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The Paleocene-Eocene Thermal Maximum (PETM), a rapid global warming event ~56 million years ago caused by a large release of isotopically-light carbon into earth’s atmosphere and oceans, provides geologic parallels to anthropogenic climate change. Thousands of petagrams of carbon were released in less than 20ka, causing a global negative carbon isotopic excursion (CIE), ocean acidification, a 5-8o C increase in global temperatures, and at least a doubling of atmospheric CO2 levels (McInerney & Wing, 2011). In midlatitude continental interiors, increased temperatures led to lower mean annual rainfall, causing more seasonally dry conditions and increased water stress (Kraus et al., 2015). PETM sandstones in both the Bighorn and Piceance Creek Basin record changes in fluvial systems, likely caused by changes in sediment flux, increased variability of precipitation, reductions in vegetation cover, or some combination of these (Foreman et al., 2012; Foreman, 2014). Few extinctions occurred during the PETM, but terrestrial and marine organisms experienced major shifts in geographic ranges, changes in food sources, and rapid evolution (McInerney & Wing, 2011). The best record of plant responses to PETM environmental change to date comes from the Bighorn Basin in northwestern Wyoming. Wing et al. (2005) demonstrated a decrease in leaf size, reflecting an increase in water stress. Taxonomic analyses showed a distinct difference in flora composition during the PETM versus directly before or after (Wing & Currano, 2013). Conifers and a combination of deciduous and evergreen broadleaved families were the primary preand post-PETM megafloras; PETM megafloras lack conifers but were abundant in the dry-tolerant Fabaceae family (Wing et al. 2005; Wing & Currano, 2013; Smith et al. 2007). During the CIE recovery, many typical Paleocene plants returned, implying that the plant populations were able to migrate to refugia during the Thermal Maximum (Wing & Currano, 2013).

Advisor: Joan E. Fryxell VEGETATION STRUCTURE AND LITHOLOGY RESPONSE TO THE PALEOCENE-EOCENE THERMAL MAXIMUM IN THE HANNA BASIN, WYOMING