Geochemistry of a 1.2 Ga carbonate-evaporite succession, northern Baffin and Bylot Islands: implications for Mesoproterozoic marine evolution

Kah, L. C.; Lyons, Timothy W.; Chesley, John T.

doi:10.1016/s0301-9268(01)00161-9

Cited by 196 publications

(163 citation statements)

References 127 publications

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“…The period when the Amazonian Craton separated from Pehrsson et al (2016), positioned by the MacKenzie dykes pole (Buchan & Halls 1990). (B) Reconstruction at 1200 Ma -Laurentia and Amazonia/West Africa were constrained by the Upper Bylot (Fahrig et al 1981, Kah et al 2001 and Nova Floresta poles (Tab. 1), respectively.…”

Section: The Amazonian Craton In Gondwanamentioning

confidence: 99%

Paleomagnetism of the Amazonian Craton and its role in paleocontinents

et al. 2016

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In the last decade, the participation of the Amazonian Craton on Precambrian supercontinents has been clarified thanks to a wealth of new paleomagnetic data. Paleo to Mesoproterozoic paleomagnetic data favored that the Amazonian Craton joined the Columbia supercontinent at 1780 Ma ago, in a scenario that resembled the South AMerica and BAltica (SAMBA) configuration. Then, the mismatch of paleomagnetic poles within the Craton implied that either dextral transcurrent movements occurred between Guiana and Brazil-Central Shield after 1400 Ma or internal rotation movements of the Amazonia-West African block took place between 1780 and 1400 Ma. The presently available late-Mesoproterozoic paleomagnetic data are compatible with two different scenarios for the Amazonian Craton in the Rodinia supercontinent. The first one involves an oblique collision of the Amazonian Craton with Laurentia at 1200 Ma ago, starting at the present-day Texas location, followed by transcurrent movements, until the final collision of the Amazonian Craton with Baltica at ca. 1000 Ma. The second one requires drifting of the Amazonian Craton and Baltica away from the other components of Columbia after 1260 Ma, followed by clockwise rotation and collision of these blocks with Laurentia along Grenvillian Belt at 1000 Ma. Finally, although the time Amazonian Craton collided with the Central African block is yet very disputed, the few late Neoproterozoic/Cambrian paleomagnetic poles available for the Amazonian Craton, Laurentia and other West Gondwana blocks suggest that the Clymene Ocean separating these blocks has only closed at late Ediacaran to Cambrian times, after the Amazonian Craton rifted apart from Laurentia at ca. 570 Ma.

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Section: The Amazonian Craton In Gondwanamentioning

confidence: 99%

Paleomagnetism of the Amazonian Craton and its role in paleocontinents

et al. 2016

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“…For instance, carbonate sequences from Siberia (Bartley et al 2001) and Canada (Kah et al 1999) On the other hand, the age of the positive isotopic plateau (3-4 • / •• PDB ) preceding the above mentioned positive excursion was constrained based on a Pb-Pb isochron for carbonates from Siberia, which yield an age of 1.03 Ga (Ovchinnikova et al 1995). Additional age data, based on isotopic analyses of glauconite-illite series minerals, provided an age of near 1.17 Ga for the stratigraphic levels presenting this isotopic plateau in the Kerpyl Group, Siberia (Bartley et al 2001 (Kah et al ,1999) Siberia Mesoproterozoic data supplemented the data obtained by Kah et al (2001), who reported values between 0.7052 and 0.706 from Mesoproterozoic carbonates of the Bylot Supergroup in Canada, as well as from gypsum successions of the Society Cliffs Formation in Canada. Nevertheless, Gorokhov et al (1995) reported increasing 87 Sr/ 86 Sr ratios, from 0.706 to 0.7065, obtained in middle-late Riphean (MesoNeoproterozoic transition) successions in Siberia.…”

Section: Regional Implications Of the São Caetano Complex C And Sr Ismentioning

confidence: 52%

“…These values perfectly meet the unaltered ratio ranges proposed by Bartley et al (2001) for unaltered limestone sequences in Siberia, and are in close agreement with those lying in the field of unaltered samples (Sr contents > 1000 ppm) proposed by Brand and Veizer (1980a). Additionally, most of the obtained Sr values fall within the unaltered range (1100 and 1400 ppm) that Kah et al (1999Kah et al ( , 2001 proposed as representative of pristine seawater composition in Meso-Neoproterozoic limestone sequences located in Canada.…”

Section: Constraining Post-depositional Isotopic Alterationmentioning

confidence: 53%

“…It has been proposed, for example, that such an increase in the seawater Sr-isotope composition (from ∼ 0.704 to ∼ 0.707) occurring between the early Mesoproterozoic and early Neoproterozoic seems to have occurred as a result of changes in the global tectonic activity (Veizer et al 1992, Hall and Veizer 1996, Bartley et al 2001. For instance, the lowest values observed during the early Mesoproterozoic have been associated to widespread early Riphean rifting activity (Veizer et al 1992) whereas the high radiogenic values obtained for the late Mesoproterozoic-early Neoproterozoic time span have been attributed to enhanced continental Sr inputs during the onset of the agglutination of Rodinia supercontinent and associate orogenic events (Bartley et al 2001, Kah et al 2001.…”

Section: Global Implications Of the Late Mesoproterozoic-early Neopromentioning

confidence: 98%

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C- and Sr-isotope stratigraphy of the São Caetano complex, Northeastern Brazil: a contribution to the study of the Meso-Neoproterozoic seawater geochemistry

Silva

Sial

Ferreira

et al. 2005

An. Acad. Bras. Ciênc.

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C-isotope and 87 Sr/ 86 Sr values for five carbonate successions from the São Caetano Complex, northeastern Brazil, were used to constrain their depositional age and to determine large variations in the C-and Srisotopic composition of seawater under the framework of global tectonic events. Three C-isotope stages were identified from base to top in a composed chemostratigraphic section: (1) The C-and Sr-chemostratigraphic pathways permit to state: (a) the C-and Sr-isotope secular curves registered primary fluctuations of the isotope composition of seawater during late Mesoproterozoic-early Neoproterozoic transition in the Borborema Province, and (b) onset of the Cariris Velhos/Greenville cycle, widespread oceanic rifting, continental magmatic arc formation and onset of the agglutination of Rodinia supercontinent, mostly controlled the C-and Sr-isotope composition of seawater during the C-isotope stages 1, 2 and 3.

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“…Because of the possible complex postdepositional history of carbonates in the study area, we expected that all samples would show geochemical evidence and nonalteration; however, many carbon isotopic studies of Paleozoic and Proterozoic carbonates have shown that carbon isotopic composition is less sensitive to diagenetic alteration than are δ 18 Previous results indicated that δ 18 O values in Precambrian carbonates generally ranged from approximately −6 to −9‰ except in samples formed in evaporated marine environments [20,21]. The current δ 18 O results reveal a higher trend in dolomite than in limestone.…”

Section: Diagenesismentioning

confidence: 99%

Carbon and Oxygen Isotopic Stratigraphy of Mesoproterozoic Carbonate Sequences (1.6–1.4 Ga) from Yanshan in North China

Kuang

Liu

Jiahua

et al. 2011

International Journal of Oceanography

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In Yanshan, located in the northern part of North China, Mesoproterozoic carbonate sequences (1.6-1.4 Ga) form a 10, 000 m thick succession in an aulacogen basin. Carbon and oxygen isotope (δ 13 O and δ 18 O, resp.) data were obtained from 110 carbonate samples across three sections of these Mesoproterozoic deposits. From the early to late Mesoproterozoic, low negative values of δ 13 O appear, followed by low positive variation and then a stable increase. An abrupt decrease in δ 13 O values, with subsequent rapid increase, is found at the end of the Mesoproterozoic. During the whole Mesoproterozoic, δ 18 O shows a mainly negative trend and occasional highly negative isotopic shifts (from lower to upper deposits). Whole-rock carbon and oxygen isotopic compositions and profiles must be studied to provide a paleogeochemical record that can be associated with paleocean sedimentary environments, temperature, biological productivity, and sea-level fluctuations. Results of the present study correlate well with other international carbon and oxygen isotope profiles, suggesting that a global marine geochemical system existed during the interval of 1.6-1.4 Ga under a globally united tectonic, sedimentary, and geochemical background.

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Geochemistry of a 1.2 Ga carbonate-evaporite succession, northern Baffin and Bylot Islands: implications for Mesoproterozoic marine evolution

Cited by 196 publications

References 127 publications

Paleomagnetism of the Amazonian Craton and its role in paleocontinents

Paleomagnetism of the Amazonian Craton and its role in paleocontinents

C- and Sr-isotope stratigraphy of the São Caetano complex, Northeastern Brazil: a contribution to the study of the Meso-Neoproterozoic seawater geochemistry

Carbon and Oxygen Isotopic Stratigraphy of Mesoproterozoic Carbonate Sequences (1.6–1.4 Ga) from Yanshan in North China

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