ライフサイエンスコーパス: soil water

1 processes such as sorption or dissolution in soil water.

2 n soil bacterial communities are mediated by soil water.

3 of both enhanced carbon supply and increased soil water.

4 ble implications for the reservoir of stored soil water.

5 ason when plants are allowed to redistribute soil water.

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

7 spheric demand and conservation of available soil water.

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

9 transpiration rates, thus reducing available soil water.

10 ymatic-mediated phosphate equilibration with soil-water.

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

46 Soil water availability represents one of the most impor

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

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

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

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

51 proximal environmental conditions related to soil water availability.

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

68 Soil water conditions were more useful for understanding

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

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

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

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

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

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

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

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

77 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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

113 aliana results in enhanced performance under soil water deficits.

114 phenotypically similar responses to various soil water deficits.

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

142 plant water savings and consequent available soil water increases.

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

193 future trajectories of important climate and soil water variables.

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

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

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