DOCSLIB.ORG

Cretaceous- Paleocene)

Total Page：16

File Type：pdf, Size：1020Kb

Download full-text PDF Read full-text
Cretaceous- Paleocene) A beautiful nature-the Himalaya Upendra BARAL P.hD. Key Laboratory of Continental Collision and Plateau Uplift Institute of Tibetan Plateau Research, Chinese Academy of Sciences WHEN?? Where?? Indian plate Asian plate India-Eurasia initial collision India-Gondwana breakup and collision with Asia India drifting towards Eurasia separation of India from Antarctica– Australia along the Southeast Indian Ridge Initial breakup of Eastern Gondwana from Western Gondwana Importance of Collision study • India-Asia collision is most spectacular geological event that formed the vast and high Tibetan Plateau • This event affects Tibet as well as central and southeast Asia • The initial collision is importance for the study of continental lithospheric deformation, environmental changes, paleoaltitue reconstruction • The collision is ongoing process, initiated by “soft collision” and remained constant as “hard collision” that leads to the loading of an accretionary prism onto a passive continental margin and formed the foreland basin Important Proxies to constrain the collision age • Faunal/ Fauna migration • Study of Magmatic rocks (e.g., Eclogite) exposed within the suture zone • Provenance analysis (geochronology Magmatic records from the THS- during the early stage of collision • Linear exposure of granitic rocks in Himalayan belt: Olig-Miocene Leucogranite and Middle Eocene granites • Eocene granites were derived from partial melting of the thickened lower crust- • Earliest stage of magmatism formed during the collision and subduction of Neo-Tethyan slab break-off • The Neo-Tethyan slab break-off was almost synchronous along the entire IYSZ during middle Eocene (ca. 45 Ma) Research progress regarding the India-Asia collision age • Tectono-sedimentary responses to the Initial collision • Deformation of the northern THS in the early collision stage • Island arc formation, and accretionary complex and trench strata emplaced on the northern margin of Indian plate. • Increase the flexure load and formation of the first peripheral foreland basin • Development of a peripheral foreland basin system • Formation is related to the collision • Argument that Miocene is the first basin formed due to collision while in Tibet Ding and team marked the basin closer to IYSZ developed between 65 Ma and 60 Ma • Cessation of marine sedimentation • Transition from marine to terrestrial facies ( an indicator of India-Asia collision in late 19s) • E.g., Balakot Fm ( 55 Ma and 50 Ma) is the oldest terrestrial foreland basin deposit • In Tibet, this transition is recorded in the early Eocnene The deposition of marine sediments would not have ended immediately after the onset of collision, the age of these strata only reflects an upper bound of the collision time, limiting the application of this approach • Paleolatitudes of Greater Indian (GI) and the TH Sangdalin Formation (Southern Tibet) The Sangdalin Formation (Paleocene-early Eocene), contains typical foredeep deposit and in Saga area the environmental change took place between 65 Ma and 63 Ma which suggest the collision age ca. 65 Ma ( Ding et al 2005) or ca. 60 Ma (Wu et al 2014). Paleolatitudes of Greater Indian (GI) and the TH • GI is the region to the north of the Indian plate, including under-thrusted Indian lithosphere and crustal shortening in the Himalaya mountain belt • The paleomagnetic study in Tibet have shown the age of Zhongshan Formation as 71 Ma and 65 Ma and Zhongpu Fm between 63 Ma and 55 Ma. • Recent development is that the Cretaceous paleomagnetic results from the Lhasa and TH block indicated the existence of ca.2675 km GIB between THS and Indian Craton. Paleolatitude of southern margin of Asia • Numerous paleomagnetic study in Cretaceous to Eocene lavas and sedimentary strata from the Lhasa block and have shown a large variation in collision age between 65 Ma and 43 Ma. • This variation is due to the compacted sediments, the incomplete field characterization of lavas, re- magnetized rocks and improper statistical methods • The Lhasa block was located at between ca. 16°N and 22°N during Cretaceous to Paleogene (Lippert et al 2014) and the collision age is 52 Ma ( youngest age) • Most recent geochronology and paleomagnetic study from upper Cretaceous volcanic rocks in western Lhasa have shown the southern margin of Asia probably had a quasi-linear orientation trending ~310° prior to collision and the collision was between 65 Ma and 60 Ma (Yi et al 2011) Comparison of different timings for the collision between India and Asia as well as events across the THS resulting from the application of different methods Time and Location of Contact between Indian and Eurasian Plates Initial contact between Indian and Asian plates The initial contact between Indian and Asian plate took in Northwestern section (e.g. Beck et al., 1995) In a central part of the IYSZ between ca. 65 Ma and 63 Ma and then spread both eastward and westward (e.g. Bin Zhu et al., 2005; Cai et al., 2011; Ding et al., 2005) Controversy regarding the India-Eurasia collision ~51 Ma (Bin Zhu et al., 2005; Bouilhol et al., 2013; Ding et al., 2005) ~65 Ma and 60 Ma (DeCelles et al., 2014; Ding et al., 2005; Wu et al., 2014) ~65 Ma and 62 Ma (Ding et al., 2017) - Central Himalaya ~55-56 Ma (Ding et al., 2016) –Western Himalaya ~30-25 Ma (Aitchison et al., 2007; Aitchison et al., 2000; Aitchison and Davis, 2001). THE HIMALAYAS and FORELAND BASINS • Sub Himalaya- Siwalik • Coarsening upward ~5 km thick fluvial sediments • Differentiated into Lower, Middle and Upper • Middle Miocene to Early Pleistocene. • Lesser Himalaya • Metasedimentary sequences and associated younger sedimentary rocks with overriding crystalline nappes and klippen • Lower Lesser Himalaya (Proterozoic) / Upper Lesser Himalaya (Paleozoic-Cenozoic) • Higher Himalaya • High-grade crystalline rocks including (gneisses, schists and migmatites). • This zone is tectonically still active due to the activity of MCT. • Granitic intrusions in several places /with high grade rocks • Tethys Himalaya • Comprises Fossiliferous sedimentary • Cambrian to Lower Cretaceous DETRITAL ZIRCON AGES FOR HIMALAYAN UNITS • Lower Lesser Himalaya: 1.7-2.0 Ga and 2.4-2.8 Ga • Higher Himalaya: 800-1200 Ma, 1.6-1.9 Ga and 540-750 Ma • Tethys and Lower Lesser Himalaya : 480–570 Ma, 750– 1200 Ma, and • 2430–2560 Ma. (Gehrels et al., 2011 and references therein) Provenance Analysis SOURCE TRANSPORT/BARRIER BASIN 22 Ma Alluvial Alluvial 23 Ma Depositional Gap 42 Ma Marine (DeCelles et al., 2004) Cretaceous-Early Miocene Strata • Dumri Formation ( Miocene) • Alternating beds of greenish grey to reddish brown, fine- to medium –grained sandstones and mudstone intercalated with marl bands is type lithology. • Bhainskati Formation ( Eocene) • About 150 m thick shallow marine to brackish water deposits. Limestone with some lenses of fossiliferous limestone intercalated with red- purple pencil cleavage shale. • Amile Formation ( Cretaceous- Paleocene) • 230 m thick at the type locality. Green to grey colored calcareous sandstone with some shale. Limestone beds yield several types of marine fossils (DeCelles et al., 2004) Cretaceous-Early Miocene Strata (Baral et al., 2018) Cretaceous-Early Miocene Strata • Dumri Formation (Miocene) the ƐHf (t) value from DZ grains of 1600-1800 Ma age are prominently negative indicate the change of source region. • In Bhainskati Formation (Eocene) and Dumri Formation (Miocene) the DZ grains have both positive and negative ƐHf (t) values suggest the orogenic source. • Dominant positive ƐHf (t) values in Amile Formation Indicate that the source is Juvenile crust. (Baral et al., 2019) Neogene Foreland Basin (Siwalik) Thick Bedded, well sorted clast supported conglomerate Thick-beeded medium to coarse grained sandstone “ Salt and pepper” texture” Variegated mudstone with fine grained sandstone and siltstone (DeCelles et al., 2004) (Baral et al., 2017) Neogene Foreland Basin (Siwalik) Thick Bedded, well sorted clast supported conglomerate Absence of these Cenozoic zircons in western Nepal, and presence in eastern Nepal foreland basin, implies that the leucogranite in the eastern Himalaya were much more Thick-beeded medium to eroded rather than in western Himalaya. coarse grained sandstone “ Salt and pepper” texture” The Cenozoic grains in the eastern Nepal shows the possibility of the source from the Gangdese arc However, since ~10 Ma ago the input of the Lesser Himalayan sediments was relatively higher in the Siwalik Group. Variegated mudstone with fine grained sandstone and siltstone (Baral et al., 2015a, b, 2017a, b) Eastern Himalayan Cenozoic Foreland Basin Paleocene-Eocene Yinkiong Group of rocks associated with the Abor Volcanics Lower Yinkiong Formation: Late Paleocene to Early Eocene Geku Formation, deposited in a distal foredeep foreland basin system in the northern Indian passive margin. Upper Yinkiong Formation: Early to Mid-Eocene (Dalbuing Formation) deposited in a foredeep depozone foreland basin system. Eastern Himalayan Cenozoic Foreland Basin • Absence of Younger detritus Early to Mid Eocene Strata (Upper Yinkiong Formation) • Younger detritus (mid to upper Cretaceous) were probably source from the Asian affinity • Mid cretaceous granitic body are wide spread in Tethyan Himalaya India-Asia collision in Siang valley NE India, took place during or before early Eocene. Baral et al., 2018 Western Himalayan Cenozoic Foreland Basin Murree Fm– Sub Himalayan foreland basin, cyclic sequence of shale, and mudstone with some siltstone and sandstone Early Miocene Kuldana
Load more

Recommended publications
  • Flexural Modeling of the Himalayan Foreland Basin: Implications for the Presence of a Forebulge and Formation of Basement Ridges
    FLEXURAL MODELING OF THE HIMALAYAN FORELAND BASIN: IMPLICATIONS FOR THE PRESENCE OF A FOREBULGE AND FORMATION OF BASEMENT RIDGES __________________________________ An Abstract of a Thesis Presented to the Faculty of the Department of Earth and Atmospheric Sciences University of Houston __________________________________ In Partial Fulfillment of the Requirements for the Degree Master of Science __________________________________ By Nicole F. Arres August 2013 FLEXURAL MODELING OF THE HIMALAYAN FORELAND BASIN: IMPLICATIONS FOR THE PRESENCE OF A FOREBULGE AND FORMATION OF BASEMENT RIDGES ____________________________________________________ Nicole F. Arres APPROVED: ____________________________________________________ Dr. Jolante van Wijk, Advisor ____________________________________________________ Dr. Michael Murphy ____________________________________________________ Dr. Peter Copeland ____________________________________________________ Dr. An Yin University of California at Los Angeles ____________________________________________________ Dean, College of Natural Sciences and Mathematics ii FLEXURAL MODELING OF THE HIMALAYAN FORELAND BASIN: IMPLICATIONS FOR THE PRESENCE OF A FOREBULGE AND FORMATION OF BASEMENT RIDGES __________________________________ An Abstract of a Thesis Presented to the Faculty of the Department of Earth and Atmospheric Sciences University of Houston __________________________________ In Partial Fulfillment of the Requirements for the Degree Master of Science __________________________________ By Nicole F. Arres
    [Show full text]
  • Himalaya - Southern-Tibet: the Typical Continent-Continent Collision Orogen
    237 Himalaya - Southern-Tibet: the typical continent-continent collision orogen When an oceanic plate is subducted beneath a continental lithosphere, an Andean mountain range develops on the edge of the continent. If the subducting plate also contains some continental lithosphere, plate convergence eventually brings both continents into juxtaposition. While the oceanic lithosphere is relatively dense and sinks into the asthenosphere, the greater sialic content of the continental lithosphere ascribes positive buoyancy in the asthenosphere, which hinders the continental lithosphere to be subducted any great distance. Consequently, a continental lithosphere arriving at a trench will confront the overriding continent. Rapid relative convergence is halted and crustal shortening forms a collision mountain range. The plane marking the locus of collision is a suture, which usually preserves slivers of the oceanic lithosphere that formerly separated the continents, known as ophiolites. The collision between the Indian subcontinent and what is now Tibet began in the Eocene. It involved and still involves north-south convergence throughout southern Tibet and the Himalayas. This youthful mountain area is the type example for studies of continental collision processes. The Himalayas Location The Himalayas form a nearly 3000 km long, 250-350 km wide range between India to the south and the huge Tibetan plateau, with a mean elevation of 5000 m, to the north. The Himalayan mountain belt has a relatively simple, arcuate, and cylindrical geometry over most of its length and terminates at both ends in nearly transverse syntaxes, i.e. areas where orogenic structures turn sharply about a vertical axis. Both syntaxes are named after the main peaks that tower above them, the Namche Barwa (7756 m) to the east and the Nanga Parbat (8138 m) to the west, in Pakistan.
    [Show full text]
  • Early Himalayan Exhumation: Isotopic Constraints from the Indian Foreland
    Paper 268 Disc Early Himalayan exhumation: Isotopic constraints from the Indian foreland basin Yani Najman{,{, Mike Bickle*,{ and Hazel Chapman{ {Department of Earth Sciences, Cambridge University, Downing St., Cambridge CB2 3EQ, UK, {Department of Geology & Geophysics, Edinburgh University, West Mains Road, Edinburgh EH9 3JW, UK ABSTRACT Nd- and Sr-isotopic compositions of Palaeogene foreland basin at least this time until the present day. The transition is sediments are used to provide insights into early Himalayan interpreted to reflect exhumation of `basement rocks' of the evolution,particularly the timing of exposure of high 87Sr/86Sr Indian plate,when the High Himalaya became a sufficient units,erosion of which may have caused the late Tertiary increase topographic barrier to separate suture zone rocks from the in oceanic Sr-isotopic ratios. During the late Palaeocene±early foreland basin. The marked rise in seawater 87Sr/86Sr from 40 Ma Eocene,erosion was from mixed sources including suture zone is consistent with the erosion of a Himalayan source with a high rocks. Exhumation of the High Himalaya was occurring by the 87Sr/86Sr ratio. time of deposition of alluvial sediments after mid-Oligocene times and this source has dominated Himalayan sediments from Terra Nova, 12, 28±34, 2000 chain from six main tectonic units (Fig. cambrian to early Permian and mainly Introduction 1) (listed from north to south below). shelf carbonate in the late Permian to The Himalayas are the prime example 1 The Trans-Himalayan zone,the An- early Eocene,unconformably overlain of an active collisional orogen. Their dean-type northern margin of Tethys by the Chulung La collisional deposits kinematics form the basis of our under- formed by Cretaceous to Eocene calc- (Critelli and Garzanti,1994; Searle et standing of crustal deformation pro- alkaline plutons intruding the Eurasian al.,1997a).
    [Show full text]
  • Najman ESR 2006.Pdf
    Earth-Science Reviews 74 (2006) 1–72 www.elsevier.com/locate/earscirev The detrital record of orogenesis: A review of approaches and techniques used in the Himalayan sedimentary basins Yani Najman Department of Environmental Science, Lancaster University, Lancaster LA1 4YQ, UK Received 20 March 2003; accepted 4 April 2005 Abstract The sediment archive, of material eroded from an active tectonic region and stored in adjacent basins, can provide a valuable record of hinterland tectonism especially when information in the source region itself is obscured by later metamorphism or removed by tectonism or erosion. Using the sediment record to document tectonism is a well established approach, but more recently there has been a burgeoning of the number of isotopic techniques which can be applied to detrital material, in particular single-grain analyses. Thus the scope for application of detrital studies to a number of different tectonic problems has widened considerably. In this review, the example of sediments eroded from the Himalayan orogen and preserved in the suture zone basin, foreland basin, remnant ocean basins and deep sea fans is used to illustrate the approach. Techniques as diverse as petrography, heavy mineral, XRF and Sr–Nd studies; single grain dating by Ar–Ar, U–Pb and fission track methodologies; and single grain Sm–Nd and Pb isotopic analyses, are described. The paper documents how the sediment record can be used to determine the thermal and tectonic evolution of the orogen, constrain mechanisms of continental deformation, exhumation rates and palaeodrainage. D 2005 Elsevier B.V. All rights reserved. Keywords: detrital sediment record; provenance techniques; Himalaya; orogenesis; exhumation; erosion 1.
    [Show full text]
  • Dynamic Fluvial Systems and Gravel Progradation in the Himalayan Foreland
    Dynamic fluvial systems and gravel progradation in the Himalayan foreland Nicholas Brozovic´* Department of Earth Sciences, University of Southern California, Los Angeles, California 90089 Douglas W. Burbank†} ABSTRACT Keywords: fold-and-thrust belt, basin analysis, posits are generally marked by a paucity of fossil Siwaliks, Himalaya, magnetostratigraphy. material of known age, making biostratigraphy Although the large-scale stratigraphy of difficult. In such areas without fossils or radio- many terrestrial foreland basins is punctu- INTRODUCTION metrically dateable volcanic rocks, magnetostra- ated by major episodes of gravel prograda- tigraphy can sometimes provide excellent temporal tion, the relationships of such facies to hinter- The evolution of terrestrial foreland basins is control if sufficiently long, continuous strati- land tectonism and climate change are often marked by the reorganization of fluvial systems on graphic sections can be studied (Burbank, 1996). unclear. Structural reentrants provide win- spatial scales of kilometers to thousands of kilo- dows into older and more proximal parts of meters at temporal scales ranging from coseismic GEOLOGIC FRAMEWORK OF THE the foreland than are usually exposed, and to millennia (e.g., Meghraoui et al., 1988; Bur- HIMALAYAN FORELAND thus provide key insights to earlier phases of bank, 1992; Talling et al., 1995; Pivnik and John- foreland evolution. Our magnetostrati- son, 1995). Depositional systems within the fore- India-Asia collision was initiated as early as graphic studies show that, although the ma- land respond to changes in at least five factors: (1) 65 Ma in the westernmost part of the orogen jor lithofacies preserved within the Himachal flexure of the loaded plate, (2) incipient deforma- (Beck et al., 1995).
    [Show full text]
  • Sequence Stratigraphic Framework of the Paleogene Succession of the Himalayan Foreland Basin: a Case Study from the Shimla Hills
    Journal of the Palaeontological Society of India ISSN 0522-9630 Vol ume 58(1), June 2013: 21-38 SEQUENCE STRATIGRAPHIC FRAMEWORK OF THE PALEOGENE SUCCESSION OF THE HIMALAYAN FORELAND BASIN: A CASE STUDY FROM THE SHIMLA HILLS S.B. BHATIA1, O.N. BHARGAVA2, BIRENDRA P. SINGH3 and HARMEET BAGI4 1441, SECTOR 6, PANCHKULA 134109 2103 SECTOR 7, PANCHKULA 134109 3CAS GEOLOGY DEPARTMENT, PANJAB UNIVERSITY, CHANDIGARH 160014 45333 PARKHIGHLAND BLVD. #9, CONCORD, CA 94521, U.S.A. E-mail: [email protected]; [email protected]; [email protected]; [email protected] ABSTRACT The Subathu Formation (Late Thanetian-Early Priabonian) of the Himalayan Foreland Basin constitutes a 2nd order depositional sequence with a subaerial unconformity at the base and a tidally influenced transitional sequence at the top. Three 3rd order T-R successions - A, B and C are recognized. Succession A (late Thanetian-late early Cuisian) includes seven facies association (FA) and commenced with transgression (TST; A.1), followed by MFS and a condensed section ( A.2; P4, SBZ 4-9), carbonate-siliciclastic coarsening upward sequence (A.3-4; HST), tectonically driven deposits (A.5-7), formation of back barrier lagoon with tidal inlet inhabited by sharks, ray fish; poor circulation in the lagoon caused mortality of the vertebrate fauna (A.6) and Early stage base level rise (A.7). Succession B. (Middle-Upper Cuisian, SBZ 11-12) includes seven FAs, B.1. Minor flooding surfaces, B.2-3. Coarsening upward succession, tidalflat, subtidal setting, B.4. Muddy tempestites, in inner shelf, B.5-6. Several benthic foraminifera and crabs indicate rise in sea level, B.7.
    [Show full text]
  • Active Strike-Slip Faults and an Outer Frontal Thrust in the Himalayan Foreland Basin
    Active strike-slip faults and an outer frontal thrust in the Himalayan foreland basin Michael J. Duvalla, John W. F. Waldrona,1, Laurent Godinb, and Yani Najmanc aDepartment of Earth and Atmospheric Sciences, University of Alberta, Edmonton, AB T6G2E3, Canada; bDepartment of Geological Sciences and Geological Engineering, Queen’s University, Kingston ON K7L 3N6, Canada; and cLancaster Environment Centre, Lancaster University, LA1 4YQ Lancaster, United Kingdom Edited by Lisa Tauxe, University of California San Diego, La Jolla, CA, and approved June 11, 2020 (received for review February 2, 2020) The Himalayan foreland basin formed by flexure of the Indian Plate unconformably on Proterozoic mobile belts, sedimentary basins, below the advancing orogen. Motion on major thrusts within the and an Archean craton, exposed along the southern edge of the orogen has resulted in damaging historical seismicity, whereas south basin. The stratigraphy of the basin is known from drilling and of the Main Frontal Thrust (MFT), the foreland basin is typically from outcrop in the sub-Himalaya and Lesser Himalaya (22). portrayed as undeformed. Using two-dimensional seismic reflection The basin fill is divided by an Oligocene disconformity in the sub- data from eastern Nepal, we present evidence of recent deformation Himalaya (23, 24), below which a thin (>90 m) Paleogene suc- propagating >37 km south of the MFT. A system of tear faults at a cession is dominated by marine mudstone (25). The overlying high angle to the orogen is spatially localized above the Munger- Miocene to Quaternary rocks are fluvial deposits that filled the Saharsa basement ridge. A blind thrust fault is interpreted in the subsiding basin (4).
    [Show full text]
  • GSA Bulletin: Neogene Foreland Basin Deposits, Erosional Unroofing, And
    Neogene foreland basin deposits, erosional unroofing, and the kinematic history of the Himalayan fold-thrust belt, western Nepal P. G. DeCelles* G. E. Gehrels J. Quade Department of Geosciences, University of Arizona, Tucson, Arizona 85721 T. P. Ojha P. A. Kapp† } B. N. Upreti Department of Geology, Tribhuvan University, Tri-Chandra Campus, Ghantaghar, Kathmandu, Nepal ABSTRACT Group manifest an upsection enrichment in slip in this duplex has been fed updip and potassium feldspar, carbonate lithic frag- southward into the Main Boundary and Main Sedimentological and provenance data ments, and high-grade metamorphic miner- Frontal thrust systems. from the lower Miocene–Pliocene Dumri For- als. Modal petrographic analyses of modern We obtained 113 U-Pb ages on detrital zir- mation and Siwalik Group in western Nepal river sands provide some control on potential cons from modern rivers and Siwalik Group provide new information about the timing of source terranes for the Miocene–Pliocene sandstones that cluster at 460–530 Ma, thrust faulting and the links between erosional sandstones. The Dumri Formation was most ~850–1200 Ma, ~1.8–2.0 Ga, and ~2.5 Ga. An unroofing of the Himalaya and the Cenozoic likely derived from erosion of sedimentary abundance of Cambrian–Ordovician grains 87Sr/86Sr record of the ocean. In western and low-grade metasedimentary rocks in the in the Siwalik Group suggests sources of Siwa- Nepal, the Dumri Formation is an ~750–1300- Tibetan (Tethyan) Himalayan zone during lik detritus in the granites of the Dadeldhura m-thick fluvial sandstone and overbank mud- early Miocene emplacement of the Main Cen- thrust sheet and possibly the Greater Hima- stone unit.
    [Show full text]
  • Geological Society of America Bulletin
    Downloaded from gsabulletin.gsapubs.org on 30 July 2009 Geological Society of America Bulletin The Kumaun and Garwhal Lesser Himalaya, India: Part 1. Structure and stratigraphy Julien Célérier, T. Mark Harrison, Andrew Alexander G. Webb and An Yin Geological Society of America Bulletin 2009;121;1262-1280 doi: 10.1130/B26344.1 Email alerting services click www.gsapubs.org/cgi/alerts to receive free e-mail alerts when new articles cite this article Subscribe click www.gsapubs.org/subscriptions/ to subscribe to Geological Society of America Bulletin Permission request click http://www.geosociety.org/pubs/copyrt.htm#gsa to contact GSA Copyright not claimed on content prepared wholly by U.S. government employees within scope of their employment. Individual scientists are hereby granted permission, without fees or further requests to GSA, to use a single figure, a single table, and/or a brief paragraph of text in subsequent works and to make unlimited copies of items in GSA's journals for noncommercial use in classrooms to further education and science. This file may not be posted to any Web site, but authors may post the abstracts only of their articles on their own or their organization's Web site providing the posting includes a reference to the article's full citation. GSA provides this and other forums for the presentation of diverse opinions and positions by scientists worldwide, regardless of their race, citizenship, gender, religion, or political viewpoint. Opinions presented in this publication do not reflect official positions of the Society. Notes © 2009 Geological Society of America Downloaded from gsabulletin.gsapubs.org on 30 July 2009 The Kumaun and Garwhal Lesser Himalaya, India: Part 1.
    [Show full text]
  • Geophysical-Petrological Model of the Crust and Upper Mantle in the India
    PUBLICATIONS Tectonics RESEARCH ARTICLE Geophysical-petrological model of the crust and upper 10.1002/2016TC004161 mantle in the India-Eurasia collision zone Key Points: Lavinia Tunini1, Ivone Jiménez-Munt1, Manel Fernandez1, Jaume Vergés1, Antonio Villaseñor1, • Thermal-compositional lithospheric 1 2 structure of the India-Eurasia collision Massimiliano Melchiorre , and Juan Carlos Afonso zone 1 2 • Identified lateral variations in the Institute of Earth Sciences Jaume Almera, CSIC, Barcelona, Spain, GEMOC-CCFS Department of Earth and Planetary lithospheric mantle compositions Sciences, Macquarie University, North Ryde, New South Wales, Australia • Different lithospheric domains have been identified in the India-Eurasia collision zone Abstract We present a new crust and upper mantle cross section of the western India-Eurasia collision zone by combining geological, geophysical, and petrological information within a self-consistent Supporting Information: thermodynamic framework. We characterize the upper mantle structure down to 410 km depth from the • Supporting Information S1 thermal, compositional, and seismological viewpoints along a profile crossing western Himalayan orogen • Supporting Information S2 and Tibetan Plateau, Tarim Basin, Tian Shan, and Junggar Basin, ending in the Chinese Altai Range. Our results Correspondence to: show that the Moho deepens from the Himalayan foreland basin (~40 km depth) to the Kunlun Shan (~90 km L. Tunini, depth), and it shallows to less than 50 km beneath the Tarim Basin. Crustal thickness between the Tian Shan [email protected]; and Altai mountains varies from ~66 km to ~62 km. The depth of the lithosphere-asthenosphere boundary [email protected] (LAB) increases from 230 km below the Himalayan foreland basin to 295 km below the Kunlun Shan.
    [Show full text]
  • Late Cenozoic Himalayan Foreland Basin: Sedimentologic Attributes
    Article 417 by Rohtash Kumar Late Cenozoic Himalayan foreland basin: Sedimentologic attributes Scientist (Retd.), Wadia Institute of Himalayan Geology, 33 GMS Road, Dehra Dun – 248001, Uttarakhand, INDIA e-mail: [email protected] (Received : 5/11/2018; Revised accepted : 24/07/2019) https://doi.org/10.18814/epiiugs/2020/020026 Late Cenozoic fluvial stratigraphic records of the understand the variability in depositional setting (Tandon, 1976, 1991; Himalayan foreland basin– the Siwalik Group between Kumar and Tandon, 1985; Burbank et al., 1996; Kumar et al., 2003a; 2004a,b; 2011; Goswami and Deopa, 2018 and references therein), Rivers Ganga and Ravi were studied and reviewed to marine to fluvial transition (Srivastava and Casshyap, 1983; Singh, understand the responses of allogenic forcing at variable 1978; Najman; 2006; Bera et al., 2008; Kumar et al; 2008 and timeframe. The Siwalik succession represents an upward references therein), biostratigraphy, faunal evolution and migration stratigraphic coarsening sequence which was initiated route (Pilgrim., 1913; Colbert., 1935; Agrawal et al., 1993; Nanda and Sehgal, 1993; Nanda, 2002; 2013; 2015; Basu., 2004; Patnaik, ~13 Ma and terminated and deformed by the Himalayan 2013; Gilbert et al., 2017; Nanda et al., 2018 and references therein), Frontal Thrust (HFT) at around 0.2 Ma. Fluvial magnetostratigraphy (Azzaroli, and Naponeone, 1982; Johnson et al., architecture, composition and paleoflow patterns exhibits 1983; Tandon et al., 1984; Ranga Rao, 1993; Ranga Rao et al., 1995, patial and temporal variations and characteristics of a Sangode et al., 1996, 1999, 2003; Chirouze et al., 2012; Sangode, large river that evolved around 10 Ma with southward 2014; Govin et al., 2018 and references therein), thrusting event (e.g.
    [Show full text]
  • Structural Evolution of the Himalayan Thrust Belt, West Nepal
    STRUCTURAL EVOLUTION OF THE HIMALAYAN THRUST BELT, WEST NEPAL ____________________________________________ A Thesis Presented to the Faculty of the Department of Earth and Atmospheric Sciences University of Houston ____________________________________________ In Partial Fulfillment of the Requirements for the Degree Master of Science in Geology ____________________________________________ By An Li August 2013 STRUCTURAL EVOLUTION OF THE HIMALAYAN THRUST BELT, WEST NEPAL _______________________________________________ An Li APPROVED: _______________________________________________ Dr. Michael Murphy, Chairman _______________________________________________ Dr. Alexander Robinson _______________________________________________ Dr. Ran Zhang _______________________________________________ Dean, College of Natural Sciences and Mathematics ii ACKNOWLEDGEMENTS I would like to express my sincere gratitude to my committee chair, Dr. Michael Murphy for his patient guidance and persistent help for my thesis research. Thanks him for taking me to the field trip at Big Bend and New Mexico. The most valuable thing I have learned from him is to be passionate to the work and be optimistic to the life. I would like to thank my committee members, Dr. Alexander Robinson and Dr. Ran Zhang for the support and assistance throughout this research project. Thanks to Sylvia Marshall and Jay Krishnan for answering all my academic and IT questions. Thanks to my classmate Yiduo Liu for giving me generous help in the field trips and constructive discussions about my thesis research. Thanks to my Uncle Faqi and Aunt Fenghua for taking care of my life at Houston. And thanks to my classmates and friends for accompanying and encouraging me in both study and life. Above all, I would like to thank my family, Zhenru, Jinbo, Dongran, Junfang. Thank you for endless love and support that gave me the strength to conquer difficulties and courage to chase my dream.
    [Show full text]