Resilient terrestrial ecosystems at the Paleocene-Eocene Thermal Maximum (Invited)

The Paleocene-Eocene Thermal Maximum (PETM) was an interval of global warming lasting ~200 ka that began ~56 Ma. Global temperature rose 5-8 °C in association with the emission of thousands of Pg of carbon into the ocean-atmosphere system. PETM rocks and fossils are extensively exposed in the SE Bighorn Basin of Wyoming, where the event is represented by ~40 m of fluvial rocks. Fossil plants demonstrate a rapid and nearly complete turnover in floral composition that also suggests a change in the structure of vegetation. Floras collected from the last ~50 ka of the Paleocene are composed of Platanaceae (sycamores), Betulaceae (birches), Fagaceae (oaks), Lauraceae (laurels), Juglandaceae (walnuts), Cercidiphyllaceae (katsura), Taxodiaceae (dawn redwood), and Arecaceae (palms), among others. Many of these families are most diverse and abundant today in temperate to subtropical, mid-latitude forests. During the body of the carbon isotope excursion (CIE) associated with the PETM fossil floras have a completely different composition. All of the latest Paleocene plant types are absent, except for palms, and instead the floras are dominated by Fabaceae (bean family). Other taxa include Sapindaceae (soapberry), Annonaceae (paw-paw), and Hernandiaceae. Where living relatives are known, they live in dry tropical forests of Central and South America. This floral composition is maintained through the ~30 m of section representing the ~110 ka-long body of the CIE, the same interval characterized by dwarfed mammalian faunas. During the recovery phase of the CIE most of the latest Paleocene plants returned to the area of study, although some new taxa appeared, apparently coming in from Europe or Asia. The distinctive PETM floral types are not seen after the recovery phase of the CIE. Change in floral composition during the PETM apparently represents regional extirpations of populations of plants that preferred warm, mesic conditions, and northward range extensions of plants that preferred dry tropical climates. This process was reversed at the end of the PETM. Although characteristics of PETM vegetation cannot be assessed directly, the distribution of living relatives is consistent with the idea that PETM vegetation was more water-stressed and more open than pre- and post-PETM vegetation. This is also matches inference from paleosol features. The radical change in composition and probable structure of vegetation across the PETM is particularly notable in light of the low extinction rates at this time. Although there is strong evidence of rapid range change and rapid evolution, the increase in temperature and decrease in precipitation do not appear to have exceeded the capacity of lineages to respond, even though the PETM is cited as an example of geologically rapid environmental change.