Incorporation of natural hydrocarbons from plant residues into an hydromorphic humic podzol following afforestation and fertilization

Jambu, P.; Amblès, André; Dinel, H.; Secouet, B.

doi:10.1111/j.1365-2389.1991.tb00109.x

Cited by 41 publications

(20 citation statements)

References 17 publications

(15 reference statements)

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“…2a-c) are also similar to each other in general features, and in their intensity distributions. The sharp peak at 30ppm in all three spectra indicates the presence of long-chain aliphatics; these could arise from suberin, as noted previously, or from the accumulation of plant waxes as Jambu et al (1991) observed in a forest soil. The spectrum of the Bm HA differs from the others in having features consistent with the presence of lignin components (Hatcher, 1987;Preston et al, 1990).…”

Section: Carbon-13 Nmr Spectroscopymentioning

confidence: 85%

Characterization of organic matter in a forest soil of coastal British Columbia by NMR and pyrolysis-field ionization mass spectrometry

et al. 1994

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Organic matter in the soil profile under a young Douglas-fir stand in coastal British Columbia was characterized by examining intact samples of fresh litterfall and organic horizons (LF, H), and fractions (floatables, humic acid [HA], fulvic acid [FA], humin [HU]) from the three mineral horizons (Ae, Bin, BC). Some 30-40% of the carbon in the mineral horizons was found in poorly-decomposed plant material floatable in water, a fraction whose characteristics changed little with depth, and which contained over 1% Fe. The proportion of soil C in HA plus FA was approximately 8%, but the ratio of C in FA/HA increased with depth. Solid-state I3C NMR spectra of litterfall, LH and H samples showed effects of decomposition, in particular a decrease in 0-alkyl C from litterfall to LH to H, and degradation of resolution from LF to H. For the mineral soil fractions, both floatables and de-ashed HU ('HU d' prepared by HCI/HF treatment) indicated high levels of the original plant biopolymers, including a large alkyl component. Solution 13C spectra of the HAs from mineral horizons showed little difference with depth, except that peaks due to lignin were more pronounced for the Bm HA. The NMR spectra of FAs were high in 0-alkyl and carboxyl C. Pyrolysis-field ionization mass spectrometry confirmed and extended the results from NMR and chemical analyses, in particular demonstrating the accumulation of suberin in some fractions and the leaching and decomposition of lignin components with increasing depth in the mineral horizons. The general features of the HA, FA and HUa from this forest soil, and the effects of decomposition and pedogenesis were similar to those widely found for agricultural and forest soils. However, the accumulation of suberin, and the leaching and decomposition of lignin are particularly associated with forest soils. The low proportion of soil C in HA and FA, and the high proportion in poorly decomposed, iron-rich plant fragments suggest that decomposition is somewhat limited at this site, which is classified as having low fertility. The high accumulations of alkyl C from suberin may also indicate, or contribute to inhibition of decomposition.70 Preston et al.

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Section: Carbon-13 Nmr Spectroscopymentioning

confidence: 85%

Characterization of organic matter in a forest soil of coastal British Columbia by NMR and pyrolysis-field ionization mass spectrometry

et al. 1994

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“…Jambu et al, 1991;Huang et al, 2000). Likewise, the n-fatty acid distribution maximizing at C 24 reflects the terrestrial plant origin of OM in the two surface soil layers 1 Figure 4.…”

Section: Distribution and Composition Of Bulk Soil Organic Mattermentioning

confidence: 99%

Organic matter composition and stabilization in a polygonal tundra soil of the Lena Delta

et al. 2013

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This study investigated soil organic matter (OM) composition of differently stabilized soil OM fractions in the active layer of a polygonal tundra soil in the Lena Delta, Russia, by applying density and particle size fractionation combined with qualitative OM analysis using solid state ¹³C nuclear magnetic resonance spectroscopy, and lipid analysis combined with ¹⁴C analysis. Bulk soil OM was mainly composed of plant-derived, little-decomposed material with surprisingly high and strongly increasing apparent ¹⁴C ages with active layer depth suggesting slow microbial OM transformation in cold climate. Most soil organic carbon was stored in clay and fine-silt fractions (< 6.3 μm), which were composed of little-decomposed plant material, indicated by the dominance of long n-alkane and n-fatty acid compounds and low alkyl/O-alkyl C ratios. Organo-mineral associations, which are suggested to be a key mechanism of OM stabilization in temperate soils, seem to be less important in the active layer as the mainly plant-derived clay- and fine-silt-sized OM was surprisingly "young", with ¹⁴C contents similar to the bulk soil values. Furthermore, these fractions contained less organic carbon compared to density fractionated OM occluded in soil aggregates – a further important OM stabilization mechanism in temperate soils restricting accessibility of microorganisms. This process seems to be important at greater active layer depth where particulate OM, occluded in soil aggregates, was "older" than free particulate OM

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“…The chain length of n-alkanes is related to their provenance: odd carbon numbered long-chained (>C 25 ) alkanes are attributed to higher plants (Eglinton et al, 1962), while odd carbon numbered short-chained (<C 21 ) alkanes derive from microbial organisms (Dinel et al, 1990). The distribution patterns of lipidic compounds like n-alkanes may therefore indicate the sources of biomass inputs in soils or sediments (Jambu et al, 1991;Amblè s et al, 1994;Marseille et al, 1999;Peters et al, 2005). Lipid analysis has been demonstrated to be a useful tool to detect vegetation or land use changes in soils after several thousands of years, e.g., to identify the use of grass turfs to build the Orkney plaggen soils (Bull et al, 1999a), or to follow the environmental history in lake sediments (Schwark et al, 2002;Fisher et al, 2003) and in a sequence of palaeosoils (Xie et al, 2003).…”

Section: Introductionmentioning

confidence: 99%

Short-chain n-alkanes (C16–20) in ancient soil are useful molecular markers for prehistoric biomass burning

Eckmeier

Wiesenberg

2009

Journal of Archaeological Science

102

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The incorporation of plant biomass into soil usually leads to long-chain n-alkanes with a relative predominance of odd carbon numbered homologues. Contrastingly, an increase in short-chain even carbon numbered n-alkanes was found in charred biomass with progressing temperatures. We applied lipid analysis to buried ancient topsoils that contained charred organic matter and to corresponding control soils, which were characterized by a lighter color and lower contents of charred materials. Commonly, the proportion of lipid extracts was found to be lower in the ancient soil than in the control samples, which indicated an enhanced degradation of organic matter, e.g., by thermal degradation. All samples displayed a particular pattern of short-chain and even carbon numbered n-alkanes (maximum at n-C16 or n-C18). The ratios CPI (carbon preference index) and ACL (average chain length) for the investigated soil samples matched the ratios found for maize and rye straw charred at 400 °C or 500 °C, respectively. These molecular ratios indicate the presence of charred biomass. The predominance of short-chain and even carbon numbered n-alkanes was a result of thermal degradation of biomass. The degradation products were preserved in ancient soils and could be applied as molecular markers in archaeological or palaeoenvironmental research.Author's personal copy b s t r a c tThe incorporation of plant biomass into soil usually leads to long-chain n-alkanes with a relative predominance of odd carbon numbered homologues. Contrastingly, an increase in short-chain even carbon numbered n-alkanes was found in charred biomass with progressing temperatures. We applied lipid analysis to buried ancient topsoils that contained charred organic matter and to corresponding control soils, which were characterized by a lighter color and lower contents of charred materials. Commonly, the proportion of lipid extracts was found to be lower in the ancient soil than in the control samples, which indicated an enhanced degradation of organic matter, e.g., by thermal degradation. All samples displayed a particular pattern of short-chain and even carbon numbered n-alkanes (maximum at n-C 16 or n-C 18 ). The ratios CPI (carbon preference index) and ACL (average chain length) for the investigated soil samples matched the ratios found for maize and rye straw charred at 400 C or 500 C, respectively. These molecular ratios indicate the presence of charred biomass. The predominance of short-chain and even carbon numbered n-alkanes was a result of thermal degradation of biomass. The degradation products were preserved in ancient soils and could be applied as molecular markers in archaeological or palaeoenvironmental research.

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Incorporation of natural hydrocarbons from plant residues into an hydromorphic humic podzol following afforestation and fertilization

Cited by 41 publications

References 17 publications

Characterization of organic matter in a forest soil of coastal British Columbia by NMR and pyrolysis-field ionization mass spectrometry

Characterization of organic matter in a forest soil of coastal British Columbia by NMR and pyrolysis-field ionization mass spectrometry

Organic matter composition and stabilization in a polygonal tundra soil of the Lena Delta

Short-chain n-alkanes (C16–20) in ancient soil are useful molecular markers for prehistoric biomass burning

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