ライフサイエンスコーパス: soil

1 ic matter through the column (analogous to a soil).

2 ng natural, incidental, or engineered NPs in soil.

3 he dominant limitation on J(CO2) on the clay soil.

4 The RSA varied between ~2 and 20 m(2)/g soil.

5 maintain greater nitrate-N levels in flooded soil.

6 ce, with somewhat smaller declines in meadow soil.

7 times in mineral soil and 2 times in organic soil.

8 ated with molybdenum and nickel found in the soil.

9 or synergism) in a nutrient-poor greenhouse soil.

10 or assessing impacts on the natural resource soil.

11 ooctaneamide ammonium compound (PFOAAmS) for soils.

12 r germination and seedling growth in flooded soils.

13 it only includes the contribution of mineral soils.

14 (RBA) of Pb in untreated (U) and remediated soils.

15 es and NTF that we found to be ubiquitous in soils.

16 ves nitrogen, and minimizes nutrient loss in soils.

17 6,7), solid tumours(8,9), bioreactors(10) or soil(11).

18 at high concentrations (maximum 448 ng/g in soil, 3.4 mg/L in groundwater).

19 soils also vary across elevation, with bare soil above the meadows potentially poorer for plant esta

20 ) pool but also impact SOC stability through soil aggregation.

21 We evaluated Streptomyces biogeography in soils along a 1200 km latitudinal transect across New Ze

22 However, soils also vary across elevation, with bare soil above t

23 Soils amended with nitrogen fertilizer exhibited increas

24 diversion strategy that generates biogas and soil amendment products.

25 These include their on-farm use as (1) soil amendments to offset nitrogen fertilizer inputs, (2

26 h is substantially more effective than other soil amendments, including P.

27 of N-cycling genes was predicted by greater soil ammonium (N-NH(4) ), organic phosphorus, and C:N.

28 sed N(2)O production, by 74 times in mineral soil and 2 times in organic soil.

29 ical perspective, these results suggest that soil and activated sludge microbial communities, althoug

30 ption-related bioavailability differences in soil and activated sludge.

31 ous ecologically relevant traits, as well as soil and climate characteristics.

32 ectively extract moderately soluble NPs from soil and experimentally separate them from their dissolv

33 ah River Site (SRS) or unamended vadose zone soil and exposed to 3 years of natural South Carolina, U

34 g semibatch microcosms with a Superfund site soil and groundwater, we showed that the high Fe(0) conc

35 ate through 2030, the annual mobilization of soil and Hg may increase by an additional 20-25% relativ

36 ssessment of nanoformulation shells' fate in soil and in the environment after release, as well as re

37 ments was similar, regardless of the type of soil and OW, (ii) >97.6% of the Zn input from OW accumul

38 eria was equally explained by local factors (soil and vegetation) and geospatial distance (11.5% and

39 of alpha-HCH indicated its transformation in soil and wheat.

40 adapted microbes-which are abundant in polar soils and have pivotal roles in nutrient cycling-typical

41 rce of N available to plants in agricultural soils and in many natural environments.

42 growth of microbial communities in Antarctic soils and in the surrounding oceanic waters.

43 imated RBA for Pb in both remediated natural soils and Pb-mineral spiked soils were reduced by >90% r

44 nerally increases carbon input in rice paddy soils and stimulates the growth of methane-producing mic

45 f (129)IO(3)(-) compared to (129)I(-) in all soils and the complete reduction of (129)IO(3)(-) to (12

46 d pathogenic fungi in increasingly arid crop soils and, secondly, through promotion of phosphorus bio

47 In vitro studies in plant, soil, and human systems have shown that microbial volati

48 ding the strength and erodibility of natural soils, and other polydisperse particulates that experien

49 ial invertebrates, surface water, sediments, soils, and plants were analyzed for 24 PFASs including b

50 ian canopy, high levels of organic carbon in soils, and suboxic conditions at shallow depths, which s

51 erate via different pathways when decreasing soil animal biomass.

52 Depending on soil, appropriate SOFs applied were able to reduce N(2)O

53 Warmer winter soils are thought to yield greater microbial respiration

54 Analysis of this dataset reveals that a soil area of 11.73 Mkm(2) located in nonfrigid zones has

55 cial environment resulted in the flushing of soil assemblages into the riverine system.

56 FSa in carbon sequestration in agricultural soils at a global scale may be overlooked.

57 primary productivity provide constraints on soil bacterial abundance independent from diversity.

58 Here, we examined soil bacterial and fungal diversity and community compos

59 rocesses in shaping geographical patterns of soil bacterial beta diversity.

60 ed the importance of variable selection, for soil bacterial community assembly within islands.

61 logical factors (i.e. plant productivity and soil bacterial diversity) and soil factors (e.g. clay, p

62 is a globin-coupled histidine kinase in the soil bacterium Anaeromyxobacter sp. Fw109-5.

63 The role of soil biodiversity in regulating multiple ecosystem funct

64 erstood, limiting our ability to predict how soil biodiversity loss might affect human wellbeing and

65 gical studies to explore general patterns in soil biodiversity-ecosystem functioning relationships, w

66 mpound participates in a number of important soil biogeochemical processes, creates endosymbiosis wit

67 forms and this process has been employed in soil bioremediation.

68 es could show a different pattern and slower soil biota development.

69 that were dominated by fungi and associated soil biota, including increased arbuscular mycorrhizal f

70 reduced rates of carbon (C) mobilisation by soil biota.

71 return is an effective strategy to alleviate soil-borne diseases.

72 lobal analysis of no-till-induced changes of soil C and crop yield based on 260 and 1,970 paired stud

73 obes and nematodes) and ecosystem functions (soil C and N mineralization), using paired grazed and un

74 anisms, challenging our understanding of how soil C may respond to climate-mediated changes in O(2) d

75 owever, the mechanisms underlying changes in soil C storage are not well understood, hampering long-t

76 om field studies and satellite imagery, that soil C(org) erosion (within the top 50 cm) following sea

77 presents comprehensive estimates of seagrass soil C(org) erosion following eutrophication-driven seag

78 te chrysosporium NK-1 isolated from a forest soil can effectively degrade and decolorize melanin in v

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

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

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

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

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

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

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

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

87 saltic rock dust, including via newly formed soil carbonate minerals whose long-term fate requires as

88 rosites in the otherwise aerobic porous bulk soil causing reduction of ferrihydrite and concomitant i

89 The warming-induced rise in soil CH(4) and N(2) O emissions (1.84 Pg CO(2) -equivale

90 diated by landscape topography, climate, and soil characteristics.

91 o identify the top influential factors among soil, climate, and farming practices, which drive the sp

92 ansport in yielding the observed patterns of soil CO(2) efflux being out of sync with soil temperatur

93 We measured daily soil CO(2) emission for the first two weeks and every ot

94 ied the contribution of canopy vegetation to soil CO(2) fluxes and belowground productivity.

95 in two 5-L lysimeters containing NOM-amended soil collected from the Savannah River Site (SRS) or una

96 s for a subset of house dust and residential soils collected in the AHHS, with the primary objective

97 The soil columns were dismantled and seven soil layers were

98 tance signaling phenomenon that may regulate soil conditioning.

99 iverse set of options, each adapted to local soil conditions and management opportunities, and accoun

100 uenced by external drivers, such as climate, soil conditions or land use.

101 lant traits, site level climate, and abiotic soil conditions.

102 ted with habitat shifts linked to particular soil conditions; 81.7% of edaphic variation could be exp

103 in pore water and postexperiment rhizosphere soil confirming ferrihydrite reduction.

104 red and compared to U distributions in three soil cores located in a wetland highly impacted by water

105 In this little-explored habitat, 250 soil cores were sampled from 10 plots hosting 10 differe

106 sm experiments were conducted with two paddy soils covering redox potentials from E(H) -260 to +200 m

107 New soil-crop models that could account for soil structure d

108 rowth, as well as the relevant timescales of soil degradation and recovery.

109 Soil degradation due to global warming, water scarcity a

110 eveals that soil mixing rate varies over the soil depth, with this depth dependency persisting across

111 anomalies, fueling heatwaves that exacerbate soil drying.

112 scales enhances nutrient fluxes that support soil ecology, contributes to dispersion of sediment and

113 Rice seeds germinating in flooded soils encounter hypoxia or even anoxia leading to poor s

114 The soil environment contains a broad diversity of organic a

115 n mixed inocula in the host, rhizosphere and soil environments.

116 o estimate the role of land cover change and soil erosion on river transport of Hg in a heavily ASGM-

117 ions are a matter of concern in agricultural soils especially when flooding (hypoxic conditions) resu

118 d of phene states that likely enable greater soil exploration by reallocating internal resources to g

119 oductivity and soil bacterial diversity) and soil factors (e.g. clay, pH, and C availability of micro

120 y provides a proof-of-concept that the plant-soil feedback concept can be applied to steer soil micro

121 ost-effective management practice to enhance soil fertility and crop production in the arid and semi-

122 Climate and soil fertility influence seed yield, nutrient uptake, an

123 nsport of antibiotics and ARGs in runoff and soil following land application of swine manure slurry.

124 nges in the structure and functioning of the soil food web along a 3000-km north-south transect acros

125 Interactions between plants and soil fungi and bacteria are ubiquitous and have large ef

126 on is about 29% and 5% of total agricultural soil GHG emissions in China and the world, respectively.

127 sphere, and it is critical to understand how soil greenhouse gas (GHG) emissions and uptake will resp

128 bae (FLA) are ubiquitous protozoa in aquatic/soil habitats and known to resist various disinfection m

129 Reflooding drained soils have been proposed as a means to sequester C for c

130 Current public investments to improve soil health seek to balance productivity and environment

131 er soil respiration and lower SOC in organic soil horizons than heather control plots.

132 Litter bags and soil hot water extracts (HWE) have frequently been used

133 shrublands without creating additional bare soil, however, reduces transmission losses.

134 aunal activity) mechanisms, their impacts on soil hydrological processes and plant growth, as well as

135 growing season length and simulated subdaily soil hydrology to parameterize ring width increment simu

136 o drive Zn speciation in both OW and amended soils (i.e., amorphous Zn-phosphate and Zn sorbed on hyd

137 ve way to reduce N(2)O emission from hypoxic soil in agricultural production systems.

138 t represent the wide-spread exposure of bare soil in the 1930s, suggest human activity fueled stronge

139 oxide (N(2)O) and nitrogen (N(2)) in arable soils include high nitrate, moisture and plants; we inve

140 rbon concentration in the upper 20 cm of the soil (including the organic fermentation-humus [FH] laye

141 ment type, the addition of organic matter to soil increased the capability of the coarse fraction (FS

142 th reactive timescales of denitrification in soil indicate that ~75% of the cultivated areas across E

143 kely enhancing plant-microbe competition for soil inorganic N, which was reduced by a factor of about

144 may underestimate the impacts of land use on soil invertebrates, whereas rarity provides clearer and

145 e at alkaline pH, and that mimosine can bind soil iron under alkaline pH; (ii) pole bean, common bean

146 In plants, iron uptake from the soil is tightly regulated to ensure optimal growth and d

147 Research on microplastics in soils is still uncommon, and the existing publications a

148 two-pool model, we then explored changes in soil labile and stable C decomposition along the thaw se

149 The soil columns were dismantled and seven soil layers were sampled and analyzed at the end of the

150 In addition, fire-induced hydrophobic soil layers, caused by condensation of pyrolysed waxes a

151 early growing season, particularly in deeper soil layers.

152 nt is removed in extracted timber and eroded soil, leading to shifts in ecosystem functioning and com

153 Agricultural management practices to enhance soil legacy P usage by crops includes increasing soil pH

154 We also identify the limitations of soil macroecological studies to explore general patterns

155 nvironmental assessment, which tested water, soil, manure, compost, and scat samples, was conducted t

156 ratio, (ii) extracting colloids/NPs from the soil matrix using sonication and a dispersing agent, and

157 opy-scale measurements been assessed against soil measurements in the tropics.

158 ide synthase gene clusters from an Antarctic soil metagenome.

159 stigated how large herbivore grazing affects soil micro-food webs (microbes and nematodes) and ecosys

160 vide new evidence supporting the theory that soil-microbe systems are self-organising states with org

161 Despite the important roles of soil microbes, especially the most diverse rare taxa in

162 haw) and biological (e.g. plant root growth, soil microbial and faunal activity) mechanisms, their im

163 Treatments without dispersal had lower soil microbial biomass and metabolic diversity but highe

164 mate and emphasize the close linkage between soil microbial C and N cycling.

165 er, the degree to which spatial variation in soil microbial communities modulates plant species' dist

166 Soil microbial residues may not only affect soil organic

167 Soil microbial respiration is an important source of unc

168 ly that natural aerial dispersal rate alters soil microbial responses to disturbance.

169 und that woody plant encroachment influenced soil microbial richness and community composition across

170 Example analysis using FT-MS data from a soil microbiology study demonstrates the core functional

171 lants; we investigate how differences in the soil microbiome due to antecedent soil treatment additio

172 etation performance, but their effect on the soil microbiome remains poorly understood.

173 d predicting the impact of climate change on soil microbiomes and the ecosystem services they provide

174 oil feedback concept can be applied to steer soil microbiomes with the goal of inducing resistance ab

175 how more divergent responses to each other's soil microbiota compared with closely related plant spec

176 and time; consequently, the biodiversity of soil microorganisms also differs spatially and temporall

177 mote stabilizing interactions between OM and soil minerals and this stabilization may be of increasin

178 the strong associations between proteins and soil minerals restrict such proteolytic reactions.

179 Soil mixing over long (>10(2) y) timescales enhances nut

180 The model-data comparison reveals that soil mixing rate varies over the soil depth, with this d

181 We use a multi-layer canopy-root-soil model to calculate the energy and entropy fluxes of

182 files), restrict uptake of water to conserve soil moisture (reduced hydraulic conductance, narrow met

183 well they each capture variation in WUE with soil moisture availability.

184 osphere coupling, associated with persistent soil moisture deficit, appears to intensify surface warm

185 nduct a systematic observational analysis of soil moisture feedbacks on propagating MCSs anywhere in

186 We found that soil moisture increased under deepened winter snow in ea

187 ) among species at 0.06 and 0.042 m(3) m(-3) soil moisture levels.

188 Specifically, we found stem growth stops at soil moisture potentials of -0.47 MPa for larch and -0.6

189 a strong link between dry line dynamics and soil moisture state.

190 200-year tree-ring reconstructions of summer soil moisture to demonstrate that the 2000-2018 SWNA dro

191 Soil moisture was computed in a thin upper layer and an

192 ate increased to 2.54 km m(-2) degrees C(-1) Soil moisture was negatively correlated with fine-root g

193 growth dynamics during drought and return of soil moisture.

194 in the rhizosphere are an essential link in soil nitrogen (N) cycling and plant N supply.

195 More importantly, soil nitrogen (N) increased in mature deciduous forests

196 l alter sorghum (Sorghum bicolor L.) growth, soil nutrient dynamics and interactions (antagonism or s

197 trade-offs, intraspecific-interactions, and soil nutrient dynamics in the context of biodiversity-ec

198 the seed decay rate and survivability in the soil of a rice field for 7 months.

199 in the carbon density in forest biomass and soils often elude detection.

200 d and show a strong positive impact of drier soils on convection within mature MCSs.

201 ver, total ecosystem C storage that includes soil organic C (SOC) must be considered to determine whe

202 an potentially alter spatial distribution of soil organic carbon (SOC) and total nitrogen (TN) concen

203 Soil organic carbon (SOC) concentration in WSA(0.106-0.2

204 Soil microbial residues may not only affect soil organic carbon (SOC) pool but also impact SOC stabi

205 vironment and potentially contributes to the soil organic carbon (SOC) pool.

206 ange, sea-level rise, and salinity increase, soil organic carbon (SOC) sequestration mechanisms in es

207 Quantifying changes in soil organic carbon (SOC) stocks and other soil properti

208 Although temperature controls the storage of soil organic carbon at mid and high latitudes(2,3), hydr

209 arbon by thermally altering the chemistry of soil organic matter (SOM), thereby reducing rates of mic

210 Oxidative decomposition of soil organic matter determines the proportion of carbon

211 as root exudation, microbial processes, and soil organic matter stabilization.

212 n per hectare per year from the breakdown of soil organic matter.

213 lated to the distribution and functioning of soil organisms to support their conservation and conside

214 storation of extremely degraded grassland on soil parameters have been equivocal.

215 This research employed a watershed-scale soil particle detachment model and environmental field s

216 which replaces grasses with shrubs and bare soil patches.

217 In addition, soil pH and plant community richness both explained sign

218 legacy P usage by crops includes increasing soil pH by liming, crop rotation, double-cropping, inter

219 lcium, magnesium and potassium and trace the soil phases that support these pools in 143 individual s

220 In combination with SOC, CMI and soil physical properties, we argued that alfalfa grassla

221 technique for discerning the composition of soil, plant and aquatic samples containing complex mixtu

222 highlighted that (i) the fate of Zn in water-soil-plant compartments was similar, regardless of the t

223 on allocation and the role of root growth on soil-plant hydraulics.

224 mical transformations and moving through the soil pore space.

225 Plant nutrient-acquisition strategies drive soil processes and vegetation performance, but their eff

226 effects of fertilization on P fractions in a soil profile in Mollisol.

227 find that downward movement of SOC along the soil profile reduces SOC loss under warming.

228 S and OM treatments increased throughout the soil profile.

229 stress can depend on the interaction between soil properties and irrigation management, which in turn

230 This study evaluates changes in plant-soil properties and the long-term effects of machine-gra

231 Multiple soil properties described sorption of PFASs better than

232 in situ observations of SOC, litterfall and soil properties from 206 sites covering different forest

233 n soil organic carbon (SOC) stocks and other soil properties is essential for understanding how soils

234 ersity, likely in response to differences in soil properties.

235 Soils provide a heterogeneous environment varying in spa

236 Soils provide numerous ecosystem services (ESs) such as

237 replete and Fe-limited cells, we uncover how soil Pseudomonas species reprogram their metabolic pathw

238 falfa grassland had the advantage to promote soil quality compared with arable land and forest land.

239 of delegating regressors for predicting the soil radon gas concentration (SRGC) and anomalies in rad

240 To better understand their fate when soil redox conditions change, that is, from flooding to

241 n, with deeper roots on sandy, nutrient-poor soils relative to clayey, nutrient-rich ones.

242 al carbon assimilation and fixation in paddy soils remain poorly characterized.

243 wth results from forces required to overcome soil resistance to deformation.

244 Plots with trees had greater soil respiration and lower SOC in organic soil horizons

245 ces shifted from plant aboveground and young soil respiration to old soil respiration.

246 boveground and young soil respiration to old soil respiration.

247 ographical location, weather suitability and soil's physiochemical and microbial parameters of its cu

248 cterizing different spatiotemporal facets of soil salinity and sodicity variability over the past fou

249 s that support these pools in 143 individual soil samples covering 3 climatic zones and 5 different s

250 for the analysis of smaller microplastics in soil samples, but slight modifications and combinations

251 controlling SD are involved in regulation of soil seedbank longevity.

252 Higher values of soil silt and depth increased C(i) /C(a) , likely by pro

253 ater transport of biocidal metal cations and soil solutes, degradation and loss of crystallinity of c

254 Globally, soils store two to three times as much carbon as current

255 However, it was shown that the soil strength does not considerably change after a certa

256 Results suggest that although soil structure affects local hydrologic response, its im

257 New soil-crop models that could account for soil structure dynamics at decadal to centennial timesca

258 se and short rainfall events mask effects of soil structure on surface fluxes and climate.

259 Soil substrate explained variation, with deeper roots on

260 r its benefits reducing evaporation from the soil surface early in the season.

261 % of the Zn input from OW accumulated in the soil surface layer, (iii) Zn uptake by lettuce increased

262 rvae in apricot (Prunus armeniaca) fruits on soil surface with high mortality rate at 50 and 100 IJs

263 riving in the rhizosphere, the thin layer of soil surrounding plant roots, plays a critical role in p

264 We describe how repeat soil surveys are used to estimate changes in SOC over ti

265 ions requires infection of the root hairs by soil symbiotic bacteria, collectively referred to as rhi

266 nd efficient design of biopolymer stabilized soil systems.

267 otential abiotic and biotic drivers of the F(soil)-T hysteresis.

268 peratures and under conditions where we held soil temperature near constant.

269 We continuously monitored soil temperature, moisture, and CO(2) for a three-year p

270 of soil CO(2) efflux being out of sync with soil temperature.

271 We found that warming soil temperatures and decreasing winter length have oppo

272 xperiments under normal, fluctuating diurnal soil temperatures and under conditions where we held soi

273 al rooting depths varied across gradients in soil texture and rainfall.

274 and leaching of radioactive contaminants in soils that are nutrient deficient, a key factor that sho

275 High plant diversity resulted in soils that were dominated by fungi and associated soil b

276 Across all soils, the K(d) values of all short-chain PFASs (<=5 -CF

277 els), and improve penetrability of hard, dry soils (thick roots with a larger proportion of stele, an

278 ised of three steps: (i) preconditioning the soil to increase the sodium adsorption ratio, (ii) extra

279 ant overestimation of overall C release from soil to the atmosphere.

280 ces in the soil microbiome due to antecedent soil treatment additionally influence denitrification.

281 Juices from the pomegranates grown on two soil types had total analyzed phenolics ranging from 438

282 from 206 sites covering different forest and soil types in Europe and China.

283 es covering 3 climatic zones and 5 different soil types.

284 trategies, were grown in irrigated synthetic soil under semiarid conditions with gravimetric moisture

285 When soil volumetric water content significantly decreased in

286 of the initial PFAS contamination on GAC or soil was emitted as PFAS in the quantifiable analytical

287 a higher cover of asbestos roofs and exposed soil was positively associated with the presence of adul

288 particular RAF in both roots and thaw front soil was positively correlated with (15) N recovered in

289 Strategies for deep soil water acquisition (WA(deep) ) are critical to a spe

290 leaf area index, harvest index and in-season soil water content from 2-year experiments in each count

291 g biophysical photosynthetic limitation when soil water is scarce.

292 feedback among exp(H), species turnover, and soil water potential.

293 ion, we tested the hypothesis that increased soil water storage and transport resulting from cultivat

294 Soil water storage capacity was also an important risk f

295 draulic behavior was explored in relation to soil water supply, atmospheric demand and temperature.

296 mediated natural soils and Pb-mineral spiked soils were reduced by >90% relative to Pb RBA for U soil

297 Soils were sampled from intact, degraded and restored al

298 ere reduced by >90% relative to Pb RBA for U soils, which is substantially more effective than other

299 roperties is essential for understanding how soils will respond to land management practices and glob

300 We treated two soils with anthropogenic Pb contamination and samples of