DOCSLIB.ORG

Map of Dolerite Dyke Swarms and Related Units of Russia and Selected Adjacent Regions

Total Page：16

File Type：pdf, Size：1020Kb

Download full-text PDF Read full-text
Map of Dolerite Dyke Swarms and Related Units of Russia and Selected Adjacent Regions Map of Dolerite Dyke Swarms and Related Units of Russia and Selected Adjacent Regions Карта роев долеритовых даек и связанных с ними комплексов России и избранных соседних регионов 45°0'0"E 70°0'0"E 95°0'0"E 120°0'0"E 145°0'0"E 170°0'0"E 180°0'0" 70°0'0"N LABEL SWARM NAME LOCATION AGE TREND LENGTH WIDTH RELATED REFERENCE (km) (km) UNITS 80°0'0"N K1 East Kola (dolerite) Kola Peninsula ?380 Ma N-S G. Fedotov K2 Pechenga (dolerite) Kola Peninsula 380 Ma Ar-Ar NNE G. Fedotov K3 Rybachy Kola Peninsula 540-600 Ma NE G. Fedotov 0 750 1,500 Km K4 Vochelambina (olivine Kola Peninsula 1160 Ma E-W Local Local G. Fedotov dolerite) K5 Verkhnetulomsky Kola Peninsula 1760 Ma G. Fedotov (lamprophyre) K6 Barenzevomorsky Kola Peninsula 1900 Ma (Sm-Nd) NW 120 km G. Fedotov (dolerite, poikioophhitic) K7 Njasjukka (ol gabbro, krs Kola Peninsula 1940 Ma NW G. Fedotov plagioperidotite) K8 Uraguba (ferropicrite) Kola Peninsula ? 1940-2000 Ma N-S G. Fedotov K9 Drozdovka (ferrodolerite) Kola Peninsula ? E-W G. Fedotov K10 Marjok (ferrodolerite) Kola Peninsula 2450-2500 Ma? N-S G. Fedotov K11 Murmansk (ferrodolerite) Kola Peninsula 1900-2100 Ma NE G. Fedotov D42 K12 Moncha-Pechenga Kola Peninsula 1900-2100 Ma swings G. Fedotov (ferrodolerite) NW to NNW K13 Dolgaja Tshely Kola Peninsula 1900-2200 Ma NW G. Fedotov D26 (picrodolerite) D11 K14 Pecheguba (low Al Kola Peninsula 2000-2200 Ma N-S G. Fedotov D15 D14 microgabbro) D12 K15 Kolmozero (low Al Kola Peninsula 2000-2200 Ma NE G. Fedotov microgabbro) D13 K16 Bauman pit (quartz Kola Peninsula Ca. 2040 Ma (Sm- NW G. Fedotov D39 dolerite) Nd) K17 North Pechenga (quartz Kola Peninsula 2050-2300 Ma NNE G. Fedotov dolerite) K18 Rosljakovo (quartz Kola Peninsula 2050-2300 Ma) NW G. Fedotov D46 D52 dolerite) A K19 Keyvy-2 (quartz dolerite) Kola Peninsula 2050-2300 Ma NE G. Fedotov K20 Keyvy-1 (olivine Kola Peninsula Ca. 2320 Ma Sm- E-W G. Fedotov gabbronorite Nd C51 D38 K21 Olegorsk pit (olivine Kola Peninsula 2495 Ma U-Pb NE G. Fedotov gabbronorite) C65 K22a Loypishnun (norite) Kola Peninsula 2487 Ma, 2496 Ma NW G. Fedotov C50 70°0'0"N U-Pb K22b Loypishnun Kola Peninsula 2506 Ma U-Pb NW G. Fedotov C43 C42 C7 D40 (gabbronorite) D36 C11 K22c Loypishnun (low K Kola Peninsula Ca. 2.52 Ma Sm- NW G. Fedotov tholeiite) Nd C18 K23 Mustatunturi (olivine Kola Peninsula Ca. 2550 Ma Sm- NNE G. Fedotov gabbronorite) Nd C38 C60 K24 Plagioclase dolerite Kola Peninsula >2600 Ma Various G. Fedotov C8 trends D37 D41 D22 K25 Kigora pit (gabbronorite) Kola Peninsula 2740 Ma U-Pb NW G. Fedotov D35 C24 BS1 Sayan swarm Sayan-Baikal 780-740 Ma Gladkochub et al. (2007) C4 area BS2 Baikal & northern Baikal Sayan-Baikal 800-760 Ma Gladkochub et al. (2007) D47 C5 swarms area U1 T Urals Triassic V.N. Puchkov G U2 C Urals Carboniferous V.N. Puchkov C47 D16 U3 D Urals Devonian dykes V.N. Puchkov C14 B U4 D Urals Devonian sheeted V.N. Puchkov D D21 complexes C16C15 C82 U5 O Urals Ordovician dykes V.N. Puchkov C17 C9 D20 E D3 (?) D1 C19 U6 O Urals Ordovician sheeted V.N. Puchkov complex C34 D44 D19 U7 UR Urals Upper Riphean V.N. Puchkov C21 C22 U8 EMR Urals Early and Middle V.N. Puchkov Riphean 60°0'0"N D5 K1 Ludikoviy Karelia 2060-1960 Ma NW V. Kulikov K2 Jatuliy Karelia 2220-2100 Ma variable V. Kulikov C56 K3 Sumiy Karelia 2500-2400 Ma NW & NE V. Kulikov M1 MZ Mongolia area Mesozoic ENE V.V. Yarmolyuk M2a P1 Mongolia area Paleozoic WNW V.V. Yarmolyuk F M2b P2 Mongolia area Paleozoic ENE-NE M2c C3-P1 Mongolia area Paleozoic E V.V. Yarmolyuk M2d D1-2 Mongolia area Devonian WSW & NNW C55 M3 NP2 Mongolia area Neoproterozoic NW V.V. Yarmolyuk D28 Uk1 Ukraine ? variable I.K. Pashkevich AD1 Eastern Aldan Proterozoic? NNE-NE A.N Didenko D31 shield AD2 Eastern Aldan Proterozoic? NW A.N Didenko shield C58 A.N Didenko C57 D49 AD3 Eastern Aldan Proterozoic? E-ESE C39 shield C84 C64 AD4 Eastern Aldan Proterozoic? E A.N Didenko D48 C79 shield C81 AD5 Eastern Aldan Proterozoic? N A.N Didenko 50°0'0"N C80 shield C54 1 Gashunnur dyke complex Mongolia, China, ~320 Ma (Sm-Nd) ESE 600 30 Baykova and Amelin C10 (1995) C78 C77 C30 C59 2 Khatanga dyke swarm Siberia Late Archean? NNW- 1000? Glukhovskii and Moralev C1 NW (2003) C27 Background and C# and D# dykes 3 Sunnagin Early Archean? Glukhovskii and Moralev C (2003) after Ernst et al., 1996 D52 Ust’Nera e. Russia 100-65 Ma E, NE, N 50 60 D52 in [1] (65.0N, 142.0E) D62 D44 Bratsk e. Russia <250 Ma N-NNW 150 120 D44 in [1] (57.5N, 101E) D42 Ebekhaya e. Russia 250 Ma ESE 400 20 D42 in [1] (72N, 110E) 45°0'0"E 70°0'0"E 95°0'0"E 120°0'0"E 40°0'0"N 145°0'0"E D45 Kochikha e. Russia <250 Ma E 220 120 D45 in [1] (70.5N, 97E) D46 Kureyka e. Russia <250 Ma NE 310 240 D46 in [1] (69N, 95E) D43 Maymecha e. Russia <250 Ma ESE-SE 450 130 D43 in [1] (70N, 101E) from D. Gladkochub D47 Mutoray e. Russia <250 Ma E 150 60 D47 in [1] Dyke swarm maps at a continental scale are a powerful tool for identification of large igneous provinces (LIPs), interpreting geodynamic settings, locating E (61.5N, 102.0E) D48 Serebryansk Russia 250-245 Ma ~NE-E 100 150 D48 in [1] mantle plumes, characterizing the breakup history of supercontinents, and paleocontinental reconstructions. Such a map at 1:5 000 000 scale is now available for (49N, 84E) DYKE SWARMS & RELATED UNITS OF THE KOLA REGION D49 Tashanta Russia 250-205 Ma E 50 70 D49 in [1] Canada and adjacent regions (Buchan & Ernst, 2004, Geol. Surv. Canada. Map 2022A) and has proven to be very important in this context. Preparation of a Archean NORTH PECHENGA RYBACHY (50N, 88E) DOLGAJA TSHELY Kirgora pit, gabbronorite(2,74 Ga , U-Pb) similar map for the dyke swarms of Russia and adjacent areas will undoubtedly prove equally useful. 30 C64 Anton-Taram Ukraine 360-328 Ma SE 200 10 C64 in [1] 35 25 30 Pl Dolerite (> 2,6 Ga) 35 30 PR 3 from Zh. Fedotov Paleoproterozoic D MUSTATUNTURI A (51N, 33E URAGUBA Mustatunturi, Ol Gabbronorite (ca 2.55 Ga, Sm-Nd) from V. Puchkov D37 --Chara-Sinsk e. Russia 360 Ma NE 700 600 D37 in [1] PR 1 NJASJUKKA Loypishnun, Low K Toleite (ca 2. 52 Ga, Sm-Nd) THE MODERN VIEW OF DYKE SWARMS: In recent years there has been a revolution in the study and understanding of dyke swarms. Aeromagnetic maps PECHENGA 56 58 60 62 64 66 68 (61N, 124E) M BARENZEVOMORSKY Loypishnun, Gabbronorite ( 2.506 Ga, U-Pb) O 70 N MURMANSK D39 --Dzhardzhan (Yakutsk e. Russia 360 Ma SE 200 200 D39 in [1] C Loypishnun, Norite (2.487, 2.496 Ga, U-Pb) H D reveal swarms of vast scale but simple geometry (linear and radiating). They can now be routinely dated to better than +/-5 million years precision using the U- A Olegorsk pit, Ol Gabbronorite (2.495 Ga, U-Pb) Northwest) (69N, 120E) - P E ROSLJAKOVO Keyvy 1, Ol Gabbronorite (ca 2.32 Ga, Sm-Nd) C D40 --Tomporuk (Yaktusk e. Russia 360 Ma N 300 100 D40 in [1] H Keyvy 2, Quartz Dolerite (2.05-2.3 Ga) Pb method on baddeleyite and zircon, and, in some instances, using the Ar-Ar technique. Dating indicates that many swarms are emplaced in short duration E Kola Block N DROZDOVKA Rosljakovo Quartz Dolerite (2.05-2.3) South) (63N, 137E) G A P - E Pl-DOLERITE North Pechenga, Quartz Dolerite (2.05-2.3 Ga) D N E. KOLA-2 D38 --Vilyui-Marcha e. Russia 360 Ma NE 800 400 D38 in [1] events of <10 million years. Paleomagnetic studies of precisely dated dykes can yield well constrained Apparent Polar Wander Paths (APWPs) and C O H Bauman pit, Quartz Dolerite (ca 2.04 Ga, Sm-Nd R E W (64N, 115E) G Kolmozero, Low Al Microgabbro(2.0-2.2 Ga) A U paleocontinental reconstructions. Y B Pecheguba, Low Al Microgabbro(2.0-2.2 Ga) A D37- Yakutsk 360 Ma NW-S D37-D40 in [1] A Dolgaja Tshely, Picrodolerite (1.9-2.2 Ga) O? OLENEGORSK PIT Т D40 (fan) BAUMAN PIT KIRGORAT PI Moncha-Pechenga, Ferrodolerite (1.9-2.1 Ga) 68 D41 Zhil’Gur e. Russia ? 360 Ma N 160 90 D41 in [1] PZ Murmansk, Ferrodolerite(1.9-2.1 Ga) CANADIAN NATIONAL DYKE SWARM MAP: The benefits of producing a Russian national dyke swarm map are well illustrated by the Canadian LOYPISHNJUN B O (61N, 127E) (local Monca Swarm) PZ KEYVY 1 Marjok, Ferrodolerite(2.45-2.5? Ga) KOLMOZERO MARJOK Drozdovka, Ferrodolerite (?) D35 Inta Russia 450-440 Ma NE 210 35 D35 in [1] VOCHELAMBINA UR D compilation (Buchan & Ernst 2004). This map compiles 453 swarms with an age distribution as follows: 35 Archean, 76 Paleoproterozoic, 60 Mesoproterozoic, Uraguba, Ferropicrite (?1.94-2.0) O (65N, 61.5E) White Sea Block Njasjukka, Ol Gabbro, Krs Plagioperidotite(1.94 Ga, U-Pb ) C 31 Neoproterozoic, and 162 Phanerozoic (97 Paleozoic, 27 Mesozoic, 38 Cenozoic) swarms, as well as 89 that are very poorly dated.
Load more

Recommended publications
  • Petroleum Geology and Resources of the Dnieper-Donets Basin, Ukraine and Russia
    Petroleum Geology and Resources of the Dnieper-Donets Basin, Ukraine and Russia By Gregory F. Ulmishek U.S. Geological Survey Bulletin 2201-E U.S. Department of the Interior U.S. Geological Survey U.S. Department of the Interior Gale A. Norton, Secretary U.S. Geological Survey Charles G. Groat, Director Version 1.0, 2001 This publication is only available online at: http://geology.cr.usgs.gov/pub/bulletins/b2201-e/ Any use of trade, product, or firm names in this publication is for descriptive purposes only and does not imply endorsement by the U.S. Government Manuscript approved for publication July 3, 2001 Published in the Central Region, Denver, Colorado Graphics by Susan Walden and Gayle M. Dumonceaux Photocomposition by Gayle M. Dumonceaux Contents Foreword ....................................................................................................................................... 1 Abstract.......................................................................................................................................... 1 Introduction .................................................................................................................................. 2 Province Overview ....................................................................................................................... 2 Province Location and Boundaries................................................................................. 2 Tectono-Stratigraphic Development .............................................................................
    [Show full text]
  • Murun Massif, Aldan Shield of the Siberian Craton: a Simple Story for an Intricate Igneous Complex
    minerals Article 40Ar/39Ar Geochronology of the Malyy (Little) Murun Massif, Aldan Shield of the Siberian Craton: A Simple Story for an Intricate Igneous Complex Alexei V. Ivanov 1,* , Nikolay V. Vladykin 2, Elena I. Demonterova 1, Viktor A. Gorovoy 1 and Emilia Yu. Dokuchits 2 1 Institute of the Earth’s Crust, Siberian Branch of the Russian Academy of Sciences, 664033 Irkutsk, Russia; [email protected] (E.I.D.); [email protected] (V.A.G.) 2 A.P. Vinogradov Institute of Geochemistry, Siberian Branch of the Russian Academy of Sciences, 664033 Irkutsk, Russia; [email protected] (N.V.V.); [email protected] (E.Y.D.) * Correspondence: [email protected]; Tel.: +7-395-242-7000 Received: 17 November 2018; Accepted: 16 December 2018; Published: 19 December 2018 Abstract: The Malyy (Little) Murun massif of the Aldan Shield of the Siberian Craton has long been a kind of Siberian Mecca for geologists. It has attracted thousands of geologists, prospectors, and mineral collectors despite its remote location. It is famous for a dozen new and rare minerals, including the gemstones charoite and dianite (the latter is the market name for strontian potassicrichrerite), as well as for a range of uncommon alkaline igneous rocks. Despite this, the age of the Malyy Murun igneous complex and associated metasomatic and hydrothermal mineral associations has remained poorly constrained until now. In this paper, we provide extensive 40Ar/39Ar geochronological data to reveal its age and temporal history. It appears that, although unique in terms of rocks and constituent minerals, the Malyy Murun is just one of multiple alkaline massifs and lavas emplaced in the Early Cretaceous (~137–128 Ma) within a framework of the extensional setting of the Aldan Shield and nearby Transbaikalian region.
    [Show full text]
  • Pan-African Orogeny 1
    Encyclopedia 0f Geology (2004), vol. 1, Elsevier, Amsterdam AFRICA/Pan-African Orogeny 1 Contents Pan-African Orogeny North African Phanerozoic Rift Valley Within the Pan-African domains, two broad types of Pan-African Orogeny orogenic or mobile belts can be distinguished. One type consists predominantly of Neoproterozoic supracrustal and magmatic assemblages, many of juvenile (mantle- A Kröner, Universität Mainz, Mainz, Germany R J Stern, University of Texas-Dallas, Richardson derived) origin, with structural and metamorphic his- TX, USA tories that are similar to those in Phanerozoic collision and accretion belts. These belts expose upper to middle O 2005, Elsevier Ltd. All Rights Reserved. crustal levels and contain diagnostic features such as ophiolites, subduction- or collision-related granitoids, lntroduction island-arc or passive continental margin assemblages as well as exotic terranes that permit reconstruction of The term 'Pan-African' was coined by WQ Kennedy in their evolution in Phanerozoic-style plate tectonic scen- 1964 on the basis of an assessment of available Rb-Sr arios. Such belts include the Arabian-Nubian shield of and K-Ar ages in Africa. The Pan-African was inter- Arabia and north-east Africa (Figure 2), the Damara- preted as a tectono-thermal event, some 500 Ma ago, Kaoko-Gariep Belt and Lufilian Arc of south-central during which a number of mobile belts formed, sur- and south-western Africa, the West Congo Belt of rounding older cratons. The concept was then extended Angola and Congo Republic, the Trans-Sahara Belt of to the Gondwana continents (Figure 1) although West Africa, and the Rokelide and Mauretanian belts regional names were proposed such as Brasiliano along the western Part of the West African Craton for South America, Adelaidean for Australia, and (Figure 1).
    [Show full text]
  • Timing of Metamorphism in the Arabian-Nubian Shield Constrained by In-Situ U-Pb Dating of Accessory and Major Metamorphic Phases
    Geophysical Research Abstracts Vol. 20, EGU2018-15645-1, 2018 EGU General Assembly 2018 © Author(s) 2018. CC Attribution 4.0 license. Timing of metamorphism in the Arabian-Nubian Shield constrained by in-situ U-Pb dating of accessory and major metamorphic phases Leo J. Millonig (1,2), Richard Albert Roper (1), Axel Gerdes (1), and Dov Avigad (2) (1) Department of Geosciences, Goethe University Frankfurt, Germany, (2) Institute of Earth Sciences, Hebrew University of Jerusalem, Israel The Arabian-Nubian Shield (ANS), which forms the northern branch of the East African Orogen, evolved from intra-oceanic island arcs into a mature continental crust in the course of ∼300 m.y. of Neoproterozoic Pan-African orogeny. The metapelitic Elat Schist in southern Israel records two metamorphic events that affected the northern part of the ANS, but the significance, extent and the exact timing of these events is controversially discussed. Previous geochronological studies on metamorphic monazite, in conjunction with field evidence, indicate that the main period of regional amphibolite-facies metamorphism occurred at ∼620 Ma, just prior to and coeval with regional-scale intrusions of late-orogenic granitoids. However, other field observations from the Elat area provide evidence that regional metamorphism also occurred prior to ∼705 Ma. This older age is inferred from an E- W trending, vertically-foliated, ∼705 Ma greenschist-facies dike swarm, which cross-cuts the shallow-dipping foliation of the garnet-bearing Elat Schist, thus indicating a more prolonged metamorphic evolution. In order to gain a more comprehensive understanding of the metamorphic history of this area, we apply in-situ U-Pb dating of monazite, garnet and staurolite to garnet-, garnet-staurolite-, and staurolite-bearing schists from the Elat area.
    [Show full text]
  • Geology of Stone
    The Geology of Stone An excerpt from the Dimension Stone Design Manual, Version VIII (May 2016) Produced and Published by the Marble Institute of America 380 East Lorain St. Oberlin, Ohio 44074 Telephone: 440-250-9222 Fax: 440-774-9222 www.naturalstoneinstitute.org © 2016 All rights reserved. No part of this document may be reproduced or transmitted in any form or by means electronic or mechanical, including photocopy, recording, or by an information storage and retrieval system, without written permission from the Natural Stone Institute. The geology of 2.0 STONE CATEGORIES Stone 2.1 Three general rock or stone categories are recognized according to their mode of 1.0 INTRODUCTION origin. This is a genetic classification, and it not only states how and under what general 1.1 Earth is geologically classified as a “stony conditions a stone was formed, but also implies planet,” as it is entirely stone (rock) of various a general compositional range. The basic stone mineral compositions and forms, excluding its groups are: water and atmosphere. 2.1.1 Igneous rock is formed by 1.2 Earth scientists prefer the term “rock,”1 solidification (cooling) or, in some cases, by while the commercial stone industry, prefers solid-state transformation3 of molten or semi- the term “stone”.2 Both words are correct in molten material in the Earth’s upper mantle or their respective frame of reference, and for crust into crystalline rock generally consisting practical purposes, interchangeable. Every of silicates (compounds with SiO4) and some type of rock or stone is composed of one or dark-colored accessory minerals such as iron more minerals.
    [Show full text]
  • Thermochronology and Exhumation History of The
    Thermochronology and Exhumation History of the Northeastern Fennoscandian Shield Since 1.9 Ga: Evidence From 40 Ar/ 39 Ar and Apatite Fission Track Data From the Kola Peninsula Item Type Article Authors Veselovskiy, Roman V.; Thomson, Stuart N.; Arzamastsev, Andrey A.; Botsyun, Svetlana; Travin, Aleksey V.; Yudin, Denis S.; Samsonov, Alexander V.; Stepanova, Alexandra V. Citation Veselovskiy, R. V., Thomson, S. N., Arzamastsev, A. A., Botsyun, S., Travin, A. V., Yudin, D. S., et al. (2019). Thermochronology and exhumation history of the northeastern Fennoscandian Shield since 1.9 Ga:evidence from 40Ar/39Ar and apatite fission track data from the Kola Peninsula. Tectonics, 38, 2317–2337.https:// doi.org/10.1029/2018TC005250 DOI 10.1029/2018tc005250 Publisher AMER GEOPHYSICAL UNION Journal TECTONICS Rights Copyright © 2019. American Geophysical Union. All Rights Reserved. Download date 01/10/2021 04:51:21 Item License http://rightsstatements.org/vocab/InC/1.0/ Version Final published version Link to Item http://hdl.handle.net/10150/634481 RESEARCH ARTICLE Thermochronology and Exhumation History of the 10.1029/2018TC005250 Northeastern Fennoscandian Shield Since 1.9 Ga: Key Points: 40 39 • Since 1.9 Ga, the NE Fennoscandia Evidence From Ar/ Ar and Apatite Fission was characterized by a slow exhumation (1‐2 m/Myr) Track Data From the Kola Peninsula • Total denudation of the NE Roman V. Veselovskiy1,2 , Stuart N. Thomson3 , Andrey A. Arzamastsev4,5 , Fennoscandia since 1.9 Ga did not 6 7,8 7,8 9 exceed ~3‐5km Svetlana Botsyun , Aleksey V. Travin , Denis S. Yudin , Alexander V. Samsonov , • The Kola part of Fennoscandia and Alexandra V.
    [Show full text]
  • Tectonic Evolution of the Mesozoic South Anyui Suture Zone, GEOSPHERE; V
    Research Paper GEOSPHERE Tectonic evolution of the Mesozoic South Anyui suture zone, GEOSPHERE; v. 11, no. 5 eastern Russia: A critical component of paleogeographic doi:10.1130/GES01165.1 reconstructions of the Arctic region 18 figures; 5 tables; 2 supplemental files; 1 animation Jeffrey M. Amato1, Jaime Toro2, Vyacheslav V. Akinin3, Brian A. Hampton1, Alexander S. Salnikov4, and Marianna I. Tuchkova5 1Department of Geological Sciences, New Mexico State University, MSC 3AB, P.O. Box 30001, Las Cruces, New Mexico 88003, USA CORRESPONDENCE: [email protected] 2Department of Geology and Geography, West Virginia University, 330 Brooks Hall, P.O. Box 6300, Morgantown, West Virginia 26506, USA 3North-East Interdisciplinary Scientific Research Institute, Far East Branch, Russian Academy of Sciences, Magadan, Portovaya Street, 16, 685000, Russia CITATION: Amato, J.M., Toro, J., Akinin, V.V., Hamp- 4Siberian Research Institute of Geology, Geophysics, and Mineral Resources, 67 Krasny Prospekt, Novosibirsk, 630091, Russia ton, B.A., Salnikov, A.S., and Tuchkova, M.I., 2015, 5Geological Institute, Russian Academy of Sciences, Pyzhevskii per. 7, Moscow, 119017, Russia Tectonic evolution of the Mesozoic South Anyui su- ture zone, eastern Russia: A critical component of paleogeographic reconstructions of the Arctic region: ABSTRACT INTRODUCTION Geosphere, v. 11 no. 5, p. 1530–1564, doi: 10 .1130 /GES01165.1. The South Anyui suture zone consists of late Paleozoic–Jurassic ultra- The South Anyui suture zone (Fig. 1) is a remnant of a Mesozoic ocean Received 19 December 2014 mafic rocks and Jurassic–Cretaceous pre-, syn-, and postcollisional sedimen- basin that separated the Arctic Alaska–Chukotka microplate from Siberia Revision received 2 July 2015 tary rocks.
    [Show full text]
  • Planet Earth
    © Jones & Bartlett Learning, LLC © Jones & Bartlett Learning, LLC NOT FOR SALE OR DISTRIBUTION NOT FOR SALE OR DISTRIBUTION © Jones & Bartlett Learning, LLC © Jones & Bartlett Learning, LLC NOT FOR SALE OR DISTRIBUTION NOT FOR SALE OR DISTRIBUTION © Jones & Bartlett Learning, LLC © Jones & Bartlett Learning, LLC NOT FOR SALE OR DISTRIBUTION NOT FOR SALE OR DISTRIBUTION © Jones & Bartlett Learning, LLC © Jones & Bartlett Learning, LLC NOT FOR SALE OR DISTRIBUTION NOT FOR SALE OR DISTRIBUTION © Jones & Bartlett Learning, LLC © Jones & Bartlett Learning, LLC NOT FOR SALE OR DISTRIBUTION NOT FOR SALE OR DISTRIBUTION © Jones & Bartlett Learning, LLC © Jones & Bartlett Learning, LLC NOT FOR SALE OR DISTRIBUTION NOT FOR SALE OR DISTRIBUTION Planet Earth © Jones & Bartlett1 Learning, LLC © Jones & Bartlett Learning, LLC NOT FOR SALE ORFrom DISTRIBUTION the beginning of our species, we have soughtNOT to understandFOR SALE our surroundings,OR DISTRIBUTION whether that was the soil beneath our feet or the stars in the heavens. Above, the Milky Way shimmers in silent splendor above the Dolomites in northeastern Italy. The Milky Way is a gigantic galaxy consisting of billions of stars, some stars are forming today and others dying explosively. Many of these stars have their own systems of planets, moons, and comets orbiting them. Earth is but one planet of many. Our planet© Jones orbits a& star Bartlett that is on Learning, the fringes of LLC the galaxy. Only since the beginning© Jones of & Bartlett Learning, LLC space explorationNOT in FOR the 1960s SALE have OR we seen DISTRIBUTION our planet as it really is, a tiny blue sphereNOT suspended FOR SALE OR DISTRIBUTION in nearly empty space.
    [Show full text]
  • Chapter 5 the Pre-Andean Phases of Construction of the Southern Andes Basement in Neoproterozoic-Paleozoic Times
    133 Chapter 5 The Pre-Andean phases of construction of the Southern Andes basement in Neoproterozoic-Paleozoic times Nemesio Heredia; Joaquín García-Sansegundo; Gloria Gallastegui; Pedro Farias; Raúl E. Giacosa; Fernando D. Hongn; José María Tubía; Juan Luis Alonso; Pere Busquets; Reynaldo Charrier; Pilar Clariana; Ferrán Colombo; Andrés Cuesta; Jorge Gallastegui; Laura B. Giambiagi; Luis González-Menéndez; Carlos O. Limarino; Fidel Martín-González; David Pedreira; Luis Quintana; Luis Roberto Rodríguez- Fernández; Álvaro Rubio-Ordóñez; Raúl E. Seggiaro; Samanta Serra-Varela; Luis A. Spalletti; Raúl Cardó; Victor A. Ramos Abstract During the late Neoproterozoic and Paleozoic times, the Southern Andes of Argentina and Chile (21º-55º S) formed part of the southwestern margin of Gondwana. During this period of time, a set of continental fragments of variable extent and allochtony was successively accreted to that margin, resulting in six Paleozoic orogenies of different temporal and spatial extension: Pampean (Ediacaran-early Cambrian), Famatinian (Middle Ordovician-Silurian), Ocloyic (Middle Ordovician-Devonian), Chanic (Middle Devonian-early Carboniferous), Gondwanan (Middle Devonian-middle Permian) and Tabarin (late Permian-Triassic). All these orogenies culminate with collisional events, with the exception of the Tabarin and a part of the Gondwanan orogenies that are subduction-related. Keywords Paleozoic, Southern Andes, Pampean orogen, Ocloyic orogen, Famatinian orogen, Chanic orogen, Gondwanan orogen, Tabarin orogen. 133 134 1 Introduction In the southern part of the Andean Cordillera (21º-55º S, Fig. 1A) and nearby areas, there are Neoproterozoic (Ediacaran)-Paleozoic basement relicts of variable extension. This basement has been involved in orogenic events prior to the Andean orogeny, which is related to the current configuration of the Andean chain (active since the Cretaceous).
    [Show full text]
  • GEOLOGY and DEVELOPMENT of the LOMONOSOV DIAMOND DEPOSIT, NORTHWESTERN RUSSIA Karen V
    FEATURE AR ICLES GEOLOGY AND DEVELOPMENT OF THE LOMONOSOV DIAMOND DEPOSIT, NORTHWESTERN RUSSIA Karen V. Smit and Russell Shor The Siberian craton in Russia hosts many of the country’s famous diamond mines.The Lomonosov mine, however, occurs within the boundaries of a different craton—the Baltic shield, most of which lies in Eu- rope. Unlike many diamond mines in South Africa, Canada, and Siberia, the Lomonosov deposit is not in a stable Archean geologic setting. Similar to the Argyle diamond mine in Australia, Lomonosov is in a younger Proterozoic orogenic (or mountain-building) region. Fancy pink diamonds at both these lo- calities likely relate to these Proterozoic tectonic processes. Along with other diamond mines in Pro- terozoic geologic regions, the Lomonosov deposit (and its fancy-color diamond inventory) demonstrates that the diamond potential of these regions should not be overlooked. ussia has been a major diamond producer for In August 2016, the authors visited the Lomonosov more than half a century. Most of its diamond deposit to document this exciting new diamond local- Rmines occur in the semi-autonomous Sakha ity. The visit included tours of the kimberlite open-pit Republic within the geological bounds of the Siberian operations, the processing plant, and the preliminary craton. However, over the last 12 years, Alrosa, a pub- diamond sorting facilities in the city of Arkhangelsk. lic joint-stock company (with both government and The authors also visited Alrosa’s central diamond sort- private ownership) operating through its subsidiary ing and sales operation, the United Selling Organisa- Severalmaz, has started development and mining at tion (USO) in Moscow.
    [Show full text]
  • Review of the Cambrian Pampean Orogeny of Argentina; a 2 Displaced Orogen Formerly Attached to the Saldania Belt of 3 South Africa? 4 5 César Casqueta*, Juán A
    1 Review of the Cambrian Pampean orogeny of Argentina; a 2 displaced orogen formerly attached to the Saldania Belt of 3 South Africa? 4 5 César Casqueta*, Juán A. Dahlquistb, Sebastián O. Verdecchiab, Edgardo G. 6 Baldob, Carmen Galindoa, Carlos W. Rapelac, Robert, J. Pankhurstd, Matias 7 M. Moralesb, Juán A. Murrab, C. Mark Fanninge 8 9 a Departamento de Petrología y Geoquímica, Facultad de Ciencias Geológicas, Instituto de 10 Geología Económica (CSIC), Universidad Complutense, 28040 Madrid, Spain1 11 b Centro de Investigaciones en Ciencias de la Tierra (CICTERRA), CONICET, Universidad 12 Nacional de Córdoba, Av. Vélez Sarsfield 1611, Pab. Geol., X5016CGA Córdoba, Argentina 13 c Centro de Investigaciones Geológicas, CONICET, Universidad Nacional de la Plata, 1900 La 14 Plata, Argentina 15 d Visiting Research Associate, British Geological Survey, Keyworth, Nottingham NG12 5GG, 16 UK 17 e Research School of Earth Sciences, Australian National University, Canberra, ACT 0200, 18 Australia 19 20 21 Keywords: Pampean orogeny; Saldanian orogeny; Sierras Pampeanas; Gondwana; Mara 22 terrane; collisional orogeny 23 24 25 Abstract 26 27 The Pampean orogeny of northern Argentina resulted from Early Cambrian oblique 28 collision of the Paleoproterozoic MARA block, formerly attached to Laurentia, with the 29 Gondwanan Kalahari and Rio de la Plata cratons. The orogen is partially preserved 30 because it is bounded by the younger Córdoba Fault on the east and by the Los Túneles 31 Ordovician shear zone on the west. In this review we correlate the Pampean Belt with 32 the Saldania orogenic belt of South Africa and argue that both formed at an active 33 continental margin fed with sediments coming mainly from the erosion of the 34 Brasiliano–Pan-African and East African–Antarctica orogens between ca.
    [Show full text]
  • The Case for Separate Taltson and Thelon Orogenies: Evidence from the Shield in Western Saskatchewan
    The case for separate Taltson and Thelon orogenies: Evidence from the Shield in western Saskatchewan C.D. Card* and K.E. Ashton Saskatchewan Ministry of Energy and Resources, Northern Geological Survey, 200-2101 Scarth St., Regina, SK S4P 2H9; e-mail: [email protected] and K.M. Bethune Department of Geology, University of Regina, 3737 Wascana Parkway, Regina, SK S4S 0A2 SUMMARY The Taltson magmatic zone is inferred to be the southern extension of the Thelon tectonic zone; together they are thought to have developed during a ca. 2.02-1.90 Ga orogeny that accreted the Rae and Slave cratons. The continuity between the Thelon tectonic and Taltson magmatic zones is predicated upon the similarity of the ages of igneous rocks and a linear aeromagnetic high that apparently links the two. The Taltson magmatic zone contains two suites of metaplutonic rocks: ca. 1.986-1.1959 Ga continental arc type plutons; and 1.955-1.910 Ga peraluminous plutons. They intruded a basement complex dominated by Mesoarchean to Paleoproterozoic orthogneisses and granitoid rocks. Peak metamorphic conditions were between 1.94 and 1.93 Ga. New mapping south of the western Athabasca Basin indicates that plutons of generally intermediate composition extend from the Virgin River shear zone beneath the western Athabasca Basin. The limited available geochronological data supports that interpretation as rocks with ages similar to the continental arc type plutons in the Taltson magmatic zone are found near the Virgin River shear zone, beneath the western Athabasca Basin and along basin‟s western margin. Plutons of similar age and composition to the peraluminous plutons of the Taltson magmatic zone and similar metamorphic ages are found in the basement to the western Athabasca Basin and the exposed Shield to the south.
    [Show full text]