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Acad., 74, 227",{},{"id":23,"text":457,"url":23,"identifiers":458},"STRAATEN L.M.J.U., 1953, Rhythmic patterns on Dutch North Sea beaches, Geologie Mijnb., 15, 31",{},{"id":23,"text":460,"url":23,"identifiers":461},"SWIFT D.J.P., 1969, The New Concepts of Continental Margin Sedimentation",{},{"id":23,"text":463,"url":23,"identifiers":464},"10.1086\u002F627629",{"doi":463},{"id":23,"text":466,"url":23,"identifiers":467},"10.1111\u002Fj.1365-3091.1967.tb01332.x",{"doi":466},{"id":23,"text":469,"url":23,"identifiers":470},"10.1130\u002FGSAB-48-723",{"doi":469},false,{"id":473,"createTime":474,"updateTime":474,"relativeEntities":475,"slug":476,"properties":477,"entityType":239,"verifyStatus":240,"verifyTime":489,"verifyNote":242,"syncStatus":22,"languages":490,"translateLanguages":23,"viewCount":24,"primaryUrl":491,"fullTextUrl":23,"authors":492,"publicationType":296,"publisherRelationship":599,"citationCount":637,"citationInfo":638,"publishDate":641,"publishYear":642,"citationAnalyzeStatus":22,"lastCitationAnalyze":23,"indexDatabases":23,"openAccess":23,"references":643,"isForceReanalyzing":471},"ae919d1c-6d51-49ee-9848-b38daa4f7df6","2024-10-02T23:21:52.089+00:00",[],"Carbonate-platform-growth-and-cyclicity-at-a-terminal-Proterozoic-passive-margin-Infra-Krol-Formation-and-Krol-Group-Lesser-Himalaya-India",{"mag":478,"keywords":480,"openalex":481,"abstract":483,"title":485,"doi":487},{"VOID":479},"1544887206",{},{"VOID":482},"W1544887206",{"EN":484},"\u003Cjats:p>\u003Cjats:bold>Abstract\u003C\u002Fjats:bold> The Infra Krol Formation and overlying Krol Group constitute a thick (< 2 km), carbonate‐rich succession of terminal Proterozoic age that crops out in a series of doubly plunging synclines in the Lesser Himalaya of northern India. The rocks include 18 carbonate and siliciclastic facies, which are grouped into eight facies associations: (1) deep subtidal; (2) shallow subtidal; (3) sand shoal; (4) peritidal carbonate complex; (5) lagoonal; (6) peritidal siliciclastic–carbonate; (7) incised valley fill; and (8) karstic fill. The stromatolite‐rich, peritidal complex appears to have occupied a location seaward of a broad lagoon, an arrangement reminiscent of many Phanerozoic and Proterozoic platforms. Growth of this complex was accretionary to progradational, in response to changes in siliciclastic influx from the south‐eastern side of the lagoon. Metre‐scale cycles tend to be laterally discontinuous, and are interpreted as mainly autogenic. Variations in the number of both sets of cycles and component metre‐scale cycles across the platform may result from differential subsidence of the interpreted passive margin. Apparently non‐cyclic intervals with shallow‐water features may indicate facies migration that was limited compared with the dimensions of facies belts. Correlation of these facies associations in a sequence stratigraphic framework suggests that the Infra Krol Formation and Krol Group represent a north‐ to north‐west‐facing platform with a morphology that evolved from a siliciclastic ramp, to carbonate ramp, to peritidal rimmed shelf and, finally, to open shelf. This interpretation differs significantly from the published scheme of a basin centred on the Lesser Himalaya, with virtually the entire Infra Krol–Krol succession representing sedimentation in a persistent tidal‐flat environment. This study provides a detailed Neoproterozoic depositional history of northern India from rift basin to passive margin, and predicts that genetically related Neoproterozoic deposits, if they are present in the High Himalaya, are composed mainly of slope\u002Fbasinal facies characterized by fine‐grained siliciclastic and detrital carbonate rocks, lithologically different from those of the Lesser Himalaya.\u003C\u002Fjats:p>",{"EN":486},"Carbonate platform growth and cyclicity at a terminal Proterozoic passive margin, Infra Krol Formation and Krol Group, Lesser Himalaya, India",{"VOID":488},"10.1046\u002Fj.1365-3091.2003.00589.x","2024-10-02T23:21:52.088+00:00",[244],"https:\u002F\u002Fonlinelibrary.wiley.com\u002Fdoi\u002F10.1046\u002Fj.1365-3091.2003.00589.x",[493,512,533,555,577],{"id":494,"sortIndex":122,"researcher":23,"roles":495,"affiliations":496,"properties":507},"93f7b4dc-fd7f-482c-88a0-c2e4b3cb055b",[],[497],{"id":498,"sortIndex":24,"affiliation":499,"properties":23},"52636548-57e7-4b82-9a8c-96e6e0049773",{"id":500,"createTime":501,"updateTime":501,"relativeEntities":502,"slug":503,"properties":504,"entityType":52,"verifyStatus":22,"verifyTime":23,"verifyNote":23,"syncStatus":22,"languages":23,"translateLanguages":23,"viewCount":24},"58ba1eb4-f49a-47fe-85c7-07c0b42e7f57","2024-10-02T23:21:52.121+00:00",[],"Department-of-Earth-and-Environmental-Sciences-and-Lamont-Doherty-Earth-Observatory-Columbia-University-Palisades-NY-10964-8000-USA",{"title":505},{"EN":506},"Department of Earth and Environmental Sciences and Lamont‐Doherty Earth Observatory, Columbia University, Palisades, NY 10964‐8000, USA",{"openalex":508,"title":510},{"VOID":509},"A5098016680",{"EN":511},"Nicholas Christie-Blick",{"id":513,"sortIndex":24,"researcher":23,"roles":514,"affiliations":515,"properties":526},"2db824d7-9e2e-4a0e-892c-45378fc6f050",[],[516],{"id":517,"sortIndex":24,"affiliation":518,"properties":23},"199ef626-9180-4eda-80be-21a201886e3f",{"id":519,"createTime":520,"updateTime":520,"relativeEntities":521,"slug":522,"properties":523,"entityType":52,"verifyStatus":22,"verifyTime":23,"verifyNote":23,"syncStatus":22,"languages":23,"translateLanguages":23,"viewCount":24},"a8472e10-acf5-462f-bcec-b1551a9d9e35","2024-10-02T23:21:52.109+00:00",[],"Department-of-Earth-Sciences-University-of-California-Riverside-CA-92521-USA-E-mail-ganqing-mail-ucr-edu-",{"title":524},{"EN":525},"Department of Earth Sciences, University of California, Riverside, CA 92521, USA (E-mail: ganqing@mail.ucr.edu)",{"openalex":527,"orcid":529,"title":531},{"VOID":528},"A5055628224",{"VOID":530},"https:\u002F\u002Forcid.org\u002F0000-0002-6627-2848",{"EN":532},"Ganqing Jiang",{"id":534,"sortIndex":115,"researcher":23,"roles":535,"affiliations":536,"properties":548},"4718d63f-6c54-4900-b47a-dc07b823e103",[],[537],{"id":538,"sortIndex":24,"affiliation":539,"properties":23},"0ce50b17-b840-480b-baa4-a1648348e8cf",{"id":540,"createTime":541,"updateTime":542,"relativeEntities":543,"slug":544,"properties":545,"entityType":52,"verifyStatus":22,"verifyTime":23,"verifyNote":23,"syncStatus":22,"languages":23,"translateLanguages":23,"viewCount":24},"a620d295-0192-4653-9cef-be4568950158","2024-01-17T16:59:05.551+00:00","2024-10-02T23:21:52.148+00:00",[],"Dept-of-Geology-University-of-Delhi-Delhi-110007-India",{"title":546},{"VI":547},"Dept. of Geology, University of Delhi, Delhi 110007, India",{"openalex":549,"orcid":551,"title":553},{"VOID":550},"A5102955435",{"VOID":552},"https:\u002F\u002Forcid.org\u002F0000-0003-4951-3360",{"EN":554},"D. 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In:Carbonate Sequence Stratigraphy – Recent Developments and Applications(EdsR.B.LoucksandJ.F.Sarg) AAPG Mem. 57 305–325.",{"doi":784},"10.1306\u002FM57579C12",{"id":23,"text":786,"url":23,"identifiers":787},"10.1130\u002F0016-7606(1992)104\u003C0872:ECOEDO>2.3.CO;2",{"doi":786},{"id":23,"text":789,"url":23,"identifiers":790},"Mustard P.S., 1990, Paleokarst breccias, calcretes, silcretes and fault breccias at the base of Upper Proterozoic ‘Windermere’ strata, northern Canadian Cordillera, J. Sed. Petrol, 60, 525",{},{"id":23,"text":792,"url":23,"identifiers":793},"10.1130\u002F0016-7606(2000)112\u003C435:REHTEA>2.0.CO;2",{"doi":792},{"id":23,"text":795,"url":23,"identifiers":796},"10.1046\u002Fj.1365-3091.1998.00171.x",{"doi":795},{"id":23,"text":798,"url":23,"identifiers":799},"Nio S.D.andYang Chang‐Shu(1991)Diagnostic attributes of clastic tidal deposits: a review. In:Clastic Tidal Sedimentology(EdsD.G.Smith G.E.Reinson B.A.ZaitlinandR.A.Rahmani) Can. Soc. Petrol. Geol. Mem. 16 3–28.",{},{"id":23,"text":801,"url":23,"identifiers":802},"10.1046\u002Fj.1365-3091.1996.d01-13.x",{"doi":801},{"id":23,"text":804,"url":23,"identifiers":805},"Osleger D.A., 1991, Relation of eustasy to stacking patterns of meter scale carbonate cycles, Late Cambrian, USA, J. Sed. Petrol, 61, 1225",{},{"id":23,"text":807,"url":23,"identifiers":808},"10.1016\u002FS0743-9547(98)00060-9",{"doi":807},{"id":23,"text":810,"url":23,"identifiers":811},"Pelechaty S.M.andGrotzinger J.P.(1988)Stromatolites bioherms of a 1.9 Ga foreland basin carbonate ramp Beechey Formation Kilohigok Basin Northwest Territories. In:Reefs – Canada and Adjacent Areas(EdsH.Geldsetzer N.P.JamesandG.Tebbut) Can. Soc. Petrol. Geol. Mem. 13 93–104.",{},{"id":23,"text":813,"url":23,"identifiers":814},"Pelechaty S.M., 1991, Dolomitized Middle Proterozoic calcretes, Bathurst Inlet, northwest Territories, Canada, J. Sed. 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Sed. Res, 64, 111",{},{"id":23,"text":846,"url":23,"identifiers":847},"Saxena M.N., 1981, Metamorphic Tectonites of the Himalaya, 303",{},{"id":23,"text":849,"url":23,"identifiers":850},"10.1016\u002F0037-0738(94)90005-1",{"doi":849},{"id":23,"text":852,"url":23,"identifiers":853},"10.2110\u002Fjsr.69.909",{"doi":852},{"id":23,"text":855,"url":23,"identifiers":856},"10.1130\u002F0016-7606(1981)92\u003C197:TPODRA>2.0.CO;2",{"doi":855},{"id":23,"text":858,"url":23,"identifiers":859},"Shanker R., 1992, Precambrian–Cambrian sequence in Krol Belt and additional Ediacaran fossils, Geophytology, 22, 27",{},{"id":23,"text":861,"url":23,"identifiers":862},"Shanker R., 1989, Stratigraphy and sedimentation in Himalaya, a reappraisal, Geol. Surv. India Spec. Publ, 26, 1",{},{"id":23,"text":864,"url":23,"identifiers":865},"Shanker R., 1993, Stratigraphy of Blaini, Infra Krol and Tal succession, Krol Belt, Lesser Himalaya, Indian J. Petrol. Geol, 2, 99",{},{"id":23,"text":867,"url":23,"identifiers":868},"Shanker R., 1997, Additional Ediacaran biota from the Krol Group, Lesser Himalaya, India and their significance, Geosci. J, 18, 79",{},{"id":23,"text":870,"url":23,"identifiers":871},"Shinn E.A.(1986)Modern carbonate tidal flats: their diagnostic features. In:Carbonate Depositional Environments. Part 3. Tidal Flats(EdsL.A.HardieandE.A.Shinn) Colorado School Mines Q. 81 7–35.",{},{"id":23,"text":873,"url":23,"identifiers":874},"Singh I.B., 1980, Sedimentological evolution of the Krol Belt sediments, Himalayan Geol, 8, 657",{},{"id":23,"text":876,"url":23,"identifiers":877},"10.1016\u002F0301-9268(80)90038-8",{"doi":876},{"id":23,"text":879,"url":23,"identifiers":880},"Singh I.B., 1980, Some observations on the depositional environment of the Krol Formation in Nainital area, Himalayan Geol, 8, 633",{},{"id":23,"text":882,"url":23,"identifiers":883},"Singh I.B., 1983, Fauna and biogenic structures in Krol‐Tal succession (Vendian–Early Cambrian), Lesser Himalaya and a biostratigraphic and palaeontological significance, J. Paleontol. Soc. India, 28, 67",{},{"id":23,"text":885,"url":23,"identifiers":886},"Singh I.B., 1980, Some observations on the sedimentology of the Krol succession of Mussoorie area, Uttar Pradesh, J. Geol. Soc. 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Himalayan Geol, 5, 193",{},{"id":23,"text":906,"url":23,"identifiers":907},"10.2113\u002Fgsecongeo.89.3.467",{"doi":906},{"id":23,"text":909,"url":23,"identifiers":910},"10.1016\u002FS0301-9268(01)00139-5",{"doi":909},{"id":23,"text":912,"url":23,"identifiers":913},"10.1130\u002F0016-7606(1970)81[451:SSTPFO]2.0.CO;2",{"doi":912},{"id":23,"text":915,"url":23,"identifiers":916},"Virdi N.S., 1991, Sedimentation and tectonics of the Krol belt – control of basement structures on the basin configuration, J. Himalayan Geol, 2, 141",{},{"id":23,"text":918,"url":23,"identifiers":919},"10.2113\u002Fgsecongeo.89.5.1183",{"doi":918},{"id":23,"text":921,"url":23,"identifiers":922},"Wright V.P., 1982, The recognition and interpretation of paleokarsts: two examples from the Lower Carboniferous of south Wales, J. Sed. 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Publ. 51 45–60.",{"doi":929},"10.2110\u002Fpec.94.12.0045",{"id":931,"createTime":932,"updateTime":932,"relativeEntities":933,"slug":934,"properties":935,"entityType":239,"verifyStatus":240,"verifyTime":947,"verifyNote":242,"syncStatus":22,"languages":948,"translateLanguages":23,"viewCount":24,"primaryUrl":949,"fullTextUrl":23,"authors":950,"publicationType":296,"publisherRelationship":1016,"citationCount":1053,"citationInfo":1054,"publishDate":1056,"publishYear":1057,"citationAnalyzeStatus":22,"lastCitationAnalyze":23,"indexDatabases":23,"openAccess":23,"references":1058,"isForceReanalyzing":471},"3ebed238-dc26-480b-a80f-6ab5ff26ed19","2024-10-02T23:21:38.506+00:00",[],"Dolomitization-gypsum-calcitization-and-silicification-in-carbonate-evaporite-shallow-lacustrine-deposits",{"mag":936,"keywords":938,"openalex":939,"abstract":941,"title":943,"doi":945},{"VOID":937},"2556141550",{},{"VOID":940},"W2556141550",{"EN":942},"\u003Cjats:title>Abstract\u003C\u002Fjats:title>\u003Cjats:p>This paper describes and interprets the mineral and facies assemblages that occur in carbonate–evaporite shallow lacustrine deposits, considering the importance of the processes pathway (i.e. dolomitization, gypsum calcitization and silicification). The Palaeogene deposits of the Deza Formation (Almazán Basin, central‐northern Spain) are selected as a case study to determine the variety of physicochemical processes taking place in carbonate–evaporite shallow lakes and their resulting diagenetic features. Dolostones are the predominant lithology and are composed mainly of dolomite with variable amounts of secondary calcite (5 to 50%), which mainly mimic lenticular gypsum (pseudomorphs). Five morphological types of dolomite crystal were identified as follows: dolomite tubes, dolomite cylinders, rhombohedral dolomite, spheroidal and quasi‐rhombohedral dolomite, and cocoon‐shaped dolomite. The dolomite cylinders and tubes are interpreted as the dolomitized cells of a widespread microbial community. The sequence of diagenetic processes started with growth of microlenticular interstitial gypsum in a calcareous mud deposited on the playa margin mudflats, and that sometimes included microbial sediments. Immediately following growth of gypsum, dolomite replaced the original calcite (or possibly aragonite) muds, the microbial community and the gypsum. Partial or total replacement of gypsum by dolomite was related mainly to the biomineralization of endolithic microbial communities on gypsum crystals. Later calcitization took place under vadose, subaerial exposure conditions. The development of calcrete in distal alluvial settings favoured the release of silica and subsequent silicification on the playa margin mudflats. Stable isotope compositions of calcite range from −9·02 to −5·83‰ \u003Cjats:italic>δ\u003C\u002Fjats:italic>\u003Cjats:sup>13\u003C\u002Fjats:sup>\u003Cjats:styled-content style=\"fixed-case\">C\u003Cjats:sub>PDB\u003C\u002Fjats:sub>\u003C\u002Fjats:styled-content> and −7·10 to 1·22‰ \u003Cjats:italic>δ\u003C\u002Fjats:italic>\u003Cjats:sup>18\u003C\u002Fjats:sup>\u003Cjats:styled-content style=\"fixed-case\">O\u003Cjats:sub>PDB\u003C\u002Fjats:sub>\u003C\u002Fjats:styled-content>; for the dolomite, these values vary from −8·93 to −3·96‰ \u003Cjats:italic>δ\u003C\u002Fjats:italic>\u003Cjats:sup>13\u003C\u002Fjats:sup>\u003Cjats:styled-content style=\"fixed-case\">C\u003Cjats:sub>PDB\u003C\u002Fjats:sub>\u003C\u002Fjats:styled-content> and −5·53 to 2·4‰ \u003Cjats:italic>δ\u003C\u002Fjats:italic>\u003Cjats:sup>18\u003C\u002Fjats:sup>\u003Cjats:styled-content style=\"fixed-case\">O\u003Cjats:sub>PDB\u003C\u002Fjats:sub>\u003C\u002Fjats:styled-content>. Quartz from the cherts has \u003Cjats:italic>δ\u003C\u002Fjats:italic>\u003Cjats:sup>18\u003C\u002Fjats:sup>\u003Cjats:styled-content style=\"fixed-case\">O\u003Cjats:sub>SMOW\u003C\u002Fjats:sub>\u003C\u002Fjats:styled-content> values ranging from 27·1 to 31·1‰. Wide variation and relatively high \u003Cjats:italic>δ\u003C\u002Fjats:italic>\u003Cjats:sup>18\u003C\u002Fjats:sup>\u003Cjats:styled-content style=\"fixed-case\">O\u003Cjats:sub>SMOW\u003C\u002Fjats:sub>\u003C\u002Fjats:styled-content> values for dolomite indicate evaporitic and closed hydrological conditions; increased influx of meteoric waters reigned during the formation of secondary calcite spar.\u003C\u002Fjats:p>",{"EN":944},"Dolomitization, gypsum calcitization and silicification in carbonate–evaporite shallow lacustrine 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(Paleogene, Almazán Basin, Spain), Basin Res., 27, 1",{},{"id":23,"text":1300,"url":23,"identifiers":1301},"10.1016\u002Fj.palaeo.2007.12.017",{"doi":1300},{"id":23,"text":1303,"url":23,"identifiers":1304},"10.1016\u002Fj.chemgeo.2007.06.032",{"doi":1303},{"id":23,"text":1306,"url":23,"identifiers":1307},"10.1016\u002FS0037-0738(01)00258-5",{"doi":1306},{"id":23,"text":1309,"url":23,"identifiers":1310},"10.1016\u002FS0012-8252(00)00022-2",{"doi":1309},{"id":23,"text":1312,"url":23,"identifiers":1313},"10.2110\u002Fpec.94.50.0159",{"doi":1312},{"id":1315,"createTime":1316,"updateTime":1316,"relativeEntities":1317,"slug":1318,"properties":1319,"entityType":239,"verifyStatus":240,"verifyTime":1316,"verifyNote":242,"syncStatus":22,"languages":1331,"translateLanguages":23,"viewCount":24,"primaryUrl":1332,"fullTextUrl":23,"authors":1333,"publicationType":296,"publisherRelationship":1375,"citationCount":1412,"citationInfo":1413,"publishDate":1419,"publishYear":1420,"citationAnalyzeStatus":22,"lastCitationAnalyze":23,"indexDatabases":23,"openAccess":23,"references":1421,"isForceReanalyzing":471},"044a3550-b9be-448a-94d4-287208a22f04","2024-10-02T23:21:35.649+00:00",[],"Precipitation-of-dolomite-using-sulphate-reducing-bacteria-from-the-Coorong-Region-South-Australia-significance-and-implications",{"mag":1320,"keywords":1322,"openalex":1323,"abstract":1325,"title":1327,"doi":1329},{"VOID":1321},"2077568485",{},{"VOID":1324},"W2077568485",{"EN":1326},"\u003Cjats:title>Abstract\u003C\u002Fjats:title>\u003Cjats:p>Dolomite was successfully precipitated in culture experiments that simulated microbiogeochemical conditions prevailing during late stages of evaporation in ephemeral, hypersaline dolomitic lakes of the Coorong region, South Australia. Analyses of lake‐ and pore‐water samples document rapid geochemical changes with time and depth in both dolomitic and non‐dolomitic lakes. Extremely high sulphate and magnesium ion concentrations in lake waters decline rapidly with depth in pore waters throughout the sulphate‐reduction zone, whereas carbonate concentrations in pore waters reach levels up to 100 times those of normal sea water. Ultimately, sulphate is totally consumed and no solid sulphate is recorded in the dolomitic lake sediments. ‘Most probable number’ calculations of lake sediment samples record the presence of large populations of sulphate‐reducing bacteria, whereas sulphur‐isotope analyses of lake‐water samples indicate microbial fractionation in all the lakes studied. Viable populations of microbes from the lake sediments were cultured in anoxic conditions in the laboratory. Samples were then injected into vials containing sterilized clastic or carbonate grains, or glass beads, immersed in a solution that simulated the lake water. Falls in the levels of sulphate and rising pH in positive vials were interpreted as indicating active bacterial sulphate reduction accompanied by increased concentrations of carbonate. Within 2 months, sub‐spherical, sub‐micron‐size crystals of dolomite identical to those of lake sediments were precipitated. It is concluded that bacterial sulphate reduction overcomes kinetic constraints on dolomite formation by removing sulphate and releasing magnesium and calcium ions from neutral ion pairs, and by generating elevated carbonate concentrations, in a hypersaline, strongly electrolytic solution. The results demonstrate that bacterial sulphate reduction controls dolomite precipitation in both the laboratory experiments and lake sediments. It is proposed that dolomite formation, through bacterial sulphate reduction, provides a process analogue applicable to thick platformal dolostones of the past, where benthic microbial communities were the sole or dominant colonizers of shallow marine environments.\u003C\u002Fjats:p>",{"EN":1328},"Precipitation of dolomite using sulphate‐reducing bacteria from the Coorong Region, South Australia: significance and implications",{"VOID":1330},"10.1111\u002Fj.1365-3091.2005.00732.x",[244],"https:\u002F\u002Fonlinelibrary.wiley.com\u002Fdoi\u002F10.1111\u002Fj.1365-3091.2005.00732.x",[1334,1356],{"id":1335,"sortIndex":122,"researcher":23,"roles":1336,"affiliations":1337,"properties":1349},"bcf73b75-140e-4c1f-9f84-af8c0718906e",[],[1338],{"id":1339,"sortIndex":24,"affiliation":1340,"properties":23},"658d597b-97b5-434b-ad49-3ae073d562aa",{"id":1341,"createTime":1342,"updateTime":1343,"relativeEntities":1344,"slug":1345,"properties":1346,"entityType":52,"verifyStatus":22,"verifyTime":23,"verifyNote":23,"syncStatus":22,"languages":23,"translateLanguages":23,"viewCount":24},"c918287e-7dcc-4d90-bce3-d69a381205bc","2024-01-08T00:54:15.878+00:00","2025-02-06T22:48:26.422+00:00",[],"Department-of-Earth-Sciences-University-of-Oxford-Parks-Road-Oxford-OX1-3PR-UK",{"title":1347},{"VI":1348},"Department of Earth Sciences, University of Oxford, Parks Road, Oxford OX1 3PR, UK",{"openalex":1350,"orcid":1352,"title":1354},{"VOID":1351},"A5088938152",{"VOID":1353},"https:\u002F\u002Forcid.org\u002F0000-0002-7124-0701",{"EN":1355},"David Wacey",{"id":1357,"sortIndex":24,"researcher":23,"roles":1358,"affiliations":1359,"properties":1370},"da408862-6e69-4c0b-aa4c-286fd687fbbe",[],[1360],{"id":1361,"sortIndex":24,"affiliation":1362,"properties":23},"68d00913-2c55-43cf-8ec4-8c087f46c38e",{"id":1363,"createTime":1364,"updateTime":1364,"relativeEntities":1365,"slug":1366,"properties":1367,"entityType":52,"verifyStatus":22,"verifyTime":23,"verifyNote":23,"syncStatus":22,"languages":23,"translateLanguages":23,"viewCount":24},"af2ec54f-9ccd-49e5-9d0b-7bbfc64548aa","2024-10-02T23:21:35.667+00:00",[],"Department-of-Geology-University-of-Leicester-University-Road-Leicester-LE1-7RH-UK-E-mail-dtw1-le-ac-uk-",{"title":1368},{"EN":1369},"Department of Geology, University of Leicester, University Road, Leicester LE1 7RH, UK (E‐mail: dtw1@le.ac.uk)",{"openalex":1371,"title":1373},{"VOID":1372},"A5104066467",{"EN":1374},"David T. 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Research, 67, 54",{},{"id":23,"text":1685,"url":23,"identifiers":1686},"10.1016\u002FS0037-0738(99)00037-8",{"doi":1685},{"id":23,"text":1688,"url":23,"identifiers":1689},"10.2110\u002Fpec.00.66.0007",{"doi":1688},{"id":23,"text":1691,"url":23,"identifiers":1692},"Wright D.T., 2000, Carbonate Platform Systems: Components and Interactions, 51",{},{"id":1694,"createTime":1695,"updateTime":1695,"relativeEntities":1696,"slug":1697,"properties":1698,"entityType":239,"verifyStatus":240,"verifyTime":1695,"verifyNote":242,"syncStatus":22,"languages":1710,"translateLanguages":23,"viewCount":24,"primaryUrl":1711,"fullTextUrl":23,"authors":1712,"publicationType":296,"publisherRelationship":1771,"citationCount":1809,"citationInfo":1810,"publishDate":1812,"publishYear":1813,"citationAnalyzeStatus":22,"lastCitationAnalyze":23,"indexDatabases":23,"openAccess":23,"references":1814,"isForceReanalyzing":471},"4a19a913-2fd2-4738-bd07-f363d439e4cf","2024-09-21T23:16:41.529+00:00",[],"Facies-and-flow-regimes-of-sandstone-hosted-columnar-intrusions-Insights-from-the-pipes-of-Kodachrome-Basin-State-Park",{"mag":1699,"keywords":1701,"openalex":1702,"abstract":1704,"title":1706,"doi":1708},{"VOID":1700},"2142235585",{},{"VOID":1703},"W2142235585",{"EN":1705},"\u003Cjats:title>Abstract\u003C\u002Fjats:title>\u003Cjats:p>Sandstone‐hosted intrusions are found in a wide variety of environments, but remain poorly understood compared with their mudstone‐hosted counterparts. In particular, they remain largely unrecognized in the subsurface, in part because they are problematic to image in seismic data. This study reports on the facies and fluid flow associated with a 20 000 km\u003Cjats:sup>3\u003C\u002Fjats:sup> sandstone intrusion province in Utah, \u003Cjats:styled-content style=\"fixed-case\">USA\u003C\u002Fjats:styled-content>. Forming a small portion of this intrusion province, the intrusions cropping out in Kodachrome Basin State Park display a very wide array of facies and morphologies, factors which would make their identification in core a significant challenge. Remobilized sediment is shown to have been injected at least 200 m vertically from its source, with flow prolonged enough to concentrate heavy minerals in placer‐style deposits at the pipe margins. Evidence for lateral pipe migration and for associated broader fluidization regions is also presented. A new approach to estimating flow parameters in injectites is implemented herein, and indicates that previous work has overestimated velocities and flow Reynolds numbers by up to two orders of magnitude. Flow modelling suggests turbulent flow in the pipes that is consistent with field observations of erosive margins and chaotic internal structures. Post‐emplacement, these pipes remained as long‐term fluid conduits, as revealed by their diagenetic history, focussing and facilitating flow of extraformational fluids, despite the relatively high porosity and permeability of the aeolian host strata.\u003C\u002Fjats:p>",{"EN":1707},"Facies and flow regimes of sandstone‐hosted columnar intrusions: Insights from the pipes of Kodachrome Basin State Park",{"VOID":1709},"10.1111\u002Fsed.12115",[244],"https:\u002F\u002Fonlinelibrary.wiley.com\u002Fdoi\u002F10.1111\u002Fsed.12115",[1713,1734,1751],{"id":1714,"sortIndex":119,"researcher":23,"roles":1715,"affiliations":1716,"properties":1727},"1f8bc230-5991-4baa-894a-fec25f45b2e1",[],[1717],{"id":1718,"sortIndex":24,"affiliation":1719,"properties":23},"9273f6a8-1a36-4159-8fab-dda876318eda",{"id":1720,"createTime":1721,"updateTime":1721,"relativeEntities":1722,"slug":1723,"properties":1724,"entityType":52,"verifyStatus":22,"verifyTime":23,"verifyNote":23,"syncStatus":22,"languages":23,"translateLanguages":23,"viewCount":24},"e42686cb-c3ce-4452-aad3-37b5bd5f7eac","2024-09-21T23:16:41.556+00:00",[],"Sorby-Group-School-of-Earth-and-Environment-University-of-Leeds-Leeds-LS2-9JT-UK",{"title":1725},{"EN":1726},"Sorby Group, School of Earth and Environment, University of Leeds, Leeds, LS2 9JT UK",{"openalex":1728,"orcid":1730,"title":1732},{"VOID":1729},"A5019016370",{"VOID":1731},"https:\u002F\u002Forcid.org\u002F0000-0002-1607-8297",{"EN":1733},"Gareth M. 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Bull., 124, 1",{},{"id":23,"text":1879,"url":23,"identifiers":1880},"Duranti D, 2007, Sand Injectites: Implications for Hydrocarbon Exploration and Production, 129",{},{"id":23,"text":1882,"url":23,"identifiers":1883},"10.1111\u002Fj.1365-3091.2004.00634.x",{"doi":1882},{"id":23,"text":1885,"url":23,"identifiers":1886},"10.1016\u002FS0264-8172(99)00044-6",{"doi":1885},{"id":23,"text":1888,"url":23,"identifiers":1889},"10.1002\u002F9781444304237.ch10",{"doi":1888},{"id":23,"text":1891,"url":23,"identifiers":1892},"Gillette D.D.andHayden M.C. (1997)A preliminary inventory of paleontological resources within the Grand Staircase‐Escalante National Monument Utah. Utah Geological Survey Professional Paper 164.",{},{"id":23,"text":1894,"url":23,"identifiers":1895},"Glennie K.W., 2007, Sand Injectites: Implications for Hydrocarbon Exploration and Production, 221",{},{"id":23,"text":1897,"url":23,"identifiers":1898},"Gregory J, 2006, Particles in Water: Properties and Processes, 188",{},{"id":23,"text":1900,"url":23,"identifiers":1901},"Hannum C., 1980, Sandstone and conglomerate‐breccia pipes and dikes of the Kodachrome Basin area, Kane County, Utah, Brigham Young Univ. Geol. Stud. Spec. 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Sed. Petrol., 63, 852",{},{"id":23,"text":1936,"url":23,"identifiers":1937},"10.1111\u002Fj.1365-2117.2010.00471.x",{"doi":1936},{"id":23,"text":1939,"url":23,"identifiers":1940},"10.1144\u002F0016-764902-091",{"doi":1939},{"id":23,"text":1942,"url":23,"identifiers":1943},"10.1016\u002Fj.marpetgeo.2005.01.002",{"doi":1942},{"id":23,"text":1945,"url":23,"identifiers":1946},"10.1111\u002Fj.1365-2117.2005.00262.x",{"doi":1945},{"id":23,"text":1948,"url":23,"identifiers":1949},"10.1016\u002Fj.sedgeo.2011.01.013",{"doi":1948},{"id":23,"text":1951,"url":23,"identifiers":1952},"10.1130\u002FG34619.1",{"doi":1951},{"id":23,"text":1954,"url":23,"identifiers":1955},"10.1007\u002Fs00367-003-0145-y",{"doi":1954},{"id":23,"text":1957,"url":23,"identifiers":1958},"Melosh H.J., 1989, Impact Cratering: A Geologic Process, 245",{},{"id":23,"text":1960,"url":23,"identifiers":1961},"10.1111\u002Fj.1365-3091.2011.01308.x",{"doi":1960},{"id":23,"text":1963,"url":23,"identifiers":1964},"10.1111\u002Fj.1365-3091.1993.tb01378.x",{"doi":1963},{"id":23,"text":1966,"url":23,"identifiers":1967},"10.1111\u002Fj.1365-3091.2011.01287.x",{"doi":1966},{"id":23,"text":1969,"url":23,"identifiers":1970},"10.1046\u002Fj.1365-3091.2002.00432.x",{"doi":1969},{"id":23,"text":1972,"url":23,"identifiers":1973},"10.1016\u002FS0169-555X(00)00096-9",{"doi":1972},{"id":23,"text":1975,"url":23,"identifiers":1976},"10.1016\u002FS0013-7952(96)00040-3",{"doi":1975},{"id":23,"text":1978,"url":23,"identifiers":1979},"O'Sullivan R.B., 1998, Geologic Investigations Series I‐2622",{},{"id":23,"text":1981,"url":23,"identifiers":1982},"10.1144\u002FGSL.SP.2003.216.01.05",{"doi":1981},{"id":23,"text":1984,"url":23,"identifiers":1985},"Peterson F.andPipiringos G.N(1979).Stratigraphic relationships of the Navajo Sandstone to Middle Jurassic formations in parts of southern Utah and northern Arizona. 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Eng., 32, 35",{},{"id":23,"text":2000,"url":23,"identifiers":2001},"10.1111\u002Fj.1365-3091.2011.01230.x",{"doi":2000},{"id":23,"text":2003,"url":23,"identifiers":2004},"10.1144\u002Fjgs2012-124",{"doi":2003},{"id":23,"text":2006,"url":23,"identifiers":2007},"10.2110\u002Fjsr.2009.062",{"doi":2006},{"id":23,"text":2009,"url":23,"identifiers":2010},"Sherry T.J., 2012, Emplacement and dewatering of the world's largest exposed sand injectite complex, Geochem. Geophys. Geosy., 13, 1",{},{"id":23,"text":2012,"url":23,"identifiers":2013},"10.1016\u002Fj.marpetgeo.2006.12.001",{"doi":2012},{"id":23,"text":2015,"url":23,"identifiers":2016},"Taylor B.J., 1982, Sedimentary dykes, pipes and related structures in the Mesozoic sediments of south‐eastern Alexander Island, Brit. Ant. Sur. Bull., 51, 1",{},{"id":23,"text":2018,"url":23,"identifiers":2019},"Thompson A.E., 1970, Stratigraphy of the San Rafael Group, southwest and south central Utah, Utah Geol. Mineral. Surv. Bull., 87, 53",{},{"id":23,"text":2021,"url":23,"identifiers":2022},"Thompson B.J., 2007, Sand Injectites: Implications for Hydrocarbon Exploration and Production, 151",{},{"id":23,"text":2024,"url":23,"identifiers":2025},"10.1144\u002F0016-76492007-096",{"doi":2024},{"id":23,"text":2027,"url":23,"identifiers":2028},"10.1016\u002Fj.jvolgeores.2006.02.005",{"doi":2027},{"id":23,"text":2030,"url":23,"identifiers":2031},"10.1016\u002Fj.sedgeo.2010.04.008",{"doi":2030},{"id":23,"text":2033,"url":23,"identifiers":2034},"10.1016\u002F0079-1946(75)90004-X",{"doi":2033},{"id":23,"text":2036,"url":23,"identifiers":2037},"10.1016\u002Fj.ces.2011.08.041",{"doi":2036},{"id":2039,"createTime":2040,"updateTime":2040,"relativeEntities":2041,"slug":2042,"properties":2043,"entityType":239,"verifyStatus":240,"verifyTime":2040,"verifyNote":242,"syncStatus":22,"languages":2054,"translateLanguages":23,"viewCount":24,"primaryUrl":2055,"fullTextUrl":23,"authors":2056,"publicationType":296,"publisherRelationship":2076,"citationCount":2114,"citationInfo":2115,"publishDate":2117,"publishYear":2118,"citationAnalyzeStatus":22,"lastCitationAnalyze":23,"indexDatabases":23,"openAccess":23,"references":2119,"isForceReanalyzing":471},"0a8d076f-811c-4609-8b9a-274189292b84","2024-09-21T23:16:14.965+00:00",[],"Seismogenically-induced-fluidization-of-Jurassic-erg-sands-south-central-Utah",{"mag":2044,"keywords":2046,"openalex":2047,"abstract":2049,"title":2051,"doi":2053},{"VOID":2045},"2005310194",{},{"VOID":2048},"W2005310194",{"EN":2050},"\u003Cjats:p>Large bodies of fluidized sandstone occur in the Jurassic Entrada, Carmel, Page and Navajo Formations at several locations in south‐central Utah. They are most abundant in the Entrada Sandstone, where they commonly occur in clusters, have a cylindrical form and have a sharp contact with their cross‐bedded host rock. These clastic pipes are as wide as 75 m and have exposed heights of as much as 100 m. Some of the Entrada pipes extend well into the underlying Carmel redbeds. Other clastic pipes in the Entrada Sandstone are less deformed and display various degrees of brittle‐to‐hydroplastic deformation and liquefaction. Clastic pipes in the Page and Navajo Sandstones are less common, but are similar in size and form to those in the Entrada and Carmel, and probably have a similar origin. Some massive sandstone bodies are irregular in form and have tongue‐like projections into the host rock, implying forcible injection of fluidized sand. Several pipe–host contacts in the Entrada Sandstone display small‐scale ring faults. Where relative displacement can be clearly demonstrated, pipe sandstones are invariably down‐faulted, locally as much as 5 m. At two sites, Carmel host rock is upwarped around the Entrada pipes. Stratified and cross‐bedded breccia blocks occur in many Entrada pipes, and preliminary petrographic analysis indicates that at least some of these breccia blocks are derived from the host rock. Homogeneous pipe sandstones are also petrographically similar to their Entrada host rock, suggesting that some pipes originate through fluidization of the fine‐grained Entrada. Fluidization of the Entrada must have occurred in a water‐saturated environment during early diagenesis but before complete lithification, most probably under considerable porewater pressure. Although there are no known modern analogues to these huge masses of structureless sandstone, they may have a small‐scale modern counterpart in earthquake‐induced sandblows. These features were most probably caused by large‐magnitude seismic events during the Middle Jurassic, although other possibilities cannot be ruled out at this point.\u003C\u002Fjats:p>",{"EN":2052},"Seismogenically induced fluidization of Jurassic erg sands, south‐central Utah",{"VOID":1969},[244],"https:\u002F\u002Fonlinelibrary.wiley.com\u002Fdoi\u002F10.1046\u002Fj.1365-3091.2002.00432.x",[2057],{"id":2058,"sortIndex":24,"researcher":23,"roles":2059,"affiliations":2060,"properties":2071},"2639b707-bf08-43bc-bdbd-a775fed0138d",[],[2061],{"id":2062,"sortIndex":24,"affiliation":2063,"properties":23},"afb6d4d5-8b09-4d0d-8b72-8d2ed449f510",{"id":2064,"createTime":2065,"updateTime":2065,"relativeEntities":2066,"slug":2067,"properties":2068,"entityType":52,"verifyStatus":22,"verifyTime":23,"verifyNote":23,"syncStatus":22,"languages":23,"translateLanguages":23,"viewCount":24},"279841e6-d8a3-411b-ba2a-62cbbf3ac8bf","2024-09-21T23:16:15.020+00:00",[],"Department-of-Geography-and-Geology-Sam-Houston-State-University-Huntsville-TX-77341-2148-USA-E-mail-email-protected-",{"title":2069},{"EN":2070},"Department of Geography and Geology, Sam Houston State University, Huntsville, TX 77341-2148, USA (E-mail: \n[email protected])",{"openalex":2072,"title":2074},{"VOID":2073},"A5014036549",{"EN":2075},"Dennis I. Netoff",{"url":23,"publisher":2077,"properties":2107},{"id":6,"createTime":7,"updateTime":8,"relativeEntities":2078,"slug":10,"properties":2079,"entityType":21,"verifyStatus":22,"verifyTime":23,"verifyNote":23,"syncStatus":22,"languages":23,"translateLanguages":23,"viewCount":24,"subjectFields":2085,"manageAffiliations":2086,"indexDatabases":2087,"url":105,"thumbnailPath":23,"statistic":2102,"gsStatistic":23,"type":23,"analyzePriority":23},[],{"country":2080,"issn":2081,"introduce":2082,"eissn":2083,"title":2084},{"VOID":13},{"VOID":15},{"EN":17},{"VOID":19},{"EN":10},[],[],[2088,2095],{"id":87,"indexDatabase":2089,"url":102,"indexYears":23,"academicFieldIds":2094,"indexDatabaseRanking":23},{"id":89,"createTime":90,"updateTime":91,"relativeEntities":2090,"label":2091,"description":2092,"key":98,"publicationTags":2093,"standard":23},[],{"EN":94,"VI":94},{"VI":96,"EN":97},[100,101],[104],{"id":67,"indexDatabase":2096,"url":80,"indexYears":81,"academicFieldIds":2101,"indexDatabaseRanking":85},{"id":69,"createTime":70,"updateTime":71,"relativeEntities":2097,"label":2098,"description":2099,"key":77,"publicationTags":2100,"standard":23},[],{"EN":74,"VI":74},{"EN":74,"VI":76},[79],[83,84],{"impactFactor":24,"impactFactorByYear":2103,"i10Index":118,"i10IndexLast5Year":119,"totalPublication":120,"totalPublicationByYear":2104,"totalCitation":125,"totalCitationByYear":2105,"totalCitationPerPublication":180,"totalCitationPerPublicationByYear":2106,"hindexLast5Year":217,"hindex":217},{"2012":108,"2013":109,"2014":110,"2015":111,"2016":112,"2017":53,"2018":53,"2019":113,"2020":114,"2021":115,"2022":116,"2023":117},{"1963":122,"1964":122,"1965":122,"1968":122,"1969":119,"1971":122,"1972":122,"1974":122,"1975":119,"1976":122,"1977":123,"1978":122,"1979":115,"1980":53,"1981":122,"1983":119,"1984":53,"1985":122,"1986":119,"1987":119,"1989":115,"1990":119,"1991":115,"1992":115,"1993":53,"1994":63,"1995":123,"1996":115,"1997":123,"1998":119,"1999":53,"2000":124,"2001":115,"2002":53,"2003":123,"2004":123,"2005":63,"2006":122,"2007":123,"2008":53,"2009":115,"2010":63,"2011":122,"2012":119,"2013":119,"2014":119,"2015":119,"2016":122,"2017":115,"2018":123,"2019":122,"2020":122,"2021":122},{"1963":127,"1964":128,"1965":129,"1968":130,"1969":131,"1971":132,"1972":133,"1974":134,"1975":135,"1976":136,"1977":137,"1978":138,"1979":139,"1980":140,"1981":141,"1983":142,"1984":143,"1985":144,"1986":145,"1987":146,"1989":147,"1990":148,"1991":149,"1992":150,"1993":151,"1994":152,"1995":153,"1996":154,"1997":155,"1998":156,"1999":157,"2000":158,"2001":159,"2002":160,"2003":161,"2004":162,"2005":163,"2006":164,"2007":165,"2008":166,"2009":167,"2010":168,"2011":169,"2012":170,"2013":171,"2014":172,"2015":173,"2016":174,"2017":175,"2018":176,"2019":177,"2020":178,"2021":179},{"1963":127,"1964":128,"1965":129,"1968":130,"1969":182,"1971":132,"1972":133,"1974":134,"1975":183,"1976":136,"1977":184,"1978":138,"1979":185,"1980":186,"1981":141,"1983":187,"1984":188,"1985":144,"1986":189,"1987":190,"1989":191,"1990":192,"1991":193,"1992":194,"1993":190,"1994":195,"1995":196,"1996":197,"1997":198,"1998":199,"1999":200,"2000":201,"2001":202,"2002":203,"2003":204,"2004":205,"2005":206,"2006":164,"2007":207,"2008":208,"2009":209,"2010":210,"2011":169,"2012":211,"2013":212,"2014":213,"2015":214,"2016":174,"2017":215,"2018":216,"2019":177,"2020":178,"2021":179},{"volume":2108,"pages":2110,"issue":2112},{"VOID":2109},"49",{"VOID":2111},"65-80",{"VOID":2113},"1",52,{"total":2114,"publishYear":23,"statisticByYear":2116},{"2013":119,"2014":53,"2015":122,"2016":53,"2017":119,"2018":115,"2019":63,"2020":119,"2021":122},"2002-02-01",2002,[2120,2123,2126,2128,2131,2134,2137,2140,2143,2146,2150,2153,2156,2160,2164,2167,2170,2173,2176,2179,2182,2185,2188,2191,2194,2197,2200,2203,2206,2209,2212,2215,2218,2221,2224,2228,2231,2234,2236,2238,2241,2244,2247,2250,2254,2257,2260,2264,2267,2270,2273,2276,2279,2282,2285],{"id":23,"text":2121,"url":23,"identifiers":2122},"Allen J.R.L., 1961, Sandstone‐plugged pipes in the lower Old Red Sandstone of Shropshire, England, J. Sed. Petrol., 31, 325",{},{"id":23,"text":2124,"url":23,"identifiers":2125},"10.1016\u002F0037-0738(86)90006-0",{"doi":2124},{"id":23,"text":1822,"url":23,"identifiers":2127},{"doi":1822},{"id":23,"text":2129,"url":23,"identifiers":2130},"Anderson P.B. Chidsey T.C. Jr Sprinkel D.A.andWillis G.C.(2000)Geology of Glen Canyon National Recreation Area Utah–Arizona. In:Geology of Utah's National Parks and Monuments(Eds D.A. Sprinkel T.C. Chidsey and P.B. Anderson) pp. 301–335. Publication 28. Utah Geological Association Salt Lake City UT.",{},{"id":23,"text":2132,"url":23,"identifiers":2133},"Baars D.L.(1995)Navajo Country: a Geology and Natural History of the Four Corners Region. University of New Mexico Press Albuquerque NM 255 pp.",{},{"id":23,"text":2135,"url":23,"identifiers":2136},"Baars D.L.(2000)Geology of Canyonlands National Park Utah. In:Geology of Utah's National Parks and Monuments(Eds D.A. Sprinkel T.C. Chidsey and P.B. Anderson) pp. 61–83. Publication 28. Utah Geological Association Salt Lake City UT.",{},{"id":23,"text":2138,"url":23,"identifiers":2139},"10.2475\u002Fajs.278.5.703",{"doi":2138},{"id":23,"text":2141,"url":23,"identifiers":2142},"Baker A.A., 1946, Geology of the Green River Desert–Cataract Canyon region, Emery, Wayne, and Garfield Counties, Utah, US Geol. Survey Bull., 951, 122",{},{"id":23,"text":2144,"url":23,"identifiers":2145},"10.1130\u002F0016-7606(1963)74[1237:CFASPN]2.0.CO;2",{"doi":2144},{"id":23,"text":2147,"url":23,"identifiers":2148},"Blakey R.andParnell R.A.(1995)Middle Jurassic magmatism: the volcanic record in the eolian Page Sandstone and related Carmel Formation Colorado Plateau. In:Jurassic Magmatism and Tectonics of the North American Cordillera(Eds D.M. Miller and C. Busby) pp. 393–411. Special Paper 299. Geological Society of America Boulder CO.",{"doi":2149},"10.1130\u002FSPE299-p393",{"id":23,"text":2151,"url":23,"identifiers":2152},"Blakey R., 1996, Stratigraphic analysis of eolian interactions with marine and fluvial deposits, Middle Jurassic Page Sandstone and Carmel Formation, Colorado Plateau, USA, J. Sed. Res., 66, 324",{},{"id":23,"text":2154,"url":23,"identifiers":2155},"Chan M.A., 2000, Diagenetic hematite and manganese oxides and fault‐related fluid flow in Jurassic sandstones, southeastern Utah, AAPG Bull., 84, 1281",{},{"id":23,"text":2157,"url":23,"identifiers":2158},"Collinson J.(1994)Sedimentary deformational structures. In:The Geologic Deformation of Sediments(Ed. A. Maltman) pp. 95–125. Chapman & Hall London.",{"doi":2159},"10.1007\u002F978-94-011-0731-0_4",{"id":23,"text":2161,"url":23,"identifiers":2162},"Crabaugh M.andKocurek G.(1993)Entrada Sandstone: an example of a wet aeolian system. In:The Dynamics and Environmental Context of Aeolian Sedimentary Systems(Ed. K. Pye) pp. 103–126. Special Publication 72. Geological Society London.",{"doi":2163},"10.1144\u002FGSL.SP.1993.072.01.11",{"id":23,"text":2165,"url":23,"identifiers":2166},"Crabaugh M.andKocurek G.(1998)Continental sequence stratigraphy of a wet eolian system: a key to relative sea‐level change. In:Relative Role of Eustasy Climate and Tectonism in Continental Rocks(Eds K. Stanley and P. McCabe) SEPM Spec. Publ. 59 213–228.",{},{"id":23,"text":2168,"url":23,"identifiers":2169},"Davidson E.S., 1967, Geology of the Circle Cliffs area, Garfield and Kane Counties, Utah, US Geol. Survey Bull., 1229, 140",{},{"id":23,"text":2171,"url":23,"identifiers":2172},"Decker P.L., 1990, Structural style and mechanics of liquefaction‐related deformation in the Lower Absaroka Volcanic Supergroup (Eocene), east‐central Absaroka Range, Wyoming, Geol. Soc. Am. Spec. Paper, 240, 80",{},{"id":23,"text":2174,"url":23,"identifiers":2175},"Eschner T.B., 1986, Marine destruction of eolian sand seas: origin of mass flows, J. Sed. Petrol., 56, 401",{},{"id":23,"text":2177,"url":23,"identifiers":2178},"10.1086\u002F626251",{"doi":2177},{"id":23,"text":2180,"url":23,"identifiers":2181},"10.1016\u002FS0040-1951(00)00118-9",{"doi":2180},{"id":23,"text":2183,"url":23,"identifiers":2184},"10.1016\u002F0037-0738(83)90069-6",{"doi":2183},{"id":23,"text":2186,"url":23,"identifiers":2187},"Hackman R.J.andWyant D.G.(1973)Geology structure and uranium deposits of the Escalante Quadrangle Utah and Arizona.US Geol. Survey Misc. Geol. Invest. MapI‐744(scale 1:250 000).",{},{"id":23,"text":2189,"url":23,"identifiers":2190},"Hannum C., 1980, Sandstone and conglomerate‐breccia pipes and dikes of the Kodachrome Basin area, Kane County, Utah, Brigham Young Univ. Geol. Studies, 27, 31",{},{"id":23,"text":2192,"url":23,"identifiers":2193},"Harshbarger J.W., 1957, Stratigraphy of the uppermost Triassic and Jurassic rocks of the Navajo Country, US Geol. Survey Prof. Paper, 291, 74",{},{"id":23,"text":2195,"url":23,"identifiers":2196},"10.1130\u002FGSAB-45-1017",{"doi":2195},{"id":23,"text":2198,"url":23,"identifiers":2199},"10.1111\u002Fj.1365-3091.1982.tb01717.x",{"doi":2198},{"id":23,"text":2201,"url":23,"identifiers":2202},"Hunter R.E., 1992, Clastic pipes of probable solution‐collapse origin in Jurassic rocks of the southern San Juan Basin, New Mexico, US Geol. Survey Bull., 1808, 1",{},{"id":23,"text":2204,"url":23,"identifiers":2205},"Huntoon P.W.(2000)Upheaval Dome Canyonlands Utah: strain indicators that reveal an impact origin. In:Geology of Utah's Parks and Monuments(Eds D.A. Sprinkel T.C. Chidsey and P.B. Anderson) Utah Geol. Assoc. Publ. 28 619–628.",{},{"id":23,"text":2207,"url":23,"identifiers":2208},"10.1130\u002F0016-7606(1998)110\u003C1547:SAEOUD>2.3.CO;2",{"doi":2207},{"id":23,"text":2210,"url":23,"identifiers":2211},"Jones B.G., 1972, Deformation structures in siltstone resulting from the migration of an Upper Devonian aeolian dune, J. Sed. Petrol., 42, 935",{},{"id":23,"text":2213,"url":23,"identifiers":2214},"10.1016\u002F0031-0182(81)90054-7",{"doi":2213},{"id":23,"text":2216,"url":23,"identifiers":2217},"Kocurek G.(1996)Desert eolian systems. In:Sedimentary Environments: Processes Facies and Stratigraphy(Ed. H.G. Reading) pp. 125–153. Blackwell Science Oxford.",{},{"id":23,"text":2219,"url":23,"identifiers":2220},"10.1111\u002Fj.1365-3091.1975.tb00290.x",{"doi":2219},{"id":23,"text":2222,"url":23,"identifiers":2223},"McKee E.D., 1972, Deformational structures in Brazilian coastal dunes, J. Sed. 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National Park Transactions and Proceedings Series NPS\u002FNRNAU\u002FNRTP‐95‐11. Colorado Plateau Research Station Flagstaff AZ.",{},{"id":23,"text":2242,"url":23,"identifiers":2243},"10.1111\u002Fj.1365-3091.1976.tb00060.x",{"doi":2242},{"id":23,"text":2245,"url":23,"identifiers":2246},"10.1111\u002Fj.1365-3091.1988.tb00949.x",{"doi":2245},{"id":23,"text":2248,"url":23,"identifiers":2249},"10.1086\u002F624003",{"doi":2248},{"id":23,"text":2251,"url":23,"identifiers":2252},"Peterson F.(1988)A synthesis of the Jurassic system in the southern Rocky Mountain region. In:The Geology of North America Vol. D‐2.Sedimentary Cover – North American Craton US(Ed. L.L. Sloss) pp. 65–76. Geological Society of America Boulder CO.",{"doi":2253},"10.1130\u002FDNAG-GNA-D2.65",{"id":23,"text":2255,"url":23,"identifiers":2256},"Peterson F.andBarnum B.(1973)Geologic map and coal resources of the northwest quarter of the Cummings Mesa Quadrangle Kane County Utah.US Geol. Survey Coal Invest. MapC‐64 1:24 000.",{},{"id":23,"text":2258,"url":23,"identifiers":2259},"Peterson F., 1979, Stratigraphic relations of the Navajo Sandstone to Middle Jurassic formations, southern Utah and northern Arizona, US Geol. Survey Prof. Paper, 1035, 43",{},{"id":23,"text":2261,"url":23,"identifiers":2262},"Phoenix D.A.(1958)Sandstone cylinders as possible guides to paleomovement of ground water. In:New Mexico Geological Society Ninth Field Conference pp. 194–196. New Mexico Geological Society Socorro NM.",{"doi":2263},"10.56577\u002FFFC-9.194",{"id":23,"text":2265,"url":23,"identifiers":2266},"Sargent K.A. Hansen D.andE.(1982)Bedrock geologic map of the Kaiparowits coal‐basin area. Utah.US Geol. Survey Misc. Geol. Invest. MapI‐1033‐I(scale 1:250 000).",{},{"id":23,"text":2268,"url":23,"identifiers":2269},"Schlee J.S., 1963, Sandstone pipes of the Laguna area, New Mexico, J. Sed. Petrol., 33, 112",{},{"id":23,"text":2271,"url":23,"identifiers":2272},"10.1130\u002F0016-7606(1999)111\u003C0590:XEFPCE>2.3.CO;2",{"doi":2271},{"id":23,"text":2274,"url":23,"identifiers":2275},"Weart W., 1998, The Waste Isolation Pilot Plant, Geotimes, 43, 14",{},{"id":23,"text":2277,"url":23,"identifiers":2278},"Weir G.W., 1961, Collapse structures of southern Spanish Valley, southeastern Utah, US Geol. Survey Prof. Paper, 424, B173",{},{"id":23,"text":2280,"url":23,"identifiers":2281},"10.2113\u002Fgsecongeo.80.6.1722",{"doi":2280},{"id":23,"text":2283,"url":23,"identifiers":2284},"Wenrich K.J., 1992, The potential of breccia pipes in the Mohawk Canyon area, Hualapai Indian Reservation, Arizona, US Geol. Survey Bull., 1683, D1",{},{"id":23,"text":2286,"url":23,"identifiers":2287},"Wills C., 1996, Liquefaction in the California desert; an unexpected geologic hazard, Calif. Geol., 49, 31",{},{"id":2289,"createTime":2290,"updateTime":2290,"relativeEntities":2291,"slug":2292,"properties":2293,"entityType":239,"verifyStatus":240,"verifyTime":2290,"verifyNote":242,"syncStatus":22,"languages":2304,"translateLanguages":23,"viewCount":24,"primaryUrl":2305,"fullTextUrl":23,"authors":2306,"publicationType":296,"publisherRelationship":2343,"citationCount":2381,"citationInfo":2382,"publishDate":2385,"publishYear":2386,"citationAnalyzeStatus":22,"lastCitationAnalyze":23,"indexDatabases":23,"openAccess":23,"references":2387,"isForceReanalyzing":471},"324de737-0857-4b8f-b9c8-217b24b8f5bf","2024-09-19T22:12:11.289+00:00",[],"Fluidization-and-injection-in-the-deep-water-sandstones-of-the-Eocene-Alba-Formation-UK-North-Sea-",{"mag":2294,"keywords":2296,"openalex":2297,"abstract":2299,"title":2301,"doi":2303},{"VOID":2295},"1814085363",{},{"VOID":2298},"W1814085363",{"EN":2300},"\u003Cjats:title>Abstract\u003C\u002Fjats:title>\u003Cjats:p>The Nauchlan Member of the Late Eocene Alba Formation (UK North Sea) consists of a deep‐water channel fill that was extensively modified by post‐depositional sand remobilization and injection. Sandstone textures, facies associations and the geometry of the channel fill were affected. A suite of sand‐rich facies was produced by large‐scale fluidization and injection within the channel fill and above it. These facies, termed here unstratified facies, are characterized by the absence of stratification surfaces and by discordant relationships with bedding in the adjacent succession. They reflect variable degrees of disruption of the primary sedimentary structures caused by escaping pore fluid, the velocity of which is estimated at least in the order of 0·1 ms\u003Cjats:sup>−1\u003C\u002Fjats:sup>. Adjacent mudstones were severely disrupted by hydraulic fracturing, and fragments of fractured mudstone were incorporated into the fluidized sand. Average porosity was decreased in the sandstones affected by fluidization. Two main phases of sand injection are inferred to occur at different burial depths. A shallow burial phase (below 100 m) produced thin dykes with ptygmatic folds. The second phase occurred at the boundary between Eocene and Oligocene (≈ 300 m burial depth) and resulted in large‐scale tabular wing‐like dykes that project from the edges of the channel fill. The significant pore‐fluid overpressure, which was required to hydraulically fracture the thick mudstone seal and to fluidize the large volume of sand, was likely to be built up by static liquefaction of the source sand and was possibly enhanced by hydrocarbon gas influx.\u003C\u002Fjats:p>",{"EN":2302},"Fluidization and injection in the deep‐water sandstones of the Eocene Alba Formation (UK North Sea)",{"VOID":1882},[244],"https:\u002F\u002Fonlinelibrary.wiley.com\u002Fdoi\u002F10.1111\u002Fj.1365-3091.2004.00634.x",[2307,2326],{"id":2308,"sortIndex":24,"researcher":23,"roles":2309,"affiliations":2310,"properties":2321},"5852d31d-264f-4327-aecc-01e1bc7aece5",[],[2311],{"id":2312,"sortIndex":24,"affiliation":2313,"properties":23},"94bfff8d-19c3-4ced-9865-e5872bdbc2c9",{"id":2314,"createTime":2315,"updateTime":2315,"relativeEntities":2316,"slug":2317,"properties":2318,"entityType":52,"verifyStatus":22,"verifyTime":23,"verifyNote":23,"syncStatus":22,"languages":23,"translateLanguages":23,"viewCount":24},"30eb17a0-b0fb-43c7-a035-414e6fb5b2db","2024-09-19T22:12:11.298+00:00",[],"Injected-Sands-Group-Department-of-Geology-and-Petroleum-Geology-University-of-Aberdeen-Kings-College-Aberdeen-AB24-3UE-UK-",{"title":2319},{"EN":2320},"Injected Sands Group, Department of Geology and Petroleum Geology, University of Aberdeen, Kings College, Aberdeen AB24 3UE, UK (",{"openalex":2322,"title":2324},{"VOID":2323},"A5090869761",{"EN":2325},"D. 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Geol. Soc. Denmark, 48, 169, 10.37570\u002Fbgsd-2001-48-10",{"doi":2655},"10.37570\u002Fbgsd-2001-48-10",{"id":23,"text":2657,"url":23,"identifiers":2658},"Thompson B.J. Garrison R.E.andMoore C.J.(1999)A late Cenozoic sandstone intrusion west of S. Cruz California. Fluidized flow of water and hydrocarbon‐saturated sediments. In:Late Cenozoic Fluid Seeps and Tectonics Along the San Gregorio Fault Zone in the Monterey Bay Region California(EdsR.E.Garrison I.W.Aiello andJ.C.Moore) pp.53–74.AAPG Pacific Section Volume and Guidebook GB‐76.",{"doi":2659},"10.32375\u002F1999-GB76.5",{"id":23,"text":2661,"url":23,"identifiers":2662},"10.1306\u002F74D725C2-2B21-11D7-8648000102C1865D",{"doi":2661},{"id":23,"text":2664,"url":23,"identifiers":2665},"10.1016\u002F0025-3227(96)00020-5",{"doi":2664},{"id":23,"text":2667,"url":23,"identifiers":2668},"10.1038\u002F43151",{"doi":2667},{"id":23,"text":2670,"url":23,"identifiers":2671},"10.1130\u002F0016-7606(1983)94\u003C1073:CDSATS>2.0.CO;2",{"doi":2670},{"id":23,"text":2673,"url":23,"identifiers":2674},"10.1016\u002FS0264-8172(00)00007-6",{"doi":2673},{"id":2676,"createTime":2677,"updateTime":2677,"relativeEntities":2678,"slug":2679,"properties":2680,"entityType":239,"verifyStatus":22,"verifyTime":2677,"verifyNote":2692,"syncStatus":22,"languages":2693,"translateLanguages":23,"viewCount":24,"primaryUrl":2694,"fullTextUrl":23,"authors":2695,"publicationType":296,"publisherRelationship":2714,"citationCount":2751,"citationInfo":2752,"publishDate":2754,"publishYear":2755,"citationAnalyzeStatus":22,"lastCitationAnalyze":23,"indexDatabases":23,"openAccess":23,"references":2756,"isForceReanalyzing":471},"afcb2840-4ddd-4d00-b873-3728f0b2dc18","2024-09-19T22:12:10.750+00:00",[],"Postglacial-colluvium-in-western-Norway-depositional-processes-facies-and-palaeoclimatic-record",{"mag":2681,"keywords":2683,"openalex":2684,"abstract":2686,"title":2688,"doi":2690},{"VOID":2682},"2153106841",{},{"VOID":2685},"W2153106841",{"EN":2687},"\u003Cjats:p>The postglacial Quaternary colluvial systems in western Norway are arrays of steep fans, often coalescing into aprons, developed along the slopes of valley sides and fjord margins. The coarse debris, derived from weathered gneissic bedrock and its glacial‐till mantle, varies from highly immature to mature. The depositional processes are mainly avalanches, ranging from rockfalls and debrisflows to snowflows, but include also waterflow and debris creep. The mechanics and sedimentary products of these processes are discussed, with special emphasis on snow avalanches, whose role as an agent of debris transport is little‐known to sedimentologists. The subsequent analysis of sedimentary successions is focused on colluvial‐fan deltas, which are very specific, yet little‐studied, coastal depositional systems. The stratigraphic variation and depositional architecture of the colluvial facies assemblages, constrained by abundant radiometric dates, are used to decipher the signal of regional climatic changes from the sedimentary record. The stratigraphic data from two dozen local colluvial successions are compiled and further compared with other types of regional palaeoclimatic proxy record. The analysis suggests that the colluvial systems, although dependent upon local geomorphic conditions, have acted as highly sensitive recorders of regional climatic changes. The study as a whole demonstrates that colluvial depositional systems are an interesting and important frontier of clastic sedimentology.\u003C\u002Fjats:p>",{"EN":2689},"Postglacial colluvium in western Norway: depositional processes, facies and palaeoclimatic record",{"VOID":2691},"10.1046\u002Fj.1365-3091.1998.00200.x","Author affiliation is 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Publ, 79, 1",{},{"id":23,"text":2803,"url":23,"identifiers":2804},"Blikra L.H.(1994)Postglacial Colluvium in Western Norway: Sedimentology Geomorphology and Palaeoclimatic Record.Unpubl. Dr.Scient. thesis University of Bergen.",{},{"id":23,"text":2806,"url":23,"identifiers":2807},"Blikra L.H., 1989, Rapid mass movements and related deposits in alpine areas, Indre Nordfjord, western Norway, Nor. Geol. Unders. Skrift, 92, 1",{},{"id":23,"text":2809,"url":23,"identifiers":2810},"10.1016\u002F0031-0182(94)00141-T",{"doi":2809},{"id":23,"text":2812,"url":23,"identifiers":2813},"Blikra L.H., 1993, Postglacial avalanche activity in western Norway: depositional facies sequences, chronostratigraphy and palaeoclimatic implications, Paläoklimaforsch, 11, 143",{},{"id":23,"text":2815,"url":23,"identifiers":2816},"Blikra L.H.&Nemec W.(1993b)Postglacial fan deltas in western Norway: a case study of snow avalanche‐dominated colluvial fans prograding into deep fjords. In:Abstr. 3rd Int. Workshop on Fan Deltas pp. 1–4. University of Seoul.",{},{"id":23,"text":2818,"url":23,"identifiers":2819},"Blikra L.H., 1997, Holocene avalanche activity in western Norway: chronostratigraphy and palaeoclimatic implications, Paläoklimaforsch, 19, 299",{},{"id":23,"text":2821,"url":23,"identifiers":2822},"Blikra L.H.&Selvik S.(1998)Palaeoclimatic signals recorded in snow avalanche‐dominated colluvium western Norway: depositional facies successions chronostratigraphy and pollen records.The Holocene in press.",{"doi":2823},"10.1191\u002F095968398674390284",{"id":23,"text":2825,"url":23,"identifiers":2826},"Bolt B.A. Horn W.L. Macdonald G.A. Scott R.F.(1975)Geological Hazards. Springer‐Verlag Berlin.",{"doi":2827},"10.1007\u002F978-3-642-86820-7",{"id":23,"text":2829,"url":23,"identifiers":2830},"Brabb E.E.&Harrod B.L.(eds) (1989)Landslides: Extent and Economic Significance.A.A. 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Geomorph., N.F, 29, 104",{},{"id":3549,"createTime":3550,"updateTime":3550,"relativeEntities":3551,"slug":3552,"properties":3553,"entityType":239,"verifyStatus":240,"verifyTime":3564,"verifyNote":242,"syncStatus":22,"languages":3565,"translateLanguages":23,"viewCount":24,"primaryUrl":3566,"fullTextUrl":23,"authors":3567,"publicationType":296,"publisherRelationship":3588,"citationCount":3626,"citationInfo":3627,"publishDate":3633,"publishYear":3634,"citationAnalyzeStatus":22,"lastCitationAnalyze":23,"indexDatabases":23,"openAccess":23,"references":3635,"isForceReanalyzing":471},"ce7a7b24-71d4-4142-8c3f-48227634cd9f","2024-09-19T22:12:05.593+00:00",[],"Experimental-soft-sediment-deformation-structures-formed-by-the-liquefaction-of-unconsolidated-sands-and-some-ancient-examples",{"mag":3554,"keywords":3556,"openalex":3557,"abstract":3559,"title":3561,"doi":3563},{"VOID":3555},"2171167339",{},{"VOID":3558},"W2171167339",{"EN":3560},"\u003Cjats:title>ABSTRACT\u003C\u002Fjats:title>\u003Cjats:p>The effects of liquefaction in saturated sand bodies under a variety of driving forces are described from shaking table experiments, and structures from the geological record are presented which are analogous to the experimental structures. The collapse of sloping heaps of cross‐bedded sand under a gravitational body force generates low‐angle, essentially uncontorted stratification. A basal zone of shearing may be present, with steepened and folded foresets. Stretching of foresets may be accommodated on normal faults, and bottomsets may be contorted into inclined folds. In natural systems the substrate may also liquefy, causing deformation driven by an unevenly distributed confining load. Stratification in the surface bedform is flattened, and stratification in the substratum contorted. Experiments failed to produce relative displacement at the interface between stacked sand bodies. Liquefaction of gravitationally unstable systems in sands generates load structures comparable to those from sand‐mud systems. Recumbent‐folded deformed cross‐bedding is formed by current shear over a liquefied bed, as has been inferred from field and theoretical analyses. Shear of nonliquefied sand forms angular folds. Other deformation mechanisms, such as fluidization or seepage, may generate structures similar to all of these. Local water‐escape structures driven by fluidization occur in the upper parts of some liquefied sand bodies. They include cusps, sand volcanoes and clastic dykes. Transient cavities formed in some experiments and seemed to be preserved as breached cusps. Although the experiments tried to isolate individual driving forces, driving forces may operate together, and there may be a continuum between deformation driven by water escape and deformation driven by loading. Different structures from those described here may form where liquefaction develops in a buried layer as opposed to at the sediment surface.\u003C\u002Fjats:p>",{"EN":3562},"Experimental soft‐sediment deformation: structures formed by the liquefaction of unconsolidated sands and some ancient 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On Riepenwand (2774 m above sea‐level, Kalkkögel range, Alps), on 6 May 2011 a 5800 m\u003Cjats:sup>3\u003C\u002Fjats:sup> rockfall of dolostone detached from the flank of a gorge in the upper part of the mountain. After first collapsing into the gorge, the fragmented rock mass fell down freely for 150 m onto a talus covered by coarse‐granular snow. Rockfall impact triggered a medium‐scale avalanche that developed: (i) a lower layer A of entrained, pure snow; and (ii) an upper layer B of clay‐sized to boulder‐sized fragments mixed with snow. This ‘two‐layer scree\u002Fsnow avalanche’ halted in the distal slope segment of the talus. Boulders within layer B mainly came to rest in the distal part of the avalanche deposit. Fragments smaller than cobble‐size grade did not show obvious downslope segregation. With snowmelt, the rockfall fragments dispersed in layer B were concentrated to a clast‐supported veneer that was draped over the older talus surface upon slower melting of avalanche layer A. In the grain‐size fraction ≤16 mm, a mean of 5 wt% matrix (silt‐sized to clay‐sized grains) of the rockfall‐derived scree of layer B is similar to a mean matrix content of 7 wt% within stratified talus slopes of the Kalkkögel range. This similarity suggests that a major share of matrix – widespread in stratified talus – stems from rockfalls. The characteristics of the scree veneer as melt‐lag of a scree‐laden snow avalanche will be blurred with time. Fossil talus successions may contain a substantial proportion of scree carried down by snow avalanches. The formation of a distinct sedimentary facies of snow avalanche‐deposited scree is impeded by processes of redeposition and deposit modification on talus.\u003C\u002Fjats:p>",{"EN":3856},"Two‐layer scree\u002Fsnow‐avalanche triggered by rockfall (Eastern Alps): Significance for sedimentology of scree 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