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This thrust‐and‐fold belt formed in the Adria‐Eurasia collision zone by the progressive formation of NE‐dipping thrusts in the footwalls of older structures. We calculated the long‐term horizontal velocity field, slip rates and related uncertainties for active faults using a thin‐shell finite element method. We incorporated active faults with different effective fault frictions, rheological properties, appropriate geodynamic boundary conditions, laterally varying heat flow and topography. The results were obtained by comparing the modeled maximum compressive horizontal stress orientations with the World Stress Map database. The calculated horizontal velocities decrease from the southeastern External Dinarides to the northwestern parts of the thrust‐and‐fold belt. This spatial pattern is also evident in the long‐term slip rates of active faults. The highest slip rate was obtained for the Montenegro active fault, while the lowest rates were obtained for active faults in northwestern Slovenia. Low slip rates, influenced by local active diapirism, are also characteristic for active faults in the offshore central External Dinarides. These findings are contradictory to the concept of Adria as an internally rigid, aseismic lithospheric block because the faults located in its interior release a part of the regional compressive stress. 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F. S. W.Fowler J.‐C.Miquel andJ.La Rosa(1998) 210Pb dating of sediments from the central and northern Adriatic Sea: Deposition and preservation of sedimentary organic carbon Rep. UCRL‐JC‐123886 Lawrence Livermore Natl. Lab. Livermore Calif.",{},{"id":23,"text":383,"url":23,"identifiers":384},"Hansen F. D.(1982) Semibrittle creep of selected crustal rocks at 1000 MPa PhD thesis 224 pp. Tex. A&M Univ. College Station.",{},{"id":23,"text":386,"url":23,"identifiers":387},"Hansen F. D., 1983, Rock Mechanics: Theory‐Experiment‐Practice. 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Mantle rocks remain near to the surface after compression and mountain building, covered by the latest Cretaceous to Paleogene sequences. 3‐D lithospheric‐scale gravity inversion demands the presence of a high‐density mantle body placed within the crust in order to justify the observed anomalies. Exhumed mantle, having ~50 km of maximum width, continuously extends beneath the Basque‐Cantabrian Basin and along the northern side of the Pyrenees. The association of this body with rift, postrift, and inversion structural geometries is tested in a balanced cross section across the Basque‐Cantabrian Basin that incorporates a major south‐dipping ramp‐flat‐ramp extensional detachment active between Valanginian and early Cenomanian times. Results indicate that horizontal extension progressed ~48 km at variable strain rates that increased from 1 to ~4 mm\u002Fyr in middle Albian times. Low‐strength Triassic Keuper evaporites and mudstones above the basement favor the decoupling of the cover with formation of minibasins, expulsion rollovers, and diapirs. The inversion of the extensional system is accommodated by doubly verging basement thrusts due to the reactivation of the former basin bounding faults in Eocene‐Oligocene times. Total shortening is estimated in ~34 km and produced the partial subduction of the continental lithosphere beneath the two sides of the exhumed mantle. 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S. Buddin T. S. Kane S. J. &Williams G. D.(1997).Three‐dimensional modelling and visualisation in structural geology: New techniques for the restoration and balancing of volumes. In Proceedings of the 1996 Geoscience Information Group Conference on Geological Visualisation. Electronic Geology (Vol. 1 pp.67–82).",{},{"id":23,"text":810,"url":23,"identifiers":811},"Espina R.(1997).La estructura y evolución tectonoestratigráfica del borde occidental de la Cuenca Vasco‐Cantábrica (Cordillera Cantábrica NO de España) PhD Thesis Univerity of Oviedo. 230 pp.",{},{"id":23,"text":813,"url":23,"identifiers":814},"Espina R., 2004, Geología de España, 338",{},{"id":23,"text":816,"url":23,"identifiers":817},"10.1016\u002FS0040-1951(98)00055-9",{"doi":816},{"id":23,"text":819,"url":23,"identifiers":820},"Fernández‐Mendiola P. 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Tesis Doctoral Univ. País Vasco 204 p.",{},{"id":23,"text":981,"url":23,"identifiers":982},"10.1002\u002F9781444304015.ch19",{"doi":981},{"id":23,"text":984,"url":23,"identifiers":985},"10.1016\u002FS0040-1951(96)00114-X",{"doi":984},{"id":23,"text":987,"url":23,"identifiers":988},"10.1016\u002Fj.tecto.2015.08.046",{"doi":987},{"id":23,"text":990,"url":23,"identifiers":991},"10.1038\u002Fnature09520",{"doi":990},{"id":23,"text":993,"url":23,"identifiers":994},"10.1111\u002Fj.1365-246X.1996.tb01547.x",{"doi":993},{"id":23,"text":996,"url":23,"identifiers":997},"10.1130\u002FG32428.1",{"doi":996},{"id":23,"text":999,"url":23,"identifiers":1000},"Robador Moreno A., 2010, GEODE",{},{"id":23,"text":1002,"url":23,"identifiers":1003},"10.1029\u002F2010TC002735",{"doi":1002},{"id":23,"text":1005,"url":23,"identifiers":1006},"Rodríguez‐Fernández L. R., 2014, Geological Map of Spain and Portugal",{},{"id":23,"text":1008,"url":23,"identifiers":1009},"10.1016\u002Fj.tecto.2015.06.010",{"doi":1008},{"id":23,"text":1011,"url":23,"identifiers":1012},"10.1029\u002FTC008i001p00041",{"doi":1011},{"id":23,"text":1014,"url":23,"identifiers":1015},"10.1190\u002Ftle32080892.1",{"doi":1014},{"id":23,"text":1017,"url":23,"identifiers":1018},"Serrano A., 2004, Geología de España, 334",{},{"id":23,"text":1020,"url":23,"identifiers":1021},"10.1029\u002F2003JB002514",{"doi":1020},{"id":23,"text":1023,"url":23,"identifiers":1024},"10.1029\u002F98TC00561",{"doi":1023},{"id":23,"text":1026,"url":23,"identifiers":1027},"10.1016\u002Fj.crte.2015.10.010",{"doi":1026},{"id":23,"text":1029,"url":23,"identifiers":1030},"10.1016\u002Fj.tecto.2015.06.003",{"doi":1029},{"id":23,"text":1032,"url":23,"identifiers":1033},"10.1002\u002F2014TC003529",{"doi":1032},{"id":23,"text":1035,"url":23,"identifiers":1036},"10.1046\u002Fj.0956-540x.2001.01393.x",{"doi":1035},{"id":23,"text":1038,"url":23,"identifiers":1039},"Vergés J., 2001, Peri‐Tethys memoir 6: Peri‐Tethyan Rift⁄wrench Basins and Passive Margins, 187",{},{"id":23,"text":1041,"url":23,"identifiers":1042},"10.1016\u002F0264-8172(95)98854-X",{"doi":1041},{"id":23,"text":1044,"url":23,"identifiers":1045},"10.1016\u002Fj.gr.2016.03.006",{"doi":1044},{"id":23,"text":1047,"url":23,"identifiers":1048},"10.1130\u002FG37812.1",{"doi":1047},{"id":23,"text":1050,"url":23,"identifiers":1051},"10.1130\u002F0091-7613(1988)016\u003C0848:OTROII>2.3.CO;2",{"doi":1050},{"id":23,"text":1053,"url":23,"identifiers":1054},"10.2973\u002Fodp.proc.ir.173.1998",{"doi":1053},{"id":23,"text":1056,"url":23,"identifiers":1057},"10.1038\u002F35093085",{"doi":1056},{"id":23,"text":1059,"url":23,"identifiers":1060},"Wood L. J., 2010, Shale Tectonics, 1",{},{"id":1062,"createTime":1063,"updateTime":1064,"relativeEntities":1065,"slug":1066,"properties":1067,"entityType":113,"verifyStatus":114,"verifyTime":1080,"verifyNote":115,"languages":1081,"translateLanguages":23,"viewCount":24,"primaryUrl":1082,"fullTextUrl":23,"authors":1083,"publicationType":161,"publisherRelationship":1134,"citationCount":1183,"citationInfo":1184,"publishDate":1188,"publishYear":1185,"citationAnalyzeStatus":22,"lastCitationAnalyze":1064,"indexDatabases":1189,"openAccess":23,"references":1190,"isForceReanalyzing":526},"604dc530-c33d-4242-802c-b5b79dec0022","2024-09-19T08:06:58.931+00:00","2025-06-20T12:00:45.925+00:00",[],"Geodynamics-of-Anatolia-Lithosphere-Thermal-Structure-and-Thickness",{"openalex":1068,"mag":1070,"abstract":1072,"title":1074,"gsPaper":1076,"doi":1078},{"VOID":1069},"W2993750047",{"VOID":1071},"2993750047",{"EN":1073},"\u003Cjats:title>Abstract\u003C\u002Fjats:title>\u003Cjats:p>We present the first thermal model for the lithosphere in Turkey, which shows a highly heterogeneous pattern associated with mosaics of the Tethyan and modern subduction systems. We calculate a regionally average crustal density of 2.90 g\u002Fcm\u003Cjats:sup>3\u003C\u002Fjats:sup> consistent with the presence of large volumes of mafic material. The Moho temperature with a regionally average value of 650–850 °C shows strong short‐wavelength variations. Lithosphere thinning to 50–75 km in most of western Anatolia may have developed in response to the Hellenic slab rollback, while the Neoproterozoic block in the Menderes Massif preserves a 150 km deep lithosphere root. In central Anatolia, the lithosphere thickness decreases southward from 100–150 to 50–60 km along a linear belt of young basaltic volcanism, followed by a belt of a 150 km thick lithosphere. We interpret this characteristic pattern by a SE dipping paleoslab beneath the western Taurides, which may cause the Cyprus subduction melting zone to deviate toward NW and NE. The Eastern Pontides‐Lesser Caucasus have 150–200 km thick lithosphere roots caused by collisional tectonics. The East Anatolian Plateau is underlain by a 80–140 km thick lithosphere, which suggests the presence of significant continental fragments; the patchy pattern of its thermal heterogeneity may be explained by teared and fragmented Tethyan slabs. A poor correlation between the lithosphere thermal structure, heat flux, the Neogene volcanic regions, and mantle seismic velocities implies that seismic anomalies are essentially controlled by heterogeneous mantle hydration by subduction systems of different ages and cannot be explained by temperature variations alone.\u003C\u002Fjats:p>",{"EN":1075},"Geodynamics of Anatolia: Lithosphere Thermal Structure and 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The crustal‐scale Outer Hebrides Fault Zone (OHFZ) in NW Scotland has been described as the type example of such a continental fault zone. It cuts Precambrian basement gneisses and is deeply exhumed, allowing direct study of the deformation products and processes that occur across a wide range of crustal depths. A number of fault rock assemblages are recognized to have formed during a long‐lived displacement history lasting in excess of 1000 Myr. During Caledonian movements that are recognized along much of the 190 km onshore fault trace, brittle, cataclasite‐bearing faults in the west of the OHFZ are unequivocally overprinted to the east by a younger fabric related to a network of ductile shear zones. Field observations and regional geochronological data demonstrate that there is no evidence for reheating of the fault zone due to thrust‐related crustal thickening or shear heating. Microstructural observations show that the onset of viscous deformation was related to a major influx of hydrous fluids. This led to retrogression, with the widespread development of new finegrained phyllosilicate‐bearing fault rocks (“phyllonites”), and the onset of fluid‐assisted, grain size‐sensitive diffusional creep in the most highly deformed and altered parts of the fault zone. Phyllonitic fault rocks also occur in older, more deeply exhumed parts of the fault zone, implying that phyllonitization had previously occurred at an earlier stage and that this process is possible over a wide temperature (depth) range within crustal‐scale faults. Our data provide an observational basis for recent theoretical and experimental studies which suggest that crustal‐scale faults containing interconnected networks of phyllosilicate‐bearing fault rocks will be characterized by long‐term relative weakness and shallow (∼5 km) frictional‐viscous transition zones. 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In the Lurestan region of the Zagros mountain belt, the deformed Arabian continental paleo‐margin can be reconstructed as originally consisting of distinct crustal domains, including a proximal sector and a distal continental ribbon, separated by a deep‐water trough, known as the Radiolarite Basin. Such an architecture was shaped by the continental rifting process, thus reflecting timing and style of continent separation, which is generally assumed to have occurred during the Permo‐Triassic interval. This study reports evidence of syn‐sedimentary extensional faults, unconformities, and facies changes in the Mesozoic stratigraphic succession of the Lurestan region, which point to a major Jurassic extensional pulse. In detail, extension reached its climax at the end of the Early Jurassic, when tectonically driven drowning of the long‐lived Triassic to Early Jurassic carbonate platform led to the transition from shallow‐ to deep‐water environments in large areas of the inner margin, coevally with the development of the Radiolarite Basin. Our findings suggest a two‐step continental rifting in this area, with the first Permo‐Triassic phase predating an Early Jurassic one.\u003C\u002Fjats:p>",{"EN":1853},"Early Jurassic Rifting of the Arabian Passive Continental Margin of the Neo‐Tethys. 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H.(1977).Le Zagros Mémoires de la Société Géologique de France 8 33–52.",{},{"id":23,"text":2226,"url":23,"identifiers":2227},"10.1144\u002FSP282.15",{"doi":2226},{"id":23,"text":2229,"url":23,"identifiers":2230},"10.1144\u002FSP330.10",{"doi":2229},{"id":23,"text":2232,"url":23,"identifiers":2233},"10.1016\u002Fj.gr.2012.10.009",{"doi":2232},{"id":23,"text":2235,"url":23,"identifiers":2236},"10.5194\u002Fse-7-659-2016",{"doi":2235},{"id":23,"text":2238,"url":23,"identifiers":2239},"Salvini F., 1982, Analisi strutturale della linea Olevano‐Antrodoco‐Posta (Ancona‐Anzio Auct.): Metodologia di studio delle deformazioni fragili e presentazione del tratto meridionale, Memorie della Societa Geologica Italiana, 24, 337",{},{"id":23,"text":2241,"url":23,"identifiers":2242},"10.1144\u002F0016-76492010-092",{"doi":2241},{"id":23,"text":2244,"url":23,"identifiers":2245},"10.1038\u002F279590a0",{"doi":2244},{"id":23,"text":1405,"url":23,"identifiers":2247},{"doi":1405},{"id":23,"text":2249,"url":23,"identifiers":2250},"10.1016\u002Fj.marpetgeo.2003.07.006",{"doi":2249},{"id":23,"text":2252,"url":23,"identifiers":2253},"10.1016\u002Fj.marpetgeo.2004.01.007",{"doi":2252},{"id":23,"text":2255,"url":23,"identifiers":2256},"10.1016\u002Fj.jsg.2005.05.010",{"doi":2255},{"id":23,"text":2258,"url":23,"identifiers":2259},"10.1144\u002F0016-76492010-107",{"doi":2258},{"id":23,"text":2261,"url":23,"identifiers":2262},"10.1016\u002FS0012-821X(01)00588-X",{"doi":2261},{"id":23,"text":2264,"url":23,"identifiers":2265},"Stöcklin J., 1968, Structural history and tectonics of Iran: A review, AAPG Bulletin, 52, 1229",{},{"id":23,"text":2267,"url":23,"identifiers":2268},"10.1111\u002Fj.1747-5457.1978.tb00611.x",{"doi":2267},{"id":23,"text":2270,"url":23,"identifiers":2271},"10.1144\u002FGSL.SP.1996.100.01.08",{"doi":2270},{"id":23,"text":2273,"url":23,"identifiers":2274},"10.1007\u002Fs12517-012-0542-5",{"doi":2273},{"id":23,"text":2276,"url":23,"identifiers":2277},"10.1016\u002Fj.jsg.2016.03.009",{"doi":2276},{"id":23,"text":2279,"url":23,"identifiers":2280},"10.1016\u002Fj.cageo.2013.10.013",{"doi":2279},{"id":23,"text":2282,"url":23,"identifiers":2283},"10.1016\u002Fj.jsg.2011.08.007",{"doi":2282},{"id":23,"text":2285,"url":23,"identifiers":2286},"10.5194\u002Fse-9-821-2018",{"doi":2285},{"id":23,"text":2288,"url":23,"identifiers":2289},"vanBellen R.C. Dunnington H.V. Wetzel R. Morton D.M. Dubertret L. 1959.Stratigraphic lexicon of Iraq. Lexique stratigraphique International III Asie fasc 10a Iraq. CNRS Paris.",{},{"id":23,"text":2291,"url":23,"identifiers":2292},"Buchem F. S., 2010, Sequence‐stratigraphic synthesis of the Barremian–Aptian of the eastern Arabian Plate and implications for the petroleum habitat. Barremian‐Aptian stratigraphy and hydrocarbon habitat of the eastern Arabian Plate, GeoArabia Special Publication, 4, 9",{},{"id":23,"text":2294,"url":23,"identifiers":2295},"10.1017\u002FS0016756811000331",{"doi":2294},{"id":23,"text":2297,"url":23,"identifiers":2298},"10.1002\u002Farp.399",{"doi":2297},{"id":23,"text":2300,"url":23,"identifiers":2301},"10.1007\u002Fs12517-010-0209-z",{"doi":2300},{"id":23,"text":2303,"url":23,"identifiers":2304},"10.2113\u002Fgeoarabia0603445",{"doi":2303},{"id":23,"text":2306,"url":23,"identifiers":2307},"10.1016\u002FS0012-8252(03)00041-2",{"doi":2306},{"id":2309,"createTime":2310,"updateTime":2310,"relativeEntities":2311,"slug":2312,"properties":2313,"entityType":113,"verifyStatus":114,"verifyTime":2324,"verifyNote":115,"languages":2325,"translateLanguages":23,"viewCount":24,"primaryUrl":2326,"fullTextUrl":23,"authors":2327,"publicationType":161,"publisherRelationship":2383,"citationCount":735,"citationInfo":2431,"publishDate":2434,"publishYear":2432,"citationAnalyzeStatus":22,"lastCitationAnalyze":23,"indexDatabases":2435,"openAccess":23,"references":2436,"isForceReanalyzing":526},"06718618-b057-478c-92b0-af8706e1ec79","2025-02-05T01:19:54.235+00:00",[],"Mantle-Dynamics-Beneath-the-Sichuan-Basin-and-Eastern-Tibet-From-Teleseismic-Tomography",{"openalex":2314,"mag":2316,"abstract":2318,"title":2320,"doi":2322},{"VOID":2315},"W3125180776",{"VOID":2317},"3125180776",{"EN":2319},"\u003Cjats:title>Abstract\u003C\u002Fjats:title>\u003Cjats:p>The cratonic Sichuan Basin is located east of the Tibetan Plateau, and is surrounded by mountains that have undergone complex deformation and uplift since the Cenozoic. Imaging mantle structure is important for understanding its formation, and to date most models suggest a deep cratonic root underlies the basin, blocking eastward extrusion of lithospheric material beneath Tibet. Here, we obtain detailed upper mantle structure from teleseismic tomography in the region utilizing travel time data from earthquakes recorded at 506 seismic stations, including 25 new stations in the poorly sampled Sichuan Basin. Contrasting to previous models, we show eastward and southeastward dipping high‐velocity anomalies extending eastward ∼150–400 km into the upper mantle from the Sichuan Basin. We suggest, the southeastward subduction of the Yangtze Block occurred in the Mesozoic and may be reactivated in the Cenozoic, with the relatively thin and weak lithosphere to the east of the Sichuan Basin prone to deformation in response to the eastward growth of the Tibetan Plateau. A west‐dipping high‐velocity anomaly beneath eastern Tibet is interpreted as delaminated lithosphere. This delamination may accelerate the development of the Xianshuihe fault zone and the horizontal extrusion of the Tibetan Plateau. Beneath the East Qinling orogen, the eastward extrusion of the plateau material is not obvious suggesting limited horizontal lithospheric extrusion is present north of the Sichuan Basin.\u003C\u002Fjats:p>",{"EN":2321},"Mantle Dynamics Beneath the Sichuan Basin and Eastern Tibet From Teleseismic Tomography",{"VOID":2323},"10.1029\u002F2020tc006319","2025-02-05T01:19:54.234+00:00",[117],"https:\u002F\u002Fagupubs.onlinelibrary.wiley.com\u002Fdoi\u002F10.1029\u002F2020TC006319",[2328,2347,2364],{"id":2329,"sortIndex":24,"researcher":23,"roles":2330,"affiliations":2331,"properties":2340,"displayName":2344,"givenName":23,"familyName":23},"0f935e15-0df1-4fd4-ba4b-5a2264a63d43",[],[2332],{"id":2333,"sortIndex":24,"affiliation":2334,"properties":23},"423a8a80-d7ed-4a58-9ad4-9b0b2694222c",{"id":2333,"createTime":23,"updateTime":23,"relativeEntities":2335,"slug":23,"properties":2336,"entityType":23,"verifyStatus":23,"verifyTime":23,"verifyNote":23,"languages":23,"translateLanguages":23,"viewCount":23,"url":23,"parentIds":2339,"statistic":23},[],{"title":2337},{"VI":2338},"Institute of Geophysics, China Earthquake Administration, Beijing, China",[],{"orcid":2341,"title":2343,"openalex":2345},{"VOID":2342},"https:\u002F\u002Forcid.org\u002F0000-0002-9065-8011",{"EN":2344},"Wei Wang",{"VOID":2346},"A5101543814",{"id":2348,"sortIndex":143,"researcher":23,"roles":2349,"affiliations":2350,"properties":2357,"displayName":2361,"givenName":23,"familyName":23},"c95169c1-fedb-40d9-a029-a696ba7b7a43",[],[2351],{"id":2333,"sortIndex":24,"affiliation":2352,"properties":23},{"id":2333,"createTime":23,"updateTime":23,"relativeEntities":2353,"slug":23,"properties":2354,"entityType":23,"verifyStatus":23,"verifyTime":23,"verifyNote":23,"languages":23,"translateLanguages":23,"viewCount":23,"url":23,"parentIds":2356,"statistic":23},[],{"title":2355},{"VI":2338},[],{"orcid":2358,"title":2360,"openalex":2362},{"VOID":2359},"https:\u002F\u002Forcid.org\u002F0000-0002-3394-1507",{"EN":2361},"Jian Wu",{"VOID":2363},"A5100599435",{"id":2365,"sortIndex":587,"researcher":23,"roles":2366,"affiliations":2367,"properties":2376,"displayName":2380,"givenName":23,"familyName":23},"e4ed9ab9-66da-47ef-a113-da28100b621e",[],[2368],{"id":2369,"sortIndex":24,"affiliation":2370,"properties":23},"39ddff4e-d32d-4041-85a8-4602fa4d02fd",{"id":2369,"createTime":23,"updateTime":23,"relativeEntities":2371,"slug":23,"properties":2372,"entityType":23,"verifyStatus":23,"verifyTime":23,"verifyNote":23,"languages":23,"translateLanguages":23,"viewCount":23,"url":23,"parentIds":2375,"statistic":23},[],{"title":2373},{"VI":2374},"Department of Earth and Planetary Sciences, Birkbeck, University of London, London, UK",[],{"orcid":2377,"title":2379,"openalex":2381},{"VOID":2378},"https:\u002F\u002Forcid.org\u002F0000-0001-9194-8689",{"EN":2380},"J. 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Masters G. Ma Z. &Pasyanos M. E.(2012).CRUST1.0: An updated global model of Earth's crust. Paper presented at EGU General Assembly Conference Abstracts (Vol. 14 pp. 3743).",{},{"id":23,"text":2502,"url":23,"identifiers":2503},"10.1002\u002F2016GC006262",{"doi":2502},{"id":23,"text":2505,"url":23,"identifiers":2506},"10.1002\u002F2013JB010503",{"doi":2505},{"id":23,"text":2508,"url":23,"identifiers":2509},"Li S., 2011, Fission track evidence for Mesozoic‐Cenozoic uplifting in the southeastern margin of Sichuan basin, Acta Petrologica Et Mineralogica, 30, 225",{},{"id":23,"text":2511,"url":23,"identifiers":2512},"10.1016\u002Fj.earscirev.2019.03.003",{"doi":2511},{"id":23,"text":2514,"url":23,"identifiers":2515},"10.1016\u002Fj.jseaes.2011.09.026",{"doi":2514},{"id":23,"text":2517,"url":23,"identifiers":2518},"10.1038\u002Fngeo2130",{"doi":2517},{"id":23,"text":2520,"url":23,"identifiers":2521},"Liu S., 2006, Timing, petrogenesis and geodynamic significance of Zheduoshan Granitoids, Acta Petrologica Sinica, 22, 343",{},{"id":23,"text":2523,"url":23,"identifiers":2524},"10.1016\u002Fj.tecto.2020.228430",{"doi":2523},{"id":23,"text":2526,"url":23,"identifiers":2527},"10.1029\u002F2009JB006882",{"doi":2526},{"id":23,"text":2529,"url":23,"identifiers":2530},"10.1016\u002Fj.tecto.2013.07.007",{"doi":2529},{"id":23,"text":2532,"url":23,"identifiers":2533},"10.1007\u002Fs11430-009-0009-z",{"doi":2532},{"id":23,"text":2535,"url":23,"identifiers":2536},"10.1111\u002Fj.1365-246X.1969.tb00259.x",{"doi":2535},{"id":23,"text":2538,"url":23,"identifiers":2539},"Molnar P., 1975, Cenozoic tectonics of Asia: Effects of a continental collision, Features of Recent Continental Tectonics in Asia can be Interpreted As Results of the India‐Eurasia Collision, 189, 419",{},{"id":23,"text":2541,"url":23,"identifiers":2542},"10.1029\u002F2003JB002414",{"doi":2541},{"id":23,"text":2544,"url":23,"identifiers":2545},"10.1130\u002F0091-7613(1992)020\u003C0498:ACTVIO>2.3.CO;2",{"doi":2544},{"id":23,"text":2547,"url":23,"identifiers":2548},"10.1029\u002F2011JB008349",{"doi":2547},{"id":23,"text":2550,"url":23,"identifiers":2551},"10.1145\u002F355984.355989",{"doi":2550},{"id":23,"text":2553,"url":23,"identifiers":2554},"10.1038\u002Fsrep45348",{"doi":2553},{"id":23,"text":2556,"url":23,"identifiers":2557},"10.1111\u002Fj.1365-246X.2004.02188.x",{"doi":2556},{"id":23,"text":2559,"url":23,"identifiers":2560},"10.1093\u002Fgji\u002Fggw084",{"doi":2559},{"id":23,"text":2562,"url":23,"identifiers":2563},"10.1016\u002F0012-821X(94)00252-T",{"doi":2562},{"id":23,"text":2565,"url":23,"identifiers":2566},"10.1016\u002FS0040-1951(98)00154-1",{"doi":2565},{"id":23,"text":2568,"url":23,"identifiers":2569},"10.1038\u002F379785a0",{"doi":2568},{"id":23,"text":2571,"url":23,"identifiers":2572},"Shen C., 2007, Architecture and tectonic evolution of composite basin‐mountain system in Sichuan basin and its adjacent areas, Geotectonica et Metallogenia, 31, 288",{},{"id":23,"text":2574,"url":23,"identifiers":2575},"Shen C., 2007, Fission track thermochronology evidence for Mesozoic‐Cenozoic uplifting of Daba Mountain, central China, Acta Geologica Sinica, 23, 2901",{},{"id":23,"text":2577,"url":23,"identifiers":2578},"10.1016\u002Fj.jseaes.2015.11.008",{"doi":2577},{"id":23,"text":2580,"url":23,"identifiers":2581},"10.1016\u002Fj.geomorph.2020.107031",{"doi":2580},{"id":23,"text":2583,"url":23,"identifiers":2584},"10.1029\u002F2001RG000108",{"doi":2583},{"id":23,"text":2586,"url":23,"identifiers":2587},"10.1016\u002FS0012-821X(04)00498-4",{"doi":2586},{"id":23,"text":2589,"url":23,"identifiers":2590},"10.1016\u002Fj.jseaes.2012.11.020",{"doi":2589},{"id":23,"text":2592,"url":23,"identifiers":2593},"10.1016\u002Fj.epsl.2019.01.012",{"doi":2592},{"id":23,"text":2595,"url":23,"identifiers":2596},"10.1016\u002Fj.gr.2013.06.014",{"doi":2595},{"id":23,"text":2598,"url":23,"identifiers":2599},"Thurber C., 1987, A fast algorithm for two‐point seismic ray tracing, Bulletin of the Seismological Society of America, 77, 972, 10.1785\u002FBSSA0770030972",{"doi":2600},"10.1785\u002FBSSA0770030972",{"id":23,"text":2602,"url":23,"identifiers":2603},"10.1130\u002F0016-7606(2000)112\u003C413:LCTHDI>2.0.CO;2",{"doi":2602},{"id":23,"text":2605,"url":23,"identifiers":2606},"10.1016\u002Fj.epsl.2018.06.007",{"doi":2605},{"id":23,"text":2608,"url":23,"identifiers":2609},"10.2747\u002F0020-6814.45.3.263",{"doi":2608},{"id":23,"text":2611,"url":23,"identifiers":2612},"10.1016\u002Fj.gr.2012.02.019",{"doi":2611},{"id":23,"text":2614,"url":23,"identifiers":2615},"10.1029\u002F2017GL076948",{"doi":2614},{"id":23,"text":2617,"url":23,"identifiers":2618},"10.1002\u002F2017JB014203",{"doi":2617},{"id":23,"text":2620,"url":23,"identifiers":2621},"10.1002\u002F2017JB013978",{"doi":2620},{"id":23,"text":2623,"url":23,"identifiers":2624},"10.1016\u002Fj.epsl.2016.12.040",{"doi":2623},{"id":23,"text":2626,"url":23,"identifiers":2627},"10.1016\u002Fj.tecto.2007.11.006",{"doi":2626},{"id":23,"text":2629,"url":23,"identifiers":2630},"10.1002\u002F2016JB013832",{"doi":2629},{"id":23,"text":2632,"url":23,"identifiers":2633},"10.1007\u002Fs11430-016-9043-3",{"doi":2632},{"id":23,"text":2635,"url":23,"identifiers":2636},"10.3390\u002Frs10091472",{"doi":2635},{"id":23,"text":2638,"url":23,"identifiers":2639},"10.1093\u002Fgji\u002Fggx287",{"doi":2638},{"id":23,"text":2641,"url":23,"identifiers":2642},"10.1002\u002Fcjg2.1020",{"doi":2641},{"id":23,"text":2644,"url":23,"identifiers":2645},"10.1130\u002FG20554.1",{"doi":2644},{"id":23,"text":2647,"url":23,"identifiers":2648},"10.1029\u002F2018TC004977",{"doi":2647},{"id":23,"text":2650,"url":23,"identifiers":2651},"10.1016\u002Fj.epsl.2010.01.046",{"doi":2650},{"id":23,"text":2653,"url":23,"identifiers":2654},"10.1029\u002F2012GC004119",{"doi":2653},{"id":23,"text":2656,"url":23,"identifiers":2657},"10.1029\u002F92JB00603",{"doi":2656},{"id":23,"text":2659,"url":23,"identifiers":2660},"10.1029\u002F94JB01149",{"doi":2659},{"id":23,"text":2662,"url":23,"identifiers":2663},"Zhao J., 2003, Lithospheric structure and dynamic processes of the Tianshan orogenic belt and the Junggar basin, Tectonophysics, 376, 199",{},{"id":23,"text":2665,"url":23,"identifiers":2666},"10.1038\u002F366557a0",{"doi":2665},{"id":23,"text":2668,"url":23,"identifiers":2669},"10.1093\u002Fnsr\u002Fnww049",{"doi":2668},{"id":23,"text":2671,"url":23,"identifiers":2672},"10.1785\u002F0120090257",{"doi":2671},{"id":23,"text":2674,"url":23,"identifiers":2675},"10.1016\u002Fj.precamres.2019.105350",{"doi":2674},{"id":2677,"createTime":2678,"updateTime":2678,"relativeEntities":2679,"slug":2680,"properties":2681,"entityType":113,"verifyStatus":114,"verifyTime":2692,"verifyNote":115,"languages":2693,"translateLanguages":23,"viewCount":24,"primaryUrl":2694,"fullTextUrl":23,"authors":2695,"publicationType":161,"publisherRelationship":2923,"citationCount":2970,"citationInfo":2971,"publishDate":2975,"publishYear":2432,"citationAnalyzeStatus":22,"lastCitationAnalyze":23,"indexDatabases":2976,"openAccess":23,"references":2977,"isForceReanalyzing":526},"3eb56952-6ab1-47e1-a90f-355a80ab39ec","2025-02-05T01:19:28.341+00:00",[],"Spatial-Slip-Rate-Distribution-Along-the-SE-Xianshuihe-Fault-Eastern-Tibet-and-Earthquake-Hazard-Assessment",{"openalex":2682,"mag":2684,"abstract":2686,"title":2688,"doi":2690},{"VOID":2683},"W3206908024",{"VOID":2685},"3206908024",{"EN":2687},"\u003Cjats:title>Abstract\u003C\u002Fjats:title>\u003Cjats:p>The Xianshuihe (XSH) fault in eastern Tibet is one of the most active faults in China, with the next large earthquake most likely to occur along its SE part, where the fault splits into three parallel branches: Yalahe, Selaha and Zheduotang (ZDT). Precisely quantifying their slip rates at various timescales is essential to evaluate regional earthquake hazard. Here, we expand our previous work on the Selaha fault to the nearby ZDT and Moxi (MX) faults, and add observations on the Yalahe fault and on the newly discovered Mugecuo South fault zone. Using tectonic‐geomorphology approaches with\u003Cjats:sup>10\u003C\u002Fjats:sup>Be dating, we had previously determined average late Quaternary slip rates of 9.75 ± 0.15 and 4.4 ± 0.5 mm\u002Fyr along the NW and SE Selaha fault, respectively. Using the same methods here, we determine a slip rate of 3.4–4.8 mm\u002Fyr on the ZDT fault and of 9.6–13.4 mm\u002Fyr on the MX fault. This is consistent with the southeastward slip rate increase we had proposed along the XSH fault system from 6‐8 mm\u002Fyr (Ganzi fault) to ∼10 mm\u002Fyr (Selaha fault), and >9.6 mm\u002Fyr (MX fault). We propose a new model for the SE XSH fault, where the large‐scale Mugecuo pull‐apart basin lies within an even larger scale compressive uplift zone in a restraining bend of the XSH fault, where the highest peak in eastern Tibet is located (Gongga Shan, 7,556 m). Our slip rate determination helps to constrain a relatively high regional M\u003Cjats:sub>w\u003C\u002Fjats:sub> ∼ 7 earthquake hazard at present on the SE XSH fault.\u003C\u002Fjats:p>",{"EN":2689},"Spatial Slip Rate Distribution Along the SE Xianshuihe Fault, Eastern Tibet, and Earthquake Hazard Assessment",{"VOID":2691},"10.1029\u002F2021tc006985","2025-02-05T01:19:28.340+00:00",[117],"https:\u002F\u002Fagupubs.onlinelibrary.wiley.com\u002Fdoi\u002F10.1029\u002F2021TC006985",[2696,2721,2746,2765,2788,2811,2830,2855,2872,2889,2906],{"id":2697,"sortIndex":24,"researcher":23,"roles":2698,"affiliations":2699,"properties":2716,"displayName":2718,"givenName":23,"familyName":23},"f1d7f5f9-449c-43c5-b5c0-625a9639d3c5",[],[2700,2708],{"id":2701,"sortIndex":24,"affiliation":2702,"properties":23},"612e0da2-ee54-430b-a311-f56476631969",{"id":2701,"createTime":23,"updateTime":23,"relativeEntities":2703,"slug":23,"properties":2704,"entityType":23,"verifyStatus":23,"verifyTime":23,"verifyNote":23,"languages":23,"translateLanguages":23,"viewCount":23,"url":23,"parentIds":2707,"statistic":23},[],{"title":2705},{"VI":2706},"Key Laboratory of Deep-Earth Dynamics of Ministry of Natural Resources, Institute of Geology, Chinese Academy of Geological Sciences, Beijing, 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L., 1994, New empirical relationships among magnitude, rupture length, rupture width, rupture area, and surface displacement, Bulletin of the Seismological Society of America, 84, 974, 10.1785\u002FBSSA0840040974",{"doi":3190},"10.1785\u002FBSSA0840040974",{"id":23,"text":3192,"url":23,"identifiers":3193},"Wen X., 2000, Character of rupture segment of Xianshuihe‐ Zemuhe–Anninghe fault zone, western Sichuan, Seismology and Geology, 22, 239",{},{"id":23,"text":3195,"url":23,"identifiers":3196},"10.1016\u002Fj.pepi.2008.04.013",{"doi":3195},{"id":23,"text":3198,"url":23,"identifiers":3199},"10.1130\u002Fb30331.1",{"doi":3198},{"id":23,"text":3201,"url":23,"identifiers":3202},"10.1016\u002Fj.tecto.2017.04.030",{"doi":3201},{"id":23,"text":3204,"url":23,"identifiers":3205},"10.1029\u002F2000jb900159",{"doi":3204},{"id":23,"text":3207,"url":23,"identifiers":3208},"10.6038\u002Fcjg2019M0593",{"doi":3207},{"id":23,"text":3210,"url":23,"identifiers":3211},"Xu J., 2013, Evolution of Coulomb stress and stress interaction among strong earthquakes along the Xianshuihe fault zone, Chinese Journal of Geophysics, 56, 1146",{},{"id":23,"text":3213,"url":23,"identifiers":3214},"10.1016\u002Fj.jog.2018.05.005",{"doi":3213},{"id":23,"text":3216,"url":23,"identifiers":3217},"10.1016\u002Fj.jog.2015.03.002",{"doi":3216},{"id":23,"text":3219,"url":23,"identifiers":3220},"10.1016\u002Fj.tecto.2016.11.014",{"doi":3219},{"id":23,"text":3222,"url":23,"identifiers":3223},"10.1002\u002Fgj.3628",{"doi":3222},{"id":23,"text":3225,"url":23,"identifiers":3226},"10.1007\u002Fs11589-015-0123-2",{"doi":3225},{"id":23,"text":3228,"url":23,"identifiers":3229},"10.1029\u002F2009JB006325",{"doi":3228},{"id":23,"text":3231,"url":23,"identifiers":3232},"10.1007\u002Fs00024-018-1989-4",{"doi":3231},{"id":23,"text":3234,"url":23,"identifiers":3235},"10.1016\u002Fj.tecto.2012.02.021",{"doi":3234},{"id":23,"text":3237,"url":23,"identifiers":3238},"10.1360\u002F03yd0509",{"doi":3237},{"id":23,"text":3240,"url":23,"identifiers":3241},"10.1016\u002Fj.epsl.2017.02.025",{"doi":3240},{"id":23,"text":3243,"url":23,"identifiers":3244},"10.1002\u002F2017JB014465",{"doi":3243},{"id":23,"text":3246,"url":23,"identifiers":3247},"Zhou R., 2001, The slip rate and recurrence of strong earthquakes of Qianning‐Kangding segment, the Xianshuihe fault zone, Acta Seismologica Sinica, 23, 250",{},{"id":3249,"createTime":3250,"updateTime":3250,"relativeEntities":3251,"slug":3252,"properties":3253,"entityType":113,"verifyStatus":22,"verifyTime":3250,"verifyNote":1459,"languages":3264,"translateLanguages":23,"viewCount":24,"primaryUrl":3265,"fullTextUrl":23,"authors":3266,"publicationType":161,"publisherRelationship":3278,"citationCount":3328,"citationInfo":3329,"publishDate":3340,"publishYear":3330,"citationAnalyzeStatus":22,"lastCitationAnalyze":23,"indexDatabases":3341,"openAccess":23,"references":3342,"isForceReanalyzing":526},"5393d2b5-466a-49f5-ad5f-38179aa2687e","2025-01-25T03:19:09.161+00:00",[],"Extensional-collapse-of-orogens",{"openalex":3254,"mag":3256,"abstract":3258,"title":3260,"doi":3262},{"VOID":3255},"W2144222955",{"VOID":3257},"2144222955",{"EN":3259},"\u003Cjats:p>Lithospheric extension is sited, preferentially, along orogenic belts because they have a thicker continental crust, contain structural inhomogeneities, and suffer extensional orogenic collapse caused by body forces resulting from isostatically compensated elevation and sharp elevation gradients. Collapse occurs especially where rapid advective thinning of the shortened thermal boundary conduction layer occurs beneath an orogen and causes rapid uplift. Where boundary forces are compressional, extension is balanced by radial thrusting to form oroclinal loops around collapsed extensional basins. Where, as in the disruption of Pangea, boundary forces change rapidly from compressional to tensional, body force collapse is continued by general extension which may lead to continental splitting. Even where overall convergence is continuing, orogenic collapse may be enhanced by subduction rollback into small remnant oceans. The extensional collapse of orogens offers a partial explanation for why oceans cyclically close and reopen in roughly the same places, preservation of very high pressure metamorphic rocks, for the return of orogenic large crustal thicknesses to normal without very much erosional denudation with the widespread preservation of supracrustal sequences, high temperature metamorphic assemblages and the minimum‐melting granite suite.\u003C\u002Fjats:p>",{"EN":3261},"Extensional collapse of orogens",{"VOID":3263},"10.1029\u002Ftc007i006p01123",[117],"https:\u002F\u002Fagupubs.onlinelibrary.wiley.com\u002Fdoi\u002F10.1029\u002FTC007i006p01123",[3267],{"id":3268,"sortIndex":24,"researcher":23,"roles":3269,"affiliations":3270,"properties":3271,"displayName":3275,"givenName":23,"familyName":23},"6392eabc-7518-4bb2-bba7-11955a50cfc2",[],[],{"orcid":3272,"title":3274,"openalex":3276},{"VOID":3273},"https:\u002F\u002Forcid.org\u002F0000-0002-6290-1635",{"EN":3275},"John 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P., Formation of the Rocky Mountains, western United States: A continuum computer model, Science, 240, 1501",{},{"id":23,"text":3368,"url":23,"identifiers":3369},"10.1098\u002Frsta.1982.0039",{"doi":3368},{"id":23,"text":3371,"url":23,"identifiers":3372},"10.1016\u002F0040-1951(84)90190-2",{"doi":3371},{"id":23,"text":3374,"url":23,"identifiers":3375},"10.1016\u002F0040-1951(80)90106-7",{"doi":3374},{"id":23,"text":3377,"url":23,"identifiers":3378},"10.1130\u002F0091-7613(1987)15\u003C142:TDOTSM>2.0.CO;2",{"doi":3377},{"id":23,"text":3380,"url":23,"identifiers":3381},"Buck R., 1988, Flexural rotation of normal faults to produce abandoned horizontal detachments, E. Trans. AGU, 69, 465",{},{"id":23,"text":3383,"url":23,"identifiers":3384},"10.1038\u002F333247a0",{"doi":3383},{"id":23,"text":3386,"url":23,"identifiers":3387},"Carey S. W., 1955, The orocline concept in geotectonics, Proc. Pap. R. Soc. Tasmania, 89, 255",{},{"id":23,"text":3389,"url":23,"identifiers":3390},"10.1144\u002Fgsjgs.140.6.0893",{"doi":3389},{"id":23,"text":3392,"url":23,"identifiers":3393},"10.1111\u002Fj.1525-1314.1985.tb00327.x",{"doi":3392},{"id":23,"text":3395,"url":23,"identifiers":3396},"10.1144\u002FGSL.SP.1987.028.01.13",{"doi":3395},{"id":23,"text":3398,"url":23,"identifiers":3399},"10.1130\u002F0091-7613(1984)12\u003C550:CMCCCE>2.0.CO;2",{"doi":3398},{"id":23,"text":3401,"url":23,"identifiers":3402},"10.1016\u002F0012-821X(87)90224-X",{"doi":3401},{"id":23,"text":3404,"url":23,"identifiers":3405},"10.1016\u002F0012-821X(81)90174-6",{"doi":3404},{"id":23,"text":3407,"url":23,"identifiers":3408},"10.1016\u002F0040-1951(79)90303-2",{"doi":3407},{"id":23,"text":3410,"url":23,"identifiers":3411},"Dewey J. F., 1980, Episodicity, sequency and style at convergent plate boundaries, The Continental Crust and its Mineral Deposits, edited by D.W. Strangway, Spec. Pap., Geol. Assoc. Can., 20, 553",{},{"id":23,"text":3413,"url":23,"identifiers":3414},"10.1144\u002Fgsjgs.139.4.0371",{"doi":3413},{"id":23,"text":3416,"url":23,"identifiers":3417},"10.1144\u002FGSL.SP.1988.037.01.03",{"doi":3416},{"id":23,"text":3419,"url":23,"identifiers":3420},"10.1086\u002F627920",{"doi":3419},{"id":23,"text":3422,"url":23,"identifiers":3423},"10.1029\u002FTC004i001p00071",{"doi":3422},{"id":23,"text":3425,"url":23,"identifiers":3426},"10.1130\u002F0016-7606(1979)90\u003C84:AASRCM>2.0.CO;2",{"doi":3425},{"id":23,"text":3428,"url":23,"identifiers":3429},"10.1130\u002F0016-7606(1973)84\u003C3137:PTATEO>2.0.CO;2",{"doi":3428},{"id":23,"text":3431,"url":23,"identifiers":3432},"10.1144\u002FGSL.SP.1986.019.01.01",{"doi":3431},{"id":23,"text":3434,"url":23,"identifiers":3435},"10.1098\u002Frsta.1988.0135",{"doi":3434},{"id":23,"text":3437,"url":23,"identifiers":3438},"10.1144\u002FGSL.SP.1989.045.01.15",{"doi":3437},{"id":23,"text":3440,"url":23,"identifiers":3441},"10.1098\u002Frsta.1988.0089",{"doi":3440},{"id":23,"text":3443,"url":23,"identifiers":3444},"10.1111\u002Fj.1365-246X.1982.tb04969.x",{"doi":3443},{"id":23,"text":3446,"url":23,"identifiers":3447},"10.1144\u002FGSL.SP.1987.028.01.12",{"doi":3446},{"id":23,"text":3449,"url":23,"identifiers":3450},"Hills E. S., 1956, A contribution to the morphotectonics of Australia, J. Geol. Soc. Aust., 3, 1",{},{"id":23,"text":3452,"url":23,"identifiers":3453},"10.1029\u002FJB086iB07p06115",{"doi":3452},{"id":23,"text":3455,"url":23,"identifiers":3456},"10.1029\u002FJB076i014p03246",{"doi":3455},{"id":23,"text":3458,"url":23,"identifiers":3459},"10.1130\u002F0016-7606(1971)82[323:SHOTMI]2.0.CO;2",{"doi":3458},{"id":23,"text":3461,"url":23,"identifiers":3462},"10.1144\u002FGSL.SP.1987.028.01.34",{"doi":3461},{"id":23,"text":3464,"url":23,"identifiers":3465},"10.1038\u002F323147a0",{"doi":3464},{"id":23,"text":3467,"url":23,"identifiers":3468},"10.1038\u002F215578a0",{"doi":3467},{"id":23,"text":3470,"url":23,"identifiers":3471},"10.1098\u002Frsta.1981.0068",{"doi":3470},{"id":23,"text":3473,"url":23,"identifiers":3474},"10.1029\u002FTC006i003p00275",{"doi":3473},{"id":23,"text":3476,"url":23,"identifiers":3477},"10.1126\u002Fscience.189.4201.419",{"doi":3476},{"id":23,"text":3479,"url":23,"identifiers":3480},"10.1130\u002F0016-7606(1986)97\u003C1037:DOOWAT>2.0.CO;2",{"doi":3479},{"id":23,"text":3482,"url":23,"identifiers":3483},"10.1029\u002FTC002i001p00091",{"doi":3482},{"id":23,"text":3485,"url":23,"identifiers":3486},"10.1029\u002FTC002i001p00063",{"doi":3485},{"id":23,"text":3488,"url":23,"identifiers":3489},"10.1016\u002F0040-1951(78)90107-5",{"doi":3488},{"id":23,"text":3491,"url":23,"identifiers":3492},"10.1029\u002FTC004i007p00739",{"doi":3491},{"id":23,"text":3494,"url":23,"identifiers":3495},"10.1029\u002FTC007i001p00087",{"doi":3494},{"id":23,"text":2244,"url":23,"identifiers":3497},{"doi":2244},{"id":23,"text":3499,"url":23,"identifiers":3500},"10.1144\u002FGSL.SP.1986.019.01.19",{"doi":3499},{"id":23,"text":3502,"url":23,"identifiers":3503},"10.1130\u002F0016-7606(1971)82[2039:ADATOA]2.0.CO;2",{"doi":3502},{"id":23,"text":3505,"url":23,"identifiers":3506},"10.1144\u002FGSL.SP.1987.028.01.14",{"doi":3505},{"id":23,"text":3508,"url":23,"identifiers":3509},"10.1016\u002F0012-821X(86)90045-2",{"doi":3508},{"id":23,"text":3511,"url":23,"identifiers":3512},"10.1144\u002FGSL.SP.1987.028.01.15",{"doi":3511},{"id":23,"text":3514,"url":23,"identifiers":3515},"Wezel F. C., 1982, The Tyrrhenian Sea: A rifted Krikogenic‐Swell basin, Mem. Geol. Soc. Italy, 24, 531",{},{"id":23,"text":3517,"url":23,"identifiers":3518},"Williams D. M., 1988, Tectonic denudation of Dalradian rocks, Connemara, Ireland, Tectonics",{},{"id":23,"text":3520,"url":23,"identifiers":3521},"10.1038\u002F211676a0",{"doi":3520},{"id":23,"text":3523,"url":23,"identifiers":3524},"Zwart H. J., 1967, The duality of orogenic belts, Geol. Mijnbouw, 46, 283",{},{"id":3526,"createTime":3527,"updateTime":3527,"relativeEntities":3528,"slug":3529,"properties":3530,"entityType":113,"verifyStatus":114,"verifyTime":3527,"verifyNote":115,"languages":3541,"translateLanguages":23,"viewCount":24,"primaryUrl":3542,"fullTextUrl":23,"authors":3543,"publicationType":161,"publisherRelationship":3659,"citationCount":3706,"citationInfo":3707,"publishDate":3711,"publishYear":3708,"citationAnalyzeStatus":22,"lastCitationAnalyze":23,"indexDatabases":3712,"openAccess":23,"references":3713,"isForceReanalyzing":526},"fd68fd17-e823-4279-a2e4-15c6cb1be7a4","2025-01-25T03:19:04.053+00:00",[],"The-ultimate-arc-Differential-displacement-oroclinal-bending-and-vertical-axis-rotation-in-the-External-Betic-Rif-arc",{"openalex":3531,"mag":3533,"abstract":3535,"title":3537,"doi":3539},{"VOID":3532},"W1612101608",{"VOID":3534},"1612101608",{"EN":3536},"\u003Cjats:p>The External Betic‐Rif arc, which lies between the converging African and Iberian plates, is one of the tightest orogenic arcs on Earth. It is a thin‐skinned fold and thrust belt formed in Miocene time around the periphery of the Alborán Domain, an older contractional orogen that underwent extensional collapse coevally with the formation of the thrust belt. Restoration of four sections across the thrust belt, together with kinematic and paleomagnetic analysis, allows a reconstruction of the prethrusting geometry of the Alborán Domain, and the identification of the following processes that contributed to the formation of the arc: (1) The Alborán Domain moved some 250 km westward relative to Iberia and Africa during the Miocene. This initiated the two limbs of the arc on its NW and SW margins, closing to the WSW in the region of Cherafat in northern Morocco. The overall convergence direction on the Iberian side of the arc was between 310° and 295°, and on the African side it was between 235° and 215°. The difference in convergence direction between the two sectors was primarily a result of the relative motion between Africa and Iberia. (2) Extensional collapse of the Alborán Domain during the Miocene modified the geometry of the western end of the arc: the Internal Rif rotated anticlockwise to form the present north trending sector of the arc, and additional components of displacement produced by extension were transferred into the external thrust belt along a series of strike‐slip faults and shear zones. These allowed the limbs of the arc to rotate and extend, tightening the arc, and creating variations in the amounts and directions of shortening around the arc. The Betic sector of the arc rotated clockwise by 25° during this process, and the southern Rif rotated anticlockwise by ∼55°. (3) Oblique convergence on the two limbs of the arc, dextral in the Betics and sinistral in the southern Rif, resulted in strongly noncoaxial deformation. This had three related effects: (1) large rotations of individual thrust sheets resulted from the oblique propagation of thrusts away from the thrust front, followed by pinning and rotation as the thrust sheets peeled off, (2) continued oblique convergence resulted in distributed shear, particularly in the rear of the thrust wedge, causing rotation of stacks of thrust sheets on the scale of a few tens of kilometers, and (3) distributed shear in the orogen resulted in the rotation of folds as they amplified, the hinges migrating through the rock body, and rotating at a slower rate than the rock. 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R. M. A structural study of an Arcuate Thrust Belt Prebetic Zone southern Spain Ph.D. thesis Univ. of Oxford Oxford U.K. 1993.",{},{"id":23,"text":3914,"url":23,"identifiers":3915},"10.1029\u002FTC007i001p00073",{"doi":3914},{"id":23,"text":3917,"url":23,"identifiers":3918},"10.1016\u002F0191-8141(96)00016-8",{"doi":3917},{"id":23,"text":3920,"url":23,"identifiers":3921},"10.1130\u002F0016-7606(1989)101\u003C0683:SOTKOI>2.3.CO;2",{"doi":3920},{"id":23,"text":3923,"url":23,"identifiers":3924},"Martín‐Algarra A. Evolucion geologica Alpina del contacto entre las zonas Internas y las zonas Externas de la Cordillera Betica Ph.D. thesis Univ. of Granada Granada Spain 1987.",{},{"id":23,"text":3926,"url":23,"identifiers":3927},"Mayfield A. Palaeomagnetic and kinematic constraints on deformation during oblique convergence Betic Cordillera southern Spain Ph.D. thesis Univ. of London London U.K. 1999.",{},{"id":23,"text":3929,"url":23,"identifiers":3930},"10.1007\u002FBF00875971",{"doi":3929},{"id":23,"text":3932,"url":23,"identifiers":3933},"10.1111\u002Fj.1365-246X.1989.tb02020.x",{"doi":3932},{"id":23,"text":3935,"url":23,"identifiers":3936},"10.1130\u002F0091-7613(1996)024\u003C0755:GATTZA>2.3.CO;2",{"doi":3935},{"id":23,"text":3938,"url":23,"identifiers":3939},"10.1130\u002F0091-7613(1993)021\u003C1123:LSLEIT>2.3.CO;2",{"doi":3938},{"id":23,"text":3941,"url":23,"identifiers":3942},"Olivier P., 1981, L'accident de Jebha‐Chrafate (Rif, Maroc), Rev. Géol. Dyn. Géogr. Phys., 23, 27",{},{"id":23,"text":3944,"url":23,"identifiers":3945},"10.1016\u002F0031-9201(88)90121-5",{"doi":3944},{"id":23,"text":3947,"url":23,"identifiers":3948},"J. Paquet 1968",{},{"id":23,"text":3950,"url":23,"identifiers":3951},"10.1016\u002F0191-8141(87)90145-3",{"doi":3950},{"id":23,"text":3953,"url":23,"identifiers":3954},"10.1029\u002F1999TC001121",{"doi":3953},{"id":23,"text":3956,"url":23,"identifiers":3957},"10.1130\u002F0091-7613(1989)017\u003C0540:ECOTCL>2.3.CO;2",{"doi":3956},{"id":23,"text":3959,"url":23,"identifiers":3960},"10.1016\u002FS0012-821X(99)00176-4",{"doi":3959},{"id":23,"text":3962,"url":23,"identifiers":3963},"10.1016\u002F0191-8141(94)00110-L",{"doi":3962},{"id":23,"text":3965,"url":23,"identifiers":3966},"10.1029\u002F98TC02204",{"doi":3965},{"id":23,"text":3968,"url":23,"identifiers":3969},"10.1130\u002F0091-7613(1992)020\u003C0311:PRATKO>2.3.CO;2",{"doi":3968},{"id":23,"text":3971,"url":23,"identifiers":3972},"10.1016\u002F0191-8141(94)90014-0",{"doi":3971},{"id":23,"text":3974,"url":23,"identifiers":3975},"10.1016\u002F0012-821X(92)90059-5",{"doi":3974},{"id":23,"text":3977,"url":23,"identifiers":3978},"10.1144\u002Fgsjgs.150.4.0707",{"doi":3977},{"id":23,"text":3980,"url":23,"identifiers":3981},"10.1144\u002Fjgs.157.6.1187",{"doi":3980},{"id":23,"text":3983,"url":23,"identifiers":3984},"10.1016\u002FS0024-4937(99)00035-3",{"doi":3983},{"id":23,"text":3986,"url":23,"identifiers":3987},"10.1016\u002F0031-0182(94)90162-7",{"doi":3986},{"id":23,"text":3989,"url":23,"identifiers":3990},"10.1017\u002FS0016756898001277",{"doi":3989},{"id":23,"text":3992,"url":23,"identifiers":3993},"Roest W. R., 1992, Kinematics of the plate boundaries between Eurasia, Iberia and Africa in the North Atlantic from the Late Cretaceous to the present, Geology, 19, 613, 10.1130\u002F0091-7613(1991)019\u003C0613:KOTPBB>2.3.CO;2",{"doi":3994},"10.1130\u002F0091-7613(1991)019\u003C0613:KOTPBB>2.3.CO;2",{"id":23,"text":3996,"url":23,"identifiers":3997},"10.1029\u002F92TC02248",{"doi":3996},{"id":23,"text":3999,"url":23,"identifiers":4000},"10.1016\u002F0040-1951(90)90062-D",{"doi":3999},{"id":23,"text":4002,"url":23,"identifiers":4003},"10.3989\u002Fegeol.96523-4260",{"doi":4002},{"id":23,"text":4005,"url":23,"identifiers":4006},"10.1016\u002F0264-8172(93)90055-W",{"doi":4005},{"id":23,"text":4008,"url":23,"identifiers":4009},"10.1130\u002F0091-7613(1994)022\u003C0555:ESOTAG>2.3.CO;2",{"doi":4008},{"id":23,"text":4011,"url":23,"identifiers":4012},"10.1029\u002F1999TC900057",{"doi":4011},{"id":23,"text":2568,"url":23,"identifiers":4014},{"doi":2568},{"id":23,"text":4016,"url":23,"identifiers":4017},"10.1093\u002Fpetroj\u002F40.1.21",{"doi":4016},{"id":23,"text":4019,"url":23,"identifiers":4020},"Thurow J., 1986, North Atlantic Palaeoceanography, 423",{},{"id":23,"text":4022,"url":23,"identifiers":4023},"Torné M., 2000, Lithospheric structure beneath the Alborán Sea basin: Results from three‐dimensional gravity modeling and tectonic relevance, J. Geophys. Res., 105, 3209, 10.1029\u002F1999JB900281",{"doi":4024},"10.1029\u002F1999JB900281",{"id":23,"text":4026,"url":23,"identifiers":4027},"Vera J. A., 1983, Geología de España (Libro Jubilar J. M. Rios), 218",{},{"id":23,"text":4029,"url":23,"identifiers":4030},"10.1016\u002F0031-9201(94)90005-1",{"doi":4029},{"id":23,"text":4032,"url":23,"identifiers":4033},"10.1029\u002F95TC00086",{"doi":4032},{"id":23,"text":4035,"url":23,"identifiers":4036},"10.1111\u002Fj.1365-2117.1993.tb00063.x",{"doi":4035},{"id":23,"text":4038,"url":23,"identifiers":4039},"10.1016\u002FS0191-8141(99)00188-1",{"doi":4038},{"id":23,"text":4041,"url":23,"identifiers":4042},"10.1016\u002F0040-1951(86)90193-9",{"doi":4041},{"id":23,"text":4044,"url":23,"identifiers":4045},"Wildi W., 1983, La chaine tello‐rifaine (Algérie, Maroc, Tunisie): Structure, stratigraphie et évolution du Trias au Miocène, Rev. Géol. Dyn. Géogr. Phys., 24, 201",{},{"id":4047,"createTime":4048,"updateTime":4048,"relativeEntities":4049,"slug":4050,"properties":4051,"entityType":113,"verifyStatus":22,"verifyTime":4048,"verifyNote":1459,"languages":4062,"translateLanguages":23,"viewCount":24,"primaryUrl":4063,"fullTextUrl":23,"authors":4064,"publicationType":161,"publisherRelationship":4087,"citationCount":4136,"citationInfo":4137,"publishDate":4149,"publishYear":4138,"citationAnalyzeStatus":22,"lastCitationAnalyze":23,"indexDatabases":4150,"openAccess":23,"references":4151,"isForceReanalyzing":526},"58a4b8f0-b113-41d5-b0f7-87df34900079","2025-01-25T03:19:00.120+00:00",[],"Origin-of-the-Betic-Rif-mountain-belt",{"openalex":4052,"mag":4054,"abstract":4056,"title":4058,"doi":4060},{"VOID":4053},"W2051704997",{"VOID":4055},"2051704997",{"EN":4057},"\u003Cjats:p>In recent years, the origin of the Betic‐Rif orocline has been the subject of considerable debate. Much of this debate has focused on mechanisms required to generate rapid late‐orogenic extension with coeval shortening. Here we summarize the principal geological and geophysical observations and propose a model for the Miocene evolution of the Betic‐Rif mountain belts, which is compatible with the evolution of the rest of the western Mediterranean. We regard palaeomagnetic data, which indicate that there have been large rotations about vertical axes, and earthquake data, which show that deep seismicity occurs beneath the Alboran Sea, to be the most significant data sets. Neither data set is satisfactorily accounted for by models which invoke convective removal or delamination of lithospheric mantle. Existing geological and geophysical observations are, however, entirely consistent with the existence of a subduction zone which rolled or peeled back until it collided with North Africa. We suggest that this ancient subducting slab consequently split into two fragments, one of which has continued to roll back, generating the Tyrrhenian Sea and forming the present‐day Calabrian Arc. The other slab fragment rolled back to the west, generating the Alboran Sea and the Betic‐Rif orocline during the early to middle Miocene.\u003C\u002Fjats:p>",{"EN":4059},"Origin of the Betic‐Rif mountain belt",{"VOID":4061},"10.1029\u002F96tc03937",[117],"https:\u002F\u002Fagupubs.onlinelibrary.wiley.com\u002Fdoi\u002F10.1029\u002F96TC03937",[4065,4076],{"id":4066,"sortIndex":24,"researcher":23,"roles":4067,"affiliations":4068,"properties":4069,"displayName":4073,"givenName":23,"familyName":23},"6cdde294-388f-4502-80f1-ef4aff2b4380",[],[],{"orcid":4070,"title":4072,"openalex":4074},{"VOID":4071},"https:\u002F\u002Forcid.org\u002F0000-0001-9858-3029",{"EN":4073},"Lidia Lonergan",{"VOID":4075},"A5018635655",{"id":4077,"sortIndex":143,"researcher":23,"roles":4078,"affiliations":4079,"properties":4080,"displayName":4084,"givenName":23,"familyName":23},"f3accfe9-2081-4347-baa0-2a5436d0f1ff",[],[],{"orcid":4081,"title":4083,"openalex":4085},{"VOID":4082},"https:\u002F\u002Forcid.org\u002F0000-0002-4460-299X",{"EN":4084},"Nicky White",{"VOID":4086},"A5080298968",{"url":23,"publisher":4088,"properties":4130},{"id":6,"createTime":7,"updateTime":8,"relativeEntities":4089,"slug":10,"properties":4090,"entityType":21,"verifyStatus":22,"verifyTime":23,"verifyNote":23,"languages":23,"translateLanguages":23,"viewCount":24,"subjectFields":4095,"manageAffiliations":4104,"indexDatabases":4115,"url":89,"thumbnailPath":23,"statistic":23,"gsStatistic":23,"type":23,"analyzePriority":23},[],{"country":4091,"eissn":4092,"issn":4093,"title":4094},{"VOID":13},{"VOID":15},{"VOID":17},{"EN":10},[4096,4100],{"id":27,"createTime":23,"updateTime":23,"relativeEntities":4097,"label":4098,"description":4099,"parentId":23,"standard":23,"scholarHubFieldId":23},[],{"EN":30},{},{"id":33,"createTime":23,"updateTime":23,"relativeEntities":4101,"label":4102,"description":4103,"parentId":23,"standard":23,"scholarHubFieldId":23},[],{"EN":36},{},[4105,4110],{"id":40,"createTime":23,"updateTime":23,"relativeEntities":4106,"slug":23,"properties":4107,"entityType":23,"verifyStatus":23,"verifyTime":23,"verifyNote":23,"languages":23,"translateLanguages":23,"viewCount":23,"url":23,"parentIds":4109,"statistic":23},[],{"title":4108},{"EN":44},[],{"id":47,"createTime":23,"updateTime":23,"relativeEntities":4111,"slug":23,"properties":4112,"entityType":23,"verifyStatus":23,"verifyTime":23,"verifyNote":23,"languages":23,"translateLanguages":23,"viewCount":23,"url":23,"parentIds":4114,"statistic":23},[],{"title":4113},{"EN":51},[],[4116,4123],{"id":55,"indexDatabase":4117,"url":66,"indexYears":67,"academicFieldIds":4122,"indexDatabaseRanking":71},{"id":57,"createTime":23,"updateTime":23,"relativeEntities":4118,"label":4119,"description":4120,"key":63,"publicationTags":4121,"standard":23},[],{"EN":60,"VI":60},{"EN":60,"VI":62},[65],[69,70],{"id":73,"indexDatabase":4124,"url":86,"indexYears":23,"academicFieldIds":4129,"indexDatabaseRanking":23},{"id":75,"createTime":23,"updateTime":23,"relativeEntities":4125,"label":4126,"description":4127,"key":82,"publicationTags":4128,"standard":23},[],{"EN":78,"VI":78},{"EN":80,"VI":81},[84,85],[88],{"issue":4131,"pages":4132,"volume":4134},{"VOID":207},{"VOID":4133},"504-522",{"VOID":4135},"16",687,{"total":4136,"publishYear":4138,"statisticByYear":4139},1997,{"2012":4140,"2013":4141,"2014":3335,"2015":4142,"2016":4143,"2017":4144,"2018":4140,"2019":4145,"2020":4141,"2021":4146,"2022":4147,"2023":2974,"2024":4148},24,35,38,34,20,27,33,25,15,"1997-06-01",[84,71],[4152,4155,4157,4159,4162,4165,4168,4171,4174,4177,4180,4183,4185,4188,4191,4194,4197,4200,4203,4206,4209,4213,4216,4219,4222,4225,4228,4231,4234,4237,4240,4243,4245,4248,4251,4254,4256,4259,4261,4264,4267,4270,4273,4275,4277,4280,4284,4286,4288,4291,4294,4297,4300,4304,4307,4310,4312,4315,4318,4321,4323,4326,4329,4331,4334,4337,4341,4344,4347,4350,4353,4356,4359,4362,4365,4368,4371,4373,4376,4379,4382,4385,4388,4390,4392,4395,4397,4399,4402,4405,4408,4410,4413,4415,4418,4421,4424,4427,4430,4433,4436,4438,4440,4443,4446],{"id":23,"text":4153,"url":23,"identifiers":4154},"Aldaya F., 1991, The Maláguide‐Alpujérride contact (Betic Cordillera, Spain): A brittle extensional detachment, C. R. Acad. Sci, Ser. I, 313, 1447",{},{"id":23,"text":3715,"url":23,"identifiers":4156},{"doi":3715},{"id":23,"text":3721,"url":23,"identifiers":4158},{"doi":3721},{"id":23,"text":4160,"url":23,"identifiers":4161},"10.1038\u002F248309a0",{"doi":4160},{"id":23,"text":4163,"url":23,"identifiers":4164},"Anderson H. J. Seismotectonics of the Western Mediterranean Ph.D. dissertation Univ. of Cambridge Cambridge England 1985.",{},{"id":23,"text":4166,"url":23,"identifiers":4167},"10.1111\u002Fj.1365-246X.1987.tb01661.x",{"doi":4166},{"id":23,"text":4169,"url":23,"identifiers":4170},"Andrieux J., 1971, La structure du Rif Central, Notes Mém. Serv. Geol Maroc, 235, 125",{},{"id":23,"text":4172,"url":23,"identifiers":4173},"Andrieux J., 1971, Sur un modèle explicatif de l'arc de Gibraltar, Bull. Soc. Géol Fr., 15, 555",{},{"id":23,"text":4175,"url":23,"identifiers":4176},"Aparico A., 1991, La edad del volcanism de las islas Columbrete Grande Alboran (Mediterraneo occidentale), Bol. Geol. Min., 102, 562",{},{"id":23,"text":4178,"url":23,"identifiers":4179},"Balanyá J. C., 1987, Les directions structurales dans le Domaine d'Alborán de part et d'autre du Détroit de Gibraltar, C. R. Acad. Sci.. Ser. I, 304, 929",{},{"id":23,"text":4181,"url":23,"identifiers":4182},"10.1111\u002Fj.1365-246X.1980.tb02635.x",{"doi":4181},{"id":23,"text":3754,"url":23,"identifiers":4184},{"doi":3754},{"id":23,"text":4186,"url":23,"identifiers":4187},"Beccaluva P., 1981, Sedimentary Basins of Mediterranean Margins, 361",{},{"id":23,"text":4189,"url":23,"identifiers":4190},"Bellon H., 1981, Sedimentary Basins of Mediterranean Margins, 341",{},{"id":23,"text":4192,"url":23,"identifiers":4193},"10.1038\u002F374249a0",{"doi":4192},{"id":23,"text":4195,"url":23,"identifiers":4196},"10.1038\u002F350124a0",{"doi":4195},{"id":23,"text":4198,"url":23,"identifiers":4199},"10.1038\u002Fphysci235023a0",{"doi":4198},{"id":23,"text":4201,"url":23,"identifiers":4202},"10.1016\u002FB978-0-444-42688-8.50017-5",{"doi":4201},{"id":23,"text":4204,"url":23,"identifiers":4205},"10.1016\u002F0040-1951(83)90178-6",{"doi":4204},{"id":23,"text":4207,"url":23,"identifiers":4208},"Buforn E., 1988, Seismicity and focal mechanisms in south Spain, Bull. Seismol. Soc. Am., 78, 2008",{},{"id":23,"text":4210,"url":23,"identifiers":4211},"Buforn E., 1990, A deep earthquake under southern Spain, 8 March 1990, Bull Seismol. Soc. Am., 81, 1403, 10.1785\u002FBSSA0810041403",{"doi":4212},"10.1785\u002FBSSA0810041403",{"id":23,"text":4214,"url":23,"identifiers":4215},"10.1029\u002F94GL00191",{"doi":4214},{"id":23,"text":4217,"url":23,"identifiers":4218},"10.1144\u002FGSL.SP.1986.019.01.15",{"doi":4217},{"id":23,"text":4220,"url":23,"identifiers":4221},"10.1029\u002FJB083iB11p05385",{"doi":4220},{"id":23,"text":4223,"url":23,"identifiers":4224},"10.1016\u002F0040-1951(80)90180-8",{"doi":4223},{"id":23,"text":4226,"url":23,"identifiers":4227},"10.1007\u002FBF02084927",{"doi":4226},{"id":23,"text":4229,"url":23,"identifiers":4230},"10.1016\u002F0031-9201(76)90073-X",{"doi":4229},{"id":23,"text":4232,"url":23,"identifiers":4233},"10.1029\u002F93TC02231",{"doi":4232},{"id":23,"text":4235,"url":23,"identifiers":4236},"10.1016\u002F0040-1951(88)90028-5",{"doi":4235},{"id":23,"text":4238,"url":23,"identifiers":4239},"Dewey J. F. Episodicity sequence and style at convergent plate boundariesGeol. Assoc. Can Spec. Pap. 20 554–573 1980.",{},{"id":23,"text":4241,"url":23,"identifiers":4242},"10.1029\u002FTC007i006p01123",{"doi":4241},{"id":23,"text":3437,"url":23,"identifiers":4244},{"doi":3437},{"id":23,"text":4246,"url":23,"identifiers":4247},"10.1130\u002F0091-7613(1989)017\u003C0430:NECITW>2.3.CO;2",{"doi":4246},{"id":23,"text":4249,"url":23,"identifiers":4250},"10.1016\u002F0040-1951(93)90087-Z",{"doi":4249},{"id":23,"text":4252,"url":23,"identifiers":4253},"10.1029\u002FJB094iB04p04589",{"doi":4252},{"id":23,"text":3440,"url":23,"identifiers":4255},{"doi":3440},{"id":23,"text":4257,"url":23,"identifiers":4258},"10.1016\u002F0040-1951(93)90158-G",{"doi":4257},{"id":23,"text":3826,"url":23,"identifiers":4260},{"doi":3826},{"id":23,"text":4262,"url":23,"identifiers":4263},"10.2113\u002Fgssgfbull.162.4.611",{"doi":4262},{"id":23,"text":4265,"url":23,"identifiers":4266},"Frizon de Lamotte D., 1991, Cinématique des chévauchements Néogène dans l'arc Bético‐Rifain. Discussion sur les modèles géodynamiques, Bull. Soc. Geol. Fr., 8, 337",{},{"id":23,"text":4268,"url":23,"identifiers":4269},"10.1007\u002FBF02084917",{"doi":4268},{"id":23,"text":4271,"url":23,"identifiers":4272},"García‐Dueñas V., 1988, Plis‐nappes, ci‐saillements syn‐ à post‐métamorphiques et cisaillements ductiles‐fragiles en distension dans les Nevado‐Filabrides (Cordillères bétiques, Espagne), C. R. Acad. Sci., Ser. I, 307, 1389",{},{"id":23,"text":3845,"url":23,"identifiers":4274},{},{"id":23,"text":3857,"url":23,"identifiers":4276},{"doi":3857},{"id":23,"text":4278,"url":23,"identifiers":4279},"Hernandez J., 1985, Chronologie K‐Ar de volcanisme Miocène du Rif oriental (Maroc). Implications tectoniques et magmatologiques, Rev. Géol. Dyn. Géogr. Phys., 26, 85",{},{"id":23,"text":4281,"url":23,"identifiers":4282},"Hernandez J., 1987, Le magmatisme Néogène bético‐rifian et le couloir de décrochement trans‐Alboran, Bull. Soc. géol. Fr., 8, 257, 10.2113\u002Fgssgfbull.III.2.257",{"doi":4283},"10.2113\u002Fgssgfbull.III.2.257",{"id":23,"text":3452,"url":23,"identifiers":4285},{"doi":3452},{"id":23,"text":3878,"url":23,"identifiers":4287},{"doi":3878},{"id":23,"text":4289,"url":23,"identifiers":4290},"10.1016\u002F0040-1951(90)90149-3",{"doi":4289},{"id":23,"text":4292,"url":23,"identifiers":4293},"10.1029\u002FGM023p0293",{"doi":4292},{"id":23,"text":4295,"url":23,"identifiers":4296},"Jeffrays H., 1952, The Earth",{},{"id":23,"text":4298,"url":23,"identifiers":4299},"Kastens K., 1990, The geological evolution of tile Tyrrhenian Sea: An introduction to the scientific results of ODP Leg 107, Proc. Ocean Drill. Program Sci. Results, 107, 3",{},{"id":23,"text":4301,"url":23,"identifiers":4302},"Kastens K., 1988, ODP Leg 107 in the Tyrrhenian Sea: Insights into passive margin and back arc basin evolution, Geol. Soc Am. Bull., 100, 1140, 10.1130\u002F0016-7606(1988)100\u003C1140:OLITTS>2.3.CO;2",{"doi":4303},"10.1130\u002F0016-7606(1988)100\u003C1140:OLITTS>2.3.CO;2",{"id":23,"text":4305,"url":23,"identifiers":4306},"10.1016\u002F0040-1951(88)90090-X",{"doi":4305},{"id":23,"text":4308,"url":23,"identifiers":4309},"10.2113\u002Fgssgfbull.S7-XVII.4.481",{"doi":4308},{"id":23,"text":3893,"url":23,"identifiers":4311},{"doi":3893},{"id":23,"text":4313,"url":23,"identifiers":4314},"10.1098\u002Frsta.1981.0069",{"doi":4313},{"id":23,"text":4316,"url":23,"identifiers":4317},"10.1144\u002Fgsjgs.151.3.0515",{"doi":4316},{"id":23,"text":4319,"url":23,"identifiers":4320},"10.1016\u002F0191-8141(95)00070-T",{"doi":4319},{"id":23,"text":3899,"url":23,"identifiers":4322},{"doi":3899},{"id":23,"text":4324,"url":23,"identifiers":4325},"Maillard A., 1993, Structure et volcanisme de la fosse de Valence (Mediterranée nord‐occidentale), Bull. Soc. Géol. 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