B14D-01 – Intensification of Climate–Carbon Feedbacks after 2100 and Implications for Disturbance Regimes (Invited)

Authors

James Randerson (jranders at uci dot edu)

University of California Irvine

Keith Lindsay

National Center for Atmospheric Research

Ernesto Muñoz

National Center for Atmospheric Research

Weiwei Fu

University of California Irvine

Forrest Hoffman

University of California Irvine; Oak Ridge National Laboratory

Jefferson Moore

University of California Irvine

Scott Doney

Woods Hole Oceanographic Institute

Natalie Mahowald

Cornell University

Gordon Bonan

National Center for Atmospheric Research

Monday, December 15, 2014 04:00 PM – 04:15 PM
Moscone West 2003

Long-term ecosystem and carbon cycle responses to climate change are needed to inform mitigation policy, yet our understanding of how these responses may evolve after 2100 remains highly uncertain. Using the Community Earth System Model (version 1.0), we quantified climate–carbon feedbacks from 1850 to 2300 for the Representative Concentration Pathway 8.5 (and its extension). In three simulations, land and ocean biogeochemical models were exposed to the same trajectory of increasing atmospheric CO₂. In one simulation, atmospheric CO₂ and other forcing agents were radiatively active (fully coupled), modifying temperature and other aspects of climate. In another, CO₂ was radiatively uncoupled, and in the third, both CO₂ and other atmospheric forcing agents (including CH₄, N₂, and aerosols) were radiatively uncoupled. In the fully coupled simulation, global mean air temperatures increased by 9.3°C from 1850 to 2300, with 4.4°C of this warming occurring after 2100. Without radiative forcing from CO₂, cumulative warming was much lower at 2.4°C, but exceeding 2°C targets needed to avoid dangerous interference with the climate system. In response to climate change, ocean and land rates of carbon uptake were reduced, with the size of the impact increasing over time. In the oceans, reductions in cumulative carbon uptake from climate change increased from 3% during the 20^th century to 40% during the 23^rd century. By 2300, climate change had reduced cumulative ocean uptake by 330 Pg C, from 1410 Pg C to 1080 Pg C. Most of this reduction occurred after 2100 as a consequence of increases in surface stratification and decreases in Atlantic meridional overturning circulation. Land fluxes similarly diverged over time, with climate change inducing a cumulative loss of 230 Pg C by 2300. On land the intensification of the hydrological cycle globally increased terrestrial water storage, although asymmetric responses were observed across different continents in the tropics. Net loss of carbon from tropical forest ecosystems, in response to large temperature increases, were partly offset by increases in carbon uptake in temperate and high latitude ecosystems. We conclude by presenting an assessment of how climate variability over land and burned area change century by century.