GEOL-106_Lecture_[08]_Paleozoic_Earth

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PALEOZOIC EARTH HISTORY GEOL106 Chapter 20
251 Ma 542 Ma Paleozoic
Introduction In 1815, William Smith, a canal builder, published the world’s first geologic map. His hand-painted map represented over 20 years of work.
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Introduction England is rich in geologic history. Development of geology proceeded rapidly with the naturalists of the 19th century. The Paleozoic history is well represented there, involving several episodes of mountain building and sea level changes, mostly related to plate tectonics and glaciation.
Continental Architecture: Cratons and MobileBelts Most continents consist of two major components: 1. relatively stable craton over which epeiric seas transgressed and regressed 2. surrounded by mobile belts in which mountain building took place Fig. 20.1, p. 505
Continental Architecture: Cratons and MobileBelts Epeiric seas – shallow seas covering part of the craton Mobile belts – elongate areas of mountain building, primarily created during plate convergence Fig. 20.1, p. 505
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Continental Architecture: Cratons and MobileBelts Mobile Belts: orogenic activity • Cordillera • Appalachian • Ouachita • Franklin Fig. 20.1, p. 505
Question: An elongated area marking the site of mountain building is a _________. A. Platform B. Shield C. Mobile belt D. Craton
Paleozoic Paleogeography Baltica, China, Gondwana, Kazakstania, Laurentia and Siberia Fig. 20.2a, p. 506 Six major continents existed at the beginning of the Paleozoic Era. Four were located near the paleoequator 510 Ma
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510 Ma Fig. 20.2a, p. 506
Paleozoic Paleogeography Early-Middle Paleozoic Global History During the Early Paleozoic (Cambrian-Silurian): ◼ Laurentia was moving northward and ◼ Gondwana moved to a south polar location, as indicated by tillite deposits 51 Ma 510 Ma Fig. 20.2a, p. 506
Paleozoic Paleogeography Late Paleozoic Global History During the Late Paleozoic (Devonian – Permian): Baltica and Laurentia collided to form Laurasia. Siberia and Kazakhstania collided and finally were sutured to Laurasia. 350 Ma Fig. 20.3b, p. 508
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Fig. 20.3b, p. 508 350 Ma Paleozoic Paleogeography
Paleozoic Paleogeography Late Paleozoic Global History During the Late Paleozoic (Devonian – Permian): Gondwana, at the South Pole, experienced several glacial-interglacial periods, resulting in global sea- level changes and transgressions and regressions along the low-lying craton margins. Fig. 20.3b, p. 508
Paleozoic Paleogeography Late Paleozoic Global History Laurasia and Gondwana underwent a series of collisions beginning in the Carboniferous . During the Permian, the formation of Pangaea was completed. Surrounding the supercontinent was a global ocean, Panthalassa . Fig. 20.4b, p. 510
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250 Ma Fig. 20.4b, p. 510
• Why late Paleozoic Era is called Carboniferous period? → Large underground coal deposits formed at that time. Mainly formed in the equatorial regions where rainfall was high and temperatures were consistently warm.
Statement: The bulk of the coal driving the Industrial Revolution and contributing to global warming today has been deposited during the Carboniferous period (359 – 299 million years ago). A. True B. False
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Paleozoic Evolution of NorthAmerica The geologic history of North America can be divided into cratonic sequences that reflect craton-wide sea transgressions and regressions . Fig. 20.5, p. 511 There are 6 cratonic sequences recognized in NorthAmerica.
Paleozoic Evolution of NorthAmerica Transgression Regression
Paleozoic Evolution of NorthAmerica The study of cratonic sequences done through sequence stratigraphy. In sequence stratigraphy rocks are studied within a time-stratigraphic framework related to facies and bounded by unconformities . Fig. 20.5, p. 511
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The white areas represent sequences of rocks separated by large-scale unconformities (brown areas). The major Cordilleran orogenies are shown on the left side, and the major Appalachian orogenies are on the right. Fig. 20.5, p. 511 Cratonic sequences of North America.
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Fig. 20.5, p. 511 The white areas represent sequences of rocks separated by large-scale unconformities (brown areas). The major Cordilleran orogenies are shown on the left side, and the major Appalachian orogenies are on the right. Cratonic sequences of North America.
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Paleozoic Evolution of NorthAmerica The Sauk Sequence
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The Sauk Sequence Neoproterozoic – Early Ordovician: The Sauk Sea was the first major sequence to transgress onto the North Americancraton. Fig. 20.7, p. 513
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The Sauk Sequence During the transgressive portions of each cycle, the North American craton was partially to completely covered by shallow seas in which a variety of clastic and carbonate sediments were deposited. Fig. 20.7, p. 513
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The Sauk Sequence At its maximum during the Late Cambrian, a sea covered the craton except for parts of the Canadian Shield and the TranscontinentalArch. Transcontinental Arch - a series of large, northeast- southwest trending islands. Fig. 20.6, p. 512
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Cambrian Paleogeography of NorthAmerica Fig. 20.6, p. 512
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The Sauk Sequence Is this sequence a - Regression? - Transgression?
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The Sauk Sequence Redwall Ls Muav Ls Bright Angel Sh Tapeats Ss
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The Sauk Sequence What are clean, mature sandstones? Mostly quartz (up to 99%) Grains well rounded and well sorted
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The Sauk Sequence Where were the sandstones deposited? A lot of trace fossils: shallow water
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The Sauk Sequence At height of transgression Little land remained No more terrigenous input Limestones form in shallow, clear, warm water ◼ Shell debris ◼ Ooids/Oolites: onion-like, sand-sized grains of carbonate precipitated in shallow, warm water
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The Sauk Sequence Oolites
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Oolithic Limestone
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Modern Oolites: Bahamas!
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The Sauk Sequence How deep was the Sauk Sea? Stromatolites widespread ◼ Need light for photosynthesis ◼ Not deeper than 200 m ◼ Indicative of sea level Stromatolites in the Hoyt Limestone (Cambrian) exposed at Lester Park, near Saratoga Springs, NY
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The Sauk Sequence How deep was the Sauk Sea? Mudcracks common ◼ Very shallow, exposure to atmosphere
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The end of the Sauk Sequence Sauk Sea regressed from craton during Early Ordovician (505 Ma) Exposed limestones deeply eroded in tropical environment Large unconformity marks the boundary between Sauk and Tippecanoe
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The end of the Sauk Sequence 6 continents around equator, Ice-free poles, Continents drowned
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Question: Carbonates from Sauk sequence contains ________ A. fragments of shells B. stromatolites C. oolitic textures D. all of the above
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Paleozoic Evolution of NorthAmerica The Tippecanoe Sequence
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The white areas represent sequences of rocks separated by large-scale unconformities (brown areas). The major Cordilleran orogenies are shown on the left side, and the major Appalachian orogenies are on the right. Fig. 20.5, p. 511 Cratonic sequences of North America.
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The Tippecanoe Sequence Fig. 20.8, p. 514 The Tippecanoe sequence began with deposition of an extensive sandstone over the eroded Sauk. Major transgression onto craton Clean, well-sorted quartz sand deposited over most of the craton ◼ St. Peter Sandstone ◼ glass manufacturing Tippecanoe - Middle Ordovician – Early Devonian
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The Tippecanoe Sequence Tippecanoe sandstone followed by carbonates deposited in shallow (epeiric) seas Tippecanoe - Middle Ordovician – Early Devonian Fig. 20.8, p. 514
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The Tippecanoe Sequence Reefs, chemical precipitates, and fossil fragments Fossils: Brachiopods, bryozoans, crinoids, cephalopods, corals, algae Tippecanoe - Middle Ordovician – Early Devonian
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Ordovician Paleogeography of NorthAmerica Fig. 20.10, p. 514
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The Tippecanoe Sequence In the Middle-Late Silurian, large barrier reefs enclosed basins, resulting in evaporite deposition within these basins. Tippecanoe - Middle Ordovician – Early Devonian Fig. 20.10, p. 516
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Tippecanoe Reefs Fig. 20.9, p. 515
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The Tippecanoe Sequence Reefs : limestone structures constructed by living organisms Various reef-building organisms ◼ Archaeocyathids (Cambrian) ◼ Stromatoporoids ◼ Corals (today) Warm, clear, shallow water Constricted to 30 ° N and S
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The Tippecanoe Sequence Archaeocyathids : calcareous sponges
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The Tippecanoe Sequence Stromatoporoids
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The Tippecanoe Sequence Corals (Rugosa)
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The Tippecanoe Sequence Reefs in the Michigan Basin restricted the flow of sea water and allowed excessive evaporation to precipitate salt deposits (evaporites). ◼ 1500 m of sediment, half of this is anhydrite and halite Fig. 20.10, p. 516
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Fig. 20.12, p. 520
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Artificial salt ponds
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Stromatoporoid barrier reef Stromatolites Algal Coral algal Crinoidal Clinton Formation Niagara Formation Carbonate Laminar stromatoporoid Anhydrite Halite Evaporite Barrier reef Pinnacle reef Laminar stromatoporoid Fig. 20-11, p. 517 SteppedArt Cross section of a stromatoporoid colony fromthe stromatoporoid barrier reef facies. Limestone from the carbonate facies. Core of rock salt from the evaporite facies.
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The Tippecanoe Sequence By early Devonian, the Tippecanoe Sea had regressed to the cratonic margin, exposing extensive low-lands. Mild warping of the craton produced many domes, arches and basins in North America. Most of these were eroded down by the time a new sea, the Kaskaskia, transgressed . The End of the Tippecanoe Sequence Fig. 20.1, p. 505
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Fig. 20.1, p. 505
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Paleozoic Evolution of NorthAmerica The Kaskaskia Sequence
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The white areas represent sequences of rocks separated by large-scale unconformities (brown areas). The major Cordilleran orogenies are shown on the left side, and the major Appalachian orogenies are on the right. Fig. 20.5, p. 511 Cratonic sequences of North America.
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The Kaskaskia Sequence The basal beds of the Kaskaskia sequence deposited on the exposed Tippecanoe surface were either: sandstones that formed from sands derived from the eroding Acadian Highlands or Carbonates (reefs) Black shales Fig. 20.13, p. 521 Kaskaskia Sequence - Middle Devonian – Late
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The Kaskaskia Sequence The Kaskaskia sequence begin with clean quartz sands on erosional unconformity Oriskany sandstone Glass manufacturing Fig. 20.13, p. 521 Kaskaskia Sequence - Middle Devonian – Late
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Devonian Paleogeography of NorthAmerica Fig. 20.13, p. 521
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The Kaskaskia Sequence Fig. 20.14, p. 522 Middle to Late Devonian Reef Development in Western Canada Most of the Kaskaskia sequence is dominated by carbonates and associated evaporites . Half the world’s potash (fertilizer) comes from Devonian evaporites
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The Kaskaskia Sequence Fig. 20.14, p. 522 Middle to Late Devonian Reef Development in Western Canada The Devonian Period was a time of major reef building . ◼ Important petroleum reservoirs A large barrier reef system restricted the flow of oceanic water, creating conditions for evaporite precipitation .
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Devonian Reef in the Canadian Rockies Back-reef Fore-reef
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The Kaskaskia Sequence Black Shales Widespread black shales were deposited over large areas of the craton during the Late Devonian and Early Mississippian. Chattanooga Shale – ◼ Thin-bedded ◼ Highly-radioactive (uranium-rich) ◼ Source rock for oil and gas Fig. 20.15, p. 522
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The Kaskaskia Sequence Black Shales Origin highly debated Probable depositional environment: ◼ Undisturbed anaerobic bottom waters ◼ Reduced supply of coarse sediment ◼ High organic productivity in overlying waters Fig. 20.15, p. 522
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The Kaskaskia Sequence Fig. 20.16, p. 523 The Late Kaskaskia - A Return toExtensive Carbonate Deposition The Mississippian Period was dominated for the most part by carbonate deposition. The broad Kaskaskian epeiric sea covered most of NorthAmerica.
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Mississippian Paleogeography of North America Fig. 20.16, p. 523
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Question: At the beginning of Kaskaskia sequence, which type of deposition occurred? A. Sandstones B. Carbonates C. Black Shales
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Paleozoic Evolution of NorthAmerica The Absaroka Sequence
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Fig. 20.5, p. 511 The white areas represent sequences of rocks separated by large-scale unconformities (brown areas). The major Cordilleran orogenies are shown on the left side, and the major Appalachian orogenies are on the right. Cratonic sequences of North America.
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The Absaroka Sequence Late Mississippian - Jurassic Significant unconformity Sediments effected by formation of the Appalachians and Ouachita mountain belts Alternating marine and nonmarine sediments Absaroka Sequence - Pennsylvanian – Early Fig. 20.17, p. 524 ss
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The Absaroka Sequence What Are Cyclothems and Why Are They Important? Group of beds recording a single advance and retreat of the sea 50 cylothems in Missouri and Kansas Cyclic advance and retreat of sea over shallow land Absaroka Sequence - Pennsylvanian – Early Fig. 20.17, p. 524 ra
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The Absaroka Sequence What Are Cyclothems and Why Are They Important? Pennsylvanian Period Gondwanan ice sheets were probably responsible for multiple transgressions and regressions of sea level over the low-lying Absaroka Sequence - Pennsylvanian – Early North American craton. Fig. 20.17, p. 524 ra
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Cyclothems Fig. 20.18, p. 525
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Cyclothems Fig. 20.18, p. 525
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The Absaroka Sequence What Are Cyclothems and Why Are They Important? The transgressions and regressions resulted in: ◼ cyclothems and ◼ the formation of coal swamps Absaroka Sequence - Pennsylvanian – Early Fig. 20.17, p. 524
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Question: What is economically valuable deposit in a cyclothem? A. Metallic ore B. Carbonate C. Coal D. Gravel
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Question: In a Cyclothem, marine fossils represent the time of __________. A. Early Transgression B. Late Transgression C. Late regression D. Late Transgression and Early Regression
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The Absaroka Sequence Cratonic mountain building, specifically the Ancestral Rockies , occurred during the Pennsylvanian Period. Resulted in thick nonmarine detrital rocks and evaporites being deposited in the intervening basins. Cratonic Uplift — The Ancestral Rockies Fig. 20.19, p. 527
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Garden of the Gods, Colorado Springs
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Statement: Formation of Ancestral Rockies are influenced by the existence of faults in the southwestern part of North American craton. A. True B. False
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The Absaroka Sequence The Late Absaroka — More Evaporite Deposits and Reefs By the Early Permian, the Absaroka Sea occupied a narrow zone of the south central craton. Here, several large reefs and associated evaporites developed. By the end of the Permian Period, the Absaroka Sea had retreated from the craton. Fig. 20.22, p. 529 Fig. 20.23, p. 529
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Permian Paleogeography of NorthAmerica Fig. 20.20, p. 528
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Permian Reef El Capitan, Guadalupe National Park (Texas)
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History of the Paleozoic Mobile Belts
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History of the Paleozoic Mobile Belts Cordilleran MB Appalachian MB Ouachita MB
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Fig. 20.5, p. 511 The white areas represent sequences of rocks separated by large-scale unconformities (brown areas). The major Cordilleran orogenies are shown on the left side, and the major Appalachian orogenies are on the right. Cratonic sequences of North America.
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History of the Paleozoic Mobile Belts Appalachian Mobile Belts
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History of the Paleozoic Mobile Belts Mountain-building activity took place primarily along the eastern and southern margins (known as mobile belts) of the North American craton during the Paleozoic Era. Appalachian Mobile Belt Several orogenies occurred in the Appalachian belt during the Paleozoic: ◼ Taconic ◼ Caledonian (Europe) ◼ Acadian ◼ Hercynian-Alleghenian
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History of the Paleozoic Mobile Belts Throughout Sauk time (Neoproterozoic to Late Ordovician), the Appalachian region was a broad , passive continental margin. Continental shelf deposits Sandstone and limestone Appalachian Mobile Belt: Taconic Orogeny Fig. 20.24a, p. 530
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History of the Paleozoic Mobile Belts During Sauk time, a divergent boundary existed along the eastern side of Laurentia widening the Iapetus Ocean. Appalachian Mobile Belt: Taconic Orogeny Fig. 20.24a, p. 530
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History of the Paleozoic Mobile Belts 510 Ma (Cambrian)
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History of the Paleozoic Mobile Belts 450 Ma (Late Ordovician)
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History of the Paleozoic Mobile Belts 410 Ma (Early Devonian)
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History of the Paleozoic Mobile Belts In the mid-Ordovician, carbonate deposition ceased and was replaced by deepwater black shales, graywackes and volcanics , marking the development of a subduction zone and the beginning of the orogeny. Appalachian Mobile Belt: Taconic Orogeny Fig. 20.24b, p. 530
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History of the Paleozoic Mobile Belts Subduction of Iapetus ocean Taconic Highlands erode, build up clastic wedge: Queenston Delta Appalachian Mobile Belt: Taconic Orogeny Fig. 20.24b, p. 530
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History of the Paleozoic Mobile Belts Fig. 20.25, p. 531 Evidence for Taconic Orogeny Volcanic activity Metamorphism and igneous intrusions ◼ Radiometric ages: 440- 480 Ma Clastic wedge ◼ Queenston delta, a thick sandstone deposit, thinning away from the Taconic mountains. Appalachian Mobile Belt: Taconic Orogeny
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History of the Paleozoic Mobile Belts The Queenston wedge represents a delta that formed from the erosion of the Taconic Highlands mountain belt in eastern New York, central Massachusetts and Vermont. Appalachian Mobile Belt: Taconic Orogeny Fig. 20.25, p. 531
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History of the Paleozoic Mobile Belts The Caledonian mobile belt is the European equivalent of the Taconic mobile belt, forming the western border of Baltica facing the Iapetus Ocean. The orogeny peaked during the Late Silurian and Early Devonian. Fig. 20.24b, p. 530 Appalachian Mobile Belt: Caledonian Orogeny
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Statement: Taconic and Caledonian orogeny was related to the closing or subduction of Iapetus ocean. A. True B. False
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History of the Paleozoic Mobile Belts Acadian Orogeny: Devonian Occurred along a convergent oceanic-continental boundary between Laurentia and Baltica during the Late Silurian into the Devonian. Marks the continental-continental collision during the Devonian. The closing of the Iapetus Ocean ended by forming a new continent called Laurasia . Fig. 20.26, p. 531 Appalachian Mobile Belt: Acadian Orogeny
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History of the Paleozoic Mobile Belts Evidence ofAcadian Orogeny Metamorphic and igneous rocks ◼ Radiometric age: 360-410 Ma Fig. 20.26, p. 531 Appalachian Mobile Belt: Acadian Orogeny
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History of the Paleozoic Mobile Belts Evidence ofAcadian Orogeny Catskill Delta clastic wedge Formed on the west side, Weathering of Catskill Mountains This delta contains conglomerates, sandstones and shales. Fig. 20.26, p. 531 Appalachian Mobile Belt: Acadian Orogeny
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Point bar deposits in the Catskill Formation (Devonian) near North Bend, PA. Catskill Delta clastic wedge
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History of the Paleozoic Mobile Belts The Catskill clastic wedge has a European counterpart in the Old Red Sandstone. The Old Red Sandstone formed from the clastics of the Caledonian Highlands, and spread eastward onto the Baltica craton in the Devonian. It is famous, as is the Catskill Delta, for its freshwater fish and early amphibian fossils, as well as early land plants. Fig. 20.26, p. 531 The Old Red Sandstone
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Lower Old Red Sandstone sedimentary rocks, including conglomerate, of the Arbuthnott-Garvock Group, of early Devonian age (Lokhovian to Pragian) at Auchmithie in Scotland. Old Red Sandstone
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Fish fossils from the Old Red Sandstone
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History of the Paleozoic Mobile Belts Taconic Orogeny: Ordovician Island arc Acadian Orogeny: Devonian Avalon, Baltica Hercynian-Alleghenian Orogeny Gondwana (Africa and South America) converged with Laurasia
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History of the Paleozoic Mobile Belts Taconic, Caledonian, and Acadian orogenies : all related to the closing of the Iapetus Ocean and the formation of Laurasia. The Hercynian mobile belt in Europe and the Alleghenian mobile belt (Appalachian) in North America mark the zone where Laurasia collided with Gondwana. The Hercynian-Alleghenian orogeny begins at its north end in Mississippian time and slowly moves to the south suturing together the continents as it goes. Appalachian Mobile Belt: Hercynian Alleghenian Orogeny
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History of the Paleozoic Mobile Belts The first continent-continent collision in the Mississippian is between eastern Laurasia and Gondwana - Hercynian Orogeny (Mississippian-Permian). Fig. 20.3b, p. 508 Appalachian Mobile Belt: Hercynian Alleghenian Orogeny
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Fig. 20.3b, p. 508 350 Ma (Mississipian)
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History of the Paleozoic Mobile Belts Next, the central and southern parts of the Appalachian mobile belt from New York to Alabama were folded and thrust toward the craton as eastern Laurasia and Gondwana collided – Alleghenian Orogeny (Pennsylvanian-Permian). The Hercynian, Alleghenian and Ouachita orogenies represent the final joining of Laurasia and Gondwana to form the supercontinent of Pangaea. Appalachian Mobile Belt: Hercynian Alleghenian Orogeny
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Fig. 20.4b, p. 510 260 Ma (Late Permian)
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History of the Paleozoic Mobile Belts Cordilleran Mobile Belts
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History of the Paleozoic Mobile Belts Fig. 20.13, p. 521 In middle Paleozoic, a volcanic arc formed off the western margin of Laurentia. The subduction created thick deep water deposits that were thrust upon the craton when the volcanic arc collided with the craton in Late Devonian. Cordilleran Mobile Belt: The Antler Orogeny Late Devonian to Pennsyl.
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History of the Paleozoic Mobile Belts The Antler orogeny marks the collision. Island arc collides with the craton in the west The Antler Highlands are composed of the deep water deposits that were thrust onto the craton. Cordilleran Mobile Belt: The Antler Orogeny Late Devonian to Pennsyl. Fig. 20.27, p. 532
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History of the Paleozoic Mobile Belts 2,100 km from MS to Marathon, TX Ouachita Mobile Belt: The Ouachita Orogeny Mississippian – Permian
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Ouachita Mountains, Oklahoma
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History of the Paleozoic Mobile Belts Fig. 20.28, p. 533 Most (80%) covered under younger sediments Exposed in Ouachita Mountains of OK and AR, and Marathon Mountains of TX Part of collision of Laurasia with Gondwana Ouachita Mobile Belt The Ouachita Orogeny Mississippian – Permian
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Ouachita Mobile Belt The Ouachita Orogeny Mississippian – Permian Fig. 20.28, p. 533 History of the Paleozoic Mobile Belts Thrusting created a large mountain range extending from the Ouachita mountains in Arkansas to the Marathon mountains in far West Texas.
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Microplates and Terranes History of the Paleozoic Mobile Belts
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What Role Did Microplates and Terranes Play in the Formation of Pangaea? During the Paleozoic Era, numerous terranes such as Avalonia, existed and played an important role in forming Pangaea. Fig. 20.4 b, p. 510
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What Role Did Microplates and Terranes Play in the Formation of Pangaea? In addition to large-scale plate interactions, microplate activity played an important role in the formation of Pangaea. There were many microplates and terranes (Iberia-Armorica, Perunica, etc) of various sizes present during the Paleozoic. These were all involved in the formation of Pangaea. Fig. 20.4 b, p. 510
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Paleozoic Mineral Resources History of the Paleozoic Mobile Belts
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Paleozoic Mineral Resources Fig. 20.29, p. 534 Paleozoic-age rocks contain a variety of mineral resources, including: petroleum coal ores of iron, lead, zinc, and other metallic deposits
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Paleozoic Mineral Resources Fig. 20.29, p. 534 building stone limestone for cement silica sand evaporites
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End of Chapter 20
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