Fig. 2: Speleothem growth periods compared with other paleoclimate archives during interglacials Marine isotope stages (MIS) 1 to MIS 11c.
From: Asynchronicity of deglacial permafrost thawing controlled by millennial-scale climate variability
a Global benthic δ18O stack78. b June 21st insolation at 30°N77. c Atmospheric CO2 concentration (gray)81 as well as the CO2 concentration that has been tuned to East Asian Summer monsoon (EASM) speleothem chronology31 (dashed dark brown). d Synthetic Greenland δ18O record82 (turquoise) and NGRIP Greenland δ18O record83 (light blue). e EASM strength as given by a composite Chinese cave speleothem δ18O record31 (orange); horizontal error bars are the distribution of speleothem ages (±2σ) for Siberia (top, blue), Canada (middle, purple) and Tibetan Plateau (bottom, red), the dates of initial continuous thawing in each permafrost region are marked in bold circles (see Methods and Supplementary Fig. 2 for details). f Glacial-interglacial bottom water δ13C reconstructions from Cibicidoides wuellerstorfi in the deep Eirik Drift37,84,85, the dashed line in MIS 1 is the bottom water δ13C reconstructions from U1304 in the North Atlantic37, indicating the Atlantic meridional overturning circulation (AMOC) strength. g Eirik Drift ice-rafted debris (IRD) records37 [percent of >150 μm entities; MIS 5e, MIS 7e, MIS 9e, MIS 11c] and ODP 983 IRD per gram86 [MIS 1]. Red [MIS 5e to MIS 11c] and blue [MIS 1] vertical bars indicate the Terminal stadials, which correspond to the onset of Tibetan Plateau permafrost thawing except for MIS 1. Source data are provided as a Source Data file.
