DOCSLIB.ORG

Lithology of Evaporite Cycles and Cycle Boundaries in the Upper Part of the Paradox Formation of the Hermosa Group of Pennsylvan

Total Page：16

File Type：pdf, Size：1020Kb

Download full-text PDF Read full-text
Lithology of Evaporite Cycles and Cycle Boundaries in the Upper Part of the Paradox Formation of the Hermosa Group of Pennsylvan Lithology of Evaporite Cycles and Cycle Boundaries in the Upper Part of the Paradox Formation of the Hermosa Group of Pennsylvanian Age in the Paradox Basin, Utah and Colorado U.S. GEOLOGICAL SURVEY BULLETIN 2000-B -3 I On the Front Cover: View south toward LaSal Mountains along Colorado River between Cisco and Moab, Utah. Fisher Towers in center are composed of Permian Cutler Formation and capped by Triassic Moenkopi Formation. Prominent mesa at left center is capped by Jurassic Kayenta Formation and Wingate Sandstone and underlain by slope-forming Triassic Chinle and Moenkopi Formations. The Chinle- Moenkopi contact is marked by a thin white ledge-forming gritstone. Valley between Fisher Towers and Fisher Mesa in background is part of Richardson Amphitheater part of Professor Valley. Photograph by Omer B. Raup, U.S. Geological Survey. Lithology of Evaporite Cycles and Cycle Boundaries in the Upper Part of the Paradox Formation of the Hermosa Group of Pennsylvanian Age in the Paradox Basin, Utah and Colorado By OMER B. RAUP and ROBERT J. KITE EVOLUTION OF SEDIMENTARY BASINS PARADOX BASIN A.C. HUFFMAN, JR., Project Coordinator U.S. GEOLOGICAL SURVEY BULLETIN 2000-B A multidisciplinary approach to research studies of sedimentary rocks and their constituents and the evolution of sedimentary basins, both ancient and modern UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1992 U.S. DEPARTMENT OF THE INTERIOR MANUEL LUJAN, JR., Secretary U.S. GEOLOGICAL SURVEY Dallas L. Peck, Director For sale by the Books and Open-File Reports Section U.S. Geological Survey Federal Center, Box 25286 Denver, CO 80225 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 Library of Congress Cataloging-in-Publication Data Evolution of sedimentary basins Paradox Basin. p. cm. (U.S. Geological Survey bulletin ; 2000) Includes bibliographical references. Contents: ch. B. Lithology of evaporite cycles and cycle boundaries in the upper part of the Paradox Formation of the Hermosa Group of Pennsylvanian age in the Paradox Basin, Utah and Colorado / by Omer B. Raup and Robert J. Kite. Supt. of Docs. no.: I 19.3:2000 (v. 2) 1. Geology Paradox Basin. I. Raup, Omer B. (Omer Beaver), 1930-. II. Kite, R. J. (Robert J.) m. Series. QE75.B9 no. 2000, etc. [QE79] 552'.5 dc20 92-15577cn» CONTENTS Abstract................................................................................................................................. Bl Introduction........................................................................................................................... 1 Geologic Setting................................................................................................................... 1 Core Description................................................................................................................... 3 Delhi-Taylor Oil Company Cane Creek No. 1........................................................... 3 Delhi-Taylor Oil Company Shafer No. 1 ................................................................... 4 Evaporite Cycles................................................................................................................... 5 Lithologic Characteristics of Cycles 2 and 3 of the Paradox Formation.............................. 6 Interbeds..................................................................................................................... 6 Anhydrite (transgressive)...................................................................................... 6 Silty Dolomite (transgressive).............................................................................. 13 Black Shale........................................................................................................... 14 Dolomite (regressive)........................................................................................... 15 Anhydrite (regressive).......................................................................................... 16 Halite Beds.................................................................................................................. 18 Anhydrite Laminations......................................................................................... 21 Bromine Distribution............................................................................................ 26 Potash Deposits..................................................................................................... 29 Interbed Contact Relationships............................................................................................. 30 Detailed Correlation of Cycle 3 Interbeds Between Cane Creek No. 1 and Shafer No. 1 Core Holes ................................................................................................................... 31 Sea-Level Control During Evaporite Deposition ................................................................. 33 Summary of Evidence for Environments of Deposition of Evaporites in the Paradox Basin............................................................................................................................. 35 References Cited................................................................................................................... 36 FIGURES 1. Map of Paradox Basin, southwestern Colorado and southeastern Utah, showing limits of evaporite facies in the Paradox Formation........................................................................................................................................... B2 2-4. Schematic stratigraphic columns of: 2. Cane Creek No. 1 core hole........................................................................................................................... 4 3. Shafer No. 1 core hole................................................................................................................................... 5 4. Cycle 2 facies in Cane Creek No. 1 core....................................................................................................... 6 5. Diagram showing correlation of lithologic units in Shafer No. 1 and Cane Creek No. 1 core.............................. 7 6. Charts showing mineral composition of penesaline and clastic intervals in Cane Creek No. 1 core as determined by X-ray diffraction............................................................................................................................. 8 7-12. Photographs of polished surface of core: 7. Cane Creek No. 1, depth 2,460.5 ft............................................................................................................... 10 8. Shafer No. 1, depth 2,588 ft........................................................................................................................... 10 9. Cane Creek No. 1, depth 2,456.5 ft............................................................................................................... 11 10. Cane Creek No. 1, depth 2,455.3 ft............................................................................................................... 11 11. Shafer No. 1, depth 2,583.5 ft........................................................................................................................ 12 12. Shafer No. 1, depth 2,581.5 ft........................................................................................................................ 12 13. Photograph of segment of Cane Creek No. 1 core, depth 2,438 ft......................................................................... 14 14. Photograph of polished surface of core from Shafer No. 1 core, depth 2,569 ft.................................................... 14 15. Photomicrograph of transgressive dolomite from Cane Creek No. 1 core, depth 2,433.5 ft................................. 15 16. Photograph of polished surface of core from Shafer No. 1 core, depth 2,542 ft.................................................... 15 m IV CONTENTS 17. Photomicrograph of black shale from Cane Creek No. 1 core, depth 2,410.5 ft................................................... 16 18-24. Photographs of polished surface of cores from: 18. Shafer No. 1, depth 2,523.5 ft........................................................................................................................ 16 19. Cane Creek No. 1, depth 2,372 ft ................................................................................................................. 17 20. Shafer No. 1, depth 2,517.5 ft........................................................................................................................ 17 21. Cane Creek No. 1, depth 2,366 ft.................................................................................................................. 18 22. Cane Creek No. 1, depth 2,364.2 ft............................................................................................................... 18 23. Cane Creek No. 1, depth 2,356.7 ft .............................................................................................................. 19 24. Cane Creek No. 1, depth 2,353.7 ft............................................................................................................... 19 25. Photographs of polished surface of core from Shafer No. 1 at consecutive depths, 2,500-2,505 ft...................... 20 26-35. Photographs of segment of: 26. Cane Creek No. 1 core, depth 2,336.5 ft......................................................................................................
Load more

Recommended publications
  • Geologic Storage Formation Classification: Understanding Its Importance and Impacts on CCS Opportunities in the United States
    BEST PRACTICES for: Geologic Storage Formation Classification: Understanding Its Importance and Impacts on CCS Opportunities in the United States First Edition Disclaimer This report was prepared as an account of work sponsored by an agency of the United States Government. Neither the United States Government nor any agency thereof, nor any of their employees, makes any warranty, express or implied, or assumes any legal liability or responsibility for the accuracy, completeness, or usefulness of any information, apparatus, product, or process disclosed, or represents that its use would not infringe privately owned rights. Reference therein to any specific commercial product, process, or service by trade name, trademark, manufacturer, or otherwise does not necessarily constitute or imply its endorsement, recommendation, or favoring by the United States Government or any agency thereof. The views and opinions of authors expressed therein do not necessarily state or reflect those of the United States Government or any agency thereof. Cover Photos—Credits for images shown on the cover are noted with the corresponding figures within this document. Geologic Storage Formation Classification: Understanding Its Importance and Impacts on CCS Opportunities in the United States September 2010 National Energy Technology Laboratory www.netl.doe.gov DOE/NETL-2010/1420 Table of Contents Table of Contents 5 Table of Contents Executive Summary ____________________________________________________________________________ 10 1.0 Introduction and Background
    [Show full text]
  • L'.3350 Deposmon and DISSOLUTION of the MIDDLE DEVONIAN PRAIRIE FORMATION, Williston BASIN, NORTH DAKOTA and MONTANA By
    l'.3350 DEPOsmON AND DISSOLUTION OF THE MIDDLE DEVONIAN PRAIRIE FORMATION, WilLISTON BASIN, NORTH DAKOTA AND MONTANA by: Chris A. Oglesby T-3350 A thesis submined to the Faculty and the Board of Trustees of the Colorado School of Mines in partial fulfillment of the requirements for the degree of Master of Science (Geology). Golden, Colorado Date f:" /2 7 /C''i::-- i ; Signed: Approved: Lee C. Gerhard Thesis Advisor Golden, Colorado - 7 Date' .' Samuel S. Adams, Head Department of Geology and Geological Engineering II T-3350 ABSTRACf Within the Williston basin, thickness variations of the Prairie Formation are common and are interpreted to originate by two processes, differential accumulation of salt during deposition, and differential removal of salt by dissolution. Unambiguous evidence for each process is rare because the Prairie/Winnipegosis interval is seldom cored within the U.S. portion of the basin. Therefore indirect methods, utilizing well logs, provide the principal method for identifying characteristics of the two processes. The results of this study indicate that the two processes can be distinguished using correlations within the Prairie Formation. Several regionally correlative upward-brining, and probably shoaling-upward sequences occur within the Prairie Formation .. Near the basin center, the lowermost sequence is transitional with the underlying Winnipegosis Formation. This transition is characterized by thinly laminated carbonates that become increasingly interbedded with anhydrites of the basin-centered Ratner Member, the remainder of the sequence progresses up through halite and culminates in the halite-dominated Esterhazy potash beds. Two overlying sequences also brine upwards, however, these sequences lack the basal anhydrite and instead begin with halite and culminate in the Belle Plaine and Mountrail potash Members, respectively.
    [Show full text]
  • 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.
    [Show full text]
  • The Arabian Gulf
    Chapter 1 The Arabian Gulf Grace O. Vaughan, Noura Al-Mansoori, John A. Burt New York University Abu Dhabi, Abu Dhabi, United Arab Emirates 1.1 THE REGION Bound by deserts and located between the north-eastern Arabian Peninsula and Iran, the Arabian Gulf (also known as the Persian Gulf, and hereafter known as “the Gulf”) is bordered by eight rapidly developing nations. The Gulf is located in the subtropics between 24°N and 30°N latitude and 48°E and 57°E longitude (Fig. 1.1), and is considered as a biogeographic subprovince of the northwestern Indian Ocean (Spalding et al., 2007). During summers, the Gulf is the hottest sea on the planet, particularly in the shallow southern basin where sea surface temperatures (SSTs) regu- larly exceed 35°C in August. Sea temperatures are also highly variable among seasons, ranging over 20°C between summer and winter. Geologically, the Gulf is relatively young with coastlines that formed only in the past 3000–6000 years when polar ice sheets receded (Riegl & Purkis, 2012a). Today, the Gulf is bordered to the northeast by the Zagros mountains in Iran and the Hajar mountains in the Musandam peninsula and in the southwest by the sedimentary Arabian coast (Purser & Seibold, 1973). Presently, it covers an area of 250,000 km2 (Riegl & Purkis, 2012a). Generally, terrestrial systems sur- rounding the Gulf are arid to hyperarid (Riegl & Purkis, 2012a), limiting the input of freshwater to this semienclosed sea. The main freshwater input enters at the northern Gulf at the Shatt Al Arab waterway through the Tigris, Euphrates, and the Karun rivers (Sheppard, Price, & Roberts, 1992), although recent damming efforts have resulted in substantial reductions in freshwater discharge from these rivers (Sheppard et al., 2010).
    [Show full text]
  • Non-Clastic Sedimentary Rocks by Cindy Grigg
    Non-Clastic Sedimentary Rocks By Cindy Grigg 1 Rocks can be put into three main groups. They are grouped by how the rocks formed. Sedimentary (sed-uh-MEN-tuh-ree) rocks are formed on or near Earth's surface. Sedimentary rocks are sorted into other groups. They can be sorted as clastic or non-clastic. This group tells something about the rocks' beginning and what they formed from. 2 Non-clastic rocks are created when water evaporates or from the remains of plants and animals. Limestone is a non-clastic sedimentary rock. Limestone is made of the mineral calcite. It often contains fossils. Limestone formed in the ocean from the shells and skeletons of dead sea creatures. Some of the fossils in limestone are too small to be seen without a microscope. Chalk is a type of limestone that is usually white. It consists almost entirely of the shells of tiny dead sea creatures. Limestone is a common building material. 3 Coal is another non-clastic rock. It formed from the dead remains of plants. Millions of years ago, plants fell into swamps. They were covered with layers of sediment and did not rot. Over millions of years, as the remains were buried deeper under more and more layers of sediment, they were changed by pressure into coal. Coal is commonly used as fuel in power plants to make electricity. 4 Evaporite rocks formed when minerals such as gypsum and halite (rock salt) were left behind as water evaporated from oceans and lakes. Evaporite is common in desert areas, where evaporation is high, such as the Great Salt Lake in Utah.
    [Show full text]
  • National Evaporite Karst--Some Western Examples
    122 National Evaporite Karst--Some Western Examples By Jack B. Epstein U.S. Geological Survey, National Center, MS 926A, Reston, VA 20192 ABSTRACT Evaporite deposits, such as gypsum, anhydrite, and rock salt, underlie about one-third of the United States, but are not necessarily exposed at the surface. In the humid eastern United States, evaporites exposed at the surface are rapidly removed by solution. However, in the semi-arid and arid western part of the United States, karstic features, including sinkholes, springs, joint enlargement, intrastratal collapse breccia, breccia pipes, and caves, locally are abundant in evaporites. Gypsum and anhydrite are much more soluble than carbonate rocks, especially where they are associated with dolomite undergoing dedolomitization, a process which results in ground water that is continuously undersaturated with respect to gypsum. Dissolution of the host evaporites cause collapse in overlying non-soluble rocks, including intrastratal collapse breccia, breccia pipes, and sinkholes. The differences between karst in carbonate and evaporite rocks in the humid eastern United States and the semi-arid to arid western United States are delimited approximately by a zone of mean annual precipitation of 32 inches. Each of these two rock groups behaves differently in the humid eastern United States and the semi-arid to arid west. Low ground-water tables and decreased ground water circulation in the west retards carbonate dissolution and development of karst. In contrast, dissolution of sulphate rocks is more active under semi-arid to arid conditions. The generally thicker soils in humid cli- mates provide the carbonic acid necessary for carbonate dissolution. Gypsum and anhydrite, in contrast, are soluble in pure water lacking organic acids.
    [Show full text]
  • Part 629 – Glossary of Landform and Geologic Terms
    Title 430 – National Soil Survey Handbook Part 629 – Glossary of Landform and Geologic Terms Subpart A – General Information 629.0 Definition and Purpose This glossary provides the NCSS soil survey program, soil scientists, and natural resource specialists with landform, geologic, and related terms and their definitions to— (1) Improve soil landscape description with a standard, single source landform and geologic glossary. (2) Enhance geomorphic content and clarity of soil map unit descriptions by use of accurate, defined terms. (3) Establish consistent geomorphic term usage in soil science and the National Cooperative Soil Survey (NCSS). (4) Provide standard geomorphic definitions for databases and soil survey technical publications. (5) Train soil scientists and related professionals in soils as landscape and geomorphic entities. 629.1 Responsibilities This glossary serves as the official NCSS reference for landform, geologic, and related terms. The staff of the National Soil Survey Center, located in Lincoln, NE, is responsible for maintaining and updating this glossary. Soil Science Division staff and NCSS participants are encouraged to propose additions and changes to the glossary for use in pedon descriptions, soil map unit descriptions, and soil survey publications. The Glossary of Geology (GG, 2005) serves as a major source for many glossary terms. The American Geologic Institute (AGI) granted the USDA Natural Resources Conservation Service (formerly the Soil Conservation Service) permission (in letters dated September 11, 1985, and September 22, 1993) to use existing definitions. Sources of, and modifications to, original definitions are explained immediately below. 629.2 Definitions A. Reference Codes Sources from which definitions were taken, whole or in part, are identified by a code (e.g., GG) following each definition.
    [Show full text]
  • S40645-019-0306-X.Pdf
    Isaji et al. Progress in Earth and Planetary Science (2019) 6:60 Progress in Earth and https://doi.org/10.1186/s40645-019-0306-x Planetary Science RESEARCH ARTICLE Open Access Biomarker records and mineral compositions of the Messinian halite and K–Mg salts from Sicily Yuta Isaji1* , Toshihiro Yoshimura1, Junichiro Kuroda2, Yusuke Tamenori3, Francisco J. Jiménez-Espejo1,4, Stefano Lugli5, Vinicio Manzi6, Marco Roveri6, Hodaka Kawahata2 and Naohiko Ohkouchi1 Abstract The evaporites of the Realmonte salt mine (Sicily, Italy) are important archives recording the most extreme conditions of the Messinian Salinity Crisis (MSC). However, geochemical approach on these evaporitic sequences is scarce and little is known on the response of the biological community to drastically elevating salinity. In the present work, we investigated the depositional environments and the biological community of the shale–anhydrite–halite triplets and the K–Mg salt layer deposited during the peak of the MSC. Both hopanes and steranes are detected in the shale–anhydrite–halite triplets, suggesting the presence of eukaryotes and bacteria throughout their deposition. The K–Mg salt layer is composed of primary halites, diagenetic leonite, and primary and/or secondary kainite, which are interpreted to have precipitated from density-stratified water column with the halite-precipitating brine at the surface and the brine- precipitating K–Mg salts at the bottom. The presence of hopanes and a trace amount of steranes implicates that eukaryotes and bacteria were able to survive in the surface halite-precipitating brine even during the most extreme condition of the MSC. Keywords: Messinian Salinity Crisis, Evaporites, Kainite, μ-XRF, Biomarker Introduction hypersaline condition between 5.60 and 5.55 Ma (Manzi The Messinian Salinity Crisis (MSC) is one of the most et al.
    [Show full text]
  • 1469 Vol 43#5 Art 03.Indd
    1469 The Canadian Mineralogist Vol. 43, pp. 1469-1487 (2005) BORATE MINERALS OF THE PENOBSQUIS AND MILLSTREAM DEPOSITS, SOUTHERN NEW BRUNSWICK, CANADA JOEL D. GRICE§, ROBERT A. GAULT AND JERRY VAN VELTHUIZEN† Research Division, Canadian Museum of Nature, P.O. Box 3443, Station D, Ottawa, Ontario K1P 6P4, Canada ABSTRACT The borate minerals found in two potash deposits, at Penobsquis and Millstream, Kings County, New Brunswick, are described in detail. These deposits are located in the Moncton Subbasin, which forms the eastern portion of the extensive Maritimes Basin. These marine evaporites consist of an early carbonate unit, followed by a sulfate, and fi nally, a salt unit. The borate assemblages occur in specifi c beds of halite and sylvite that were the last units to form in the evaporite sequence. Species identifi ed from drill-core sections include: boracite, brianroulstonite, chambersite, colemanite, congolite, danburite, hilgardite, howlite, hydroboracite, kurgantaite, penobsquisite, pringleite, ruitenbergite, strontioginorite, szaibélyite, trembathite, veatchite, volkovskite and walkerite. In addition, 41 non-borate species have been identifi ed, including magnesite, monohydrocalcite, sellaite, kieserite and fl uorite. The borate assemblages in the two deposits differ, and in each deposit, they vary stratigraphically. At Millstream, boracite is the most common borate in the sylvite + carnallite beds, with hilgardite in the lower halite strata. At Penobsquis, there is an upper unit of hilgardite + volkovskite + trembathite in halite and a lower unit of hydroboracite + volkov- skite + trembathite–congolite in halite–sylvite. At both deposits, values of the ratio of B isotopes [␦11B] range from 21.5 to 37.8‰ [21 analyses] and are consistent with a seawater source, without any need for a more exotic interpretation.
    [Show full text]
  • Ancient Potash Ores
    www.saltworkconsultants.com John Warren - Friday, Dec 31, 2018 BrineSalty evolution Matters & origins of pot- ash: primary or secondary? Ancient potash ores: Part 3 of 3 Introduction Crossow of In the previous two articles in this undersaturated water series on potash exploitation, we Congruent dissolution looked at the production of either Halite Mouldic MOP or SOP from anthropo- or Porosity genic brine pans in modern saline sylvite lake settings. Crystals of interest formed in solar evaporation pans Dissolved solute shows stoichiometric match to precursor, and dropped out of solution as: dissolving salt goes 1) Rafts at the air-brine interface, A. completely into solution 2) Bottom nucleates or, 3) Syn- depositional cements precipitated MgCl in solution B. 2 within a few centimetres of the Crossow of depositional surface. In most cases, undersaturated water periods of more intense precipita- Incongruent dissolution tion tended to occur during times of brine cooling, either diurnally Carnallite Sylvite or seasonally (sylvite, carnallite and halite are prograde salts). All Dissolved solute does not anthropogenic saline pan deposits stoichiometrically match its precursor, examples can be considered as pri- while the dissolving salt goes partially into solution and a mary precipitates with chemistries new daughter mineral remains tied to surface or very nearsurface Figure 1. Congruent (A) versus incongruent (B) dissolution. brine chemistry. In contrast, this article discusses the Dead Sea and the Qaidam sump most closely resemble ancient potash deposits where the post-deposition chem- those of ancient MgSO4-depleted oceans, while SOP fac- istries and ore textures are responding to ongoing alter- tories in Great Salt Lake and Lop Nur have chemistries ation processes in the diagenetic realm.
    [Show full text]
  • Origin of Intraformational Folds in the Jurassic Todilto Limestone, Ambrosia Lake Uranium Mining District, Mckinley and Valencia Counties, New Mexico by Morris W
    DEPARTMENT OF THE INTERIOR GEOLOGICAL SURVEY Origin of Intraformational Folds in the Jurassic Todilto Limestone, Ambrosia Lake Uranium Mining District, McKinley and Valencia Counties, New Mexico By Morris W. Green U.S. Geological Survey Open-file Report 82-69 1982 Contents Page Abstract................................................................ 1 Introducti on............................................................ 3 Stratigraphy and Environments of Deposition.............................3 The Formation of Intraformational Folds................................10 Todilto Uranium Deposits...............................................22 Exploration and Favorability...........................................24 References ci ted....................................................... 25 Illustrations Figure 1. Index map showing location of mineral belt, the Todilto study area, and adjacent areas.....................4 2. Index map of the Ambrosia Lake mining area...................5 3. Schematic diagram showing a segment of the Todilto depositional basin.........................................9 4. Remnants of a Summerville (Js) eolian dune overlying the Todilto Limestone (Jt)................................12 5. Schematic diagram showing the plastic and shear phases of Todilto load deformation...............................13 6. Large-scale, low amplitude intraformational fold within the Todilto Limestone.....................................14 7. Large-scale, high amplitude, intraformational fold within the Todilto Limestone..............................14
    [Show full text]
  • Coral Reefs Within a Siliciclastic Setting, 1997
    Proc 8th Int Coral Reef Sym 2:1737-1742.1997 CORAL REEFS AND CARBONATE PLATFORMS WITHIN A SILICICLASTIC SETTING. GENERAL ASPECTS AND EXAMPLES FROM THE LATE JURASSIC OF PORTUGAL. Reinhold Leinfelder Institute of Geology and Paleontology, University of Stuttgart, Herdweg 51, D-70174 Stuttgart, Germany. ABSTRACT in the water (op. cit.). Additionally, terrigeneous influx is mostly accompanied by an unfavourable increase Both in the Modern and Ancient examples coral reefs and in nutrient and sometimes even freshwater influx. carbonate platforms occur frequently very close to or even directly within areas of siliciclastic sediment- ation. Particularly fine grained, often suspended terri- geneous influx is mostly problematic for the reef fauna due to lowering of illumination and oxygenation, in- TableÊ1: Possible negative effects of terrigeneous creasing nutrient values or directly settling on the influx on reefs: organims. The modern examples show that reef growth in such settings is only possible by the existence of sheltering mechanisms such as arid climate, structural REEFS AND SILICS? WHAT'S BAD ABOUT IT? and sedimentary traps or longshore currents. If not completely effective, reefs may still prosper under 1 . Increase of nutrient concentration reduced but noticeable siliciclastic sedimentation, but 2 . Freshwater influx both composition and diversity of the reefs changes drastically. The Ancient examples show that temporal 3 . Reduction of oxygen concentration relations are important as well: Autocyclic switches in 4 . Impoverished illumination depositional systems and especially allocyclic events 5 . Loss of hard substrates such as tectonic activation/deactivation or sea level 6 . Pollution / suffocation of reef organisms change may open and close reef windows through time.
    [Show full text]