Bond event

Bond events are North Atlantic climate fluctuations occurring every ≈1,470 ± 500 years throughout the Holocene. Eight such events have been identified, primarily from fluctuations in ice-rafted debris. Bond events may be the interglacial relatives of the glacial Dansgaard–Oeschger events,[1] with a magnitude of perhaps 15–20% of the glacial-interglacial temperature change.

Gerard C. Bond of the Lamont–Doherty Earth Observatory at Columbia University, was the lead author of the 1997 paper that postulated the theory of 1470-year climate cycles in the Holocene, mainly based on petrologic tracers of drift ice in the North Atlantic.[2][3]

The existence of climatic changes, possibly on a quasi-1,500 year cycle, is well established for the last glacial period from ice cores. Less well established is the continuation of these cycles into the Holocene. Bond et al. (1997) argue for a cyclicity close to 1470 ± 500 years in the North Atlantic region and that their results imply a variation in Holocene climate in this region. In their view, many, if not most, of the Dansgaard–Oeschger events of the last ice age conform to a 1,500-year pattern, like some climate events of later eras such as the Little Ice Age, the 8.2 kiloyear event, and the start of the Younger Dryas.

The North Atlantic ice-rafting events happen to correlate with most weak events of the Asian monsoon for at least the past 9000 years[4][5] and also correlate with most aridification events in the Middle East for the past 55,000 years (both Heinrich and Bond events).[6][7] Also, there is widespread evidence that a ≈1,500 yr climate oscillation caused changes in vegetation communities across all of North America.[8]

For reasons that are unclear, the only Holocene Bond event that has a clear temperature signal in the Greenland ice cores is the 8.2 kyr event.

The hypothesis holds that the 1500-year cycle displays nonlinear behavior and stochastic resonance; not every instance of the pattern is a significant climate event, though some rise to major prominence in environmental history.[9] Causes and determining factors of the cycle are under study; researchers have focused attention on variations in solar output, and "reorganizations of atmospheric circulation."[9] Bond events may also be correlated with the 1800-year lunar tidal cycle.[10]

List

Most Bond events do not have a clear climate signal; some correspond to periods of cooling, but others are coincident with aridification in some regions.

No. Time
(BP)		 Time
(AD, BC)		 Notes
0 ≈ −0.5 ka ≈ 1500 AD See Little Ice Age;[11]
1 ≈ −1.4 ka ≈ 600 AD See Migration Period;[11]
2 ≈ −2.8 ka ≈ 800 BC Late Bronze Age collapse may have been triggered by drought in the Eastern Mediterranean.[12][13][14]
3 ≈ −4.2 ka ≈ 2200 BC See 4.2 kiloyear event; collapse of the Akkadian Empire and the end of the Egyptian Old Kingdom.[15][16]
4 ≈ −5.9 ka ≈ 3900 BC See 5.9 kiloyear event;
5 ≈ −8.2 ka ≈ 6200 BC See 8.2 kiloyear event;
6 ≈ −9.4 ka ≈ 7400 BC Erdalen event of glacier activity in Norway,[17] as well as with a cold event in China.[18]
7 ≈ −10.3 ka ≈ 8300 BC
8 ≈ −11.1 ka ≈ 9100 BC transition from the Younger Dryas to the boreal.[19]

See also

References

  1. ↑ Bond, G.; Showers, W.; Elliot, M.; Evans, M.; Lotti, R.; Hajdas, I.; Bonani, G.; Johnson, S. (1999). "The North Atlantic’s 1–2 kyr climate rhythm: relation to Heinrich Events, Dansgaard/Oeschger cycle and the Little Ice Age". In Clark, P.; Webb, R.; Keigwin, L. Mechanisms of Global Climate Change at Millennial Time Scales. Geophysical Monograph Series 112. Washington, DC: American Geophysical Union. pp. 35–58. ISBN 087590095X.
  2. ↑ Bond, G.; et al. (1997). "A Pervasive Millennial-Scale Cycle in North Atlantic Holocene and Glacial Climates" (PDF). Science 278 (5341): 1257–1266. Bibcode:1997Sci...278.1257B. doi:10.1126/science.278.5341.1257.
  3. ↑ Bond, G.; et al. (2001). "Persistent Solar Influence on North Atlantic Climate During the Holocene". Science 294 (5549): 2130–2136. Bibcode:2001Sci...294.2130B. doi:10.1126/science.1065680. PMID 11739949.
  4. ↑ Gupta, Anil K.; Anderson, David M.; Overpeck, Jonathan T. (2003). "Abrupt changes in the Asian southwest monsoon during the Holocene and their links to the North Atlantic Ocean". Nature 421 (6921): 354–357. Bibcode:2003Natur.421..354G. doi:10.1038/nature01340. PMID 12540924.
  5. ↑ Yongjin Wang; et al. (2005). "The Holocene Asian Monsoon: Links to Solar Changes and North Atlantic Climate". Science 308 (5723): 854–857. Bibcode:2005Sci...308..854W. doi:10.1126/science.1106296. PMID 15879216.
  6. ↑ Bartov, Yuval; Goldstein, Steven L.; Stein, Mordechai; Enzel, Yehouda (2003). "Catastrophic arid episodes in the Eastern Mediterranean linked with the North Atlantic Heinrich events". Geology 31 (5): 439–442. Bibcode:2003Geo....31..439B. doi:10.1130/0091-7613(2003)031<0439:CAEITE>2.0.CO;2.
  7. ↑ Parker, Adrian G.; et al. (2006). "A record of Holocene climate change from lake geochemical analyses in southeastern Arabia". Quaternary Research 66 (3): 465–476. Bibcode:2006QuRes..66..465P. doi:10.1016/j.yqres.2006.07.001.
  8. ↑ Viau, André E.; et al. (2002). "Widespread evidence of 1,500 yr climate variability in North America during the past 14 000 yr". Geology 30 (5): 455–458. Bibcode:2002Geo....30..455V. doi:10.1130/0091-7613(2002)030<0455:WEOYCV>2.0.CO;2.
  9. 1 2 Cox, John D. (2005). Climate Crash: Abrupt Climate Change and What It Means for Our Future. Washington DC: Joseph Henry Press. pp. 150–155. ISBN 0-309-09312-0.
  10. ↑ Keeling, Charles; Whorf, TP (2000). "The 1,800-Year Oceanic Tidal Cycle: A Possible Cause of Rapid Climate Change". Proceedings of the National Academy of Sciences of the United States of America 97 (8): 3814–3819. Bibcode:2000PNAS...97.3814K. doi:10.1073/pnas.070047197. JSTOR 122066. PMC 18099. PMID 10725399.
  11. 1 2 Zhao, Keliang; et al. (2012). "Climatic variations over the last 4000 cal yr BP in the western margin of the Tarim Basin, Xinjiang, reconstructed from pollen data". Palaeogeography, Palaeoclimatology, Palaeoecology. 321–322: 16–23. doi:10.1016/j.palaeo.2012.01.012.
  12. ↑ Weis, Barry (1982). "The decline of Late Bronze Age civilization as a possible response to climatic change". Climate Change 4 (2): 173–198. doi:10.1007/BF00140587.
  13. ↑ Kaniewski, D.; et al. (2008). "Middle East coastal ecosystem response to middle-to-late Holocene abrupt climate changes". PNAS 105 (37): 13941–13946. Bibcode:2008PNAS..10513941K. doi:10.1073/pnas.0803533105.
  14. ↑ Kaniewski, D.; et al. (2010). "Late second–early first millennium BC abrupt climate changes in coastal Syria and their possible significance for the history of the Eastern Mediterranean". Quaternary Research 74 (2): 207–215. Bibcode:2010QuRes..74..207K. doi:10.1016/j.yqres.2010.07.010.
  15. ↑ Gibbons, Ann (1993). "How the Akkadian Empire Was Hung Out to Dry". Science 261 (5124): 985. Bibcode:1993Sci...261..985G. doi:10.1126/science.261.5124.985. PMID 17739611.
  16. ↑ Stanley, Jean-Daniel; et al. (2003). "Nile flow failure at the end of the Old Kingdom, Egypt: Strontium isotopic and petrologic evidence". Geoarchaeology 18 (3): 395–402. doi:10.1002/gea.10065.
  17. ↑ Dahl, Svein Olaf; et al. (2002). "Timing, equilibrium-line altitudes and climatic implications of two early-Holocene glacier readvances during the Erdalen Event at Jostedalsbreen, western Norway". The Holocene 12 (1): 17–25. doi:10.1191/0959683602hl516rp.
  18. ↑ Zhou Jing; Wang Sumin; Yang Guishan; Xiao Haifeng (2007). "Younger Dryas Event and Cold Events in Early-Mid Holocene: Record from the sediment of Erhai Lake" (PDF). Advances in Climate Change Research 3 (Suppl.): 1673–1719.
  19. ↑ Allen, Harriet D. (2003). "Response of past and present Mediterranean ecosystems to environmental change". Progress in Physical Geography 27 (3): 359–377. doi:10.1191/0309133303pp387ra.
This article is issued from Wikipedia - version of the Saturday, April 09, 2016. The text is available under the Creative Commons Attribution/Share Alike but additional terms may apply for the media files.