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  • 1
    Online Resource
    Online Resource
    Cambridge :Cambridge University Press,
    Keywords: Theology, Doctrinal. ; Electronic books.
    Description / Table of Contents: Using a range of the most up to date isotope geochronology, geomathematics and orbital tuning methods, an international team of over forty researchers has built the most modern stratigraphic framework for the Precambrian and Phanerozoic. Including a wallchart, this book is an invaluable reference source for researchers and students.
    Type of Medium: Online Resource
    Pages: 1 online resource (611 pages)
    Edition: 1st ed.
    ISBN: 9780511196928
    DDC: 551.701
    Language: English
    Note: Cover -- Half-title -- Title -- Copyright -- Dedication -- Contents -- Contributors -- Preface -- Acknowledgments -- Abbreviations and acronyms -- ORGANIZATIONS -- TIME SCALE PUBLICATIONS -- GEOSCIENTIFIC CONCEPTS -- SYMBOLS -- Part I Introduction -- 1 Introduction -- 1.1 A GEOLOGIC TIME SCALE 2004 -- 1.2 HOW THIS BOOK IS ARRANGED -- 1.3 CONVENTIONS AND STANDARDS -- 1.3.1 Universal time -- 1.3.2 Ephemeris time -- 1.4 HISTORICAL OVERVIEW OF GEOLOGIC TIME SCALES -- 1.4.1 Arthur Holmes and age-thickness interpolations -- 1.4.2 Phanerozoic radiometric databases, statistical scales, and compilations -- 1.4.3 Paleozoic scales -- 1.4.4 Mesozoic scales -- 1.4.5 Cenozoic scales -- 2 Chronostratigraphy: linking time and rock -- 2.1 TIME AND ROCK -- 2.2 STANDARDIZATION OF THE CHRONOSTRATIGRAPHIC SCALE -- 2.2.1 History of geologic stratigraphic standardization -- 2.2.2 Global boundary Stratotype Section and Point (GSSP) -- 2.2.3 Global Standard Stratigraphic Age (GSSA) -- 2.2.4 Other considerations for choosing a GSSP -- 2.2.5 Subdividing long stages -- 2.2.6 Do GSSP boundary stratotypes simplify stratigraphic classification? -- 2.3 CASE EXAMPLES OF GSSPs -- 2.3.1 Pliocene-Pleistocene boundary -- 2.3.2 Eocene-Oligocene boundary -- 2.3.3 Permian-Triassic boundary -- 2.4 MAJOR SUBDIVISIONS OF THE GEOLOGIC TIME SCALE -- 2.4.1 Archean and Proterozoic Eons (Precambrian) -- 2.4.2 Phanerozoic Eon -- THE PALEOZOIC ERA -- THE MESOZOIC ERA -- 2.5 EXAMPLES OF STRATIGRAPHIC CHARTS AND TABLES -- Part II Concepts and methods -- 3 Biostratigraphy: time scales from graphic and quantitative methods -- 3.1 INTRODUCTION -- 3.2 GRAPHIC CORRELATION -- 3.3 CONSTRAINED OPTIMIZATION -- 3.4 RANKING AND SCALING -- 4 Earth's orbital parameters and cycle stratigraphy -- 4.1 INTRODUCTION -- 4.2 EARTH'S ORBITAL PARAMETERS -- 4.3 ORBITALLY FORCED INSOLATION. , 4.4 ORBITAL SIGNALS IN CYCLE STRATIGRAPHY -- 4.5 ESTIMATING ORBITAL CHRONOLOGIES -- 5 The geomagnetic polarity time scale -- 5.1 PRINCIPLES -- 5.1.1 Magnetic field reversals and magnetostratigraphy -- 5.1.2 Polarity intervals, zones, and chrons -- 5.1.3 Events, excursions, magnetic anomaly wiggles, and cryptochrons -- 5.2 LATE CRETACEOUS-CENOZOIC GEOMAGNETIC POLARITY TIME SCALE -- 5.2.1 C-sequence of marine magnetic anomalies and associated chron nomenclature -- 5.2.2 Calibration and ages of the Late Cretaceous-Cenozoic geomagnetic polarity time scale -- 5.3 MIDDLE JURASSIC-EARLY CRETACEOUS GEOMAGNETIC POLARITY TIME SCALE -- 5.3.1 M-sequence of marine magnetic anomalies -- 5.3.2 Constructing a composite M-sequence -- ANOMALIES M0R (BASE-APTIAN) TO M25N (BASE-KIMMERIDGIAN) -- ANOMALIES M25R (BASE-KIMMERIDGIAN) TO M41 (BATHONIAN) -- 5.3.3 Calibration and ages of the Middle Jurassic-Early Cretaceous geomagnetic polarity time scale -- AGE CONSTRAINTS ON M-SEQUENCE SCALING -- SPREADING MODEL AND AGES OF M-SEQUENCE POLARITY CHRONS -- 5.4 GEOMAGNETIC POLARITY TIME SCALE FOR MIDDLE JURASSIC AND OLDER ROCKS -- 5.4.1 Paleozoic to Middle Jurassic -- SPREADING MODEL AND AGES OF M-SEQUENCE 5.4.1 Paleozoic to Middle Jurassic -- 5.4.2 Precambrian -- 5.5 SUPERCHRONS AND POLARITY BIAS -- 5.6 SUMMARY AND CONCLUSIONS -- 6 Radiogenic isotope geochronology -- 6.1 INTRODUCTION -- 6.2 TYPES OF UNCERTAINTIES -- 6.2.1 Decay constants, isotopic ratios, and comparison between 40Ar/39Ar and U-Pb systems -- 6.2.2 Calibration of reference materials -- 6.2.3 Changes induced by geological processes -- 6.3 DATING METHODS -- 6.3.1 U-Pb -- THERMAL IONIZATION MASS SPECTROMETRIC (TIMS) METHODS -- HIGH-RESOLUTION-SECONDARY ION MASS SPECTROMETRY (HR-SIMS) -- 6.3.2 K-Ar and 40Ar/39Ar -- K-Ar METHODS -- 40Ar/39Ar METHODS -- 6.3.3 Other methods -- 6.4 SUMMARY AND CONCLUSIONS. , 7 Strontium isotope stratigraphy -- 7.1 INTRODUCTION -- 7.2 MATERIALS FOR STRONTIUM ISOTOPE STRATIGRAPHY -- 7.3 A GEOLOGIC TIME SCALE 2004 (GTS2004) DATABASE -- 7.3.1 Numerical ages -- 7.3.2 Fitting the database -- 7.3.3 The quality of the fit -- CONFIDENCE LIMITS ON THE LOWESS FIT -- RUBIDIUM CONTAMINATION -- 7.4 COMMENTS ON THE LOWESS FIT -- 8 Geomathematics -- 8.1 HISTORY AND OVERVIEW -- 8.1.1 Statistical estimation of chronostratigraphic boundary ages (with error bars) -- 8.1.3 Spline-curve fitting with consideration of stratigraphic uncertainty -- 8.1.4 General comments on straight-line fitting -- 8.2 PALEOZOIC APPLICATIONS -- 8.2.1 Straight-line fitting for Ordovician and Silurian ages -- 8.2.2 Straight-line fitting for Devonian ages -- AVERAGE SQUARE OF SCALED RESIDUAL ADJUSTMENT -- 8.2.3 Carboniferous-Permian -- 8.2.4 Permian-Triassic boundary -- 8.3 LATE CRETACEOUS AND PALEOGENE APPLICATIONS -- 8.3.1 Late Cretaceous -- SAMPLE-POINT DISTRIBUTION ADJUSTMENT -- ADJUSTMENT TO ACCOUNT FOR EXTERNAL VARIABILITY OF LATE CRETACEOUS 40Ar/39Ar DATES -- TOTAL ADJUSTMENT AND 2-SIGMA ERROR BAR OF STAGE DURATION -- COMPARISON TO 87Sr/86Sr CURVE -- 8.3.2 Paleogene time scale -- 8.4 CONCLUDING REMARKS -- Part III Geologic periods -- 9 The Precambrian: the Archean and Proterozoic Eons -- 9.1 INTRODUCTION -- 9.2 HISTORY AND RECOMMENDED SUBDIVISION -- 9.2.1 The Archean Eon -- 9.2.2 The Proterozoic Eon -- 9.3 NOMENCLATURE OF THE SUBDIVISIONS -- 9.3.1 Eons -- 9.3.2 Eras -- 9.3.3 Periods -- 9.4 THE NEOPROTEROZOIC -- 9.5 ISOTOPE STRATIGRAPHY IN THE PRECAMBRIAN -- 9.5.1 Strontium isotope stratigraphy -- 9.5.2 Carbon isotope stratigraphy -- 9.5.3 Oxygen isotope stratigraphy -- 9.5.4 Sulfur isotope stratigraphy -- 9.5.5 The role of isotope stratigraphy in global correlation -- 9.6 BIOSTRATIGRAPHY IN THE NEOPROTEROZOIC. , 9.7 NEOPROTEROZOIC ICE AGES AND CHRONOMETRIC CONSTRAINTS -- 9.8 SUMMARY -- 10 Toward a "natural" Precambrian time scale -- 10.1 INTRODUCTION -- 10.2 CURRENT PRECAMBRIAN SUBDIVISIONS AND PROBLEMS -- 10.3 A "NATURAL" PRECAMBRIAN TIME SCALE -- 10.3.1 The "Accretion and Differentiation" or "Genesis" Eon -- 10.3.2 The Hadean Eon -- 10.3.3 The Archean and "Transition" Eons -- 10.3.4 The Proterozoic Eon -- 10.3.5 The Ediacaran Period (base-Paleozoic?) -- 10.4 CONCLUSIONS -- 11 The Cambrian Period -- 11.1 HISTORY AND SUBDIVISIONS -- 11.1.1 Base of the Cambrian System and Paleozoic Erathem -- 11.1.2 Biostratigraphic datums with potential for global correlation -- BASE OF THE CORDYLODUS PROAVUS ZONE -- BASE OF THE GLYPTAGNOSTUS RETICULATUS ZONE, BASE OF THE PAIBIAN STAGE, LOWERMOST FURONGIAN SERIES -- BASE OF THE PTYCHAGNOSTUS PUNCTUOSUS ZONE -- BASE OF THE ACIDUSUS ATAVUS ZONE -- BASE OF THE TRIPLAGNOSTUS GIBBUS ZONE -- BASE OF THE ORYCTOCEPHALUS INDICUS ZONE -- 11.1.3 Regional Cambrian stage suites -- AUSTRALIAN CAMBRIAN STAGES -- NORTH AMERICAN CAMBRIAN STAGES -- 11.2 CAMBRIAN STRATIGRAPHY -- 11.2.1 Faunal provinces -- 11.2.2 Trilobite zones -- 11.2.3 Archaeocyathan zones -- 11.2.4 Conodont zones -- 11.2.5 Magnetostratigraphy -- 11.2.6 Chemostratigraphy -- 11.2.7 Cambrian evolutionary "explosion" -- 11.3 CAMBRIAN TIME SCALE -- 11.3.1 Age of boundaries -- 12 The Ordovician Period -- 12.1 HISTORY AND SUBDIVISIONS -- 12.1.1 Stages of the Lower Ordovician -- CAMBRIAN-ORDOVICIAN BOUNDARY AND STAGE 1: THE TREMADOCIAN -- STAGE 2 (UNNAMED) -- 12.1.2 Stages of the Middle Ordovician -- STAGE 3 (UNNAMED) -- STAGE 4: THE DARRIWILIAN -- 12.1.3 Stages of the Upper Ordovician -- STAGE 5 (UNNAMED) -- STAGE 6 (UNNAMED) -- STAGE 7: THE HIRNANTIAN -- 12.2 PREVIOUS STANDARD DIVISIONS -- 12.2.1 Tremadoc -- 12.2.2 Arenig -- 12.2.3 Llanvirn -- 12.2.4 Caradoc -- 12.2.5 Ashgill. , 12.2.6 Australasian stages -- 12.3 ORDOVICIAN STRATIGRAPHY -- 12.3.1 Biostratigraphy -- GRAPTOLITE ZONES -- CONODONT ZONES -- EVOLUTIONARY EVENTS -- 12.3.2 Magnetostratigraphy -- 12.3.3 Eustatic and climatic events -- 12.3.4 Sr isotope stratigraphy -- 12.4 ORDOVICIAN TIME SCALE -- 12.4.1 Radiometric dates -- 12.4.2 HR-SIMS (SHRIMP) dates -- 12.4.3 Calibration of stage boundaries by composite standard optimization -- 12.4.4 Age of stage boundaries -- 13 The Silurian Period -- 13.1 HISTORY AND SUBDIVISIONS -- 13.1.1 Llandovery Series -- RHUDDANIAN -- AERONIAN -- TELYCHIAN -- 13.1.2 Wenlock Series -- SHEINWOODIAN -- HOMERIAN -- 13.1.3 Ludlow Series -- GORSTIAN -- LUDFORDIAN -- 13.1.4 Pridoli Series -- 13.1.5 Other important stage classifications -- 13.2 SILURIAN STRATIGRAPHY -- 13.2.1 Biostratigraphy -- GRAPTOLITE ZONES -- CONODONT ZONES -- CHITINOZOAN ZONES -- OTHER ZONAL GROUPS -- BIOEVENTS -- 13.2.2 Physical stratigraphy -- MAGNETOSTRATIGRAPHY -- CHEMOSTRATIGRAPHY -- EUSTASY -- CLIMATIC EVENTS -- VOLCANISM AND K-BENTONITE STRATIGRAPHY -- 13.3 SILURIAN TIME SCALE -- 13.3.1 Radiometric dates -- 13.3.2 Methods to estimate relative duration of zones and stages -- 13.3.3 Calibration of stage boundaries by composite standard optimization -- 13.3.4 Age of stage boundaries -- 14 The Devonian Period -- 14.1 HISTORY AND SUBDIVISIONS -- 14.1.1 Lower Devonian Series -- LOCHKOVIAN -- PRAGIAN -- EMSIAN -- 14.1.2 Middle Devonian Series -- EIFELIAN -- GIVETIAN -- 14.1.3 Upper Devonian Series -- FRASNIAN -- FAMENNIAN -- BASE OF THE CARBONIFEROUS -- 14.2 DEVONIAN STRATIGRAPHY -- 14.2.1 Biostratigraphy -- CONODONT ZONATIONS -- AMMONOID ZONATIONS -- OSTRACOD ZONATION -- DACRYCONARID ZONATION -- SPORE AND ACRITARCH ZONATIONS -- PLANT MEGAFOSSIL ZONATION -- VERTEBRATE ZONATIONS -- 14.2.2 Physical stratigraphy -- EXTINCTION AND ANOXIA EVENT STRATIGRAPHY. , CYCLOSTRATIGRAPHY.
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  • 2
    Online Resource
    Online Resource
    San Diego : Elsevier
    Keywords: Electronic books
    Description / Table of Contents: 9780128243619v1_WEB -- Quotes -- 9780128243619v2_WEB -- Quotes -- Contents -- Appendix 1: Recommended colorcoding of stages -- Appendix 2: Radioisotopic ages used in GTS2020.
    Type of Medium: Online Resource
    Pages: 1 online resource (2504 pages)
    ISBN: 9780128243619
    DDC: 551.701
    Language: English
    Note: Description based on publisher supplied metadata and other sources
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  • 3
    ISSN: 1520-4804
    Source: ACS Legacy Archives
    Topics: Chemistry and Pharmacology
    Type of Medium: Electronic Resource
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  • 4
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    PANGAEA
    In:  Supplement to: Li, Mingsong; Huang, Chunju; Hinnov, Linda A; Ogg, James; Chen, Zhong-Qiang; Zhang, Yang (2016): Obliquity-forced climate during the Early Triassic hothouse in China. Geology, 44(8), 623-626, https://doi.org/10.1130/G37970.1
    Publication Date: 2023-04-22
    Description: The start of the Mesozoic Era is marked by roughly five million years (myr) of Earth system upheavals, including unstable biotic recovery, repeated global warming, ocean anoxia, and perturbations in the global carbon cycle. Intervals between crises were comparably hospitable to life. The causes of these upheavals are unknown, but are thought to be linked to recurrent Siberian volcanism. Here, two marine sedimentary successions at Chaohu and Daxiakou, South China are evaluated for paleoclimate change from astronomical forcing. In these sections, gamma-ray variations indicative of terrestrial weathering reveal enhanced obliquity cycling over prolonged intervals, characterized by a periodicity of 32.8 kiloyear and strong 1.2 myr modulations. This suggests a 22-hour length-of-day and 1.2 myr interaction between the orbital inclinations of Earth and Mars. The 1.2 myr obliquity modulation cycles in these sections are compared with Early Triassic records of global sea-level, temperature, redox and biotic evolution. The evidence collectively suggests that long-term astronomical forcing was involved in the repeated climatic and biotic upheavals that took place throughout the Early Triassic.
    Type: Dataset
    Format: application/zip, 6.7 kBytes
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  • 5
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    PANGAEA
    In:  Supplement to: Ogg, James G (1987): Early Cretaceous magnetic polarity time scale and the magnetostratigraphy of Deep Sea Drilling Project Sites 603 and 534, western Central Atlantic. In: van Hinte, JE; Wise, SW Jr; et al. (eds.), Initial Reports of the Deep Sea Drilling Project, Washington (U.S. Govt. Printing Office), 93, 849-879, https://doi.org/10.2973/dsdp.proc.93.131.1987
    Publication Date: 2023-05-12
    Description: Drilling at Sites 534 and 603 of the Deep Sea Drilling Project recovered thick sections of Berriasian through Aptian white limestones to dark gray marls, interbedded with claystone and clastic turbidites. Progressive thermal demagnetization removed a normal-polarity overprint carried by goethite and/or pyrrhotite. The resulting characteristic magnetization is carried predominantly by magnetite. Directions and reliability of characteristic magnetization of each sample were computed by using least squares line-fits of magnetization vectors. The corrected true mean inclinations of the sites suggest that the western North Atlantic underwent approximately 6° of steady southward motion between the Berriasian and Aptian stages. The patterns of magnetic polarity of the two sites, when plotted on stratigraphic columns of the pelagic sediments without turbidite beds, display a fairly consistent magnetostratigraphy through most of the Hauterivian-Barremian interval, using dinoflagellate and nannofossil events and facies changes in pelagic sediment as controls on the correlations. The composite magnetostratigraphy appears to include most of the features of the M-sequence block model of magnetic anomalies from Ml to Ml ON (Barremian-Hauterivian) and from M16 to M23 (Berriasian-Tithonian). The Valanginian magnetostratigraphy of the sites does not exhibit reversed polarity intervals corresponding to Ml 1 to M13 of the M-sequence model; this may be the result of poor magnetization, of a major unrecognized hiatus in the early to middle Valanginian in the western North Atlantic, or of an error in the standard block model. Based on these tentative polarity-zone correlations, the Hauterivian/Barremian boundary occurs in or near the reversed-polarity Chron M7 or M5, depending upon whether the dinoflagellate or nannofossil zonation, respectively, is used; the Valanginian/Hauterivian boundary, as defined by the dinoflagellate zonation, is near reversed-polarity Chron M10N.
    Keywords: Deep Sea Drilling Project; DSDP
    Type: Dataset
    Format: application/zip, 4 datasets
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  • 6
    Publication Date: 2023-06-27
    Description: New paleomagnetic and paleontologic data from Pacific DSDP Sites 463 and 167 define the magnetic reversals that predate the Cretaceous Normal Polarity Superchron (K-N). Data from Mid-Pacific Mountain Site 463 provide the first definition of polarity chron M0 in the Pacific deep-sea sedimentary record. Foraminiferal biostratigraphy suggests that polarity chron M0 is contained entirely within the lower Aptian Hedbergella similis Zone, in agreement with foraminiferal data from the Italian Southern Alps and Atlantic Ocean. Nannofossil assemblages also suggest an early Aptian age for polarity chron M0, contrary to results from the Italian Umbrian Apennines and Southern Alps, which place polarity chron M0 on the Barremian-Aptian boundary. Biostratigraphic dating discrepancies caused by the time-transgressive, preservational, or provincial nature of paleontological species might be reconciled by the use of magnetostratigraphy, specifically polarity chron M0 which lies close to the Barremian-Aptian boundary. At Magellan Rise Site 167, five reversed polarity zones are recorded in Hauterivian to Aptian sediments. Correlation with M-anomalies is complicated by synsedimentary and postsedimentary sliding about 25 m.y. after basement formation, producing gaps in, and duplications of, the stratigraphic sequence. The magnitude and timing of such sliding must be addressed when evaluating the stratigraphy of these oceanic-rise environments.
    Keywords: 17-167; 62-463; Deep Sea Drilling Project; DRILL; Drilling/drill rig; DSDP; Glomar Challenger; Leg17; Leg62; North Pacific/CONT RISE; North Pacific/SEAMOUNT
    Type: Dataset
    Format: application/zip, 4 datasets
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  • 7
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    PANGAEA
    In:  Supplement to: Ogg, James G; Robertson, Alastair H F; Jansa, Lubomir F (1983): Jurassic sedimentation history of Site 534 (western North Atlantic) and of the Atlantic-Tethys Seaway. In: Sheridan, RE; Gradstein, FM; et al. (eds.), Initial Reports of the Deep Sea Drilling Project (U.S. Govt. Printing Office), 76, 829-884, https://doi.org/10.2973/dsdp.proc.76.141.1983
    Publication Date: 2023-06-27
    Description: Site 534 reflects a complex interplay of global, basinal, and local influences on sedimentation during the Callovian and Late Jurassic. Rifting and rapid subsidence of the continental margins of the North Atlantic-Tethys seaway occurred during the late Early Jurassic (Sinemurian-Pliensbachian), but rapid spreading between the North American margin (Blake Spur Ridge and magnetic lineation) and the northwest African margin did not commence until the Bathonian or earliest Callovian. Site 534, drilled on marine magnetic anomaly "M-28" of Bryan et al. (1980), was initially about 150 km from either continental margin. The ?middle Callovian basal sediments are dusky red silty marl. Callovian transgression led to active carbonate platforms on the margin, recorded at Site 534 as a rise in the CCD (carbonate compensation depth), then arrival of lime-rich turbidites from the Blake Plateau platform across the Blake Spur Ridge. The host pelagic sediment is greenish black, organic-rich, radiolarian-rich, silty claystone. Hydrothermal activity on the nearby spreading ridge enriched this lower unit in metals. In the Oxfordian, the input of terrestrial silt rapidly diminished; radiolarians or other bioclasts were not preserved. The dark variegated claystone has fine-grained marl and reddish claystone turbidite beds. The late Callovian-Oxfordian Western Tethys has radiolarian chert deposition, marine hiatuses, or organic-rich sediments. The Kimmeridgian and Tithonian had a stable or receding sea level. Near the end of the Jurassic many of the carbonate platforms of the margins were buried beneath prograding fan or alluvial deposits. Carbonate deposition shifted to the deep sea. Site 534 records the deepening of the CCD and ACD (aragonite compensation depth) during the Kimmeridgian and early Tithonian, then a rise of the ACD in the middle Tithonian. Similar trends occurred throughout the Western Tethys-Atlantic. High nannofossil productivity of the seaway led to deposition of very widespread white micritic limestone in the late Tithonian-Berriasian. The underlying sediment had a slower deposition rate of carbonate, therefore its higher clay and associated Fe content produced a red marl. A short sea-level incursion occurred on the Atlantic margins during the Kimmeridgian and is reflected in the Site 534 greenish gray marl unit by numerous turbidite beds of shallow-water carbonates.
    Keywords: 76-534A; Deep Sea Drilling Project; DRILL; Drilling/drill rig; DSDP; Glomar Challenger; Leg76; North Atlantic/BASIN
    Type: Dataset
    Format: application/zip, 9 datasets
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  • 8
    Publication Date: 2023-06-27
    Keywords: 93-603B; ChRM, Declination; ChRM, Inclination; ChRM, Intensity; Deep Sea Drilling Project; DRILL; Drilling/drill rig; DSDP; DSDP/ODP/IODP sample designation; Glomar Challenger; Leg93; Polarity; Sample code/label
    Type: Dataset
    Format: text/tab-separated-values, 2205 data points
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  • 9
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    PANGAEA
    In:  Supplement to: Ogg, James G (1986): Paleolatitudes and magnetostratigraphy of Cretaceous and lower Tertiary sedimentary rocks, Deep Sea Drilling Project Site 585, East Mariana Basin, Western Central Pacific. In: Moberly, R; Schlanger, SO; et al. (eds.), Initial Reports of the Deep Sea Drilling Project, Washington (U.S. Govt. Printing Office), 89, 629-645, https://doi.org/10.2973/dsdp.proc.89.127.1986
    Publication Date: 2023-06-27
    Description: Coring in two adjacent holes at DSDP Site 585 (13.5°N, 156.8°E) recovered lower Tertiary through Aptian sedimentary rocks. The paleolatitudes of each hole from the late Aptian through Paleocene were derived from an extensive set of paleomagnetic minicores. Each sample underwent progressive thermal demagnetization, and the characteristic direction of magnetization was derived from the region of stable directions. True mean inclinations were computed for each lithologic unit and for each stage or pair of stages, using the method of Kono (1980b). The results yield average paleolatitudes of 1°S for the Paleocene-Maestrichtian, 7°S for the Santonian-Turonian, and 15°S for the Albian-late Aptian. The Aptian-Albian paleolatitudes agree with paleomagnetic results from DSDP Sites 462 and 289 in the western central Pacific. The average rate of northward drift by the site was about 30 km/m.y. through the Late Cretaceous and earliest Tertiary. The Maestrichtian paleolatitude agrees with a Pacific paleomagnetic pole computed by Gordon (1982) from North Pacific data, but the site is about 12° farther north than predicted by Campanian and Cenomanian North Pacific poles (Gordon, 1983; Gordon and Cox, 1980). Recovery of the latest Cretaceous-early Tertiary sediments was inadequate to allow unique determination of the magnetostratigraphy. No reversed interval could be identified within the late Aptian or early Albian.
    Keywords: 89-585; 89-585A; Calculated, see reference(s); Deep Sea Drilling Project; DRILL; Drilling/drill rig; DSDP; DSDP/ODP/IODP sample designation; Event label; Glomar Challenger; Inclination; Leg89; Lithologic unit/sequence; North Pacific/BASIN; Polarity; Quality code; Sample code/label; Sample comment; see reference(s); Stage
    Type: Dataset
    Format: text/tab-separated-values, 1376 data points
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  • 10
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    PANGAEA
    In:  Supplement to: Ogg, James G; Haggerty, Janet A; Sarti, Massimo; von Rad, Ulrich (1987): Lower Cretaceous pelagic sediments of Deep Sea Drilling Project Site 603, western North Atlantic: A synthesis. In: van Hinte, JE; Wise, SW Jr; et al. (eds.), Initial Reports of the Deep Sea Drilling Project, Washington (U.S. Govt. Printing Office), 93, 1305-1331, https://doi.org/10.2973/dsdp.proc.93.161.1987
    Publication Date: 2023-06-27
    Description: Pelagic sedimentation during the Early Cretaceous at Site 603 produced alternations of laminated marly limestone and bioturbated limestone--a facies typical of the "Blake-Bahama Formation" of the western Atlantic. This limestone is a nannofossil micrite, rich in calcified radiolarians, with variable amounts of organic matter, pyritized radiolarian tests, fish debris, and micaceous silt. The laminated marly limestone layers are enriched in organic matter when compared with the intervals of bioturbated limestone. The organic carbon is predominantly terrestrial plant debris; where the organic-carbon content is in excess of 1%, there is also a significant marine-derived component. Laminations can result either from bands of alternately enriched and depleted opaque material and clay, or from bands of elongate lenses (microflasers) of micrite, which could be plastically deformed pellets or diagenetic features. The alternating intervals of laminated and bioturbated structures may have resulted from combined changes in surface productivity, in the influx of terrigenous organic matter, and in the intensity of bottom circulation, which led to episodic oxygen depletion in the bottom water and sediments. Variations in the relative proportions of laminated clay-rich and bioturbated lime-rich limestone and in the development of cycles between these structures make it possible to subdivide the Lower Cretaceous pelagic facies into several subunits which appear to be regional in extent. Bioturbated limestone is dominant in the Berriasian, laminated marly limestone in the Valanginian and Barremian-lower Aptian, and well-developed alternations between these end members in the Hauterivian. The Hauterivian to lower Aptian sediments contain abundant terrigenous clastic turbidites associated with a submarine fan complex. These changes in the general characteristics of the pelagic sediment component of the Blake-Bahama Formation at Site 603 are synchronous with those in the Blake-Bahama Basin (Sites 534 and 391) to the south. Carbonate sedimentation ended in the early Aptian, probably because of a regional shoaling of the carbonate compensation depth.
    Keywords: 93-603B; Amorphous phase; Calcite; Calcium carbonate; Carbon, organic, total; Chlorite; Clay minerals; Clinoptilolite; Collinite; Color code HLS-system; Comment; Comment 2 (continued); Deep Sea Drilling Project; Diagenesis; DRILL; Drilling/drill rig; DSDP; DSDP/ODP/IODP sample designation; Element analyser CHN, LECO; Feldspar; Fish remains; Foraminifera, benthic; Foraminifera, planktic; Glomar Challenger; Grain size, maximum; Grain size description; Iron oxide; Kaolinite; Leg93; Lithologic unit/sequence; Lithology/composition/facies; Mica; Micrite; Mollusca; Munsell Color System (1994); Muscovite; Petrography description; Plant debris; Pyrite, FeS2; Quartz; Radiolarians; Rock fragments; Sample code/label; Smectite; Stage; Visual description; X-ray diffraction (XRD)
    Type: Dataset
    Format: text/tab-separated-values, 1233 data points
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