Phanerozoic Large Igneous Provinces (LIPs), HEATT (Haline Euxinic Acidic Thermal Transgression) episodes, and mass extinctions

Kidder, David L.; Worsley, Thomas R.

doi:10.1016/j.palaeo.2010.05.036

Cited by 185 publications

(135 citation statements)

References 260 publications

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“…Modelling of the CIEs performed by Kump and Arthur (1999) shows that δ 13 C positive excursions can also be due to an increase in the rate of phosphate or phosphate and inorganic carbon delivery to the ocean, and that large positive excursions in the isotopic composition of the ocean can also result from an increase in the proportion of carbonate weathering relative to organic carbon and silicate weathering. Other authors argue that an increase of δ 13 C in bulk organic carbon may reflect a massive expansion of marine archaea bacteria that do not isotopically discriminate in the type of carbon they use, giving rise to positive δ 13 C shifts (Kidder and Worsley, 2010).…”

Section: Carbon Isotope Curvementioning

confidence: 99%

Palaeoclimatic oscillations in the Pliensbachian (Early Jurassic) of the Asturian Basin (Northern Spain)

Gómez

Comas-Rengifo²,

Goy

2016

Clim. Past

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Abstract. One of the main controversial themes in palaeoclimatology involves elucidating whether climate during the Jurassic was warmer than the present day and if it was the same over Pangaea, with no major latitudinal gradients. There has been an abundance of evidence of oscillations in seawater temperature throughout the Jurassic. The Pliensbachian (Early Jurassic) constitutes a distinctive time interval for which several seawater temperature oscillations, including an exceptional cooling event, have been documented. To constrain the timing and magnitude of these climate changes, the Rodiles section of the Asturian Basin (Northern Spain), a well exposed succession of the uppermost Sinemurian, Pliensbachian and Lower Toarcian deposits, has been studied. A total of 562 beds were measured and sampled for ammonites, for biochronostratigraphical purposes, and for belemnites, to determine the palaeoclimatic evolution through stable isotope studies. Comparison of the recorded latest Sinemurian, Pliensbachian and Early Toarcian changes in seawater palaeotemperature with other European sections allows characterization of several climatic changes that are likely of a global extent. A warming interval partly coinciding with a δ 13 C bel negative excursion was recorded at the Late Sinemurian. After a "normal" temperature interval, with temperatures close to average values of the Late Sinemurian-Early Toarcian period, a new warming interval containing a short-lived positive δ 13 C bel peak, developed during the Early-Late Pliensbachian transition. The Late Pliensbachian represents an outstanding cooling interval containing a δ 13 C bel positive excursion interrupted by a small negative δ 13 C bel peak. Finally, the Early Toarcian represented an exceptional warming period, which has been pointed out as being responsible for the prominent Early Toarcian mass extinction.

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Section: Carbon Isotope Curvementioning

confidence: 99%

Palaeoclimatic oscillations in the Pliensbachian (Early Jurassic) of the Asturian Basin (Northern Spain)

Gómez

Comas-Rengifo²,

Goy

2016

Clim. Past

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“…to greenhouse levels and temperatures, providing positive warming feedbacks and the development of hothouse conditions (Kidder and Worsley, 2010). Extrusion of the massive Siberian Traps at the end of the Permian may have initiated the greenhouse to hothouse transition (Reichow et al, 2009).…”

Section: Paleoclimate Implicationsmentioning

confidence: 99%

“…High latitude forests are of special interest, as forests in these regions are especially sensitive to climate change. Ancient high paleolatitude forests give insight into forest distribution, structure, and carbon cycling during periods of greenhouse, icehouse, and hothouse conditions and during transitions between climate states (Kidder and Worsley, 2010). …”

Section: Introductionmentioning

confidence: 99%

“…The Permian succession in the Beardmore Glacier area of the Central Transantarctic Mountains reflects a transition in the Permian from icehouse to greenhouse to hothouse conditions (e.g., Kidder and Worsley, 2004;2010;Shi and Waterhouse, 2010 (Bond et al, 2010;Shi and Waterhouse, 2010;Kidder and Worsley, 2010;Joachimski et al, 2012). Unfortunately, there is insufficient biostratigraphic control and radiometric dating to closely link the Lamping Peak forests in time to these events.…”

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confidence: 99%

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Highly productive polar forests from the Permian of Antarctica

Miller

Knepprath

Cantrill

et al. 2016

Palaeogeography, Palaeoclimatology, Palaeoecology

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Two stratigraphically closely spaced bedding planes exposed at Lamping Peak in the Upper Buckley Formation, Beardmore Glacier area, Antarctica contain abundant in situ stumps (n=53, n=21) and other plant fossils that allow reconstruction of forest structure and biomass of Glossopteris forests that thrived at Presence of these highly productive fossil forests at high paleolatitude is consistent with hothouse conditions during the Late Permian, prior to the eruption of the Siberian flood basalts.

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“…2) deposited in a broad swathe of sedimentary environments from lakes to the abyssal plains of the ocean (Arthur, 1979;Jenkyns, 1980;Waples, 1983;Bohacs et al, 2000;Tyson, 2005). Depending on sedimentary environment, black shales can be deposited by any one or combination of processes that control fine-grained sedimentation: pelagic settling, hemipelagic deposition (including lateral advection of sediment), hemiturbiditic and Extinction of marine genera and major OAEs Raup & Sepkoski, 1986 87 Petroleum reserves generated by source rocks Klemme & Ulmishek, 1991 Oil Gas Climate mode Frakes et al, 1992 G r e e n h o u s e G r e e n h o u s e G r e e n h o u s e I c e h o u s e (Gradstein et al, 2004), climate mode (Frakes et al, 1992), major orogenic intervals, magnetic field reversals (Ogg et al, 2008), oceanic crust production (Stanley, 1999) and LIP aereal extent (Kidder and Worsley, 2010), carbon isotope curve (Prokoph et al, 2008), strontium isotope curve (McArthur, 2010), RCO 2 and CO 2 proxy record (Berner, 2006;Royer, 2006), global temperature (Frakes et al, 1992), eustatic sea level stand (Exxon curve; Haq et al, 1987;Haq and Al-Qahtani, 2005;Miller et al, 2005), continental glaciations (Ridgwell, 2005), extinction of marine genera and major oceanic anoxic events (OAEs) (Raup and Sepkoski, 1986), petroleum reserves generated by source rocks (Klemme and Ulmishek, 1991), and passive margin extension (Bradley, 2008).…”

Section: Introductionmentioning

confidence: 99%

Phanerozoic environments of black shale deposition and the Wilson Cycle

Trabucho‐Alexandre

Hay²,

Boer

2012

Solid Earth

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Abstract. The spatial and temporal distribution of black shales is related to the development of environments in which they accumulate and to a propitious combination of environmental variables. In recent years, much has been done to improve our understanding of the mechanisms behind the temporal distribution of black shales in the Phanerozoic and of the environmental variables that result in their deposition. However, the interpretation of ancient black shale depositional environments is dominated by an oversimplistic set of three depositional models that do not capture their complexity and dynamics. These three models, the restricted circulation, the (open) ocean oxygen minimum and the continental shelf models, are an oversimplification of the variety of black shale depositional environments that arise and coexist throughout the course of a basin's Wilson Cycle, i.e. the dynamic sequence of events and stages that characterise the evolution of an ocean basin, from the opening continental rift to the closing orogeny. We examine the spatial distribution of black shales in the context of the Wilson Cycle using examples from the Phanerozoic. It is shown that the geographical distribution of environments of black shale deposition and the position of black shales in the basin infill sequence strongly depend on basin evolution, which controls the development of sedimentary environments where black shales may be deposited. The nature of the black shales that are deposited, i.e. lithology and type of organic matter, also depends on basin evolution and palaeogeography. We propose that in studies of black shales more attention should be given to the sedimentary processes that have led to their formation and to the interpretation of their sedimentary environments.

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Phanerozoic Large Igneous Provinces (LIPs), HEATT (Haline Euxinic Acidic Thermal Transgression) episodes, and mass extinctions

Cited by 185 publications

References 260 publications

Palaeoclimatic oscillations in the Pliensbachian (Early Jurassic) of the Asturian Basin (Northern Spain)

Palaeoclimatic oscillations in the Pliensbachian (Early Jurassic) of the Asturian Basin (Northern Spain)

Highly productive polar forests from the Permian of Antarctica

Phanerozoic environments of black shale deposition and the Wilson Cycle

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