Organic matter in density fractions of water-stable aggregates in silty soils: Effect of land use

Yamashita, Tamon; Flessa, Heiner; John, B.; Helfrich, Mirjam; Ludwig, Bernard

doi:10.1016/j.soilbio.2006.04.013

Cited by 183 publications

(114 citation statements)

References 29 publications

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“…1), which is again in line with previous findings for other soils (von Lützow et al, 2007). Yet the apparent C-turnover time of oPOM increased with decreasing aggregate size from 20 to 30 y in aggregates >1000 lm to 166 y in aggregates <53 lm (Yamashita et al, 2006). These findings support the hypothesis that macro-aggregates (>250 lm), micro-aggregates (53 to 250 lm), and the smallest microaggregate stuctures (<53 lm) have different roles in the protection of SOM (Besnard et al, 1996;Jastrow et al, 1996).…”

Section: Organic Matter In Density Fractionssupporting

confidence: 78%

“…Soil density fractionation was used to determine the quantity, composition, and stability of free particulate OM (fPOM, density < 1.6 g cm -3 ), particulate OM occluded in aggregates (oPOM with the density < 1.6 g cm -3 [oPOM <1.6 ] and 1.6 to 2.0 g cm -3 [oPOM 1.6-2.0 ]), and mineral-bound OM (density > 2 g cm -3 ) (John, 2003;John et al, 2005;Yamashita et al, 2006). The particulate OM (fPOM + oPOM) contributed 13% (Luvisol) and 31% (Phaeozem) to the total soil OC stored in the Ap horizons (Fig.…”

Section: Organic Matter In Density Fractionsmentioning

confidence: 99%

“…Several physical procedures have been proposed to isolate physically stabilized SOM fractions with different composition and stability and to characterize and quantify mechanisms of SOM stabilization in soils. These methods include aggregate-size fractionations (e.g., Oades and Waters, 1991;Jastrow et al, 1996;Puget et al, 2000), particle-size fractionations (e.g., Tiessen et al, 1981;Christensen, 2001;Jolivet et al, 2003), density fractionations (e.g., Balesdent et al, 1998;Baisden et al, 2002;Yamashita et al, 2006), and their combinations (e.g., Cambardella and Elliott, 1993;Rodionov et al, 2000;Six et al, 2002;John et al, 2005). To account for chemical stabilization processes, different extraction procedures (Balesdent, 1996;Ludwig et al, 2003), wet oxidation (Eusterhus et al, 2005;Mikutta et al, 2005), acid hydrolyses (Paul et al, 2001;Poirier et al, 2003;Plante et al, 2006), and various combinations of these procedures (Helfrich et al, 2007) have been used, frequently on physically isolated soil fractions (cf., e.g., von Lützow et al, 2007 for a recent review).…”

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: Organic Matter In Density Fractionssupporting

confidence: 78%

Section: Organic Matter In Density Fractionsmentioning

confidence: 99%

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.

Self Cite

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“…These results contradict to those reported by Farsang et al (2012) according to which recent deposition was trapped, while our results refer to deposits buried a long time ago. SOC enrichment and SOM compound variations in soil loss strongly depend on initial soil moisture content, precipitation parameters, aggregates and crusting (Kuhn et al, 2012;Yamashita et al, 2006), consequently results gained from different scales can be compared only with difficulties (Chaplot and Poesen, 2012). When comparing average values of silt content by group the same phenomenon is observed as in the case of SOC and absorbance at 280 nm.…”

Section: Data Evaluation Techniques Appliedmentioning

confidence: 95%

Redistribution of Soil Organic Carbon Triggered by Erosion at Field Scale Under Subhumid Climate, Hungary

et al. 2016

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Soil organic carbon (SOC) has primary importance in terms of soil physics, fertility and even of climate change control. An intensively cultivated Cambisol was studied in order to quantify SOC redistribution under subhumid climate. One hundred soil samples were taken from the representative points of the solum along the slopes from the depth of 20-300 cm with a mean 1.2 % SOC content. They were measured by the simultaneous application of diffuse reflectance (240-1900 nm) and traditional physico-chemical methods in order to compare the results. On the basis of the results hierarchical cluster analyses were performed. The spatial pattern of the groups created were similar, and even though the classifications were not the same, diffuse reflectance has proven to be a suitable method for soil/sediment classification even within a given arable field. Both organic and inorganic carbon distribution was found a proper tool for estimations of past soil erosion process. Results show SOC enrichment on two sedimentary spots with different geomorphological positions. Soil organic matter compound also differs between the two spots due to selective deposition of the delivered organic matter. The components of low molecular weight reach the bottom of the slope and there can leach into the profile, while the more polymerised organic matter compounds are delivered and deposited even before, on a higher segment of the slope in an aggregated form. This spatial difference appears below the uppermost tilled soil layer as well; referring the lower efficiency of conventional ploughing tillage in spatial soil homogenisation.

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“…Studies show that the aggregates contain labile carbon that is physically protected by action of the microorganisms and that large aggregates protect large amounts of carbon (Amelung and Zech, 1999). Differences in composition and in stability of carbon in the intra-aggregated fractions are believed to be results of recalcitrance and of soil-aggregate protection mechanisms (John et al, 2005;Yamashita et al, 2006).…”

Section: Soil Physical Characteristics and Soc In Each Soil Layersmentioning

confidence: 99%

Soil Carbon Stocks under Amazonian Forest: Distribution in the Soil Fractions and Vulnerability to Emission

Marques¹,

Luizão²,

Teixeira³

et al. 2017

OJF

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Organic matter in density fractions of water-stable aggregates in silty soils: Effect of land use

Cited by 183 publications

References 29 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

Redistribution of Soil Organic Carbon Triggered by Erosion at Field Scale Under Subhumid Climate, Hungary

Soil Carbon Stocks under Amazonian Forest: Distribution in the Soil Fractions and Vulnerability to Emission

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