1077, Document: v, 112 p.; 7 Plates: 38.91 x 33.74 inches or smaller, https://doi.org/10.3133/b1077.","productDescription":"Document: v, 112 p.; 7 Plates: 38.91 x 33.74 inches or smaller","costCenters":[{"id":382,"text":"Michigan Water Science Center","active":true,"usgs":true}],"links":[{"id":96076,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1077/plate-1.pdf","size":"5234","linkFileType":{"id":1,"text":"pdf"}},{"id":96077,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1077/plate-2.pdf","size":"3204","linkFileType":{"id":1,"text":"pdf"}},{"id":96078,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1077/plate-3.pdf","size":"3526","linkFileType":{"id":1,"text":"pdf"}},{"id":96079,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1077/plate-4.pdf","size":"981","linkFileType":{"id":1,"text":"pdf"}},{"id":96080,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1077/plate-5.pdf","size":"2776","linkFileType":{"id":1,"text":"pdf"}},{"id":96081,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1077/plate-6.pdf","size":"2526","linkFileType":{"id":1,"text":"pdf"}},{"id":96082,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1077/plate-7.pdf","size":"289","linkFileType":{"id":1,"text":"pdf"}},{"id":109296,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_20736.htm","linkFileType":{"id":5,"text":"html"},"description":"20736"},{"id":61608,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1077/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":163861,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1077/report-thumb.jpg"}],"country":"United States","state":"Michigan","county":"Iron County","otherGeospatial":"Lake Mary quadrangle","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -88.25,\n 46.125\n ],\n [\n -88.25,\n 46\n ],\n [\n -88.125,\n 46\n ],\n [\n -88.125,\n 46.125\n ],\n [\n -88.25,\n 46.125\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4acee4b07f02db67f91d","contributors":{"authors":[{"text":"Bayley, Richard W.","contributorId":106084,"corporation":false,"usgs":true,"family":"Bayley","given":"Richard","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":211857,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":34836,"text":"b1046R - 1959 - Uranium in Sharon Springs member of Pierre shale, South Dakota and northeastern Nebraska","interactions":[],"lastModifiedDate":"2012-02-02T00:09:27","indexId":"b1046R","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1046","chapter":"R","title":"Uranium in Sharon Springs member of Pierre shale, South Dakota and northeastern Nebraska","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/b1046R","usgsCitation":"Kepferle, R.C., 1959, Uranium in Sharon Springs member of Pierre shale, South Dakota and northeastern Nebraska: U.S. Geological Survey Bulletin 1046, p. 577-604, ill., maps (fold. in pocket) ;24 cm., https://doi.org/10.3133/b1046R.","productDescription":"p. 577-604, ill., maps (fold. in pocket) ;24 cm.","costCenters":[],"links":[{"id":109228,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_20656.htm","linkFileType":{"id":5,"text":"html"},"description":"20656"},{"id":163976,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1046r/report-thumb.jpg"},{"id":62785,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1046r/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":62786,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1046r/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":62787,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1046r/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":62788,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1046r/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":62789,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1046r/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a18e4b07f02db6054ce","contributors":{"authors":[{"text":"Kepferle, Roy Clark","contributorId":46072,"corporation":false,"usgs":true,"family":"Kepferle","given":"Roy","email":"","middleInitial":"Clark","affiliations":[],"preferred":false,"id":213667,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":39082,"text":"pp296 - 1959 - Geology of Glacier National Park and the Flathead Region, Northwestern Montana","interactions":[],"lastModifiedDate":"2018-12-10T08:08:20","indexId":"pp296","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","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":"296","title":"Geology of Glacier National Park and the Flathead Region, Northwestern Montana","docAbstract":"This report summarizes available data on two adjacent and partly overlapping regions in northwestern Montana. The first of these is Glacier National Park plus small areas east and west of the park. The second is here called, for convenience, the Flathead region; it embraces the mountains from the southern tip of Glacier Park to latitude 48 deg north and between the Great Plains on the east and Flathead Valley on the west. The fieldwork under the direction of the writer was done in 1948, 1949, 1950, and 1951, with some work in 1952 and 1953.\r\n\r\nThe two regions together include parts of the Swan, Flathead, Livingstone, and Lewis Ranges. They are drained largely by branches of the Flathead River. On the east and north, however, they are penetrated by tributaries of the Missouri River and in addition by streams that flow into Canada. Roads and highways reach the borders of the regions; but there are few roads in the regions and only two highways cross them. The principal economic value of the assemblage of mountains described in the present report is as a collecting ground for snow to furnish the water used in the surrounding lowlands and as a scenic and wildlife recreation area. A few metallic deposits and lignitic coal beds are known, but these have not proved to be important and cannot, as far as can now be judged, be expected to become so. No oil except minor seeps has yet been found, and most parts of the two regions covered do not appear geologically favorable to the presence of oil in commercial quantities. The high, Hungry Horse Dam on which construction was in progress during the fieldwork now floods part of the Flathead region and will greatly influence the future of that region.\r\n\r\nThe rocks range in age from Precambrian to Recent. The thickest units belong to the Belt series of Precambrian age, and special attention was paid to them. As a result, it is clear that at least the upper part of the series shows marked lateral changes within short distances. This fact introduces complexities into stratigraphic correlation and should be remembered wherever the series is studied. The stromatolites, or fossil algae, in the Belt series, although still imperfectly understood, give clues with respect to problems of ecology and stratigraphy.\r\n\r\nThe subdivisions of the Belt series within the areas covered by the present report are, in ascending order, Altyn limestone, Appekunny argillite, Grinnell argillite, Siyeh limestone, and Missoula group. Local subdivisions of the Missoula group are possible in certain areas, and all the units just named are expected to be subdivided when detailed studies are undertaken.\r\n\r\nIn the Glacier National Park and Flathead regions together, it is probable that between 25,000 and 30,000 feet of beds belonging to the Belt series, possibly more, are present. These consist largely of quartzitic argillite, quartzite, and carbonate rocks, mostly dolomitic. Small gabbroic and diabasic intrusive bodies and, at one horizon, basaltic lava are associated with the Belt series. Above the Belt series is a thick sequence of Cambrian, Devonian, and Carboniferous strata, in which limestone is dominant, followed by strata of Jurassic and Cretaceous age, largely limestone and shale and partly of terrestrial origin. Slightly consolidated gravel, sand, and silt of Tertiary age are preserved in some valleys and as erosional remnants on the plains close to the mountain border. Pleistocene and Recent glacial and fluviatile deposits are plentiful in mountain valleys and on the plains east of the mountains.\r\n\r\nSufficient crustal movements took place during the latter part of Belt time to produce tension cracks that permitted some intrusion and related extrusion to occur. Broad crustal warping probably took place at intervals during the Paleozoic era, but these successive movements left little record other than the absence of sedimentary rock units that might otherwise have been deposited. The same can be said of much of the Me","language":"ENGLISH","publisher":"U.S. Geological Survey","doi":"10.3133/pp296","usgsCitation":"Ross, C.P., 1959, Geology of Glacier National Park and the Flathead Region, Northwestern Montana: U.S. Geological Survey Professional Paper 296, 125 p. & plates, https://doi.org/10.3133/pp296.","productDescription":"125 p. & plates","costCenters":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":66396,"rank":399,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0296/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":122228,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0296/report-thumb.jpg"},{"id":66397,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0296/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":66398,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0296/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":66399,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0296/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":66400,"rank":299,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0296/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -116.25,46.25 ], [ -116.25,49 ], [ -111.75,49 ], [ -111.75,46.25 ], [ -116.25,46.25 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad5e4b07f02db683bd1","contributors":{"authors":[{"text":"Ross, Clyde P.","contributorId":10473,"corporation":false,"usgs":true,"family":"Ross","given":"Clyde","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":220917,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1948,"text":"wsp1476 - 1959 - Investigations of Sediment Transportation, Middle Loup River at Dunning, Nebraska: With Application of Data from Turbulence Flume","interactions":[],"lastModifiedDate":"2012-02-02T00:05:22","indexId":"wsp1476","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","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":"1476","title":"Investigations of Sediment Transportation, Middle Loup River at Dunning, Nebraska: With Application of Data from Turbulence Flume","docAbstract":"An investigation of fluvial sediments of the Middle Loup River at Dunning, Nebr., was begun in 1946 and expanded in 1949 to provide information on sediment transportation. Construction of an artificial turbulence flume at which the total sediment discharge of the Middle Loup River at Dunning, Nebr., could be measured with suspended-sediment sampling equipment was completed in 1949. Since that time. measurements have been made at the turbulence flume and at several selected sections in a reach upstream and downstream from the flume. The Middle Loup River upstream from Dunning traverses the sandhills region of north-central Nebraska and has a drainage area of approximately 1,760 square miles. The sandhills are underlain by the Ogallala formation of Tertiary age and are mantled by loess and dune sand. The topography is characterized by northwest-trending sand dunes, which are stabilized by grass cover. The valley floor upstream from Dunning is generally about half a mile wide, is about 80 feet lower than the uplands, and is composed of sand that was mostly stream deposited. The channel is defined by low banks. Bank erosion is prevalent and is the source of most of the sediment load. The flow originates mostly from ground-water accretion and varies between about 200 and 600 cfs (cubic feet per second). Measured suspended-sediment loads vary from about 200 to 2,000 tons per day, of which about 20 percent is finer than 0.062 millimeter and 100 percent is finer than 0.50 millimeter. Total sediment discharges vary from about 500 to 3,500 tons per day, of which about 10 percent is finer than 0.062 millimeter, about 90 percent is finer than 0.50 millimeter, and about 98 percent is finer than 2.0 millimeters. The measured suspended-sediment discharge in the reach near Dunning averages about one-half of the total sediment discharge as measured at the turbulence flume. \r\n\r\nThis report contains information collected during the period October 1, 1948, to September 30, 1952. The information includes sediment discharges; particle-size analyses of total load, of measured suspended sediment, and of bed material; water discharges and other hydraulic data for the turbulence flume and the selected sections. \r\n\r\nSediment discharges have been computed with several different formulas, and insofar as possible, each computed load has been compared with data from the turbulence flume. Sediment discharges computed with the Einstein procedure did not agree well, in general, with comparable measured loads. However, a satisfactory representative cross section for the reach could not be determined with the cross sections that were selected for this investigation. If the computed cross section was narrower and deeper than a representative cross section for the reach, computed loads were high; and if the computed cross section was wider and shallower than a representative cross section for the reach, computed loads were low. Total sediment discharges computed with the modified Einstein procedure compared very well with the loads of individual size ranges and the measured total loads at the turbulence flume. Sediment discharges computed with the Straub equation averaged about twice the measured total sediment discharge at the turbulence flume. Bed-load discharges computed with the Kalinske equation were of about the right magnitude; however, high computed loads were associated with low total loads, low unmeasured loads, and low concentrations of measured suspended sediment coarser than 0.125 millimeter. Bed-load discharges computed with the Schoklitsch equation seemed somewhat high; about one-third of the computed loads were slightly higher than comparable unmeasured loads. Although, in general, high computed discharges with the Schoklitsch equation were associated with high measured total loads, high unmeasured loads, and high concentrations of measured suspended sediment coarser than 0.125 millimeter, the trend was not consistent. Bed-load discharges computed ","language":"ENGLISH","publisher":"Geological Survey (U.S.)","doi":"10.3133/wsp1476","collaboration":"Prepared in cooperation with the U.S. Bureau of Reclamation as part of a program of the Department of the Interior \r\nfor development of the Missouri River basin","usgsCitation":"Hubbell, D.W., and Matejka, D.Q., 1959, Investigations of Sediment Transportation, Middle Loup River at Dunning, Nebraska: With Application of Data from Turbulence Flume: U.S. Geological Survey Water Supply Paper 1476, vi, 123 p., https://doi.org/10.3133/wsp1476.","productDescription":"vi, 123 p.","costCenters":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":138428,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1476/report-thumb.jpg"},{"id":27279,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1476/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":247069,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1476/plate-06.pdf","size":"869","linkFileType":{"id":1,"text":"pdf"}},{"id":247070,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1476/plate-07.pdf","size":"1038","linkFileType":{"id":1,"text":"pdf"}},{"id":247071,"rank":410,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1476/plate-08.pdf","size":"2110","linkFileType":{"id":1,"text":"pdf"}},{"id":247072,"rank":411,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1476/plate-09.pdf","size":"4117","linkFileType":{"id":1,"text":"pdf"}},{"id":247073,"rank":412,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1476/plate-10.pdf","size":"4227","linkFileType":{"id":1,"text":"pdf"}},{"id":247074,"rank":413,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1476/plate-11.pdf","size":"3435","linkFileType":{"id":1,"text":"pdf"}},{"id":247075,"rank":414,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1476/plate-12.pdf","size":"1509","linkFileType":{"id":1,"text":"pdf"}},{"id":247076,"rank":415,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1476/plate-13.pdf","size":"3463","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afde4b07f02db696b8a","contributors":{"authors":[{"text":"Hubbell, David Wellington","contributorId":88330,"corporation":false,"usgs":true,"family":"Hubbell","given":"David","email":"","middleInitial":"Wellington","affiliations":[],"preferred":false,"id":144418,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Matejka, Donald Quintin","contributorId":103658,"corporation":false,"usgs":true,"family":"Matejka","given":"Donald","email":"","middleInitial":"Quintin","affiliations":[],"preferred":false,"id":144419,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2917,"text":"wsp1308 - 1959 - Compilation of records of surface waters of the United States through September 1950: Part 5. Hudson Bay and Upper Mississippi River Basins","interactions":[],"lastModifiedDate":"2022-01-06T20:41:59.615126","indexId":"wsp1308","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","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":"1308","title":"Compilation of records of surface waters of the United States through September 1950: Part 5. Hudson Bay and Upper Mississippi River Basins","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1308","usgsCitation":"Wells, J.V., 1959, Compilation of records of surface waters of the United States through September 1950: Part 5. Hudson Bay and Upper Mississippi River Basins: U.S. Geological Survey Water Supply Paper 1308, 708 p., https://doi.org/10.3133/wsp1308.","productDescription":"708 p.","costCenters":[],"links":[{"id":29619,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1308/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":139199,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1308/report-thumb.jpg"},{"id":393980,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24310.htm"}],"country":"United States","state":"Illinois, Iowa, Minnesota, Wisconsin","otherGeospatial":"Upper Mississippi River basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -96.767578125,\n 40.3130432088809\n ],\n [\n -88.505859375,\n 40.3130432088809\n ],\n [\n -88.505859375,\n 47.931066347509784\n ],\n [\n -96.767578125,\n 47.931066347509784\n ],\n [\n -96.767578125,\n 40.3130432088809\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1de4b07f02db6a99b7","contributors":{"authors":[{"text":"Wells, J. 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It combines in one curve the flow characteristics of a stream throughout the range of discharge, without regard to the sequence of occurrence. If the period upon which the curve is based represents the long-term flow of a stream, the curve may be used to predict the distribution of future flows for water- power, water-supply, and pollution studies. \r\n\r\nThis report shows that differences in geology affect the low-flow ends of flow-duration curves of streams in adjacent basins. Thus, duration curves are useful in appraising the geologic characteristics of drainage basins. \r\n\r\nA method for adjusting flow-duration curves of short periods to represent long-term conditions is presented. The adjustment is made by correlating the records of a short-term station with those of a long-term station.","language":"ENGLISH","publisher":"U.S. Govt. Print. 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