ライフサイエンスコーパス: soil carbon

1 on responses mediate the observed changes in soil carbon.

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

3 groups represented the major fraction of the soil carbon.

4 anic farming has the potential to accumulate soil carbon.

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

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

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

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

9 diversity and globally significant stores of soil carbon.

10 and whether plant species loss will decrease soil carbon.

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

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

13 ng systems provided net mitigation, although soil carbon accumulation in no-till systems came closest

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

65 Soil carbon changes, direct and indirect land use change

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

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

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

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

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

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

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

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

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

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

76 Soil carbon cycling processes potentially play a large r

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

99 riation in key biogeochemical processes like soil carbon formation.

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

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

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

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

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

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

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

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

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

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

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

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

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

113 Soil carbon in permafrost ecosystems has the potential t

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

136 The stability of the soil carbon pool ( approximately 150 tons C ha-1) appear

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

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

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

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

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

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

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

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

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

146 stration of 117 Gt C into the vegetation and soil carbon reservoirs.

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

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

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

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

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

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

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

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

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

156 Soil carbon sequestration and the conservation of existi

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

194 10(12) kg) C reduction in the vegetation and soil carbon storage, in an atmosphere with pCO(2) = 0.03

195 lationship between nitrogen availability and soil carbon storage.

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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