Priming of soil organic matter: Chemical structure of added compounds is more important than the energy content

Lonardo, D.P. Di; Boer, Wietse de; Gunnewiek, Paulien J. A. Klein; Hannula, S. Emilia; Wal, Annemieke van der

doi:10.1016/j.soilbio.2017.01.017

Cited by 96 publications

(82 citation statements)

References 83 publications

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“…Root litter is an important belowground input, but several other classes of root-derived C also make large contributions to SOM (Crow et al, 2009;Kong and Six, 2010;Clemmensen et al, 2013;. These inputs include several classes of root exudates, including those that contribute to priming (Kuzyakov et al, 2000;Kuzyakov, 2010;Di Lonardo et al, 2017), desorption (Keiluweit et al, 2015), defense (Jung et al, 2012), and symbiont signaling/support (Badri and Vivanco, 2009;Jung et al, 2012).…”

Section: Rootsmentioning

confidence: 99%

“…Root exudation is an important component of belowground C inputs because it can promote the decomposition of SOM compounds that require more energy to degrade or don't have a stoichiometric ratio that matches microbial demand Drake et al, 2013;Di Lonardo et al, 2017). Such root exudates may promote microbial N mining in some circumstances by providing the energy required to decompose N rich SOM (Dijkstra et al, 2013).…”

Section: Rootsmentioning

confidence: 99%

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Constraining Carbon and Nutrient Flows in Soil With Ecological Stoichiometry

et al. 2019

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Soil organic matter (SOM) is central to soil carbon (C) storage and terrestrial nutrient cycling. New data have upended the traditional model of stabilization, which held that stable SOM was mostly made of undecomposed plant molecules. We now know that microbial by-products and dead cells comprise unexpectedly large amounts of stable SOM because they can become attached to mineral surfaces or physically protected within soil aggregates. SOM models have been built to incorporate the microbial to mineral stabilization of organic matter, but now face a new challenge of accurately capturing microbial productivity and metabolism. Explicitly representing stoichiometry, the relative nutrient requirements for growth and maintenance of organisms, could provide a way forward. Stoichiometry limits SOM formation and turnover in nature, but important nutrients like nitrogen (N), phosphorus (P), and sulfur (S) are often missing from the new generation of SOM models. In this synthesis, we seek to facilitate the addition of these nutrients to SOM models by (1) reviewing the stoichiometric biasthe tendency to favor one element over another-of four key processes in the new framework of SOM cycling and (2) applying this knowledge to build a stoichiometrically explicit budget of C, N, P, and S flow through the major SOM pools. By quantifying the role of stoichiometry in SOM cycling, we discover that constraining the C:N:P:S ratio of microorganisms and SOM to specific values reduces uncertainty in C and nutrient flow as effectively as using microbial C use efficiency (CUE) parameters. We find that the value of additional constraints on stoichiometry vs. CUE varies across ecosystems, depending on how precise the available data are for that ecosystem and which biogeochemical pathways are present. Moreover, because CUE summarizes many different processes, stoichiometric measurements of key soil pools are likely to be more robust when extrapolated from soil incubations to plot or biome scale estimates. Our results suggest that measuring SOM stoichiometry should be a priority for future empirical work and that the inclusion of new nutrients in SOM models may be an effective way to improve precision.

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Section: Rootsmentioning

confidence: 99%

Section: Rootsmentioning

confidence: 99%

Constraining Carbon and Nutrient Flows in Soil With Ecological Stoichiometry

et al. 2019

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“…1). The whole region is underlain by continuous permafrost reaching depths of 450-700 m onshore and 200-600 m offshore (Romanovskii et al, 2004), with ground temperatures of −11 • C for terrestrial permafrost (Drozdov et al, 2005) and −1 • C for submarine permafrost (Overduin et al, 2015). Long, cold winters and short, cool summers characterize the current climate.…”

Section: Study Region and Sample Materialsmentioning

confidence: 99%

Greenhouse gas production in degrading ice-rich permafrost deposits in northeastern Siberia

et al. 2018

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Abstract. Permafrost deposits have been a sink for atmospheric carbon for millennia. Thaw-erosional processes, however, can lead to rapid degradation of ice-rich permafrost and the release of substantial amounts of organic carbon (OC). The amount of the OC stored in these deposits and their potential to be microbially decomposed to the greenhouse gases carbon dioxide (CO2) and methane (CH4) depends on climatic and environmental conditions during deposition and the decomposition history before incorporation into the permafrost. Here, we examine potential greenhouse gas production as a result of degrading ice-rich permafrost deposits from three locations in the northeastern Siberian Laptev Sea region. The deposits span a period of about 55 kyr from the last glacial period and Holocene interglacial. Samples from all three locations were incubated under aerobic and anaerobic conditions for 134 days at 4 ∘C. Greenhouse gas production was generally higher in deposits from glacial periods, where 0.2 %–6.1 % of the initially available OC was decomposed to CO2. In contrast, only 0.1 %–4.0 % of initial OC was decomposed in permafrost deposits from the Holocene and the late glacial transition. Within the deposits from the Kargin interstadial period (Marine Isotope Stage 3), local depositional environments, especially soil moisture, also affected the preservation of OC. Sediments deposited under wet conditions contained more labile OC and thus produced more greenhouse gases than sediments deposited under drier conditions. To assess the greenhouse gas production potentials over longer periods, deposits from two locations were incubated for a total of 785 days. However, more than 50 % of total CO2 production over 785 days occurred within the first 134 days under aerobic conditions, while 80 % were produced over the same period under anaerobic conditions, which emphasizes the nonlinearity of the OC decomposition processes. Methanogenesis was generally observed in active layer samples but only sporadically in permafrost samples and was several orders of magnitude smaller than CO2 production.

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“…In temperate forests, about 50% of carbon emissions result from the decomposition of different kinds of soil organic matter by the soil microbial community [10,11]. The easy accessibility of soil organic carbon by soil microorganisms has been proposed to trigger the fast carbon cycling process [12,13]. Normally, the soil organic carbon pool is partitioned into recalcitrant organic carbon and labile organic carbon [14].…”

Section: Introductionmentioning

confidence: 99%

Inorganic Nitrogen Addition Affects Soil Respiration and Belowground Organic Carbon Fraction for a Pinus tabuliformis Forest

Zhang

Liu

Zhou

et al. 2019

Forests

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The capability of forest ecosystems to sequester carbon from the atmosphere largely depends on the interaction of soil organic matter and nitrogen, and thus, this process will be greatly influenced by nitrogen deposition under the future scenario of global change. To clarify this interaction, the current study explored the variations in soil carbon fraction and soil respiration with different levels of nitrogen deposition. NH4NO3 was added at concentrations of 0, 50, 100, 200, and 400 kg N ha−1 year−1 separately on twenty 100 m2 plots in a Pinus tabuliformis Carr forest in northern China. Soil samples were analyzed for their nutrient content and biophysical properties two years after nitrogen application, and the soil respiration rate was measured every month during the study period. Seasonal variation and nitrogen addition significantly affected soil respiration rate. On average, nitrogen addition significantly reduced the annual soil respiration rate by 23.74%. Fine root biomass significantly decreased by an average of 43.55% in nitrogen treatment plots compared to the control plot. However, the average proportions of autumn and winter soil respiration rates out of the annual cumulative soil respiration rate greatly increased from 23.57% and 11.04% to 25.90% and 12.18%, respectively. The soil microbial biomass carbon content in the control plot was 342.39 mg kg−1, 23.50% higher than the average value in nitrogen treatment plots. The soil dissolved organic carbon was reduced by 22.60%, on average, following nitrogen addition. Significant correlations were detected between fine root biomass and the annual cumulative soil respiration rate, soil microbial biomass carbon content, and soil dissolved organic carbon content. This demonstrates that nitrogen addition affects soil organic carbon transformation and carbon emission, mainly by depressing fine root production.

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Priming of soil organic matter: Chemical structure of added compounds is more important than the energy content

Cited by 96 publications

References 83 publications

Constraining Carbon and Nutrient Flows in Soil With Ecological Stoichiometry

Constraining Carbon and Nutrient Flows in Soil With Ecological Stoichiometry

Greenhouse gas production in degrading ice-rich permafrost deposits in northeastern Siberia

Inorganic Nitrogen Addition Affects Soil Respiration and Belowground Organic Carbon Fraction for a Pinus tabuliformis Forest

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