ライフサイエンスコーパス: soil carbon

1 uts under elevated CO2 fueling a loss of old soil carbon.

2 Earth's land surface, but store one-third of soil carbon.

3 cally alter the stability of major stores of soil carbon.

4 and whether plant species loss will decrease soil carbon.

5 il and less by the decomposition of existing soil carbon.

6 on responses mediate the observed changes in soil carbon.

7 Permafrost contains about 50% of the global soil carbon.

8 groups represented the major fraction of the soil carbon.

9 anic farming has the potential to accumulate soil carbon.

10 concentrations, and not with wetland type or soil carbon.

11 hich contain up to two-thirds of the world's soil carbon.

12 rrelated with soil factors, especially total soil carbon.

13 gen slows litter decomposition, may increase soil carbon.

14 urrent-generation datasets on vegetation and soil carbon.

15 gions that store the majority of the world's soil carbon.

16 diversity and globally significant stores of soil carbon.

17 ion; however, the magnitude and direction of soil carbon accumulation following afforestation and its

18 We find that the direct impact of warming on soil carbon accumulation rates is more subtle than the i

19 asing costs of N acquisition with increasing soil carbon, adequately reproduced global GPP distributi

20 n of soil texture, aggregates stability, and soil carbon affected by land uses.

21 We found a significant loss of soil carbon and a major reduction in taxonomic and funct

22 grees C limit should be developed to include soil carbon and agriculture-related mitigation options.

23 This information has been incorporated into soil carbon and Earth-system models, which suggest that

24 , little is known about the quantity of deep soil carbon and its sensitivity to management.

25 irical data are available on the response of soil carbon and microbial physiology to warming in tropi

26 NA gene copies significantly correlated with soil carbon and nitrogen contents, suggesting the contro

27 de hardwood forest, we documented changes in soil carbon and nitrogen cycling in order to investigate

28 We also observe comparable soil carbon and nitrogen losses in an independent field

29 il gas exchange with longer-term dynamics of soil carbon and nitrogen stocks.

30 urned plots experienced a decline in surface soil carbon and nitrogen that was non-saturating through

31 adgil effect' and its consequences on forest soil carbon and nutrient cycling.

32 Root litter is the dominant soil carbon and nutrient input in many ecosystems, yet f

33 ecies affect North American temperate forest soil carbon and nutrient processes.

34 understand the long-term effects of fire on soil carbon and nutrient storage, or whether fire-driven

35 he observed shifts in ambient vegetation and soil carbon and that the vegetation responses mediate th

36 early four times that of permafrost per gram soil carbon, and CH4 production per gram soil carbon was

37 Habitat type, soil carbon, and soil N largely explained the total N pa

38 gion containing globally important stores of soil carbon, and where the most rapid climate change is

39 dual lignin contributing up to 30% of forest soil carbon--and is derived from an ancestral white rot

40 formation rates of total and acid-insoluble soil carbon are reduced by 50 per cent relative to the a

41 y drivers for denitrification, in particular soil carbon, are slow to develop in restored wetlands.

42 ion for nitrogen as an independent driver of soil carbon balance and demonstrate the need to understa

43 how that ESMs underestimated the mean age of soil carbon by a factor of more than six (430 +/- 50 yea

44 verity fires can increase the pool of stable soil carbon by thermally altering the chemistry of soil

45 The soil carbon (C) : N ratio was found to explain most of t

46 chment experiments in forests is the lack of soil carbon (C) accumulation owing to microbial priming

47 ut the long-term impacts of this practice on soil carbon (C) and greenhouse gas (GHG) dynamics are po

48 anagement did not have consistent effects on soil carbon (C) and N mineralization under elevated temp

49 along with changes in plant communities and soil carbon (C) and nitrogen (N) dynamics.

50 l enzymes, tannins play an important role in soil carbon (C) and nitrogen (N) mineralization.

51 le is known about how this conversion alters soil carbon (C) and nitrogen (N).

52 t a significant and highly labile portion of soil carbon (C) and nitrogen (N).

53 ts of multiple drivers on the persistence of soil carbon (C) are poorly understood.

54 ry manure and inorganic fertilizers (INF) on soil carbon (C) as well as nitrogen (N) fractions, enzym

55 st soils, but the effects of such changes on soil carbon (C) cycling and storage remain largely unkno

56 nderstanding the processes that control deep soil carbon (C) dynamics and accumulation is of key impo

57 l, but the consequences of these changes for soil carbon (C) dynamics are poorly understood.

58 ing recognized that roots play a key role in soil carbon (C) dynamics, the magnitude and direction of

59 n and climate change may substantially alter soil carbon (C) dynamics, which in turn may impact futur

60 Climate warming affects soil carbon (C) dynamics, with possible serious conseque

61 Almost half of the global terrestrial soil carbon (C) is stored in the northern circumpolar pe

62 Changes in soil carbon (C) levels as a result of potting substrate

63 anthropogenic influences on the dynamics of soil carbon (C) loss.

64 ndent function in current microbial-explicit soil carbon (C) models.

65 The global soil carbon (C) pool is massive, so relatively small cha

66 phosphorus (P) availability often constrains soil carbon (C) pool, and elevated N deposition could fu

67 ds store a significant portion of the global soil carbon (C) pool.

68 ssible consequences for the turnover rate of soil carbon (C) pools and feedbacks to the atmosphere.

69 Soil carbon (C) pools and plant community composition ar

70 Determining soil carbon (C) responses to rising temperature is criti

71 Soil carbon (C) sequestration, as an ecosystem property,

72 Soil carbon (C) stabilisation is known to depend in part

73 World soil carbon (C) stocks are third only to those in the oc

74 Typical soil carbon (C) stocks used in global carbon models only

75 Accurately quantifying changes in soil carbon (C) stocks with land-use change is important

76 s to climate change through their effects on soil carbon (C) storage, nutrient cycling, and plant hea

77 pes, with unknown effects on properties like soil carbon (C) storage.

78 requires land use activities that accumulate soil carbon (C) while contributing to food production.

79 Peatlands contain one-third of soil carbon (C), mostly buried in deep, saturated anoxic

80 main modules: soil water, soil temperature, soil carbon (C), soil N, and crop growth.

81 de ecosystems store approximately 1700 Pg of soil carbon (C), which is twice as much C as is currentl

82 itical control on the cycling and storage of soil carbon (C).

83 system because they contain vast amounts of soil carbon (C).

84 Peatlands contain one-third of the world's soil carbon (C).

85 Coastal wetlands are large reservoirs of soil carbon (C).

86 fine root decay and increased the storage of soil carbon (C; +18%) across a widespread northern hardw

87 arming may stimulate microbial metabolism of soil carbon, causing a carbon-cycle-climate feedback whe

88 marginal per multiple definitions, we model soil carbon changes upon transitions from marginal cropl

89 Soil carbon changes, direct and indirect land use change

90 e change thus constitutes a yet unrecognized soil carbon-climate feedback that should be incorporated

91 e of soil organic matter for aquatic health, soil carbon-climate interactions and land management.

92 These results may help build confidence in soil-carbon-climate feedback projections by improving un

93 al turnover times) while further stabilizing soil carbon compounds in heavier, mineral-associated fra

94 f variation in temperature, soil texture, or soil carbon concentration.

95 This disparity increases with depth, with soil carbon concentrations reduced by a factor of 4.9 to

96 ent) have on average 1.7 to 3.7 times higher soil carbon concentrations within 20 centimetres of the

97 cation is a widely used practice to increase soil carbon content and maintain soil fertility.

98 relative rate of carbon loss increased with soil carbon content and was more than 2% yr(-1) in soils

99 vegetation or the atmosphere, and changes in soil carbon content can have a large effect on the globa

100 Hence the effect of mycorrhizal type on soil carbon content holds at the global scale.

101 ate of 0.6% yr(-1) (relative to the existing soil carbon content).

102 es C over 50 years, although some, including soil carbon content, remained stable after 5-8 years.

103 d rapid mycorrhizal pathway of carbon in the soil carbon cycle.

104 Soil carbon cycling processes potentially play a large r

105 de hardwood forest, we documented changes in soil carbon cycling to investigate the potential consequ

106 Empirical evidence for the response of soil carbon cycling to the combined effects of warming,

107 study the effect of changes in snow cover on soil carbon cycling within the context of natural climat

108 ased renewable energy sources to alter plant-soil carbon cycling, hypothesize likely effects and iden

109 icrobial activity, and the related impact on soil carbon cycling, is thus greater in regions with low

110 hat may represent an overlooked component of soil carbon cycling.

111 a and biomass (where and when available) and soil carbon data to retrieve the first global estimates,

112 'E (43.6 years) and small xi (0.14 on litter/soil carbon decay rates).

113 orization of carbonate rocks, wildfires, and soil carbon decay; and (iv) ocean overturn bringing high

114 re change of +/- 15 degrees C, we found that soil carbon declined over 5 years by 4% in response to e

115 The temperature sensitivity of soil carbon decomposition is commonly determined by meas

116 ges in primary productivity, suggesting that soil carbon decomposition may have been restricted.

117 et emerged on the temperature sensitivity of soil carbon decomposition.

118 undances of fungi and higher activities of a soil carbon-degrading enzyme, which led to more rapid ra

119 Future changes in soil carbon depend on changes in litter and root inputs

120 in tropical regions are likely to accelerate soil carbon destabilization, further increasing atmosphe

121 Soil carbon dioxide (CO(2)) efflux is a major component

122 nthesis, ecosystem-level carbon exchange and soil carbon dioxide efflux with local meteorology data.

123 e first to use decadal-scale observations of soil carbon dynamics and results of multifactor manipula

124 nce of tundra heterogeneity for representing soil carbon dynamics at fine to coarse spatial scales.

125 n experimental grasslands that can influence soil carbon dynamics irrespective of GEC.

126 ble uncertainty in the potential response of soil carbon dynamics to the rapid global increase in rea

127 y critically influence root productivity and soil carbon dynamics under future climate change scenari

128 s needed on carbon stock changes in forests, soil carbon dynamics, and bioenergy crop production on d

129 ems can provide more accurate assessments of soil carbon dynamics.

130 ver, within certain biomes soil moisture and soil carbon emerge as dominant predictors of Rs.

131 es, declining 27 and 15%, respectively, once soil carbon equilibrates within several decades of estab

132 they do not include multidecadal changes in soil carbon, especially in drier savanna grasslands.

133 nties in global carbon (C) budgets stem from soil carbon estimates and associated challenges in distr

134 soil temperature, primary productivity, and soil carbon estimates with observations of annual Rs fro

135 educe losses of organic matter and sequester soil carbon for climate change mitigation, but a renewal

136 se woody debris, belowground live carbon and soil carbon) for data-deficient regions, using a combina

137 r, the influence of elevated ozone levels on soil carbon formation and decomposition are unknown.

138 due to elevated ozone levels will also lower soil carbon formation rates significantly.

139 riation in key biogeochemical processes like soil carbon formation.

140 nificantly accelerate decomposition of light soil carbon fractions (with decadal turnover times) whil

141 g 14C, 13C and compound-specific analyses of soil carbon from long-term nitrogen fertilization plots,

142 efold higher maximum CH4 production per gram soil carbon from organic soils than mineral soils.

143 g Earth's orbital properties with release of soil carbon from permafrost provides a unifying model ac

144 Although nutrient enrichment caused soil carbon gains most dry, sandy regions, considerable

145 The influence of climate on decomposition of soil carbon has been well documented, but there remains

146 ents in our understanding of the dynamics of soil carbon have shown that 20-40% of the approximately

147 , we observed no significant changes in bulk soil carbon, highlighting a limitation inherent to the s

148 Plant mortality and soil carbon iCO(2) responses are highly uncertain.

149 years of experimental CO(2) doubling reduced soil carbon in a scrub-oak ecosystem despite higher plan

150 m nonwoody to woody vegetation and a loss of soil carbon in ambient plots and show that these changes

151 Our findings indicate that losses of soil carbon in England and Wales--and by inference in ot

152 ld, which makes up a large fraction of total soil carbon in forest soils globally.

153 CLM4 has low soil carbon in global earth system simulations.

154 We estimate grassland soil carbon in Great Britain to be 2097 Tg C to a depth

155 Soil carbon in permafrost ecosystems has the potential t

156 o projections of large long-term releases of soil carbon in response to warming of forest ecosystems.

157 soils contain some of the highest stores of soil carbon in the biosphere.

158 thawing of permafrost can lead to a loss of soil carbon in the form of methane and carbon dioxide em

159 infall have controlled the residence time of soil carbon in the Ganges-Brahmaputra basin over the pas

160 , the simulations show a significant loss of soil carbon in the past due to salinization, with a high

161 These results demonstrate that soil carbon in tropical forests is highly sensitive to w

162 Soil carbon increased by 12.67-63.30% with the use of so

163 crobial models, when forced with climate and soil carbon input predictions from the 5th Coupled Model

164 ease soil N cycling rates because of greater soil carbon inputs and microbial N immobilization.

165 However, most soil carbon inventories only consider surface soils, and

166 ontrolling the accumulation and stability of soil carbon is critical to predicting the Earth's future

167 The effect of mycorrhizal type on soil carbon is independent of, and of far larger consequ

168 in subsoil horizons where most of the arctic soil carbon is located.

169 tury or longer to re-attain pre-agricultural soil carbon levels.

170 o the atmosphere, with phases of substantial soil carbon loss alternating with phases of no detectabl

171 Our study demonstrates that soil carbon loss due to R(h) in Tibetan alpine soils-esp

172 iming, magnitude, and thermal acclimation of soil carbon loss.

173 stimulate plant productivity and thus offset soil carbon losses from tundra ecosystems.

174 In the seventh year, warming-induced soil carbon losses were almost totally compensated for b

175 We did not detect an increase in old soil carbon losses with warming at either site.

176 ) enhancement of AMF results in considerable soil carbon losses.

177 unity composition could retard or accelerate soil carbon losses.

178 ndy regions, considerable absolute losses of soil carbon may occur in high-latitude regions that stor

179 Here, we show that a multi-pool soil carbon model can match the change in bulk turnover

180 s newly engaged members of the International Soil Carbon Network, we have identified gaps in data, mo

181 B) ratios, extracellular enzyme activities, soil carbon : nitrogen ratio, and soil pH over a growing

182 ic contribution of the Gadgil effect to high soil carbon : nitrogen ratios in ectomycorrhizal ecosyst

183 ystems with ectomycorrhizal plants have high soil carbon : nitrogen ratios, but it is not clear why.

184 haracterized by nine enzymes associated with soil carbon, nitrogen, phosphorous and sulfur cycling, w

185 il ammonium, and soil pH, but decreased with soil carbon:nitrogen and carbon:nitrogen of microbial bi

186 changed at elevated C(a) where losses of old soil carbon offset increases in new carbon.

187 ecomposer activity, but did not change total soil carbon or nitrogen stocks, thereby increasing net e

188 , hydroclimate may be the dominant driver of soil carbon persistence in the tropics(4,5); however, th

189 robic microsites are important regulators of soil carbon persistence, shifting microbial metabolism t

190 mosphere and fluctuations in the size of the soil carbon pool directly influence climate conditions.

191 Strategies to increase the soil carbon pool include soil restoration and woodland r

192 One-third of the global soil carbon pool is stored in northern latitudes, so the

193 An increase of 1 ton of soil carbon pool of degraded cropland soils may increase

194 t, because of the limited size of the labile soil carbon pool.

195 use pre-industrial climate to initialize the soil carbon pool.

196 The amount and turnover time of C in passive soil carbon pools (organic matter strongly stabilized on

197 y shift ecosystem carbon storage by changing soil carbon pools and nitrogen limitations on plant grow

198 Despite being a significant input into soil carbon pools of many high-latitude ecosystems, litt

199 pected to be important for predicting future soil carbon pools.

200 issues in biodiversity, and vulnerability of soil carbon pools.

201 High latitudes contain nearly half of global soil carbon, prompting interest in understanding how the

202 ffset of ecosystem carbon uptake by enhanced soil carbon release under CO(2) enrichment.

203 Recent work has suggested that soil carbon respiration may be reduced by competition fo

204 at ectomycorrhizal roots and hyphae decrease soil carbon respiration rates by up to 67% under field c

205 n our estimates, the direction of the global soil carbon response is consistent across all scenarios.

206 y used single-pool approach to investigating soil carbon responses to changing environmental conditio

207 icroorganisms, and in turn the rate at which soil carbon returns to the atmosphere.

208 to the global scale, we provide estimates of soil carbon sensitivity to warming that may help to cons

209 val technologies (GGRTs); one such GGRT uses soil carbon sequestration (SCS) in agricultural land.

210 is article, we explore two CDR technologies: soil carbon sequestration (SCS), and carbon capture and

211 ing atmospheric CO(2) concentrations through soil carbon sequestration and afforestation; reducing pr

212 ss the potential for negative emissions from soil carbon sequestration and biochar addition to land,

213 Results indicate that soil carbon sequestration and biochar have useful negati

214 Soil carbon sequestration and the conservation of existi

215 etter understanding of plant root effects on soil carbon sequestration and the sensitivity of SOC sto

216 Limitations of soil carbon sequestration as a NET centre around issues

217 assumed to be a major mechanism facilitating soil carbon sequestration by increasing carbon inputs to

218 Enhanced soil carbon sequestration could offset only a small part

219 framework in which to comprehensively assess soil carbon sequestration in biochars.

220 continued and strong potential for enhanced soil carbon sequestration in some ecosystems to mitigate

221 The implementation of soil carbon sequestration measures requires a diverse se

222 is possible that increasing crop albedo and soil carbon sequestration might contribute towards mitig

223 ntegrated assessment models do not represent soil carbon sequestration or biochar.

224 Sustainable soil carbon sequestration practices need to be rapidly s

225 ons suggest that a warmer climate may change soil carbon sequestration rates in forest ecosystems owi

226 crucial to their successful deployment as a soil carbon sequestration strategy.

227 h decreased use of farm inputs and increased soil carbon sequestration, but it might also exacerbate

228 conversion to organic farming contributes to soil carbon sequestration, but until now a comprehensive

229 which can have detrimental consequences for soil carbon sequestration, nitrous oxide emissions, nitr

230 productivity of AM fungi, thereby modifying soil carbon sequestration, nutrient cycling and host pla

231 tions of plant residue and organic manure to soil carbon sequestration.

232 oots, which regulates both root function and soil carbon sequestration.

233 h ) determines rates of biomass turnover and soil carbon sequestration.

234 s in agriculture, ecosystem restoration, and soil-carbon sequestration.

235 system models (ESMs) estimate a significant soil carbon sink by 2100, yet the underlying carbon dyna

236 rocesses as well as soil textural effects on soil carbon stabilization were larger than direct temper

237 Aquaculture conversion removed 60% of soil carbon stock and 85% of live biomass carbon stock,

238 ing SOC which is the main component of total soil carbon stock and the most relevant to global change

239 ing the impacts of paleoclimatic extremes on soil carbon stock can shed light on the vulnerability of

240 ds have accumulated one third of the Earth's soil carbon stock since the last Ice Age.

241 We derive a new estimate of modern soil carbon stock to 3 m depth by including the paleocli

242 attern and magnitude of the predicted future soil carbon stock will mainly rely on the temperature se

243 ng are contingent on the size of the initial soil carbon stock, with considerable losses occurring in

244 management intensity increased, but greatest soil carbon stocks (accounting for bulk density differen

245 cantly correlated with fine root biomass and soil carbon stocks (r(2) = 0.62-0.71; p < 0.1), suggesti

246 odels generated similar estimates of initial soil carbon stocks (roughly 1,400 Pg C globally, 0-100 c

247 Soil carbon stocks accounted for >98% of TECS in the sea

248 al uncertainty on the global distribution of soil carbon stocks and turnover times we developed a soi

249 eir potential importance in the evolution of soil carbon stocks but have been largely ignored in aqua

250 nsive analysis of warming-induced changes in soil carbon stocks by assembling data from 49 field expe

251 mbination with potassium and micronutrients, soil carbon stocks changed considerably, with an average

252 Replenishment of permafrost soil carbon stocks following peak warming probably contr

253 Assessment to provide unbiased estimates of soil carbon stocks for wetlands at regional and national

254 Soil carbon stocks in both topsoil and subsoil are posit

255 al models used to forecast changes in global soil carbon stocks in response to warming.

256 empirical relationship suggests that global soil carbon stocks in the upper soil horizons will fall

257 ivergent projections about the fate of these soil carbon stocks over the 20(th) century, with models

258 glaciation period, a depletion of basin-wide soil carbon stocks was triggered by increasing rainfall

259 , energy/water fluxes) and reservoirs (e.g., soil carbon stocks).

260 rest harvesting did not significantly affect soil carbon stocks, despite an elevated dead wood densit

261 questration and the conservation of existing soil carbon stocks, given its multiple benefits includin

262 ding the effects of climate change on global soil carbon stocks.

263 del initialization for simulating permafrost soil carbon stocks.

264 The resulting vegetation and soil carbon storage and global land carbon fluxes were c

265 Here we present evidence that soil carbon storage and nitrogen cycling in a grassland

266 and so knowledge of the factors controlling soil carbon storage and turnover is essential for unders

267 ying the positive plant diversity effects on soil carbon storage are poorly understood.

268 utrient enrichment might influence grassland soil carbon storage at a global scale.

269 s suggest that China's crop productivity and soil carbon storage could be enhanced through minimizing

270 omposers, which is consistent with increased soil carbon storage in ectomycorrhizal ecosystems global

271 his leads to the theoretical prediction that soil carbon storage is greater in ecosystems dominated b

272 The higher soil carbon storage rates of the second period (years 13

273 es ecosystem functions and services, such as soil carbon storage.

274 feedback from soil N to canopy greenness to soil carbon storage.

275 lationship between nitrogen availability and soil carbon storage.

276 rogen and phosphorous had minimal impacts on soil carbon storage.

277 ecosystems contain one-third of the world's soil carbon store and many have been exposed to drought

278 Considering the 1,035 Pg of arctic soil carbon, such an additional stimulation of decomposi

279 els of SOC help reveal the interaction among soil carbon systems, climate and land management, and th

280 Total stocks of soil carbon (t ha(-1) ) to 1 m depth were 10.7% greater

281 cially on reductions in the turnover time of soil carbon (tau(s)) with warming.

282 This feedback will occur if organic-soil carbon that escaped burning in previous fires, term

283 w that warming caused a considerable loss of soil carbon that was enhanced by associated changes in m

284 mate change projections, and the response of soil carbon to climate change contributes the greatest u

285 hich do not currently account for changes in soil carbon to depth with management.

286 temperatures will stimulate the net loss of soil carbon to the atmosphere, driving a positive land c

287 conservative assumption that the response of soil carbon to warming occurs within a year, a business-

288 Our results highlight the vulnerability of soil carbon to warming that is years-to-decades old, whi

289 Soil carbon transformation and sequestration have receiv

290 However, emerging evidence suggests that soil carbon turnover is not dominantly controlled by the

291 s(4,5); however, the sensitivity of tropical soil carbon turnover to large-scale hydroclimate variabi

292 c plant effects, particularly on measures of soil carbon turnover.

293 eliorate the predicted respiratory losses of soil carbon under climate change scenarios, but unlike p

294 of total and decay-resistant acid-insoluble soil carbon under conditions of elevated carbon dioxide

295 In mid- and long-term abandoned field soil, carbon uptake by fungi increases without an increa

296 The decline in soil carbon was driven by changes in soil microbial comp

297 Soil carbon was lost at subambient C(a), but was unchang

298 ram soil carbon, and CH4 production per gram soil carbon was two times greater from sites without per

299 Increases in soil carbon were related to the enhanced accumulation of

300 Our data document significant losses of soil carbon with permafrost thaw that, over decadal time