TY  - JOUR
A1  - Hoogakker, Babette A. A.
A1  - Smith, Robin S.
A1  - Singarayer, Joy
A1  - Marchant, Robert
A1  - Prentice, I. Colin
A1  - Allen, Judy R. M.
A1  - Anderson, R. Scott
A1  - Bhagwat, Shonil A.
A1  - Behling, Hermann
A1  - Borisova, Olga
A1  - Bush, Mark B.
A1  - Correa-Metrio, Alexander
A1  - De Vernal, Anne
A1  - Finch, Jemma M.
A1  - Fréchette, Bianca
A1  - Lozano-García, Socorro
A1  - Gosling, William D.
A1  - Granoszewski, Wojciech
A1  - Grimm, Eric C.
A1  - Grüger, Eberhard
A1  - Hanselman, Jennifer
A1  - Harrison, Sandy P.
A1  - Hill, Trevor R.
A1  - Huntley, Brian
A1  - Jimenez-Moreno, Gonzalo
A1  - Kershaw, Arnold Peter
A1  - Ledru, Marie-Pierre
A1  - Magri, Donatella
A1  - McKenzie, Merna
A1  - Müller, Ulrich
A1  - Nakagawa, Takeshi
A1  - Novenko, Elena
A1  - Penny, Daniel
A1  - Sadori, Laura
A1  - Scott, Louis
A1  - Stevenson, Janelle
A1  - Valdes, Paul J.
A1  - Vandergoes, Marcus
A1  - Velichko, Andrey
A1  - Whitlock, Cathy
A1  - Tzedakis, Chronis
T1  - Terrestrial biosphere changes over the last 120 kyr and their impact on ocean δ 13 C
T2  - Climate of the past discussions
N2  - A new global synthesis and biomization of long (> 40 kyr) pollen-data records is presented, and used with simulations from the HadCM3 and FAMOUS climate models to analyse the dynamics of the global terrestrial biosphere and carbon storage over the last glacial–interglacial cycle. Global modelled (BIOME4) biome distributions over time generally agree well with those inferred from pollen data. The two climate models show good agreement in global net primary productivity (NPP). NPP is strongly influenced by atmospheric carbon dioxide (CO2) concentrations through CO2 fertilization. The combined effects of modelled changes in vegetation and (via a simple model) soil carbon result in a global terrestrial carbon storage at the Last Glacial Maximum that is 210–470 Pg C less than in pre-industrial time. Without the contribution from exposed glacial continental shelves the reduction would be larger, 330–960 Pg C. Other intervals of low terrestrial carbon storage include stadial intervals at 108 and 85 kaBP, and between 60 and 65 kaBP during Marine Isotope Stage 4. Terrestrial carbon storage, determined by the balance of global NPP and decomposition, influences the stable carbon isotope composition (δ 13C) of seawater because terrestrial organic carbon is depleted in 13C. Using a simple carbon-isotope mass balance equation we find agreement in trends between modelled ocean δ 13C based on modelled land carbon storage, and palaeo-archives of ocean δ 13C, confirming that terrestrial carbon storage variations may be important drivers of ocean δ 13 C changes.
Y1  - 2015
UR  - http://publikationen.ub.uni-frankfurt.de/frontdoor/index/index/docId/42016
UR  - https://nbn-resolving.org/urn:nbn:de:hebis:30:3-420167
UR  - http://www.clim-past-discuss.net/11/1031/2015
SN  - 1814-9359
SN  - 1814-9340
N1  - © Author(s) 2015. CC Attribution 3.0 License.
VL  - 11
SP  - 1031
EP  - 1091
PB  - European Geosciences Union
CY  - Katlenburg-Lindau
ER  -