Dynamics of soil carbon following destruction of tropical rainforest and the subsequent establishment of <i><scp>I</scp>mperata</i> grassland in <scp>I</scp>ndonesian <scp>B</scp>orneo using stable carbon isotopes

Yonekura, Yusuke; Ohta, Seiichi; Kiyono, Yoshiyuki; Aksa, Darul; Morisada, Kazuhito; Tanaka, Nagaharu; Tayasu, Ichiro

doi:10.1111/j.1365-2486.2012.02722.x

Cited by 20 publications

(13 citation statements)

References 39 publications

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“…Contrary to common expectations, the forest‐to‐pasture transition may sometimes lead to an increase in soil carbon, especially in the surface layers of soil (Guo & Gifford, ; Don et al ., ; Eclesia et al ., ; Yonekura et al ., ) as suspected from earlier research on South‐American pastures made up of introduced grasses (Fisher et al ., ). Often, the largest increases are in the wetter sites.…”

Section: The Terrestrial Surfacementioning

confidence: 97%

Perturbations in the carbon budget of the tropics

Grace

Mitchard

Gloor

2014

Global Change Biology

164

126

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The carbon budget of the tropics has been perturbed as a result of human influences. Here, we attempt to construct a ‘bottom-up’ analysis of the biological components of the budget as they are affected by human activities. There are major uncertainties in the extent and carbon content of different vegetation types, the rates of land-use change and forest degradation, but recent developments in satellite remote sensing have gone far towards reducing these uncertainties. Stocks of carbon as biomass in tropical forests and woodlands add up to 271 ± 16 Pg with an even greater quantity of carbon as soil organic matter. Carbon loss from deforestation, degradation, harvesting and peat fires is estimated as 2.01 ± 1.1 Pg annum−1; while carbon gain from forest and woodland growth is 1.85 ± 0.09 Pg annum−1. We conclude that tropical lands are on average a small carbon source to the atmosphere, a result that is consistent with the ‘top-down’ result from measurements in the atmosphere. If they were to be conserved, they would be a substantial carbon sink. Release of carbon as carbon dioxide from fossil fuel burning in the tropics is 0.74 Pg annum−1 or 0.57 MgC person−1 annum−1, much lower than the corresponding figures from developed regions of the world.

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Section: The Terrestrial Surfacementioning

confidence: 97%

Perturbations in the carbon budget of the tropics

Grace

Mitchard

Gloor

2014

Global Change Biology

164

126

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“…Land‐use change greatly impacts soil C dynamics by altering C inputs, decomposition, and turnover (Post & Kwon, ; Guo & Gifford, ; Elmore & Asner, ; Zhang et al ., ), and thus potentially affects C sequestration and loss (Lal, ; Lemma et al ., ). As the dominant land‐use change during past century, deforestation for agriculture has greatly altered the soil C dynamic at ecosystem, regional, and global scales (Foley et al ., ; Bala et al ., ; Yonekura et al ., ). A meta‐analysis showed that conversion of native forests to croplands reduced soil C stocks by 42%, while soil C stocks increased by 8% after the conversion from forest to pasture (Guo & Gifford, ).…”

Section: Introductionmentioning

confidence: 99%

“…Whether soil C pool acts either as a source or as a sink for atmospheric CO 2 is largely depended on land-use and climate condition (Houghton et al, 1987;Don et al, 2011;Zatta et al, 2013). A number of studies have reported land use significantly affects soil organic C (SOC) pool and decomposition rate (Post & Kwon, 2000;Wu et al, 2003;Yonekura et al, 2012;Zatta et al, 2013). Yet, our understanding of soil C dynamics is still limited, particularly the vulnerability of SOC to land-use and climate change (IPCC, 2001;Del Galdo et al, 2003).…”

Section: Introductionmentioning

confidence: 99%

“…Worldwide land-use changes involving a conversion of vegetation with different photosynthetic pathways (e.g. C 3 vegetation and C 4 vegetation) offer a unique opportunity to quantify the soil C dynamics across large climatic gradients using the stable isotope techniques (Marin-Spiotta et al, 2009;Dalal et al, 2011;Wolf et al, 2011;Yonekura et al, 2012;Mendez-Millan et al, 2014). Naturally, C 4 (d 13 C ca.…”

Section: Introductionmentioning

confidence: 99%

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Soil carbon dynamics following land‐use change varied with temperature and precipitation gradients: evidence from stable isotopes

Zhang

Dang

Zhang

et al. 2015

Global Change Biology

116

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Knowledge of soil organic matter (SOM) dynamics following deforestation or reforestation is essential for evaluating carbon (C) budgets and cycle at regional or global scales. Worldwide land-use changes involving conversion of vegetation with different photosynthetic pathways (e.g. C and C ) offer a unique opportunity to quantify SOM decomposition rate and its response to climatic conditions using stable isotope techniques. We synthesized the results from 131 sites (including 87 deforestation observations and 44 reforestation observations) which were compiled from 36 published papers in the literatures as well as our observations in China's Qinling Mountains. Based on the C natural abundance analysis, we evaluated the dynamics of new and old C in top soil (0-20 cm) following land-use change and analyzed the relationships between soil organic C (SOC) decomposition rates and climatic factors. We found that SOC decomposition rates increased significantly with mean annual temperature and precipitation in the reforestation sites, and they were not related to any climatic factor in deforestation sites. The mean annual temperature explained 56% of variation in SOC decomposition rates by exponential model (y = 0.0014e ) in the reforestation sites. The proportion of new soil C increased following deforestation and reforestation, whereas the old soil C showed an opposite trend. The proportion of new soil C exceeded the proportion of old soil C after 45.4 years' reforestation and 43.4 years' deforestation, respectively. The rates of new soil C accumulation increased significantly with mean annual precipitation and temperature in the reforestation sites, yet only significantly increased with mean annual precipitation in the deforestation sites. Overall, our study provides evidence that SOC decomposition rates vary with temperature and precipitation, and thereby implies that global warming may accelerate SOM decomposition.

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“…Soil depth increases in δ 13 C higher than this threshold are generally interpreted as a sign of the presence of C 4 carbon in the soil's organic matter (Martinelli et al, 1996;Ehleringer et al, 2000;Schwendenmann and Pendall, 2006;Yonekura et al, 2012). The presence of C 4 , in turn, could be due to some recent land changes that introduced C 4 into one of the cropping systems, or due to a natural shift in vegetation (Martinelli et al, 1996;Ehleringer et al 2000;Schwendenmann and Pendall, 2006;Yonekura et al, 2012). In three of our sites, the increase in δ 13 C was higher than 3-4 ‰, indicating a past presence of C 4 vegetation.…”

Section: Depth Variability Of δ 13 C In Forests and Pastures Of Pairementioning

confidence: 99%

Changes in soil carbon stocks in Brazil due to land use: paired site comparisons and a regional pasture soil survey

et al. 2013

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Abstract. In this paper we calculated soil carbon stocks in Brazil studying 17 paired sites where soil stocks were determined in native vegetation, pastures and crop-livestock systems (CPS), and in other regional samplings encompassing more than 100 pasture soils, from 6.58 to 31.53 • S, involving three major Brazilian biomes: Cerrado, Atlantic Forest, and the Pampa. The average native vegetation soil carbon stocks at 10, 30 and 60 cm soil depth were equal to approximately 29, 64, and 92 Mg ha −1 , respectively. In the paired sites, carbon losses of 7.5 Mg ha −1 and 11.6 Mg ha −1 in CPS systems were observed at 10 cm and 30 cm soil depths, respectively. In pasture soils, carbon losses were similar and equal to 7.5 Mg ha −1 and 11.0 Mg ha −1 at 10 cm and 30 cm soil depths, respectively. Differences at 60 cm soil depth were not significantly different between land uses. The average soil δ 13 C under native vegetation at 10 and 30 cm depth were equal to −25.4 ‰ and −24.0 ‰, increasing to −19.6 ‰ and −17.7 ‰ in CPS, and to −18.9 ‰, and −18.3 ‰ in pasture soils, respectively; indicating an increasing contribution of C 4 carbon in these agrosystems. In the regional survey of pasture soils, the soil carbon stock at 30 cm was equal to approximately 51 Mg ha −1 , with an average δ 13 C value of −19.6 ‰. Key controllers of soil carbon stock in pasture sites were sand content and mean annual temperature. Collectively, both could explain approximately half of the variance of soil carbon stocks. When pasture soil carbon stocks were compared with the average soil carbon stocks of native vegetation estimated for Brazilian biomes and soil types by Bernoux et al. (2002) there was a carbon gain of 6.7 Mg ha −1 , which is equivalent to a carbon gain of 15 % compared to the carbon soil stock of the native vegetation. The findings of this study are consistent with differences found between regional comparisons like our pasture sites and plot-level paired study sites in estimating soil carbon stocks changes due to land use changes.

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Dynamics of soil carbon following destruction of tropical rainforest and the subsequent establishment of Imperata grassland in Indonesian Borneo using stable carbon isotopes

Cited by 20 publications

References 39 publications

Perturbations in the carbon budget of the tropics

Perturbations in the carbon budget of the tropics

Soil carbon dynamics following land‐use change varied with temperature and precipitation gradients: evidence from stable isotopes

Changes in soil carbon stocks in Brazil due to land use: paired site comparisons and a regional pasture soil survey

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