Carbon-13 natural abundance as a tool to study the dynamics of lignin monomers in soil: an appraisal at the Closeaux experimental field (France)

Dignac, Marie-France; Bahri, Haithem; Rumpel, Cornélia; Rasse, Daniel P.; Bardoux, Gérard; Balesdent, Jérôme; Girardin, Cyril; Chenu, Claire; Mariotti, André

doi:10.1016/j.geoderma.2004.12.022

Cited by 200 publications

(180 citation statements)

References 40 publications

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“…Hence, the apparent slow turnover rate of lipid C in the Phaeozem was mirrored by fossil-C contaminations, and, if the latter are likely to be ubiquitous, turnover times of lipid compound classes in general may be underestimated. Nevertheless, and in agreement with other findings on individual C constituents (Dignac et al, 2005;Derrien et al, 2006), the turnover of the lipids was faster than that of bulk soil OC (Fig. 3).…”

Section: Extractable Lipidssupporting

confidence: 92%

“…Apparently there was a minor contribution of fresh plant material to this SOM (Nierop et al, 2005). And indeed, it has also been reported for similar soil types that lignin rapidly decomposes and does not contribute as much to SOM as other, potentially more labile compounds may (Dignac et al, 2005;Rasse et al, 2006;Heim and Schmidt, 2007). The differences in natural 13 C abundances allowed for the calculation of turnover times for the pyrolysis products.…”

Section: Pyrolysis Productsmentioning

confidence: 61%

“…In addition, analysis of the quantity and recalcitrance of individual organic compounds and groups of compounds provides information about their stability and their significance for sequestration and stabilization of soil OC. This approach has recently been successfully applied to soil lipids (Wiesenberg et al, 2004a, b), lignin (Dignac et al, 2005;Heim and Schmidt, 2007), carbohydrates (Derrien et al, 2006), amino acid enantiomers (Glaser and Amelung, 2002), phospholipids fatty acids (Kramer and Gleixner, 2006), and pyrolysis products (Gleixner et al, 2002). Much of this research has been performed in the framework of the Priority Program 1090 ("Soils as sinks and sources of CO 2 ") of the German Science Foundation (cf., Kögel-Knabner et al, 2008, this issue, pp.…”

Section: Introductionmentioning

confidence: 99%

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Storage and stability of organic matter and fossil carbon in a Luvisol and Phaeozem with continuous maize cropping: A synthesis

Flessa

Amelung

Helfrich

et al. 2008

Z. Pflanzenernähr. Bodenk.

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Quantitative information about the amount and stability of organic carbon (OC) in different soil organic-matter (OM) fractions and in specific organic compounds and compound-classes is needed to improve our understanding of organic-matter sequestration in soils. In the present paper, we summarize and integrate results performed on two different arable soils with continuous maize cropping (a) Stagnic Luvisol with maize cropping for 24 y, b) Luvic Phaeozem with maize cropping for 39 y) to identify (1) the storage of OC in different soil organic-matter fractions, (2) the function of these fractions with respect to soil-OC stabilization, (3) the importance and partitioning of fossil-C deposits, and (4) the rates of soil-OC stabilization as assessed by compound-specific isotope analyses. The fractionation procedures included particle-size fractionation, density fractionation, aggregate fractionation, acid hydrolysis, different oxidation procedures, isolation of extractable lipids and phospholipid fatty acids, pyrolysis, and the determination of black C. Stability of OC was determined by 13 C and 14 C analyses. The main inputs of OC were plant litter (both sites) and deposition of fossil C likely from coal combustion and lignite dust (only Phaeozem). Total soil OC stocks down to a depth of 65 cm (7.83 kg m -2 in the Luvisol and 9.66 kg m -2 in the Phaeozem) consisted mainly of mineral-bound OC (87% of total SOC in the Luvisol and 69% in the Phaeozem). In the Luvisol, free light particulate OM, OM associated with sand and coarse silt, and particulate OM occluded in macro-aggregates represented SOM fractions with mean turnover times shorter than that of the bulk soil OC (54 y). Additionally, the turnover of all individual compounds or compound classes (except for black carbon) was faster than that of bulk soil OC. These OM fractions that were less stable than the bulk soil OM made up 13% to 20% of the total OC. Organic matter in fine and medium silt and clay fractions, particulate OM occluded in micro-aggregates (53-250 lm) and OM resistant to acid hydrolysis had intermediate turnover times of about 50-100 y. These fractions with intermediate turnover times contributed 70%-80% to total soil OC. Passive OM with turnover times >200 y was isolated from the mineral-bound OM by different oxidation procedures (H 2 O 2 , Na 2 S 2 O 8 ) and made up ≤10% of the total OC. The isotopic signature of PLFAs suggests an efficient recycling of OC derived from C3 substrate. In the Phaeozem, partitioning of maize-derived C exhibited a pattern similar to the Luvisol, but turnover rates of vegetation-derived soil OC were lower, probably because of the considerably smaller input of plant residues. Fossil C contributed approx. 50% to the total OC and accumulated preferentially in the particulate OM occluded in aggregates and in the fine-sand and

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Section: Extractable Lipidssupporting

confidence: 92%

Section: Pyrolysis Productsmentioning

confidence: 61%

Section: Introductionmentioning

confidence: 99%

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Storage and stability of organic matter and fossil carbon in a Luvisol and Phaeozem with continuous maize cropping: A synthesis

Flessa

Amelung

Helfrich

et al. 2008

Z. Pflanzenernähr. Bodenk.

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“…Different functions of the continuous changes of SOM availability with its aging were suggested (Bosatta andÅgren, 1985;Manzoni et al, 2009;Bruun et al, 2010) and were proven experimentally (Ågren and Bosatta, 1998). A good possibility to provide experimental basis for such continuous quality function are C 3 → C 4 chronosequence experiments such as "Les Closeaux" INRA field experiment in Versailles (Dignac et al, 2005).…”

Section: Abrupt Permanent Impact = Continuous Labelingmentioning

confidence: 99%

How to link soil C pools with CO<sub>2</sub> fluxes?

Kuzyakov¹

2011

Biogeosciences

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Abstract. Despite the importance of carbon (C) pools and CO 2 fluxes in terrestrial ecosystems and especially in soils, as well as many attempts to assign fluxes to specific pools, this challenge remains unsolved. Interestingly, scientists investigating pools are not closely linked with scientists studying fluxes. This review therefore focused on experimental approaches enabling soil C pools to be linked with CO 2 flux from the soil. The background, advantages and shortcomings of uncoupled approaches (measuring only pools or fluxes) and of coupled approaches (measuring both pools and fluxes) were evaluated and their prerequisites -steady state of pools and isotopic steady state -described. The uncoupled approaches include: (i) monitoring the decrease of C pools in long-term fallow bare soil lacking C input over decades, (ii) analyzing components of CO 2 efflux dynamics by incubating soil without new C input over months or years, and (iii) analyzing turnover rates of C pools based on their 13 C and 14 C isotopic signature. The uncoupled approaches are applicable for non-steady state conditions only and have limited explanatory power. The more advantageous coupled approaches partition simultaneously pools and fluxes based on one of three types of changes in the isotopic signature of input C compared to soil C: (i) abrupt permanent, (ii) gradual permanent, and (iii) abrupt temporary impacts. I show how the maximal sensitivity of the approaches depends on the differences in the isotopic signature of pools with fast and slow turnover rates. The promising coupled approaches include: (a) δ 13 C of C pools and CO 2 efflux from soil after C 3 /C 4 vegetation changes or in FACE experiments (both corresponding to continuous labeling), (b) addition of 13 C or 14 C labeled organics (corresponding to pulse labeling), and (c) bomb-14 C. I show that physical separation of soil C pools is not a prerequisite to estimate pool size or to link pools with Correspondence to: Y. Kuzyakov (kuzyakov@gwdg.de) fluxes. Based on simple simulation of C aging in soil after the input, the discordance of MRT of C in pools and of C released in CO 2 was demonstrated. This discordance of MRT between pools and fluxes shows that the use of MRT of pools alone underestimates the fluxes at least for two times. The future challenges include combining two or more promising approaches to elucidate more than two C sources for CO 2 fluxes, and linking scientific communities investigating the pools with those investigating the fluxes. PreambleTwo high-ranking international conferences motivated me to prepare this review. At the first conference the results of various approaches to separate pools of soil organic matter (SOM), and thus carbon (C) pools in soil, were presented and discussed. These approaches are based on chemical and physical fractionations (extractability, particle and aggregate size, density, etc.) as well as their combinations (von Lutzow et al., 2007;Bruun et al., 2010). Despite some progress to separate C pools of different age and thus...

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“…Recently, the study of lignin decay on a molecular level has improved through compound-specific stable isotope analysis of isotopically labeled lignin biomarkers (Dignac et al, 2005;Heim and Schmidt, 2007a). This method provides the opportunity to study the decay of the SOC component lignin in long-term field experiments (Bahri et al, 2006;Hofmann et al, 2009).…”

Section: Introductionmentioning

confidence: 99%

Mineral fertilization did not affect decay of old lignin and SOC in a <sup>13</sup>C-labeled arable soil over 36 years

et al. 2009

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Abstract. Retardation of soil organic carbon (SOC) decay after nitrogen addition to litter or soil has been suggested in several recent studies and has been attributed to a retardation in lignin decay. With our study we tested the long-term effect of mineral fertilization (N+P) on the decay of the SOC component lignin in arable soil. To achieve this, we tracked 13 C-labeled lignin and SOC in an arable soil that is part of a 36-year field experiment (conversion from C 3 to C 4 crops) with two mineral fertilization levels. We could show that fertilization neither retarded nor enhanced the decay of old SOC or lignin over a period of 36 years, proposing that decay of lignin was less sensitive to fertilization than previously suggested. However, for new, C 4 -derived lignin there were indications that decay might have been enhanced by the fertilization treatment, whereas decay of new SOC was unaffected.

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Carbon-13 natural abundance as a tool to study the dynamics of lignin monomers in soil: an appraisal at the Closeaux experimental field (France)

Cited by 200 publications

References 40 publications

Storage and stability of organic matter and fossil carbon in a Luvisol and Phaeozem with continuous maize cropping: A synthesis

Storage and stability of organic matter and fossil carbon in a Luvisol and Phaeozem with continuous maize cropping: A synthesis

How to link soil C pools with CO<sub>2</sub> fluxes?

Mineral fertilization did not affect decay of old lignin and SOC in a <sup>13</sup>C-labeled arable soil over 36 years

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Carbon-13 natural abundance as a tool to study the dynamics of lignin monomers in soil: an appraisal at the Closeaux experimental field (France)

Cited by 200 publications

References 40 publications

Storage and stability of organic matter and fossil carbon in a Luvisol and Phaeozem with continuous maize cropping: A synthesis

Storage and stability of organic matter and fossil carbon in a Luvisol and Phaeozem with continuous maize cropping: A synthesis

How to link soil C pools with CO&lt;sub&gt;2&lt;/sub&gt; fluxes?

Mineral fertilization did not affect decay of old lignin and SOC in a &lt;sup&gt;13&lt;/sup&gt;C-labeled arable soil over 36 years

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How to link soil C pools with CO<sub>2</sub> fluxes?

Mineral fertilization did not affect decay of old lignin and SOC in a <sup>13</sup>C-labeled arable soil over 36 years