Ocean Circulation in the Toarcian (Early Jurassic)
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Substantial Vegetation Response to Early Jurassic Global Warming with Impacts on Oceanic Anoxia
ARTICLES https://doi.org/10.1038/s41561-019-0349-z Substantial vegetation response to Early Jurassic global warming with impacts on oceanic anoxia Sam M. Slater 1*, Richard J. Twitchett2, Silvia Danise3 and Vivi Vajda 1 Rapid global warming and oceanic oxygen deficiency during the Early Jurassic Toarcian Oceanic Anoxic Event at around 183 Ma is associated with a major turnover of marine biota linked to volcanic activity. The impact of the event on land-based eco- systems and the processes that led to oceanic anoxia remain poorly understood. Here we present analyses of spore–pollen assemblages from Pliensbachian–Toarcian rock samples that record marked changes on land during the Toarcian Oceanic Anoxic Event. Vegetation shifted from a high-diversity mixture of conifers, seed ferns, wet-adapted ferns and lycophytes to a low-diversity assemblage dominated by cheirolepid conifers, cycads and Cerebropollenites-producers, which were able to sur- vive in warm, drought-like conditions. Despite the rapid recovery of floras after Toarcian global warming, the overall community composition remained notably different after the event. In shelf seas, eutrophication continued throughout the Toarcian event. This is reflected in the overwhelming dominance of algae, which contributed to reduced oxygen conditions and to a marked decline in dinoflagellates. The substantial initial vegetation response across the Pliensbachian/Toarcian boundary compared with the relatively minor marine response highlights that the impacts of the early stages of volcanogenic -
Mesozoic Central Atlantic and Ligurian Tethys1
42. RIFTING AND EARLY DRIFTING: MESOZOIC CENTRAL ATLANTIC AND LIGURIAN TETHYS1 Marcel Lemoine, Institut Dolomieu, 38031 Grenoble Cedex, France ABSTRACT The Leg 76 discovery of Callovian sediments lying above the oldest Atlantic oceanic crust allows us to more closely compare the Central Atlantic with the Mesozoic Ligurian Tethys. As a matter of fact, during the Late Jurassic and Ear- ly Cretaceous, both the young Central Atlantic Ocean and the Ligurian Tethys were segments of the Mesozoic Tethys Ocean lying between Laurasia and Gondwana and linked by the Gibraltar-Maghreb-Sicilia transform zone. If we as- sume that the Apulian-Adriatic continental bloc (or Adria) was then a northern promontory of Africa, then the predrift and early drift evolutions of both these oceanic segments must have been roughly the same: their kinematic evolution was governed by the east-west left-lateral motion of Gondwana (including Africa and Adria) relative to Laurasia (in- cluding North America, Iberia, and Europe), at least before the middle Cretaceous (=100 Ma). By the middle Cretaceous, opening of the North Atlantic Ocean led to a drastic change of the relative motions between Africa-Adria and Europe-Iberia. From this time on, closure of the Ligurian segment of the Tethys began, whereas the Central Atlan- tic went on spreading. In fact, field data from the Alps, Corsica, and the Apennines show evidence of a Triassic-Jurassic-Early Cretaceous paleotectonic evolution rather comparable with that of the Central Atlantic. Rifting may have been started during the Triassic (at least the late Triassic) but reached its climax in the Liassic. -
Speleothem Paleoclimatology for the Caribbean, Central America, and North America
quaternary Review Speleothem Paleoclimatology for the Caribbean, Central America, and North America Jessica L. Oster 1,* , Sophie F. Warken 2,3 , Natasha Sekhon 4, Monica M. Arienzo 5 and Matthew Lachniet 6 1 Department of Earth and Environmental Sciences, Vanderbilt University, Nashville, TN 37240, USA 2 Department of Geosciences, University of Heidelberg, 69120 Heidelberg, Germany; [email protected] 3 Institute of Environmental Physics, University of Heidelberg, 69120 Heidelberg, Germany 4 Department of Geological Sciences, Jackson School of Geosciences, University of Texas, Austin, TX 78712, USA; [email protected] 5 Desert Research Institute, Reno, NV 89512, USA; [email protected] 6 Department of Geoscience, University of Nevada, Las Vegas, NV 89154, USA; [email protected] * Correspondence: [email protected] Received: 27 December 2018; Accepted: 21 January 2019; Published: 28 January 2019 Abstract: Speleothem oxygen isotope records from the Caribbean, Central, and North America reveal climatic controls that include orbital variation, deglacial forcing related to ocean circulation and ice sheet retreat, and the influence of local and remote sea surface temperature variations. Here, we review these records and the global climate teleconnections they suggest following the recent publication of the Speleothem Isotopes Synthesis and Analysis (SISAL) database. We find that low-latitude records generally reflect changes in precipitation, whereas higher latitude records are sensitive to temperature and moisture source variability. Tropical records suggest precipitation variability is forced by orbital precession and North Atlantic Ocean circulation driven changes in atmospheric convection on long timescales, and tropical sea surface temperature variations on short timescales. On millennial timescales, precipitation seasonality in southwestern North America is related to North Atlantic climate variability. -
1219421 the Opening of Neo-Tethys and the Formation of the Khuff Passive Margin
1219421 The Opening of Neo-Tethys and the Formation of the Khuff Passive Margin 1219421 The Opening of Neo-Tethys and the Formation of the Khuff Passive Margin *1 2 Bell, Andrew ; Spaak, Pieter (1) Shell Global Solutions International BV, Rijswijk, Netherlands. (2) Shell International Exporation and Production BV, The Hague, Netherlands. Any investigation of regional geology and palaeomagnetism in the Middle East will show that in the Permian, a series of terranes separated from Gondwana and drifted north, opening the Neo-Tethys Ocean in their wake. To the north of these terranes, the Palaeo-Tethys Ocean closed and was largely subducted. Eventually in a non-synchronous movement but largely in late Triassic and early Jurassic times, these terranes docked with the northern margin of the former Palaeo- Tethys during the Cimmerian Orogeny. The opening of the Neo-Tethys in Arabia does not follow the classic pattern of continental break-up resulting in oceanic crust. Classically we should expect thermal up-doming, followed by the onset of syn-rift deposition, frequently but not always associated with volcanism. The formation of en-echelon systems of rotated fault blocks are also characteristic, followed by a break-up unconformity and the formation of the first oceanic crust. What we see in Arabia as a consequence of the opening of Neo-Tethys exhibits few of these features. Distinguishing thermal up-doming from the uplift associated with the ‘Hercynian’ event in Arabia, coupled with the glacial sculpting of the Permo-Carboniferous Unayzah Formation is fraught with difficulty. Although locally volcanics of Permian age are known from Oman, they are absent over most of Arabia. -
Climate Change
Optional EffectWhatAddendum: Isof Causing Climate Weather Climate Change and Change,on HumansClimate and and How the DoClimate Environment We Know? Change Optional EffectWhatAddendum: Isof Causing Climate Weather Climate Change and Change,on HumansClimate and and How the DoClimate Environment We Know? Change Part I: The Claim Two students are discussing what has caused the increase in temperature in the last century (100 years). Optional EffectWhatAddendum: Isof Causing Climate Weather Climate Change and Change,on HumansClimate and and How the DoClimate Environment We Know? Change Part II: What Do We Still Need to Know? Destiny Emilio Know from Task 1 Need to Know • Has this happened in • Is more carbon the past? dioxide being made • Are we just in a now than in the past? warm period? • Are humans responsible? Optional EffectWhatAddendum: Isof Causing Climate Weather Climate Change and Change,on HumansClimate and and How the DoClimate Environment We Know? Change Part III: Collect Evidence To support a claim, we need evidence!!! Optional EffectWhatAddendum: Isof Causing Climate Weather Climate Change and Change,on HumansClimate and and How the DoClimate Environment We Know? Change Climate Readings to the Present Data: Petit, J.R., et al., 2001, Vostok Ice Core Data for 420,000 Years, IGBP PAGES/World Data Center for Paleoclimatology Data Contribution Series #2001-076. NOAA/NGDC Paleoclimatology Program, Boulder CO, USA. https://www1.ncdc.noaa.gov/pub/data/paleo/icecore/antarctica/vostok/deutnat.tXt, …/co2nat.tXt Optional EffectWhatAddendum: Isof Causing Climate Weather Climate Change and Change,on HumansClimate and and How the DoClimate Environment We Know? Change How do we know about the climate from thousands of years ago? Optional EffectWhatAddendum: Isof Causing Climate Weather Climate Change and Change,on HumansClimate and and How the DoClimate Environment We Know? Change Measuring Devices • Thermometers were not invented until 1724. -
Unit 1 Lesson 4: Coral Reefs As Indicators of Paleoclimate
CORAL REEFS Unit 1 Lesson 4: Coral Reefs as Indicators of Paleoclimate esson Objectives: Students will gain knowledge of how the marine environment can tell a story about years past through naturally recorded geographic and environmental phenomenon. Vocabulary: Paleoclimate, greenhouse effect, proxy data information gathered from www.noaa.gov Paleoclimatology is the study temperature increases may of the weather and climate from have a natural cause, for ages past. The word is derived example, from elevated from the Greek root word volcanic activity. "paleo-," which means "long ago" with combined with Gases in the earth’s "climate," meaning weather. atmosphere which trap heat, Scientists and meteorologists and cause an increase in have been using instruments to temperature cause the measure climate and weather greenhouse effect. Carbon for only the past 140 years! dioxide (CO2), water vapor, How do they determine what and other gases in the the Earth's climate was like atmosphere absorb the infrared before then? They use rays forming a kind of blanket historical evidence called proxy around the earth. Scientists data. Examples of proxy data fear that if humans continue to include tree rings, old farmer’s place too much carbon dioxide diaries, ice cores, frozen pollen in the atmosphere, too much and ocean sediments. heat will be trapped, causing the global temperature to rise Scientists know the Earth's and resulting in devastating average temperature has effects. increased approximately 1°F since 1860. Is this warming Some scientists speculate that due to something people are natural events like volcanic releasing into the atmosphere eruptions or an increase in the or natural causes? Many sun's output, may be people today are quick to influencing the climate. -
Paleoclimatology
Paleoclimatology ATMS/ESS/OCEAN 589 • Ice Age Cycles – Are they fundamentaly about ice, about CO2, or both? • Abrupt Climate Change During the Last Glacial Period – Lessons for the future? • The Holocene – Early Holocene vs. Late Holocene – The last 1000 years: implications for interpreting the recent climate changes and relevance to projecting the future climate. Website: faculty.washington.edu/battisti/589paleo2005 Class email: [email protected] Theory of the Ice Ages: Orbital induced insolation changes and global ice volume “Strong summer insolation peaks pace rapid deglaciation” Theory of the Ice Ages: Ice Volume and Atmospheric Carbon Dioxide are highly correlated •Summer (NH) insulation tends to lead ice volume. •Ice Volume and Carbon Dioxide seem to be in phase (except for in rapid deglaciation, when Ice volume leads Carbon Dioxide) CO2 measured at Vostok, South Pole The Ice Age Cycles: Some big unsolved questions we will examine • Is the Ice Age cycle fundamentaly about cycles in ice volume induced by high latitude insolation changes (with CO2 being a weak positive feedback)? • Or, is the Ice Age cycle fundamentally about changes in CO2 that are driven by insolation changes (with weak positive feedbacks associated with ice albedo feedbacks)? • Why do (high latitude) insolation changes cause changes in atmospheric CO2? Why is it CO2 so highly correlated with ice volume? Abrupt Climate Change during the Last Glacial Period During Glacial stages, the climate system featured large rapid rearrangements. Dansgaard/Oeschger (D/O) events show: – Rapid onset of warming at Greenland ( 10 K in < 30 years!) – Long-lived (~ 200 - 600 years) Greenland Temperature Tropical-Extratropical Linkages during Glacial Times: Extratropics forcing Tropics • Paleo data show strong linkages between the millennial variability in the North Atlantic, the tropical Atlantic and the Northern Hemisphere during the last Glacial Period. -
Coevolution of Global Brachiopod Palaeobiogeography and Tectonopalaeogeography During the Carboniferous Ning Li1,2*, Cheng-Wen Wang1, Pu Zong3 and Yong-Qin Mao4
Li et al. Journal of Palaeogeography (2021) 10:18 https://doi.org/10.1186/s42501-021-00095-z Journal of Palaeogeography ORIGINAL ARTICLE Open Access Coevolution of global brachiopod palaeobiogeography and tectonopalaeogeography during the Carboniferous Ning Li1,2*, Cheng-Wen Wang1, Pu Zong3 and Yong-Qin Mao4 Abstract The global brachiopod palaeobiogeography of the Mississippian is divided into three realms, six regions, and eight provinces, while that of the Pennsylvanian is divided into three realms, six regions, and nine provinces. On this basis, we examined coevolutionary relationships between brachiopod palaeobiogeography and tectonopalaeogeography using a comparative approach spanning the Carboniferous. The appearance of the Boreal Realm in the Mississippian was closely related to movements of the northern plates into middle–high latitudes. From the Mississippian to the Pennsylvanian, the palaeobiogeography of Australia transitioned from the Tethys Realm to the Gondwana Realm, which is related to the southward movement of eastern Gondwana from middle to high southern latitudes. The transition of the Yukon–Pechora area from the Tethys Realm to the Boreal Realm was associated with the northward movement of Laurussia, whose northern margin entered middle–high northern latitudes then. The formation of the six palaeobiogeographic regions of Mississippian and Pennsylvanian brachiopods was directly related to “continental barriers”, which resulted in the geographical isolation of each region. The barriers resulted from the configurations of Siberia, Gondwana, and Laurussia, which supported the Boreal, Tethys, and Gondwana realms, respectively. During the late Late Devonian–Early Mississippian, the Rheic seaway closed and North America (from Laurussia) joined with South America and Africa (from Gondwana), such that the function of “continental barriers” was strengthened and the differentiation of eastern and western regions of the Tethys Realm became more distinct. -
GEOLOGIC TIME SCALE V
GSA GEOLOGIC TIME SCALE v. 4.0 CENOZOIC MESOZOIC PALEOZOIC PRECAMBRIAN MAGNETIC MAGNETIC BDY. AGE POLARITY PICKS AGE POLARITY PICKS AGE PICKS AGE . N PERIOD EPOCH AGE PERIOD EPOCH AGE PERIOD EPOCH AGE EON ERA PERIOD AGES (Ma) (Ma) (Ma) (Ma) (Ma) (Ma) (Ma) HIST HIST. ANOM. (Ma) ANOM. CHRON. CHRO HOLOCENE 1 C1 QUATER- 0.01 30 C30 66.0 541 CALABRIAN NARY PLEISTOCENE* 1.8 31 C31 MAASTRICHTIAN 252 2 C2 GELASIAN 70 CHANGHSINGIAN EDIACARAN 2.6 Lopin- 254 32 C32 72.1 635 2A C2A PIACENZIAN WUCHIAPINGIAN PLIOCENE 3.6 gian 33 260 260 3 ZANCLEAN CAPITANIAN NEOPRO- 5 C3 CAMPANIAN Guada- 265 750 CRYOGENIAN 5.3 80 C33 WORDIAN TEROZOIC 3A MESSINIAN LATE lupian 269 C3A 83.6 ROADIAN 272 850 7.2 SANTONIAN 4 KUNGURIAN C4 86.3 279 TONIAN CONIACIAN 280 4A Cisura- C4A TORTONIAN 90 89.8 1000 1000 PERMIAN ARTINSKIAN 10 5 TURONIAN lian C5 93.9 290 SAKMARIAN STENIAN 11.6 CENOMANIAN 296 SERRAVALLIAN 34 C34 ASSELIAN 299 5A 100 100 300 GZHELIAN 1200 C5A 13.8 LATE 304 KASIMOVIAN 307 1250 MESOPRO- 15 LANGHIAN ECTASIAN 5B C5B ALBIAN MIDDLE MOSCOVIAN 16.0 TEROZOIC 5C C5C 110 VANIAN 315 PENNSYL- 1400 EARLY 5D C5D MIOCENE 113 320 BASHKIRIAN 323 5E C5E NEOGENE BURDIGALIAN SERPUKHOVIAN 1500 CALYMMIAN 6 C6 APTIAN LATE 20 120 331 6A C6A 20.4 EARLY 1600 M0r 126 6B C6B AQUITANIAN M1 340 MIDDLE VISEAN MISSIS- M3 BARREMIAN SIPPIAN STATHERIAN C6C 23.0 6C 130 M5 CRETACEOUS 131 347 1750 HAUTERIVIAN 7 C7 CARBONIFEROUS EARLY TOURNAISIAN 1800 M10 134 25 7A C7A 359 8 C8 CHATTIAN VALANGINIAN M12 360 140 M14 139 FAMENNIAN OROSIRIAN 9 C9 M16 28.1 M18 BERRIASIAN 2000 PROTEROZOIC 10 C10 LATE -
Climate and Deep Water Formation Regions
Cenozoic High Latitude Paleoceanography: New Perspectives from the Arctic and Subantarctic Pacific by Lindsey M. Waddell A dissertation submitted in partial fulfillment of the requirements for the degree of Doctor of Philosophy (Oceanography: Marine Geology and Geochemistry) in The University of Michigan 2009 Doctoral Committee: Assistant Professor Ingrid L. Hendy, Chair Professor Mary Anne Carroll Professor Lynn M. Walter Associate Professor Christopher J. Poulsen Table of Contents List of Figures................................................................................................................... iii List of Tables ......................................................................................................................v List of Appendices............................................................................................................ vi Abstract............................................................................................................................ vii Chapter 1. Introduction....................................................................................................................1 2. Ventilation of the Abyssal Southern Ocean During the Late Neogene: A New Perspective from the Subantarctic Pacific ......................................................21 3. Global Overturning Circulation During the Late Neogene: New Insights from Hiatuses in the Subantarctic Pacific ...........................................55 4. Salinity of the Eocene Arctic Ocean from Oxygen Isotope -
A Reconstruction of Iberia Accounting for Western Tethys–North Atlantic Kinematics Since the Late-Permian–Triassic
Solid Earth, 11, 1313–1332, 2020 https://doi.org/10.5194/se-11-1313-2020 © Author(s) 2020. This work is distributed under the Creative Commons Attribution 4.0 License. A reconstruction of Iberia accounting for Western Tethys–North Atlantic kinematics since the late-Permian–Triassic Paul Angrand1, Frédéric Mouthereau1, Emmanuel Masini2,3, and Riccardo Asti4 1Geosciences Environnement Toulouse (GET), Université de Toulouse, UPS, Univ. Paul Sabatier, CNRS, IRD, 14 av. Edouard Belin, 31400 Toulouse, France 2M&U sas, 38120 Saint-Égrève, France 3ISTerre, Université Grenoble Alpes, 38000 Grenoble, France 4Université de Rennes, CNRS, Géosciences Rennes-UMR 6118, 35000 Rennes, France Correspondence: Paul Angrand ([email protected]) Received: 20 February 2020 – Discussion started: 6 March 2020 Revised: 12 May 2020 – Accepted: 27 May 2020 – Published: 21 July 2020 Abstract. The western European kinematic evolution results 1 Introduction from the opening of the western Neotethys and the Atlantic oceans since the late Paleozoic and the Mesozoic. Geolog- Global plate tectonic reconstructions are mostly based on the ical evidence shows that the Iberian domain recorded the knowledge and reliability of magnetic anomalies that record propagation of these two oceanic systems well and is there- age, rate, and direction of sea-floor spreading (Stampfli and fore a key to significantly advancing our understanding of Borel, 2002; Müller et al., 2008; Seton et al., 2012). Where the regional plate reconstructions. The late-Permian–Triassic these constraints are lacking or their recognition is ambigu- Iberian rift basins have accommodated extension, but this ous, kinematic reconstructions rely on the description and in- tectonic stage is often neglected in most plate kinematic terpretation of the structural, sedimentary, igneous and meta- models, leading to the overestimation of the movements be- morphic rocks of rifted margins and orogens (e.g., Handy tween Iberia and Europe during the subsequent Mesozoic et al., 2010; McQuarrie and Van Hinsbergen, 2013). -
49. GENESIS of the TETHYS and the MEDITERRANEAN Kenneth J
49. GENESIS OF THE TETHYS AND THE MEDITERRANEAN Kenneth J. Hsü, Geologisches Institut, ETH Zurich, Switzerland and Daniel Bernoulli, Geologisch-Palàontologisches Institut, Universitàt Basel, Switzerland ABSTRACT The Triassic Paleotethys was a wedge-like ocean opening to the east, which was totally eliminated during the early Mesozoic by subduction along the Cimmerian and Indosinian suture zone. The Tethys, s.s., was an Early Jurassic creation formed when Africa moved east relative to Europe. The sinistral movement of Africa continued until Late Cretaceous when the movement became dextral. The closing of the gap between Africa and Europe led to the Alpine orogeny and the elimination of much of the Tethys. Only the eastern Mediterranean Ionian and Levantine basins are left as possible relics of this Mesozoic ocean. The western Mediter- ranean and the Aegean are post-orogenic basins. The Balearic Ba- sin was created during late Oligocene or earliest Miocene time by rifting tectonics. The Tyrrhenian Basin was probably somewhat younger. The presence of oceanic tholeiites under its abyssal plain indicates that submarine basalt volcanism played a major role in the genesis of this basin. The Aegean Basin is probably the youngest and has undergone considerable Pliocene-Quaternary subsidence. Tectonic synthesis indicates that the Mediterranean basins, ex- cept perhaps the Aegean, were in existence and deep prior to the Messinian Salinity Crisis. FOREWORD nent Gondwana was the home of the late Paleozoic Glossopteria flora. Its inclusion in the definition of Several attempts have been made to reconstruct the Tethys seemed to imply the existence of this mediterra- tectonic history of the Tethys and its descendent, the nean during the Paleozoic.