The Marble exploration hole 4 was drilled to determine the chemical and physical properties of marble from the surface to depth of about 1,200 feet. The drill hole is in the north-central part of the Tippipah Spring quadrangle, approximately 40 miles north of Mercury, Nev. The collar of the hole is at an elevation of 5,490.28 feet and has the Nevada State grid coordinates of N. 904,480.13 and E. 637,758.38. The hole is accessible by a graded dirt road easily traversed by heavy construction equipment, that connects to the highway between Mercury and Groom Lake.
\nThe hole was core drilled by Minerals Engineering Company, Grand Junction, Colo., with a 2,000-foot capacity Portadrill drilling rig and conventional NX coring equipment. Drilling was started July 13, and completed August 30, 1959. The drilling fluid was water for most of the hole. At some places in the hole, where loss of drilling fluid was high, the water was thickened with bentonitic mud. At 1,103 feet, presumed caving of the hole caused the drill stem to stick so that it could not be withdrawn; subsequently about 920 feet of the drill stem was recovered. The hole was then reamed to 800 feet and cemented from 785 to 855 feet. A whipstock was emplaced at depth of 805 feet so that the hole, which was vertical to this depth, would be deflected 4° from the vertical. Core was recovered for this part of the hole from 1,088 to 1,187 feet, the total depth. Seven feet of 8-inch outside diameter casing was set from the collar.
\nThis report summarizes the information obtained during preparation of the lithologic log of the core and presents results of chemical analyses of marble samples collected from surface near the drill hole. The report was prepared by the U.S. Geological Survey on behalf of the Albuquerque Operations Office, U.S. Atomic Energy Commission. The writers acknowledge the assistance of Mr. John Foster, drilling foreman for Minerals Engineering Company and Mr. Walter A. Johnson, field engineer for Holmes and Narver, Inc., the engineering-contracting firm.
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Monetary loss from floods in 1953 was much lower than in any one of the preceding 3 years and was less than half the national annual average as computed by the Weather Bureau.
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Floods of 1953 (Water Supply Paper 1320)","largerWorkSubtype":{"id":1,"text":"Federal Government Series"},"language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1320E","collaboration":"Prepared in cooperation with Federal, State, and local agencies","usgsCitation":"Wells, J.V., 1959, Summary of floods in the United States during 1953: U.S. Geological Survey Water Supply Paper 1320, v, 24 p., https://doi.org/10.3133/wsp1320E.","productDescription":"v, 24 p.","startPage":"341","endPage":"364","numberOfPages":"30","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":139013,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1320e/report-thumb.jpg"},{"id":29635,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1320e/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b04e4b07f02db69929a","contributors":{"authors":[{"text":"Wells, J. V. B.","contributorId":57037,"corporation":false,"usgs":true,"family":"Wells","given":"J.","email":"","middleInitial":"V. B.","affiliations":[],"preferred":false,"id":146012,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":61727,"text":"gq119 - 1959 - Surficial geology of the New Britain quadrangle, Connecticut","interactions":[],"lastModifiedDate":"2021-11-10T19:49:19.545083","indexId":"gq119","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":316,"text":"Geologic Quadrangle","code":"GQ","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"119","title":"Surficial geology of the New Britain quadrangle, Connecticut","docAbstract":"No abstract available.
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1959 - Characteristics of tide-effected flow of Brazos River below Freeport, Texas, November 12-13, 1958","interactions":[],"lastModifiedDate":"2012-02-02T00:12:12","indexId":"ofr5946","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","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":"59-46","title":"Characteristics of tide-effected flow of Brazos River below Freeport, Texas, November 12-13, 1958","language":"ENGLISH","doi":"10.3133/ofr5946","usgsCitation":"Grozier, R., 1959, Characteristics of tide-effected flow of Brazos River below Freeport, Texas, November 12-13, 1958: U.S. Geological Survey Open-File Report 59-46, 33 p., 22 figs., https://doi.org/10.3133/ofr5946.","productDescription":"33 p., 22 figs.","costCenters":[],"links":[{"id":184145,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e2e4b07f02db5e4ef6","contributors":{"authors":[{"text":"Grozier, R.U.","contributorId":105704,"corporation":false,"usgs":true,"family":"Grozier","given":"R.U.","affiliations":[],"preferred":false,"id":257633,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":39758,"text":"pp309 - 1959 - The Geology of the Upper Mississippi Valley Zinc-Lead District","interactions":[],"lastModifiedDate":"2017-10-26T14:34:21","indexId":"pp309","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"309","title":"The Geology of the Upper Mississippi Valley Zinc-Lead District","docAbstract":"The upper Mississippi Valley zinc-lead district includes the southwest part of Wisconsin, the northwest corner of Illinois, and a narrow fringe of Iowa extending from Bellevue to McGregor, just west of the Mississippi River. The total area of the district is 4,000 square miles. The entire district is drained by the Mississippi River and its tributaries. The central part is a rolling plain dissected to a depth of about 300 feet by the larger stream valleys. Marginal parts of the district are relatively hilly. Most of the district lies within the so-called \"Driftless Area\", but glacial deposits occur in the eastern, southeastern, and western fringes of the district.
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States","state":"Illinois, Iowa, Wisconsin","otherGeospatial":"Upper Mississippi Valley","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -91.51885986328125,\n 42.02481360781777\n ],\n [\n -89.26391601562499,\n 42.02481360781777\n ],\n [\n -89.26391601562499,\n 43.23719944365308\n ],\n [\n -91.51885986328125,\n 43.23719944365308\n ],\n [\n -91.51885986328125,\n 42.02481360781777\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c671","contributors":{"authors":[{"text":"Heyl, Allen V. 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Jr.","contributorId":14880,"corporation":false,"usgs":true,"family":"Behre","given":"Charles","suffix":"Jr.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":222103,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Flint, Arthur E.","contributorId":45300,"corporation":false,"usgs":true,"family":"Flint","given":"Arthur E.","affiliations":[],"preferred":false,"id":222104,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":177,"text":"wsp1353 - 1959 - Quality of surface waters of the United States, 1954 : Parts 9-14, Colorado River basin to Pacific slope basins in Oregon and lower Columbia river basin","interactions":[],"lastModifiedDate":"2012-02-02T00:05:12","indexId":"wsp1353","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1353","title":"Quality of surface waters of the United States, 1954 : Parts 9-14, Colorado River basin to Pacific slope basins in Oregon and lower Columbia river basin","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1353","usgsCitation":"Water Resources Division, U.S. Geological Survey, 1959, Quality of surface waters of the United States, 1954 : Parts 9-14, Colorado River basin to Pacific slope basins in Oregon and lower Columbia river basin: U.S. Geological Survey Water Supply Paper 1353, xiii, 426 p. :ill., map ;24 cm., https://doi.org/10.3133/wsp1353.","productDescription":"xiii, 426 p. :ill., map ;24 cm.","costCenters":[],"links":[{"id":137360,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1353/report-thumb.jpg"},{"id":24788,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1353/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a8be4b07f02db651bd0","contributors":{"authors":[{"text":"Water Resources Division, U.S. Geological Survey","contributorId":128075,"corporation":true,"usgs":false,"organization":"Water Resources Division, U.S. Geological Survey","id":527217,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":33913,"text":"b1028L - 1959 - Geology of Umnak and Bogoslof Islands, Aleutian Islands, Alaska","interactions":[{"subject":{"id":12861,"text":"ofr5522 - 1955 - The petrology of Umnak and Bogoslof Islands, Alaska","indexId":"ofr5522","publicationYear":"1955","noYear":false,"title":"The petrology of Umnak and Bogoslof Islands, Alaska"},"predicate":"SUPERSEDED_BY","object":{"id":33913,"text":"b1028L - 1959 - Geology of Umnak and Bogoslof Islands, Aleutian Islands, Alaska","indexId":"b1028L","publicationYear":"1959","noYear":false,"chapter":"L","title":"Geology of Umnak and Bogoslof Islands, Aleutian Islands, Alaska"},"id":1}],"lastModifiedDate":"2012-02-02T00:09:28","indexId":"b1028L","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1028","chapter":"L","title":"Geology of Umnak and Bogoslof Islands, Aleutian Islands, Alaska","language":"ENGLISH","publisher":"U.S. Govt. 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Off.,","doi":"10.3133/b1028L","usgsCitation":"Byers, F., 1959, Geology of Umnak and Bogoslof Islands, Aleutian Islands, Alaska: U.S. Geological Survey Bulletin 1028, p. 267-369, ill., maps ;23 cm., https://doi.org/10.3133/b1028L.","productDescription":"p. 267-369, ill., maps ;23 cm.","costCenters":[],"links":[{"id":109178,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_20598.htm","linkFileType":{"id":5,"text":"html"},"description":"20598"},{"id":96186,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1028l/report.pdf","size":"10553","linkFileType":{"id":1,"text":"pdf"}},{"id":163062,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1028l/report-thumb.jpg"},{"id":61803,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1028l/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":61804,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1028l/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":61805,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1028l/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":61806,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1028l/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":61807,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1028l/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b08e4b07f02db69b96e","contributors":{"authors":[{"text":"Byers, F.M. Jr.","contributorId":78338,"corporation":false,"usgs":true,"family":"Byers","given":"F.M.","suffix":"Jr.","affiliations":[],"preferred":false,"id":212164,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":33740,"text":"b1077 - 1959 - Geology of the Lake Mary quadrangle, Iron County, Michigan","interactions":[{"subject":{"id":12610,"text":"ofr565 - 1956 - Preliminary report on the geology of Lake Mary quadrangle, Iron County, Michigan","indexId":"ofr565","publicationYear":"1956","noYear":false,"title":"Preliminary report on the geology of Lake Mary quadrangle, Iron County, Michigan"},"predicate":"SUPERSEDED_BY","object":{"id":33740,"text":"b1077 - 1959 - Geology of the Lake Mary quadrangle, Iron County, Michigan","indexId":"b1077","publicationYear":"1959","noYear":false,"title":"Geology of the Lake Mary quadrangle, Iron County, Michigan"},"id":1}],"lastModifiedDate":"2016-08-26T14:32:11","indexId":"b1077","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1077","title":"Geology of the Lake Mary quadrangle, Iron County, Michigan","docAbstract":"The Lake Mary quadrangle is in eastern Iron County, in the west part of the Upper Peninsula of Michigan. The quadrangle is underlain by Lower and Middle Precambrian rocks, formerly designated Archean and Algonkian rocks, and is extensively covered by Pleistocene glacial deposits. A few Upper Precambrian (Keweenawan) diabase dikes and two remnants of sandstone and dolomite of early Paleozoic age are also found in the area.
The major structural feature is the Holmes Lake anticline, the axis of which strikes northwest through the northeast part of the quadrangle. Most of the quadrangle, therefore, is underlain by rock of the west limb of the anticline. To the northwest along the fold axis, the Holmes Lake anticline is separated from the Amasa oval by a saddle of transverse folds in the vicinity of Michigamme Mountain in the Kiernan quadrangle.
The Lower Precambrian rocks are represented by the Dickinson group and by porphyritic red granite whose relation to the Dickinson group is uncertain, but which may be older. The rocks of the Dickinson group are chiefly green to black metavolcanic schist and red felsite, some of the latter metarhyolite. The dark schist is commonly magnetic. The Dickinson group underlies the core area of the Holmes Lake anticline, which is flanked by steeply dipping Middle Precambrian formations of the Animikie series.
A major unconformity separates the Lower Precambrian rocks from the overlying Middle Precambrian rocks. In ascending order the formations of the Middle Precambrian are the Randville dolomite, the Hemlock formation, which includes the Mansfield iron-bearing slate member, and the Michigamme slate. An unconformity occurs between the Hemlock formation and Michigamme slate. The post-Hemlock unconformity is thought to be represented in the Lake Mary quadrangle by the absence of iron-formation of the Amasa formation, which is known to lie between the Hemlock and the Michigamme to the northwest of the Lake Mary quadrangle in the Crystal Falls quadrangle. Post-Hemlock erosion may account also for the absence of iron-formation of the Fence River formation on the east limb of the Holmes Lake anticline within the Lake Mary quadrangle.
The Randville dolomite is not exposed and is known only from diamond drilling in the northeast part of the area where it occurs in the east and west limbs of the Holmes Lake anticline. The formation has a maximum thickness of about 2,100 feet; this includes a lower arkosic phase, some of which is quartz pebble conglomerate, a medial dolomitic phase, and an upper slate phase. The triad is gradational. Included within the formation are a few beds of chloritic schist thought to be of volcanic origin. An unconformity between the Randville and the succeeding Hemlock is not indicated in the quadrangle, but is probably present.
The Hemlock formation is best exposed in the northwest and south-central parts of the area. The apparent thickness of the formation is 10,000- 17,000 feet. It is composed mainly of mafic metavolcanic rocks and intercalated slate and iron-formation. In the north part of the quadrangle the volcanic rocks are greenstone, which includes altered basaltic flow rocks, volcanic breccia, tuff, and slate. Pillow structures are common in the metabasalt. It is not certain if any Hemlock rocks are present in the east limb of the Holmes Lake anticline. In the south part of the quadrangle, the rocks of the Hemlock are chiefly chlorite and hornblende schist and hornfels. Pyroxene hornfels is sparingly present.
At least two sedimentary slate belts are included in the Hemlock formation. One of these, the Mansfield iron-bearing slate member, includes in its upper part an altered chert-siderite iron-formation 30 to over 150 feet thick from which iron ore has been mined at the Mansfield location. The position of the iron-bearing rocks has been determined magnetically, and past explorations for iron ore are discussed.
Though probably; unconformable, the contact between the Hemlock and the Michigamme formations appears conformable. The Michigamme slate consists of at least 4,000 feet of interbedded mica schist and granulite, the altered equivalents of the slate and graywacke characteristic of the Michigamme in adjacent areas. The Michigamme rocks are best exposed in the south part of the quadrangle in the vicinity of Peavy Pond.
Two periods of regional metamorphism have resulted in the alteration of almost all of the rocks of the quadrangle. The Lower Precambrian rocks underwent at least one period of metamorphism, uplift, and erosion before the deposition of the Randville dolomite. After the deposition of the Michigamme slate, a post-Middle Precambrian period of regional metamorphism occurred with attending deformation and igneous intrusion. The grade of metamorphism rises toward the south in the area. The rocks in the northern two-thirds of the quadrangle are representative of greenschist facies of regional metamorphism, whereas the rocks in the southern onethird of the quadrangle are representative of the albite-epidote-amphibolite, the amphibolite, and the pyroxene hornfels facies, the metamorphic node centering about the intrusive Peavy Pond complex in the Peavy Pond area.
The Precambrian sedimentary and volcanic rocks are cut by intrusive igneous rocks of different types and several different ages. Gabbroic sills and dikes invaded the Hemlock rocks at some time after the Hemlock was deposited and before the post-Middle Precambrian orogeny and metamorphism. Some contact metamorphism attended the intrusion of the major sills. One of the sills, the West Kiernan sill, is well differentiated. A syntectonic igneous body, composed of gabbro and minor ultramafic parts and fringed with intermediate and felsic differentiates and hybrids, the Peavy; Pond complex, was intruded into the Hemlock and Michigamme formations during the post-Middle Precambrian orogeny. The complex is situated in the Peavy Pond area at the crest of the regional metamorphic node. Contact-altered sedimentary and volcanic rocks margin the complex.
The effects of regional metamorphism have been superposed on the contact metamorphic rocks peripheral to the complex and on the igneous rocks of the complex as well. The mafic augite-bearing rocks of the complex emplaced early in the orogeny were deformed by granulation at the peak of the deformation and subsequently metamorphosed to hornblende rocks. Some of the intermediate and felsic rocks of the complex were foliated by the deformation, while the more fluid, felsic parts of the complex were intruded under orogenic stress and crystallized after the peak of deformation. The deformation culminated in major faulting during which the formations were dislocated, and some of the granite of the complex was extremely brecciated.
A few diabase dikes, probably of Keweenawan age, have intruded the deformed and altered Animikie rocks.
The only known metallic resource is iron ore. The Mansfield mine produced 1¥2 million tons of high-grade iron ore between the years 1890 and 1913. Sporadic exploration since 1913 has failed to reveal other ore deposits of economic importance.
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S.","contributorId":16807,"corporation":false,"usgs":true,"family":"Pomeroy","given":"J.","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":275184,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":14101,"text":"ofr5954 - 1959 - Occurrences of alunite, pyrophyllite, and clays in the Cerro La Tiza area, Puerto Rico","interactions":[],"lastModifiedDate":"2023-07-17T12:11:43.302622","indexId":"ofr5954","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","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":"59-54","title":"Occurrences of alunite, pyrophyllite, and clays in the Cerro La Tiza area, Puerto Rico","docAbstract":"A deposit of hydrothermally altered rocks in the Cerro La Tiza area located between the towns of Comerio and Aguas Buenas, approximately 25 kilometers southwest of San Juan, Puerto Rico, was mapped and studied to determine the principal minerals, their extent distribution and origin, and the possibility of their economic utilization, especially in Puerto Rico. The Cerro la Tiza area is about 71/2 kilometers long, has an average width of about 11/2 kilometers and embraces a total area of approximately 15 square kilometers. The principal mineralized zone, a dike-like mass of light-colored rocks surrounded by dark-colored volcanic country rocks, occupies the crest and upper slopes of east-trending Cerro La Tiza ridge and is believed to be of Late Cretaceous or Eocene age. This zone is approximately 5,300 meters long, 430 meters wide and has an area of approximately 225 hectares (556 acres). The rocks of the mineralized zone are of mixed character and consist mainly of massive quartzose rocks and banded quartz-alunite rocks closely associated with foliated pyrophyllitic, sericitic and clayey rocks. The principal minerals in probably order of abundance are quartz, alunite, pyrophyllite, kaolin group clays (kaolinite and halloysite) and sericite. Minerals of minor abundance are native sulfure, diaspore, svanbergite (?), sunyite (?), hematite, goethite, pyrite, rutile (?) and very small quantities of unidentified minerals. The mineralized zone has broken down to deposits of earth-rock debris of Quaternary age that cover much of the slopes and flanks of Cerro La Tiza. This debris consists generally of fragments and boulders with a very large size range embedded in a clayey matrix. The distribution of the earth-rock debris with respect to the present topography and drainage suggests that it may have undergone at least two cycles of erosion. Underlying the earth-rock debris and completely enclosing the mineralized zone are country rocks of probably Late Cretaceous age. These consist principally of low flows and volcanic and flow breccias but contain thin interbedded siltstones and sandstones. The lavas are generally predominant at the western end of the area and the breccias at the eastern end. The mineralized zone and the country rocks are sheared along two predominant directions that are approximately N 70 degrees E and N 70 degrees W. The ridge of Cerro La Tiza appears to be a broad shear zone through which hydrothermal emanations gained access to the country rocks. The emanations are believed to have originated from intrusive rocks that probably underlie the area. The surrounding area contains both large and small exposed intrusive bodies. The largest one is the San Lorenzo batholith of Late Cretaceous or Eocene age whose exposed northwest edge is approximately 19 kilometers southeast of the eastern end of the Cerro La Tiza area. Other zones of hydrothermally altered rocks were discovered along a mineralized belt extending eastward from Cerro La Tiza through the Rio Gurabo Valley nearly to the Vieques Passage bordering the east coast of Puerto Rico. Other zones were discovered north and south of this belt and still others were found circumventing the San Lorenzo batholith. The most abundant minerals of the mineralized zone can be exploited for economic utilization in Puerto Rico. Alunite can be utilized in the manufacture of aluminum sulfate for water purification. It can also be used in the manufacture of alumina refractory materials. Pyrophyllite can be used as a carrier for insecticides and fungicides. It can also be utilized for the manufacture of ceramic products, as a filler in the soap industry and as a carrier for paint pigments. Kaolinite can be used in the ceramic industry and in the manufacture of glass as a substitute for feldspar. Halloysite might be utilized as a catalyst support in the cracking of petroleum. Tonnages of reserve ore on Cerro La Tiza are calculated to be 1,590,000 inferred short tons (1,440,000,000 inferred metric tons) of mixed minerals. These tonnages are based on the assumption that the depth of the mineralized zone is one-half of the exposed width. The deposit is well situated for open pit mining, but because of the existing cover of earth-rock debris, soil foliage, exploration should proceed exploitation for better determination of the most promising areas containing the best concentrations of the minerals sought.
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