Paleocene-Eocene Thermal Maximum
The Paleocene–Eocene Thermal Maximum (PETM) was a 'blip' in the smooth running of Earth's environment and climate that took place about 56 million years ago (see image to right). It is of great significance because it most probably represents the closest analogue to the changes being forced on the Earth at present by humanity. If we can work out what happened at the PETM, then it will most likely be very useful in helping us understand what is likely to happen in the future.
The PETM Event
Paleoclimatologists have collected large amounts of evidence about what happened at the PETM, both on land and also in the oceans. It seems clear that there was rapid and considerable global warming by ~5 °C. There is also evidence of ocean acidification, although this evidence needs to be carefully interpreted. Many species of benthic foraminifera went extinct. There was both rapid extinction and speciation (birth of new species) among mammals. There was a pronounced 'excursion' (temporary shift) to more negative δ13C values in ocean sediments. This is in addition to the temporary shift in δ18O shift shown in the right-hand image.
What Triggered the PETM?
A first question is what caused the PETM? A whole raft of hypotheses have been put forward, but out of these there are two main candidates that most people currently favour. The first of these suggests that it was a release of biogenic methane from methane clathrates on the seafloor that caused the global warming (Dickens et al, 1997). The second of these also invokes an input of methane, but this time of thermogenic methane (Svensen et al, 2004). The two different carbon sources have different characteristic δ13C values.
This exercise shows how we can get an idea of the process that initiated the PETM. In reality, however, at the present time we are limited in the data that is available to constrain these three parameters of global change. The change in δ13C of benthic foraminifera is the number that is most well known; the magnitude of global warming is also reasonably well-constrained, but the change in global average lysocline depth is less well determined. We know that it shallowed by at least 2km in the South Atlantic (Zachos et al, 2005), but to accurately constrain this number requires a depth transect of ocean cores - an enormous amount of work. We do not have equivalent data from other ocean basins.
How did the Earth System Recover from the Carbon Injection?
Current theory predicts two main responses to the carbon injection and ocean acidification at the PETM.
Carbonate Ion Recovery
The first predicted response is that carbonate compensation should return the saturation state (carbonate ion concentration) of the ocean back to pre-PETM levels over the course of about 10,000 years.
How does this predicted speed of recovery compare to the time that it takes for CaCO3 MAR (mass accumulation rates) and lysocline depth to recover in the South Atlantic (Zachos et al., 2005)?
Left-Over CO2 and Global Warming
A second aspect of the predicted response is that any injection of CO2 should leave behind a long-lasting (hundreds of thousands of years) residual of elevated CO2 and global warming. This is described for the present-day and fossil fuels on the page describing the long-term legacy of elevated CO2.
- Zachos, J.C. et al. (2005). Rapid Acidification of the Ocean During the Paleocene-Eocene Thermal Maximum. Science 308, 1611-1615.
- Nunes, F. & Norris, R.D. (2006). Abrupt reversal in ocean overturning during the Palaeocene/Eocene warm period. Nature 439, 60-63.
- Zeebe, R.E. & Zachos, J.C. (2007). Reversed deep-sea carbonate ion basin gradient during Paleocene-Eocene thermal maximum. Paleoceanography 22, PA3201, doi:10.1029/2006PA001395.
- Dickens, G.R., Castillo, M.M. & Walker, J.C.G. (1997). A blast of gas in the latest Paleocene; simulating first-order effects of massive dissociation of oceanic methane hydrate. Geology 25, 259-262.
- Svensen, H. et al. (2004). Release of methane from a volcanic basin as a mechanism for initial Eocene global warming. Nature 429, 542-545.