Foraminiferal oxygen and carbon isotope data for DSDP Sites 32-305 and 62-463 and ODP Sites 171-1049 and 171-1050

Oxygen isotope analyses of well-preserved foraminifera from Blake Nose (30°N paleolatitude, North Atlantic) and globally distributed deep-sea sites provide a long-term paleotemperature record for the late Albian-Maastrichtian interval that is difficult to reconcile with the existence of significant...

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Bibliographic Details
Main Authors: Huber, Brian T, Norris, Richard D, MacLeod, Kenneth G
Format: Other/Unknown Material
Language:English
Published: PANGAEA 2002
Subjects:
171-1049
171-1050
32-305
62-463
Blake Nose
North Atlantic Ocean
COMPCORE
Composite Core
DRILL
Drilling/drill rig
Glomar Challenger
Joides Resolution
Leg171B
Leg32
Leg62
North Pacific/CONT RISE
North Pacific/SEAMOUNT
Ocean Drilling Program
ODP
North Atlantic
Online Access:https://doi.pangaea.de/10.1594/PANGAEA.713059
https://doi.org/10.1594/PANGAEA.713059
Description
Summary:Oxygen isotope analyses of well-preserved foraminifera from Blake Nose (30°N paleolatitude, North Atlantic) and globally distributed deep-sea sites provide a long-term paleotemperature record for the late Albian-Maastrichtian interval that is difficult to reconcile with the existence of significant Cretaceous ice sheets. Given reasonable assumptions about the isotopic composition of Cretaceous seawater, our results suggest that middle bathyal water temperatures at Blake Nose increased from ~12°C in the late Albian through middle Cenomanian to a maximum of 20°C during the latest Cenomanian and earliest Turonian. Bottom waters were again ~12°C during the middle Campanian and cooled to a minimum of 9°C during the Maastrichtian. Correlative middle bathyal foraminifera from other ocean basins yield paleotemperature estimates that are very similar to those from Blake Nose. Comparison of global bottom-water temperatures and latitudinal thermal gradients suggests that global climate changed from a warm greenhouse state during the late Albian through late Cenomanian to a hot greenhouse phase during the latest Cenomanian through early Campanian, then to cool greenhouse conditions during the mid-Campanian through Maastrichtian.

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