Effect of C3–C4 Vegetation Change on δ13C and δ15N Values of Soil Organic Matter Fractions Separated by Thermal Stability

Kuzyakov, Yakov; Mitusov, Andrei; Schneckenberger, Katja

doi:10.1007/s11104-006-0015-2

Cited by 24 publications

(19 citation statements)

References 27 publications

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“…1), which accords with observations in other studies (e.g., Plante et al, 2005;Kuzyakov et al, 2006). Total contents of residual SOC after thermal oxidation differed significantly between land-use regimes with the highest contents in the grassland soil (Tab.…”

Section: Resultssupporting

confidence: 91%

“…Consequently, despite a significant trend of decreasing C 4 -SOC with increasing temperature, thermal oxidation was incapable of isolating residual SOC fractions of considerably increased microbial stability in this soil. Similarly, Kuzyakov et al (2006) found comparable proportions of C 4 -SOC in thermally labile and stable fractions isolated using TG-DSC in a silty loam 10.5 y after C 3 /C 4 vegetation change. As thermal oxidation is prone to charring, we cannot exclude the possibility that charring of OM contributed to the observed high proportions of young C 4 -SOC fractions resistant to thermal oxidation.…”

Section: Soilmentioning

confidence: 61%

“…200°C and generally have two main peaks (at approx. 300°C and 450°C) (Plante et al, 2005;Kuzyakov et al, 2006). No significant C losses or shifts in d 13 C were found at <200°C and thermal degradation of SOM was found to be largely completed at approx.…”

Section: Methodsmentioning

confidence: 88%

“…No significant C losses or shifts in d 13 C were found at <200°C and thermal degradation of SOM was found to be largely completed at approx. 500°C (Kuzyakov et al, 2006). After thermal oxidation, soil fractions were weighed, gently ground, and analyzed for SOC, total N (Heraeus Vario EL), 13 C : 12 C (Finnigan MAT, DELTA plus ), and 14 C : 12 C ratios (3 MV Tandetron 4130 AMS).…”

Section: Methodsmentioning

confidence: 99%

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Is thermal oxidation at different temperatures suitable to isolate soil organic carbon fractions with different turnover?

Helfrich

Flessa

Dreves

et al. 2010

Z. Pflanzenernähr. Bodenk.

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Findings of previous studies suggest that there are relations between thermal stability of soil organic matter (SOM), organo-mineral associations, and stability of SOM against microbial decay. We aimed to test whether thermal oxidation at various temperatures (200°C, 225°C, 275°C, 300°C, 400°C, or 500°C) is capable of isolating SOM fractions with increasing stability against microbial degradation. The investigation was carried out on soils (Phaeozem and Luvisol) under different land-use regimes (field, grassland, forest). The stability of the obtained soil organic carbon (SOC) fractions was determined using the natural-13 C approach for continuously maize-cropped soils and radiocarbon dating. In the Luvisol, thermal oxidation with increasing temperatures did not yield residual SOC fractions of increasing microbial stability. Even the SOC fraction resistant to thermal oxidation at 300°C contained considerable amounts of young, maize-derived C. In the Phaeozem, the mean 14 C age increased considerably (from 3473 y BP in the mineral-associated SOC fraction to 9116 y BP in the residual SOC fraction after thermal oxidation at 300°C). An increasing proportion of fossil C (calculated based on 14 C data) in residual SOC fractions after thermal oxidation with increasing temperatures indicated that this was mainly due to the relative accumulation of thermally stable fossil C. We conclude that thermal oxidation with increasing temperature was not generally suitable to isolate mineral-associated SOC fractions of increasing microbial stability.

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Section: Resultssupporting

confidence: 91%

Section: Soilmentioning

confidence: 61%

Section: Methodsmentioning

confidence: 88%

Section: Methodsmentioning

confidence: 99%

See 2 more Smart Citations

Is thermal oxidation at different temperatures suitable to isolate soil organic carbon fractions with different turnover?

Helfrich

Flessa

Dreves

et al. 2010

Z. Pflanzenernähr. Bodenk.

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show abstract

“…Another suitable approach for SOM partitioning is based on its thermal stability Siewert 2001Siewert , 2004Lopez-Capel et al 2005a, 2005bPlante et al 2005;Kuzyakov et al 2006). Thermogravimetry analysis coupled with differential scanning calorimetry involves a continuous, gradual temperature increase which decomposes (mainly oxidizes) different organic compounds according to their thermal stability.…”

Section: Introductionmentioning

confidence: 99%

Effects of atmospheric CO2 enrichment on δ 13C, δ 15N values and turnover times of soil organic matter pools isolated by thermal techniques

2007

Self Cite

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CO 2 applied for Free-Air CO 2 Enrichment (FACE) experiments is strongly depleted in 13 C and thus provides an opportunity to study C turnover in soil organic matter (SOM) based on its δ 13 C value. Simultaneous use of 15 N labeled fertilizers allows N turnover to be studied. Various SOM fractionation approaches (fractionation by density, particle size, chemical extractability etc.) have been applied to estimate C and N turnover rates in SOM pools. The thermal stability of SOM coupled with C and N isotopic analyses has never been studied in experiments with FACE. We tested the hypothesis that the mean residence time (MRT) of SOM pools is inversely proportional to its thermal stability. Soil samples from FACE plots under ambient (380 ppm) and elevated CO 2 (540 ppm; for 3 years) treatments were analyzed by thermogravimetry coupled with differential scanning calorimetry (TG-DSC). Based on differential weight losses (TG) and energy release or consumption (DSC), five SOM pools were distinguished. Soil samples were heated up to the respective temperature and the remaining soil was analyzed for δ 13 C and δ 15 N by IRMS. Energy consumption and mass losses in the temperature range 20-200°C were mainly connected with water volatilization. The maximum weight losses occurred from 200-310°C. This pool contained the largest amount of carbon: 61% of the total soil organic carbon in soil under ambient treatment and 63% in soil under elevated CO 2 , respectively. δ 13 C values of SOM pools under elevated CO 2 treatment showed an increase from −34.3‰ of the pool decomposed between 20-200°C to −18.1‰ above 480°C. The incorporation of new C and N into SOM pools was not inversely proportional to its thermal stability. SOM pools that decomposed between 20-200 and 200-310°C contained 2 and 3% of the new C, with a MRT of 149 and 92 years, respectively. The pool decomposed between 310-400°C contained the largest proportion of new C (22%), with a MRT of 12 years. The amount of fertilizer-derived N after 2 years of application in ambient and elevated CO 2 treatments was not significantly different in SOM pools decomposed up Plant Soil (2007) 297: [15][16][17][18][19][20][21][22][23][24][25][26][27][28] to 480°C having MRT of about 60 years. In contrast, the pool decomposed above 480°C contained only 0.5% of new N, with a MRT of more than 400 years in soils under both treatments. Thus, the separation of SOM based on its thermal stability was not sufficient to reveal pools with contrasting turnover rates of C and N.

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Thermal oxidation does not fractionate soil organic carbon with differing biological stabilities

Schiedung¹,

Don²,

Wordell‐Dietrich³

et al. 2016

J. Plant Nutr. Soil Sci.

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Thermal analysis techniques have been used to differentiate soil organic carbon (SOC) pools with differing thermal stability. A correlation between thermal and biological stability has been indicated in some studies, while others reported inconsistent relationships. Despite these controversial findings and no standardized method, several recently published studies used thermal analysis techniques to determine the biological stability and quality of SOC in mineral soils. This study examined whether thermal oxidation at temperature levels between 200°C and 400°C, combined with evolving gas analysis and isotope ratio mass spectrometry, is capable of identifying SOC pools with differing biological stability in mineral soils. Soil samples from three sites being under Miscanthus (C4‐plant) cultivation for more than 17 years following former agricultural cropland (only C3‐plant) cultivation were used. Due to natural shifts in 13C content, young and labile Miscanthus‐derived SOC could be distinguished from stable and old C3‐plant‐derived SOC. The proportion of Miscanthus‐derived SOC increased significantly with increasing temperatures up to 350°C in bulk soil samples, indicating increasing oxidation of labile and young SOC with increasing temperatures. Use of density fractions to validate the thermally oxidized SOC from bulk soil samples revealed that the thermal oxidation patterns did not reflect the biological stability of SOC. The suggested biologically labile particulate organic carbon (light fraction from density fractionation) was clearly enriched in Miscanthus‐derived young SOC. The thermal oxidation patterns, however, revealed preferential oxidation of these biologically labile fractions not at low temperatures, but rather at higher temperatures. The reverse was found for the biologically stable mineral‐associated density fraction (heavy fraction). Based on different soil types, it was concluded that the thermal stability of SOC between 200°C and 400°C is not a suitable indicator of the biological stability of SOC and, thus, thermal oxidation is not capable of fractionating SOC pools with differing biological stability.

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Effect of C3–C4 Vegetation Change on δ13C and δ15N Values of Soil Organic Matter Fractions Separated by Thermal Stability

Cited by 24 publications

References 27 publications

Is thermal oxidation at different temperatures suitable to isolate soil organic carbon fractions with different turnover?

Is thermal oxidation at different temperatures suitable to isolate soil organic carbon fractions with different turnover?

Effects of atmospheric CO2 enrichment on δ 13C, δ 15N values and turnover times of soil organic matter pools isolated by thermal techniques

Thermal oxidation does not fractionate soil organic carbon with differing biological stabilities

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