Atmospheric carbon dioxide through the Eocene–Oligocene climate transition

  title={Atmospheric carbon dioxide through the Eocene–Oligocene climate transition},
  author={Paul N. Pearson and Gavin L. Foster and Bridget S. Wade},
Geological and geochemical evidence indicates that the Antarctic ice sheet formed during the Eocene–Oligocene transition, 33.5–34.0 million years ago. Modelling studies suggest that such ice-sheet formation might have been triggered when atmospheric carbon dioxide levels () fell below a critical threshold of ∼750 p.p.m.v., but the timing and magnitude of relative to the evolution of the ice sheet has remained unclear. Here we use the boron isotope pH proxy on exceptionally well-preserved… 

New Caledonian carbon sinks at the onset of Antarctic glaciation

  • D. Reusch
  • Environmental Science, Geography
  • 2011
During the latest Eocene, as Earth9s climate transitioned from a greenhouse to an icehouse state, likely forced by declining atmospheric carbon dioxide pressure ( p CO 2 ), a large tract of basic and

The respective role of atmospheric carbon dioxide and orbital parameters on ice sheet evolution at the Eocene-Oligocene transition

The continental scale initiation of the Antarctic ice sheet at the Eocene-Oligocene boundary (Eocene-Oligocene transition (EOT), 34 Ma) is associated with a global reorganization of the climate. If

Declining atmospheric CO2 during the late Middle Eocene climate transition

The transition from the extreme greenhouse of the early Paleogene (∼52 Ma) to the present-day icehouse is the most prominent change in Earth’s Cenozoic climate history. During the late Middle Eocene

Atmospheric carbon dioxide variations across the middle Miocene climate transition

Abstract. The middle Miocene climate transition ∼  14 Ma marks a fundamental step towards the current “ice-house” climate, with a ∼  1 ‰ δ18 O increase and a ∼  1 ‰ transient δ13 C rise in the deep

Terrestrial cooling in Northern Europe during the Eocene–Oligocene transition

The authors' data show a decrease in growing-season surface water temperatures corresponding to an average decrease in mean annual air temperature from the Late Eocene to Early Oligocene, which suggests a close linkage between atmospheric carbon dioxide concentrations, Northern Hemisphere temperature, and expansion of the Antarctic ice sheets.

The Eocene–Oligocene transition: a review of marine and terrestrial proxy data, models and model–data comparisons

Abstract. The Eocene-Oligocene transition (EOT) from a largely ice-free greenhouse world to an icehouse climate with the first major glaciation of Antarctica was a phase of major climate and

Global carbon cycle perturbation across the Eocene-Oligocene climate transition

The Eocene-Oligocene transition (EOT), ~34?Ma, marks a tipping point in the long-term Cenozoic greenhouse to icehouse climate transition. Paleorecords reveal stepwise rapid cooling and ice growth

Antarctic Ice Sheet variability across the Eocene-Oligocene boundary climate transition

Sedimentary cycles from a drillcore in the western Ross Sea provide direct evidence of orbitally controlled glacial cycles between 34 million and 31 million years ago and provide insight into the potential of the AIS for threshold behavior and have implications for its sensitivity to atmospheric CO2 concentrations above present-day levels.



Cooling and ice growth across the Eocene-Oligocene transition

The Eocene-Oligocene (E-O) climate transition (ca. 34 Ma) marks a period of Antarctic ice growth and a major step from early Cenozoic greenhouse conditions toward today's glaciated climate state. The

Extinction and environmental change across the Eocene-Oligocene boundary in Tanzania

The Eocene-Oligocene transition (between ca. 34 and 33.5 Ma) is the most profound episode of lasting global change to have occurred since the end of the Cretaceous. Diverse geological evidence from

Eocene/Oligocene ocean de-acidification linked to Antarctic glaciation by sea-level fall

A global biogeochemical box model is used to test competing hypotheses put forward to explain the Eocene/Oligocene transition and finds that, of the candidate hypotheses, only shelf to deep sea carbonate partitioning is capable of explaining the observed changes in both carbon isotope composition and calcium carbonate accumulation at the sea floor.

Increased seasonality through the Eocene to Oligocene transition in northern high latitudes

Northern high-latitude terrestrial climate estimates for the Eocene to Oligocene interval, based on bioclimatic analysis of terrestrially derived spore and pollen assemblages preserved in marine sediments from the Norwegian–Greenland Sea indicate a cooling of ∼5 °C in cold-month (winter) mean temperatures to 0–2‬C, and a concomitant increased seasonality before the Oi-1 glaciation event.

Rapid Cenozoic glaciation of Antarctica induced by declining atmospheric CO2

In this simulation, declining Cenozoic CO2 first leads to the formation of small, highly dynamic ice caps on high Antarctic plateaux, and at a later time, a CO2 threshold is crossed, initiating ice-sheet height/mass-balance feedbacks that cause the ice caps to expand rapidly with large orbital variations, eventually coalescing into a continental-scale East Antarctic Ice Sheet.

Thresholds for Cenozoic bipolar glaciation

It is found that Oi-1 is best explained by Antarctic glaciation alone, combined with deep-sea cooling of up to 4 °C and Antarctic ice that is less isotopically depleted than previously suggested, which implies that episodic northern-hemispheric ice sheets have been possible some 20 million years earlier than currently assumed and could explain some of the variability in Miocene sea-level records.

Global Cooling During the Eocene-Oligocene Climate Transition

About 34 million years ago, Earth's climate shifted from a relatively ice-free world to one with glacial conditions on Antarctica characterized by substantial ice sheets. How Earth's temperature

Oxygen isotopic evidence for the development of the psychrosphere 38 Myr ago

THREE major elements were involved in the evolution of oceanic circulation during the Cainozoic. The first of these was the diminishing role of oceanic meridional circulation in equatorial areas, the