Abrupt climate events 500,000 to 340,000 years ago: Evidence from subpolar North Atlantic sediments

Science

Volumn 279, Issue 5355, 1998, Pages 1335-1338

  Oppo, D W ^a   McManus, J F ^a   Cullen, J L ^b  

^a WOODS HOLE OCEANOGRAPHIC INSTITUTION   (United States)

^b SALEM STATE UNIVERSITY   (United States)

Author keywords

[No Author keywords available]

Indexed keywords

ICE;

CLIAMTE PROXY RECORD; CLIMATE PROXY RECORD; OCEAN CIRCULATION; PALAEOCLIMATE CHANGE; QUATERNARY CLIMATE; SEA SURFACE TEMEPRATURE; SEA SURFACE TEMPERATURE;

ARTICLE; CLIMATE; MARINE ENVIRONMENT; PRIORITY JOURNAL; SEDIMENT; TEMPERATURE ACCLIMATIZATION;

ATLANTIC, (NORTH);

EID: 0032570567     PISSN: 00368075     EISSN: None     Source Type: Journal    
DOI: 10.1126/science.279.5355.1335     Document Type: Article

References (47)

1. H. Heinrich, Quat. Res, 29, 142 (1988).
2. G. Bond et al., Nature 365, 143 (1993).
3. W. S. Broecker, G. Bond, M. Klas, E. Clark, J. McManus, Clim. Dyn. 6, 265 (1992).
4. W. Dansgaard et al., in Climate Processes and Climate Sensitivity, J. E. Hansen and T. Takahashi, Eds. (American Geophysical Union, Washington, DC, 1984), vol. 5, pp. 288-298.
5. G. Bond and R. Lotti, Science 267, 1005 (1995).
6. G. Bond et al., ibid. 278, 1257 (1997).
7. P. A. Mayewski et al., J. Geophys. Res. 102, 26345 (1997).
8. S. R. O'Brien et al., Science 270, 1962 (1995); L. D. Keigwin, ibid. 274, 1504 (1996).
9. S. R. O'Brien et al., Science 270, 1962 (1995); L. D. Keigwin, ibid. 274, 1504 (1996).
10. W. S. Broecker, G. Bond, M. Klas, G. Bonani, W. Wolfi, Paleoceanography 5, 469 (1990).
11. U. Mikolajewicz, T. J. Crowley, A. Schiller, R. Voss, Nature 387, 384 (1997).
12. L. D. Keigwin and G. A. Jones, J. Geophys. Res. 99, 12397 (1994); L. Vidai et al., Earth Planet. Sci. Lett. 146, 13 (1997).
13. L. D. Keigwin and G. A. Jones, J. Geophys. Res. 99, 12397 (1994); L. Vidai et al., Earth Planet. Sci. Lett. 146, 13 (1997).
14. D. W. Oppo and S. J. Lehman, Paleoceanography 10, 901 (1995).
15. M. E. Raymo, K. Ganley, S. Carter, D. W. Oppo, J. McManus, in preparation.
16. W. B. Curry and D. W. Oppo, Paleoceanography 12, 1 (1997).
17. N. G. Pisias and T. C. Moore, Earth Planet Sci. Lett. 52, 450 (1981);
18. W. F. Ruddiman, A. McIntyre, M. Raymo, ibid. 80, 117 (1986);
19. W. F. Ruddiman, M. E. Raymo, D. G. Martinson, B. M. Clement, J. Backman, Paleoceanography 4, 353 (1989).
20. We used the time scale presented by N. J. Shackleton, A. Berger, and W. R. Peltier [Trans. R. Soc. Edinburgh Earth Sci. 81, 25 (1990)].
21. Because of its high sedimentation rates and sensitive location just north of the glacial polar front, the Feni Drift has been the focus of many studies of suborbital-scale climate variability over the last glacial cycle [(2, 3, 5, 6); G, Bond et al., Nature 360, 245 (1992); J. F. McManus et al., ibid. 371, 326 (1994); E. Cortijo, P. Yiou, L. Labeyrie, M. Cremer, Paleoceanography 10, 911 (1995); S. G. Robinson, M. Maslin, I. N. McCave, ibid., p. 221; L. D. Labeyrie et al., Philos. Trans. R. Soc. London Ser. B 348, 255 (1995)]. ODP site 980 was drilled with the goal of extending the results from the last glacial cycle to earlier intervals. Sedimentation rates average 11 cm/ky over the study interval.
22. Because of its high sedimentation rates and sensitive location just north of the glacial polar front, the Feni Drift has been the focus of many studies of suborbital-scale climate variability over the last glacial cycle [(2, 3, 5, 6); G, Bond et al., Nature 360, 245 (1992); J. F. McManus et al., ibid. 371, 326 (1994); E. Cortijo, P. Yiou, L. Labeyrie, M. Cremer, Paleoceanography 10, 911 (1995); S. G. Robinson, M. Maslin, I. N. McCave, ibid., p. 221; L. D. Labeyrie et al., Philos. Trans. R. Soc. London Ser. B 348, 255 (1995)]. ODP site 980 was drilled with the goal of extending the results from the last glacial cycle to earlier intervals. Sedimentation rates average 11 cm/ky over the study interval.
23. Because of its high sedimentation rates and sensitive location just north of the glacial polar front, the Feni Drift has been the focus of many studies of suborbital-scale climate variability over the last glacial cycle [(2, 3, 5, 6); G, Bond et al., Nature 360, 245 (1992); J. F. McManus et al., ibid. 371, 326 (1994); E. Cortijo, P. Yiou, L. Labeyrie, M. Cremer, Paleoceanography 10, 911 (1995); S. G. Robinson, M. Maslin, I. N. McCave, ibid., p. 221; L. D. Labeyrie et al., Philos. Trans. R. Soc. London Ser. B 348, 255 (1995)]. ODP site 980 was drilled with the goal of extending the results from the last glacial cycle to earlier intervals. Sedimentation rates average 11 cm/ky over the study interval.
24. Because of its high sedimentation rates and sensitive location just north of the glacial polar front, the Feni Drift has been the focus of many studies of suborbital-scale climate variability over the last glacial cycle [(2, 3, 5, 6); G, Bond et al., Nature 360, 245 (1992); J. F. McManus et al., ibid. 371, 326 (1994); E. Cortijo, P. Yiou, L. Labeyrie, M. Cremer, Paleoceanography 10, 911 (1995); S. G. Robinson, M. Maslin, I. N. McCave, ibid., p. 221; L. D. Labeyrie et al., Philos. Trans. R. Soc. London Ser. B 348, 255 (1995)]. ODP site 980 was drilled with the goal of extending the results from the last glacial cycle to earlier intervals. Sedimentation rates average 11 cm/ky over the study interval.
25. Because of its high sedimentation rates and sensitive location just north of the glacial polar front, the Feni Drift has been the focus of many studies of suborbital-scale climate variability over the last glacial cycle [(2, 3, 5, 6); G, Bond et al., Nature 360, 245 (1992); J. F. McManus et al., ibid. 371, 326 (1994); E. Cortijo, P. Yiou, L. Labeyrie, M. Cremer, Paleoceanography 10, 911 (1995); S. G. Robinson, M. Maslin, I. N. McCave, ibid., p. 221; L. D. Labeyrie et al., Philos. Trans. R. Soc. London Ser. B 348, 255 (1995)]. ODP site 980 was drilled with the goal of extending the results from the last glacial cycle to earlier intervals. Sedimentation rates average 11 cm/ky over the study interval.
26. W. S. Broecker and J. V. Donk, Rev. Geophys. Space Phys. 8, 169 (1970).
27. W. R. Howard, Nature 388, 418 (1997).
28. A. L. Berger, J. Atmos. Sci. 35, 2362 (1978).
29. W. Broecker, G. Bond, J. McManus, in Ice in the Climate System, W. R. Peltier, Ed. (Springer-Verlag, Berlin, 1993), vol. 12, pp. 161-166.
30. 13C = 1.95 VPDB).
31. D. W. Oppo, M. Horowitz, S. J. Lehman, Paleoceanography 12, 51 (1997).
32. 18O. If true, the faunal estimates must also underestimate the full amplitude of the glacial-interglacial SST change.
33. 18O.
34. 18O.
35. 18O.
36. F. E. Grousset et al., Paleoceanography 8, 175 (1993).
37. 13C values are low within DWE-2 and only began to rise in association with the warming out of the last cold event. With the existing (orbital-scale resolution) deep North Atlantic records, we cannot address whether the weakening of GNAIW was associated with strengthening of NADW, as has been documented for the last degladation (T. M. J. Marchitto, W. B. Curry, D. W. Oppo, in preparation). However, the decreasing strength of GNAIW associated with Termination V confirms that vertical water-mass reorganization is an important and persistent feature of deglaciations [M. Sarnthein and R. Tiedemann, Paleoceanography 5, 1041 (1990)]. Water-mass restructuring, which results in an increase in heat release at high northern latitudes, has probably been one of the most important climatic feedbacks accelerating deglaciation [S. J. Lehman and L. D. Keigwin, Nature 356, 757 (1992)].
38. 13C values are low within DWE-2 and only began to rise in association with the warming out of the last cold event. With the existing (orbital-scale resolution) deep North Atlantic records, we cannot address whether the weakening of GNAIW was associated with strengthening of NADW, as has been documented for the last degladation (T. M. J. Marchitto, W. B. Curry, D. W. Oppo, in preparation). However, the decreasing strength of GNAIW associated with Termination V confirms that vertical water-mass reorganization is an important and persistent feature of deglaciations [M. Sarnthein and R. Tiedemann, Paleoceanography 5, 1041 (1990)]. Water-mass restructuring, which results in an increase in heat release at high northern latitudes, has probably been one of the most important climatic feedbacks accelerating deglaciation [S. J. Lehman and L. D. Keigwin, Nature 356, 757 (1992)].
39. 13C values are low within DWE-2 and only began to rise in association with the warming out of the last cold event. With the existing (orbital-scale resolution) deep North Atlantic records, we cannot address whether the weakening of GNAIW was associated with strengthening of NADW, as has been documented for the last degladation (T. M. J. Marchitto, W. B. Curry, D. W. Oppo, in preparation). However, the decreasing strength of GNAIW associated with Termination V confirms that vertical water-mass reorganization is an important and persistent feature of deglaciations [M. Sarnthein and R. Tiedemann, Paleoceanography 5, 1041 (1990)]. Water-mass restructuring, which results in an increase in heat release at high northern latitudes, has probably been one of the most important climatic feedbacks accelerating deglaciation [S. J. Lehman and L. D. Keigwin, Nature 356, 757 (1992)].
40. 13C values are low within DWE-2 and only began to rise in association with the warming out of the last cold event. With the existing (orbital-scale resolution) deep North Atlantic records, we cannot address whether the weakening of GNAIW was associated with strengthening of NADW, as has been documented for the last degladation (T. M. J. Marchitto, W. B. Curry, D. W. Oppo, in preparation). However, the decreasing strength of GNAIW associated with Termination V confirms that vertical water-mass reorganization is an important and persistent feature of deglaciations [M. Sarnthein and R. Tiedemann, Paleoceanography 5, 1041 (1990)]. Water-mass restructuring, which results in an increase in heat release at high northern latitudes, has probably been one of the most important climatic feedbacks accelerating deglaciation [S. J. Lehman and L. D. Keigwin, Nature 356, 757 (1992)].
41. 13C values are low within DWE-2 and only began to rise in association with the warming out of the last cold event. With the existing (orbital-scale resolution) deep North Atlantic records, we cannot address whether the weakening of GNAIW was associated with strengthening of NADW, as has been documented for the last degladation (T. M. J. Marchitto, W. B. Curry, D. W. Oppo, in preparation). However, the decreasing strength of GNAIW associated with Termination V confirms that vertical water-mass reorganization is an important and persistent feature of deglaciations [M. Sarnthein and R. Tiedemann, Paleoceanography 5, 1041 (1990)]. Water-mass restructuring, which results in an increase in heat release at high northern latitudes, has probably been one of the most important climatic feedbacks accelerating deglaciation [S. J. Lehman and L. D. Keigwin, Nature 356, 757 (1992)].
42. K. Sakai and W. R. Peltier, J. Clim. 10, 949 (1997).
43. K. E. Kohfield, R. G. Fairbanks, S. L. Smith, I. D. Walsh, Paleoceanography 11, 679 (1996).
44. G. M. Jenkins and D. G. Watts, Spectral Analysis and Its Applications (Holden-Day, San Francisco, 1968). Multiple-taper methods [D. J. Thomson, Philos. Trans. R. Soc. London Ser. A 332, 539 (1990)] gave similar results.
45. G. M. Jenkins and D. G. Watts, Spectral Analysis and Its Applications (Holden-Day, San Francisco, 1968). Multiple-taper methods [D. J. Thomson, Philos. Trans. R. Soc. London Ser. A 332, 539 (1990)] gave similar results.
46. A zero-phase, 128-order Hamming window with cutoff frequencies 1/6.7 and 1/1 ky. The change in amplitude through time is similar for narrower pass bands centered at, for example, the 1.5- and 3.8-ky periods.
47. We thank S, Healy, L. Zou, T. Norris, D. Ostermann, and M. Jeglinski for laboratory assistance. We also thank A. Martin and R. Norris for lending their expertise on foramifer taxonomy, P. Howell for making the time series programs available, ODP, and co-chiefs M. Raymo and E. Jansen and the rest of the Leg 162 shipboard party for acquiring the samples. We especially thank T. C. E. van Weering for generously providing the site survey data for site 980. We also thank M. Raymo, W. Curry, and two reviewers for comments on the manuscript. This work was funded by NSF grant OCE-9632172 (D.W.O.), a Woods Hole Oceanographic Institution postdoctoral scholarship (J.F.M.), and a Joint Oceanographic Institutions-U.S. Science Advisory Committee grant (J.L.C.).