Constraining paleo-latitude of a biogeographic boundary in mid-Panthalassa: Fusuline province shift on the Late Guadalupian (Permian) migrating seamount

Kasuya, Akihisa; Isozaki, Yukio; Igo, Hisayoshi

doi:10.1016/j.gr.2011.06.001

Cited by 40 publications

(25 citation statements)

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“…This calculation entails removal of the Signor-Lipps numbers restored to the Changhsingian. Possibly the Guadalupian event began before the end of the late Guadalupian (24,25), but close to the end of this interval there was heavy extinction of fusulinidoidean foraminiferans (13,(25)(26)(27). A recent thorough study of this group found that 88% its species that existed within the last million years of the Guadalupian became extinct by the end of this brief interval (27).…”

Section: Magnitudes Of Other Major Extinctionsmentioning

confidence: 99%

Estimates of the magnitudes of major marine mass extinctions in earth history

Stanley

2016

Proc. Natl. Acad. Sci. U.S.A.

253

134

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Procedures introduced here make it possible, first, to show that background (piecemeal) extinction is recorded throughout geologic stages and substages (not all extinction has occurred suddenly at the ends of such intervals); second, to separate out background extinction from mass extinction for a major crisis in earth history; and third, to correct for clustering of extinctions when using the rarefaction method to estimate the percentage of species lost in a mass extinction. Also presented here is a method for estimating the magnitude of the Signor-Lipps effect, which is the incorrect assignment of extinctions that occurred during a crisis to an interval preceding the crisis because of the incompleteness of the fossil record. Estimates for the magnitudes of mass extinctions presented here are in most cases lower than those previously published. They indicate that only ∼81% of marine species died out in the great terminal Permian crisis, whereas levels of 90-96% have frequently been quoted in the literature. Calculations of the latter numbers were incorrectly based on combined data for the Middle and Late Permian mass extinctions. About 90 orders and more than 220 families of marine animals survived the terminal Permian crisis, and they embodied an enormous amount of morphological, physiological, and ecological diversity. Life did not nearly disappear at the end of the Permian, as has often been claimed. mass extinction | paleontology | biodiversity A global mass extinction can be defined qualitatively as an event in which an unusually large percentage of higher taxa in several biological groups died out globally within a brief interval of geologic time. There is no satisfactory way to provide a universally applicable quantitative definition of a mass extinction. Major marine mass extinctions have been associated with relatively abrupt excursions of the stable carbon isotope ratio in seawater, as reflected in fossil skeletal material. Contemporaneous oxygen isotope excursions that have paralleled the carbon isotope excursions, as well as other forms of evidence, connect the biotic crises to global climate change and support other evidence that the crises were relatively sudden events (1). Most major pulses of extinction occurred at or near the ends of formally recognized geologic intervals. In fact, the resulting biotic transitions have led to the establishment of the boundaries between most geologic systems and many geologic stages. Any extinctions scattered within such an interval or within an interval not containing a mass extinction are known collectively as background extinction.Comparing models to empirical numbers, Foote (2) considered two extreme scenarios for extinctions in the marine realm: one in which all extinctions occurred in pulses, primarily at the ends of geologic ages (the intervals representing stages) and one in which they were spread throughout ages (see also ref.3). He found the pulsed model to be more strongly supported, which would imply that substantial backward smearing of extinctions ...

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Section: Magnitudes Of Other Major Extinctionsmentioning

confidence: 99%

Estimates of the magnitudes of major marine mass extinctions in earth history

Stanley

2016

Proc. Natl. Acad. Sci. U.S.A.

253

134

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“…4), occurring in 463 the Neoschwagerina craticulifera fusulinid assemblage zone (Kirschvink et al 2015). N. craticulifera 464 has its first appearance in the late Roadian (Henderson et al 2012), but Kasuya et al (2012) Lueckisporites virkkiae (Edwards et al 1997;Słowakiewicz et al 2009). Generally, the end of the 509…”

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confidence: 99%

A geomagnetic polarity timescale for the Permian, calibrated to stage boundaries

Hounslow

Balabanov

2016

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The reverse polarity Kiaman Superchron has strong evidence for at least three, or probably four, normal magnetochrons during the early Permian. Normal magnetochrons are during the early Asselian (base CI1r.1n at 297.94±0.33 Ma), late Artinskian (CI2n at 281.24±2.3 Ma), mid-Kungurian (CI3n at 275.86±2.0 Ma) and Roa"dian (CI3r.an at 269.54±1.6 Ma). The mixed-polarity Illawarra Superchron begins in the early Wordian at 266.66±0.76 Ma. The Wordian–Capitanian interval is biased to normal polarity, but the basal Wuchiapingian begins the beginning of a significant reverse polarity magnetochron LP0r, with an overlying mixed-polarity interval through the later Lopingian. No significant magnetostratigraphic data gaps exist in the Permian geomagnetic polarity record. The early Cisuralian magnetochrons are calibrated to a succession of fusulinid zones, the later Cisuralian and Guadalupian to a conodont and fusulinid biostratigraphy, and Lopingian magnetochrons to conodont zonations. Age calibration of the magnetochrons is obtained through a Bayesian approach using 35 radiometric dates, and 95% confidence intervals on the ages and chron durations are obtained. The dating control points are most numerous in the Gzhelian–Asselian, Wordian and Changhsingian intervals. This significant advance should provide a framework for better correlation and dating of the marine and non-marine Permian.

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“…The Akasaka Limestone originated in a paleo-atoll complex deposited on a paleoseamount in the low-latitude superocean of Panthalassa (Figure 4), secondarily was transported northward by the plate motion, and was consequently accreted to the Jurassic continental margin of Japan (South China) (e.g. Kasuya et al, 2012;Kofukuda et al, 2014). The gastropod fauna thus provides paleoenvironmental information for the Permian mid-Panthalassa but tells us nothing about Permian Japan per se.…”

Section: Discussionmentioning

confidence: 99%