Estimating primary and secondary subsidence in an organic soil 15, 20, and 30 years after drainage

Ewing, Justin M.; Vepraskas, M. J.

doi:10.1672/0277-5212(2006)26[119:epassi]2.0.co;2

Cited by 57 publications

(44 citation statements)

References 6 publications

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“…They also indicate that soils of our study sites were characteristic of European fens and resembled typical properties of managed organic soils (Berglund, 1995;Kechavarzi et al, 2010;Eickenscheidt et al, 2015;Krueger et al, 2015;Wüst-Galley et al, 2016;Brouns et al, 2016). Several studies assume that deeper layer peat of managed organic soils is less decomposed (Ewing and Vepraskas, 2006;Rogiers et al, 2008;Leifeld et al, 2011a, b;Krueger et al, 2015;Wüst-Galley et al, 2016). We therefore interpret the different SOM characteristics found in the topsoils of our samples as indicators of advanced decomposition triggered by drainage.…”

Section: Som Characteristicssupporting

confidence: 70%

Peat decomposability in managed organic soils in relation to land use, organic matter composition and temperature

et al. 2018

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Abstract. Organic soils comprise a large yet fragile carbon (C) store in the global C cycle. Drainage, necessary for agriculture and forestry, triggers rapid decomposition of soil organic matter (SOM), typically increasing in the order forest < grassland < cropland. However, there is also large variation in decomposition due to differences in hydrological conditions, climate and specific management. Here we studied the role of SOM composition on peat decomposability in a variety of differently managed drained organic soils. We collected a total of 560 samples from 21 organic cropland, grassland and forest soils in Switzerland, monitored their CO 2 emission rates in lab incubation experiments over 6 months at two temperatures (10 and 20 • C) and related them to various soil characteristics, including bulk density, pH, soil organic carbon (SOC) content and elemental ratios (C / N, H / C and O / C). CO 2 release ranged from 6 to 195 mg CO 2 -C g −1 SOC at 10 • C and from 12 to 423 mg g −1 at 20 • C. This variation occurring under controlled conditions suggests that besides soil water regime, weather and management, SOM composition may be an underestimated factor that determines CO 2 fluxes measured in field experiments. However, correlations between the investigated chemical SOM characteristics and CO 2 emissions were weak. The latter also did not show a dependence on land-use type, although peat under forest was decomposed the least. High CO 2 emissions in some topsoils were probably related to the accrual of labile crop residues. A comparison with published CO 2 rates from incubated mineral soils indicated no difference in SOM decomposability between these soil classes, suggesting that accumulation of recent, labile plant materials that presumably account for most of the evolved CO 2 is not systematically different between mineral and organic soils. In our data set, temperature sensitivity of decomposition (Q 10 on average 2.57 ± 0.05) was the same for all land uses but lowest below 60 cm in croplands and grasslands. This, in turn, indicates a relative accumulation of recalcitrant peat in topsoils.

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Section: Som Characteristicssupporting

confidence: 70%

Peat decomposability in managed organic soils in relation to land use, organic matter composition and temperature

et al. 2018

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“…The high variability of this property directly affects OCst estimates and may be related to differences in the source of organic matter and/or soil coverage conditions and management practices. Agricultural usage is reported as a common reason for an increase in Bd in Organosols (Ewing and Vepraskas, 2006;Kechavarzi et al, 2010;Leifeld et al, 2011), and the values of Bd in the literature for Organosols are similar to the ones observed in this study. In Danish riparian wetlands, Bd values ranged from 0.30 to 0.50 Mg m -3 (Audet et al, 2013).…”

Section: Resultssupporting

confidence: 90%

“…In contrast, changes in SOM contents and in the proportions of soil humic fractions caused by deforestation and deficient or non-existent soil management can decrease soil quality (Valladares et al, 2007). In Organosols, SOM is ordinarily reduced by human activity and agricultural intensity, mainly related to decreasing addition of plant residue, artificial drainage for agriculture, and promotion of microbial activity by increasing soil aeration by drainage (Pereira et al, 2005;Ewing and Vepraskas, 2006;Valladares et al, 2008a,b;Kechavarzi et al, 2010;Cayci et al, 2011;Leifeld et al, 2011).…”

Section: Introductionmentioning

confidence: 99%

Carbon and Nitrogen Stocks and Humic Fractions in Brazilian Organosols

Valladares

Pereira

Benites

et al. 2016

Rev. Bras. Ciênc. Solo

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ABSTRACT:Despite limited geographic expression of Organosols in Brazil, their high carbon storage capacity and natural environmental vulnerability justifies further studies on C and N stocks in these soils and their relationship to the nature of organic matter. Evaluation of physical and chemical properties of organic soils and their ability to store C is important so as to develop sustainable management practices for their preservation. The objectives of the study were to measure the total organic carbon stock (OCst), total nitrogen stock (Nst), and humic fractions in Organosols from different environments and regions of Brazil, and to correlate the data with soil chemical (pH, P, K, Ca 2+ , Mg 2+ , Al 3+ , H+Al, CEC, V) and physical properties (soil bulk density, Bd; organic matter density, OMd; total pore space, TPS; minimum residue, MinR; and proportion of mineral matter, MM), and degree of organic matter decomposition (rubbed fiber content; pyrophosphate index, PyI; and von Post index). For that purpose, 18 Organosol profiles, in a total of 49 horizons, were sampled under different land usage and plant coverage conditions. The profiles were located in the following Brazilian states -Alagoas, Bahia, Distrito Federal, Espírito Santo, Mato Grosso do Sul, Minas Gerais, Paraná, Rio de Janeiro, Rio Grande do Sul, Santa Catarina, and São Paulo. The OCst and Nst varied significantly among horizons and profiles. The Organosols exhibited, on average, 203.59 Mg ha -1 OCst and 8.30 Mg ha -1 Nst, and the highest values were found in profiles with pasture usage. The content of the humic fraction (humin, HUM; fulvic acid, FAF; and humic acid, HAF) and C storage varied in the soil horizons and profiles according to the degree of decomposition and other factors of soil formation. The OCst, Nst, OMd and the C stocks in the humic fractions were positively correlated. The values of acidity were lower in the soils with higher contents of mineral material, and low pH values were related to a high C/N ratio. The OCst and Nst were correlated with different soil properties, the most important being the degree of soil organic matter decomposition, which was inversely correlated.

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“…Stephens and Speir, 1969;Schothorst, 1972;Ewing and Vepraskas, 2006;Leifeld et al, 2011). We used a variation modified from Driessen and Soepraptohardjo (1974), as follows:…”

Section: Determining the Compaction Component Of Subsidencementioning

confidence: 99%

Subsidence and carbon loss in drained tropical peatlands

et al. 2012

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Abstract. Conversion of tropical peatlands to agriculture leads to a release of carbon from previously stable, longterm storage, resulting in land subsidence that can be a surrogate measure of CO 2 emissions to the atmosphere. We present an analysis of recent large-scale subsidence monitoring studies in Acacia and oil palm plantations on peatland in SE Asia, and compare the findings with previous studies. Subsidence in the first 5 yr after drainage was found to be 142 cm, of which 75 cm occurred in the first year. After 5 yr, the subsidence rate in both plantation types, at average water table depths of 0.7 m, remained constant at around 5 cm yr −1 . The results confirm that primary consolidation contributed substantially to total subsidence only in the first year after drainage, that secondary consolidation was negligible, and that the amount of compaction was also much reduced within 5 yr. Over 5 yr after drainage, 75 % of cumulative subsidence was caused by peat oxidation, and after 18 yr this was 92 %. The average rate of carbon loss over the first 5 yr was 178 t CO 2eq ha −1 yr −1 , which reduced to 73 t CO 2eq ha −1 yr −1 over subsequent years, potentially resulting in an average loss of 100 t CO 2eq ha −1 yr −1 over 25 yr. Part of the observed range in subsidence and carbon loss values is explained by differences in water table depth, but vegetation cover and other factors such as addition of fertilizers also influence peat oxidation. A relationship with groundwater table depth shows that subsidence and carbon loss are still considerable even at the highest water levels theoretically possible in plantations. This implies that improved plantation water management will reduce these impacts by 20 % at most, relative to current conditions, and that high rates of carbon loss and land subsidence are inevitable consequences of conversion of forested tropical peatlands to other land uses.

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Estimating primary and secondary subsidence in an organic soil 15, 20, and 30 years after drainage

Cited by 57 publications

References 6 publications

Peat decomposability in managed organic soils in relation to land use, organic matter composition and temperature

Peat decomposability in managed organic soils in relation to land use, organic matter composition and temperature

Carbon and Nitrogen Stocks and Humic Fractions in Brazilian Organosols

Subsidence and carbon loss in drained tropical peatlands

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