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

Christian Linnert,Paul R Bown,Irene Pérez-Rodríguez,Maria Rose Petrizzo,Jackie A Lees,Stuart A Robinson,Hugh C Jenkyns,Francesca Falzoni,José A Arz

doi:10.1127/nos/51/2018/145

Abstract

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

Highlights

The early Late Cretaceous (Cenomanian – Turonian) was characterised by one of the warmest palaeoclimates of the past 140 million years (ʻhothouse climate: Wilson et al 2002, Hay 2008, 2011, Friedrich et al 2012, Kidder and Worseley 2012, MacLeod et al 2013)
The stratigraphic variations in total organic carbon (TOC) and %CaCO3 from the Shuqualak-Evans core are shown in Figure 2 and provided in Supplementary Table 1
Significant temporal offsets between the cooling of both bottom and surface waters and the negative carbon-isotope excursions (CIEs) suggest that a simple cause-and-effect relationship, such as might be imagined through glacio-eustasy, is unlikely

Summary

Introduction

The early Late Cretaceous (Cenomanian – Turonian) was characterised by one of the warmest palaeoclimates of the past 140 million years (ʻhothouse climate: Wilson et al 2002, Hay 2008, 2011, Friedrich et al 2012, Kidder and Worseley 2012, MacLeod et al 2013). It has been suggested that opening of the Equatorial Atlantic Seaway contributed to Late Cretaceous cooling by allowing cool southerncomponent waters to enter the warm North Atlantic Basin (e. g. Frank and Arthur 1999, Friedrich et al 2012)

Methods

Results

Discussion

Conclusion