The McCallum anticlines, embracing an area about 2 miles wide and 12 miles long, are about 6 miles east of the town of Walden, Jackson County, Colo., on the east side of the Continental Divide. A cover of flat-lying Quaternary gravel obscures the outcrop of Pierre shale at many points on the two anticlines. Wells start in the upper part of the Pierre and penetrate all of the underlying Upper Cretaceous series to the top of the Dakota sandstone, where production of oil and carbon dioxide is obtained. The first prospecting for oil was reported in 1912, but it was not until December 1926 that oil was discovered in commercial quantities.
Two geologic sections across the anticlines, extending to the outcrop of the Dakota sandstone at the base of the Medicine Bow Range, to, the east, disclosed a marked thickening between this formation and a fossiliferous sandstone in the Pierre shale which was used as a key bed. Immediately beneath the Dakota sandstone along ore of these cross sections a sandy volcanic ash resembling that found at the horizon of the Mowry shale in Wyoming was discovered. However, it is considered here the top bed of the Morrison formation.
The impossibility of obtaining dips along the crests, owing to the cover of terrace gravel, made it necessary to construct ten structure sections across these anticlines, using the geometry of conic sections in their development. From the geometric figures developed structure contours were obtained graphically.
The occurrence of carbon dioxide in large volumes in association with petroleum on each of these anticlines provides an unusual problem in oil production. Experimental data relative to the physical properties of this gas offer an approach to the solution of the problem. The applicability of such data to actual operating conditions is yet to be tried, but the work of early investigators in the field of physical chemistry suggests the feasibility of mixing air with the carbon dioxide to assure continuity of production, which heretofore has not been attained in this area.
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The quadrangle conta ins fragmentary exposures of Algonkian and Paleozoic sedimentary rocks, extensive deposits of old volcanic strata, presumably Permian, not heretofore recognized in this part of Idaho, and a thick succession of Oligocene(?) lava and pyroclastic rocks. The Idaho batholith and its satellites extend into the quadrangle, and in addition there a re large masses of Tertiary granitic rock, not previously distinguished in Idaho, and many Tertiary dikes, some of which are genetically associated with contact-metamorphic deposits. The area contains injection gneiss of complex origin, largely related to the Idaho batholith but in part resulting from injection by ~he Tertiary granitic rocks under relatively light load. Orogenic movement took place in Algonkian, Paleozoic, and Tertiary time. There is a summit peneplain or par tial peneplain of Tertiary, perhaps Pliocene age, and the erosional history since its elevation has been complex. The ore deposits include lodes and placers. The lodes are related to both the Idaho batholith and the Tert iary intrusive rocks and have yielded gold and copper ore of a total value of about 1,000,000. Placers, largely formed in an interglacial inter val, have yielded about an equal amount. There has been some prospecting but almost no production since 1916.
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1934 - Bibliography of North American geology, 1931 and 1932","interactions":[],"lastModifiedDate":"2012-02-02T00:09:49","indexId":"b858","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1934","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":"858","title":"Bibliography of North American geology, 1931 and 1932","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/b858","usgsCitation":"Nickles, J.M., 1934, Bibliography of North American geology, 1931 and 1932: U.S. Geological Survey Bulletin 858, 300 p. ;24 cm., https://doi.org/10.3133/b858.","productDescription":"300 p. ;24 cm.","costCenters":[],"links":[{"id":93293,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/0858/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":164486,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/0858/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a51e4b07f02db6299cf","contributors":{"authors":[{"text":"Nickles, John M.","contributorId":8527,"corporation":false,"usgs":true,"family":"Nickles","given":"John","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":214518,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":32822,"text":"pp185G - 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\"}}]}","volume":"15","issue":"1","noUsgsAuthors":false,"publicationDate":"2014-08-18","publicationStatus":"PW","contributors":{"authors":[{"text":"Ross, Clarence S.","contributorId":7251,"corporation":false,"usgs":true,"family":"Ross","given":"Clarence S.","affiliations":[],"preferred":false,"id":775358,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70206681,"text":"70206681 - 1934 - The Rôle of volatiles in the formation of Virginia titanium deposits","interactions":[],"lastModifiedDate":"2019-11-16T17:40:10","indexId":"70206681","displayToPublicDate":"1934-06-30T17:35:19","publicationYear":"1934","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1578,"text":"Eos, Transactions, American Geophysical Union","onlineIssn":"2324-9250","printIssn":"0096-394","active":true,"publicationSubtype":{"id":10}},"title":"The Rôle of volatiles in the formation of Virginia titanium deposits","docAbstract":"The feldspathic rock with which the titanium deposits of Virginia are associated appears to be an anorthosite, although the plagioclase is somewhat more sodic than in normal anorthosites. That is, this rock shows evidence of having been introduced as a mush‐like mass of crystals and intersititial magma, and of undergoing very thorough crushing during introduction. This rook was later very thoroughly altered by hydrothermal solutions which migrated through the fractures in the feldspar rook and new minerals including the titanium minerals—rutile and ilmenite—were introduced. The elements introduced into the feldspathic rock ware TiO2 FeO, MgO, P2O5, and F. The other elements that went into the formation of new minerals were derived from the feldspar originally present. There was a distinct order in the abstraction of the introduced elements from the carrying solutions, as shown by the zonal relatione of the secondary minerals. Ferrous iron was abstracted first in the formation of the ferromagnesian silicates and ilmenite. Magnesium and titanium, in the absence of iron, traveled farther from the source of the solutions and deposited rutile and magnesian silicates. At greater distances most of the introduced elements had been abstracted from the solutions but notwithstanding this the feldspar was extensively altered, but without any marked changes between the chemical composition of the original feldspar rook and the resulting altered rook. ©1934. American Geophysical Union. All Rights Reserved.
","language":"English","publisher":"American Geophysical Union","doi":"10.1029/TR015i001p00245","issn":"00028606","usgsCitation":"Ross, C.S., 1934, The Rôle of volatiles in the formation of Virginia titanium deposits: Eos, Transactions, American Geophysical Union, v. 15, no. 1, p. 245-245, https://doi.org/10.1029/TR015i001p00245.","productDescription":"1 p. 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\"}}]}","volume":"15","issue":"1","noUsgsAuthors":false,"publicationDate":"2014-08-18","publicationStatus":"PW","contributors":{"authors":[{"text":"Ross, C. S.","contributorId":18337,"corporation":false,"usgs":true,"family":"Ross","given":"C.","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":775357,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70221684,"text":"70221684 - 1934 - Relation of stream‐flow to ground‐water levels","interactions":[],"lastModifiedDate":"2021-06-28T17:37:08.351486","indexId":"70221684","displayToPublicDate":"1934-06-01T12:31:54","publicationYear":"1934","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1578,"text":"Eos, Transactions, American Geophysical Union","onlineIssn":"2324-9250","printIssn":"0096-394","active":true,"publicationSubtype":{"id":10}},"title":"Relation of stream‐flow to ground‐water levels","docAbstract":"In recent years the Water Resources Branch of the United States Geological Surrey has given considerable attention to the relation of ground‐water to stream‐flow. One locality in which this relation is being studied is about 13 miles from Washington, near Colesvllle, Maryland, where a Kinnison float‐gage is being maintained in a well In connection with the operation of a gaging‐station on the Northwest Branch of the Anacostia River. The well is opposite the gaging‐station, on a gentle slope about one. fifth of a mile from the stream, where the land‐surface ia about 20 feet above the bed of the stream. The well is an abandoned dug well 20 feet deep and is lined with loose stone and presumably admits water freely. The fluctuations of the water‐level in the well are believed to afford a fairly close index of fluctuations in the water‐table at the well‐site and may be typical of the fluctuations that occur in a large part of the area drained by the Northwest Branch above the gaging‐station, consisting of about 21 square miles of gently rolling farm‐land. During the period of the observations herein considered the water‐level in the well ranged from 10 to 16 feet below the ground‐surface at the well and from 10 to 4 feet above the bed of the stream.
","language":"English","publisher":"American Geophysical Union","doi":"10.1029/TR015i002p00414","usgsCitation":"Harrold, L., 1934, Relation of stream‐flow to ground‐water levels: Eos, Transactions, American Geophysical Union, v. 15, no. 2, p. 414-416, https://doi.org/10.1029/TR015i002p00414.","productDescription":"3 p.","startPage":"414","endPage":"416","costCenters":[],"links":[{"id":386811,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Maryland","city":"Colesville","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -77.02136993408203,\n 39.06264886527909\n ],\n [\n -76.98051452636719,\n 39.06264886527909\n ],\n [\n -76.98051452636719,\n 39.08397168286113\n ],\n [\n -77.02136993408203,\n 39.08397168286113\n ],\n [\n -77.02136993408203,\n 39.06264886527909\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"15","issue":"2","noUsgsAuthors":false,"publicationDate":"2014-08-18","publicationStatus":"PW","contributors":{"authors":[{"text":"Harrold, L.L.","contributorId":260661,"corporation":false,"usgs":false,"family":"Harrold","given":"L.L.","email":"","affiliations":[],"preferred":false,"id":818424,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ]}