Preliminary Terrane and Overlap Assemblage Map of Altay-Sayan

Total Page:16

File Type:pdf, Size:1020Kb

Preliminary Terrane and Overlap Assemblage Map of Altay-Sayan EXPLANATION TECTONIC ENVIRONMENTS ABBREVIATIONS FOR OVERLAP SEDIMENTARY and Early Proterozoic) RA Rudny-Altai (island arc) (Late Devonian and AND VOLCANIC ASSEMBLAGES BK Belaya-Kitoi (cratonal) (Archean? and Early Early Carboniferous) Proterozoic) SG Sugash (island arc) (Cambrian) Basement of craton and cratonal terranes ag Agul molasse basin with Lochkovian-Pragian BL Belokurikha (metamorphic) (SH) Sharizhalgai block (cratonal basement) rift-related volcanic rocks (Devonian and BR Baratal (island arc) (Vendian and Early (Archean) Passive continental margin tarrane Early Carboniferous) Cambrian) SHT Shutkhulai (metamorphic) am Altai-Mongolia volcano-sedimentary belt with BS Borus (accretionary wedge, predominantly SL Salair (island arc) (Cambrian to Early o o 84 90 96o Emsian subduction-related volcanic rocks oceanic rocks) (Vendian and Early Cambrian) Ordovician) Continental margin turbidite terrane (Early and Middle Devonian) BZ Bazibai (metamorphic) SM Sisim (island arc) (Vendian and Early Mzs ba Biya molasse basin (Late Cambrian and CH Charysh (continental margin turbidites) Cambrian) Island-arc terrane Ordovician) (Cambrian to Silurian) SN Saratan (oceanic) (Vendian and Early CzMzs Mzs bs Bokson-Sarkhoi sedimentary basin (Vendian CHU Chagan-Uzun (accretionary wedge, Cambrian) Back-arc terranes undivided to Middle Cambrian) predominantly oceanic rocks) (Vendian and SR Sarkhoi (continental margin arc) (Late mn Krasnoyarsk NSC o KS (SY) 56 is Intrasayan volcano-sedimentary belt with Early Cambrian) Proterozoic) Continental margin arc terrane Lochkovian-Pragian volcanic rocks DB Dibi (accretionary wedge, predominantly SS South Sangilen (passive continental margin) td (Devonian and Early Carboniferous) turbidites) (Late Proterozoic?) (late Proterozoic) TT KS KV Mzs Accretionary wedge terrane, kh Khmelev back-arc basin (Late Devonian and DR Derba (passive continental margin) (Late (SY) South Yenisei block (cratonal basement) KZ Mzs KS predominantly turbidites Early Carboniferous) Proterozoic) (Archean and Early Proterozoic) kt Mzs DR Novosibirsk ag khs Khemchik-Sistigkhem molasse basin (Late DZ Dzhebash (accretionary wedge, SZ Sizim (passive continental margin) (Late kt NSC Accretionary wedge terrane, Mzs KA ma Cambrian to Silurian) predominantly turbidites) (Vendian and Early Proterozoic) ag (TN) KV predominantly oceanic rocks sl kt Kolyvan-Tom back-arc basin (Late Devonian Cambrian) TA Talitsk (continental margin turbidites) mn NSC and Early Carboniferous) ET East Tuva (back-arc terranes collage) (Cambrian and Ordovician) kz SM KN o KM KS Accretionary wedge undivided Mzs 102 kz Kuznetsk molasse basin (Late Devonian to (Vendian to Middle Cambrian) TK Terekta (accretionary wedge, predominantly KM SM KS DR KV NSC Oceanic terrane Permian) GR Gargan (cratonal) (Archean) turbidites) (Vendian and Early Cambrian) kh SL sl KK (BI) tb ma Mana sedimentary basin (Vendian to Middle IL Ilchir (accretionary wedge, predominantly TL Teletsk (accretionary wedge, predominantly SL Mzs Cambrian) oceanic rocks) (Late Proterozoic) turbidites) (Vendian and Early Cambrian) kz mr Metamorphic terrane KS KK mn Minusa molasse basin with Lochkovian- IR Irkut (metamorphic) TM Tomsk(metamorphic) Mzs KS AL KV (UR) Pragian rift-related volcanic rocks (Devonian IZR Izikh (accretionary wedhe terrane, (TN) Tumanshet block (cratonal basement) mn BZ NSC NSC to Early Permian) predominantly oceanic rocks) (Vendian (Proterozoic) CzMzs TM NRS KS NSC OVERLAP ASSEMBLAGES mr Mirichun sedimentary basin (Vendian and and Early Cambrian) TO Tannuola (island arc) (Vendian and Early (OT) Early Cambrian) KA Kuznetsk-Alatau (oceanic) (Vendian Cambrian) CzMzs AL TT KH ET na North Altai volcano-sedimentary belt with and Early Cambrian) TT Tebes-Kitat (island arc) (Early and Middle AN AI ET volcanic rocks (rift-related) KTK khs NSC Czv Early Givetian subduction-related volcanic KBN Kalba-Narym (accretionary wedge, Cambrian) AL tb BK (Neogene and Quaternary) ET Irkutsk rocks (Early and Middle Devonian) predominantly turbidites) (Devonian and TU Tunka (island arc) (Early Paleozoic) kz o KS tv Czv OK 52 sedimentary and volcanic rocks ok Oka molasse basin (Ordovician and Silurian) Early Carboniferous) TT Telbes-Kitat (island arc) (Early and Middle ul KH (SH) NSC Czsv KS is SHT KHO (rift-related)(Tertiary and Quaternary) sa South Altai back-arc basin (Late Devonian KH Khamsara (island arc) (Vendian to Early Cambrian) BL KH tv na ul NRS DZ (SH) na BS WS bs and Early Carboniferous) Cambrian) UC Ulus-Cherga (island arc) (Early and Middle AL IZ ET IR sedimentary rocks (intracontinental MR UO UO Czsv Czs sl Salair volcano-sedimentary belt with Early KHO Khugein-Oka (accretionary wedge, Cambrian) AL DB IL TU Lake Baikal basins) (Cenozoic) UL tv KHO ZS ACH ba SR Givetian subduction-related volcanic rocks predominantly turbidites) (Late Proterozoic) UL Uimen-Lebed (island arc) (Vendian to Middle Mzs sm sedimentary rocks (intracontinental UL GR (Early and Middle Devonian) KK Kizir-Kazir (island arc) (Vendian and Early Cambrian) KRT KT CzMzs basins) (Cenozoic and Mesozoic) ACH sm Shumak sedimentary basin (Vendian and Cambrian) UO Ulugo (island arc) (Vendian to Early am TA na ul KT AO NS UC KT Mzs ON sedimentary rocks (intracontinental Early Carboniferous) KM Kanim (island arc) (Vendian and Early Cambrian) is is is khs KT Mzs AM Hovsgol-Nuur basins) (Jurassic) tb Telbes-Barzas volcano-sedimentary belt Cambrian) (UR) Urik-Iya block (cratonal basement) UL Mzs tv KBN ACH SN tv ET am UC KT tv with Emsian and Early Givetian subduction- KN Kan (cratonal) (Archean and Early (Proterozoic) na TL tv Late Paleozoic (Devonian to Permian) related volcanic rocks (Early and Middle Proterozoic) WS West Sayan (continental margin turbidites) RA ul Czs is WS tv Devonian ) KR Kurai (island arc) (Vendian and Early (Cambrian to Silurian) TK ACH SN khs Czs SZ ET Vendian and Early Paleozoic (Vendian TO td Taidon molasse basin (Late Cambrian and Cambrian) ZS Zasurin (oceanic) (Late Cambrian and Early TK na KT to Silurian) CHU Czs Early Ordovician) KRT Kurtushiba (accretionary wedge, Ordovician) KR NS TO am BR khs Uvs-Nuur tv Tuva molasse basin with Lochkovian- predominantly oceanic rocks) (Vendian and SG MB AG Czs Riphean to Silurian for craton KTN SS Pragian rift-related volcanic rocks (Devonian Early Cambrian) REFERENCES Czs am and Early Carboniferous KS Kuznetsk-East Sayan (back-arc terranes AM am AM am KHO SYMBOLS ul Uimen-Lebed volcano-sedimentary belt with collage) (Vendian to Middle Cambrian) This map is compiled from the following references. Eifelian and Early Givetian subduction- KT Khemchik-Tapsa (accretionary wedge, sa am Depositional contact along margin of overlap related volcanic rocks (Early and Middle predominantly oceanic rocks) (Vendian and Berzin, N.A., Coleman, R.G., Dobretsov, N.L., assemblage.Accretionary fault between terranes Devonian) Early Cambrian) Zonenshain,L.P., Xiao, Xuchang, and Chang, where not reactivated along post-accretionary KTN Kaitanak (accretionary wedge, predominantly E.Z., 1994, Geodynamic map of the western part fault or where not partly covered by overlap ABBREVIATIONS FOR CRATON AND oceanic rocks) (Vendian and Early Cambrian) of the Paleoasian Ocean. Geology and assemblage. TECTONOSTRATIGRAPHIC TERRANES KV Kuvai (accretionary wedge undivided) (Late Geophysics, v. 35, p. 5-22. (interpreted tectonic environment in Proterozoic) Berzin, N.A., and Dobretsov, N.L., 1994, Geodynamic o Post-accretion major fault; sense of displacement parantheses) KZ Kozhukhov (island arc) (Vendian to Middle evolution of Southern Siberia in late Precambrian- 48 unknown. Dashed where approximately located. Cambrian) early Paleozoic time,in Coleman, R.G., ed., ACH Anui-Chuya (continental margin turbidites) MB Mogen-Buren (oceanic) (Vendian and Early Reconstruction of the Paleo-Asian Ocean: Post-accretion thrust fault, sawteeth on upper (Cambrian to Silurian) Cambrian) Proceedings of the 29th International Geological plate. Dashed where approximately located. AG Agardag (oceanic) (Vendian and Early MR Maralikha (accretionary wedge, Congress, Part B, Utrecht, Netherlands, p. 53-70. SCALE Cambrian) predominantly turbidites)(Devonian?) Berzin, N.A., and Kungurtsev, L.V., 1996, Geodynamic 0 500 KM Digital cartography by Larisa V. Smirnova, Post-accretion strike-slip fault, arrows denote AI Amil (accretionary wedge, predominantly NRS North Sayan (island arc) (Vendian to Middle interpretation of Altai-Sayan Geological Annia O. Avchenko,and Warren J. Nokleberg relative strike-slip displacement. Dashed where turbidites) (Vendian and Early Cambrian) Cambrian) complexes: Geology and Geophysics, v. 37, no. 1, approximately located; dotted where concealed. AL Alambai (accretionary wedge, predominantly NS North Sangilen (passive continental margin) p. 56-73. oceanic rocks) (Vendian and Early Cambrian) (Late Proterozoic) Chang, E.Z., Coleman, R.G., and Ying D.X., 1995, NSC North Asian Craton (Archean and Early Tectonic transect map across Russia-Mongolia- AM Altai-Mongolia (continental margin turbidites) Proterozoic) China (western part): Stanford University and (Cambrian to Silurian) ON Ondum (island arc) (Vendian and Early U.S. Geological Survey, scale 1:2,500,000. AN Angurep (metamorphic) Cambrian) AO Agoi (metamorphic) (OT) Onot block (cratonal basement) (Late (BI) Biryusa block (cratonal basement) (Archean Archean and Early Proterozoic) PRELIMINARY TERRANE AND OVERLAP ASSEMBLAGE MAP OF ALTAY- SAYAN REGION, SOUTHERN SIBERIA, RUSSIA By Nikolay A. Berzin, Russian Academy of Sciences, Novosibirsk.
Recommended publications
  • Kinematic Reconstruction of the Caribbean Region Since the Early Jurassic
    Earth-Science Reviews 138 (2014) 102–136 Contents lists available at ScienceDirect Earth-Science Reviews journal homepage: www.elsevier.com/locate/earscirev Kinematic reconstruction of the Caribbean region since the Early Jurassic Lydian M. Boschman a,⁎, Douwe J.J. van Hinsbergen a, Trond H. Torsvik b,c,d, Wim Spakman a,b, James L. Pindell e,f a Department of Earth Sciences, Utrecht University, Budapestlaan 4, 3584 CD Utrecht, The Netherlands b Center for Earth Evolution and Dynamics (CEED), University of Oslo, Sem Sælands vei 24, NO-0316 Oslo, Norway c Center for Geodynamics, Geological Survey of Norway (NGU), Leiv Eirikssons vei 39, 7491 Trondheim, Norway d School of Geosciences, University of the Witwatersrand, WITS 2050 Johannesburg, South Africa e Tectonic Analysis Ltd., Chestnut House, Duncton, West Sussex, GU28 OLH, England, UK f School of Earth and Ocean Sciences, Cardiff University, Park Place, Cardiff CF10 3YE, UK article info abstract Article history: The Caribbean oceanic crust was formed west of the North and South American continents, probably from Late Received 4 December 2013 Jurassic through Early Cretaceous time. Its subsequent evolution has resulted from a complex tectonic history Accepted 9 August 2014 governed by the interplay of the North American, South American and (Paleo-)Pacific plates. During its entire Available online 23 August 2014 tectonic evolution, the Caribbean plate was largely surrounded by subduction and transform boundaries, and the oceanic crust has been overlain by the Caribbean Large Igneous Province (CLIP) since ~90 Ma. The consequent Keywords: absence of passive margins and measurable marine magnetic anomalies hampers a quantitative integration into GPlates Apparent Polar Wander Path the global circuit of plate motions.
    [Show full text]
  • Developing the Orogenic Gold Deposit Model: Insights from R&D for Exploration Success
    "Accretionary Wedge Geodynamic Evolution, Metamorphic Equilibria, Metasomatic Processes, & GOLD” by Dave Lentz (UNB) Accretionary ophiolitic sequence (with quartz veins), basement Santorini, Greece 2m Orogenic Gold first used by Bohlke (1982) Developing the Orogenic Gold Deposit Model: Insights from R&D for Exploration Success by Dave Lentz (UNB) Accretionary ophiolitic sequence (with quartz veins), basement Santorini, Greece 2m Orogenic Gold first used by Bohlke (1982) SPONSORS INTRODUCTION PART I: Review Gold Deposit Settings • Historical Evolution of ideas • Description of Orogenic Au Systems • Enigmatic aspects of the metamorphogenic model PART II: Geothermal to Hydrothermal Evolution • Metamorphic Considerations to Thermal Evolution • Fluid Source (and Solubility Implications) PART III: Geodynamic Evolution • Accretionary Geodynamics (to collision) • Structural-Metamorphic Evolution & Settings • Implications for refining the metamorphogenic Orogenic Gold Model PART I: Review Gold Deposit Settings Mineralization in forearc to back arc system Accretionary Wedge fore arc settings Mitchell & Garson (1982) OROGENIC GOLD: Magmatic to Metamorphic hydrothermal continuum Groves et al. (1998) How are Gold Systems Related to Crustal Growth? From Goldfarb (2006) Magmatic-dominated Metamorphic-dominated Groves et al. (1998) Metamorphic,Metamorphic, Transitional,Transitional, andand MagmaticMagmatic GoldGold ModelsModels Poulsen (2000) Metamorphic dominated Setting Juneau Belt Prehnite- Donlin Creek pumpellite Ross Mine Kirkland Lake Dome Brittle Sigma/Giant-Con Greenschist Hollinger-McIntyre Ductile-Brittle Amphibolite Red Lake Eastmain/Lynn Lake Musselwhite Granulite Ductile Lake Lilois Fluid Egress along Advective Crustal-scale Heat n Shear Zone o i t Transfer a n o Z l a t e Zone of deposition M Low salinities (< 3 wt % NaCl, KCl, etc.) Source Region (or deeper) Fyfe & Henley (1973) RETROGRESSION PART II: Geothermal to Hydrothermal Evolution Fluid movement Ethridge et al.
    [Show full text]
  • Analog Experiments and Mechanical Analysis Applied to the Alaskan Accretionary Wedge Marc-André Gutscher, Nina Kukowski, Jacques Malavieille, Serge Lallemand
    Analog experiments and mechanical analysis applied to the Alaskan Accretionary Wedge Marc-André Gutscher, Nina Kukowski, Jacques Malavieille, Serge Lallemand To cite this version: Marc-André Gutscher, Nina Kukowski, Jacques Malavieille, Serge Lallemand. Analog experiments and mechanical analysis applied to the Alaskan Accretionary Wedge. Journal of Geophysical Research, American Geophysical Union, 1998, 103 (B5), pp.10161-10176. hal-01261538 HAL Id: hal-01261538 https://hal.archives-ouvertes.fr/hal-01261538 Submitted on 26 Jan 2016 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. JOURNAL OF GEOPHYSICAL RESEARCH, VOL. 103, NO. B5, PAGES 10,161-10,176,MAY 10, 1998 Episodic imbricate thrusting and underthrusting' Analogexperiments and mechanicalanalysis applied to the Alaskan Accretionary Wedge Marc-Andrd Gu•scher • and Nina Kukowski GEOMAR, Kiel, Germany JacquesMalavieille and SergeLallemand Laboratoire de G•ophysique et Tectonique, Universit• de Montpellier II, Montpellier, France Abstract. Seismic reflection profiles from the sediment rich Alaska subduction zone image short, frontally accreted, imbricate thrust slices and repeated se- quencesof long, underthrust sheets. Rapid landward increasesin wedgethickness, backthrusting,and uplift of the forearc are observed,suggesting underthrusting beneaththe wedge.These features and a widely varyingfrontal wedgemorphology are interpreted to be caused by different modes of accretion active concurrently along the trench at different locations.
    [Show full text]
  • Active Structures in the Barbados Accretionary Wedge of the Lesser Antilles Subduction: Implications for Slip Partitioning
    EGU2020-10732 https://doi.org/10.5194/egusphere-egu2020-10732 EGU General Assembly 2020 © Author(s) 2021. This work is distributed under the Creative Commons Attribution 4.0 License. Main active structures in the Barbados accretionary wedge of the Lesser Antilles Subduction: implications for slip partitioning Gaëlle Bénâtre1, Nathalie Feuillet1, Hélène Carton1, Eric Jacques1, and Thibaud Pichot2 1Université de Paris, Institut de Physique du Globe de Paris, CNRS UMR7154, Paris, F-75005, France ([email protected]) 2Beicip-Franlab, Rueil-Malmaison, France At the Lesser Antilles Subduction Zone (LASZ), the American plates subduct under the Caribbean plate at a slow rate of ~2 cm/yr. No major subduction megathrust earthquakes have occurred in the area since the 1839 and 1843 historical events, and the LASZ is typically considered weakly coupled. At the front of the LASZ, the Barbados accretionary wedge (BAW) is one of the largest accretionary wedges in the world. The width of the BAW decreases northward, owing to the increasing distance to the sediment source (Orinoco river) and the presence of several aseismic oceanic ridges, in particular the Tiburon ridge, that stops sediment progression. Marine geophysical studies conducted to date over the northern part of the BAW (Guadeloupe-Martinique sector) have mostly focused on resolving the geometry of the backstop. However, the structure of the wedge and the mechanical behavior of the subduction interface remain poorly known. Our study aims to describe the geometry of the BAW by a detailed morpho-tectonic analysis in order to place constraints on present and past dynamic interactions between the subducting and overriding plates.
    [Show full text]
  • Coulomb Stress Evolution in Northeastern Caribbean Over the Past 250 Years Due to Coseismic, Postseismic and Interseismic Deformation
    Geophys. J. Int. (2008) 174, 904–918 doi: 10.1111/j.1365-246X.2008.03634.x Coulomb stress evolution in Northeastern Caribbean over the past 250 years due to coseismic, postseismic and interseismic deformation Syed Tabrez Ali,1 Andrew M. Freed,1 Eric Calais,1 David M. Manaker1,∗ and William R. McCann2 1Department of Earth and Atmospheric Sciences, Purdue University, 550 Stadium Mall Dr, West Lafayette, IN 47907, USA. E-mail: [email protected] 2Earth Scientific Consultants, 10210 West 102nd Ave, Westminster, CO 80021,USA Accepted 2007 September 24. Received 2007 September 19; in original form 2007 July 21 SUMMARY The Northeastern Caribbean region accommodates ∼20 mm yr−1 of oblique convergence be- tween the North American and Caribbean plates, which is distributed between the subduction interface and major strike-slip faults within the overriding plate. As a result, this heavily populated region has experienced eleven large (M ≥ 7.0) earthquakes over the past 250 yr. In an effort to improve our understanding of the location and timing of these earthquakes, with an eye to understand where current seismic hazards may be greatest, we calculate the evolution of Coulomb stress on the major faults since 1751 due to coseismic, postseismic, and interseismic deformation. Our results quantify how earthquakes serve to relieve stress accumulated due to interseismic loading and how fault systems communicate with each other, serving both to advance or retard subsequent events. We find that the observed progressive westwards propagation of earthquakes on the Septentrional and Enriquillo strike-slip faults and along the megathrust was encouraged by coseismic stress changes associated with prior earthquakes.
    [Show full text]
  • 8. Growth of Accretionary Wedges Off Vancouver Island and Oregon1
    Westbrook, G.K., Carson, B., Musgrave, R.J., et al., 1994 Proceedings of the Ocean Drilling Program, Initial Reports, Vol. 146 (Part 1) 8. GROWTH OF ACCRETIONARY WEDGES OFF VANCOUVER ISLAND AND OREGON1 G.K. Westbrook2 ABSTRACT A simple formulation for the growth of a wedge of constant taper accreting a sediment layer of given thickness and exponential decrease of porosity with depth was used to estimate the rates of growth of the accretionary wedges off Vancouver Island and Oregon. Application to the section off Vancouver Island indicates that the accreted sediments penetrated at Site 889 were added to the toe of the wedge between 0.8 and 1.1 Ma. Application to the Oregon section shows that the thickness of the accreted layer before 0.3 Ma must have been substantially less than the present 1.5 km for Pliocene sediments at Site 892. For both wedges the accretion of a thick layer of sediment from the Cascadia Basin appears to have occurred over only the past few hundred thousand years, and no more than about a million years. Since the Eocene, the equivalent average thickness of the layer of sediment that has been accreted is about 0.5 km. INTRODUCTION For an interpretation of the results of drilling into the accretionary wedge, it is useful to be able to estimate when a sequence penetrated by a borehole in the accretionary wedge was actually accreted. The time taken to build the accretionary wedge is an important parameter in the analysis of the geologic evolution of the continental margin. To provide a straightforward means of making a first-order estimate of these parameters, a simple model of a wedge that accretes a layer of sediment with a given thickness and porosity/depth function has been developed.
    [Show full text]
  • Geodynamics of Wedges
    1 DRIVING MECHANISMS OF THRUST SYSTEMS Dynamics of accretionary, orogenic wedges Tens of kilometres long displacements are reported for only a few thousands meters thick thrust sheets. With accepted values of frictional resistance, stresses necessary to push a thrust sheet on a horizontal or slightly up-inclined basal thrust exceed the failure strength of intact rocks. Accordingly, hinterlands should deform and crush before fronts of thrust sheets would move. This mechanical paradox has triggered formulation of a few working hypotheses. The question is still not fully resolved, possibly because all envisioned mechanisms are involved on a scale-dependent importance. Concepts and definitions Thrust systems are common in converging settings, resulting from compressional deformation of rocks once the shear strength along weak layers or planes is exceeded. In convergent plate boundaries, thrusts cutting through accretionary wedges are virtually splays of the subduction plane. This mechanism, where the accretionary hanging wall is deformed while the subducting footwall plate descends undeformed, is typical of thin-skinned tectonics depicted in mountain systems. Therefore, mechanics developed from accretionary wedges are often applied to foreland fold-and-thrust belts and even to orogenic belts (see lecture on thrust systems). Geometry A thrust sheet (or nappe; distinguish from fold nappe = large recumbent fold) is an allochthonous unit that has been transported and lies almost horizontally, away from its original position, on an autochthonous substratum. The bottom boundary is an originally shallow-dipping thrust fault or shear zone along which most of the displacement has taken place. The frontal part in the direction of movement is the leading edge.
    [Show full text]
  • Techniques for Understanding Fold-And-Thrust Belt Kinematics and Thermal Evolution
    The Geological Society of America Memoir 213 Techniques for understanding fold-and-thrust belt kinematics and thermal evolution Nadine McQuarrie Department of Geology and Environmental Science, University of Pittsburgh, Pittsburgh, Pennsylvania 15260, USA Todd A. Ehlers Department of Geoscience, University of Tübingen, Tübingen 72074, Germany ABSTRACT Fold-and-thrust belts and their adjacent foreland basins provide a wealth of information about crustal shortening and mountain-building processes in conver- gent orogens. Erosion of the hanging walls of these structures is often thought to be synchronous with deformation and results in the exhumation and cooling of rocks exposed at the surface. Applications of low-temperature thermochronology and bal- anced cross sections in fold-and-thrust belts have linked the record of rock cooling with the timing of deformation and exhumation. The goal of these applications is to quantify the kinematic and thermal history of fold-and-thrust belts. In this review, we discuss different styles of deformation preserved in fold-and-thrust belts, and the ways in which these structural differences result in different rock cooling histories as rocks are exhumed to the surface. Our emphasis is on the way in which different numerical modeling approaches can be combined with low-temperature thermochro- nometry and balanced cross sections to resolve questions surrounding the age, rate, geometry, and kinematics of orogenesis. INTRODUCTION for fold-and-thrust belt formation is an extensive preexisting sedimentary basin of platformal to passive-margin strata (Fig. 1). Folding and thrust faulting are the primary mechanisms for The mechanical anisotropy of stratigraphic layering exerts a fi rst- the shortening and thickening of continental crust and thus are order control on the style and magnitude of shortening (Price, common geologic features of convergent margins.
    [Show full text]
  • 15. Genesis and Evolution of Small-Scale Structures in the Toe of the Barbados Ridge Accretionary Wedge1
    Moore, J. C, Mascle, A., et al., 1990 Proceedings of the Ocean Drilling Program, Scientific Results, Vol. 110 15. GENESIS AND EVOLUTION OF SMALL-SCALE STRUCTURES IN THE TOE OF THE BARBADOS RIDGE ACCRETIONARY WEDGE1 K. M. Brown2 and J. Behrmann3 ABSTRACT Cores from Leg 110 document the development of small-scale structures generated both during the initial propaga• tion of the basal decollement zone into the abyssal plane section and the subsequent thickening of the wedge. At the macroscopic accretionary front, sub-horizontal compressive stresses become localized in the off-scraped section rather than in the underthrust sediments. In contrast, strata associated with the basal decollement zone may experience layer parallel extension resulting from a combination of simple shear and possible flattening strains (with the latter being the possible consequence of increased tectonic loading due to the thickening of the overlying wedge). The zone of intense scaly fabrics associated with the basal decollement and other thrusts appears to thicken with increasing displacement. This thickening, together with increasing numbers of thrusts (of both an in-sequence and out-of-sequence nature), may account for why 50% of the volume of the wedge is affected by scaly fabrics of Site 674, 18 km back from the accretion• ary front. General bedding and thrust dips increase back in the wedge, most probably in response to both folding and back rotation of imbricate thrusts. Intense stratal disruption, Syntectonic carbonate veins, occasional isoclinal folds (with axial planar fabrics), and web structures are all developed by 18 km from the accretionary front. At this point, the sediments still have porosities in excess of 40%, and the small-scale structures are found at present depths of less than 400 mbsf.
    [Show full text]
  • Thrust-Wrench Interference Tectonics in the Gulf of Cadiz
    Thrust-wrench interference tectonics in the Gulf of Cadiz (Africa-Iberia plate boundary in the North-East Atlantic): Insights from analog models João Duarte, Filipe Rosas, Pedro Terrinha, Marc-André Gutscher, Jacques Malavielle, Sonia Silva, Luis Matias To cite this version: João Duarte, Filipe Rosas, Pedro Terrinha, Marc-André Gutscher, Jacques Malavielle, et al.. Thrust- wrench interference tectonics in the Gulf of Cadiz (Africa-Iberia plate boundary in the North-East Atlantic): Insights from analog models. Marine Geology, Elsevier, 2011, 289 (1-4), pp.135-149. 10.1016/j.margeo.2011.09.014. insu-00643630 HAL Id: insu-00643630 https://hal-insu.archives-ouvertes.fr/insu-00643630 Submitted on 24 Nov 2011 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. Thrust - wrench interference tectonics in the Gulf of Cadiz (Africa - Iberia plate boundary in the North-East Atlantic): insights from analog models João C. Duarte a, b, c, Filipe M. Rosas a, b, Pedro Terrinha b, c, Marc-André Gutscher d, Jacques Malavieille e, Sónia Silva a, b, c, Luis Matias f a Instituto Dom Luiz, Campo Grande, Ed. C1, Piso 2, 1749-016 Lisboa, Portugal b Universidade de Lisboa, Faculdade de Ciências, Departamento de Geologia, Campo Grande, Ed.
    [Show full text]
  • Along-Arc Segmentation and Interaction of Subducting Ridges with the Lesser Antilles Subduction Forearc Crust Revealed by MCS Imaging M
    Along-arc segmentation and interaction of subducting ridges with the Lesser Antilles Subduction forearc crust revealed by MCS imaging M. Laigle, A. Bécel, B. de Voogd, M. Sachpazi, G. Bayrakci, Jean-Frederic Lebrun, M. Evain To cite this version: M. Laigle, A. Bécel, B. de Voogd, M. Sachpazi, G. Bayrakci, et al.. Along-arc segmentation and interaction of subducting ridges with the Lesser Antilles Subduction forearc crust revealed by MCS imaging. Tectonophysics, Elsevier, 2013, 603, pp.32-54. 10.1016/j.tecto.2013.05.028. hal-00932801 HAL Id: hal-00932801 https://hal.archives-ouvertes.fr/hal-00932801 Submitted on 29 Mar 2021 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. Tectonophysics Archimer September 2013, Volume 603, Pages 32-54 http://archimer.ifremer.fr http://dx.doi.org/10.1016/j.tecto.2013.05.028 © 2013 Published by Elsevier B.V. Along-arc segmentation and interaction of subducting ridges with the is available on the publisher Web site Webpublisher the on available is Lesser Antilles Subduction forearc crust revealed by MCS imaging Mireille Laiglea, f, *, Anne Becela, b, Béatrice de Voogdc, Maria Sachpazid, Gaye Bayrakcia, Jean-Frédéric Lebrune, Mikael Evainf, the "Thales Was Right" Seismic Reflection working groupa, 1 authenticated version authenticated - a Institut de Physique du Globe de Paris, UMR 7154 CNRS, Sorbonne Paris Cité, Paris, France b CEREGE, Aix-en-Provence, France c Laboratoire Géophysique, Univ.
    [Show full text]
  • Mélanges and Mélange-Forming Processes: a Historical Overview
    International Geology Review Vol. 52, Nos. 10–12, October–December 2010, 1040–1105 TIGR0020-68141938-2839International GeologyMélanges Review,Review Vol. 1, No. 1, Jan 2010: pp. 0–0 and mélange-forming processes: a historical overview and new concepts InternationalA. Festa et al. Geology Review Andrea Festaa,c*, Gian Andrea Pinib, Yildirim Dilekc and Giulia Codegonea aDipartimento di Scienze della Terra, Università di Torino, Torino, Italy; bDipartimento di Scienze della Terra e Geologico-Ambientali, Università di Bologna, Bologna, Italy; cDepartment of Geology, Miami University, Oxford, OH, USA (Accepted 11 December 2009) Mélanges represent a significant component of collisional and accretionary orogenic belts and occur widely around the world. Since its first introduction and use, the term has evolved to cover both processes (tectonic, sedimentary, and diapiric) and tectonic settings of mélange formation. The meaning and significance of various terms refer- ring to the origin of ‘block-in-matrix chaotic rocks’ are still subject to debate. This study presents a historical overview of the evolving mélange concept and investigates the relationships between mélange types and their tectonic settings of formation. We investigate the contribution of mass-transport versus contractional deformation proc- esses at the onset of mélange formation and throughout the evolution of different mélange types, and the nature of the continuum and transition from broken formations to true tectonic mélanges. A mélange is a mappable chaotic body of mixed rocks with a block-in-matrix fabric whose internal structure and evolution are intimately linked to the structural, sedimentary, magmatic, and metamorphic processes attending its origin. On the basis of a comparative analysis of exhumed, ancient on-land mélanges and modern tectonic environments, where mélange-forming processes are at work, such units are classified into those related to extensional tectonics, passive margin evolu- tion, strike-slip tectonics, subduction zones, collisional tectonics, and intracontinental deformation.
    [Show full text]