A stable and hot Turonian without glacial δ18O excursions is indicated by exquisitely preserved Tanzanian foraminifera

MacLeod, Kenneth G.; Huber, Brian T.; Berrocoso, Álvaro Jiménez; Wendler, Ines

doi:10.1130/g34510.1

Cited by 104 publications

(67 citation statements)

References 26 publications

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“…Note the Tanzanian planktonic foraminifera1225 have not been sorted by depth ecology, and consequently the range of SSTs calculated likely encompasses estimates from mixed-layer to thermocline-dwelling species. It is likely that the warmest temperatures are most representative of mixed-layer conditions.…”

Section: Figurementioning

confidence: 99%

Evidence for global cooling in the Late Cretaceous

et al. 2014

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The Late Cretaceous ‘greenhouse’ world witnessed a transition from one of the warmest climates of the past 140 million years to cooler conditions, yet still without significant continental ice. Low-latitude sea surface temperature (SST) records are a vital piece of evidence required to unravel the cause of Late Cretaceous cooling, but high-quality data remain illusive. Here, using an organic geochemical palaeothermometer (TEX86), we present a record of SSTs for the Campanian–Maastrichtian interval (~83–66 Ma) from hemipelagic sediments deposited on the western North Atlantic shelf. Our record reveals that the North Atlantic at 35 °N was relatively warm in the earliest Campanian, with maximum SSTs of ~35 °C, but experienced significant cooling (~7 °C) after this to <~28 °C during the Maastrichtian. The overall stratigraphic trend is remarkably similar to records of high-latitude SSTs and bottom-water temperatures, suggesting that the cooling pattern was global rather than regional and, therefore, driven predominantly by declining atmospheric pCO2 levels.

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Section: Figurementioning

confidence: 99%

Evidence for global cooling in the Late Cretaceous

et al. 2014

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“…Since 2002, a major focus of the Tanzania Drilling Project (TDP) has been to study Late Cretaceous-Neogene climates using outcrop and cored sediment samples from southeastern Tanzania (Fig. 1), a well-known province for the occurrence of calcareous microfossils with excellent preservation (Pearson et al, 2001Bown, 2005a;Lees, 2007;Bown et al, 2008;Jiménez Berrocoso et al, 2010Falzoni and Petrizzo, 2011;Petrizzo et al, 2011;Wendler et al, 2011Falzoni et al, 2013;MacLeod et al, 2013;Wendler and Bown, 2013;Huber and Petrizzo, 2014;Haynes et al, 2015;Lees and Bown, 2014). The excellent preservation of microfossils has been attributed to shallow burial of sediments that are clay rich and relatively impermeable (e.g., Pearson et al, 2004Pearson et al, , 2006Nicholas et al, 2006Nicholas et al, , 2007.…”

Section: Introductionmentioning

confidence: 98%

The Lindi Formation (upper Albian–Coniacian) and Tanzania Drilling Project Sites 36–40 (Lower Cretaceous to Paleogene): Lithostratigraphy, biostratigraphy and chemostratigraphy

Berrocoso

Huber

MacLeod

et al. 2015

Journal of African Earth Sciences

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“…This isotope anomaly, however, occurs well below the bases of the two index taxa Radotruncana calcarata (planktonic foraminifer, 89.89 m) and Uniplanarius trifidus (calcareous nannofossil, 91.44 m; Linnert et al 2014), which constrain the stratigraphic position of the LCE at other localities. According to data from those other localities, the LCE appears within (Gubbio, Italy and Shatsky Rise, NW Pacific), or above (Tercis, France and Tibet), the R. calcarata planktonic foraminiferal zone (Wendler et al 2011, Voigt et al 2012, Wendler 2013. Thus, it is unlikely that the δ 13 C excursion below ~90 m represents the LCE, as defined by Voigt et al (2012), unless a minor hiatus exists.…”

Section: Carbon-isotope Stratigraphy and Refinement Of The Age-model mentioning

confidence: 99%

“…Previous high-resolution studies of Upper Cretaceous carbon-isotope stratigraphy (e. g. Jarvis et al 2002, Voigt et al 2010, Thibault et al 2012a, b, Wendler 2013 have revealed five to seven stratigraphically significant carbon-isotope excursions (CIEs) in the Santonian -Maastrichtian interval. These excursions include the Santonian -Campanian Boundary Event (SCBE, positive excursion), the LCE (negative excursion), the CMBE (negative excursion), the MidMaastrichtian Event (MME, a two step positive excursion) and the Cretaceous -Paleogene Boundary Event (KPgE, major negative excursion; e. g. Jarvis et al 2002, Voigt et al 2010.…”

Section: Carbon-isotope Stratigraphy and Refinement Of The Age-model mentioning

confidence: 99%

Did Late Cretaceous cooling trigger the Campanian–Maastrichtian Boundary Event?

Linnert¹,

Robinson²,

Lees³

et al. 2018

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Abstract. The Campanian-Maastrichtian (83-66 Ma) was a period of global climate cooling, featuring significant negative carbon-isotope (δ 13 C) anomalies, such as the Late Campanian Event (LCE) and the Campanian-Maastrichtian Boundary Event (CMBE). A variety of factors, including changes in temperature, oceanic circulation and gateway opening, have been invoked to explain these δ 13 C perturbations, but no precise mechanism has yet been well constrained. In order to improve our understanding of these events, we measured stable carbon and oxygen isotopes of hemipelagic sediments from the Shuqualak-Evans cored borehole (Mississippi, USA) and compared the data with previously published sea-surface temperature (SST) estimates from the same core. We found that the CMBE can be recognised, unambiguously, in the ShuqualakEvans core, and that it is associated with an interval of cooler SSTs suggesting a possible mechanistic link between palaeotemperature change and this event. Determining the precise position of the LCE in the Shuqualak-Evans core is more problematic, but it may also be associated with cooler SSTs. Our combined records of carbon cycling and SSTs compare well with other studies and provide evidence that cooling during the CMBE (and possibly LCE) was global in nature and affected surface waters, in addition to the deep-ocean. We suggest that short-term cooling drove intensification of high-latitude deep-water formation, which in turn led to changes in the ratio of carbonate to organic carbon burial that led to a negative δ 13 C excursion. Critically, the absence of warming during these intervals implies that the Late Cretaceous events must not have been associated with an appreciable increase in atmospheric pCO 2 , and was likely associated with decreased pCO 2 .

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A stable and hot Turonian without glacial δ18O excursions is indicated by exquisitely preserved Tanzanian foraminifera

Cited by 104 publications

References 26 publications

Evidence for global cooling in the Late Cretaceous

Evidence for global cooling in the Late Cretaceous

The Lindi Formation (upper Albian–Coniacian) and Tanzania Drilling Project Sites 36–40 (Lower Cretaceous to Paleogene): Lithostratigraphy, biostratigraphy and chemostratigraphy

Did Late Cretaceous cooling trigger the Campanian–Maastrichtian Boundary Event?

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