Carbon Isotope Discrimination in C3 Land Plants is Independent of Natural Variations in p_CO2

The δ ¹³ C of terrestrial C3 plant tissues and soil organic matter is important for understanding the carbon cycle, inferring past climatic and ecological conditions, and predicting responses of vegetation to future climate change. Plant δ ¹³ C depends on the δ ¹³ C of atmospheric CO ₂ and and mean annual precipitation (MAP), but an unresolved decades-long debate centres on whether terrestrial C3 plant δ ¹³ C responds to p _{CO 2} . In this study, the p _{CO 2} -dependence of C3 land plant δ ¹³ C was tested using isotopic records from low- and high-p _{CO 2} times spanning historical through Eocene data. Historical data do not resolve a clear p _{CO 2} -effect (-1.2 ± 1.0 to 0.6 ± 1.0 ‰/100 ppmv). Organic carbon records across the Pleistocene-Holocene transition are too affected by changes in MAP, carbon sources, and potential differential degradation to quantify p _{CO 2} -effects directly, but limits of ≤1.0 ‰/100 ppmv or ~0 ‰/100 ppmv are permissible. Fossil collagen and tooth enamel data constrain p _{CO 2} -effects most tightly to -0.03 ± 0.13 and -0.03 ± 0.24 ‰/100 ppmv between 200 and 700 ppmv. Combining all constraints yields a preferred value of 0.0 ± 0.3 ‰/100 ppmv (2 s.e.). Recent models of p _{CO 2} -dependence imply unrealistic MAP for Cenozoic records.