ライフサイエンスコーパス: soil water

1 spheric demand and conservation of available soil water.

2 lds' hypothesis based on isotope profiles of soil water.

3 ), and despite the fact that warming reduced soil water.

4 transpiration rates, thus reducing available soil water.

5 processes such as sorption or dissolution in soil water.

6 n soil bacterial communities are mediated by soil water.

7 of both enhanced carbon supply and increased soil water.

8 ble implications for the reservoir of stored soil water.

9 ason when plants are allowed to redistribute soil water.

10 nutrient concentrations and availability of soil water.

11 ymatic-mediated phosphate equilibration with soil-water.

12 arbon dioxide in the partly closed system of soil waters.

13 significant increase in the availability of soil water (11%) was observed under elevated CO2 treatme

14 tant in explaining grass cover, collectively soil water accounted for 40-60% of the total explained v

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

16 lationship, soot-water and sediment-water or soil-water adsorption coefficients of HOCs of interest (

17 spike-recovery experiments with equilibrated soil-water-AFFF and analytical standards.

18 and light-use efficiency (Q) as functions of soil water, air temperature, vapor pressure deficit, veg

19 Chemical pollution of soil, water, air and food is a major environmental threa

20 For both microhabitats, antecedent soil water and Asat significantly affected Rsoil , but R

21 Trees utilized deep soil water and avoided strongly negative water potential

22 cover type, phenological period, antecedent soil water and biological inertia (i.e. the influence of

23 isk that too much early growth might deplete soil water and lead to more severe terminal drought stre

24 WHCNS gave better estimations of soil water and N dynamics, dry matter accumulation and N

25 uropean International Conference on Modeling Soil Water and N Dynamics.

26 Soil water and nutrient availability are key drivers of

27 The effects of soil water and nutrient availability on photosynthesis s

28 ld be largely attributable to the changes in soil water and nutrient availability.

29 than indirectly through nano-TiO2 affecting soil water and organic matter pools.

30 ccounting for the effects of plant-available soil water and other site-specific characteristics might

31 nderstanding A. fruticosa plants response to soil water and salt stress is essential for water irriga

32 quantified to determine the distribution of soil water and soil nitrate content.

33 trategies to tolerate limited access to deep soil water and stressful leaf environments.

34 Soil, water and food supply composition data have been c

35 cts with past environmental (e.g. antecedent soil water) and biological (e.g. biological inertia) fac

36 ncorporated effects of antecedent exogenous (soil water) and endogenous (Asat ) conditions.

37 ared to IRMS across 136 samples of xylem and soil water, and a set of ethanol- and methanol-water mix

38 ven changes in storage of water as snowpack, soil water, and ground water; storage in ice sheets and

39 With field data on rainfall, soil water, and leaf and canopy responses, we tested whe

40 exchange between bound (immobile) and mobile soil water, and whether there is isotope fractionation d

41 low-frequency variability of precipitation, soil water, and wildfire probabilities in close agreemen

42 -Gangetic plains, issues of deterioration in soil, water, and environment quality coupled with low pr

43 r of studies have identified GBH residues in soil, water, and even human food that may expose nontarg

44 s result in simulated concentrations in air, soil, water, and foliage that tend to fall close to or b

45 agricultural to human clinical settings via soil, water, and food.

46 milk fingerprint with those corresponding to soil, water, and forage.

47 ood, produced on less land, while conserving soil, water, and genetic resources.

48 Fluoride ion, ubiquitous in soil, water, and marine environments, is a chronic threa

49 lar concern, as plants closely interact with soil, water, and the atmosphere, and constitute one of t

50 le gram-negative bacteria found naturally in soil, water, and the rhizosphere of plants.

51 saprophytic bacterium commonly isolated from soil, water, and the surfaces and tissues of plants and

52 food supply chains and harmonize nutrients, soil, water, and waste management in different urban env

53 terest in the presence of these compounds in soils, water, and food.

54 This research integrates the Soil Water Assessment Tool (SWAT) watershed model and th

55 Climate change will both directly impact soil water availability and change plant biomass, with r

56 ps that account for the spatial variation in soil water availability and soil fertility as well as by

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

58 rgent ecotypes in response to differences in soil water availability between habitats.

59 Climate change will result in reduced soil water availability in much of the world either due

60 Vegetation change will mostly exacerbate low soil water availability in regions already expected to s

61 rylands, it is suggested that the additional soil water availability is a likely driver of observed i

62 e most apparent during the cool season; when soil water availability is projected to increase in nort

63 indirectly affect soil bacteria by changing soil water availability or other properties.

64 Soil water availability represents one of the most impor

65 Both crop yield and soil water availability required 15 years or longer to g

66 ecause dryland ecosystems depend directly on soil water availability that may become increasingly lim

67 g summer drought, we slightly augmented deep soil water availability to 14 HL+ treatment plants throu

68 sponses to atmospheric moisture demand D and soil water availability W, but the timescales of influen

69 at g(night) and E(night) would decrease when soil water availability was limited, and results from al

70 of continuous no-till agriculture on yield, soil water availability, and N(2) O fluxes.

71 ecies richness was controlled by climate and soil water availability, vegetation carbon storage was s

72 the amount and pattern of precipitation and soil water availability, which will directly affect plan

73 mate change-induced changes in vegetation on soil water availability.

74 eased sensitivity of root tips to decreasing soil water availability.

75 predisposition and/or response to changes in soil water availability.

76 proximal environmental conditions related to soil water availability.

77 not enhance NPP at a given L, regardless of soil water availability.

78 photosynthesis and net ecosystem exchange to soil-water availability and of the increased temperature

79 Thus in adapting to low soil-water availability, acetyl-DAP could refrain stomat

80 or 59 tree species in the western US along a soil water balance gradient and found high variability i

81 Projected climate scenarios are then used in Soil Water Balance groundwater infiltration simulations

82 ined model of SUHI coupled with a stochastic soil water balance is developed to demonstrate that the

83 dominant vegetation, substrate type and age, soil water balance, and disturbance history), allowing u

84 To compare the soil water balance, yield and water use efficiency (WUE)

85 Thus, PM is sustainable with respect to soil water balance.

86 parameters covering physical, environmental, soil, water, bio-climatic and disturbance aspects were c

87 regulating the feedback of vegetation on the soil water budget of salt-affected basins.

88 ctance in P. smithii, contributing to higher soil water, but not in L. dalmatica.

89 proxy for soil-bound water as well as total soil water by cryogenic distillation.

90 ell-watered conditions: the former conserved soil water by limiting maximum stomatal conductance per

91 nly from the dissolution of rock minerals by soil water carbon dioxide, a process called chemical wea

92 Results show that the soil water change of dryland spring maize was as deep as

93 Following incubation, the soil water characteristics, organic matter, total carbon

94 l period (10,000-15,000 yr ago), as shown by soil water chloride accumulations.

95 Discharge, and simulated riparian soil water concentrations profiles, represented by two c

96 AFs normalized to soil-water concentrations increased with chain length fo

97 Soil water conditions were more useful for understanding

98 escription of this process together with the soil water conditions.

99 t to uncertainty in predicted NPP were plant-soil water conductance and growth respiration, both unob

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

101 tures and the oxygen isotope compositions of soil waters, constrained by measurements of abundances o

102 aphic conditions, on global dry lands, where soil-water consumption impacts can be critical.

103 to provide a framework for assessing direct soil-water consumption, also termed green water in the l

104 in concert with a significant enhancement in soil water content (p = 0.0003) at intermediate hillslop

105 ap flow displayed a strong relationship with soil water content (SWC) (positive) and soil electrical

106 Both low soil water content (SWC) and high atmospheric dryness (v

107 with antecedent soil conditions [e.g., past soil water content (SWC) and temperature (SoilT)] and ab

108 Alternatively, warming-induced reductions in soil water content (SWC) can also decrease earthworm per

109 ns of isoprene based on leaf temperature and soil water content (SWC) were incorporated into current

110 hment of air to 600 p.p.m.v. CO(2) increased soil water content (SWC), 1.5/3.0 degrees C day/night wa

111 -term observations of O(3) mixing ratios and soil water content (SWC), we implemented empirical droug

112 measured leaf area index (L) and volumetric soil water content (theta) on a co-located spatial grid

113 r profiler (SWaP), which can determine local soil water content (theta) with a precision of 6.10(-5)

114 sed stomatal conductance (gs ) and increased soil water content (VSWC ) and second, through increased

115 ed on temperature alone assuming nonlimiting soil water content - by ca. 0.7% per 1.0% reduction in r

116 traits, spatially-distributed soil texture, soil water content and canopy temperature) were used to

117 e length of the border or furrow is weak for soil water content and is moderate for nitrate content,

118 B. pseudomallei was associated with a high soil water content and low total nitrogen, carbon and or

119 f belowground plant activity to increases in soil water content and N have shown inconsistent pattern

120 r seasonal pattern explained by temperature, soil water content and sap flux.

121 gate the responses of beta (and thus chi) to soil water content and suction across seed plant groups,

122 oxide (N2 O) fluxes to (i) temperature, (ii) soil water content as percent water holding capacity (%W

123 Interannually, low soil water content decreased annual Fsoil from potential

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

125 d + DMPP) were assayed under two contrasting soil water content levels (40% and 80% of water filled p

126 km south-north transect was established and soil water content of the 0-5 m depth soil layer repeate

127 d thus the soil hydraulic parameters and the soil water content signals we observe.

128 eta-analytic techniques were used to compare soil water content under ambient and elevated CO2 treatm

129 Soil water content was adjusted at an early stage of pla

130 CCs and REFs, but the groundwater table and soil water content were significantly higher at CCs than

131 measure the RWU and redistribution of sandy-soil water content with unprecedented precision.

132 quantified that after 15 months of depleted soil water content, >90% of the dominant, overstory tree

133 At a 40 cm depth, soil water content, air humidity, and atmospheric pressu

134 antity and quality, vapour pressure deficit, soil water content, and CO2 concentration are detected b

135 ted with greater community biomass and lower soil water content, and driven by the loss of species ch

136 rent drought algorithms (i.e., a function of soil water content, of soil water supply to demand ratio

137 cipitation regime significantly lowered mean soil water content, overall this plant community was rem

138 due attributes, i.e., soil pH, soil texture, soil water content, residue C and N input, and residue C

139 Simulated soil water content, soil nitrate concentrations, crop dr

140 tween the Bowen ratio Bo=Hs/LE and root-zone soil water content, suggesting that young/mature pines e

141 may significantly contribute to variation in soil water content, thereby influencing ecosystem proces

142 well as fundamental soil properties such as soil water content, water infiltration, nutrient status,

143 cing rapid changes in evaporative demand and soil water content, which affect their water status and

144 O2 concentration, vapor pressure deficit and soil water content.

145 ve to soil moisture variability than to mean soil water content.

146 vironments where production relies on stored soil water content.

147 nspiration in the UMRB by approximately +2%, soil-water content by about -2%, and discharge to stream

148 osphorus loadings in streams) and resources (soil-water content, evapotranspiration, and runoff) unde

149 sample varies significantly depending on the soil-water content, which is spatially and temporally va

150 gh altitudes (2100 m a.s.l.) due to improved soil water contents, with the exception of alpha-tocophe

151 efficiency of the DMPP both at low and high soil water contents.

152 in soils can increase P transfers across the soil-water continuum that impair aquatic ecosystem funct

153 especially under abiotic constraints such as soil water deficit (drought [D]) and high temperature (h

154 The responses of growth to soil water deficit and evaporative demand share an appre

155 eir midday leaf water potential (PsiM) under soil water deficit by closing their stomata, anisohydric

156 Soil water deficit can reduce plant survival, and is lik

157 A comparative transcriptome analysis of soil water deficit drought stress treatments revealed th

158 For this purpose, progressing soil water deficit is communicated from roots to shoots.

159 ened for 2 y under well-watered and moderate soil water deficit scenarios.

160 hanced recovery of plants from an episode of soil water deficit stress.

161 environments in the glasshouse, contrasting soil water deficit, elevated temperature and their inter

162 ld platform with contrasting temperature and soil water deficit, we determined the periods of sensiti

163 During dry periods, soil-water deficit can limit evapotranspiration, leading

164 phenotypically similar responses to various soil water deficits.

165 aliana results in enhanced performance under soil water deficits.

166 leads to raising transpiration rate (TR) and soil-water demand, risking productivity penalties.

167 New modules include: soil water-dependent water uptake and xylem flow; tiller

168 on, land competition for food production and soil-water depletion challenge the longevity of this car

169 he root network appears to be independent of soil water distribution or water demand.

170 ss whether the scaling laws are invariant to soil water distribution.

171 properties showed some correlations with the soil-water distribution coefficient (K(d)).

172 ining raw exudates had a significantly lower soil-water distribution coefficient (Kd) than slurries w

173 related with soil organic matter content and soil-water distribution coefficients, and was inhibited

174 ven if the feedback mechanisms and resulting soil-water distributions are different, as we indeed fou

175 erage low quarter distribution uniformity of soil water (DU(lqW)) was 96.34, there was a significant

176 istic patterns of canopy water potential and soil water dynamics at the studied sites.

177 where and the degree to which incorporating soil water dynamics enhances our ability to understand t

178 Agricultural management practices influence soil water dynamics, as well as carbon cycling by changi

179 and temporal distribution characteristics of soil water, electrical conductivity, and nitrate.

180 red nanoparticle (ENP) fate and transport in soil-water environments is important for the evaluation

181 exist as mixtures with other metal oxides in soil-water environments; however, information is only av

182 r determination of MTBE in water samples and soil water extracts.

183 ng) and 3-kDa filtered (nearly colloid-free) soil-water extracts from Andisols and Oxisols.

184 The results indicate that soil water filled pore space (WFPS) is the primary facto

185 t and stimulatory effects occurred at 60-90% soil water-filled pore space and soil pH 7.1-7.8.

186 , maintaining dry soil conditions and upward soil water flow since the last glacial period (10,000-15

187 mperature accompanied by a shift in paths of soil water flow within the watershed, but this effect ex

188 or millennia can rapidly adjust to increased soil water flows.

189 ultiple industrial chemicals occur from air, soil, water, food, and products in our workplaces, schoo

190 sis (GPA) demonstrated the consensus between soil, water, forage and milk, in addition to differences

191 limitation and inhibited microbial growth at soil water freezing points compared to warmer temperatur

192 ion (HR), the nocturnal vertical transfer of soil water from moister to drier regions in the soil pro

193 us organic compounds, thoroughly tested with soil-water from a C3-C4 vegetation change experiment, an

194 Here, we present the first soil water-growth response function and parameter range

195 An integrated model WHCNS (soil Water Heat Carbon Nitrogen Simulator) was developed

196 ential CH4 oxidation rates and soil texture, soil water holding capacity, and dissolved organic carbo

197 eria (MOB) is controlled by soil texture and soil water holding capacity, both of which limit the dif

198 The endpoint soil water holding had been reported previously as not c

199 Under water deficit (50% of soil water-holding capacity), total root length was stro

200 Here we analyse soil water in basaltic soils across the Hawaiian islands

201 bution analysis showed that the variation of soil water in the 0-60 cm soil layer was larger than tha

202 by sustaining river base-flow and root-zone soil water in the absence of rain, but little is known a

203 model that accounts for both competition for soil water in the shallow soil and fire-induced disturba

204 mended as the minimum depth when measure the soil water in this region.

205 plicit representation of growth responses to soil water in vegetation models.

206 omes mainly from its interaction with system soil/water in the reducing conditions typical of paddy f

207 plant water savings and consequent available soil water increases.

208 Average near-saturated soil water infiltration rates were 12.6, 14.9, and 6.0 c

209 uch as the distribution of components at the soil-water interface and conformational information.

210 r lipid heads and carbohydrates dominate the soil-water interface while lignin and microbes are arran

211 ding the influence of the contaminant on the soil-water interface, specific biological interactions,

212 The osmolality of rhizosphere soil water is expected to be elevated in relation to bul

213 py (IRMS), but its use in studying plant and soil water is limited by the spectral interference cause

214 as temperature limitation diminishes, higher soil water is needed to support increased vegetation act

215 g biophysical photosynthetic limitation when soil water is scarce.

216 ated with R. ponticum were identified in any soil water leachates, and soil leachates from cleared si

217 under both [CO(2)] levels (depending on the soil water level), while also decreasing the grain yield

218 When plants encounter soil water logging or flooding, roots are the first orga

219 and this discrimination is a function of the soil water loss and soil type.

220 Greatest soil water loss was observed for the experiment with the

221 ochar benefits, such as crop yield increase, soil water management, and N2O reductions.

222 eatment factors (elevated CO2 , warming, and soil water manipulation) and their interactions with ant

223 Soil water metrics, including the number of dry days and

224 imate and soil properties with a mechanistic soil water model to explain temporal fluctuations in per

225 Thus, soil water movement potential of NTMI2 was lowest during

226 Neither vertical infiltration of soil water nor the upwelling of deep fluids was the majo

227 in late winter, when the soil was frozen and soil water not available for the trees.

228 Root signals are thought to reflect soil water, nutrient, and mechanical attributes, as sens

229 effect on the uniformity and distribution of soil water or nitrate.

230 Alternatively, soil water or other environmental factors may mediate EN

231 The soil water, or the "soil solution," contains silicon, ma

232 expected to be elevated in relation to bulk-soil water osmolality as a result of the exclusion of so

233 The aim of this study was to assess the soil-water partitioning behavior of a wider range of per

234 Soil-water partitioning coefficients (log K(d) values) o

235 Octanol-water (Dow(pH)) and soil-water partitioning were measured at several pH valu

236 e has been detected recently in a variety of soils, waters, plants, and food products at levels that

237 ace water is derived from the plant-accessed soil water pool.

238 ce the accessibility of shallower vs. deeper soil water pools.

239 em growth (air temperature > 2 degrees C and soil water potential > -0.6 MPa).

240 o vapor pressure difference (D) at night and soil water potential (Psi(soil)) during the day, Great B

241 ), and canopy xylem pressure (Pcanopy ) from soil water potential (Psoil ) and vapor pressure deficit

242 n single hyphae, resulting in an increase in soil water potential after 72 h.

243 etabolism in response to drought and reduced soil water potential has impeded efforts to improve stre

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

245 Faced with declining soil-water potential, plants synthesize abscisic acid (A

246 he discrepancy between isotope ratios of the soil water profile and other water compartments in the h

247 Here, we present a sensor, the soil water profiler (SWaP), which can determine local so

248 rong sensitivities of rooting depth to local soil water profiles determined by precipitation infiltra

249 We used a coupled model (Hydrus-1D) for soil water propagation, heat transfer, and diffusive gas

250 2) , CH(4) and dissolved organic carbon) and soil-water quality characteristics in an intact and a de

251 ferent from the water that supplies parts of soil water recharge and plant transpiration.

252 served clear changes in plant-driven RWU and soil water redistribution profiles.

253 lant water uptake, and distinguishes it from soil water redistribution via soil pores and roots.

254 The warm spring also depleted soil water resources earlier, and thus exacerbated water

255 es in the first hour is mainly a function of soil water retention and % Corg, at longer times it is a

256 However, it is usually difficult to measure soil water retention characteristics.

257 y (FBD) concept was presented for estimating soil water retention curves.

258 Soil water retention determines plant water availability

259 Drought tolerance and soil water retention were assessed using Arabidopsis epi

260 r the determination of ammonia in sewage and soil water samples.

261 ect effects (e.g. increased leaf area index, soil water savings) may amplify or dampen the direct eff

262 d microscopy, mineral particles derived from soil-water show biomimetic morphologies, including large

263 n of beta as a simple, empirical function of soil water significantly improves chi predictions by up

264 ecies, which had lower requirements for deep soil water, soil nitrate, and light, were strong competi

265 It included five main modules: soil water, soil temperature, soil carbon (C), soil N, a

266 Our results highlight the importance of soil water status on stomatal functions and plant water-

267 and water uptake capacity and we found that soil water status surrounding root tips differed between

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

269 Soil water storage capacity was also an important risk f

270 nse to elevated winter precipitation reduced soil water storage to half of that in a nonvegetated lys

271 yer of cinders, enhancing crop access to the soil water stored below the intact cinders.

272 ore effective than grasses for reaching deep soil water stores that can be enhanced under elevated CO

273 Moreover, in the absence of soil water stress (REW(0-40 cm) > 0.4), A. fruticosa can

274 , our results suggest that in the absence of soil water stress (REW(0-40 cm) > 0.4), the nocturnal sa

275 driven by an external environmental factor, 'soil water stress' and consequently by a constant or dec

276 Under soil water stress, nocturnal sap flow is mainly used to

277 to examine the acclimated response of chi to soil water stress.

278 ulic functions into the model to account for soil water stress.

279 (i.e., a function of soil water content, of soil water supply to demand ratio, and of actual to pote

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

281 the balance between energy availability and soil water supply.

282 l freshwater, or 0.001% of all global water, soil water supports all terrestrial biological life.

283 ed by germinating zygotes of Chara in either soil water (SW) medium or artificial pond water (APW) me

284 ith silicate mineral weathering to enter the soil-water system and to produce pedogenic calcium carbo

285 PFASs of various charge states in saturated soil-water systems and assess critical influencing facto

286 ution was observed in both octanol-water and soil-water systems particularly for BPS and BPAF, which

287 organisms play in the transport of (129)I in soil-water systems, bacteria isolated from subsurface se

288 In a soil-water-TCE system, NZVI together with AC EMF thermal

289 responses of angiosperms and gymnosperms to soil water tend to converge, consistent with the optimal

290 eoric water line, suggesting that plants use soil water that does not itself contribute to groundwate

291 ameters to represent seasonality in riparian soil water THg and MeHg concentrations profiles.

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

293 g the follow up from environmental matrixes (soil + water) to dairy products through the food web (fo

294 ixation in response to exogenous ureides and soil-water treatments for the cultivars Jackson and KS48

295 caused by an earlier or greater depletion of soil water under e[CO(2) ] and the mechanisms responsibl

296 future trajectories of important climate and soil water variables.

297 Climate Experiment satellites and simulated soil-water variations from a data-integrating hydrologic

298 d chemical contrasts in shallow water (e.g., soil water) versus deep waters (e.g., groundwater), indu

299 had little effect on B. tectorum invasion or soil water, while reducing soil and plant nitrogen (N).

300 logic connectivity of bound, plant-available soil waters with more mobile surface waters.