Marine rapid environmental/climatic change in the Cretaceous greenhouse world

Hu, Xiumian; Wagreich, Michael; Yılmaz, İsmail Ömer

doi:10.1016/j.cretres.2012.04.012

Cited by 66 publications

(44 citation statements)

References 55 publications

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“…Multiple causes have been suggested for their deposition, including intense transgressive periods from rapidly changing sea levels (Lipinski, Warning & Brumsack, 2003), tectonic activity restricting flow patterns and increasing productivity (Wignall & Hallam, 1991;Weissert et al, 1998), and decreased erosion rates and warmer, more arid climates (Kessels, Mutterlose & Ruffell, 2003;Föllmi, 2012). The Early Cretaceous saw several episodes of intense ocean water stagnation, possibly leading to anoxia, including the Valanginian Weissert and the late Hauterivian Faraoni oceanic anoxic events (Erba, Bartolini & Larson, 2004;Hu, Wagreich & Yilmaz, 2012;Mattioli et al, 2014). However, Kujau et al (2012) proposed that the Valanginian Weissert carbon excursion was not part of a global oceanic anoxic event, and that episodes of anoxia were instead restricted to the Atlantic, Pacific, and Southern Ocean, possibly with enhanced terrestrial carbon storage acting as the primary driver for the isotope excursion.…”

Section: (2) Sea Level and Stratigraphymentioning

confidence: 99%

Biotic and environmental dynamics through the Late Jurassic–Early Cretaceous transition: evidence for protracted faunal and ecological turnover

et al. 2016

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The Late Jurassic to Early Cretaceous interval represents a time of environmental upheaval and cataclysmic events, combined with disruptions to terrestrial and marine ecosystems. Historically, the Jurassic/Cretaceous (J/K) boundary was classified as one of eight mass extinctions. However, more recent research has largely overturned this view, revealing a much more complex pattern of biotic and abiotic dynamics than has previously been appreciated. Here, we present a synthesis of our current knowledge of Late Jurassic-Early Cretaceous events, focusing particularly on events closest to the J/K boundary. We find evidence for a combination of short-term catastrophic events, large-scale tectonic processes and environmental perturbations, and major clade interactions that led to a seemingly dramatic faunal and ecological turnover in both the marine and terrestrial realms. This is coupled with a great reduction in global biodiversity which might in part be explained by poor sampling. Very few groups appear to have been entirely resilient to this J/K boundary 'event', which hints at a 'cascade model' of ecosystem changes driving faunal dynamics. Within terrestrial ecosystems, larger, more-specialised organisms, such as saurischian dinosaurs, appear to have suffered the most. Medium-sized tetanuran theropods declined, and were replaced by larger-bodied groups, and basal eusauropods were replaced by neosauropod faunas. The ascent of paravian theropods is emphasised by escalated competition with contemporary pterosaur groups, culminating in the explosive radiation of birds, although the timing of this is obfuscated by biases in sampling. Smaller, more ecologically diverse terrestrial non-archosaurs, such as lissamphibians and mammaliaforms, were comparatively resilient to extinctions, instead documenting the origination of many extant groups around the J/K boundary. In the marine realm, extinctions were focused on low-latitude, shallow marine shelf-dwelling faunas, corresponding to a significant eustatic sea-level fall in the latest Jurassic. More mobile and ecologically plastic marine groups, such as ichthyosaurs, survived the boundary relatively unscathed. High rates of extinction and turnover in other macropredaceous marine groups, including plesiosaurs, are accompanied by the origin of most major lineages of extant sharks. Groups which occupied both marine and terrestrial ecosystems, including crocodylomorphs, document a selective extinction in shallow marine forms, whereas turtles appear to have diversified. These patterns suggest that different extinction selectivity and ecological processes were operating between marine and terrestrial ecosystems, which were ultimately important in determining the fates of many key groups, as well as the origins of many major extant lineages. We identify a series of potential abiotic candidates for driving these patterns, including multiple bolide impacts, several episodes of flood basalt eruptions, dramatic climate change, and major disruptions to oceanic systems. The J/K t...

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Section: (2) Sea Level and Stratigraphymentioning

confidence: 99%

Biotic and environmental dynamics through the Late Jurassic–Early Cretaceous transition: evidence for protracted faunal and ecological turnover

et al. 2016

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“…In particular, OAE 1a is marked by a complex C isotopic anomaly that has been recognized in the Tethys, North Atlantic, and Pacifi c Oceans (Weissert, 1989;Weissert and Lini, 1991;Grötsch, 1993;Bralower et al, 1994Bralower et al, , 1999Jenkyns, 1995;Vahrenkamp, 1996Vahrenkamp, , 2010Ferreri et al, 1997;Menegatti et al, 1998;Erba et al, 1999;Jenkyns and Wilson, 1999;Luciani et al, 2001;Ando et al, 2002;Bellanca et al, 2002;Price, 2003;Immenhauser et al, 2005;Millán et al, 2009;Hu et al, 2012a;Huck et al, 2012;Bottini et al, 2014), and in terrestrial sequences (Gröcke et al, 1999;Hesselbo et al, 2000;Jahren et al, 2001;Heimhofer et al, 2003). An initial negative spike documented in marine and terrestrial records suggests a large input of isotopically light carbon into the ocean-atmosphere system, perhaps due to intensifi ed volcanogenic CO 2 emissions during the GOJE (Larson, 1991a;Weissert and Lini, 1991;Bralower et al, 1994;Erba, 1994;Weissert et al, 1998;Menegatti et al, 1998;Larson and Erba, 1999;Price, 2003), methane liberation from gas-hydrate dissociation (Gröcke et al, 1999;Hesselbo et al, 2000;Jahren et al, 2001;Beerling et al, 2002;…”

Section: Mamentioning

confidence: 99%

“…Short-and long-term temperature changes have been reconstructed for the latest Barremian through Aptian time interval using micropaleontological proxies (e.g., Kemper, 1987;Premoli Silva et al, 1989a, 1999Hochuli et al, 1999;Herrle and Mutterlose, 2003;Heimhofer et al, 2004;Rückheim et al, 2006a;Mutterlose et al, 2009;Keller et al, 2011;McAnena et al, 2013;Bottini et al, 2014Bottini et al, , 2015, stable oxygen isotopes (Weissert and Lini, 1991;Jenkyns, 1995;Menegatti et al, 1998;Luciani et al, 2001;Bellanca et al, 2002;Price, 2003;Ando et al, 2008;Millán et al, 2009;Kuhnt et al, 2011;Jenkyns et al, 2012;Hu et al, 2012a;Price et al, 2012;Maurer et al, 2012;Bottini et al, 2014), and biomarkers (Schouten et al, 2003;Mutterlose et al, 2010;Keller et al, 2011;McAnena et al, 2013;Bottini et al, 2014Bottini et al, , 2015. A global warming marked OAE 1a, while generally cooler temperatures persisted in the late Aptian, as indicated by the presence of glendonites and possible ice-rafted debris at high latitudes (Kemper, 1987;Frakes and Francis, 1988;De Lurio and Frakes, 1999;Price, 1999).…”

Section: Mamentioning

confidence: 99%

Environmental consequences of Ontong Java Plateau and Kerguelen Plateau volcanism

Erba¹,

Duncan²,

Bottini³

et al.

The Origin, Evolution, and Environmental Impact of Oceanic Large Igneous Provinces

110

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The mid-Cretaceous was marked by emplacement of large igneous provinces (LIPs) that formed gigantic oceanic plateaus, affecting ecosystems on a global scale, with biota forced to face excess CO 2 resulting in climate and ocean perturbations. Volcanic phases of the Ontong Java Plateau (OJP) and the southern Kerguelen Plateau (SKP) are radiometrically dated and correlate with paleoenvironmental changes, suggesting causal links between LIPs and ecosystem responses. Aptian biocalcifi cation crises and recoveries are broadly coeval with C, Pb, and Os isotopic anomalies, trace metal infl uxes, global anoxia, and climate changes. Early Aptian greenhouse or supergreenhouse conditions were followed by prolonged cooling during the late Aptian, when OJP and SKP developed, respectively. Massive volcanism occurring at equatorial versus high paleolatitudes and submarine versus subaerial settings triggered very different climate responses but similar disruptions in the marine carbonate system. Excess CO 2 arguably induced episodic ocean acidifi cation that was detrimental to

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“…The Valanginian registered a positive C-isotope excursion of ~ 2‰ (Hu et al 2012, Weissert et al 1998, Funk et al 1993Föllmi 1996, Föllmi et al 2006, Gréselle & Pittet 2010). This isotopic excursion, which seems to be of global nature, has been related to the Weissert Oceanic Anoxic Event (Weissert et al 1998, Weissert & Erba 2004, Funk et al 1993, Föllmi 1996, Föllmi et al 2006, Gréselle & Pittet 2010.…”

Section: Depositional Age Of the Kesima Membermentioning

confidence: 99%

“…C-and Sr-isotope chemostratigraphy is an alternative tool for determining the depositional age of carbonate successions (Jacobsen & Kaufman 1999, Hu et al 2012, Föllmi et al 2006, Föllmi 2012. This paper reports the Cand Sr-isotope chemostratigraphy of a carbonate from the Kesima Member of the Palanz Formation from which its depositional age is constrained.…”

Section: Introductionmentioning

confidence: 99%

Sedimentology and chemostratigraphy of a Valanginian carbonate succession from the Baja Guajira Basin, northern Colombia

et al. 2016

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ABSTRACT:The Kesima Member of the Palanz Formation constitutes the first record of Cretaceous marine sedimentation along the Baja Guajira Basin, northern Colombia. Sedimentologic and petrographic analyses suggest a deposition along a coral reef dominated rimmed carbonate platform.87 Sr/ 86 Sr values between 0.707350 and 0.707400 suggest a Valanginian (136 -132 Ma) depositional age for the Kesima Member. A positive anomaly on the δ 13 C values of ~2.2‰ suggests that this rimmed carbonate platform registered the Valanginian Weissert oceanic anoxic event. Although the Weissert oceanic anoxic event resulted on a major drowning of the Circum Tethyan carbonate platforms, it seems to have not affected those from the Circum Caribbean, where several shallow marine carbonate platform successions crop out. The Kesima Member displays a change from an organically produced carbonate factory into an inorganically produced, ooids dominated, carbonate factory during the peak of the Weissert event δ 13 C anomaly. This change in the carbonate factory, which may represent a major perturbation of the marine carbonate budget along tropical settings during the Weissert event, coincides with a major decrease in global sea level. Finally, the age of the Kesima Member is considerably older than that of other Cretaceous carbonate successions cropping out in other northern South America sedimentary basins (i.e. Perija-Merida, Cesar-Rancheria). Differences in the timing of the Cretaceous marine incursion along northern South America, together with the differences in the Triassic-Jurassic stratigraphy of several sedimentary basins in northern South America, suggest that the Baja Guajira and Maracaibo basins remained as an isolated tectonic block separated from northern South America after the breakup of Pangea. KEYWORDS:

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Marine rapid environmental/climatic change in the Cretaceous greenhouse world

Cited by 66 publications

References 55 publications

Biotic and environmental dynamics through the Late Jurassic–Early Cretaceous transition: evidence for protracted faunal and ecological turnover

Biotic and environmental dynamics through the Late Jurassic–Early Cretaceous transition: evidence for protracted faunal and ecological turnover

Environmental consequences of Ontong Java Plateau and Kerguelen Plateau volcanism

Sedimentology and chemostratigraphy of a Valanginian carbonate succession from the Baja Guajira Basin, northern Colombia

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