The mineral barite, barium sulfate, is the chief source of barium and its compounds needed for many industrial processes and products. Barite is found the world over and is abundant and widely distributed throughout the United States. The barite deposits of the United States (exclusive of Alaska and Hawaii) are shown on the accompanying map. The principal geologic type of deposit is indicated by the shape of symbol and the relative importance of the deposit is indicated by the size of symbol.
This text lists localities by State, and index numbers are keyed to the map. Localities are distinguished by name of mine, prospect, or geographic area; their coordinates are given to the nearest minute of latitude and longitude. Geologic relations of each occurrence, if known, are summarized briefly. The text and map were compiled from published and unpublished information, and at least one reference is given for each locality, if reports have been published. The listings in some States are preceded by a principal reference which is a major source of information about deposits in those States.
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Known tin-bearing deposits in the conterminous United States are small, few in number, and widely scattered; only small amounts of tin concentrates are being recovered at the present time (1964). The total amount of metallic tin produced since 1950, mainly as a by-product of molybdenum ores, is less than 500 tons, and the total production from all sources prior to 1950 is similar.
Map locations are shown by symbols, the shapes of which denote different geologic types of occurrence; some areas of scattered occurrences in pegmatites are shown by a stippled pattern. Occurrences are numbered by State on the map and identified by number in the index. The index also gives the geographic coordinates, brief geologic descriptions, and references to the principal published reports. The more important or better known localities are named on the map.
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","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/pp441","usgsCitation":"Iorns, W.V., Hembree, C.H., and Oakland, G.L., 1965, Water resources of the Upper Colorado River Basin - Technical report: U.S. Geological Survey Professional Paper 441, Report: iv, 370 p.; 9 Plates: 31.50 in. x 39.75 in. or smaller, https://doi.org/10.3133/pp441.","productDescription":"Report: iv, 370 p.; 9 Plates: 31.50 in. x 39.75 in. or smaller","numberOfPages":"405","costCenters":[{"id":114,"text":"Alaska Science Center","active":true,"usgs":true},{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":33023,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0441/plate-1.pdf","text":"Plate 1","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map of Upper Colorado River Basin showing the distribution of hydrologic units and average annual precipitation"},{"id":33032,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0441/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":121448,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0441/report-thumb.jpg"},{"id":33031,"rank":11,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0441/plate-9.pdf","text":"Plate 9","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map of the native vegetation zones and irrigated lands in the San Juan division, Upper Colorado River basin"},{"id":33030,"rank":10,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0441/plate-8.pdf","text":"Plate 8","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map of San Juan division, Upper Colorado River basin, showing average annual precipitation and evaporation, key streamflow-gaging stations, and coefficients of variation of annual runoff"},{"id":33029,"rank":9,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0441/plate-7.pdf","text":"Plate 7","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map of the native vegetation zones and irrigated lands in the Green division, Upper Colorado River basin"},{"id":33028,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0441/plate-6.pdf","text":"Plate 6","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map of Green division, Upper Colorado River basin, showing average annual precipitation and evaporation, key streamflow-gaging stations, and coefficients of variations of annual runoff"},{"id":33027,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0441/plate-5.pdf","text":"Plate 5","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map of the native vegetation zones and irrigated lands in the Grand division, Upper Colorado River basin"},{"id":389573,"rank":12,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4435.htm","text":"Water resources of the upper Colorado River Basin - 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1965 - Geology of the Romanzof Mountains, Brooks Range, northeastern Alaska","interactions":[{"subject":{"id":15753,"text":"ofr65141 - 1965 - Geology of the Romanzof Mountains, Brooks Range, northeastern Alaska","indexId":"ofr65141","publicationYear":"1965","noYear":false,"title":"Geology of the Romanzof Mountains, Brooks Range, northeastern Alaska"},"predicate":"SUPERSEDED_BY","object":{"id":6313,"text":"pp897 - 1977 - Geology of the western Romanzof Mountains, Brooks Range, northeastern Alaska","indexId":"pp897","publicationYear":"1977","noYear":false,"title":"Geology of the western Romanzof Mountains, Brooks Range, northeastern Alaska"},"id":1},{"subject":{"id":15754,"text":"ofr59106 - 1959 - Preliminary report on sedimentary and metamorphic rocks in part of the Romanzof Mountains, Brooks Range, northeastern Alaska","indexId":"ofr59106","publicationYear":"1959","noYear":false,"title":"Preliminary report on sedimentary and metamorphic rocks in part of the Romanzof Mountains, Brooks Range, northeastern Alaska"},"predicate":"SUPERSEDED_BY","object":{"id":15753,"text":"ofr65141 - 1965 - Geology of the Romanzof Mountains, Brooks Range, northeastern Alaska","indexId":"ofr65141","publicationYear":"1965","noYear":false,"title":"Geology of the Romanzof Mountains, Brooks Range, northeastern Alaska"},"id":2}],"supersededBy":{"id":6313,"text":"pp897 - 1977 - Geology of the western Romanzof Mountains, Brooks Range, northeastern Alaska","indexId":"pp897","publicationYear":"1977","noYear":false,"title":"Geology of the western Romanzof Mountains, Brooks Range, northeastern Alaska"},"lastModifiedDate":"2024-03-25T18:59:14.568941","indexId":"ofr65141","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","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":"65-141","title":"Geology of the Romanzof Mountains, Brooks Range, northeastern Alaska","docAbstract":"This remote 700 square mile area in the Brooks Range is topographically rugged and geologically diverse; it contains a granitic pluton, low-grade metamorphic rocks, sedimentary rocks, and mafic igneous rocks, as well as glacial features.
Rocks of sedimentary origin include from oldest to youngest:
1.Neruokpuk Formation Middle and Upper Devonian(?), more than 4000 feet thick, a variety of units which represent the greenschist facies, including quartzitic- and schistose-feldspathic graywacke; phyllite, argillite, and slate, as well as dark limestone, sandy limestone, and silicified carbonate rocks. The succession of units in parts of the area is uncertain. Correlations between these units and with others in the eastern Brooks Range are provisional.
2.Kekiktuk Conglomerate and Kayak(?) Shale (Upper Devonian(?) to Upper Mississippian), a single map unit, from absent(?) to 400+ feet thick, containing dark shale Kayak(?) in its uppermost part and quartzite, interbedded dark shale, and some pebble- to boulder-conglomerate in the locally absent lower part (Kekiktuk). The unit overlies the Neruokpuk with angular unconformity, which may reflect either a pre-Kayak(?) or pre-Kekiktuk hiatus or both.
3.Lisburne Group, almost entirely carbonate rocks, and relatively thin in this area, 600 to 800 feet thick. Alapah Limestone (Upper Mississippian), to 560 feet thick, includes gray sandy, crystalline, and cherty limestone; minor dark shale; and dark cherty carbonate rocks in the upper part. The lower contact is gradational with the Kayak(?). Wahoo(?) Limestone (Pennsylvanian(?) to Permian) conformably overlies the Alapah, is absent to 200+ feet thick, and is characterized by light-gray crinoidal limestones in its upper part.
4. Sadlerochit Formation, consisting of three intraconformable units: ferruginous sandstone member (Permian) of ironstained orthoquartzite and dark slate, 175 to 240 feet thick which unconformably overlies the Wahoo(?) and Alapah Limestones; shale member of dark shale, slate, and minor quartzite averaging 400 feet in thickness; and quartzite member (Lower(?) Triassic), 700 feet thick, mostly orthoquartzite with minor shale and conglomerate. The basal clastics were probably shed from the north.
5.Shublik Formation (Middle(?) and Upper Triassic), 600 to 700 feet thick, with the thin phosphatic sandstone member overlain by dark phosphatic limestones and limy shales of the limestone member.
6.Kingak Formation (Jurassic), more than 1000 feet thick. The siltstone member, resistant sandstone and siltstone 75 to 150 feet thick, is overlain by an undetermined thickness of black shale. The basal part contrasts sharply with the underlying Shublik, indicating possible disconformity.
7.Ignek(?) Formation (Cretaceous), represented in the foothills where lithic graywacke, shale, and coaly shale constitute the few exposures examined.
8.Glacial and glaciofluvial materials of five advances recognized on the basis of morphology and position, which are tentatively correlated with five glaciations 15 miles west of the area.
9. Recent alluvial and colluvial deposits including fans which appear to represent at least three stages of encroachment.
The Ramanzof granite, exposed in the Okpilak batholith and Jago stock, is mostly light-gray quartz monzonite to granite, and contains essential quartz, perthitic microcline, albite-oligoclase, and partly chloritized biotite. Limited modal and chemical data are presented. Three textural facies are: 1) porphyritic (marginal), with abundant large microcline megacrysts; 2) variable (middle to marginal), which exhibits textural and mineralogical banding; and 3) coarse (inner to marginal), which is gneissoid to equigranular. Facies relationships appear to be mostly gradational but may be locally intrusive. Some schistose metasedimentary(?) rock occurs in the granite. Aplite dikes, inclusions, tourmaline veins and replacements, and chlorite and quartz veins are locally common, as well as quartz monzonite and mafic igneous dikes. Contacts with Neruokpuk Formation rocks are mostly abrupt, concordant to cross-cutting, and locally adjoin tactite and hornfels of the albite-epidote-hornfels and hornblende-hornfels facies. Contacts with Kekiktuk Conglomerate are apparently gradational through a schistoze zone. Both primary and secondary structural elements are present in the Romanzof in granite. Textural and mineralogical banding and, in general, feldspar foliation are considered to be primary in origin; biotite foliation, gneissic and schistose foliation, and schistose zones are considered secondary. Lead-alpha age of zircons appears to be Late Devonian, K-Ar age of biotite is Cretaceous, possibly indicating updating by later reheating. Field age relationships are inconclusive but suggest pre-Kayak(?) (Upper Devonian) granite emplacement. The pluton is interpreted to be essentially the product of melt crystallization, synorogenically emplaced by forceful injection with minor stoping, and may include marginally granitized rock.
Mafic igneous rocks of altered basaltic composition (greenstones) include dikes in granitic and Neruokpuk Formation rocks, and volcanics(?). A late Paleozoic age is suggested for them.
Structural grain strikes east-northeast; south-dipping elements are common. Structures include the major positive nature of the area (first order), relatively broad folds (second order) which contain small tight folds (third order). Related south-dipping cleavage, schistosity, and biotite foliation in granite in the northern part of the area are cut by prominent sets of transverse joints and faults. Other features are longitudinal normal and reverse faults, at least one large-scale overthrust fault, and sheared zones in granite with possible attendant retrograde metamorphism.
Although Mesozoic and Tertiary deformational features are dominant in northern Alaska, the Romanzof area may have been part of a Late Devonian orogenic belt continuous with one in northern Canada. Three alternate trends of such a belt in northern Alaska are discussed, but evidence is inconclusive.
The mineral potential of the area is largely unknown. Minor amounts of metallic sulfides and oxides are present in granite and Neruokpuk Formation rocks. Analyses of stream silt samples suggest the possibility of tin and beryllium potential. The Shublik Formation contains rock phosphate.
In the central York Mountains, carbonate rocks of Lower and Middle Ordovician age and aggregating at least 8,000 feet thick are thrust northward over slate and argillaceous limestone of pre-Ordovician age which were intruded by gabbro in pre-Ordovician time. Normal faults of four distinct systems cut the thrust plates, and in Late Cretaceous time, stocks of biotite granite, abnormally rich in beryllium, tin, boron and certain other trace elements, pierced the thrust plates. In part following the intrusion of the granites, a strong set of normal faults developed striking N. 60°-85° E. through the central York Mountains and locally these faults cut the granites. Dikes of granite, rhyolite porphyry, and lamprophyre were injected into some of these faults, the lamprophyres being younger. Trace elements in the lamprophyres prove they are mafic rocks probably derived from the lama, and that they cannot be related genetically to granite. Shortly after the intrusion of lamprophyre dikes, ore deposits of tin, beryllium, and fluorite were formed from solutions probably derived from deeply-buried hot granite where the granite was ruptured by normal faults. Ore shoots were localized beneath thrust faults where the faults are intruded by dikes, and a major ore-bearing structure, the Rapid River fault, is mineralized for half its length for a distance of eight miles. The tin deposits contain cassiterite and stannite in topaz greisen with abundant sulfides of copper, lead, zinc, and iron, as well as wolframite. The beryllium deposits contain fluorite, chrysoberyl, diaspore, muscovite, and tourmaline, with trace to small amounts of euclase, bertrandite, helvite, phenikite(?), todorokite and hematite. Beryl occurs sparingly in late veins of quartz and fluorite. Chrysoberyl is the earliest and commonest beryllium mineral, followed by euclase and bertrandite, and then phenakite(?) and beryl. Helvite is restricted to banded skarns near granite, and which consist of magnetite and fluorite. Throughout the district, a strong zonation is displayed from tin deposits in greisen through transitional veins of sulfide minerals with fluorite and chrysoberyl to fluorite-beryllium deposits and thence to barren veins of silica and fluorite with trace amounts of beryllium. This zonal arrangement of deposits probably will be found elsewhere in the world where greisen tin deposits occur in carbonate rocks. The geochemical cycle of the trace elements Be, Sn, W, B, Li, Cu, Pb, Zn and Nb shows that these elements were enriched in the biotite granites and were strongly fractionated among the minerals of granites. Fran the granites, these rare elements moved outward into contact rocks and ore deposits. During the supergene cycle, clear geochemical anomalies were formed in stream sediments, soils and plants near ore deposits, and geochemical prospecting led to the discovery of the beryllium lodes. With the possible exception of zinc and niobium, the rare elements that are associated in the rocks and ores remain associated in the supergene processes. Fixation of zinc in clay soil and tundra plants may account for the relatively small amount of zinc in strew sediments.
Datable Pleistocene events in the York Mountains begin with the Yarmouth Interglaciation when the York Terrace, a wide marine platform, was cut. In Illinoian time, the York Terrace was uplifted almost 400 feet, and during the Sangamon Interglaciation a second marine platform (Lost River Terrace) was cut and is not deformed. During Wisconsin time the widespread York Glaciation was followed by the more restricted Mint River Glaciation. Because uplift of the York Terrace extended into the Bering Strait, it is probable that prior to the uplift in Illinoian time the Bering Strait was a seaway and a barrier to land migration rather than a land bridge.
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Notable changes in land level occurred over an area in excess of 50,000 square miles in a broad northeast-trending belt more than 500 miles long and as much as 250 miles wide, which lies between the Aleutian Trench and the Aleutian Volcanic Arc. The northwest part of this belt, which includes most of the Kenai Peninsula and the Kodiak Island group, sank as much as 7 feet, bringing some roads, rail lines, docks, and settlements within reach of high tides and producing a fringe of salt-water-killed vegetation along the drowned coasts. The area to the southeast, including most of Prince William Sound and the adjacent continental shelf as far south as southern Kodiak Island, rose generally 4 to 8 feet, and locally at least 33 feet. Some beaches and surf-cut platforms were permanently raised above the reach of tides, resulting in mass extermination of intertidal faunas and floras and impaired usefulness of harbors, channels, and many shoreline installations.
Surface faulting was confined to Montague Island, and was dominantly vertical and subsidiary to regional uplift. Of the two known faults one has been traced more than 16 miles on land and about 15 miles in the submarine topography to the southwest of the island. Maximum measured vertical fault displacement on land was 16 feet on one fault and about 18 feet on the other.
Submarine uplift of the continental shelf generated a train of long-period large-amplitude seismic sea waves, the first of which struck the outer coasts of the Kenai Peninsula and Kodiak Island between 19 and 30 minutes after the initial shock. The highest waves inundated shorelines locally to elevations of 35 to 40 feet, causing 20 deaths and damage to property all along the coast of the Gulf of Alaska, especially in those areas that had been lowered relative to sea level by tectonic subsidence. The sea waves were recorded on tide gauges throughout the Pacific Ocean and resulted in casualties and local damage at points as distant as British Columbia, Oregon, and California.
The earthquake caused widespread subaqueous sliding and sedimentation in Prince William Sound, along the south coast of the Kenai Peninsula, and in Kenai Lake. These slides carried away the port facilities of Seward and Valdez and the small boat harbor at Homer. Local violent surges of water, many of which were generated by known subaqueous slides that occurred during the earthquake, left swash marks as much as 170 feet above water level and caused heavy damage and took 85 lives at Seward, Valdez, Whittier, Chenega, and several smaller communities in Prince William Sound.
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George","contributorId":3920,"corporation":false,"usgs":false,"family":"Plafker","given":"George","email":"","affiliations":[],"preferred":false,"id":182713,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Mayo, L.R.","contributorId":21541,"corporation":false,"usgs":true,"family":"Mayo","given":"L.R.","email":"","affiliations":[],"preferred":false,"id":182714,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70112253,"text":"70112253 - 1965 - Photointerpretation of Alaskan post-earthquake photography","interactions":[],"lastModifiedDate":"2017-03-27T13:40:15","indexId":"70112253","displayToPublicDate":"1990-06-12T09:35:00","publicationYear":"1965","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3051,"text":"Photogrammetric Engineering","active":true,"publicationSubtype":{"id":10}},"title":"Photointerpretation of Alaskan post-earthquake photography","docAbstract":"Aerial photographs taken after the March 27, 1964, Good Friday, Alaskan earthquake were examined stereoscopically to determine effects of the earthquake in areas remote from the towns, highways, and the railroad. The two thousand black and white photographs used in this study were taking in April, after the earthquake, by the U. S. Coast & Geodetic Survey and were generously supplied to the U. S. Geological Survey. Part of the photographs, at a scale of 1/24,000, provide blanket coverage of approximately 2,000 square miles of land area north and west of Prince William Sound, including parts of the mainland and some of the adjacent islands. The epicenter of the earthquake, near the head of Unakwik Inlet, is located in this area. The rest of the photographs, at scales ranging from 1/17,000 to 1/40,000, cover isolated strips of the coastline of the mainland and nearby islands in the general area of Prince William Sound.
\nFigure 1 shows the area of new photo coverage used in this study. The objective of the study was to determine quickly whether geological features resulting from the earthquake, such as faults, changes in shoreline, cracks in surficial material, pressure ridges in lake ice, fractures in glaciers and lake ice, and rock slides and avalanches, might be identifiable by photointerpretation. The study was made without benefit of comparisons with older, or pre-earthquake photography, which was not readily available for immediate use.
","language":"English","publisher":"American Society of Photogrammetry","publisherLocation":"Falls Church, VA","usgsCitation":"Hackman, R., 1965, Photointerpretation of Alaskan post-earthquake photography: Photogrammetric Engineering, v. 31, no. 4, p. 604-610.","productDescription":"7 p.","startPage":"604","endPage":"610","numberOfPages":"7","costCenters":[{"id":222,"text":"Earth Resources Observation and Science (EROS) Center","active":true,"usgs":true}],"links":[{"id":288442,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -150.0122,59.6906 ], [ -150.0122,61.8408 ], [ -144.9482,61.8408 ], [ -144.9482,59.6906 ], [ -150.0122,59.6906 ] ] ] } } ] }","volume":"31","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"539acc05e4b0e83db6d08f77","contributors":{"authors":[{"text":"Hackman, R.J.","contributorId":95086,"corporation":false,"usgs":true,"family":"Hackman","given":"R.J.","email":"","affiliations":[],"preferred":false,"id":686346,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70197612,"text":"70197612 - 1965 - Ordovician, Silurian, and Devonian biostratigraphy of east-central Alaska","interactions":[],"lastModifiedDate":"2023-02-01T14:25:21.059833","indexId":"70197612","displayToPublicDate":"1965-12-31T00:00:00","publicationYear":"1965","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":701,"text":"American Association of Petroleum Geologists Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Ordovician, Silurian, and Devonian biostratigraphy of east-central Alaska","docAbstract":"A predominantly shale and chert sequence has been mapped from the Canadian border at Latitude 65°00′ N. to the Nation River about 25 miles northwest. It has Ordovician and Silurian graptolites in the lower half, and Middle Devonian corals and Upper Devonian spores in the upper half.
The lower half of the sequence consists of about 400 to 900 feet of predominantly dark gray graptolitic shale with lesser amounts of grayish black laminated chert. This unit has been traced by Green and Roddick from the international border southeastward into the Dawson area of the Yukon Territory and northeastward into the Ogilvie and Richardson Mountains where it has been mapped by Jackson & Lenz, Norris, and others as the Road River Formation. In the Tatonduk-Nation Rivers area the Road River Formation rests disconformably on a sequence of Middle and Upper Cambrian limestone that locally may include Lower Ordovician (Tremadoc) beds at its top. The sequence of graptolite faunas from the Road River Formation in Alaska is essentially the same as the graptolite zones established by Elles and Wood in Great Britain. All the standard series of the Ordovician and Silurian are probably represented in the formation with the exception of the Tremadoc and possibly the Arenig and Wenlock.
Overlying the Road River Formation is a formation, 200 to 800 feet thick, consisting predominantly of thinly bedded and laminated light gray to black chert and siliceous shale that is here named the McCann Hill Chert. This new formation disconformably overlies the Road River Formation, and its lower boundary is at the base of a distinctive limestone and shale member. The basal limestone and shale member of the McCann Hill Chert contains a remarkably varied fauna including corals, brachiopods, trilobites, conodonts, ostracods, and fish of Eifelian (early Middle Devonian) age. Spores from the upper part of the formation resemble those from the overlying Nation River Formation and indicate a Late Devonian age. The McCann Hill Chert is conformably overlain by the Nation River Formation—a thick succession of inter-bedded graywacke, chert conglomerate, and silty shale of Late Devonian age.
In the vicinity of Jones Ridge, only 7 miles north of exposures of the Road River Formation, Upper Cambrian limestone is overlain by a pure limestone section containing Ordovician, Middle Devonian, and perhaps Silurian shelly faunas contemporaneous with the Road River Formation and the thinner basal limestone and shale member of the McCann Hill Chert. The rapid change from graptolitic shale to limestone probably reflects changes in conditions of sedimentation, but could be a result of thrust faulting.
The Tatonduk-Nation Rivers area seems to lie in a transitional zone between an early Paleozoic eugeosynclinal belt south of the Yukon River and a contemporaneous miogeosynclinal belt along the Porcupine River. One puzzling feature of the lower Paleozoic sequence in the Tatonduk-Nation Rivers area is its thinness in contrast to the much thicker volcanic and detrital sequence on the south and the considerably thicker carbonate sequence on the north.
","language":"English","publisher":"American Association of Petroleum Geologists","doi":"10.1306/A6633526-16C0-11D7-8645000102C1865D","usgsCitation":"Churkin, M., and Brabb, E.E., 1965, Ordovician, Silurian, and Devonian biostratigraphy of east-central Alaska: American Association of Petroleum Geologists Bulletin, v. 49, no. 2, p. 172-185, https://doi.org/10.1306/A6633526-16C0-11D7-8645000102C1865D.","productDescription":"14 p.","startPage":"172","endPage":"185","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":355007,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"Nation-Tatonduk Rivers area","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -142.38695878694335,\n 65.46836165464507\n ],\n [\n -142.38695878694335,\n 64.62502455781637\n ],\n [\n -141.00230856836862,\n 64.62502455781637\n ],\n [\n -141.00230856836862,\n 65.46836165464507\n ],\n [\n -142.38695878694335,\n 65.46836165464507\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"49","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Churkin, Michael Jr.","contributorId":62566,"corporation":false,"usgs":true,"family":"Churkin","given":"Michael","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":737908,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Brabb, Earl E.","contributorId":8545,"corporation":false,"usgs":true,"family":"Brabb","given":"Earl","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":737909,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70222078,"text":"70222078 - 1965 - Biota of a late glacial rocky mountain pond","interactions":[],"lastModifiedDate":"2021-07-16T13:23:47.276661","indexId":"70222078","displayToPublicDate":"1965-07-16T08:15:55","publicationYear":"1965","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":"Biota of a late glacial rocky mountain pond","docAbstract":"The sediments of a late glacial sag pond in Huerfano Park, south-central Colorado, have yielded a varied biota consisting of vertebrates, terrestrial and fresh-water mollusks, sponges, and pollen. Wood from the sediments has a radiocarbon age of 9600 ± 200 years. The vertebrate fauna contains the tooth of a prairie dog and the remains of frog, salamander, snake, and fish—all characteristic of present-day montane lakes and ponds and their margins in Colorado. The mollusks are all living species, and the fauna is dominated by gastropods. With the exception of one form (Vitrina alaskana Dall), whose known range does not extend as far south as Huerfano Park, the fauna is not significantly different from the mollusks living in the area today. The sediments also contain an abundant and unusually diversified sponge fauna in which as many as six species may be represented. A pollen spectrum from the sediments is composed of arboreal pollen characteristic of the present-day Transition Zone flora which, in Colorado, grows on the upper edge of the Great Plains and all of the foothills belt.
Vertical variation in the sediment types and the enclosed biota makes it possible to recreate the changing depositional environment and local climate throughout the life of the pond. The basal sediments, interbedded marl and clastic materials, are interpreted as indicating deposition during alternating wet and dry periods. A bed of nearly pure calcium carbonate marl, which reaches a thickness of 2 feet, forms the middle stratigraphic unit. It is highly fossiliferous and is thought to have been deposited during a warm dry period with relatively mild winters. The uppermost stratigraphic unit is a gray carbonaceous clay which filled the basin as vegetation encroached upon the lake and the lake itself was reduced to a marsh.
Because of the radiocarbon age and the reconstruction of the climate based upon faunal and sedimentological changes, the lower two stratigraphic units are thought to correlate with the Lubbock Subpluvial, and the uppermost unit, the gray carbonaceous clay, with the early part of the Yellow House Interval as described in the Llano Estacado, New Mexico.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1965)76[1203:BOALGR]2.0.CO;2","usgsCitation":"Kauffman, E., and McCulloch, D.S., 1965, Biota of a late glacial rocky mountain pond: GSA Bulletin, v. 76, no. 11, p. 1203-1232, https://doi.org/10.1130/0016-7606(1965)76[1203:BOALGR]2.0.CO;2.","productDescription":"30 p.","startPage":"1203","endPage":"1232","costCenters":[],"links":[{"id":387223,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Colorado","otherGeospatial":"Huerfano 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\"}}]}","volume":"76","issue":"11","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Kauffman, E.G.","contributorId":77676,"corporation":false,"usgs":true,"family":"Kauffman","given":"E.G.","email":"","affiliations":[],"preferred":false,"id":819447,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"McCulloch, David S. dmccullo@usgs.gov","contributorId":3100,"corporation":false,"usgs":true,"family":"McCulloch","given":"David","email":"dmccullo@usgs.gov","middleInitial":"S.","affiliations":[],"preferred":true,"id":819448,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70010602,"text":"70010602 - 1965 - Tectonic deformation associated with the 1964 Alaska earthquake","interactions":[],"lastModifiedDate":"2026-02-11T15:00:12.272329","indexId":"70010602","displayToPublicDate":"1965-06-25T00:00:00","publicationYear":"1965","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3338,"text":"Science","active":true,"publicationSubtype":{"id":10}},"title":"Tectonic deformation associated with the 1964 Alaska earthquake","docAbstract":"Alaska's Good Friday earthquake of 27 March 1964 was accompanied by vertical tectonic deformation over an area of 170,000 to 200,000 square kilometers in south-central Alaska. The deformation included two major northeast-trending zones of uplift and subsidence situated between the Aleutian Trench and the Aleutian Volcanic Arc; together they are 700 to 800 kilometers long and from 150 to 250 kilometers wide. The seaward zone is one in which uplift of as much as 10 meters on land and 15 meters on the sea floor has occurred as a result of both crustal warping and local faulting. Submarine uplift within this zone generated a train of seismic sea waves with half-wave amplitudes of more than 7 meters along the coast near the source. The adjacent zone to the northwest is one of subsidence that averages about 1 meter and attains a measured maximum of 2.3 meters. A second zone of slight uplift may exist along all or part of the Aleutian and Alaska ranges northwest of the zone of subsidence.
","language":"English","publisher":"American Association for the Advancement of Science","doi":"10.1126/science.148.3678.1675","issn":"00368075","usgsCitation":"Plafker, G., 1965, Tectonic deformation associated with the 1964 Alaska earthquake: Science, v. 148, no. 3678, p. 1675-1687, https://doi.org/10.1126/science.148.3678.1675.","productDescription":"13 p.","startPage":"1675","endPage":"1687","costCenters":[],"links":[{"id":219101,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"Aleutian Trench","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -179.9,\n 52.89848022223302\n ],\n [\n -179.9,\n 50.34742724365566\n ],\n [\n -165.90072947118094,\n 52.38515601893195\n ],\n [\n -157.1802921694297,\n 54.89759776829018\n ],\n [\n -155.36618380411227,\n 56.73058764922936\n ],\n [\n -158.829392131228,\n 58.11065126044281\n ],\n [\n -172.99044772182424,\n 53.805294237333726\n ],\n [\n -179.9,\n 52.89848022223302\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n },\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n 179.9,\n 52.84464206876427\n ],\n [\n 172,\n 54.15161662224946\n ],\n [\n 172,\n 51.89469832853055\n ],\n [\n 179.9,\n 50.32814578749236\n ],\n [\n 179.9,\n 52.84464206876427\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"148","issue":"3678","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505ba44ce4b08c986b320232","contributors":{"authors":[{"text":"Plafker, George 0000-0003-3972-0390","orcid":"https://orcid.org/0000-0003-3972-0390","contributorId":36603,"corporation":false,"usgs":true,"family":"Plafker","given":"George","affiliations":[],"preferred":false,"id":359251,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70010596,"text":"70010596 - 1965 - Alaskan glaciers: Recent observations in respect to the earthquake-advance theory","interactions":[],"lastModifiedDate":"2026-02-10T21:31:56.04714","indexId":"70010596","displayToPublicDate":"1965-04-16T00:00:00","publicationYear":"1965","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3338,"text":"Science","active":true,"publicationSubtype":{"id":10}},"title":"Alaskan glaciers: Recent observations in respect to the earthquake-advance theory","docAbstract":"Preliminary aerial photographic studies indicate that the Alaskan earthquake produced some rockfalls but no significant snow and ice avalanches on glaciers. No rapid, short-lived glacier advances (surges) are conclusively associated with this earthquake. Recent evidence fails to support the earthquake-advance theory of Tarr and Martin.","language":"English","publisher":"American Association for the Advancement of Science","doi":"10.1126/science.148.3668.366","issn":"00368075","usgsCitation":"Post, A., 1965, Alaskan glaciers: Recent observations in respect to the earthquake-advance theory: Science, v. 148, no. 3668, p. 366-368, https://doi.org/10.1126/science.148.3668.366.","productDescription":"3 p.","startPage":"366","endPage":"368","costCenters":[],"links":[{"id":219095,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United 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