DOCSLIB.ORG

Back Matter (PDF)

Total Page：16

File Type：pdf, Size：1020Kb

Download full-text PDF Read full-text

Load more

Index Page numbers in italic denote figures. Page numbers in bold denote tables. Acadian orogenesis 274, 286, 291–302, 305 Appalachians Acadian slab 299, 300 northern microcontinents 276–277 Acatla´n Complex 239, 240, 256, 347 oceanic terranes 277 mafic rocks 346–350 apparent polar wander path, Laurentia 375, 376–378, palaeogeography 261–265, 263, 264 379, 380, 383 U–Pb zircon analysis 241, 243–256, Apulia, plate tectonics 90, 91, 92,93 257–260, 348 Apulian–Hyblean foreland 115, 115, 117 Ackley Granite 272 40Ar/39Ar dating, Capricorn Orogen 446–451 Aconcagua fold and thrust belt 35, 37,46 Arabian Platform 147, 149 Adria 90, 91, 92, 93, 117 Aracena massif 217, 219–220, 227 Aeolian Islands 114, 118 Aracena Metamorphic Belt 354 African–Anatolian plate boundary 127–152 Arauco Basin 40 Akdag Massif 139, 140, 141 Arisaig Group 272, 275, 291 Albany–Fraser Belt 379–380, 445 Armorican microplate 359 Alleghanian orogeny 164, 271, 273, 276, 346 Ası´s Lithodeme 243, 246, 257, 349 Allochthon Boundary Thrust 406, 407–408, 411, asthenosphere, upwelling 216 419–421, 421–423, 425 Anatolia 133, 137–138, 144, 145, 150, 151 hanging wall 423, 425, 429, 434 Appalachians 284, 286, 291 Orogenic Lid 432 Australia Allochthonous High Pressure Belt 425, 426, 433, 436 Mawsonland 379–380 Allochthonous Medium-Low Pressure Belt 425, Rodinia reconstruction 382, 384 427–428, 429, 436 Austroalpine domain 93, 100, 103 Alpine cycle 104–106 Austroalpine–Carpathian orogen 97–98 Alpine realm, plate tectonics 89–107 Avalonia 276–277, 318 Alpine Tethys 90, 95, 96, 97, 98, 103 accretion of Meguma 302–303 subduction 105–106 accretion to Laurentia 291–293, 300 Altaides 162, 163 Lizard Complex 355 Altiplano flat-slab segment 41–42, 47,48 Amate Unit 244, 247, 249, 256, 258 Badger Basin 272, 285 Amazonia Baffin Suture 460–461, 468 collision with Laurentia 406 Baie Verte oceanic tract 272, 275, 277 Rodinia reconstruction 382, 389–391 Baie Verte–Brompton Line 272, 281, 283 ANACONDA reconstruction 381, 383–384 Baltica 161, 163 Anatolia magnetic anomalies 167, 169 central orogenic belt passive margin 171–173, 180 geology 139, 140, 141–143 rifting 167, 384 tectonic evolution 143, 144, 145 Rodinia reconstruction 377–378, 381 eastern, geology 145–146, 147, 148–151 Bamford Brook fault 272, 275, 289, 290 western Bangemall Supergroup 446, 447, 451, 452 geology 134, 135, 136 Basal Unit 352 tectonic evolution 136–139 Lizard Complex 355 Anatolian plate basalt, K Trig 15 boundary with African plate 127–152 basalt flooding 48 Anatolide block 134, 135, 138 Baskil arc 147, 148 Andes Bazar ophiolite 319, 320, 324–325, 353 flat-slab subduction 31–48 origin and history 334–335 arc magmatism 33, 35,35 Benedict Fault 415, 417 sedimentation 35, 36 Benioff zone tectonics 32,35–36 Chiapas fold-and-thrust belt 66, 67 uplift 46 see also Wadati–Benioff zone Annieopsquotch accretionary tract 277, 279, 281, 283, Bergeron Suture 462–463, 474 284, 305 Bermejo foreland basin 46 Annieopsquotch ophiolite belt 275 Big Island Suture 462, 471, 474 Apennine–Maghrebide peninsula 123 Bitlis massif 146, 146, 147, 148–149, 150, 151 Apennine–Sicilian fold-and-thrust belt 113–117 Bohemian Massif 197, 198, 318 buckling 119, 121–123 Rheic Ocean mafic rocks 356, 357 palaeogeographic evolution 116, 120 U–Pb zircon analysis 204, 205–206, 208, 209, 210 Appalachian orogenesis 4, 164, 271–308, 345 Variscan orogeny 197–212, 211, 356 Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3900358/9781862395756_backmatter.pdf by guest on 25 September 2021 482 INDEX Bolkar Mountains 142 Cookson Group 272, 290 Bouguer gravity anomaly, Lake Taupo 24 Cordillera Blanca 37, 46 Braganc¸a Complex 353 Cordillera de Maran˜o´n 37, 46 Brianc¸onnais terrane 89, 91, 92, 99, 102, 105, 106 Coromandel Volcanic Zone 9, 12 Bridge River terrane 81, 83 Cosoltepec Formation 244, 250, 251, 256, 259, 264 Bucaramanga segment 32, 37, 39–40, 46, 47 mafic rocks 349–350 buckling, Apennine–Sicilian fold-and-thrust belt 119, cratons, reconstruction 375–376 121–123 Cretaceous Burgeo batholith 272 Alpine tectonics 97–104 Burntwood back-arc basin 469–470 oceans 99–102 crystallization, assimilation fractional 142, 143, 144 Cabo Otegal Complex 320, 321 Cumberland Batholith 468, 469, 471 Cabot fault 272 Cut Throat Island Fault 415, 417 Cache Creek terrane 71, 72 Cyprean Arc 128, 132 geological setting 73, 75, 76 subduction zone 131–132, 133 high-pressure rocks 81–82 extrusion model 82–84 Dashwoods microcontinent 276, 277, 278, 279, stratigraphy 74 281, 283, 303–304, 306 Cadomian orogeny 199, 209 De Pas Batholith 469, 471 Calabrian nappes 115 deformation Calabrian orocline 3, 113–117, 118 Acadian orogeny 295–296 tectonic model 119, 118–120 Andes 48 Calabrian subduction zone 117–118 Ossa Morena Zone 216–234 Calabrian–Peloritanian nappes 114 Salinic orogeny 288, 289–291 caldera volcanoes, Taupo Volcanic Zone 12,16–25 Saxo-Thuringian Zone 201, 202 Caledonia fault 272, 291 Taconic orogeny 281, 306 Canadian Cordillera 71–84, 72 Urals 182 Canadian Shield 457, 458 Dewar Formation 75 Canoas Unit 244, 247, 249, 256, 258, 350 Dog Bay Line 272, 289–290, 293, 297 Cantabrian zone 350, 351 Do¨hlen Basin 202, 203, 204, 207, 209, 211–212 Cape Ray fault–Victoria Lake shear zone 296 Dover fault 272, 291 Cappadocian volcanic province 140, 143 Dunn Point volcanics 275 Capricorn Orogen 5–6, 445–454, 446 Dunnage me´lange 284, 285 Carballo–Bazar slice 324 dykes, mafic Careo´n ophiolite 319, 320, 327–329, 353 Appalachians 276–277 origin and history 333, 336–338 Grenville Front 413, 415–416, 418, 423 Carnegie Ridge 32,40 Trans-Hudson Orogen 467, 471 Carreiro shear zone 331, 333, 338 West Australian Craton 452 Central Anatolian Crystalline Complex 139, 140, see also Sudbury dykes 141–142 late-Cretaceous plutons 142, 143, 144 East Anatolian High Plateau 145, 146, 148 Central Asian ocean 161 deformation and volcanism 149, 151 Central Atlantic opening 95, 96 tectonic evolution 150, 151 Central Uralian megazone 166 East Anatolian subduction-accretion complex tectonostratigraphy 168 148–149, 150, 151 Chain Lakes Massif 272 East Magnitogorsk Fault 165, 166, 185 channel flow, Grenville Province 406, 431, 432, tectonostratigraphy 168 434, 435, 436, 437 East Magnitogorskian me´lange zone 166 Chazumba Formation 244, 252, 254, 256, 260 East Pontide arc 145–146, 146 Chiapas fold-and-thrust belt 55–67, 56 East Uralian zone 165, 166, 185, 188 China tectonostratigraphy 168 North, Rodinia reconstruction 382, 388–389, 392 Eastern Cordillera 39–40, 41, 42, 46 South, Rodinia reconstruction 382, 386–388 Eastern Turkey Seismic Experiment 151 Choiyoi Group 44–45 Edgecumbe volcanoes 13 Cilo ophiolite 147, 149 Edmundian Orogenesis 446, 451–452, 454 Cimmerian orogeny 182 El Epazote Unit 244, 247, 249, 256, 258, 261 Coaker porphyry 275 El Rodeo Formation 244, 247, 249, 256, 258, 262 Coastal arc 292, 294 Elazig–Palu nappe 147, 148 Coatlaco Unit 244, 250, 251, 256, 259, 350 Elbe Zone 198, 201–204, 203 Cobequid–Chedabucto fault 272, 303 exhumation 204, 212 COBRA reconstruction 390–391 geochronology 209–212 Cold Spring Pond me´lange 275 strike-slip processes 201–202, 202, 211 Congo craton, Rodinia reconstruction 380–381, U–Pb zircon analysis 204, 205–206, 208, 209, 210 382, 383–384 Eocene, Alpine tectonics 103, 106 Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3900358/9781862395756_backmatter.pdf by guest on 25 September 2021 INDEX 483 erosion, subduction Gondwana Cache Creek HP rocks 82–83 Appalachian microcontinents 276–277 Chiapas fold-and-thrust belt 64 collision with Avalonia 216 Errabiddy Shear Zone 449–450, 451, 452 collision with Laurussia 198, 319, 321 Erzgebirge nappe complex 201, 202 Mexican terranes 264–265 Esperanza granitoids 243, 244, 245, 247 palaeogeography 345 ESRU–SB profile 185, 186, 187 Gondwanaland 391, 393–394 Europe, Eastern, Rheic Ocean mafic rocks graben systems, western Anatolia 135, 138 357–358 granite, biotite, Evora massif, U–Th–Pb analysis Evora Massif 217, 218, 219, 227 222, 226, 229, 230, 232 U–Th–Pb analysis 222–230, 232 granite magmatism, Urals 181 E´ vora–Aracena–Lora del Rı´o metamorphic belt Granite Supersuite plutons 140, 142, 144 216–217, 232 granitoids exhumation Acatla´n Complex 244, 245, 247, 248, 256, 257, Anatolia 138 258, 259, 261 Elbe Zone 204, 212 Appalachians 273, 284 Grenville Front 417, 420, 433–434, 437 Elbe Zone 203–204, 209 Ossa–Morena Zone 216, 232 Lausitz Block 202, 209 Piaxtla Suite 350 Ossa Morena Zone 217 Salinic 290 Granjeno Schist 240, 252, 255, 256, 257, 260, 261–265 San Rafael block 43 Granville Lake Structural Zone 468–469, 472 Taconic 284 Green Bay fault 272 extension greenstone belt, Grenville Front 414, 416, 418 Andes 48 Grenville APW loop 376–377, 385 eastern Mediterranean 137, 138–139, 145 Grenville foreland 413, 415–417, 418 Variscan, SW Iberian Massif 231–234 Grenville Front 406, 407, 409–411, 413–414, 414–417, 418, 420 faulting exhumation 417, 420, 433–434, 437 Central Anatolian Crystalline Complex 145 Lithoprobe seismic study 409–410, 411 East Anatolian High Plateau 149 Grenville Front Tectonic Zone 409, 410–411, 413, Sonda de Campeche 63 414–416, 417, 418 STEP 133 Grenville Orogen 406–407, 407, 420 Taupo Volcanic zone 13–16, 14 Grenville Province Fitzcarrald arch 37, 38 channel flow 406, 431, 432, 434, 435, 436, 439 Flin Flon–Glennie Complex 460, 463–464, 466–467, general features 406–409, 407 469–470, 471, 472 interior, metamorphism and deformation 421–429 flysch large hot long-duration orogen 5, 405–438 Alpine 104 metamorphism 406–409 Anatolian orogenic belt 136 Ottawan event 421–429, 430, 432–433, 435 Uralides
Recommended publications
  • Programme Monday, March 24

    Programme Monday, March 24

    23rd LAK, 2014, Heidelberg Programme 13 Programme Monday, March 24 INF 252, Hörsäle Chemie 18:00– CONFERENCE DESK OPENING 21:00 18:00– ICEBREAKER PARTY 22:00 * Sponsored by DFG travel grants 14 Programme 23rd LAK, 2014, Heidelberg Tuesday I, March 25 INF 252, Hörsaal Ost INF 252, Hörsaal West 09:30 Welcome Christina Ifrim and Wolfgang Stinnesbeck DAAD-Fördermöglichkeiten für Geowissenschaftler aus/nach Lateinamerika Sybilla Tinnap, DAAD, Bonn Talk 141: Funding Opportunities for Scientific and Technological Cooperation: The Role of the Project Management Agency European and International Cooperation International Bureau of the Bmbf Inge Lamberz de Bayas, Internationales Büro, Bundesministerium für Bildung und Forschung, Bonn International Cooperation in DFG-Programmes – Earth Sciences in Latin America Dietrich Halm, DFG, Bonn 11:00 COFFEE BREAK and POSTER SESSION Session 1: The southernmost dinosurs in Latin Session 2: Water America and their environment Chair: Heinrich Adolf Horn Chair: Marcelo Leppe 11:20 Talk 205: Late Cretaceous Terrestrial Biota from Las Talk 132: Nutrient fluxes in the groundwater affecting Chinas-Cerro Guido Complex, Magallanes Region, the northern mangrove coast of the peninsula Yucatán Southern Chile: A Key Area for the Antarctic-South (México) American Biogeography Lisa Krienen, Thomas Rüde, Eduardo Graniel Castro and Antonio Marcelo Leppe, Wolfgang Stinnesbeck, Eberhard Frey, Héctor Cardona Benavides Mansilla, Manfred Vogt, Edwin Gonzalez, Leslie Manriquez, Katherine Cisternas, Maritza Mihoc and Toshiro Jujihara
  • Longitudinal and Temporal Evolution of the Tectonic Style Along The

    Longitudinal and Temporal Evolution of the Tectonic Style Along The

    Longitudinal and Temporal Evolution of the Tectonic Style Along the Cyprus Arc System, Assessed Through 2-D Reflection Seismic Interpretation Vasilis Symeou, Catherine Homberg, Fadi H. Nader, Romain Darnault, Jean-claude Lecomte, Nikolaos Papadimitriou To cite this version: Vasilis Symeou, Catherine Homberg, Fadi H. Nader, Romain Darnault, Jean-claude Lecomte, et al.. Longitudinal and Temporal Evolution of the Tectonic Style Along the Cyprus Arc System, Assessed Through 2-D Reflection Seismic Interpretation. Tectonics, American Geophysical Union (AGU), 2018, 37 (1), pp.30 - 47. 10.1002/2017TC004667. hal-01827497 HAL Id: hal-01827497 https://hal.sorbonne-universite.fr/hal-01827497 Submitted on 2 Jul 2018 HAL is a multi-disciplinary open access L’archive ouverte pluridisciplinaire HAL, est archive for the deposit and dissemination of sci- destinée au dépôt et à la diffusion de documents entific research documents, whether they are pub- scientifiques de niveau recherche, publiés ou non, lished or not. The documents may come from émanant des établissements d’enseignement et de teaching and research institutions in France or recherche français ou étrangers, des laboratoires abroad, or from public or private research centers. publics ou privés. Longitudinal and Temporal Evolution of the Tectonic Style Along the Cyprus Arc System, Assessed Through 2-D Reflection Seismic Interpretation Vasilis Symeou1,2 , Catherine Homberg1, Fadi H. Nader2, Romain Darnault2, Jean-Claude Lecomte2, and Nikolaos Papadimitriou1,2 1ISTEP, Universite Pierre et Marie Curie, Paris, France, 2Geosciences Division, IFP Energies nouvelles, Rueil-Malmaison, Key Points: • Lateral changes from a compressional France to a strike-slip regime along the Cyprus Arc • Different crustal nature in the eastern Abstract The Cyprus Arc system constitutes a major active plate boundary in the eastern Mediterranean Mediterranean region.
  • The Terrane Concept and the Scandinavian Caledonides: a Synthesis

    The Terrane Concept and the Scandinavian Caledonides: a Synthesis

    The terrane concept and the Scandinavian Caledonides: a synthesis DAVID ROBERTS Roberts , D. 1988: The terrane concept and the Scandinavian Caledonides: a synthesis. Nor. geol . unders . Bull. 413. 93-99. A revised terrane map is presented for the Scandinavian Caledcnldes. and an outline is given of the principal suspect and exot ic terranes and terrane-complexe s identified outboa rd from the Baltoscand ian miogeocline. The outermost part of the Baltoscandian continental margin is itself suspect , in the terrane sense. since the true palaeogeographical location s of rocks now represented in the Seve and serey-seuano Nappes, while inferred, are not known. The orogen -internal exotic terranes embrace the oceanic/eugeoclinal elements of the Caledonides, represented by the mag­ matosed imentary assemblages of the Koli Nappes, including ophiolite fragments and island arc products. Even more exot ic terranes occur in the highest parts of the tectonostratigraphy, inclu­ ding units which are thought possibly to derive from the Laurentian side of lapetus . D. Roberts. Norges geologiske uruierseketse, Postboks 3006. Lade, N-7002 Trondbeim , Norway . Introduction Project 233 has been to prepare a preliminary Earlier in this decade much of the research terrane map' at 1:5 M scale (Roberts et al. effort in the Caledonides of Scandinavia was 1986) for a larger, circum-Atlantic compilation. channelled through the highly successfu l IGCP This map, much simplified, is really one of Project 27 The Caledonide Orogen ' (Gee & palaeo-environments (marginal basins, vol­ Sturt 1985). An important aspect of the collabo­ canic arc comp lexes, overstep sequences , rative work in this project was that of map etc.), and not of terranes in the true sense.
  • Resolving the Variscan Evolution of the Moldanubian Sector of The

    Resolving the Variscan Evolution of the Moldanubian Sector of The

    Journal of Geosciences, 52 (2007), 9–28 DOI: 10.3190/jgeosci.005 Original paper Resolving the Variscan evolution of the Moldanubian sector of the Bohemian Massif: the significance of the Bavarian and the Moravo–Moldanubian tectonometamorphic phases Fritz FINGER1*, Axel GERDEs2, Vojtěch JANOušEk3, Miloš RENé4, Gudrun RIEGlER1 1University of Salzburg, Division of Mineralogy, Hellbrunnerstraße 34, A-5020 Salzburg, Austria; [email protected] 2University of Frankfurt, Institute of Geoscience, Senckenberganlage 28, D-60054 Frankfurt, Germany 3Czech Geological Survey, Klárov 3, 118 21 Prague 1, Czech Republic 4Academy of Sciences, Institute of Rock Structure and Mechanics, V Holešovičkách 41, 182 09 Prague 8, Czech Republic *Corresponding author The Variscan evolution of the Moldanubian sector in the Bohemian Massif consists of at least two distinct tectonome- tamorphic phases: the Moravo–Moldanubian Phase (345–330 Ma) and the Bavarian Phase (330–315 Ma). The Mora- vo–Moldanubian Phase involved the overthrusting of the Moldanubian over the Moravian Zone, a process which may have followed the subduction of an intervening oceanic domain (a part of the Rheiic Ocean) beneath a Moldanubian (Armorican) active continental margin. The Moravo–Moldanubian Phase also involved the exhumation of the HP–HT rocks of the Gföhl Unit into the Moldanubian middle crust, represented by the Monotonous and Variegated series. The tectonic emplacement of the HP–HT rocks was accompanied by intrusions of distinct magnesio-potassic granitoid melts (the 335–338 Ma old Durbachite plutons), which contain components from a strongly enriched lithospheric mantle source. Two parallel belts of HP–HT rocks associated with Durbachite intrusions can be distinguished, a western one at the Teplá–Barrandian and an eastern one close to the Moravian boundary.
  • Investigation of the Effects of Nazca-South America

    Investigation of the Effects of Nazca-South America

    Investigation of the Effects of Nazca-South America Plate Collision along the Peruvian-Chilean Active Continental Margin through Teleseismic Receiver Function Analysis Item Type text; Electronic Dissertation Authors Bishop, Brandon Publisher The University of Arizona. Rights Copyright © is held by the author. Digital access to this material is made possible by the University Libraries, University of Arizona. Further transmission, reproduction or presentation (such as public display or performance) of protected items is prohibited except with permission of the author. Download date 10/10/2021 22:07:29 Link to Item http://hdl.handle.net/10150/627698 INVESTIGATION OF THE EFFECTS OF NAZCA-SOUTH AMERICA PLATE COLLISION ALONG THE PERUVIAN-CHILEAN ACTIVE CONTINENTAL MARGIN THROUGH TELESEISMIC RECEIVER FUNCTION ANALYSIS by Brandon T. Bishop __________________________ Copyright © Brandon T. Bishop 2018 A Dissertation Submitted to the Faculty of the DEPARTMENT OF GEOSCIENCES In Partial Fulfillment of the Requirements For the Degree of DOCTOR OF PHILOSOPHY In the Graduate College THE UNIVERSITY OF ARIZONA 2018 STATEMENT BY AUTHOR This dissertation has been submitted in partial fulfillment of the requirements for an advanced degree at the University of Arizona and is deposited in the University Library to be made available to borrowers under rules of the Library. Brief quotations from this dissertation are allowable without special permission, provided that an accurate acknowledgement of the source is made. Requests for permission for extended quotation from or reproduction of this manuscript in whole or in part may be granted by the head of the major department or the Dean of the Graduate College when in his or her judgment the proposed use of the material is in the interests of scholarship.
  • Trans-Lithospheric Diapirism Explains the Presence of Ultra-High Pressure

    Trans-Lithospheric Diapirism Explains the Presence of Ultra-High Pressure

    ARTICLE https://doi.org/10.1038/s43247-021-00122-w OPEN Trans-lithospheric diapirism explains the presence of ultra-high pressure rocks in the European Variscides ✉ Petra Maierová1 , Karel Schulmann1,2, Pavla Štípská1,2, Taras Gerya 3 & Ondrej Lexa 4 The classical concept of collisional orogens suggests that mountain belts form as a crustal wedge between the downgoing and overriding plates. However, this orogenic style is not compatible with the presence of (ultra-)high pressure crustal and mantle rocks far from the plate interface in the Bohemian Massif of Central Europe. Here we use a comparison between geological observations and thermo-mechanical numerical models to explain their formation. 1234567890():,; We suggest that continental crust was first deeply subducted, then flowed laterally under- neath the lithosphere and eventually rose in the form of large partially molten trans- lithospheric diapirs. We further show that trans-lithospheric diapirism produces a specific rock association of (ultra-)high pressure crustal and mantle rocks and ultra-potassic magmas that alternates with the less metamorphosed rocks of the upper plate. Similar rock asso- ciations have been described in other convergent zones, both modern and ancient. We speculate that trans-lithospheric diapirism could be a common process. 1 Center for Lithospheric Research, Czech Geological Survey, Prague 1, Czech Republic. 2 EOST, Institute de Physique de Globe, Université de Strasbourg, Strasbourg, France. 3 Institute of Geophysics, Department of Earth Science, ETH-Zurich,
  • A Pliocene Mega-Tsunami Deposit and Associated Features in the Ranquil Formation, Southern Chile ⁎ J.P

    A Pliocene Mega-Tsunami Deposit and Associated Features in the Ranquil Formation, Southern Chile ⁎ J.P

    A Pliocene mega-tsunami deposit and associated features in the Ranquil Formation, southern Chile ⁎ J.P. Le Roux a, , Sven N. Nielsen b,1, Helga Kemnitz b, Álvaro Henriquez a a Departamento de Geología, Facultad de Ciencias Físicas y Matemáticas, Universidad de Chile, Casilla 13518, Correo 21, Santiago, Chile b GeoForschungsZentrum Potsdam, Section 3.1, Telegrafenberg, 14473 Potsdam, Germany Abstract An exceptionally large tsunami affected the coastline of southern Chile during the Pliocene. Its backflow eroded coarse beach and coastal dune sediments and redistributed them over the continental shelf and slope. Sandstone dykes and sills injected from the base of the resulting hyperconcentrated flow into underlying cohesive muds, assisted in plucking up large blocks of the latter and incorporating them into the flow. Locally, the rip-up intraclasts were fragmented further by smaller-scale injections to form a distinct breccia of angular to rounded mudstone clasts within a medium to coarse sandstone matrix. Sandstone sills in places mimic normal sedimentary beds, complete with structures resembling inverse gradation, planar laminae, as well as ripple and trough cross-lamination. These were probably formed by internal sediment flow and shear stress as the semi-liquefied sand was forcefully injected into cracks. In borehole cores, such sills can easily be misinterpreted as normal sedimentary beds, which can have important implications for hydrocarbon exploration. Keywords: Tsunami; Sandstone dykes; Debris flow; Mimic sedimentary structures; Eltanin impact; Hydrocarbon reservoirs 1. Introduction associated sedimentological features including large rip-up clasts and well rounded basement boulders incorporated in- The west coast of South America has a narrow shelf and to the debris, as well as sand injection from the base of the steep continental slope into a deep subduction trench.
  • Pore-Water in Marine Sediments Associated to Gas Hydrate Dissociation Offshore Lebu, Chile. Carolina Cárcamo1,2, Iván Vargas-C

    Pore-Water in Marine Sediments Associated to Gas Hydrate Dissociation Offshore Lebu, Chile. Carolina Cárcamo1,2, Iván Vargas-C

    Hydrol. Earth Syst. Sci. Discuss., https://doi.org/10.5194/hess-2018-362 Manuscript under review for journal Hydrol. Earth Syst. Sci. Discussion started: 29 August 2018 c Author(s) 2018. CC BY 4.0 License. 1 Pore-water in marine sediments associated to gas hydrate dissociation 2 offshore Lebu, Chile. 3 4 Carolina Cárcamo1,2, Iván Vargas-Cordero1, Francisco Fernandoy1, Umberta 5 Tinivella3, Diego López-Acevedo4, Joaquim P. Bento5, Lucía Villar-Muñoz6, Nicole 6 Foucher1, Marion San Juan1, Alessandra Rivero1 7 8 1 Universidad Andres Bello, Facultad de Ingeniería, Quillota 980, Viña del Mar, Chile 9 2 Centro de Investigación Marina Quintay. CIMARQ. Facultad de Ciencias de la Vida. Universidad 10 Andres Bello, Viña del Mar, Chile. 11 3 OGS Istituto Nazionale di Oceanografia e di Geofisica Sperimentale, Borgo Grotta Gigante 42/C, 12 34010, Sgonico, Italy. 13 4 Universidad de Concepción, Departamento de Oceanografía, Programa COPAS Sur-Austral, 14 Campus Concepción Víctor Lamas 1290, P.O. Box 160-C, Concepción, Chile 15 5 Escuela de Ciencias del Mar, Pontificia Universidad Católica de Valparaíso, Av. Altamirano 1480, 16 2360007 Valparaíso, Chile. 17 6 GEOMAR Helmholtz Centre for Ocean Research, Wischhofstr. 1-3, 24148 Kiel, Germany. 18 19 ABSTRACT 20 Gas hydrate occurrences along the Chilean margin has been documented, but the 21 processes associated to fluid escapes originated by gas hydrate dissociation yet are 22 unknown. Here, we report morphologies growing related to fluid migration in the 23 continental shelf offshore western Lebu (37 °S) by analysing mainly geochemical 24 features. In this study oxygen and deuterium stable water isotopes in pore water 25 were measured.
  • Crustal Structure of the Eastern Anatolia Region (Turkey) Based on Seismic Tomography

    Crustal Structure of the Eastern Anatolia Region (Turkey) Based on Seismic Tomography

    geosciences Article Crustal Structure of the Eastern Anatolia Region (Turkey) Based on Seismic Tomography Irina Medved 1,2,* , Gulten Polat 3 and Ivan Koulakov 1 1 Trofimuk Institute of Petroleum Geology and Geophysics SB RAS, Prospekt Koptyuga, 3, 630090 Novosibirsk, Russia; [email protected] 2 Sobolev Institute of Geology and Mineralogy SB RAS, Prospekt Koptyuga, 3, 630090 Novosibirsk, Russia 3 Department of Civil Engineering, Yeditepe University, 26 Agustos Yerleskesi, 34755 Istanbul, Turkey; [email protected] * Correspondence: [email protected]; Tel.: +7-952-922-49-67 Abstract: Here, we investigated the crustal structure beneath eastern Anatolia, an area of high seismicity and critical significance for earthquake hazards in Turkey. The study was based on the local tomography method using data from earthquakes that occurred in the study area provided by the Turkiye Cumhuriyeti Ministry of Interior Disaster and Emergency Management Directorate Earthquake Department Directorate of Turkey. The dataset used for tomography included the travel times of 54,713 P-waves and 38,863 S-waves from 6355 seismic events. The distributions of the resulting seismic velocities (Vp, Vs) down to a depth of 60 km demonstrate significant anomalies associated with the major geologic and tectonic features of the region. The Arabian plate was revealed as a high-velocity anomaly, and the low-velocity patterns north of the Bitlis suture are mostly associated with eastern Anatolia. The upper crust of eastern Anatolia was associated with a ~10 km thick high-velocity anomaly; the lower crust is revealed as a wedge-shaped low-velocity anomaly. This kind of seismic structure under eastern Anatolia corresponded to the hypothesized existence of Citation: Medved, I.; Polat, G.; a lithospheric window beneath this collision zone, through which hot material of the asthenosphere Koulakov, I.
  • Redalyc.Depositional Environment of Stelloglyphus Llicoensis Isp. Nov

    Redalyc.Depositional Environment of Stelloglyphus Llicoensis Isp. Nov

    Andean Geology ISSN: 0718-7092 [email protected] Servicio Nacional de Geología y Minería Chile Le Roux, Jacobus P.; Nielsen, Sven N.; Henríquez, Álvaro Depositional environment of Stelloglyphus llicoensis isp. nov.: a new radial trace fossil from the Neogene Ranquil Formation, south-central Chile Andean Geology, vol. 35, núm. 2, julio, 2008, pp. 307-319 Servicio Nacional de Geología y Minería Santiago, Chile Disponible en: http://www.redalyc.org/articulo.oa?id=173918441006 Cómo citar el artículo Número completo Sistema de Información Científica Más información del artículo Red de Revistas Científicas de América Latina, el Caribe, España y Portugal Página de la revista en redalyc.org Proyecto académico sin fines de lucro, desarrollado bajo la iniciativa de acceso abierto Revista Geológica de Chile 35 (2): 307-319. July, 2008 Revista Geológica de Chile www.scielo.cl/rgch.htm Depositional environment of Stelloglyphus llicoensis isp. nov.: a new radial trace fossil from the Neogene Ranquil Formation, south-central Chile jacobus P. Le Roux1, Sven N. Nielsen2, álvaro Henríquez1 1 Departamento de Geología, Facultad de Ciencias Físicas y Matemáticas, Universidad de Chile, Casilla 13518, Correo 21, Santiago, Chile. [email protected]; [email protected] 2 Institut für Geowissenschaften, Christian-Albrechts-Universität, Ludewig-Meyn-Str.10, 24118 Kiel, Germany. [email protected] ABSTRACT. Stelloglyphus llicoensis isp. nov. is a large radial, discoidal to ellipsoidal trace fossil with a central shaft and single to bifurcating branches radiating from different levels. A 30 m thick measured section of the Ranquil For- mation at Punta Litre contains an associated trace fossil assemblage including Zoophycos, Chondrites, Phycosiphon, Nereites missouriensis, Lockeia siliquaria, Psammichnites(?), Parataenidium, Ophiomorpha, and Rhizocorallium, some of which reworked the Stelloglyphus traces.
  • 3D Seismic Velocity Structure Around Plate Boundaries and Active Fault Zones 47

    3D Seismic Velocity Structure Around Plate Boundaries and Active Fault Zones 47

    ProvisionalChapter chapter 3 3D Seismic Velocity Structure AroundAround PlatePlate BoundariesBoundaries and Active Fault Zones and Active Fault Zones Mohamed K. Salah Mohamed K. Salah Additional information is available at the end of the chapter Additional information is available at the end of the chapter http://dx.doi.org/10.5772/65512 Abstract Active continental margins, including most of those bordering continents facing the Pacific Ocean, have many earthquakes. These continental margins mark major plate boundaries and are usually flanked by high mountains and deep trenches, departing from the main elevations of continents and ocean basins, and they also contain active volcanoes and, sometimes, active fault zones. Thus, most earthquakes occur predomi‐ nantly at deep‐sea trenches, mid‐ocean spreading ridges, and active mountain belts on continents. These earthquakes generate seismic waves; strong vibrations that propagate away from the earthquake focus at different speeds, due to the release of stored stress. Along their travel path from earthquake hypocenters to the recording stations, the seismic waves can image the internal Earth structure through the application of seismic tomography techniques. In the last few decades, there have been many advances in the theory and application of the seismic tomography methods to image the 3D structure of the Earth's internal layers, especially along major plate boundaries. Applications of these new techniques to arrival time data enabled the detailed imaging of active fault zones, location of magma chambers beneath active volcanoes, and the forecasting of future major earthquakes in seismotectonically active regions all over the world. Keywords: 3D seismic structure, seismic tomography, Vp/Vs ratio, plate boundaries, crustal structure 1.
  • A New Classification of the Turkish Terranes and Sutures and Its Implication for the Paleotectonic History of the Region

    A New Classification of the Turkish Terranes and Sutures and Its Implication for the Paleotectonic History of the Region

    Available online at www.sciencedirect.com Tectonophysics 451 (2008) 7–39 www.elsevier.com/locate/tecto A new classification of the Turkish terranes and sutures and its implication for the paleotectonic history of the region ⁎ Patrice Moix a, , Laurent Beccaletto b, Heinz W. Kozur c, Cyril Hochard a, François Rosselet d, Gérard M. Stampfli a a Institut de Géologie et de Paléontologie, Université de Lausanne, CH-1015 Lausanne, Switzerland b BRGM, Service GEOlogie / Géologie des Bassins Sédimentaires, 3 Av. Cl. Guillemin - BP 36009, FR-45060 Orléans Cedex 2, France c Rézsü u. 83, H-1029 Budapest, Hungary d IHS Energy, 24, chemin de la Mairie, CH-1258 Perly, Switzerland Received 15 October 2007; accepted 6 November 2007 Available online 14 December 2007 Abstract The Turkish part of the Tethyan realm is represented by a series of terranes juxtaposed through Alpine convergent movements and separated by complex suture zones. Different terranes can be defined and characterized by their dominant geological background. The Pontides domain represents a segment of the former active margin of Eurasia, where back-arc basins opened in the Triassic and separated the Sakarya terrane from neighbouring regions. Sakarya was re-accreted to Laurasia through the Balkanic mid-Cretaceous orogenic event that also affected the Rhodope and Strandja zones. The whole region from the Balkans to the Caucasus was then affected by a reversal of subduction and creation of a Late Cretaceous arc before collision with the Anatolian domain in the Eocene. If the Anatolian terrane underwent an evolution similar to Sakarya during the Late Paleozoic and Early Triassic times, both terranes had a diverging history during and after the Eo-Cimmerian collision.