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Paleoclimatology Why is it important?

Paleoclimatology Why is it important?

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Paleoclimatology Why is it important?

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  1. PaleoclimatologyWhy is it important? Angela Colbert Climate Modeling Group October 24, 2011

  2. What is Paleoclimatology? • The study of past climates. • Use proxies to reconstruct temperature and other records • Use models to try to test theories to explain the proxy records • Proxy Examples • Sediment cores – lakes and oceans, use forams • Ice cores – very detailed for more “recent” history • Tree rings – annual ring made, very detailed

  3. Geological Time Scale Holocene Began ~ 10,000 years ago Last Glacial Maximum ~ 21,000 years ago Pleistocene – Last Glacial Period Pliocene – Last Non-Glacial Period

  4. What Can We Learn? • The importance and impact of changing levels of carbon dioxide • Past changes in ocean/atmospheric circulations • What has occurred naturally in the past and on what time scales • Climate sensitivity

  5. Interactions within Climate System

  6. Why Is It Important? • Rates of Climate Change • Tectonic, Orbital, Abrupt • Climate Sensitivity • What are the triggers for climate change? • How much natural variability is there? • Adaptation of ecosystems

  7. Rates of Climate Change

  8. Orbital Climate Change

  9. Abrupt Climate Change Amy will discuss this more later!

  10. Marine Isotope Stages

  11. Climate Sensitivity • Lea (2004) – Comparing tropical SSTs to ice core records to isolate CO2 changes and determine climate sensitivity. • Hansen and Sato (2011) – A slightly more urgent approach…

  12. Lea (2004)

  13. Methodology for Climate Sensitivity • Linear Regression • Can be achieved by interpolating both records (SST and ice core) to a constant 2,000 yr sample interval. • Radiative effect of CO2 is first order, estimated climate forcing is calculated by: • With the effect of methane taken into account.

  14. Slope: 1.4 + 0.1°C (W m-2)-1 • Intercept: 0.5 + 0.2°C • Positive due to warmer than present conditions at some previous interglacials • For 4 W m-2 = 4.4 - 5.6°C warming for doubling of CO2

  15. Methodology for Climate Sensitivity • Multivariate Regression • Linear regression does not take into account other factors: ice volume, atmospheric dust • Derive relative weightings for each independent factor that can control tropical SST • Total greenhouse forcing, local insolation, NH insolation, two different records of ice volume, Vostok ice core dust • Find 1.3 + 0.1°C (W m-2)-1 slope

  16. Comparing Observations to Models • For tropical SST found sensitivity to be 4.4 - 5.6°C • 15 Climate models – 3.5°C (mean) with range of 2.0 – 5.1°C • Why different? • Smaller effect that glacial CO2 reduction has on tropical ocean temps in models (1-2°C) • Strong cooling effect on the Tropics from heat transport of ice sheets (possible factor?)

  17. The Paleoclimatic Approach (according to Lea) • Advantage • Provides series of equilibrium climate sensitivity experiments over a range of atmos. CO2 levels • No model assumptions • Disadvantage • Other climatic influences (size and distribution of glacial ice sheets, surface albedo, insolation changes, concomitant changes in ocean and atmos. circulation) could influence the past in a way that is not applicable to the future • Dust shows a comparable signal amplitude, but is limited spatially by sources

  18. Hansen and Sato (2011) • The formation of ice sheets resulted in global cooling. • Global temperatures were much warmer in the past than even today. • Shows the influence of plate tectonics.

  19. What They Argue • Paleoclimate data on climate change and climate sensitivity can yield accurate estimates for “the dangerous level of global warming” • The current agreement is the try to keep the warming below 2°C relative to pre-industrial times. • They argue that this would be “a disaster scenario for much of humanity” • A global warming of 2°C would result in heading back towards Pliocene-like conditions.

  20. Why They Argue That • Can use interglacial periods to assess what the threshold is before its dangerous • Peak Holocene temp occurred around 8,000 BP • MIS 5e and 11 were less than 1°C warmer than the peak Holocene, thus also less than 1°C warmer than in the year 2000. • Early Pliocene with sea levels 25 m higher than present also shows about a 1°C warming higher than present

  21. Climate Modeling • Otto-Bliesner et al. (2006) • Examined the IPCC CCSM3 Models • Last Glacial Maximum • Global cooling of 4.5°C with Tropical SST cooling of 1.7°C • Half of the cooling is from reduced CO2 levels (~50% of present-day) • Increase in Antarctic currents and deep water stratification and weaker North Atlantic • Mid-Holocene • Global cooling of less than 0.1°C • Regional and seasonal variations are more significant with weaker ENSO variability

  22. The Paleoclimatic Approach • Advantages • Can test theories on the limits and sensitivities of the climate system with boundary conditions that can be validated to a certain extent. • If models show something significant, it’s possible to examine cores to try to find evidence • Disadvantages • If it happened in the past, it does not mean the climate system will react the same way • Although improvements have been made, there are uncertainties for both models and the proxy records

  23. Resources • Larry Peterson – MGG 676 Paleoclimatology • Lea, D.W. (2004): The 100,000-Yr Cycle in Tropical SST, Greenhouse Forcing, and Climate Sensitivity. Journal of Climate, 17, 2170-2179. • Otto-Bliesner, B.L. and co-authors (2006): Last Glacial Maximum and Holocene Climate in CCSM3. Journal of Climate, 19, 2526-2544. • Hansen and Sato 2011: