Ice Age Terminations

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1 Supporting Online Material for Ice Age Terminations Hai Cheng, R. Lawrence Edwards,* Wallace S. Broecker, George H. Denton, Xinggong Kong, Yongjin Wang, Rong Zhang, Xianfeng Wang This PDF file includes: *To whom correspondence should be addressed. Published 9 October 2009, Science 326, 248 (2009) DOI: /science Materials and Methods SOM Text Figs. S1 to S5 Tables S1 and S2 References

2 Supplementary Materials "Ice age terminations" By Cheng et al., 2009 Supplementary Figures Westerlies Siberian-Mongolian Highs Winter Monsoon China Sanbao Hulu Linzhu Dongge East Asian Monsoon Indian Monsoon Figure S1. Cave locations. Two red stars indicate Sanbao (110º26'E, 31º40'N) and Linzhu (110º19'E, 31º31'N) caves, central China. Hulu (119 10'E, 32 30'N) and Dongge (108 5'E, 25 17'N) caves are also shown with white stars. Arrows depict wind directions of the Asian Monsoon (yellow, including the East Asian Monsoon and the Indian Monsoon), the Westerlies (gray) and the winter monsoon (light blue). 1

3 SB SB SB61 (upper) SB61 (lower) Th age (ky BP) LZ LZ Figure S2. Age models of stalagmites SB25, SB11 and SB61 from Sanbao Cave (dark green), and LZ15 and LZ36 from Linzhu Cave (olivie green). There is a visible hiatus in sample SB61 at ~533.5 mm from the top which separates SB61 into two growth periods. The chronologies of samples SB61, SB25 and LZ36 are established by linear interpolations between 230 Th dates and samples SB11 and LZ15 are based on polynomial fitting of 230 Th dates. The vertical error bars depict errors of 230 Th dates (2σ). 2

4 SB61 (upper) -10 SB61 (lower) LZ36-10 LZ Age (ky BP) 3 δ 18 O (, VPDB) δ 18 O (, VPDB) δ 18 O (, VPDB) -6 Figure S3. Replication tests between the δ 18 O time series of the Sanbao record (dark green) and the Linzhu record (olive green, LZ15, LZ36) over cotemporaneous growth periods. Error bars indicate 230 Th ages and errors. The replication of records from two caves demonstrates that kinetic factors and water/rock interactions are not likely to have had a significant effect on the cave δ 18 O values (S1).

5 Sanbao SB25-6 Dongge D4 18 O (, VPDB) Age (ky BP) Figure S4. Comparison between the 18 O time series of Sanbao (SB25, dark green) and Dongge records (S2) over Termination II. The error bars are color coded and indicate 230 Th ages and 2 errors. The replication of 18 O records between two caves (~1000 km away from each other) demonstrates that changes in the 18 O values mainly reflect changes in the oxygen isotopic composition of meteoric precipitation, which are similar over broad regions of China. 4

6 Termination IIIA δ 18 O (, VPDB) i Insolation at 65 o N (W/m 2 ) δ D IRD (%) Dust (ppm) (, VSMOW) ii iii iv v vi vii viii δ 18 Oatm CO 2 (ppmv) CH 4 (ppbv) (, VSMOW) Forams-b δ 18 O (, VPDB) Age (ky BP) Figure S5. Comparison of events surrounding Termination IIIA (T IIIA). (i) Sanbao record (light green (S3); green, this study), Linzhu record (olive green) and July 21 insolation at 65ºN (S4) (gray). Vostok records of (ii) CH 4, (iii) δd (temperature), (iv) CO 2, (v) dust and (vi) atmospheric δ 18 O (S5). ODP980 records of (vii) IRD and (viii) foraminifera δ 18 O of benthic (C. wuellerstorfi) (S6). Vostok records are plotted on the GT4 timescale (S5) with an absolute shift applied, so that the jump of CH 4 correlates with the abrupt rise in the monsoon at about 226 ky B.P. The shift adds about 6 ky to the original Vostok age. The vertical bar (green) indicates the Weak Monsoon Interval (WMI). We also applied an absolute shift to the ODP980 record so that the weakest portion of the monsoon, as recorded in Sanbao, correlates to the IRD peak in ODP980. The shift adds about 3 ky to the original ODP980 age. 5

7 Analytical Methods Stalagmites SB61 (recording T-III and T-IV; diameter 33 cm, length 146 cm), SB25 (T-II; diameter 30 cm, length 47 cm) and SB11 (T-IIIA; diameter 33 cm, length 80 cm) were collected from Sanbao Cave about 1500 m from the cave entrance. Stalagmites LZ15 (diameter 12 cm, length 25 cm) and LZ36 (diameter 10 cm, length 15 cm) were collected from Linzhu Cave about 35 m from the cave entrance. All five stalagmites were halved along the growth axis and the surface polished. Each subsample for oxygen isotope ratio analysis was milled using 0.3 mm carbide dental burrs along the length of the stalagmites, parallel to the central growth axis. The oxygen isotope ratios were measured at the College of Geography, Nanjing Normal University, China using a Finnigan-MAT 253 mass spectrometer fitted with a Kiel Carbonate Device III. The analytical procedures are described in ref. S3. Data were calibrated against standards NBS-18 and NBS-19 and are reported as 18 O ( ) relative to the Vienna Pee Dee Belemnite (VPDB). Duplicates were analyzed every 10 to 20 samples to check for homogeneity, all of which replicated within All 18 O data are listed in Table S2. The chemical procedures used to separate the uranium and thorium for 230 Th dating are similar to those described in ref. S Th dating of stalagmites was performed at the Minnesota Isotope Laboratory on a multi-collector inductively coupled plasma mass spectrometer (MC-ICP- MS, Thermo-Finnigan Neptune). All uranium isotopes were measured on Faraday cups with tail corrections performed by measuring masses and 237 on a MasCom multiplier. The smallest uranium isotope ( 234 U) beam intensities are measured at ~30 mv with a ohm resistor. Instrumental mass fractionations was determined by measuring the 233 U 236 U double spike simultaneously. Thorium isotope analyses for samples SB11 and LZ15 were performed on the multiplier behind the retarding potential quadrupole (RPQ) in peak-jumping mode. The procedures of characterizing the multiplier are similar to those described in ref. S8. Instrumental mass fractionation was determined by bracketing measurements of a 233 U 236 U spike. Thorium isotope analyses for samples SB61 and LZ36 were made on Faraday cups with mass fractionation corrected with an admixed 233 U 236 U spike simultaneously. 230 Th dating techniques are described in refs. S8 and S9. Half-life values are those reported in ref. S9. All dates are in stratigraphic order within analytical errors. The typical dating errors for samples with sufficient uranium measured on the Faraday cups are ~100 years around Termination II, ~200 years at Termination III and ~500 years at Termination IV (see Table S1). 6

8 Within errors, records from SB25 and SB23 replicate each other, as do records from SB61, LZ15, and LZ36 (Fig. S3), suggesting that cave 18 O values have not been affected by kinetic processes or by water-rock interactions. Thus, changes in 18 O are likely caused by variations in meteoric 18 O and in temperature-dependent fractionation during calcite precipitation. For a reasonable shift in temperature (~5 degrees), the effect of fractionation is small relative to the full amplitude of variation in the record, leaving changes in the 18 O of meteoric precipitation as the main process affecting stalagmite 18 O. Energy calculation for melting of ice-sheets during glacial terminations Assuming an average sea level rise rate of 0.01 m/year (or 100 m/10ky) resulting mainly from the ice-sheet at high latitude of Northern Hemisphere (around 65 N), the total energy for melting of the icesheets is: E = d * * V (here d = 910 kg/m 3 is the density of ice; = 3.34*10 5 Joule/kg is the latent heat of fusion; V is the total volume of melted global ice sheets during the glacial terminations, which can be estimated through sea level rise: V=A * h, A is global ocean area (~3.5*10 14 m 2 ), h is the sea level rise (100m). Hence the total energy loss is E = 910 kg/m 3 *3.34*10 5 Joule/kg *3.5*10 14 m 2 *100m = 1.1*10 25 Joule over 10 ky or 1.1*10 24 Joule over 1 ky (assuming such energy loss is linearly distributed over the 10 ky of the glacial termination period). As the insolation increase rates over the last four terminations are similar, on the order of ~5 W/m 2 over 1 ky in the area around 65 N (Fig. 4), the additional energy from this increase in insolation would be: E increase (1/2)*5((Joule/s)/m 2 ) *1000*365*24*3600(s) = 7.9* Joule/m 2 over 1ky. If we distribute the increased energy uniformly over the whole area of ice sheets (assume ~5 % of total Earth area), then the total additional energy is: E total = 7.9*10 10 (Joule/m 2 )*2.5*10 13 (m 2 ) = 1.9*10 24 Joule over 1ky. Therefore, the additional energy from the increase in insolation would be of the same order as the energy required for maintaining icesheet melting at a reasonable rate during terminations. As such, a high solar insolation increase rate, comparable to the energy consumed by ice-sheet melting appears to be important for continuing deglaciation to interglacial conditions. This is consistent with our observations that the past four terminations all occurred when insolation increase rates were at high values (Fig. 4). 7

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