Temperature sensitivity of decomposition in relation to soil organic matter pools: critique and outlook

Reichstein, Markus; Kätterer, Thomas; Andrén, Olof; Ciais, Philippe; Schulze, Ernst Detlef; Crämer, Wolfgang; Papale, Dario; Валентини, Р.

doi:10.5194/bg-2-317-2005

Cited by 120 publications

(95 citation statements)

References 27 publications

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“…It is worth noting that many models assume decomposition of recent C additions is just as sensitive to temperature as decomposition of older SOM [29][30][31]. However, this is not always accurate [32][33][34][35]. Therefore further emphasising the importance of understanding the influence of new crops and their C additions on SOM decomposition.…”

Section: Introductionmentioning

confidence: 99%

Carbon Inputs from Miscanthus Displace Older Soil Organic Carbon Without Inducing Priming

et al. 2016

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The carbon (C) dynamics of a bioenergy system are key to correctly defining its viability as a sustainable alternative to conventional fossil fuel energy sources. Recent studies have quantified the greenhouse gas mitigation potential of these bioenergy crops, often concluding that C sequestration in soils plays a primary role in offsetting emissions through energy generation. Miscanthus is a particularly promising bioenergy crop and research has shown that soil C stocks can increase by more than 2 t C ha −1 yr −1 . In this study, we use a stable isotope ( 13 C) technique to trace the inputs and outputs from soils below a commercial Miscanthus plantation in Lincolnshire, UK, over the first 7 years of growth after conversion from a conventional arable crop. Results suggest that an unchanging total topsoil (0-30 cm) C stock is caused by Miscanthus additions displacing older soil organic matter. Further, using a comparison between bare soil plots (no new Miscanthus inputs) and undisturbed Miscanthus controls, soil respiration was seen to be unaffected through priming by fresh inputs or rhizosphere. The temperature sensitivity of old soil C was also seen to be very similar with and without the presence of live root biomass. Total soil respiration from control plots was dominated by Miscanthus-derived emissions with autotrophic respiration alone accounting for ∼50 % of CO 2 . Although total soil C stocks did not change significantly over time, the Miscanthus-derived soil C accumulated at a rate of 860 kg C ha −1 yr −1 over the top 30 cm. Ultimately, the results from this study indicate that soil C stocks below Miscanthus plantations do not necessarily increase during the first 7 years.

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Section: Introductionmentioning

confidence: 99%

Carbon Inputs from Miscanthus Displace Older Soil Organic Carbon Without Inducing Priming

et al. 2016

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“…A long-term temperature change would then change the pool ratios and, consequently, the effective temperature sensitivity of the soil. It is still under debate whether these effects are of a measurable and relevant magnitude or not (Fang et al, 2005;Knorr et al, 2005;Reichstein et al, 2005b;Conen et al, 2006;Larinova et al, 2007).…”

Section: Temperature Sensitivity Functionsmentioning

confidence: 99%

Measurement depth effects on the apparent temperature sensitivity of soil respiration in field studies

Graf¹,

Weihermüller²,

Huisman³

et al. 2008

Biogeosciences

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Abstract. CO 2 efflux at the soil surface is the result of respiration in different depths that are subjected to variable temperatures at the same time. Therefore, the temperature measurement depth affects the apparent temperature sensitivity of field-measured soil respiration. We summarize existing literature evidence on the importance of this effect, and describe a simple model to understand and estimate the magnitude of this potential error source for heterotrophic respiration. The model is tested against field measurements. We discuss the influence of climate (annual and daily temperature amplitude), soil properties (vertical distribution of CO 2 sources, thermal and gas diffusivity), and measurement schedule (frequency, study duration, and time averaging). Q 10 as a commonly used parameter describing the temperature sensitivity of soil respiration is taken as an example and computed for different combinations of the above conditions. We define conditions and data acquisition and analysis strategies that lead to lower errors in field-based Q 10 determination. It was found that commonly used temperature measurement depths are likely to result in an underestimation of temperature sensitivity in field experiments. Our results also apply to activation energy as an alternative temperature sensitivity parameter.

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“…In compartment models simulating soil C turnover, this stable SOM fraction is represented by a C pool with a slow turnover (several centuries) or even by an inert C pool (Falloon and Smith, 2000). However, the lack of knowledge on the characteristics of the stable SOM fraction remains critical for its modeling: the vulnerability to increased temperature of the stable C pool is unsettled (Knorr et al, 2005;Reichstein et al, 2005;Fang et al, 2006) and generally the size of the stable C pool is estimated from model outputs or is extrapolated from experiments 2 to 3 orders of magnitude shorter than the typical turnover time of the slowest C pools. A more detailed insight into the properties of this C pool is crucial as it represents a potentially large and long lasting sink for atmospheric CO 2 .…”

Section: Introductionmentioning

confidence: 99%

Quantifying and isolating stable soil organic carbon using long-term bare fallow experiments

et al. 2010

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Abstract. The stability of soil organic matter (SOM) is a major source of uncertainty in predicting atmospheric CO 2 concentration during the 21st century. Isolating the stable soil carbon (C) from other, more labile, C fractions in soil is of prime importance for calibrating soil C simulation models, and gaining insights into the mechanisms that lead to soil C stability. Long-term experiments with continuous bare fallow (vegetation-free) treatments in which the decay of soil C is monitored for decades after all inputs of C have stopped, provide a unique opportunity to assess the quantity of stable soil C. We analyzed data from six bare fallow experiments of long-duration (>30 yrs), covering a range of soil types and climate conditions, and sited at Askov (Denmark), Grignon and Versailles (France), Kursk (Russia), Rothamsted (UK), and Ultuna (Sweden). A conceptual three pool model dividing soil C into a labile pool (turnover time of a several years), an intermediate pool (turnover time of a several decades) and a stable pool (turnover time of a several centuries or more) fits well with the long term C decline observed in the bare fallow soils. The estimate of stable C ranged from 2.7 g C kg −1 at Rothamsted to 6.8 g C kg −1 at Grignon. The uncertainty Correspondence to: P. Barré (barre@geologie.ens.fr) associated with estimates of the stable pool was large due to the short duration of the fallow treatments relative to the turnover time of stable soil C. At Versailles, where there is least uncertainty associated with the determination of a stable pool, the soil contains predominantly stable C after 80 years of continuous bare fallow. Such a site represents a unique research platform for characterization of the nature of stable SOM and its vulnerability to global change.

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Temperature sensitivity of decomposition in relation to soil organic matter pools: critique and outlook

Cited by 120 publications

References 27 publications

Carbon Inputs from Miscanthus Displace Older Soil Organic Carbon Without Inducing Priming

Carbon Inputs from Miscanthus Displace Older Soil Organic Carbon Without Inducing Priming

Measurement depth effects on the apparent temperature sensitivity of soil respiration in field studies

Quantifying and isolating stable soil organic carbon using long-term bare fallow experiments

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