Late Albian paleoceanography of the western subtropical North Atlantic

A late Albian-early Cenomanian record (∼103.3 to 99.0 Ma), including organic-rich deposits and a δ13C increase associated with oceanic anoxic event 1d (OAE 1d), is described from Ocean Drilling Program sites 1050 and 1052 in the subtropical Atlantic. Foraminifera are well preserved at these sites. P...

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Bibliographic Details
Published in:Paleoceanography
Main Authors: Petrizzo M. R., Huber B. T., Wilson P. A., MacLeod K. G.
Other Authors: M.R. Petrizzo, B.T. Huber, P.A. Wilson, K.G. MacLeod
Format: Article in Journal/Newspaper
Language:English
Published: American Geophysical Union 2008
Subjects:
oceanic anoxic event
seawater carbonate concentration
living planktonic-faraminifera
organic-matter
vertical-distribution
isotopic composition
se France
evolution
oxygen
circulation
Settore GEO/01 - Paleontologia e Paleoecologia
North Atlantic
Planktonic foraminifera
Online Access:http://hdl.handle.net/2434/761808
https://doi.org/10.1029/2007PA001517
Description
Summary:A late Albian-early Cenomanian record (∼103.3 to 99.0 Ma), including organic-rich deposits and a δ13C increase associated with oceanic anoxic event 1d (OAE 1d), is described from Ocean Drilling Program sites 1050 and 1052 in the subtropical Atlantic. Foraminifera are well preserved at these sites. Paleotemperatures estimated from benthic δ18O values average ∼14°C for middle bathyal Site 1050 and ∼17°C for upper bathyal Site 1052, whereas surface temperatures are estimated to have ranged from 26°C to 31°C at both sites. Among planktonic foraminifera, there is a steady balance of speciation and extinction with no discrete time of major faunal turnover. OAE 1d is recognized on the basis of a 1.2‰ δ13C increase (∼100.0-99.6 Ma), which is similar in age and magnitude to δ13 C excursions documented in the North Atlantic and western Tethys. Organic-rich "black shales" are present throughout the studied interval at both sites. However, deposition of individual black shale beds was not synchronous between sites, and most of the black shale was deposited before the OAE 1d δ13C increase. A similar pattern is observed at the other sites where OAE 1d has been recognized indicating that the site(s) of excess organic carbon burial that could have caused the δ13C increase has (have) yet to be found. Our findings add weight to the view that OAEs should be chemostratigraphically (δ13C) rather than lithostratigraphically defined.

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