Permian World Brochure
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Geologic Time Scale Cards
PreCambrian SuperEon (4.6 BYA – 541 MYA) Hadean Eon (4.6 BYA - 4 BYA) Slide # 1 46 feet Earth Forms • Earth is formed from a mass of dust and gas that gravity pulled together. • The process causes a huge amount of radioactive decay and Earth is a boiling ball of lava. • At 4.5 BYA a protoplanet named Theia collides with Earth and a debris ring forms which later becomes our moon. • Earth cools and forms the layers – core, mantel, and outer crust. • Meteors bombard earth bringing frozen droplets of water that later become our oceans. • Volcanic activity continues and Earth’s earliest continental crust forms before 4.03 BYA. The Acasta gneiss is one of the oldest rocks on Earth dating 4.03 billion years.. PreCambrian SuperEon (4.6 BYA – 541 MYA) Archaean Eon (4 BYA – 2.5 BYA) Slide # 2 40 feet Primitive, Simple Life Forms • Earth’s crust cools and plate tectonics forms. • Ancient rock formations form from 4 to 2.5 BYA. • The Primordial soup theory suggests early minerals and compounds from meteors made the perfect recipe for primitive, simple life to form at the thermal vents of the ocean. • Single cell life formed the ocean and over time stromatolites, photosynthesizing colonial bacteria, formed in shallow water and released oxygen. • The oxygen attached to trace iron in the oceans and formed sedimentary layers of banded iron formations (BIFS) that are presently mined for iron ore. Banded iron formations from the late Archaean and early Proterozoic eons Stromatolite fossil image PreCambrian SuperEon (4.6 BYA – 541 MYA) Proterozoic Eon (2.5 BYA – 541 MYA) Slide # 3 25 feet Early life • Photosynthesizing life further establishes and releases oxygen throughout the ocean. -
Timeline of Natural History
Timeline of natural history This timeline of natural history summarizes significant geological and Life timeline Ice Ages biological events from the formation of the 0 — Primates Quater nary Flowers ←Earliest apes Earth to the arrival of modern humans. P Birds h Mammals – Plants Dinosaurs Times are listed in millions of years, or Karo o a n ← Andean Tetrapoda megaanni (Ma). -50 0 — e Arthropods Molluscs r ←Cambrian explosion o ← Cryoge nian Ediacara biota – z ←Earliest animals o ←Earliest plants i Multicellular -1000 — c Contents life ←Sexual reproduction Dating of the Geologic record – P r The earliest Solar System -1500 — o t Precambrian Supereon – e r Eukaryotes Hadean Eon o -2000 — z o Archean Eon i Huron ian – c Eoarchean Era ←Oxygen crisis Paleoarchean Era -2500 — ←Atmospheric oxygen Mesoarchean Era – Photosynthesis Neoarchean Era Pong ola Proterozoic Eon -3000 — A r Paleoproterozoic Era c – h Siderian Period e a Rhyacian Period -3500 — n ←Earliest oxygen Orosirian Period Single-celled – life Statherian Period -4000 — ←Earliest life Mesoproterozoic Era H Calymmian Period a water – d e Ectasian Period a ←Earliest water Stenian Period -4500 — n ←Earth (−4540) (million years ago) Clickable Neoproterozoic Era ( Tonian Period Cryogenian Period Ediacaran Period Phanerozoic Eon Paleozoic Era Cambrian Period Ordovician Period Silurian Period Devonian Period Carboniferous Period Permian Period Mesozoic Era Triassic Period Jurassic Period Cretaceous Period Cenozoic Era Paleogene Period Neogene Period Quaternary Period Etymology of period names References See also External links Dating of the Geologic record The Geologic record is the strata (layers) of rock in the planet's crust and the science of geology is much concerned with the age and origin of all rocks to determine the history and formation of Earth and to understand the forces that have acted upon it. -
Assembly, Configuration, and Break-Up History of Rodinia
Author's personal copy Available online at www.sciencedirect.com Precambrian Research 160 (2008) 179–210 Assembly, configuration, and break-up history of Rodinia: A synthesis Z.X. Li a,g,∗, S.V. Bogdanova b, A.S. Collins c, A. Davidson d, B. De Waele a, R.E. Ernst e,f, I.C.W. Fitzsimons g, R.A. Fuck h, D.P. Gladkochub i, J. Jacobs j, K.E. Karlstrom k, S. Lu l, L.M. Natapov m, V. Pease n, S.A. Pisarevsky a, K. Thrane o, V. Vernikovsky p a Tectonics Special Research Centre, School of Earth and Geographical Sciences, The University of Western Australia, Crawley, WA 6009, Australia b Department of Geology, Lund University, Solvegatan 12, 223 62 Lund, Sweden c Continental Evolution Research Group, School of Earth and Environmental Sciences, University of Adelaide, Adelaide, SA 5005, Australia d Geological Survey of Canada (retired), 601 Booth Street, Ottawa, Canada K1A 0E8 e Ernst Geosciences, 43 Margrave Avenue, Ottawa, Canada K1T 3Y2 f Department of Earth Sciences, Carleton U., Ottawa, Canada K1S 5B6 g Tectonics Special Research Centre, Department of Applied Geology, Curtin University of Technology, GPO Box U1987, Perth, WA 6845, Australia h Universidade de Bras´ılia, 70910-000 Bras´ılia, Brazil i Institute of the Earth’s Crust SB RAS, Lermontova Street, 128, 664033 Irkutsk, Russia j Department of Earth Science, University of Bergen, Allegaten 41, N-5007 Bergen, Norway k Department of Earth and Planetary Sciences, Northrop Hall University of New Mexico, Albuquerque, NM 87131, USA l Tianjin Institute of Geology and Mineral Resources, CGS, No. -
PERMIAN BASIN PROVINCE (044) by Mahlon M
PERMIAN BASIN PROVINCE (044) By Mahlon M. Ball INTRODUCTION The Permian Basin is one of the largest structural basins in North America. It encompasses a surface area in excess of 86,000 sq mi and includes all or parts of 52 counties located in West Texas and southeast New Mexico. Structurally, the Permian Basin is bounded on the south by the Marathon-Ouachita Fold Belt, on the west by the Diablo Platform and Pedernal Uplift, on the north by the Matador Arch, and on the east by the Eastern Shelf of the Permian (Midland) Basin and west flank of the Bend Arch. The basin is about 260 mi by 300 mi in area and is separated into eastern and western halves by a north-south trending Central Basin Platform. In cross section, the basin is an asymmetrical feature; the western half contains a thicker and more structurally deformed sequence of sedimentary rock. The Permian Basin has been characterized as a large structural depression formed as a result of downwarp in the Precambrian basement surface located at the southern margin of the North American craton. The basin was filled with Paleozoic and, to a much lesser extent, younger sediments. It acquired its present structural form by Early Permian time. The overall basin is divisible into several distinct structural and tectonic elements. They are the Central Basin Platform and the Ozona Arch, which separate the Delaware and Val Verde Basins on the south and west from the Midland Basin on the north and east, the Northwestern Shelf on the southern extremity of the Pedernal Uplift and Matador Arch, and the Eastern Shelf on the western periphery of the Bend Arch. -
Chapter 2 Paleozoic Stratigraphy of the Grand Canyon
CHAPTER 2 PALEOZOIC STRATIGRAPHY OF THE GRAND CANYON PAIGE KERCHER INTRODUCTION The Paleozoic Era of the Phanerozoic Eon is defined as the time between 542 and 251 million years before the present (ICS 2010). The Paleozoic Era began with the evolution of most major animal phyla present today, sparked by the novel adaptation of skeletal hard parts. Organisms continued to diversify throughout the Paleozoic into increasingly adaptive and complex life forms, including the first vertebrates, terrestrial plants and animals, forests and seed plants, reptiles, and flying insects. Vast coal swamps covered much of mid- to low-latitude continental environments in the late Paleozoic as the supercontinent Pangaea began to amalgamate. The hardiest taxa survived the multiple global glaciations and mass extinctions that have come to define major time boundaries of this era. Paleozoic North America existed primarily at mid to low latitudes and experienced multiple major orogenies and continental collisions. For much of the Paleozoic, North America’s southwestern margin ran through Nevada and Arizona – California did not yet exist (Appendix B). The flat-lying Paleozoic rocks of the Grand Canyon, though incomplete, form a record of a continental margin repeatedly inundated and vacated by shallow seas (Appendix A). IMPORTANT STRATIGRAPHIC PRINCIPLES AND CONCEPTS • Principle of Original Horizontality – In most cases, depositional processes produce flat-lying sedimentary layers. Notable exceptions include blanketing ash sheets, and cross-stratification developed on sloped surfaces. • Principle of Superposition – In an undisturbed sequence, older strata lie below younger strata; a package of sedimentary layers youngs upward. • Principle of Lateral Continuity – A layer of sediment extends laterally in all directions until it naturally pinches out or abuts the walls of its confining basin. -
Late Paleozoic Sea Levels and Depositional Sequences Charles A
Western Washington University Western CEDAR Geology Faculty Publications Geology 1987 Late Paleozoic Sea Levels and Depositional Sequences Charles A. Ross Western Washington University, [email protected] June R. P. Ross Western Washington University Follow this and additional works at: https://cedar.wwu.edu/geology_facpubs Part of the Geology Commons, and the Paleontology Commons Recommended Citation Ross, Charles A. and Ross, June R. P., "Late Paleozoic Sea Levels and Depositional Sequences" (1987). Geology Faculty Publications. 61. https://cedar.wwu.edu/geology_facpubs/61 This Article is brought to you for free and open access by the Geology at Western CEDAR. It has been accepted for inclusion in Geology Faculty Publications by an authorized administrator of Western CEDAR. For more information, please contact [email protected]. Cushman Foundation for Foraminiferal Research, Special Publication 24, 1987. LATE PALEOZOIC SEA LEVELS AND DEPOSITIONAL SEQUENCES CHARLES A. ROSSI AND JUNE R. P. ROSS2 1 Chevron U.S.A., Inc.,P. O. BOX 1635, Houston, TX 77251 2 Department of Biology, Western Washington University, Bellingham, WA 98225 ABSTRACT studies on these changes in sea level and their paleogeographic distribution (Ross, 1979; Ross Cyclic sea level charts for the Lower and Ross, 1979, 1981a, 1981b, 1985a, 1985b) are Carboniferous (Mississippian), Middle and Upper elaborated on in this paper with charts in a Carboniferous (Pennsylvanian), and Permian show similar format to that used for Mesozoic and considerable variability in the duration and Cenozoic sea-level cyclic fluctuations by Haq, magnitude of third-order depositional sequences, Hardenbol, and Vail (1987 and this volume). and also in the position of general sea level as represented by second-order sea level. -
Grand Canyon National Park Centennial Paleontological Resource Inventory (Non-Sensitive Version)
Grand Canyon National Park Centennial Paleontological Resource Inventory (Non-Sensitive Version) Natural Resource Report NPS/GRCA/NRR—2020/2103 Vincent L. Santucci1 and Justin S. Tweet,2 editors 1National Park Service Geologic Resources Division 1849 “C” Street, NW Washington, D.C. 20240 2National Park Service 9149 79th St. S. Cottage Grove, Minnesota 55016 March 2020 U.S. Department of the Interior National Park Service Natural Resource Stewardship and Science Fort Collins, Colorado Chapter 1. Introduction and Summary: The Paleontological Heritage of Grand Canyon National Park By Vincent L. Santucci1 1National Park Service Geologic Resources Division 1849 “C” Street, NW Washington, D.C. 20240 Throughout my life I have been bestowed the privilege of experiencing the world-renowned landscape and resources of the Grand Canyon from many perspectives and viewsheds (Figure 1-1). My first views were standing and taking photos from the many vantage points and overlooks along the North and South rims. I have enjoyed many hikes into the canyon with colleagues from the National Park Service (NPS) or with academic geologists and paleontologists. On a few occasions I ventured down and then back up the trails of the canyon with my children Sarah, Bethany, Luke, Jacob, Brianna and Abigail, often carrying one or more in my arms on the climb against gravity. I traversed by foot to the base of the canyon at Phantom Ranch and gained a greater appreciation for the geologic story preserved in the park strata. I have gazed intensely out the window of many commercial aircraft from above this geologic wonder of Earth, contemplating the geomorphic “grandeur” created over "Deep Time" and the artistry of processes perfected by “Mother Nature.” I pinch myself when I recall the opportunity when my friend Justin Tweet and I were granted permission to fly into the western portion of the Grand Canyon on a small NPS plane operated by a pilot from Lake Mead National Recreation Area. -
Paleogeographic Isolation of the Cretaceous To
Paleogeographic isolation of the Cretaceous to Eocene Sevier hinterland, east-central Nevada: Insights from U-Pb and (U-Th)/He detrital zircon ages of hinterland strata P. Druschke1,†, A.D. Hanson1, M.L. Wells1, G.E. Gehrels2, and D. Stockli3 1Department of Geoscience, University of Nevada, Las Vegas, Nevada 89154, USA 2Department of Geosciences, University of Arizona, Tucson, Arizona 85721, USA 3Department of Geology, University of Kansas, Lawrence, Kansas 66045, USA ABSTRACT cover. Early Cretaceous (ca. 135 Ma) cool- The Late Cretaceous and Paleogene Sevier ing ages are potentially coeval with shorten- hinterland of central Nevada, located west of The Late Cretaceous to Paleogene Sevier ing along the central Nevada fold-and-thrust the foreland fold-and-thrust belt, has previously hinterland of east-central Nevada is widely belt, although ca. 80 Ma cooling ages within been interpreted as a region of high-elevation regarded as an orogenic plateau that has the Sheep Pass Formation are coeval with and low topographic relief, characterized by since undergone topographic collapse. New hinter land midcrustal extension. Together, broad, open folding (Armstrong, 1968, 1972; U-Pb detrital zircon age data consisting of these new data provide support for previous Gans and Miller, 1983; Miller and Gans, 1989; 1296 analyses from the Lower Cretaceous interpretations that the Sevier hinterland DeCelles, 2004). However, Upper Cretaceous Newark Canyon Formation and the Upper represents an ancient high-elevation oro- to Lower Eocene strata of east-central Nevada Cretaceous to Eocene Sheep Pass Formation genic plateau, and that the latest Cretaceous and adjacent Utah are widely interpreted as ex- indicate that Precambrian detrital zircon locally marks a transition from contraction tensional basin deposits (Winfrey, 1958, 1960; populations recycled from local Paleozoic to extension. -
Two Stages of Late Carboniferous to Triassic Magmatism in the Strandja
Geological Magazine Two stages of Late Carboniferous to Triassic www.cambridge.org/geo magmatism in the Strandja Zone of Bulgaria and Turkey ł ń 1,2 3 1 1 Original Article Anna Sa aci ska , Ianko Gerdjikov , Ashley Gumsley , Krzysztof Szopa , David Chew4, Aleksandra Gawęda1 and Izabela Kocjan2 Cite this article: Sałacińska A, Gerdjikov I, Gumsley A, Szopa K, Chew D, Gawęda A, and 1Institute of Earth Sciences, Faculty of Natural Sciences, University of Silesia in Katowice, Będzińska 60, 41-200 Kocjan I. Two stages of Late Carboniferous to 2 3 Triassic magmatism in the Strandja Zone of Sosnowiec, Poland; Institute of Geological Sciences, Polish Academy of Sciences, Warsaw, Poland; Faculty of ‘ ’ Bulgaria and Turkey. Geological Magazine Geology and Geography, Sofia University St. Kliment Ohridski , 15 Tzar Osvoboditel Blvd., 1504 Sofia, Bulgaria 4 https://doi.org/10.1017/S0016756821000650 and Department of Geology, School of Natural Sciences, Trinity College Dublin, Dublin, Ireland Received: 9 February 2021 Abstract Revised: 3 June 2021 Accepted: 8 June 2021 Although Variscan terranes have been documented from the Balkans to the Caucasus, the southeastern portion of the Variscan Belt is not well understood. The Strandja Zone along Keywords: the border between Bulgaria and Turkey encompasses one such terrane linking the Strandja Zone; Sakar unit; U–Pb zircon dating; Izvorovo Pluton Balkanides and the Pontides. However, the evolution of this terrane, and the Late Carboniferous to Triassic granitoids within it, is poorly resolved. Here we present laser ablation Author for correspondence: – inductively coupled plasma – mass spectrometry (LA-ICP-MS) U–Pb zircon ages, coupled ł ń Anna Sa aci ska, with petrography and geochemistry from the Izvorovo Pluton within the Sakar Unit Email: [email protected] (Strandja Zone). -
The Geologic Time Scale Is the Eon
Exploring Geologic Time Poster Illustrated Teacher's Guide #35-1145 Paper #35-1146 Laminated Background Geologic Time Scale Basics The history of the Earth covers a vast expanse of time, so scientists divide it into smaller sections that are associ- ated with particular events that have occurred in the past.The approximate time range of each time span is shown on the poster.The largest time span of the geologic time scale is the eon. It is an indefinitely long period of time that contains at least two eras. Geologic time is divided into two eons.The more ancient eon is called the Precambrian, and the more recent is the Phanerozoic. Each eon is subdivided into smaller spans called eras.The Precambrian eon is divided from most ancient into the Hadean era, Archean era, and Proterozoic era. See Figure 1. Precambrian Eon Proterozoic Era 2500 - 550 million years ago Archaean Era 3800 - 2500 million years ago Hadean Era 4600 - 3800 million years ago Figure 1. Eras of the Precambrian Eon Single-celled and simple multicelled organisms first developed during the Precambrian eon. There are many fos- sils from this time because the sea-dwelling creatures were trapped in sediments and preserved. The Phanerozoic eon is subdivided into three eras – the Paleozoic era, Mesozoic era, and Cenozoic era. An era is often divided into several smaller time spans called periods. For example, the Paleozoic era is divided into the Cambrian, Ordovician, Silurian, Devonian, Carboniferous,and Permian periods. Paleozoic Era Permian Period 300 - 250 million years ago Carboniferous Period 350 - 300 million years ago Devonian Period 400 - 350 million years ago Silurian Period 450 - 400 million years ago Ordovician Period 500 - 450 million years ago Cambrian Period 550 - 500 million years ago Figure 2. -
Proto-Adamastor Ocean Crust (920 Ma) Described in Brasiliano Orogen from Coetaneous Zircon and Tourmaline
Geoscience Frontiers xxx (xxxx) xxx HOSTED BY Contents lists available at ScienceDirect China University of Geosciences (Beijing) Geoscience Frontiers journal homepage: www.elsevier.com/locate/gsf Research Paper Proto-Adamastor ocean crust (920 Ma) described in Brasiliano Orogen from coetaneous zircon and tourmaline Léo A. Hartmann a,*, Mariana Werle a, Cassiana R.L. Michelin a, Cristiano Lana b, Gláucia N. Queiroga b, Marco P. Castro b, Karine R. Arena a a Instituto de Geociências, Universidade Federal do Rio Grande do Sul, Avenida Bento Gonçalves, 9500, 91501-970, Porto Alegre, Rio Grande do Sul, Brazil b Departamento de Geologia, Escola de Minas, Universidade Federal de Ouro Preto, Morro do Cruzeiro, 35400-000, Ouro Preto, Minas Gerais, Brazil article info abstract Article history: Proto-Adamastor ocean bathed Rodinia and successor continental fragments from 1.0e0.9 Ga up to Received 25 March 2018 0.75 Ga, and evolved into world Adamastor Ocean at 0.75e0.60 Ga. Mesoproterozoic oceanic crust is Received in revised form poorly preserved on continents, only indirect evidence registered in Brasiliano Orogen. We report first 27 June 2018 evidence of ophiolite originated in proto-Adamastor. We use multi-technique U-Pb-Hf zircon and d11B Accepted 18 September 2018 tourmaline isotopic and elemental compositions. The host tourmalinite is enclosed in metaserpentinite, Available online xxx ¼þ ¼ Handling Editor: R. Damian Nance both belonging to the Bossoroca ophiolite. Zircon is 920 Ma-old, 3 Hf(920 Ma) 12, HfTDM 1.0 Ga and has ‘oceanic’ composition (e.g., U/Yb < 0.1). Tourmaline is dravite with d11B ¼þ1.8& (Tur 1), 0& (Tur 2), À & Keywords: 8.5 (Tur 3). -
The Parallels Between the End-Permian Mass Extinction And
Drawing Connections: The Parallels Between the End-Permian Mass Extinction and Current Climate Change An undergraduate of East Tennessee State University explains that humans’ current effects on the biosphere are disturbingly similar to the circumstances that caused the worst mass extinction in biologic history. By: Amber Rookstool 6 December 2016 About the Author: Amber Rookstool is an undergraduate student at East Tennessee State University. She is currently an English major and dreams of becoming an author and high school English Teacher. She hopes to publish her first book by the time she is 26 years old. Table of Contents Introduction .................................................................................................................................1 Brief Geologic Timeline ...........................................................................................................2 The Anthropocene ......................................................................................................................3 Biodiversity Crisis ....................................................................................................................3 Habitat Loss .........................................................................................................................3 Invasive Species ..................................................................................................................4 Overexploitation ...................................................................................................................4