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   <subfield code="a">Minor stable carbon isotope fractionation between respired carbon dioxide and bulk soil organic matter during laboratory incubation of topsoil</subfield>
   <subfield code="h">[Elektronische Daten]</subfield>
   <subfield code="c">[D. Breecker, S. Bergel, M. Nadel, M. Tremblay, R. Osuna-Orozco, T. Larson, Z. Sharp]</subfield>
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   <subfield code="a">A common assumption in paleoenvironmental reconstructions using soils is that the carbon isotope composition of soil-respired CO2 is equivalent to the carbon isotope composition of bulk soil organic matter (SOM). However, the occurrence of a non-zero per mil carbon isotope enrichment factor between CO2 and SOM ( $$\varepsilon_{{{\text{CO}}_{ 2} - {\text{SOM}}}}$$ ε CO 2 - SOM ) during soil respiration is the most widely accepted explanation for the down-profile increase in SOM δ13C values commonly observed in well-drained soils. In order to shed light on this apparent discrepancy, we incubated soil samples collected from the top 2cm of soils with pure C3 vegetation and compared the δ13C values of soil-respired CO2 to the δ13C values of bulk SOM. Our results show near-zero $$\varepsilon_{{{\text{CO}}_{ 2} - {\text{SOM}}}}$$ ε CO 2 - SOM values (−0.3 to 0.4‰), supporting the use of paleosol organic matter as a proxy for paleo soil-respired CO2. Significantly more negative $$\varepsilon_{{{\text{CO}}_{ 2} - {\text{SOM}}}}$$ ε CO 2 - SOM values are required to explain the typical δ13C profiles of SOM in well-drained soils. Therefore our results also suggest that typical SOM δ13C profiles result from either (1) a process other than carbon isotope fractionation between CO2 and SOM during soil respiration or (2) $$\varepsilon_{{{\text{CO}}_{ 2} - {\text{SOM}}}}$$ ε CO 2 - SOM values that become increasingly negative as SOM matures.</subfield>
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   <subfield code="u">The Department of Geological Sciences, The University of Texas at Austin, Austin, TX, USA</subfield>
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   <subfield code="a">Metadata rights reserved</subfield>
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