Minor stable carbon isotope fractionation between respired carbon dioxide and bulk soil organic matter during laboratory incubation of topsoil
A common assumption in paleoenvironmental reconstructions using soils is that the carbon isotope composition of soil-respired CO₂is 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 C...
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| Veröffentlicht in: | Biogeochemistry 2015-03, Vol.123 (1-2), p.83-98 |
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| creator | Breecker, D. O Bergel, S Nadel, M Tremblay, M. M Osuna-Orozco, R Larson, T. E Sharp, Z. D |
| description | A common assumption in paleoenvironmental reconstructions using soils is that the carbon isotope composition of soil-respired CO₂is 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 CO₂and SOM ([Formula: see text]) 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 2 cm of soils with pure C₃vegetation and compared the δ¹³C values of soil-respired CO₂to the δ¹³C values of bulk SOM. Our results show near-zero [Formula: see text] values (−0.3 to 0.4 ‰), supporting the use of paleosol organic matter as a proxy for paleo soil-respired CO₂. Significantly more negative [Formula: see text] 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 CO₂and SOM during soil respiration or (2) [Formula: see text] values that become increasingly negative as SOM matures. |
| doi_str_mv | 10.1007/s10533-014-0054-3 |
| format | Article |
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O ; Bergel, S ; Nadel, M ; Tremblay, M. M ; Osuna-Orozco, R ; Larson, T. E ; Sharp, Z. D</creator><creatorcontrib>Breecker, D. O ; Bergel, S ; Nadel, M ; Tremblay, M. M ; Osuna-Orozco, R ; Larson, T. E ; Sharp, Z. D</creatorcontrib><description>A common assumption in paleoenvironmental reconstructions using soils is that the carbon isotope composition of soil-respired CO₂is 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 CO₂and SOM ([Formula: see text]) 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 2 cm of soils with pure C₃vegetation and compared the δ¹³C values of soil-respired CO₂to the δ¹³C values of bulk SOM. Our results show near-zero [Formula: see text] values (−0.3 to 0.4 ‰), supporting the use of paleosol organic matter as a proxy for paleo soil-respired CO₂. Significantly more negative [Formula: see text] 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 CO₂and SOM during soil respiration or (2) [Formula: see text] values that become increasingly negative as SOM matures.</description><identifier>ISSN: 0168-2563</identifier><identifier>EISSN: 1573-515X</identifier><identifier>DOI: 10.1007/s10533-014-0054-3</identifier><language>eng</language><publisher>Cham: Springer-Verlag</publisher><subject>biogeochemistry ; Biogeosciences ; Carbon ; Carbon dioxide ; Carbon isotopes ; Earth and Environmental Science ; Earth Sciences ; Ecosystems ; Environmental Chemistry ; Fractionation ; Isotope fractionation ; Isotopes ; Isotopic enrichment ; Life Sciences ; Organic matter ; paleosolic soil types ; Paleosols ; Respiration ; Soil organic matter ; soil respiration ; soil sampling ; Soils ; stable isotopes ; Topsoil</subject><ispartof>Biogeochemistry, 2015-03, Vol.123 (1-2), p.83-98</ispartof><rights>Springer International Publishing 2015</rights><rights>Springer International Publishing Switzerland 2014</rights><rights>Springer International Publishing Switzerland 2015</rights><lds50>peer_reviewed</lds50><woscitedreferencessubscribed>false</woscitedreferencessubscribed><citedby>FETCH-LOGICAL-a488t-8c9e0db7fdafa0c1966e9759c81a4993781d86dc9c346dce9bd02c0ad24e7a313</citedby><cites>FETCH-LOGICAL-a488t-8c9e0db7fdafa0c1966e9759c81a4993781d86dc9c346dce9bd02c0ad24e7a313</cites></display><links><openurl>$$Topenurl_article</openurl><openurlfulltext>$$Topenurlfull_article</openurlfulltext><thumbnail>$$Tsyndetics_thumb_exl</thumbnail><linktopdf>$$Uhttps://www.jstor.org/stable/pdf/24713177$$EPDF$$P50$$Gjstor$$H</linktopdf><linktohtml>$$Uhttps://www.jstor.org/stable/24713177$$EHTML$$P50$$Gjstor$$H</linktohtml><link.rule.ids>314,776,780,799,27901,27902,41464,42533,51294,57992,58225</link.rule.ids></links><search><creatorcontrib>Breecker, D. O</creatorcontrib><creatorcontrib>Bergel, S</creatorcontrib><creatorcontrib>Nadel, M</creatorcontrib><creatorcontrib>Tremblay, M. M</creatorcontrib><creatorcontrib>Osuna-Orozco, R</creatorcontrib><creatorcontrib>Larson, T. E</creatorcontrib><creatorcontrib>Sharp, Z. D</creatorcontrib><title>Minor stable carbon isotope fractionation between respired carbon dioxide and bulk soil organic matter during laboratory incubation of topsoil</title><title>Biogeochemistry</title><addtitle>Biogeochemistry</addtitle><description>A common assumption in paleoenvironmental reconstructions using soils is that the carbon isotope composition of soil-respired CO₂is 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 CO₂and SOM ([Formula: see text]) 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 2 cm of soils with pure C₃vegetation and compared the δ¹³C values of soil-respired CO₂to the δ¹³C values of bulk SOM. Our results show near-zero [Formula: see text] values (−0.3 to 0.4 ‰), supporting the use of paleosol organic matter as a proxy for paleo soil-respired CO₂. Significantly more negative [Formula: see text] 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 CO₂and SOM during soil respiration or (2) [Formula: see text] values that become increasingly negative as SOM matures.</description><subject>biogeochemistry</subject><subject>Biogeosciences</subject><subject>Carbon</subject><subject>Carbon dioxide</subject><subject>Carbon isotopes</subject><subject>Earth and Environmental Science</subject><subject>Earth Sciences</subject><subject>Ecosystems</subject><subject>Environmental Chemistry</subject><subject>Fractionation</subject><subject>Isotope fractionation</subject><subject>Isotopes</subject><subject>Isotopic enrichment</subject><subject>Life Sciences</subject><subject>Organic matter</subject><subject>paleosolic soil types</subject><subject>Paleosols</subject><subject>Respiration</subject><subject>Soil organic matter</subject><subject>soil respiration</subject><subject>soil sampling</subject><subject>Soils</subject><subject>stable isotopes</subject><subject>Topsoil</subject><issn>0168-2563</issn><issn>1573-515X</issn><fulltext>true</fulltext><rsrctype>article</rsrctype><creationdate>2015</creationdate><recordtype>article</recordtype><sourceid>BENPR</sourceid><recordid>eNp9kc-q1TAQxosoeLz6AC7EgBs31UnSJulSLtc_cMWFXnAXpsn0kGNPUpMWvS_hM9tSFXHhZmYxv--bYb6qeszhBQfQLwuHVsoaeFMDtE0t71QH3mpZt7z9fLc6AFemFq2S96sHpZwAoNMgD9WP9yGmzMqM_UjMYe5TZKGkOU3EhoxuDiniVlhP8zeiyDKVKWTyv2kf0vfgiWH0rF_GL6ykMLKUjxiDY2ecZ8rMLznEIxuxTxnnlG9ZiG7pd-c0sHXfJntY3RtwLPToV7-obl5ffbp8W19_ePPu8tV1jY0xc21cR-B7PXgcEBzvlKJOt50zHJuuk9pwb5R3nZPN2qjrPQgH6EVDGiWXF9Xz3XfK6etCZbbnUByNI0ZKS7FcKSOUEiBW9Nk_6CktOa7XbRRIrkCZleI75XIqJdNgpxzOmG8tB7slZPeE7JqQ3RKyctWIXVOm7TmU_3L-j-jJLjqV9Y1_tohGc8m1XudP9_mAyeIxh2JvPgrgLYCAxgiQPwGsgKmU</recordid><startdate>20150301</startdate><enddate>20150301</enddate><creator>Breecker, D. 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O</au><au>Bergel, S</au><au>Nadel, M</au><au>Tremblay, M. M</au><au>Osuna-Orozco, R</au><au>Larson, T. E</au><au>Sharp, Z. D</au><format>journal</format><genre>article</genre><ristype>JOUR</ristype><atitle>Minor stable carbon isotope fractionation between respired carbon dioxide and bulk soil organic matter during laboratory incubation of topsoil</atitle><jtitle>Biogeochemistry</jtitle><stitle>Biogeochemistry</stitle><date>2015-03-01</date><risdate>2015</risdate><volume>123</volume><issue>1-2</issue><spage>83</spage><epage>98</epage><pages>83-98</pages><issn>0168-2563</issn><eissn>1573-515X</eissn><abstract>A common assumption in paleoenvironmental reconstructions using soils is that the carbon isotope composition of soil-respired CO₂is 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 CO₂and SOM ([Formula: see text]) 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 2 cm of soils with pure C₃vegetation and compared the δ¹³C values of soil-respired CO₂to the δ¹³C values of bulk SOM. Our results show near-zero [Formula: see text] values (−0.3 to 0.4 ‰), supporting the use of paleosol organic matter as a proxy for paleo soil-respired CO₂. Significantly more negative [Formula: see text] 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 CO₂and SOM during soil respiration or (2) [Formula: see text] values that become increasingly negative as SOM matures.</abstract><cop>Cham</cop><pub>Springer-Verlag</pub><doi>10.1007/s10533-014-0054-3</doi><tpages>16</tpages></addata></record> |
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| subjects | biogeochemistry Biogeosciences Carbon Carbon dioxide Carbon isotopes Earth and Environmental Science Earth Sciences Ecosystems Environmental Chemistry Fractionation Isotope fractionation Isotopes Isotopic enrichment Life Sciences Organic matter paleosolic soil types Paleosols Respiration Soil organic matter soil respiration soil sampling Soils stable isotopes Topsoil |
| title | Minor stable carbon isotope fractionation between respired carbon dioxide and bulk soil organic matter during laboratory incubation of topsoil |
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