ライフサイエンスコーパス: soil

1 oils with bacterial wilt (termed as degraded soils).

2 reased in topsoil while decreasing in deeper soil.

3 ich facilitate nutrient acquisition from the soil.

4 ppm, covering the normal range of nitrate in soil.

5 cies among the 76 isolates from the tropical soil.

6 attributed to dissolution of CuO NPs in the soil.

7 t for life and to be an analogue for Martian soils.

8 ve, compromising their persistence in low pH soils.

9 atly exceeding the levels found in temperate soils.

10 andscapes underlain by intensively weathered soils.

11 e attributed to methanogenesis in oxygenated soils.

12 s more methanogenesis activity in oxygenated soils.

13 d plant biomass production on phosphate-poor soils.

14 zyme activities when compared to the healthy soils.

15 e in organic layers and others favor mineral soils.

16 was significantly increased in the degraded soils.

17 the amount of carbon stored in agricultural soils.

18 re (MAT) was similar for organic and mineral soils (0.029 degrees C(-1) ).

19 ls (2.43) and the lowest found for grassland soils (1.67) and significantly increased with increasing

20 21, ranging from the highest found in forest soils (2.43) and the lowest found for grassland soils (1

21 Soils account for the largest terrestrial pool of carbon

22 Through an analysis of soil aggregate fractal properties supported by 3D microt

23 In P-rich areas of all investigated soil aggregates, P was predominantly co-located with alu

24 ealth risks through exposure to contaminated soil and groundwater.

25 ize and proliferate in distinct niches, from soil and plants to diverse tissues in human hosts.

26 matrices are critical to the preservation of soil and sediment organic matter.

27 easible strategies for cleaning up DNAN from soil and water have not been developed.

28 ed C60 are unlikely to accumulate in surface soils and are readily mineralized by a range of soil mic

29 chromium (Cr(VI)) is generated in serpentine soils and exported to surface and groundwaters at levels

30 and carbon dioxide from natural gas well pad soils and from nearby undisturbed soils in eastern Utah.

31 exclude C. flamarioni from areas with softer soils and higher food availability.

32 ical determinant of Cr(VI) generation within soils and sediments is the necessary interaction of two

33 oxides within fixed solid matrices common to soils and sediments.

34 mineral sorbents and organic matter (OM) in soils and sediments; however, this tertiary system has r

35 mulate the distribution of P in agricultural soils and to assess the contributions of the different d

36 nd-atmosphere feedbacks involving desiccated soils and vegetation might have played a role in driving

37 ce C storage in forest or wetland biomass or soil, and will not suffer from the non-permanence risk t

38 These results highlight the importance of soil- and leaf-P in defining the photosynthetic capacity

39 elling animals and microorganisms in shallow soil are affected as well.

40 radients and when concentration centroids in soil are closer to trees.

41 artitioning, and mineralization of carbon in soils are under increasing scrutiny as we develop a more

42 oducts can be irreversibly bound to humin in soils as a remediation strategy, which can be enhanced b

43 nd corresponding to P inherited from natural soils at the conversion to agriculture (BIOG) and farmin

44 s of abiotic CO2 uptake in arid and semiarid soils: atmospheric pressure pumping, carbonate dissoluti

45 ic bacterium (E. coli K-12) in mixtures with soil bacteria (Pseudomonas putida F1 and Bacillus subtil

46 ut FTCs could lead to divergent responses in soil bacteria and their microinvertebrate consumers, pot

47 ying ichips for environmental cultivation of soil bacteria as an example; the protocol consists of (i

48 eraction between legumes and nitrogen-fixing soil bacteria results in a specialized plant organ (i.e.

49 mers, it is seldom mineralized by indigenous soil bacteria.

50 a proof of principle, PLSR was used to build soil-bacterium compatibility models to predict the bioau

51 calcitrant organic or mineral sources in the soil, besides increasing fungal competition for progress

52 tite positive feedback relationships between soil biodiversity, fertility and plant productivity are

53 of -66.2 +/- 6.4 per mil, consistent with a soil biogenic origin.

54 We found that the soil biogeochemical background corresponding to P inheri

55 However, most studies have considered soil biota as a black box or focussed on specific groups

56 They compete for iron with soil-borne pathogens or induce a systemic resistance tha

57 gs, experimental additions of inorganic N to soils broadly show a suppression of microbial activity,

58 associated anaerobic conditions, leading to soil C accumulation.

59 ving trees, biomass of trees and shrubs, and soil C content.

60 t-duration events such as fire can influence soil C dynamics with implications for both the parameter

61 Nitrogen deposition alone increased the soil C input (+20%), but the interaction of warming and

62 rming and N deposition greatly increased the soil C input by 49%.

63 Because increased turnover rates of new soil C limit the potential for additional soil C sequest

64 nconsistent with predictions of conventional soil C models and suggest that elevated CO2 might increa

65 ns of climate, soil properties, C inputs and soil C pools in determining rC .

66 ew soil C limit the potential for additional soil C sequestration, the capacity of land ecosystems to

67 ave also served as a pathway for substantial soil C sequestration.

68 d carbon (C) sequestration and contain large soil C stocks.

69 N deposition have the potential to increase soil C storage by reducing the decay of plant litter and

70 ikely differ and alter the long-term fate of soil C, but these separate pools, which can be distingui

71 The temporal trends in soil C-N-P stoichiometry differed among vegetation, soil

72 ted CO2 might increase turnover rates of new soil C.

73 average soil N concentration did not change, soil C:N increased in topsoil while decreasing in deeper

74 t, where Q10 was primarily influenced by the soil C:N ratio and soil pH.

75 d by the content of soil organic carbon (C), soil C:N ratio, and clay content, where Q10 was primaril

76 ols, and more pronounced temporal changes in soil C:N, N:P, and C:P ratios at low elevations.

77 s study suggest that the radicals present in soil can play an important role in natural remediation m

78 of soil organic carbon (SOC) in agricultural soils can not only improve soil quality but also influen

79 ations with those found on less contaminated soils can provide insights into ecological processes tha

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

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

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

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

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

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

86 diversity and globally significant stores of soil carbon.

87 to Ndep has enhanced detrital inputs of C to soils, causing an average increase of 1.2 kgCm(-2) (c. 1

88 The isotopic partitioning of soil Cd sources in this system was aided by a change in

89 hermore, winter foraging exclusion increased soil cellulolytic and hemicellulolytic enzyme potential

90 veral bioclimatic conditions as well as with soil characteristics and land use.

91 d the outcome for possible pathways by which soil characteristics may increase the probability of CWD

92 leading indicator of marsh migration, while soil characteristics such as redox potential and surface

93 eflect the independent roles tree mortality, soil chemistry and geographical distance play in regulat

94 tance of host tree mortality from changes in soil chemistry following tree death.

95 r layer only accounted for 19% increases in soil CO2 flux, suggesting that the leaching of dissolved

96 e topsoil is the major cause of rain-induced soil CO2 pulse.

97 leached DOC input in regulating rain-induced soil CO2 pulses and microbial community composition, and

98 synthetic domain composition and richness in soils collected across the Australian continent.

99 concentration in the effluent suggested that soil colloids facilitated the release of AgNP (cotranspo

100 Soil communities are diverse taxonomically and functiona

101 munities in the rhizosphere, but altered the soil communities where hybrid maize was grown.

102 k a generalizable understanding of how these soil communities will change in response to predicted in

103 for growth compared with arable or grassland soil communities.

104 Increased soil strength due to soil compaction or soil drying is a major limitation to

105 nization of the manifold mineral and organic soil components to distinct mineral assemblages, which a

106 and therefore, has been employed to predict soil composition and heavy metal contents.

107 s is significantly affected by in planta and soil concentration gradients and when concentration cent

108 Until now, the mechanisms governing soil concentrations have been evaluated in small-scale s

109 hylation in paddy environments, and thus the soil conditions conducive to the accumulation of methyla

110 ays high productivity under drought and poor soil conditions, it is susceptible to disease, postharve

111 er, the data suggest that, regardless of the soil conditions, trees enrich variable bacterial communi

112 mportantly, the C1 (OE) rice plants grown on soil contain higher endogenous iron concentration than w

113 es that demonstrate the long-term effects of soil contamination.

114 late that the pore structure of many mineral soils could undergo N-dependent changes as atmospheric C

115 We used 33,241 soil data points to model recent (1980-1999) global dist

116 t a given location if samples are taken at a soil depth of at least 60 cm.

117 rmined on an equivalent mass basis to 30 cm soil depth.

118 t the continental scale and across different soil depths is lacking.

119 ol for a rapid characterisation of water and soil DOM.

120 ased soil strength due to soil compaction or soil drying is a major limitation to root growth and cro

121 r(VI)/km(2)/yr and subsequently flushed from soil during water infiltration, exporting 0.01 to 3.9 kg

122 whole ecosystem such as natural wild plants, soil dwelling animals and microorganisms in shallow soil

123 w that some biocides are degraded rapidly in soil (e.g., isothiazolinones: T1/2 < 10 days) while othe

124 cape changes and alters the functionality of soil ecosystems.

125 Here, we present a new method that collects soil-emitted NO through NO conversion to NO2 in excess o

126 soils was obviously decreased with weakened soil enzyme activities when compared to the healthy soil

127 r example, attempting a mass balance between soil erosion and production, which indicates that barren

128 found to experience the highest estimates of soil erosion rates.

129 cial risk, increasing biodiversity, reducing soil erosion, and improving nutrient- and water-use effi

130 d measured dissolved concentrations in CaCl2 soil extracts, using the different extractions as altern

131 t mycorrhizal type, through effects on plant-soil feedbacks, could be an important contributor to pop

132 ion explained much of the variation in plant-soil feedbacks.

133 e due to its influence on soil functions and soil fertility.

134 evealed a different induction in response to soil flooding (CsPYL5) or drought (CsPYL8).

135 ecting energy and nutrient transfer rates in soil food webs of cold ecosystems.

136 ecause of their ability to remain dormant in soil for many years.

137 g a natural capital accounting structure for soil, for example, attempting a mass balance between soi

138 ating the compounding effects of non-climate soil forming factors is a nontrivial challenge that must

139 We cultured soil from a rice field in Laos for B. pseudomallei at di

140 tion in soil science due to its influence on soil functions and soil fertility.

141 rministic and stochastic processes structure soil fungal communities following landscape-scale insect

142 entally removed arthropods, foliar fungi and soil fungi from the longest-running plant diversity expe

143 e, we investigated the response of plant and soil fungi to drought of different intensities using a w

144 y in regulating the community composition of soil fungi.

145 We find that escape of soil gas through wetland trees is the dominant source of

146 building is limited by diffusion through the soil gas.

147 dence of how management decisions can impact soil GHG emissions and surface SOC stocks.

148 body and the ecosystem, can be released into soils, ground-, and surface waters either from ore miner

149 Deep roots connect deep soil/groundwater to the atmosphere, thus influencing the

150 Chloroform emission from soil has been reported from diverse Arctic, temperate, a

151 ata clearly show that northern boreal forest soils have a strong sink capacity for Hg, and indicate t

152 Hitherto, ancient frozen soils have proved excellent in preserving DNA molecules,

153 Tundra uptake of gaseous Hg(0) leads to high soil Hg concentrations, with Hg masses greatly exceeding

154 In acid soils, however, heterotrophic denitrification was the ma

155 entories of total Hg are strongly related to soil humus C accumulation (R(2) = 0.94, p < 0.001).

156 nmental variables relevant to diffusion into soils (i.e., soil moisture, snow depth, snow density).

157 s well pad soils and from nearby undisturbed soils in eastern Utah.

158 The rhizosphere is the zone of soil influenced by a plant root and is critical for plan

159 Overall, glucose added at 1.8 wt % and soil inoculum added at 0.1 wt % provided the most effect

160 The importance of climate-soil interactions to Se distributions suggests that othe

161 Se concentrations were dominated by climate-soil interactions.

162 Soil is a crucial component of the biosphere and is a ma

163 The bioavailability of heavy metals in soil is controlled by their concentrations and soil prop

164 e unexplored diversity found in the tropical soil is possibly related to biogeographical patterns.

165 tland area with saturated and warmer organic soils is expected to increase landscape methane (CH4 ) e

166 rting to subtropical drylands, and that deep soil layers could be increasingly dry during the growing

167 s as much (15) N was retained in the O and A soil layers when N was derived from litter decomposition

168 porters have roles in amino acid uptake from soil, long-distance transport, remobilization from veget

169 crop areas are most vulnerable to potential soil loss.

170 challenge that must be overcome to establish soil magnetism as a trusted paleoenvironmental tool.

171 Soil may therefore be a previously unrecognized, natural

172 omoionic montmorillonites and to heteroionic soils (mean absolute error of 0.27 log unit).

173 age, than their typical counterparts in most soil metagenomes and the abundance of bacterial amoA was

174 30 years of carefully managed restoration on soil microbial communities at the Nachusa Grasslands in

175 Here we compared soil microbial communities in 41 urban parks of (i) dive

176 forests harboured distinct but less diverse soil microbial communities than urban parks that are und

177 Ecosystem carbon losses from soil microbial respiration are a key component of global

178 Soil microfauna and especially root-feeding nematodes we

179 ls and are readily mineralized by a range of soil microorganisms.

180 e the fate of organic matter associated with soil mineral and aggregate fractions in some of the ecos

181 Spatial heterogeneity in soil moisture and conspecific density were the predomina

182 lobal models; however, within certain biomes soil moisture and soil carbon emerge as dominant predict

183 The inferred temporal evolution of soil moisture is remarkably consistent between independe

184 tors of the Mediterranean coast; and earlier soil moisture maxima have led to earlier winter floods i

185 with age when nonnative biomass was high and soil moisture was low.

186 ese data to observations of water potential, soil moisture, and vapor pressure deficit over 2 yr in t

187 ies of monthly meteorological, hydrological, soil moisture, and vegetation droughts from 1981 to 2013

188 hydrological responses (evapotranspiration, soil moisture, seasonal and annual streamflow, and water

189 bles relevant to diffusion into soils (i.e., soil moisture, snow depth, snow density).

190 e global scale by linking global datasets of soil moisture, soil temperature, primary productivity, a

191 of mortality by 40% compared to LSM-modeled soil moisture.

192 ities and positive or nonlinear responses to soil moisture.

193 hesis that realistic land conditions such as soil moisture/soil temperature (SM/ST) can significantly

194 provided empirical evidence supporting that soil N availability, under global warming scenarios, is

195 Although average soil N concentration did not change, soil C:N increased

196 global implications for our understanding of soil N cycling pathways and N2 O production.

197 l effects on both plant N pools and rates of soil N cycling that were independent of those of species

198 consideration of factors such as aridity and soil N status is crucial for predicting plant and ecosys

199 ct the contribution of microbial residues to soil N transformation.

200 Soil N2 O and CH4 fluxes were measured for five crop-yea

201 groups, whereas little is known about entire soil networks.

202 In a region of intermediate soil nitrogen availability, the dominant leaf strategy m

203 ntrolled) due to feedbacks of leaf traits on soil nitrogen mineralization through litter quality.

204 proved understanding of biochar's impacts on soil NO emissions.

205 y and health cost models to assess how these soil NO reductions could influence U.S. air quality and

206 on strategy, which can be enhanced by adding soil OC.

207 Emissions of NO from soils occur primarily during denitrification and nitrifi

208 n the present study the degradation rates in soil of 11 biocides used for the protection of building

209 ich is dominant species on the saline/alkali soil of northeast China.

210 ssing and turnover of dead organic matter in soils of arid regions), reduce human exposure to mycotox

211 reased penetration stress when elongating in soils of greater strength.

212 netration stress and root elongation rate in soils of greater strength.

213 dialkylated PFPiAs was investigated in seven soils of varying geochemical parameters.

214 l greenhouse gas emissions from agricultural soils or wastewater treatment systems.

215 min was primarily affected by the content of soil organic carbon (C), soil C:N ratio, and clay conten

216 Restoration of soil organic carbon (SOC) in agricultural soils can not

217 Soil organic carbon is projected to increase in Australi

218 and climatic influences on the formation of soil organic matter (SOM).

219 ge by reducing the decay of plant litter and soil organic matter (SOM).

220 l warming results in a four-phase pattern of soil organic matter decay and carbon dioxide fluxes to t

221 indicate that the sequestered Hg is bound in soil organic matter pools accumulating over millennia.

222 nd C pools.Most molecular scale knowledge on soil organo-mineral interactions remains qualitative due

223 ivers of the spatial variability in cropland soil P content but that their contribution varied betwee

224 al data sets describing these drivers with a soil P dynamics model to simulate the distribution of P

225 Soil [P] and leaf Pa were key explanatory factors for mo

226 N-P stoichiometry differed among vegetation, soil, parent material types, and spatial climate variati

227 ater where percent clay is less than 18% and soil pH is greater than 6.6.

228 imarily influenced by the soil C:N ratio and soil pH.

229 s were constructed from measured aqueous and soil phase concentrations and were fit sufficiently well

230 ities and the ability to efficiently extract soil phosphorus, for example Carex appressa, are, thus,

231 uated in small-scale studies, which identify soil physicochemical properties as governing variables.

232 phytoavailability, and provided evidence for soil-plant transfers at concentrations lower than those

233 etal presents problems for the management of soil-plant-animal systems, because the magnitude and dir

234 We hypothesized that soil Po would initially increase with paddy management a

235 ging" on millennial time scales in catchment soils prior to its ultimate deposition.

236 d a network of intercorrelations of climate, soil properties, C inputs and soil C pools in determinin

237 Ignorance of the impact of changes in soil properties, C pool composition and C input (quantit

238 il is controlled by their concentrations and soil properties.

239 influence the extraction efficiency were the soil properties; a high organic matter or clay content w

240 ) in agricultural soils can not only improve soil quality but also influence climate change and agron

241 ISG ranks third and LFGTE fourth on all four soil-quality and productivity indicators.

242 The bioconcentration factors (BCFs; plant/soil ratios) were highest in foliage, while the total tr

243 versity, abundance, and fate in contaminated soils remain to be elucidated.

244 onmental and industrial applications such as soil remediation, CO2 sequestration, and enhanced oil re

245 Heterogeneous soil resources, such as water, nitrogen and phosphate, a

246 ves of 32.6 and 24.5 days in forest and farm soils, respectively.

247 bal warming and may have profound impacts on soil respiration (Rs) and its components, that is, autot

248 th observations of annual Rs from the Global Soil Respiration Database (SRDB).

249 examined the effects of fire severity on the soil respiration rate (Rs) and its component change in a

250 However, response patterns of soil respiration to precipitation changes remain uncerta

251 iarid grasslands will release less C through soil respiratory processes under the projected seasonal

252 A comparison of oxic to anoxic soils reveal up to ten times greater methane production

253 anding mineral controls on As cycling in the soil-rice nexus, and the sampling approach can be adopte

254 valuated through the determination of DNZ in soil, river water and wastewater samples and satisfactor

255 s were quite different, and some indicators (soil salinity, foraminifera) appeared to migrate more ea

256 s versutus strain L10.15(T), isolated from a soil sample obtained near an elephant seal wallow in Ant

257 ncentrations in over 50 groundwater and 1000 soil samples collected from a tetrachloroethylene- (PCE-

258 Soil samples from 38 homes were analyzed to determine wh

259 To characterize source composition, soil samples were collected from local playa and desert

260 recently has received increased attention in soil science due to its influence on soil functions and

261 Contrary to small-scale studies, soil Se concentrations were dominated by climate-soil in

262 Microbial communities in bare fallowed soil showed a marked capacity to utilise phytate for gro

263 The tests without soil (simulating pore-water exposure) revealed higher to

264 average increase of 1.2 kgCm(-2) (c. 10%) in soil SOC over the period 1750-2010.

265 , did not support increased PFAA removal via soil sorption.

266 of genetic admixture between the serpentine-soil specialist leather oak (Quercus durata) and the wid

267 Increased soil strength due to soil compaction or soil drying is a

268 Under moderate and high soil strength, smaller root tip radius-to-length ratio w

269 g pesticide degradation and transport in the soil-surface water continuum remains challenging at the

270 exacerbate the impacts of climate change on soil systems, with profound implications for terrestrial

271 listic land conditions such as soil moisture/soil temperature (SM/ST) can significantly improve the m

272 ebruary minimum), positively correlated with soil temperature and negatively correlated with environm

273 Soil temperature is comparable with previously reported

274 by linking global datasets of soil moisture, soil temperature, primary productivity, and soil carbon

275 structural and biogeochemical components of soils that can be strongly altered by redox-driven proce

276 ssion rates match those from tropical forest soils, the world's largest natural terrestrial N2O sourc

277 ting in the transfer of 40-70 Pg carbon from soil to the atmosphere each year.

278 duality in the functional linkage of organic soils to aquatic ecosystems whereby they can help buffer

279 While DNAN is known to biotransform in soils to aromatic amines and azo-dimers, it is seldom mi

280 is study suggests that rehabilitation of NCP soils to reduce salinity and increase crop yields have a

281 responses to eCO2 are positively related to soil total N.

282 treatment reduces the severe consequences of soil-transmitted helminthiasis.

283 Mass deworming for soil-transmitted helminths compared with controls led to

284 system, management equipment/timing/history, soil type, location, weather, and the depth to which Del

285 ications for CO2 losses from tropical forest soils under future rainfall changes.

286 Soil uptake was highly seasonal (July maximum, February

287 Most conceptual and mathematical models of soil vapor intrusion assume that the transport of volati

288 warming in moist acidic tundra, we show that Soil warming had a much stronger effect on CO2 flux than

289 ng data from 7 years of experimental Air and Soil warming in moist acidic tundra, we show that Soil w

290 We found that soil warming results in a four-phase pattern of soil org

291 Biological activity of degraded soils was obviously decreased with weakened soil enzyme

292 and non-essential isoprenoids in response to soil water availability and solar radiation.

293 water use efficiency, drought tolerance, and soil water conservation properties.

294 g, carbonate dissolution, and percolation of soil water through the vadose zone.

295 Within soils, we detected Cr(VI) in the same horizons where Cr(

296 r the snail directly exposed to contaminated soil were lower than trophic transfer by consumption of

297 abolite profiling of non-sterile rhizosphere soil, which represents a technical advance towards the e

298 Acidic and SOM-rich soils, which typically develop under mesic conditions, a

299 and shows that the diffuse contamination of soils will remain a source for PCBs and PCDD/Fs in our f

300 ential significantly altered in the degraded soils with bacterial wilt (termed as degraded soils).

301 f this novel methodology is still limited to soils with high organic phosphorus content.