Paleoclimate: What can the past tell us about the …Paleoclimate: What can the past tell us about...
Transcript of Paleoclimate: What can the past tell us about the …Paleoclimate: What can the past tell us about...
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Paleoclimate: What can the past tell us about
the present and future?
12.340 Global Warming Science February 14, 2012
David McGee
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Recent observed trends: Greenhouse gases
Image courtesy of NOAA.
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Recent observations: Land surface temperature
Climate Change 2007: The Physical Science Basis. Working Group I Contribution to the Fourth Assessment Reportof the Intergovernmental Panel on Climate Change, Figure 3.1. Cambridge University Press. Used with permission.
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Recent observations: Sea surface temperature
Land
Sea
Climate Change 2007: The Physical Science Basis. Working Group I Contribution to the Fourth Assessment Reportof the Intergovernmental Panel on Climate Change, Figure 3.8. Cambridge University Press. Used with permission.
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Recent observations: Drought
Climate Change 2007: The Physical Science Basis. Working Group I Contribution to the Fourth Assessment Report of theIntergovernmental Panel on Climate Change, FAQ 3.2, Figure 1. Cambridge University Press. Used with permission.
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Recent observations: Sea ice
Public domain image courtesy of National Snow and Ice Data Center, University of Colorado, Boulder.6
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Recent observed trends: Glacier extent
Muir Glacier, Alaska
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Public domain image courtesy of National Snow and Ice Data Center, University of Colorado, Boulder.
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Recent observed trends: Glacier extent
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Public domain image courtesy of National Snow and Ice Data Center, University of Colorado, Boulder.
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Recent observed trends: Ice sheet mass loss
This image has been removed due to copyright restrictions. Please see Figure 2 on http://onlinelibrary.wiley.com/doi/10.1029/2011GL046583/full.
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Recent observed trends: Sea level rise
Climate Change 2007: The Physical Science Basis. Working Group I Contribution to the Fourth Assessment Report of theIntergovernmental Panel on Climate Change, Figure SPM.3. Cambridge University Press. Used with permission.
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Given these observations, what questions do you have that
records of the pre-instrumental past could help answer?
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How do we get information about past climates?
Climate archives • ice cores • tree rings • ocean and lake sediments • corals • fossils • glacial features • boreholes • stalagmites
Image courtesy of NASA. 12
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A paleoclimatic tour from 400 to 1 Myr ago
(with a few interruptions)
This image has been removed due to copyright restrictions. Please see the photo on http://www.raleighite.com/2013/hs-76-the-tour-guide.
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Climate and CO2 over the last 400 Myr
Climate Change 2007: The Physical Science Basis. Working Group I Contribution to the Fourth Assessment Reportof the Intergovernmental Panel on Climate Change, Figure 6.1. Cambridge University Press. Used with permission.
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This image has been removed due to copyright restrictions. Please see: Figure 2. Beerling, D. J., & Royer, D. L. (2011). Convergent Cenozoic CO2 history. Nature Geoscience, 4(7), 418–420. doi:10.1038/ngeo1186
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Oxygen isotopes: Versatile recorders of paleoclimatic
conditions
Image courtesy of NASA.
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Oxygen isotope fractionation
As a general rule of thumb, 18O tends to be enriched relative to 16O in the most “immobile” state involved in
a reaction or transformation Figure: more energy is needed to break bonds involving heavier isotopes (in this case, H-H vs. H-D vs. D-D, where D=2H, H=1H)
Figure by MIT OpenCourseWare. 17
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Oxygen isotope fractionation
Fractionation increases with decreasing temperature
Figure by MIT OpenCourseWare., after Erez et al., 1983
Figure: δ18O enrichment in cultured foraminifera vs. temperature
This image has been removed due to copyright restrictions.
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Climate over the last 65 Myr (beware the flipping x-axis…)
This image has been removed due to copyright restrictions.
Please see Figure 2 in https://pangea.stanford.edu/research/Oceans/GES206/readings/Zachos2001.pdf
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Oxygen isotope fractionation Water vapor is depleted in 18O relative to liquid water due to the greater mass of H2
18O vs. H216O
Air masses become more 18O-depleted with increasing rain-out and decreasing temperatures
Image courtesy of NASA. 20
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Oxygen isotope fractionation
Because ice sheets are made with 18O-depleted precipitation, ice sheet growth causes global oceans to be enriched in 18O. As a result, global oceans at the peak of the last glacial period had δ18O ~1‰ more positive than at present
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Climate over the last 65 Myr (beware the flipping x-axis…)
This image has been removed due to copyright restrictions.
Please see Figure 2 on https://pangea.stanford.edu/research/Oceans/GES206/readings/Zachos2001.pdf
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Climate and CO2 over the last 65 Myr
This image has been removed due to copyright restrictions. Please see: Figure 1. Beerling, D. J., & Royer, D. L. (2011). Convergent Cenozoic CO2 history. Nature Geoscience, 4(7), 418–420. doi:10.1038/ngeo1186.
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The Pliocene, 5.3-2.6 Myr ago
• pCO2 likely ~400 ppmv • Continents near present positions • Abundant marine and terrestrial sediments
available for study
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The Pliocene, 5.3-2.6 Myr ago
USGS PRISM3 project
Annual average SST anomaly
Reconstructed global average temperature ~2-3 ˚C warmer
than at present
Image courtesy of USGS. 25
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Models appear to underestimate high latitude warming in the Pliocene
What are models missing?
Annual average reconstructed SST-modeled SST
Map view (squares = faunal SST estimates; stars = Mg/Ca or alkenone SST
estimates)
Zonal average
(solid line)
This image has been removed due to copyright restrictions.
Please see: Figure 3 on page, http://www.nature.com/ngeo/journal/v3/n1/full/ngeo706.html
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Pliocene sea levels ~20-30 m above modern
Modern elevation above sea level of a Pliocene shoreline reflecting 14m higher sea level (i.e., full deglaciation of Greenland and West Antarctica) – note that
isostatic adjustments to Plio-Pleistocene ice sheet growth and recent deglaciation causes significant deviations from the “real” (eustatic) sea level difference
This image has been removed due to copyright restrictions.
Please see Figure 2 on http://www.moraymo.us/2011_Raymoetal.pdf
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Problem: Equilibrium vs. transient response
to high pCO2
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The Paleocene-Eocene Thermal Maximum (PETM), 55 Myr ago
Temperature rise
Addition of low-13C carbon to the atmosphere and ocean
This image has been removed due to copyright restrictions.
Please see Figure 5 on https://pangea.stanford.edu/research/Oceans/GES206/readings/Zachos2001.pdf
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The Paleocene-Eocene Thermal Maximum (PETM), 55 Myr ago
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Global temps rose ~5-9˚C in 1-10 kyr
This image has been removed due to copyright restrictions.
Please see Figure 2 on http://www.sciencemag.org/content/302/5650/1551.full
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PETM ocean acidification consistent with large pCO2 increase
This image has been removed due to copyright restrictions.
Please see Figure 1 on http://www.sciencemag.org/content/308/5728/1611.full
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How much carbon was added to the atmosphere?
Method 1: use d13C of source and d13C anomaly to estimate Problem: d13C of potential sources very different (-5 to -60 per mil) Estimates: mostly 3000-8000 GtC (order 1-10 GtC/yr)
Method 2: use amount of carbonate dissolution in ocean sediment cores to estimate how much ocean pH was lowered Problem: requires good spatial coverage of cores, accurate ocean model, and estimate of ocean alkalinity Estimates: <=3000 GtC, or an increase in atmospheric pCO2 by factor of ~1.7. New problem: not enough to explain 5-9˚C warming! (Zeebe et al., Nat. Geosci. 2009)
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Duration of perturbation ~200 kyr
This image has been removed due to copyright restrictions.
Please see Figure 5 on https://pangea.stanford.edu/research/Oceans/GES206/readings/Zachos2001.pdf
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A few questions for paleo-records
• Are modern conditions and rates of change exceptional?
• What the links between GHGs and climate? – CO2-temperature sensitivity (˚C/doubling of CO2) – Natural controls on atmospheric GHG levels
• What were conditions during past warm climates and warmings? – Temp gradients, droughts, sea level, ice sheet
stability in past warm climates – Climate model performance – Potential for nonlinear responses
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References Beerling, D. J., & Royer, D. L. (2011). Convergent Cenozoic CO2 history. Nature Geoscience, 4(7), 418–420. Nature Publishing Group. doi:10.1038/ngeo1186
Lunt, D. J., Haywood, A. M., Schmidt, G. A., Salzmann, U., Valdes, P. J., & Dowsett, H. J. (2009). Earth system sensitivity inferred from Pliocene modelling and data. Nature Geoscience, 3(1), 60–64. Nature Publishing Group. doi:10.1038/ngeo706
Zachos, J., Pagani, M., Sloan, L., Thomas, E., & Billups, K. (2001). Trends, rhythms, and aberrations in global climate 65 Ma to present. Science, 292(5517), 686–693. doi:10.1126/science.1059412
Zachos, J. C. (2003). A Transient Rise in Tropical Sea Surface Temperature During the Paleocene-Eocene Thermal Maximum. Science, 302(5650), 1551–1554. doi:10.1126/science.1090110
Zachos, J. C. (2005). Rapid Acidification of the Ocean During the Paleocene-Eocene Thermal Maximum. Science, 308(5728), 1611–1615. doi:10.1126/science.1109004
Zeebe, R. E., Zachos, J. C., & Dickens, G. R. (2009). Carbon dioxide forcing alone insufficient to explain Palaeocene--Eocene Thermal Maximum warming. Nature Geoscience, 2(8), 576–580. Nature Publishing Group. doi:10.1038/ngeo578
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