Does Antarctic glaciation cool the world?

• Published in: Climate of the Past
• Main Authors: A. Goldner, M. Huber, R. Caballero
• Format: Article in Journal/Newspaper
• Language: English
• Published: Copernicus Publications 2013
• Subjects: Environmental pollution; TD172-193.5; Environmental protection; TD169-171.8; Environmental sciences; GE1-350; Antarctic; Antarc*; Antarctica; Ice Sheet; Sea ice
• Online Access: https://doi.org/10.5194/cp-9-173-2013; https://doaj.org/article/ecac901604944b5a8727f5a56e68784c

In this study, we compare the simulated climatic impact of adding an Antarctic ice sheet (AIS) to the "greenhouse world" of the Eocene and removing the AIS from the modern world. The modern global mean surface temperature anomaly (Δ T ) induced by Antarctic Glaciation depends on the background CO 2 levels and ranges from −1.22 to −0.18 K. The Eocene Δ T is nearly constant at ~−0.25 K. We calculate an climate sensitivity parameter S [Antarctica] which we define as Δ T divided by the change in effective radiative forcing (Δ Q Antarctica ) which includes some fast feedbacks imposed by prescribing the glacial properties of Antarctica. The main difference between the modern and Eocene responses is that a negative cloud feedback warms much of the Earth's surface as a large AIS is introduced in the Eocene, whereas this cloud feedback is weakly positive and acts in combination with positive sea-ice feedbacks to enhance cooling introduced by adding an ice sheet in the modern. Because of the importance of cloud feedbacks in determining the final temperature sensitivity of the AIS, our results are likely to be model dependent. Nevertheless, these model results suggest that the effective radiative forcing and feedbacks induced by the AIS did not significantly decrease global mean surface temperature across the Eocene–Oligocene transition (EOT −34.1 to 33.6 Ma) and that other factors like declining atmospheric CO 2 are more important for cooling across the EOT. The results illustrate that the efficacy of AIS forcing in the Eocene is not necessarily close to one and is likely to be model and state dependent. This implies that using EOT paleoclimate proxy data by itself to estimate climate sensitivity for future climate prediction requires climate models and consequently these estimates will have large uncertainty, largely due to uncertainties in modelling low clouds.