Upper Precambrian and lower Cambrian strata in the southern Great Basin, California and Nevada

Stewart, John H.

doi:10.3133/pp620

Cited by 141 publications

(222 citation statements)

References 17 publications

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“…The depositional environment of the Great Basin is relatively well known and three major environments are recognized; inner, middle and outer shelf facies (Stewart, 1970;Webster, 2011). Although brachiopods are known from all three facies belts, the distributions of individual taxa remain poorly understood, and a detailed discussion of this topic is presently impossible.…”

Section: Western Laurentiamentioning

confidence: 99%

Depth related brachiopod faunas from the lower Cambrian Forteau Formation of southern Labrador and western Newfoundland, Canada

Skovsted

Knight

Balthasar³

2017

Palaeontologia Electronica

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Section: Western Laurentiamentioning

confidence: 99%

Depth related brachiopod faunas from the lower Cambrian Forteau Formation of southern Labrador and western Newfoundland, Canada

Skovsted

Knight

Balthasar³

2017

Palaeontologia Electronica

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“…3). The ages of these units are well-constrained through temporal correlations built upon biostratigraphic, chemostratigraphic and radiometric data (Stewart, 1970;Stewart et al, 1984;ChristieBlick and Levy, 1989;Heaman and Grotzinger, 1992;Corsetti and Hagadorn, 2000;Jenkins et al, 2002;Corsetti and Kaufman, 2003;Zhou et al, 2004;Jiang et al, 2007;Sour-Tovar et al, 2007;Loyd et al, 2012b). Fig.…”

Section: Geologic Contextmentioning

confidence: 99%

Evolution of Neoproterozoic Wonoka–Shuram Anomaly-aged carbonates: Evidence from clumped isotope paleothermometry

Loyd

Corsetti

Eagle

et al. 2015

Precambrian Research

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a b s t r a c tThe Wonoka-Shuram Anomaly represents the largest negative carbon isotope excursion recognized in the geologic record and is associated with the emergence and diversification of metazoan life ca. 580 million years ago (Ma). The origin of the anomaly is highly debated, with interpretations ranging from primary to diagenetic, each having unique and potentially transformative implications for early life. Here, we apply carbonate clumped isotope thermometry to three sections expressing the anomaly in order to constrain mineral formation temperatures and thus directly calculate water oxygen isotope compositions (␦ 18 O w ) with which carbonate minerals equilibrated. With ␦ 18 O w known, it is possible to address previous hypotheses for the origin of the anomaly. In each section, precipitation temperatures correlate positively with reconstructed ␦ 18 O w . Previous hypotheses, based on the covariance of ␦ 18 O carb vs. ␦ 13 C carb (uncorrected for temperature effects), suggested a meteoric diagenetic origin for the anomaly. However, reconstructed ␦ 18 O w values do not covary with carbon isotope compositions (␦ 13 C carb ) within anomaly facies. Rather, the oxygen isotope and temperature data are consistent with carbonate recrystallization and equilibration under increasingly rock-buffered conditions. Based on simple modeling and comparison to modern formation fluids, recrystallization may have occurred in an environment far removed from the initial depositional or early diagenetic regime. In addition, although clumped isotope temperatures vary significantly and reach elevated values consistent with burial diagenesis, it is unclear to what degree, if at all, carbon isotope values were reset during recrystallization. Ultimately, these new data indicate that Wonoka-Shuram-aged carbonates experienced equilibration with fluids under increasingly closedsystem conditions. The clumped isotope data do not provide a means to distinguish previous hypotheses outright, but provide additional context for the evaluation of geochemical signatures within these ancient carbonate rocks.

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“…1, 2). Based on lithofacies and trilobite distribution patterns, the depositional environment is separated into inner, middle, and outer shelf facies realms (e.g., Stewart, 1970;Palmer and Halley, 1979;Sundberg and McCollum, 2003a;Sundberg, 2011;Webster, 2011a;Figs. 1, 2).…”

Section: General Geology and Stratigraphymentioning

confidence: 99%

“…The Dyeran Mule Spring Limestone is represented by predominately shallow subtidal-intertidal carbonates and is subdivided into: (1) a lower unit, composed of cliff-forming bioturbated limestone; (2) a middle unit, composed of bioclastic, oncolitic, oolitic, and peloidal limestones with numerous claystone intercalations; and (3) an upper cliff-forming unit composed of oncolitic and fenestral limestones with intercalated intraformational conglomerates ( Fig. 2; Nelson, 1962;Stewart, 1970;Albers and Stewart, 1972;Webster, 2011a, b). The Mule Spring Limestone is overlain by the siliciclastic and carbonate, partly highly condensed Emigrant Formation (uppermost Dyeran-Sunwaptan Stage) in western Nevada and by the Monola Formation in Death Valley National Park of eastern California (e.g., Palmer, 1971;Palmer and Halley, 1979;Sundberg, 2011;Sundberg et al, 2011).…”

Section: General Geology and Stratigraphymentioning

confidence: 99%

Small shelly fossils from the Montezuman–Delamaran of the Great Basin in Nevada and California

Wotte¹,

Sundberg²

2017

J. Paleontol.

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Upper Precambrian and lower Cambrian strata in the southern Great Basin, California and Nevada

Cited by 141 publications

References 17 publications

Depth related brachiopod faunas from the lower Cambrian Forteau Formation of southern Labrador and western Newfoundland, Canada

Depth related brachiopod faunas from the lower Cambrian Forteau Formation of southern Labrador and western Newfoundland, Canada

Evolution of Neoproterozoic Wonoka–Shuram Anomaly-aged carbonates: Evidence from clumped isotope paleothermometry

Small shelly fossils from the Montezuman–Delamaran of the Great Basin in Nevada and California

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