Evolution of mean ocean temperature in Marine Isotope Stage 4

• Published in: Climate of the Past
• Main Authors: S. Shackleton, J. A. Menking, E. Brook, C. Buizert, M. N. Dyonisius, V. V. Petrenko, D. Baggenstos, J. P. Severinghaus
• Format: Article in Journal/Newspaper
• Language: English
• Published: Copernicus Publications 2021
• Subjects: Environmental pollution; TD172-193.5; Environmental protection; TD169-171.8; Environmental sciences; GE1-350; Antarctic; Antarc*; Ice Sheet
• Online Access: https://doi.org/10.5194/cp-17-2273-2021; https://doaj.org/article/d11481853d1f4bbdbc4cd1631af426c0

Deglaciations are characterized by relatively fast and near-synchronous changes in ice sheet volume, ocean temperature, and atmospheric greenhouse gas concentrations, but glacial inception occurs more gradually. Understanding the evolution of ice sheet, ocean, and atmosphere conditions from interglacial to glacial maximum provides insight into the interplay of these components of the climate system. Using noble gas measurements in ancient ice samples, we reconstruct mean ocean temperature (MOT) from 74 to 59.7 ka, covering the Marine Isotope Stage (MIS) 5a–4 boundary, MIS 4, and part of the MIS 4–3 transition. Comparing this MOT reconstruction to previously published MOT reconstructions from the last and penultimate deglaciation, we find that the majority of the last interglacial–glacial ocean cooling must have occurred within MIS 5. MOT reached equally cold conditions in MIS 4 as in MIS 2 ( −2.7 ± 0.3 ∘ C relative to the Holocene, −0.1 ± 0.3 ∘ C relative to MIS 2). Using a carbon cycle model to quantify the CO 2 solubility pump, we show that ocean cooling can explain most of the CO 2 drawdown (32 ± 4 of 40 ppm) across MIS 5. Comparing MOT to contemporaneous records of benthic δ 18 O, we find that ocean cooling can also explain the majority of the δ 18 O increase across MIS 5 (0.7 ‰ of 1.3 ‰). The timing of ocean warming and cooling in the record and the comparison to coeval Antarctic isotope data suggest an intimate link between ocean heat content, Southern Hemisphere high-latitude climate, and ocean circulation on orbital and millennial timescales.