{"pageNumber":"157","pageRowStart":"3900","pageSize":"25","recordCount":4111,"records":[{"id":15295,"text":"ofr71222 - 1971 - Selected fluvial monazite deposits in the southeastern United States","interactions":[],"lastModifiedDate":"2012-02-02T00:06:47","indexId":"ofr71222","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1971","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":"71-222","title":"Selected fluvial monazite deposits in the southeastern United States","docAbstract":"Farther southwest in Georgia, around Griffin and Zebullon, along streams tributary to the Flint River in the monazite belt the flood plains are generally small and discontinuous, and only about 1 percent of the sediment is gravel. The area between Griffin, Zebullon, and the Flint River is underlain by biotite schist and biotite gneiss into which biotite granite has been intruded. Only along one stream, Flat Creek, which drains monazite-bearing granite near Zetella, Ga., are the tenors in monazite even moderately high, but a combination of thick, clayey overburden and discontinuous flood plains make the stream unsuitable for placer mining. Elsewhere in the Flint River area the heavy-mineral concentrates contain less than 1 percent monazite. \r\n\r\nThe southwesternmost area in which reconnaissance of the monazite belt was conducted includes a groups of southwest-flowing tributaries to the Chattahoochee River north of Pine Mountain and near La Grange, Ga. A combination of three characteristics of the alluvium make the area unfavorable for mining: (1) the upper half of the sedimentary sequence is clay and silt, (2) there is scant gravel, and (3) much of the sand is fine grained. Monazite is associated with the Snelson Granite, schists, and gneisses north of the Towaliga fault, but even in this area the tenor of most riffle sediments is only 0.1 to 0.5 pound of monazite per cubic yard, and the average tenor of the alluvium is about 0.2 pound per cubic Yard. Rocks south of the Towaliga fault contain scant monazite. The monazite-bearing area in the drainage basin of the Chattahoochee River has no monazite placers.\r\n\r\nEvidence from the areas on the Flint and Chattahoochee Rivers shows that streams in western Georgia are a much poorer source of monazite than streams farther to the northeast in Georgia, South Carolina, and North Carolina. Also, the northeastern part of the belt in the drainage basins of the Yadkin and Dan Rivers is a poorer source for monazite than the area between the Savannah and Catawba Rivers, S.C.-N.C. \r\n\r\nMonazite-bearing crystalline rocks in the western belt contain about 0.06 pound of monazite per cubic yard. Residual soil derived from the crystalline rocks contains about 0.3 to 0.4 pound of monazite per cubic yard, and colluvial sediments formed by sheet-wash from saprolite, residual soil, and, rarely, old stream deposits, have an average of 3.1 pounds of monazite to the cubic yard. The data on the tenors of residual and colluvial deposits are far less comprehensive than those an the quantity of monazite in the crystalline rocks, but the tenors are probably of the correct order of magnitude. Neither the crystalline rocks nor the residual soils are ores of monazite. Because the colluvial deposits are thin and have patch distribution they could not be mined independently, but some colluvium could be stripped from the adjoining hills in conjunction with the mining of alluvial deposits in the valleys. \r\n\r\nIt is most unlikely that alluvial monazite placers have formed in the trunk streams leading southeastward out of the monazite belt. Churn drilling on the Broad and North Tyger Rivers, South Carolina, at the east edge of the belt has shown that the bulk of the alluvium is fine-grained sediment that contains 0.2 to 0.4 pound of monazite per cubic yard--tenors that represent no considerable enrichment over those in the crystalline rocks and residual soils. The probable persistence of predominantly fine-grained alluvium downstream to the Coastal Plain and the certain dilution of monazite-bearing concentrates by the inflow of monazite-free suites of heavy minerals between the belt and the fall line suggest that the trunk streams east of the belt are the least favorable sources for alluvial monazite in the Piedmont?","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/ofr71222","usgsCitation":"Overstreet, W.C., White, A.M., Theobald, P., and Caldwell, D.W., 1971, Selected fluvial monazite deposits in the southeastern United States: U.S. Geological Survey Open-File Report 71-222, iv, 108 leaves :4 folded maps ;27 cm., https://doi.org/10.3133/ofr71222.","productDescription":"iv, 108 leaves :4 folded maps ;27 cm.","costCenters":[],"links":[{"id":146455,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1971/0222/report-thumb.jpg"},{"id":44219,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1971/0222/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":44220,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1971/0222/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":44221,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1971/0222/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":44222,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1971/0222/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":44223,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1971/0222/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a08e4b07f02db5fa31c","contributors":{"authors":[{"text":"Overstreet, William C.","contributorId":73586,"corporation":false,"usgs":true,"family":"Overstreet","given":"William","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":170908,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"White, A. M.","contributorId":86778,"corporation":false,"usgs":true,"family":"White","given":"A.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":170909,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Theobald, P. K.","contributorId":45293,"corporation":false,"usgs":true,"family":"Theobald","given":"P. K.","affiliations":[],"preferred":false,"id":170907,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Caldwell, D. W.","contributorId":27461,"corporation":false,"usgs":true,"family":"Caldwell","given":"D.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":170906,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}}
,{"id":70207469,"text":"70207469 - 1971 - Interstitial water studies on small core samples, deep sea drilling Project, leg 7","interactions":[],"lastModifiedDate":"2019-12-19T17:23:27","indexId":"70207469","displayToPublicDate":"1971-12-31T17:19:02","publicationYear":"1971","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1997,"text":"Initial reports of the Deep Sea Drilling Project","active":true,"publicationSubtype":{"id":10}},"title":"Interstitial water studies on small core samples, deep sea drilling Project, leg 7","docAbstract":"<p>The sediments cored on Leg 7 are predominantly deep sea biogenic oozes and chalks; only rarely were significant quantities of pelagic clays and volcanic detritus encountered. The biogenic sections include both siliceous and calcareous deposits. At three sites the drilling terminated in basalt, one of which (Site 62) is interpreted as being intrusive on the basis of intense alteration of the overlying sediment. With the exception of Ca++ and Sr , compositional changes in the pore waters are characteristically small relative to those reported previously for rapidly deposited, non-biogenic sediments. Ca++ and Sr + , however, exhibit concentrations of up to three times and ten times, respectively, those found in sea water. In several instances, constant concentration gradients as a function of depth have been found. </p><p>The sampling, storage and analytical procedures employed have been briefly described in an earlier report (Sayles et al, 1970) and are detailed in a manuscript in preparation (Manheim and Chan). Sodium has been calculated as the difference between the summation of the anions and the summation of the major cations exclusive of sodium; to date, this method has proven more accurate than direct analytical methods. Agreement between the two types of silica determination used (emission spectrometric and colorimetric) is poor; the values obtained by emission spectrometry are characteristically higher. The colorimetric technique measures only \"reactive\" silica (monomeric and possibly dimeric) while the emission spectrometric technique will determine all of the silica in solution and in suspension. The silica content of most of the solutions is high (60 ppm) and polymerization is likely. We are currently investigating this discrepancy. The pH and water content data reported were obtained aboard the Glomar Challenger immediately after sampling</p>","language":"English","publisher":"National Science Foundation","doi":"10.2973/dsdp.proc.7.112.1971","usgsCitation":"Sayles, F., and Manheim, F.T., 1971, Interstitial water studies on small core samples, deep sea drilling Project, leg 7: Initial reports of the Deep Sea Drilling Project, v. 7, p. 871-881, https://doi.org/10.2973/dsdp.proc.7.112.1971.","productDescription":"11 p.","startPage":"871","endPage":"881","costCenters":[{"id":678,"text":"Woods Hole Coastal and Marine Science Center","active":true,"usgs":true}],"links":[{"id":488847,"rank":0,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"http://doi.org/10.2973/dsdp.proc.7.112.1971","text":"Publisher Index Page"},{"id":370528,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"7","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Sayles, F.L.","contributorId":77657,"corporation":false,"usgs":true,"family":"Sayles","given":"F.L.","email":"","affiliations":[],"preferred":false,"id":778168,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Manheim, Frank T. 0000-0003-4005-4524","orcid":"https://orcid.org/0000-0003-4005-4524","contributorId":20770,"corporation":false,"usgs":true,"family":"Manheim","given":"Frank","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":778169,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70227383,"text":"70227383 - 1971 - Sedimentary and gravity-slide emplacement of serpentinite","interactions":[],"lastModifiedDate":"2022-01-12T17:53:30.626953","indexId":"70227383","displayToPublicDate":"1971-04-01T11:30:10","publicationYear":"1971","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":"Sedimentary and gravity-slide emplacement of serpentinite","docAbstract":"<p>Large deposits of serpentinite in alpine-type orogenic areas have been formed by sedimentary processes ranging from the detrital accumulation of bedded serpentinite sandstone and shale to the emplacement of chaotic breccias (olistostromes) and gigantic slide blocks. Known occurrences of sedimentary serpentinite are listed, and eight deposits from the circum-Pacific, Caribbean, and Mediterranean areas are described in detail. Sedimentary serpentinites range in age from early Paleozoic to Quaternary, although most are Cretaceous or Tertiary. Most were deposited in eugeosynclinal environments, early in the geosynclinal cycle. Individual deposits range in thickness from a few centimeters to nearly 3 km, and several extend laterally for tens of kilometers. Graded bedding is common, and many deposits contain marine fossils.</p><p>Serpentinite is the dominant rock constituent, and clasts foreign to the alpine ultramafic assemblage are rare. Chemical analyses often detrital serpentinites show that these rocks contain slightly more silica and alumina than do nondetrital serpentinites, due to contamination by aluminosilicate minerals and quartz during deposition. This and nine other criteria are potentially useful in the recognition of sedimentary serpentinites.</p><p>Several features suggest that most sedimentary serpentinites were deposited very rapidly by submarine landslides, mudflows, or turbidity currents. The sources of this serpentinite debris are postulated to be upward-migrating serpentinite protrusions which penetrate the seafloor or Earth's surface upslope from eventual depositional sites.</p><p>Sedimentary serpentinites are much more abundant in alpine-type orogenic areas than is commonly thought, and many ultramafic masses presently regarded as igneous intrusions or tectonic protrusions may in fact be coeval with, instead of younger than, their enclosing sedimentary or metasedimentary rocks. In eugeosynclinal sequences such as the Franciscan Formation, some elongate bodies now regarded as serpentinite sills may be beds of ultramafic detritus whose sedimentary features have been masked by post-depositional shearing; isolated masses may be exotic slide blocks. A sedimentary origin can explain some of the most persistent and perplexing characteristics of many alpine serpentinites: their conformity with enclosing sedimentary rocks, their grossly planar shapes, and the absence of metamorphism along their contacts.</p>","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1971)82[919:SAGEOS]2.0.CO;2","usgsCitation":"Lockwood, J.P., 1971, Sedimentary and gravity-slide emplacement of serpentinite: Bulletin of the Geological Society of America, v. 82, no. 4, p. 919-936, https://doi.org/10.1130/0016-7606(1971)82[919:SAGEOS]2.0.CO;2.","productDescription":"18 p.","startPage":"919","endPage":"936","costCenters":[],"links":[{"id":394249,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Colombia, Cuba, Italy, Russia, United States","state":"California","otherGeospatial":"Apennine Mountains, Coast Ranges, Guajira Peninsula, Oriente, Penzhinskaya 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P.","contributorId":104473,"corporation":false,"usgs":true,"family":"Lockwood","given":"J.","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":830718,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":1000081,"text":"1000081 - 1971 - Albinism in lampreys in the upper Great Lakes","interactions":[],"lastModifiedDate":"2013-02-04T14:14:48","indexId":"1000081","displayToPublicDate":"1971-01-01T00:00:00","publicationYear":"1971","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1337,"text":"Copeia","active":true,"publicationSubtype":{"id":10}},"title":"Albinism in lampreys in the upper Great Lakes","docAbstract":"Albinism in fishes is relatively rare except in some stocks of hatchery-reared salmonids. In the Petromyzonidae, only four albino lampreys have been reported.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Copeia","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","doi":"10.2307/1441626","usgsCitation":"Braem, R.A., and King, E.L., 1971, Albinism in lampreys in the upper Great Lakes: Copeia, v. 1971, no. 1, p. 176-179, https://doi.org/10.2307/1441626.","productDescription":"4 p.","startPage":"176","endPage":"179","numberOfPages":"4","costCenters":[{"id":324,"text":"Great Lakes Science Center","active":true,"usgs":true}],"links":[{"id":128767,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":266953,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.2307/1441626"}],"volume":"1971","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae0e4b07f02db688203","contributors":{"authors":[{"text":"Braem, Robert A.","contributorId":34858,"corporation":false,"usgs":true,"family":"Braem","given":"Robert","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":308048,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"King, Everett L.","contributorId":54922,"corporation":false,"usgs":true,"family":"King","given":"Everett","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":308049,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":5221247,"text":"5221247 - 1970 - Organochlorine pesticide residues in whooping cranes and Everglade kites","interactions":[],"lastModifiedDate":"2017-06-07T12:57:44","indexId":"5221247","displayToPublicDate":"2010-06-16T12:18:01","publicationYear":"1970","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3544,"text":"The Auk","onlineIssn":"1938-4254","printIssn":"0004-8038","active":true,"publicationSubtype":{"id":10}},"title":"Organochlorine pesticide residues in whooping cranes and Everglade kites","docAbstract":"<p>Three Whooping Cranes (<i>Grus americana</i>), two Everglade Kites (<i>Rostrhamus sociabilis</i>), and one kite egg were analyzed for pesticide residues at this laboratory. This is the first time that specimens from this rare population from the wild have ever been analyzed, and the results are herein reported. </p>","language":"English","publisher":"American Ornithological Society","doi":"10.2307/4083669","usgsCitation":"Lamont, T., and Reichel, W.L., 1970, Organochlorine pesticide residues in whooping cranes and Everglade kites: The Auk, v. 87, no. 1, p. 158-159, https://doi.org/10.2307/4083669.","productDescription":"2 p.","startPage":"158","endPage":"159","costCenters":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":480286,"rank":1,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.2307/4083669","text":"Publisher Index Page"},{"id":197183,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"87","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae5e4b07f02db68a887","contributors":{"authors":[{"text":"Lamont, Thair","contributorId":56321,"corporation":false,"usgs":true,"family":"Lamont","given":"Thair","email":"","affiliations":[],"preferred":false,"id":333394,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Reichel, William L.","contributorId":62707,"corporation":false,"usgs":false,"family":"Reichel","given":"William","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":333395,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":14926,"text":"ofr70208 - 1970 - Economic geology of the Zipaquira quadrangle and adjoining area, Department of Cundinamarca, Colombia","interactions":[],"lastModifiedDate":"2012-02-02T00:06:47","indexId":"ofr70208","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1970","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"70-208","title":"Economic geology of the Zipaquira quadrangle and adjoining area, Department of Cundinamarca, Colombia","docAbstract":"At least four evaporite sequences are interbedded with Cretaceous strata in the Bogotga area of the Cordillera Oriental of Colombia. The easternmost and oldest evaporite interval is of probable Berriasian-Valanglnian age; the next oldest is of probable late Barremian-early Aptian age, and is followed by a possible late Aptian sequence. The westernmost and best known sequence is Turonian-early Coniacian in age, in the Sabana de Bogota. This youngest sequence contains the thickest known salt deposits and is probably the most widespread geographically. \r\n\r\nThree gypsum deposits of probable Barremian-Valanginian age are in the eastern part of the area under investigation. These deposits may have been leached from former salt accumulations. No other evaporites are exposed, but numerous brine springs are known, That the sources of these brines are neither deep not distant is suggested by the generally high concentrations, of the brines, the local presence of rute (leached salt residue), and the commonly significant amounts of H2S gas emitted at these springs. \r\n\r\nThe rock salt exposed in three accessible mines commonly has a characteristic lamination caused by alternating layers of relatively pure halite and very argillaceous halite. Ubiquitously scattered throughout all salt deposits are small clasts of black, commonly pyritic, marly claystone. This lithology is also present as large claystone bodies conformably interbedded in the salt strata. Anhydrite is rare and is apparently more abundant at the Zipaquira mine that at the Nemocon and Upin mine. \r\n\r\nPaleontologic evidence in the Sabana de Bogota demonstrates that the salt-claystone series, hematite impregnated strata, and carbonaceous to locally coaly claystone are coeval. The salt-claystone facies may have been deposited in shallow evaporite pans that were separated within the overall evaporite interval by barriers on which the locally hematitic strata were deposited. The carbonaceous facies may also have formed in barrier areas or on the edges of the evaporite basins. Whether or not this facies relationship prevails in the older evaporite intervals is not known; meager evidence suggests that it does. \r\n\r\nNonmetallic mineral resources other than the evaporite minerals are phosphate rock, limestone, kaolinite, and emeralds. Metallic mineral deposits present in the Zone include hematite at Pericos, La Caldera, Tibirita, Nueva Vizcaya, and Cerro de Montecristo; chalcopyrite at Cerro do Cobre and at Farallones de Medina; galena in several places along the Rio Farallones and Rio Gacheta; and spahlerite in the Junin district.","language":"ENGLISH","publisher":"U.S. Geological Survey],","doi":"10.3133/ofr70208","usgsCitation":"McLaughlin, D.H., and Arce Herrera, M., 1970, Economic geology of the Zipaquira quadrangle and adjoining area, Department of Cundinamarca, Colombia: U.S. Geological Survey Open-File Report 70-208, 125 p. ill., maps (some col.) ;27 cm., https://doi.org/10.3133/ofr70208.","productDescription":"125 p. ill., maps (some col.) ;27 cm.","costCenters":[],"links":[{"id":146298,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1970/0208/report-thumb.jpg"},{"id":43739,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1970/0208/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43740,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1970/0208/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43741,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1970/0208/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43742,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1970/0208/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43743,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1970/0208/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43744,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1970/0208/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43745,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1970/0208/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43746,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1970/0208/plate-8.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43747,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1970/0208/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adce4b07f02db6867ae","contributors":{"authors":[{"text":"McLaughlin, Donald H. Jr.","contributorId":73215,"corporation":false,"usgs":true,"family":"McLaughlin","given":"Donald","suffix":"Jr.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":170261,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Arce Herrera, Marino","contributorId":76756,"corporation":false,"usgs":true,"family":"Arce Herrera","given":"Marino","email":"","affiliations":[],"preferred":false,"id":170262,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":20131,"text":"ofr71210 - 1970 - Petrology of the Plutonic Rocks of west-central Alaska","interactions":[],"lastModifiedDate":"2012-02-02T00:07:42","indexId":"ofr71210","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1970","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":"71-210","title":"Petrology of the Plutonic Rocks of west-central Alaska","docAbstract":"A series of plutons in west-central Alaska defines the Hogatza plutonic belt which extends for about 200 miles in an east-west direction from the northeastern Seward Peninsula to the Koyukuk River. The plutonic rocks have an aggregate area of about 1,200 square miles and their composition, distribution, and possible petrogenesis are discussed for the first time in this report. \r\n\r\nField, petrographic and chemical data supported by K/Ar age dating indicate the plutonic rocks are divisible into two suites differing in age, location, and composition. The western plutons are mid-Cretaceous (~100 m.y.) in age and consist of a heterogeneous assemblage of monzonite, syenite, quartz monzonite. Associated with these granitic rocks is a group of alkaline sub-silicic rocks that forma belt of intrusive complexes extending for a distance of at least 180 miles from west-central Alaska to the Bering Sea. The complex at Granite Mountain shows a rare example of zoning from an alkaline rim to a quartz-bearing core. The occurrence of a similar complex at Cape Dezhnev on the easternmost tip of Siberia suggests the alkaline province may extend into Siberia. The easternmost plutons are Late Cretaceous (180 m.y.) in age and composed primarily of granodiorite and quartz monzonite similar to calc-alkaline plutons found throughout the North America Cordillera.\r\n\r\nThe plutons are epizonal and intrude deformed but unmetamorphosed Lower Cretaceous andesitic volcanics and volcanic graywacke which constitute the highly mobile Yukon-Koyukuk volcanogenic province of west-central Alaska. No older rocks have been found within the confines of this vast tract; the occurrence of a bounding ophiolite sequence has lead to the suggestion that the province was formed by large-scale rifting and is underlain by oceanic crust. \r\n\r\nThe possibility of no juvenile sialic crust over much of the area suggests that the potassium-rich magma now represented by the alkaline rocks originated in the mantle. The distribution of the alkaline rocks appears to be related to regional structural features, particularly the boundary between the Mesozoic volcanogenic province of west-central Alaska and the thrust-faulted province of metamorphic-plutonic and sedimentary rocks of Paleozoic and Precambrian age that forms the eastern Seward Peninsula. This boundary may have been a zone of structural weakness along which alkaline magma was generated. Modal and chemical trends suggest that the potassium-rich magma influenced the composition of more granitic magmas forming at higher levels. The latter may have been forming as a result of anatexis of andesite and mixing of mantle-derived mafic magma. The result is the heterogeneous assemblage of generally potassium-rich plutonic rocks that forms the west end of the Hogataza plutonic belt.\r\n\r\nThe loci of magmatism in west-central Alaska shifted east in Late Cretaceous time and the eastern plutons show only local signs of potassium enrichment. They are compositionally homogeneous and differences within plutons appear due to local contamination.","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/ofr71210","usgsCitation":"Miller, T.P., 1970, Petrology of the Plutonic Rocks of west-central Alaska: U.S. Geological Survey Open-File Report 71-210, xi, 132, [2] leaves :ill., maps ;27 cm.; 136 p., https://doi.org/10.3133/ofr71210.","productDescription":"xi, 132, [2] leaves :ill., maps ;27 cm.; 136 p.","costCenters":[],"links":[{"id":106510,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_8615.htm","linkFileType":{"id":5,"text":"html"},"description":"8615"},{"id":153233,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1971/0210/report-thumb.jpg"},{"id":49672,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1971/0210/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":49673,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1971/0210/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":49674,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1971/0210/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":49675,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1971/0210/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adce4b07f02db68668e","contributors":{"authors":[{"text":"Miller, Thomas P. tmiller@usgs.gov","contributorId":4183,"corporation":false,"usgs":true,"family":"Miller","given":"Thomas","email":"tmiller@usgs.gov","middleInitial":"P.","affiliations":[{"id":121,"text":"Alaska Volcano Observatory","active":false,"usgs":true}],"preferred":false,"id":182117,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":34913,"text":"b1312N - 1970 - Some rare-element mineral deposits in mainland China","interactions":[],"lastModifiedDate":"2012-02-02T00:09:29","indexId":"b1312N","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1970","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":"1312","chapter":"N","title":"Some rare-element mineral deposits in mainland China","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/b1312N","usgsCitation":"Lee, K.Y., 1970, Some rare-element mineral deposits in mainland China: U.S. Geological Survey Bulletin 1312, 34 p, https://doi.org/10.3133/b1312N.","productDescription":"34 p","costCenters":[],"links":[{"id":96707,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1312n/report.pdf","size":"2742","linkFileType":{"id":1,"text":"pdf"}},{"id":166258,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1312n/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e7e4b07f02db5e8254","contributors":{"authors":[{"text":"Lee, K. Y.","contributorId":74351,"corporation":false,"usgs":true,"family":"Lee","given":"K.","email":"","middleInitial":"Y.","affiliations":[],"preferred":false,"id":213798,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":61976,"text":"mr56 - 1970 - Uranium, thorium, and rare-earth elements in Alaska","interactions":[],"lastModifiedDate":"2025-05-13T13:38:52.557702","indexId":"mr56","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1970","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":324,"text":"Mineral Investigations Resource Map","code":"MR","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"56","title":"Uranium, thorium, and rare-earth elements in Alaska","docAbstract":"<p>No abstract available.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/mr56","usgsCitation":"Cobb, E.H., 1970, Uranium, thorium, and rare-earth elements in Alaska: U.S. Geological Survey Mineral Investigations Resource Map 56, Report: 3 p.; 1 Plate: 49.00 x 37.00 inches, https://doi.org/10.3133/mr56.","productDescription":"Report: 3 p.; 1 Plate: 49.00 x 37.00 inches","costCenters":[],"links":[{"id":485794,"rank":4,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/mr/56/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":485630,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_1786.htm","linkFileType":{"id":5,"text":"html"}},{"id":260431,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mr/56/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":179995,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/mr/56/report-thumb.jpg"}],"scale":"2500000","country":"United States","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -168.25,52.25 ], [ -168.25,70.11749999999999 ], [ -129.5,70.11749999999999 ], [ -129.5,52.25 ], [ -168.25,52.25 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a18e4b07f02db60534f","contributors":{"authors":[{"text":"Cobb, Edward Huntington","contributorId":13629,"corporation":false,"usgs":true,"family":"Cobb","given":"Edward","email":"","middleInitial":"Huntington","affiliations":[],"preferred":false,"id":266641,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":68319,"text":"ha333 - 1970 - Reconnaissance of the Pigeon River, a cold-water river in the northcentral part of Michigan's southern peninsula","interactions":[],"lastModifiedDate":"2021-10-21T15:12:36.579623","indexId":"ha333","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1970","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":318,"text":"Hydrologic Atlas","code":"HA","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"333","title":"Reconnaissance of the Pigeon River, a cold-water river in the northcentral part of Michigan's southern peninsula","docAbstract":"<p>The cold-water streams of the northern states provide unique recreational values to the American people (wilderness or semi-wilderness atmosphere, fast-water canoeing, and trout fishing), but the expanding recreational needs must be balanced against the growing demand of water for public and industrial supplies, for irrigation, and for the dilution of sewage and other wastes. In order to make intelligent decisions regarding use and management of the water resource for recreation and other demands, an analysis of the hydrologic factors related to recreational values is essential.</p><p>The Pigeon River is one of Michigan's outstanding trout streams and is the favorite of a large number of anglers who return year after year. Camping is also popular and is usually, but not always, associated with fishing. Boating is very rare on the Pigeon because of numerous portages around log jams. Cabin-living and resorting are relatively minor on this river as yet, but much of the private river front may be developed in future years.</p><p>The Pigeon is located in the north-central part of the southern peninsula of Michigan (see index map). Headwaters are a few miles northeast of Gaylord, and the mouth is at Mullet Lake, a few miles northeast of Indian River. Interstate Highway 75 roughly parallels the river about 5 to 10 miles to the west. Exits from this highway at Gaylord, Vanderbilt, Wolverine, and Indian River, provide easy access to the Pigeon.</p><p>The recreational value of the river depends on the streamflow characteristics, quality of water, and character of stream channel, and bed and banks. The purpose of this atlas is to describe these characteristics, and to show how they relate to recreational uses.</p><p>Most of the information presented here was obtained from a field reconnaissance in June, 1966, and from basic records of the U.S. Geological Survey's Water Resources Division. The area of field study is limited to the channel, bed, and banks of the main stem of the Pigeon from source to mouth. The study was made in cooperation with the Michigan Geological Survey, Gerald E. Eddy, Chief. Advice and assistance were also obtained from other sections of the Michigan Conservation Department.</p><p>Sheet 1 of this atlas presents information on streamflow characteristics and water quality. Sheet 2 describes the physical characteristics of the stream channel, and bed and banks, and shows how these physical characteristics relate to streamflow, water quality, and recreational use.</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/ha333","usgsCitation":"Hendrickson, G.E., and Doonan, C.J., 1970, Reconnaissance of the Pigeon River, a cold-water river in the northcentral part of Michigan's southern peninsula: U.S. Geological Survey Hydrologic Atlas 333, 5 Plates: 30.5 x 40.0 inches or smaller, https://doi.org/10.3133/ha333.","productDescription":"5 Plates: 30.5 x 40.0 inches or smaller","costCenters":[{"id":382,"text":"Michigan Water Science Center","active":true,"usgs":true}],"links":[{"id":185889,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ha333.JPG"},{"id":89776,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/ha/333/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":390726,"rank":7,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_15708.htm"},{"id":89775,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/ha/333/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":89774,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/ha/333/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":89773,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/ha/333/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":89772,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/ha/333/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"62500","country":"United States","state":"Michigan","otherGeospatial":"Pigeon River","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -84.61666666666666,45.03333333333333 ], [ -84.61666666666666,45.43333333333333 ], [ -84.41666666666667,45.43333333333333 ], [ -84.41666666666667,45.03333333333333 ], [ -84.61666666666666,45.03333333333333 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a68e4b07f02db63afc9","contributors":{"authors":[{"text":"Hendrickson, G. E.","contributorId":99958,"corporation":false,"usgs":true,"family":"Hendrickson","given":"G.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":278021,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Doonan, C. J.","contributorId":62592,"corporation":false,"usgs":true,"family":"Doonan","given":"C.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":278020,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":13422,"text":"ofr70115 - 1970 - Seismic activity in the Sunnyside mining district, Carbon and Emery Counties, Utah, during 1968","interactions":[],"lastModifiedDate":"2012-02-02T00:06:50","indexId":"ofr70115","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1970","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"70-115","title":"Seismic activity in the Sunnyside mining district, Carbon and Emery Counties, Utah, during 1968","docAbstract":"More than 20,000 local earth tremors were recorded by the seismic monitoring network in the Sunnyside mining district during 1968. This is about 40 percent of the number of tremors recorded by the network in 1967. In 1968 a total of 281 tremors were of sufficient magnitude to be located accurately--about 50 percent of the number of tremors in 1967 that were located accurately. \r\n\r\nAs in previous years, nearly all the earth tremors originated near, or within a few thousand feet of, the mine workings. This distribution indicates that mine-induced stress changes caused most of the seismic activity. However, over periods of weeks and months there were significant changes in the distribution of seismic activity caused by tremors that were not directly related to mining but probably were caused by adjustment of natural stresses 6r by a complex combination of both natural and mine-induced stress changes. \r\n\r\nIn 1968 the distribution of tremor hypocenters varied considerably with time, relative to active mining areas and to faults present in the mine workings. During the first 6 months, most tremors originated along or near faults that trend close to or through the active mine workings. However, in the last 6 months, the tremor hypocenters tended to concentrate in the rock mass closer to, or around, the active mining areas. This shift in concentration of seismic activity with time has been noted throughout the district many times since recording began in 1963, and is apparently caused by spontaneous releases of stored strain energy resulting from mine-induced stress changes. These spontaneous releases of strain energy, together with rock creep, apparently are the mechanism of adjustment within the rock mass toward equilibrium conditions, which are continually disrupted by mining. \r\n\r\nAlthough potentially hazardous bumps were rare in the Sunnyside mining district during 1968, smaller bumps and rock falls were more common in a given active mining area whenever hypocenters of larger-magnitude earth tremors concentrated near it.","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/ofr70115","usgsCitation":"Dunrud, C., Maberry, J.O., and Hernandez, J.H., 1970, Seismic activity in the Sunnyside mining district, Carbon and Emery Counties, Utah, during 1968: U.S. Geological Survey Open-File Report 70-115, 27 p. ill., 4 col. maps ;29 cm., https://doi.org/10.3133/ofr70115.","productDescription":"27 p. ill., 4 col. maps ;29 cm.","costCenters":[],"links":[{"id":106460,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_8465.htm","linkFileType":{"id":5,"text":"html"},"description":"8465"},{"id":146155,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1970/0115/report-thumb.jpg"},{"id":41856,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1970/0115/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41857,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1970/0115/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41858,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1970/0115/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41859,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1970/0115/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41860,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1970/0115/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"24000","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9ce4b07f02db65e78a","contributors":{"authors":[{"text":"Dunrud, C. Richard","contributorId":48964,"corporation":false,"usgs":true,"family":"Dunrud","given":"C. Richard","affiliations":[],"preferred":false,"id":167783,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Maberry, John O.","contributorId":87134,"corporation":false,"usgs":true,"family":"Maberry","given":"John","email":"","middleInitial":"O.","affiliations":[],"preferred":false,"id":167784,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hernandez, Jerome H.","contributorId":16839,"corporation":false,"usgs":true,"family":"Hernandez","given":"Jerome","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":167782,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":70226542,"text":"70226542 - 1970 - Boulder Creek batholith, Colorado part I: Allanite and its bearing upon age patterns","interactions":[],"lastModifiedDate":"2021-11-23T15:36:47.311412","indexId":"70226542","displayToPublicDate":"1970-07-01T09:12:52","publicationYear":"1970","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":"Boulder Creek batholith, Colorado part I: Allanite and its bearing upon age patterns","docAbstract":"<p>Allanite is abundant and commonly attains unusually large size as a late-replacement mineral in: (1) the comagnatic rocks of the Precambrian Boulder Creek batholith; (2) associated amphibolite xenoliths and related hybrid rocks; and (3) distinctly younger intrusions of Silver Plume Granite that cut the complex. Allanite porphyroblasts develop by replacement of biotite, probably in the presence of emanations from the rare earth-rich and thorium-rich Silver Plume Granite. The largest allanite crystals are made up of nearly isotropic (metamict) cores and birefringent (recrystallized) rims. Smaller crystals are made up exclusively of birefringent material. The maximum birefringence is shown to be that expectable in allanite of Late Cretaceous to early Tertiary age. As plotted on maps, the birefringence increases, and the thorium and uranium contents of the allanite decrease toward a Laramide stock. The variation in birefringence is, therefore, largely relatable to variations in the post-Laramide radiation dosage brought about by differences in the amounts of uranium and thorium lost during recrystallization. The recrystallized allanite is itself partly replaced by epidote which characteristically occurs as a border between allanite and biotite.</p><p>Total rare-earth oxides for the eight samples of allanite analyzed range from 17.5 to 21.3 percent by weight. In 13 samples, thorium ranged from 0.50 to 1.14 percent by weight, and uranium from 54 to 158 parts pparts per million. Ranges in optical measurements for 20 samples using the spindle stage are: Nα = 1.719–1.759, Nβ = 1.731-1.774, N<sub>γ</sub><span>&nbsp;</span>= 1.741–1.784, birefringence = 0.020–0.032, 2V<sub>X</sub><span>&nbsp;</span>(calc.) 70°–84°. Ranges for unit-cell data obtained on 8 samples are: a = 8.948–8.985Å, b = 5.721-5.763Å, c = 10.184–10.240Å, β = 115°7.50′–115°25.89′ and volume = 473.02–478.43Å<span>&nbsp;</span><sup>3</sup>. The average value for the ratio a:b:c = 1.561:1:1.778.</p>","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1970)81[1973:BCBCPI]2.0.CO;2","usgsCitation":"Hickling, N.L., Phair, G., Moore, R., and Rose, H.J., 1970, Boulder Creek batholith, Colorado part I: Allanite and its bearing upon age patterns: Bulletin of the Geological Society of America, v. 81, no. 7, p. 1973-1993, https://doi.org/10.1130/0016-7606(1970)81[1973:BCBCPI]2.0.CO;2.","productDescription":"21p.","startPage":"1973","endPage":"1993","costCenters":[],"links":[{"id":392049,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Colorado","otherGeospatial":"Boulder Creek batholith","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -105.96450805664062,\n              39.536880650643056\n            ],\n            [\n              -104.98672485351562,\n              39.536880650643056\n            ],\n            [\n              -104.98672485351562,\n              40.263808598903566\n            ],\n            [\n              -105.96450805664062,\n              40.263808598903566\n            ],\n            [\n              -105.96450805664062,\n              39.536880650643056\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","volume":"81","issue":"7","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Hickling, Nelson L.","contributorId":16456,"corporation":false,"usgs":true,"family":"Hickling","given":"Nelson","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":827291,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Phair, George","contributorId":91512,"corporation":false,"usgs":true,"family":"Phair","given":"George","email":"","affiliations":[],"preferred":false,"id":827292,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Moore, Roosevelt","contributorId":55029,"corporation":false,"usgs":true,"family":"Moore","given":"Roosevelt","email":"","affiliations":[],"preferred":false,"id":827293,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Rose, Harry J. Jr.","contributorId":39013,"corporation":false,"usgs":true,"family":"Rose","given":"Harry","suffix":"Jr.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":827294,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}}
,{"id":1000167,"text":"1000167 - 1970 - A hermaphroditic coregonine from Lake Michigan","interactions":[],"lastModifiedDate":"2013-01-28T11:03:55","indexId":"1000167","displayToPublicDate":"1970-01-01T00:00:00","publicationYear":"1970","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3624,"text":"Transactions of the American Fisheries Society","active":true,"publicationSubtype":{"id":10}},"title":"A hermaphroditic coregonine from Lake Michigan","docAbstract":"Hermaphroditism is relatively rare among the Salmonidae  (See Atz, 1964 for a comprehensive review) and has never been reported for coregonine fishes. Recent examination of a collection of coregonines  at the Great Lakes Fishery Laboratory disclosed a hermaphroditic bloater(<i>Coregonus hoyi</i>). The fish was captured in a gill net set at 50 fathoms on the bottom of Lake Michigan approximately 7.5 miles NNW of Frankfort, Michigan, on November 2, 1955. The fish had a normal rate of growth and was 234 mm long and in its 5th year of life; it was normal in external appearance but was easily identified as a hermaphrodite by gross examination of its gonads","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Transactions of the American Fisheries Society","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisher":"Taylor & Francis","publisherLocation":"London, UK","doi":"10.1577/1548-8659(1970)99<611:AHCFLM>2.0.CO;2","collaboration":"Out-of-print","usgsCitation":"Edsall, T.A., 1970, A hermaphroditic coregonine from Lake Michigan: Transactions of the American Fisheries Society, v. 99, no. 3, https://doi.org/10.1577/1548-8659(1970)99<611:AHCFLM>2.0.CO;2.","productDescription":"611 p.","startPage":"611 p.","costCenters":[{"id":324,"text":"Great Lakes Science Center","active":true,"usgs":true}],"links":[{"id":266599,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1577/1548-8659(1970)99<611:AHCFLM>2.0.CO;2"},{"id":130365,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"99","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b24e4b07f02db6ae48e","contributors":{"authors":[{"text":"Edsall, Thomas A.","contributorId":84302,"corporation":false,"usgs":true,"family":"Edsall","given":"Thomas","email":"","middleInitial":"A.","affiliations":[{"id":324,"text":"Great Lakes Science Center","active":true,"usgs":true}],"preferred":false,"id":308175,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":1000408,"text":"1000408 - 1970 - Effects of alewife predation on zooplankton populations in Lake Michigan","interactions":[],"lastModifiedDate":"2016-03-14T13:51:53","indexId":"1000408","displayToPublicDate":"1970-01-01T00:00:00","publicationYear":"1970","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2620,"text":"Limnology and Oceanography","active":true,"publicationSubtype":{"id":10}},"title":"Effects of alewife predation on zooplankton populations in Lake Michigan","docAbstract":"<p>The zooplankton populations in southeastern Lake Michigan underwent striking, size-related changes between 1954 and 1966. Forms that decline sharply were the largest cladocerans (Leptodora kindtii, Daphnia galeata, and D. retrocurva), the largest calanoid copepods (Limnocalanus macrurus, Epischura lacustris, and Diaptomus sicilis), and the largest cyclopoid copepod (Mesocyclops edax). Two of these, D. galeata and M. edax (both abundant in 1954), became extremely rare. Certain medium-sized or small species increased in numbers: Daphnia longiremis, Holopedium gibberum, Polyphemus pediculus, Bosmina longirostris, Bosmina coregoni, Ceriodaphnia sp., Cyclops bicuspidatus, Cyclops vernalis, and Diaptomus ashlandi. Evidence is strong that the changes were due to selective predation by alewives. The alewife was uncommon in southeastern Lake Michigan in 1954 but had increased to enormous proportions by 1966; there was a massive dieoff in spring 1967, and abundance remained relatively low in 1968. The composition of zooplankton populations in 1968 generally had shifted back toward that of 1954, although D. galeata and M. edax remained rare. The average size, and size at onset of maturity, of D. retrocurva decreased noticeably between 1954 and 1966 but increased between 1966 and 1968.</p>","language":"English","publisher":"Wiley","doi":"10.4319/lo.1970.15.4.0556","usgsCitation":"Wells, L., 1970, Effects of alewife predation on zooplankton populations in Lake Michigan: Limnology and Oceanography, v. 15, no. 4, p. 556-565, https://doi.org/10.4319/lo.1970.15.4.0556.","productDescription":"10 p.","startPage":"556","endPage":"565","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":324,"text":"Great Lakes Science Center","active":true,"usgs":true}],"links":[{"id":480290,"rank":1,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.4319/lo.1970.15.4.0556","text":"Publisher Index Page"},{"id":132983,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"15","issue":"4","noUsgsAuthors":false,"publicationDate":"2003-12-22","publicationStatus":"PW","scienceBaseUri":"4f4e4ad8e4b07f02db684761","contributors":{"authors":[{"text":"Wells, LaRue","contributorId":75476,"corporation":false,"usgs":true,"family":"Wells","given":"LaRue","email":"","affiliations":[],"preferred":false,"id":308520,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70001709,"text":"70001709 - 1969 - Petrological, magnetic and chemical properties of basalt dredged from an abyssal hill in the North-east pacific","interactions":[],"lastModifiedDate":"2020-11-29T17:26:59.159329","indexId":"70001709","displayToPublicDate":"2010-09-28T23:09:25","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2840,"text":"Nature","active":true,"publicationSubtype":{"id":10}},"title":"Petrological, magnetic and chemical properties of basalt dredged from an abyssal hill in the North-east pacific","docAbstract":"<div id=\"Abs1-section\" class=\"c-article-section\"><div id=\"Abs1-content\" class=\"c-article-section__content\"><p>OVER the years, samples of basalt from the oceanic crust have been taken mainly from seamounts, fracture zones and ridge and rise crests<sup>1–6</sup>, and rarely from the vast fields of abyssal hills which cover a large part of the deep-sea floor. The basalt sampled from the deeper regions of the oceanic crust (for example, on fault scarps) is a distinct variety of tholeiitic basalt, while alkali basalt is restricted to the volcanic edifices<sup>4</sup>. Oceanic tholeiitic basalt differs from alkali basalt and continental tholeiite chiefly in having a relatively low percentage of K<sub>2</sub>O (0.2 weight per cent)<sup>4</sup>. Some authors have speculated that this type of tholeiitic basalt is the major extrusion from the upper mantle and constitutes the predominant rock type in the upper oceanic crust.</p></div></div>","language":"English","publisher":"Nature","doi":"10.1038/2231049a0","issn":"00280836","usgsCitation":"Luyendyk, B., and Engel, C., 1969, Petrological, magnetic and chemical properties of basalt dredged from an abyssal hill in the North-east pacific: Nature, v. 223, no. 5210, p. 1049-1050, https://doi.org/10.1038/2231049a0.","productDescription":"2 p.","startPage":"1049","endPage":"1050","costCenters":[],"links":[{"id":203460,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"223","issue":"5210","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adce4b07f02db686274","contributors":{"authors":[{"text":"Luyendyk, B.P.","contributorId":53074,"corporation":false,"usgs":true,"family":"Luyendyk","given":"B.P.","email":"","affiliations":[],"preferred":false,"id":346815,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Engel, C.G.","contributorId":18489,"corporation":false,"usgs":true,"family":"Engel","given":"C.G.","email":"","affiliations":[],"preferred":false,"id":346814,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":34086,"text":"b1288 - 1969 - Surficial Geology of Mount Rainier National Park, Washington","interactions":[],"lastModifiedDate":"2012-02-10T00:10:09","indexId":"b1288","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1288","title":"Surficial Geology of Mount Rainier National Park, Washington","docAbstract":"Much of the ground surface around Mount Rainier volcano is directly underlain by loose geologic deposits that veneer the hard rock formations. Examples of these deposits are sand and gravel bars along the rivers, ridges of loose rock debris beside the glaciers, and sloping aprons of rock fragments beneath almost every cliff. Even though they are generally thin and inconspicuous when compared with the rock formations, these surficial deposits are clues to geologic events that have profoundly influenced the shape of the park's landscape. Thus, from the character and extent of glacial deposits one can judge the age and size of former glaciers that carved the cirques and deep canyons of the park; from the mudflows which streamed down nearly every valley one can infer the age and size of huge landslides of the past that helped determine Mount Rainier's present shape; and from the pumice deposits some of the volcano's recent eruptive activity can be reconstructed.\r\n\r\nThe map (plate 1, in pocket) that accompanies this description of the surficial deposits of Mount Rainier National Park shows the location of the various geologic formations, and the explanation shows the formations arranged in order of their relative age, with the oldest at the bottom. The text describes the surficial deposits in sequence from older to younger. A discussion of the pumice deposits of the park, which were not mapped, is followed by a description of the formations shown on the geologic map.\r\n\r\nInspection of the geologic map may lead the viewer to question why the surficial deposits are shown in more detail in a zone several miles wide around the base of the volcano than elsewhere. This is partly because the zone is largely near or above timberline, relatively accessible, and the surficial deposits there can be readily recognized, differentiated, and mapped. In contrast, access is more difficult in the heavily timbered parts of the park, and surficial deposits there are generally blanketed by a dense virgin forest and are rarely exposed. Geologic investigations in such areas of the park were of a reconnaissance nature.","language":"ENGLISH","publisher":"U.S. Geological Survey","doi":"10.3133/b1288","usgsCitation":"Crandell, D.R., 1969, Surficial Geology of Mount Rainier National Park, Washington: U.S. Geological Survey Bulletin 1288, 41 p., https://doi.org/10.3133/b1288.","productDescription":"41 p.","costCenters":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":109692,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_21385.htm","linkFileType":{"id":5,"text":"html"},"description":"21385"},{"id":163981,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1288/report-thumb.jpg"},{"id":12496,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://www.nps.gov/history/history/online_books/geology/publications/bul/1288/index.htm","linkFileType":{"id":5,"text":"html"}},{"id":61998,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1288/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -122,46.666666666666664 ], [ -122,47 ], [ -121.41666666666667,47 ], [ -121.41666666666667,46.666666666666664 ], [ -122,46.666666666666664 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae3e4b07f02db68957c","contributors":{"authors":[{"text":"Crandell, Dwight Raymond","contributorId":6440,"corporation":false,"usgs":true,"family":"Crandell","given":"Dwight","email":"","middleInitial":"Raymond","affiliations":[],"preferred":false,"id":212436,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70207813,"text":"70207813 - 1969 - Glacial sedimentology of the Precambrian Gowganda Formation, Ontario, Canada","interactions":[],"lastModifiedDate":"2020-01-14T13:55:15","indexId":"70207813","displayToPublicDate":"1969-12-31T13:52:06","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1723,"text":"GSA Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Glacial sedimentology of the Precambrian Gowganda Formation, Ontario, Canada","docAbstract":"<p>The Gowganda Formation is part of the thick Huronián sequence of Precambrian sedimentary rocks that crop out in central Ontario from Lake Superior to Quebec. Although it has long been considered to be glacial, recent work on submarine slump and turbidite deposits has reopened the question of its origin. This study was made to determine its origin and paleogeography.</p><p>Till-like conglomerates, varved argillites, and abundant dropstones characterize the Gowganda and provide strong evidence for a glacial origin. Pebble fabric parallel to regional paleocurrents, rare striated and grooved pavements, and abundant unweathered detritus are also in harmony with a glacial origin. Local thin-bedded sandstones contain flame structure, graded bedding, contorted bedding, and rippled tops, suggesting deposition by turbidity flows. Association of these sandstones with varved argillites and rafted stones indicates that Gowganda turbidites are glaciolacustrine.</p><p>Along the southern margin of the Gowganda, at Whitefish Falls, thick, laterally continuous till-like conglomerates contain internal stratification indicative of subaqueous deposition. Argillites that lack varved structure and associated silty limestones suggest a glacial marine environment.</p><p>In the Cobalt region the apparent long axes of pebbles in conglomerates show a predominant north-south alignment. In the Bruce Mines-Elliot Lake region, the orientation of the long axes of pebbles is more variable. Differences in orientation are related to stratigraphic position. Ripple cross-lamination in sandstones that are interbedded with argillite indicates south-trending paleocurrents. Distribution of varved argillite, silty limestone, and probable marine argillites suggests a northern fresh-water facies and a southern marine facies. Abundant plutonic pebbles and feldspar indicate that the Gowganda ice sheets eroded a northern plutonic terrane and deposited much of their sediment load on the underlying Huronian sediments to the south.</p>","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1969)80[1685:GSOTPG]2.0.CO;2","usgsCitation":"Lindsey, D.A., 1969, Glacial sedimentology of the Precambrian Gowganda Formation, Ontario, Canada: GSA Bulletin, v. 80, no. 9, p. 1685-1702, https://doi.org/10.1130/0016-7606(1969)80[1685:GSOTPG]2.0.CO;2.","productDescription":"8 p.","startPage":"1685","endPage":"1702","costCenters":[{"id":35995,"text":"Geology, Geophysics, and Geochemistry Science Center","active":true,"usgs":true}],"links":[{"id":371225,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Canada","state":"Ontario","otherGeospatial":"Gowganda Formation","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -84.4189453125,\n              45.30580259943578\n            ],\n            [\n              -80.7275390625,\n              45.30580259943578\n            ],\n            [\n              -80.7275390625,\n              47.07012182383309\n            ],\n            [\n              -84.4189453125,\n              47.07012182383309\n            ],\n            [\n              -84.4189453125,\n              45.30580259943578\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","volume":"80","issue":"9","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Lindsey, David A. 0000-0002-9466-0899 dlindsey@usgs.gov","orcid":"https://orcid.org/0000-0002-9466-0899","contributorId":773,"corporation":false,"usgs":true,"family":"Lindsey","given":"David","email":"dlindsey@usgs.gov","middleInitial":"A.","affiliations":[{"id":171,"text":"Central Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":779418,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70206436,"text":"70206436 - 1969 - Merumite occurrence in Guyana","interactions":[],"lastModifiedDate":"2019-11-04T07:33:45","indexId":"70206436","displayToPublicDate":"1969-12-01T07:25:57","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1472,"text":"Economic Geology","active":true,"publicationSubtype":{"id":10}},"displayTitle":"Merumite occurrence in Guyana","title":"Merumite occurrence in Guyana","docAbstract":"<p><span>Merumite was discovered with associated diamonds and gold in 1937 in gravels of the Merume River in Guyana. It was described as essentially a hydrous chromium oxide that contains more than 80 percent Cr2Oa. Milton and Chao in 1958 found it to be a complex aggregate, mainly eskolaite (Cr2Oa) with five or more new chromium minerals which have recently been identified. The deposit is unique. The richest gravel, averaging several ounces merumite per cubic yard, extends about 2 miles along the base of an east-dipping (35°) ridge of sandstone and ash beds, perhaps an outlier of the Precambrian Roraima Formation that forms bold mountainous scarps a few miles south. No chromium mineralization has been observed in the ridge or anywhere in the region, other than the merumite in the placer gravel. Merumite commonly occurs as grains a few millimeters across, but specimens as large as 10 cm have been found. Almost all the merumite is in rounded grains, many with broken worn edges, indicating wear in transport. Granular gold is enclosed in merumite, as is chromian pyrophyllite. Many merumite grains have impressions, and some contain crystals, of doubly terminated \"needle\" quartz. Water-worn gorceixite, rutile, tourmaline-quartz fels, jasper, euhedral glassy quartz (as much as several centimeters long), and fragments of basaltic rock accompany merumite at all localities; rarely, gold and diamonds are associated in the placers. Merumite was probably derived from a local moderate-temperature hydrothermal deposit possibly formed in the adjacent sandstone-volcanic ash bed from solutions related to local ash deposits and massive gabbro-dolerite intrusive bodies in the Roraima Formation. If the deposit was formed at depths of less than a few thousand feet, erosion may have reached it and re-deposited the merumite and accompanying resistant minerals, mostly'quartz and jasper, in local stream beds. © 1969 Society of Economic Geologists, Inc.</span></p>","language":"English ","publisher":"Elsevier","doi":"10.2113/gsecongeo.64.8.910","issn":"03610128","usgsCitation":"Milton, C., and Narain, S., 1969, Merumite occurrence in Guyana: Economic Geology, v. 64, no. 8, p. 910-914, https://doi.org/10.2113/gsecongeo.64.8.910.","productDescription":"5 p. ","startPage":"910","endPage":"914","costCenters":[],"links":[{"id":368914,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Guyana ","otherGeospatial":"Merume River","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -59.3756103515625,\n              5.4683637496808535\n            ],\n            [\n              -57.864990234375,\n              5.4683637496808535\n            ],\n            [\n              -57.864990234375,\n              7.035475652433024\n            ],\n            [\n              -59.3756103515625,\n              7.035475652433024\n            ],\n            [\n              -59.3756103515625,\n              5.4683637496808535\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","volume":"64","issue":"8","noUsgsAuthors":false,"publicationDate":"1969-12-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Milton, C.","contributorId":37472,"corporation":false,"usgs":true,"family":"Milton","given":"C.","affiliations":[],"preferred":false,"id":774536,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Narain, S","contributorId":220228,"corporation":false,"usgs":false,"family":"Narain","given":"S","email":"","affiliations":[],"preferred":false,"id":774537,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70224626,"text":"70224626 - 1969 - Mud Lake, Florida: Its algae and alkaline brown water","interactions":[],"lastModifiedDate":"2021-09-30T18:42:48.373315","indexId":"70224626","displayToPublicDate":"1969-11-01T13:27:52","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2620,"text":"Limnology and Oceanography","active":true,"publicationSubtype":{"id":10}},"title":"Mud Lake, Florida: Its algae and alkaline brown water","docAbstract":"<div class=\"article-section__content en main\"><p>Mud Lake (Marion County, Florida), in the Ocala National Forest, is elliptical, has an area of ca. 180 ha, and a mean depth of less than 50 cm. The water contains about 200 ppm dissolved solids, ranges from brown to nearly colorless (15 to 100 Pt units), and is always alkaline (<i>p</i>H 7.7 to 10.2). Dissolved Fe, Ca, PO<sub>4</sub>, tannin-lignin, and the specific conductance, color, and temperature of the water were measured monthly for 1 yr, and temperature and<span>&nbsp;</span><i>p</i>H were measured many other times during the 3-yr study (1966–1968). The lake is surrounded by a zone of mixed hardwood swamp flora and a floating mat of vegetation and has no submerged higher plants and only 1 or 2 m<sup>2</sup><span>&nbsp;</span>of emergent plants. The lake sediment consists exclusively of minute fecal pellets produced mainly by chironomid larvae and composed solely of blue-green algae. Myxophyceae are represented by at least 10 genera and 12 species, which live exclusively on, or in, the fecal pellets; less than half show a seasonal distribution. The Chlorophyceae consist dominantly of<span>&nbsp;</span><i>Spirogyra triplicata</i><span>&nbsp;</span>with minor amounts of<span>&nbsp;</span><i>Sirogonium</i><span>&nbsp;</span>sp. and generally occur in enormous winter blooms, correlated with changing amounts of dissolved PO<sub>4</sub><span>&nbsp;</span>and apparently inversely with both temperature and incident light. Bacillariophyceae are represented by 18 species and varieties, but the total population is small. Nanno-, zoo- and phytoplankton are extremely rare, probably because of the prevailing high intensity illumination and the extremely shallow water. Only the fish population is large, and this is dominated by minnows, gars, and sunfish. The midge population is remarkably small. A bacterial inhibitor probably accounts for the small population of bacteria both in the water and in the top layer of the sediment.</p></div>","language":"English","publisher":"Association for the Sciences of Limnology and Oceanography","doi":"10.4319/lo.1969.14.6.0889","usgsCitation":"Bradley, W.H., and Beard, M.E., 1969, Mud Lake, Florida: Its algae and alkaline brown water: Limnology and Oceanography, v. 14, no. 6, p. 889-897, https://doi.org/10.4319/lo.1969.14.6.0889.","productDescription":"9 p.","startPage":"889","endPage":"897","costCenters":[],"links":[{"id":390057,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Florida","county":"Marion County","otherGeospatial":"Mud Lake, Ocala National Forest","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n     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H.","contributorId":102452,"corporation":false,"usgs":true,"family":"Bradley","given":"W.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":824402,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Beard, M. E.","contributorId":266144,"corporation":false,"usgs":false,"family":"Beard","given":"M.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":824403,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70225578,"text":"70225578 - 1969 - History of the Redwall Limestone of northern Arizona","interactions":[],"lastModifiedDate":"2022-11-21T18:01:35.023539","indexId":"70225578","displayToPublicDate":"1969-01-01T14:27:35","publicationYear":"1969","noYear":false,"publicationType":{"id":4,"text":"Book"},"publicationSubtype":{"id":15,"text":"Monograph"},"title":"History of the Redwall Limestone of northern Arizona","docAbstract":"<p>Throughout most of northern Arizona the Redwall Limestone of Mississippian age is readily divisible into four lithologic units, designated in ascending order as the Whitmore Wash, Thunder Springs, Mooney Falls, and Horseshoe Mesa Members. The first and third members are thick-bedded to massive carbonate rock. The Horseshoe Mesa Member is relatively thin-bedded limestone, and the Thunder Springs Member is distinctive because it consists of chert beds alternating with thin beds of carbonate rock.</p><p>Trends in thickness of the various members indicate that the sediment that formed the Redwall was deposited on an even, gently sloping shelf that extended westward from the Defiance positive element, a low landmass located near the present eastern border of northern Arizona. The Peach Springs and Payson ridges projected west and southwest, respectively, from the positive element. These ridges, which were partly submerged and partly above sea level during Mississippian time, are indicated by the patterns of isopach lines and, in part, by the distribution of faunas. The ridges divided the Arizona section of the shelf into three segments: the northern-most, which slopes northwest toward the Cordilleran geosyncline, and the other two, which slope toward the south and southwest.</p><p>Two transgressions and two regressions of the western and southern seaways are believed to be represented by the Redwall. The first transgression, which is recorded by thick beds of clastic sediment of the Whitmore Wash Member, was less extensive than the second, which is recorded by massive beds of the Mooney Falls Member, for on the western margins of the Defiance positive element the Mooney Falls Member overlaps the two lower members. Furthermore, south of Grand Canyon the Whitmore Wash and Thunder Springs Members lap against the Payson ridge without covering it, whereas the Mooney Falls Member, although relatively thin, extends across it. Regression is believed to be represented by thin beds of the Thunder Springs and Horseshoe Mesa Members, which are interpreted to be the result of low base level caused by silting up with clastic material and consequent retreat of the sea.</p><p>Cycles in sedimentation are well developed in some parts of the Redwall, especially in the upper two members in which differences in grain size represent five major cycles recognized throughout the extent of the Grand Canyon. These textural differences, ranging from aphanitic to coarse grained, are considered to be not measures of the amount of transportation, as with terrigenous sediments, but reflections of the degree of turbulence or the lack of turbulence during deposition.</p><p>They are interpreted as indicators of cyclic fluctuations in environment, probably related to changes in wave base.</p><p>Several clearly defined facies within the Redwall indicate environments of deposition. The clastic limestone that forms a major part of the formation, especially in the offshore areas to the west and south, is believed to represent normal marine conditions where circulation was good and turbulence moderate to strong. Uniform finely crystalline dolomite probably developed through early diagenetic processes on the sea floor. On the basis of its distribution pattern the dolomite seems to have formed under shoal conditions, especially where it borders the shore of the Defiance positive element and along Peach Springs ridge. Oölitic limestone at the top of both major transgressive units is interpreted as reflecting the oscillatory conditions of sea level that provided wave and current agitation at times of maximum sea advance in shoal areas bordering the ridges. Aphanitic limestone, representing accumulations of lime mud, seems to be developed best in the uppermost, or Horseshoe Mesa, member, where, as the seas regressed, nearshore waters may have been isolated and certainly were very calm.</p><p>Original textures and some structures are preserved in most limestones of the Redwall, and they give much evidence concerning oceanographic factors of the time. Generalizations have been developed concerning the character of the bottom, degrees of energy represented, depth, salinity, and other factors for various parts of the formation. Although these factors differed greatly with time and space, the general conclusions reached are that (1) depths were very shallow to moderate, (2) the sea floor was composed nearly entirely of lime mud and lime sand, which contained no terrigeneous material but with great crinoidal accumulations locally, (3) turbulence ranged from considerable to none, and (4) the sea was clear and warm and nowhere contained saline concentrations sufficient to form evaporites.</p><p>Chert forming thin irregular beds, locally lenticular and nodular, occurs at two prinicpal positions in the stratigraphic section, and in each it alternates with thin beds of carbonate rock. Chert is prominent throughout the Thunder Springs Member and forms thin but definite zones near the top of the Mooney Falls Member. This chert is believed to have formed on the sea floor during early diagenesis, as evidenced by petrography, paleogeography, and faunal relations. Regional differences in the abundance and type of associated fossils, recorded on a series of 4-foot-square sample plots made throughout the Grand Canyon, suggest a probable relation between fossil distribution and genesis of the chert.</p><p>The fauna of the Redwall is abundant and varied, but preservation in many places is poor, and numerous specimens can be collected only locally. The most common fossils are brachiopods, corals, foraminifers, and crinoids, but blastoids, gastropods, cephalopods, and pelecypods are not rare. Bryozoans are abundant in the chert of the Thunder Springs Member but uncommon elsewhere. Other organisms locally distributed but not common are algae, trilobites, fish, holothurians, and ostracodes. These groups have been studied by specialists and are the subject of Chapters V through XIII.</p><p>Certain of the faunal groups, notably the corals and foraminifers, show some degree of vertical zoning and so have furnished important data on age and correlation. Among the corals, the zones of<span>&nbsp;</span><i>Dorlodotia inconstans</i><span>&nbsp;</span>and<span>&nbsp;</span><i>Michelinia expansa</i><span>&nbsp;</span>are especially significant because of their persistence from section to section across broad areas. The foraminiferal zones are broader and less sharply defined, but they represent a series of major changes in species from bottom to top of the formation.</p><p>Age determination made on the basis of foraminifers and brachiopods indicate that the base of the Redwall is progressively younger as it passes from areas that were offshore eastward or northward toward the Defiance positive element; the top of the Redwall, in contrast, is shown to be progressively younger away from the positive element. Thus basal beds of Kinderhook age are recognized at Grand Wash, Quartermaster, and Meriwitica Canyons to the northwest, but the lowest strata are of Osage age at Bridge Canyon, Grandview, and other sections closer to the landmass. Likewise, units with fossils of middle Meramec age occur in western Grand Canyon, but, except in the one place discussed in the following paragraph, topmost beds farther east in Grand Canyon are of Osage age. South of Grand Canyon the youngest member of the Redwall (Horseshoe Mesa) has been removed by pre-Supai Formation erosion.</p><p>Rocks still younger than the Horseshoe Mesa once may have covered the entire region, possibly representing a third sequence of transgression and regression. At Bright Angel trail in eastern Grand Canyon, for example, a unique unit at the top of the Redwall section contains fossils of Chester age and apparently represents a remnant of Late Mississippian rocks that survived as an inlier there.</p>","language":"English","publisher":"Geological Society of America","doi":"10.1130/MEM114","usgsCitation":"McKee, E.D., and Gutschick, R.C., 1969, History of the Redwall Limestone of northern Arizona, v. 114, 700 p., https://doi.org/10.1130/MEM114.","productDescription":"700 p.","costCenters":[],"links":[{"id":480312,"rank":0,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.1130/mem114","text":"Publisher Index Page"},{"id":390903,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Arizona","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -114.488525390625,\n              34.07996230865873\n            ],\n            [\n              -109.00634765625,\n              34.07086232376631\n            ],\n            [\n              -109.00634765625,\n              37.02886944696474\n            ],\n            [\n              -114.08203125,\n              37.020098201368114\n            ],\n            [\n              -114.10400390625,\n              36.32397712011264\n            ],\n            [\n              -114.2138671875,\n              36.06686213257888\n            ],\n            [\n              -114.3896484375,\n              36.24427318493909\n            ],\n            [\n              -114.774169921875,\n              36.10237644873644\n            ],\n            [\n              -114.7412109375,\n              35.567980458012094\n            ],\n            [\n              -114.7412109375,\n              35.40696093270201\n            ],\n            [\n              -114.63134765625001,\n              35.200744801724014\n            ],\n            [\n              -114.7412109375,\n              35.110921809704756\n            ],\n            [\n              -114.7412109375,\n              34.813803317113155\n            ],\n            [\n              -114.488525390625,\n              34.542762387234845\n            ],\n            [\n              -114.466552734375,\n              34.415973384481866\n            ],\n            [\n              -114.202880859375,\n              34.279914398549934\n            ],\n            [\n              -114.488525390625,\n              34.07996230865873\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","volume":"114","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"McKee, Edwin D.","contributorId":60207,"corporation":false,"usgs":true,"family":"McKee","given":"Edwin","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":825662,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Gutschick, Raymond C.","contributorId":12054,"corporation":false,"usgs":true,"family":"Gutschick","given":"Raymond","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":825663,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":2000006,"text":"2000006 - 1969 - The benthic macrofauna of Lake Ontario","interactions":[],"lastModifiedDate":"2012-02-02T00:14:59","indexId":"2000006","displayToPublicDate":"1969-01-01T01:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":1,"text":"Federal Government Series"},"seriesTitle":{"id":91,"text":"Technical Report","active":true,"publicationSubtype":{"id":1}},"seriesNumber":"14","title":"The benthic macrofauna of Lake Ontario","docAbstract":"The presence and relative abundance of bottom macrofauna in Lake Ontario are documented. Bottom samples were collected at 24 stations in September 1964. The quantity of organisms and the distribution of some species were affected by depth of water. Samples from the shallower stations (47.5 m or less) yielded an average of 41,631 organisms per mA? whereas the deeper stations (91.5 m or more) yielded an average of only 7,938. The Oligochaeta, the most abundant group of macroinvertebrates, was represented by four families - Enchytraeidae, Lumbriculidae, Naididae, and Tubificidae. The lumbriculid worm, Stylodrilus heringianus, and the burrowing amphipod, Pontoporeia affinis, were rare or absent in areas affected by pollution. In kinds and abundance of organisms, the bottom fauna in Lake Ontario was generally similar to that in Lake Michigan.","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Limnological survey of Lake Ontario, 1964","largerWorkSubtype":{"id":1,"text":"Federal Government Series"},"language":"English","publisher":"Great Lakes Fishery Commission","collaboration":"Out-of-print","usgsCitation":"Hiltunen, J.K., 1969, The benthic macrofauna of Lake Ontario: Technical Report 14, p. 39-50.","productDescription":"p. 39-50","startPage":"39","endPage":"50","numberOfPages":"12","costCenters":[{"id":324,"text":"Great Lakes Science Center","active":true,"usgs":true}],"links":[{"id":198576,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":91894,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://www.glfc.org/pubs/TechReports/Tr14.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a85e4b07f02db64d4bc","contributors":{"authors":[{"text":"Hiltunen, Jarl K.","contributorId":27820,"corporation":false,"usgs":true,"family":"Hiltunen","given":"Jarl","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":324915,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70009828,"text":"70009828 - 1969 - Magnetic susceptibility and exchange coupling in the mineral ardennite","interactions":[],"lastModifiedDate":"2020-11-29T20:16:10.19269","indexId":"70009828","displayToPublicDate":"1969-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2428,"text":"Journal of Physics and Chemistry of Solids","active":true,"publicationSubtype":{"id":10}},"title":"Magnetic susceptibility and exchange coupling in the mineral ardennite","docAbstract":"<p><span>Ardennite, a rare silicate mineral, contains about 19 wt.% manganese. Some of the manganese atoms are in positions which are close enough to allow negative exchange and hence a reduction of the total magnetic susceptibility. It is shown that the susceptibility can be accounted for approximately by the treatment of Earnshaw and Lewis (1958) for&nbsp;</span><span class=\"math\"><span id=\"MathJax-Element-1-Frame\" class=\"MathJax_SVG\" data-mathml=\"<math xmlns=&quot;http://www.w3.org/1998/Math/MathML&quot;><mtext>S =</mtext><mtext>5</mtext><mtext>2</mtext></math>\"><span class=\"MJX_Assistive_MathML\">S =52</span></span></span><span>&nbsp;and a Hamiltonian&nbsp;</span><i>H</i><span>&nbsp;= −2</span><i>g</i><span>μ</span><i>H</i><sub><i>b</i></sub><span>−2</span><i>JS</i><sub>1</sub><span>·</span><i>S</i><sub>2</sub><span>.</span></p>","language":"English","publisher":"Elsevier","doi":"10.1016/0022-3697(69)90149-8","issn":"00223697","usgsCitation":"Thorpe, A.N., Senftle, F.E., and Donnay, G., 1969, Magnetic susceptibility and exchange coupling in the mineral ardennite: Journal of Physics and Chemistry of Solids, v. 30, no. 9, p. 2235-2239, https://doi.org/10.1016/0022-3697(69)90149-8.","productDescription":"5 p.","startPage":"2235","endPage":"2239","numberOfPages":"5","costCenters":[],"links":[{"id":219723,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"30","issue":"9","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a4b8ce4b0c8380cd6960a","contributors":{"authors":[{"text":"Thorpe, A. N.","contributorId":53504,"corporation":false,"usgs":true,"family":"Thorpe","given":"A.","email":"","middleInitial":"N.","affiliations":[],"preferred":false,"id":357239,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Senftle, F. E.","contributorId":47788,"corporation":false,"usgs":true,"family":"Senftle","given":"F.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":357238,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Donnay, G.","contributorId":97625,"corporation":false,"usgs":true,"family":"Donnay","given":"G.","email":"","affiliations":[],"preferred":false,"id":357240,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":70010799,"text":"70010799 - 1969 - The relationship of the rare-earth composition of minerals to geological environment","interactions":[],"lastModifiedDate":"2020-11-29T18:40:05.657968","indexId":"70010799","displayToPublicDate":"1969-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1759,"text":"Geochimica et Cosmochimica Acta","active":true,"publicationSubtype":{"id":10}},"title":"The relationship of the rare-earth composition of minerals to geological environment","docAbstract":"<p>It has been known for a long time that the composition of the lanthanides in minerals is controlled to a large degree by crystallo-chemical factors, but is also greatly influenced by changes in geological environment. In general, igneous rocks rich in silica are favourable for the concentration of the heavy lanthanides and yttrium; those low in silica and high in carbonate are favourable for the concentration of the light lanthanides.</p><p>These generalizations are illustrated by summaries of the available data on monazite, sphene, and apatite from different geological environments. Apatite of marine sedimentary origin (a large potential source of rare earths) shows marked depletion of cerium, as has been noted previously for sea water.</p>","language":"English","publisher":"Elsevier","doi":"10.1016/0016-7037(69)90118-5","issn":"00167037","usgsCitation":"Fleischer, M., and Altschuler, Z., 1969, The relationship of the rare-earth composition of minerals to geological environment: Geochimica et Cosmochimica Acta, v. 33, no. 6, p. 725-732, https://doi.org/10.1016/0016-7037(69)90118-5.","productDescription":"8 p.","startPage":"725","endPage":"732","numberOfPages":"8","costCenters":[],"links":[{"id":218803,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"33","issue":"6","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505baf27e4b08c986b3245ae","contributors":{"authors":[{"text":"Fleischer, M.","contributorId":84069,"corporation":false,"usgs":true,"family":"Fleischer","given":"M.","email":"","affiliations":[],"preferred":false,"id":359675,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Altschuler, Z. S.","contributorId":42962,"corporation":false,"usgs":true,"family":"Altschuler","given":"Z. S.","affiliations":[],"preferred":false,"id":359674,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70038235,"text":"70038235 - 1968 - Water resources inventory of Connecticut Part 3: lower Thames and southeastern coastal river basins","interactions":[],"lastModifiedDate":"2014-06-17T11:29:43","indexId":"70038235","displayToPublicDate":"2012-04-22T10:47:00","publicationYear":"1968","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":2,"text":"State or Local Government Series"},"seriesTitle":{"id":108,"text":"Connecticut Water Resources Bulletin","active":false,"publicationSubtype":{"id":2}},"seriesNumber":"15","title":"Water resources inventory of Connecticut Part 3: lower Thames and southeastern coastal river basins","docAbstract":"<p>The lower Thames and southeastern coastal river basins have a relatively abundant supply of water of generally good quality which is derived from streams entering the area and precipitation that has fallen on the area. Annual precipitation has ranged from about 32 inches to 65 inches and has averaged about 48 inches over a 30-year period. Approximately 22 inches of water are returned to the atmosphere each year by evaporation and transpiration; the remainder of the annual precipitation either flows overland to streams or percolates downward to the water table and ultimately flows out of the report area through estuaries and coastal streams or as underflow through the deposits beneath. During the autumn and winter months precipitation normally is sufficient to cause a substantial increase in the amount of water stored underground and in surface reservoirs within the report area, whereas in the summer most of the precipitation is lost through evaporation and transpiration, resulting in sharply reduced stream-flow and lowered ground-water levels. The mean monthly storage of water on an average is about 3.8 inches higher in November than it is in June.</p>\n<br/>\n<p>The amount of water that flows through and out of the report area represents the total amount of water potentially available for use by man. For the 30-year period 1931 through 1960, the annual runoff from the report area has averaged nearly 26 inches (200 billion gallons), from the entire Thames River basin above Norwich about 24 inches (530 billion gallons), and from the Pawcatuck River basin about 26 inches (130 billion gallons). A total average annual runoff of 860 billion gallons is therefore available. Although runoff indicates the total amount of water potentially available, it is usually not economically feasible for man to use all of it. On the other hand, with increased development, it is possible that some water will be reused several times.</p>\n<br/>\n<p>The water available may be tapped as it flows through the area or is temporarily stored in streams, lakes, and aquifers. The amounts that can be developed vary from place to place and time to time, depending on the amount of precipitation, on the size of drainage area, on the thickness, permeability, and areal extent of aquifers, and on the variations in chemical and physical quality of the water.</p>\n<br/>\n<p>Differences in streamflow from point to point are due primarily to differences in the proportion of stratified drift in the drainage basin above each point, which affect the timing of streamflow, and to differences in precipitation, which affect the amount of streamflow.</p>\n<br/>\n<p>Ground water can be obtained from wells almost anywhere in the area, but the amount obtainable at any particular point depends upon the type and water-bearing  properties of the aquifers. For practical purposes, the earth materials in the report area comprise three aquifers--stratified drift, bedrock, and till.</p>\n<br/>\n<p>Stratified drift is the only aquifer generally capable of yielding more than 100 gpm (gallons per minute) to individual wells. It covers about 20 percent of the area and occurs chiefly in lowlands where it overlies till and bedrock. The coefficient of permeability of the coarse-grained unit of stratified drift averages about 1,500 gbd (gallons per day) per sq ft. Drilled, screened wells tapping this unit are known to yield from 4 to 88o gpm and average 146 gpm. Dug wells in coarse-grained stratified drift supply about 2 gpm per foot of drawdown over a period of a few hours. Fine-grained stratified drift has an average coefficient of permeability of about 300 gpd per sq ft and can usually yield supplies sufficient for household use to dug wells.</p>\n<br/>\n<p>Bedrock and till are widespread in extent but generally provide only small water supplies. Bedrock is tapped chiefly by drilled wells, about 90 percent of which will supply at least 3 gpm. Very few, however, will supply more than 50 gpm. Till is tapped in a few places by dug wells which can yield small supplies of only a few hundred gpd throughout all or most of the year. The coefficient of permeability of till ranges from about 0.2 gpd per sq ft to 120 gpd per sq ft.</p>\n<br/>\n<p>The amount of ground water potentially available in the report area depends upon the amount of ground-water outflow, the amount of ground water in storage, and the quantity of water available by induced infiltration from streams and lakes. From data on permeability, saturated thickness, recharge, yield from aquifer storage, well performance, and streamflow, preliminary estimates of ground-water availability can be made for any point in the report area. Long-term yields estimated for 18 areas of stratified drift especially favorable for development of large ground-water supplies ranged from 1.3 to 66 mgd. Detailed site studies to determine optimum yields, drawdowns, and spacing of individual wells are needed before major ground-water development is undertaken in these or other areas.</p>\n<br/>\n<p>The chemical quality of water in the report area is generally good to excellent. Samples of naturally occurring surface water collected at 24 sites contained less than 151 ppm (parts per million) of dissolved solids and less than 63 ppm of hardness. Water from wells is more highly mineralized than naturally occurring water from streams. Even so only 12 percent of the wells sampled yielded water with more than 200 ppm of dissolved solids and only 8 percent yielded water with more than 120 ppm of hardness.</p>\n<br/>\n<p>Even in major streams, which are used to transport industrial waste, hardness rarely exceeds 60 ppm and the dissolved mineral content is generally less than 200 ppm. At a few places in the town of Montville however, waters may contain dissolved mineral concentrations of 2,000 to 4,000 ppm. </p>\n<br/>\n<p>Iron and manganese in both ground water and surface water are the only constituents whose concentrations commonly exceed recommended limits for domestic and industrial use. Most wells in the report area yield clear water with little or no iron or manganese, but distributed  among them are wells yielding ground water that contains enough of these dissolved constituents to be troublesome for most uses.</p>\n<br/>\n<p>Iron concentrations in naturally occurring stream water exceed 0.3 ppm under low-flow conditions at 33 percent of the sites sampled. Large concentrations of iron in stream water result from discharge of iron-bearing water from aquifers or from swamps where it is released largely from decaying vegetation.</p>\n<br/>\n<p>Ground water more than 30 feet below the land surface has a relatively constant temperature, usually between 48°F and 52°F. Water temperature in very shallow wells may fluctuate from about 38°F in February or March to about 55°F in late summer. Water temperature in the larger streams fluctuates much more widely, ranging from 32°F at least for brief periods in winter, to about 85°F occasionally during summer.</p>\n<br/>\n<p>The quality of suspended sediment transported by streams in the area is negligible. Turbidity in streams is generally not a problem although amounts large enough to be troublesome may occur locally at times.</p>\n<br/>\n<p>The total amount of water used in the report area for all purposes during 1964 was about 118,260 million gallons, of which 105,600 million gallons was estuarine water used for cooling by industry. The average per capita water use, excluding estuarine, temporary summer residence, and institutional water was equivalent to 186 gpd. Public water systems supplied the domestic needs of nearly tw0-thirds the population of the report area. All of the 19 systems, which were sampled, provided water of better quality than the U.S. Public Health Service suggests for drinking water standards.</p>","language":"English","publisher":"Connecticut Water Resources Commission","collaboration":"Prepared by the U.S. Geological Survey in cooperation with the Connecticut Water Resources Commission","usgsCitation":"Thomas, C.E., Cervione, M.A., and Grossman, I., 1968, Water resources inventory of Connecticut Part 3: lower Thames and southeastern coastal river basins: Connecticut Water Resources Bulletin 15, Report: viii, 105 p.; 4 Plates: 23.80 x 23.86 inches and smaller.","productDescription":"Report: viii, 105 p.; 4 Plates: 23.80 x 23.86 inches and smaller","numberOfPages":"122","costCenters":[],"links":[{"id":258795,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/ctwrb/0015/report.pdf","size":"22138","linkFileType":{"id":1,"text":"pdf"}},{"id":258796,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/ctwrb/0015/report-thumb.jpg"},{"id":285977,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70038235/plate-c.pdf"},{"id":285978,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70038235/plate-d.pdf"},{"id":285975,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70038235/plate-a.pdf"},{"id":285976,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70038235/plate-b.pdf"}],"scale":"48000","country":"United States","state":"Connecticut","otherGeospatial":"Coastal River Basins;Thames","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -72.316667,41.283333 ], [ -72.316667,41.7 ], [ -71.766667,41.7 ], [ -71.766667,41.283333 ], [ -72.316667,41.283333 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bcb79e4b08c986b32d687","contributors":{"authors":[{"text":"Thomas, Chester E. Jr.","contributorId":37182,"corporation":false,"usgs":true,"family":"Thomas","given":"Chester","suffix":"Jr.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":463702,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Cervione, Michael A. Jr.","contributorId":23988,"corporation":false,"usgs":true,"family":"Cervione","given":"Michael","suffix":"Jr.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":463701,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Grossman, I.G.","contributorId":52574,"corporation":false,"usgs":true,"family":"Grossman","given":"I.G.","email":"","affiliations":[],"preferred":false,"id":463703,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":70379,"text":"rp34 - 1968 - Rare and endangered fish and wildlife of the United States","interactions":[],"lastModifiedDate":"2016-11-02T14:42:42","indexId":"rp34","displayToPublicDate":"2005-04-11T09:36:11","publicationYear":"1968","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":1,"text":"Federal Government Series"},"seriesTitle":{"id":79,"text":"Resource Publication","active":false,"publicationSubtype":{"id":1}},"seriesNumber":"34","title":"Rare and endangered fish and wildlife of the United States","docAbstract":"<p>No abstract available</p>","language":"ENGLISH","publisher":"U.S. Fish and Wildlife Service","publisherLocation":"Washington, D.C.","usgsCitation":"Committee on Rare And Endangered Wildlife Species, B.F., 1968, Rare and endangered fish and wildlife of the United States: Resource Publication 34, 150 p.","productDescription":"150 p.","costCenters":[],"links":[{"id":186173,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a80e4b07f02db6492ef","contributors":{"authors":[{"text":"Committee on Rare And Endangered Wildlife Species, Bureau Of Sport Fisheries And Wildlife (compiler)","contributorId":51849,"corporation":false,"usgs":true,"family":"Committee on Rare And Endangered Wildlife Species","given":"Bureau Of Sport","suffix":"(compiler)","email":"","middleInitial":"Fisheries And Wildlife","affiliations":[],"preferred":false,"id":282319,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
]}