ライフサイエンスコーパス: soil moisture

1 d the enhanced vegetation index (a proxy for soil moisture).

2 armer air temperatures, and higher levels of soil moisture.

3 ern Mediterranean, adding to the drawdown of soil moisture.

4 ities and positive or nonlinear responses to soil moisture.

5 a resulting voltage shift in the presence of soil moisture.

6 linearly with fertilization, temperature and soil moisture.

7 naturally fluctuating evaporative demand and soil moisture.

8 ments with respect to temperature, light and soil moisture.

9 es are increasingly unable to utilize pulsed soil moisture.

10 drier soils, and/or mesoscale variability in soil moisture.

11 re and humidity, which in turn feeds back on soil moisture.

12 e spring snowpack and late spring and summer soil moisture.

13 s for further height growth, even with ample soil moisture.

14 ovide a mechanism for the unexpected rise in soil moisture.

15 iomass, with resulting indirect feedbacks on soil moisture.

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

17 l surface temperature, available soil N, and soil moisture.

18 y the response of photosynthesis to changing soil moisture.

19 N sink, limiting NO emissions under optimal soil moisture.

20 eflecting greater differences in soil pH and soil moisture.

21 lowground biomass, MBC, soil temperature and soil moisture.

22 ronmental signals, including temperature and soil moisture.

23 cm) promoted increased ALTs, whereas deeper soil moisture (11-16 cm) acted to modify the impact of t

24 tterns of water demand reflected in variable soil moisture across space and time.

25 mites and nematodes increased with available soil moisture across the CEMG, within individual ecosyst

26 Yet there is considerable uncertainty in how soil moisture affects convective storms across the world

27 e report the first potentiometric sensor for soil moisture analysis by bringing in the concept of Gal

28 g aberration conditions often encountered in soil moisture analysis.

29 ly reduced levels of transpiration, conserve soil moisture and are highly drought tolerant but show l

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

31 hile, constraining the immediate increase in soil moisture and drying out over the following months,

32 opical drylands is well constrained, whereas soil moisture and ecological droughts, which drive veget

33 pensated by the accelerated drying trends of soil moisture and enhanced ET, leading to an acceleratio

34 t saturating functions of enzyme activity to soil moisture and extracted half saturation and maximum

35 ntiguous United States using remotely sensed soil moisture and gauge-based precipitation observations

36 d CO(2) treatment interacted with antecedent soil moisture and had significantly greater effects on f

37 h droughts" accompanied by extreme heat, low soil moisture and high evapotranspiration (ET), occurred

38 ollowed by the contributions from decreasing soil moisture and increasing ET.

39 nd N loss in the early decomposition stages, soil moisture and legacy effects of initial differences

40 d magnetite in forest soils due to increased soil moisture and lower pH.

41 usality to estimate the relationship between soil moisture and occurrence of subsequent precipitation

42 res but the degree of response may depend on soil moisture and other local factors.

43 ed the stomatal conductance, which preserved soil moisture and plant fitness under drought.

44 quantity, increased temporal variability in soil moisture and plant species diversity.

45 servational analysis of the coupling between soil moisture and precipitation.

46 r Mississippi basin that gradually builds up soil moisture and reduces the basin's infiltration capac

47 s in the amount of precipitation reduced the soil moisture and Rs by -12% and -6%, respectively, but

48 Overall, our synthesis suggests that soil moisture and Rs tend to be more sensitive to increa

49 rmalized to 28% below the ambient level, the soil moisture and Rs values decreased by an average of -

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

51 This phenomenon rapidly increased soil moisture and stimulated microbial carbon (C) cyclin

52 ient were most clearly related to changes in soil moisture and temperature.

53 CH4 and DIC at three depths in the soil, and soil moisture and temperature.

54 agasta sauropods were specifically using the soil moisture and thermoradiance to incubate their eggs,

55 gions, where surface fluxes are sensitive to soil moisture, and convective events are frequent.

56 -year record of tree growth (n = 200 trees), soil moisture, and ecosystem C balance at the Morgan-Mon

57 duce soil erosion, conserve energy, increase soil moisture, and increase crop yields.

58 ation, lowering soil temperature, increasing soil moisture, and leaving soil undisturbed.

59 luxes, fine root biomass, microbial biomass, soil moisture, and nutrient fluxes.

60 spiration response to event size, antecedent soil moisture, and post-event vapor pressure deficit.

61 fference Vegetation Index (NDVI), antecedent soil moisture, and temperature but these models provided

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

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

64 e state, stomatal conductance, soil texture, soil moisture, and water table depth.

65 ypothesis that in continental regions summer soil moisture anomalies affect the probability of occurr

66 in the Colorado River Basin, as judged from soil moisture anomalies and other hydrological measures.

67 on Earth where precipitation is affected by soil moisture anomalies during Northern Hemisphere summe

68 l variability in precipitation, we find that soil moisture anomalies significantly influence rainfall

69 onset of warm temperatures and depletion of soil moisture are all likely to occur earlier in the yea

70 While increases in soil moisture are generally associated with increased mi

71 While increasing temperatures and altered soil moisture arising from climate change in the next 50

72 arrived during assays and increased surface soil moisture around all plants.

73 ong our ER models revealed the importance of soil moisture as a driving variable, likely through its

74 d longleaf pine savannas along a gradient of soil moisture availability (mesic, intermediate and xeri

75 On the other hand, reduced soil moisture availability may limit evapotranspiration

76 totrophic respiration; and the impact of low soil moisture availability on plant processes.

77 r future climate change scenarios is reduced soil moisture availability.

78 sed substantially after >10 years of reduced soil moisture availability.

79 determine community responses to changes in soil moisture availability.

80 l be conditional on topographically mediated soil moisture availability; (ii) in extreme drought year

81 mid-latitudes is determined by the amount of soil moisture available to plants with the greatest warm

82 Vegetation and soil moisture become increasingly homogenized and couple

83 Grazing had no effect on soil moisture, but wetter soils retarded root decomposit

84 a pseudoacacia seedlings under the same mean soil moisture, but with different drought frequency caus

85 periment, simulated warming increased spring soil moisture by 5-10% under both ambient and elevated C

86 The increase in soil moisture by hydraulic redistribution significantly

87 gnitude of microbial functional responses to soil moisture can be predicted from historical climate a

88 ABSTARCT: Constraints on soil moisture can guide agricultural practices, act as i

89 Soil moisture can influence the development of convectiv

90 Based on in-situ measurements of soil moisture collected in agricultural plots during 198

91 ore prone to wilting when grown with limited soil moisture compared with wild-type plants.

92 athogen metabolic rates; and changing spring soil moisture conditions and thus pathogen growth rates

93 e change on vegetation when assessing future soil moisture conditions in water-limited ecosystems.

94 k (Quercus robur) saplings under wet and dry soil moisture conditions to (18) O-depleted water vapour

95 le wetting patterns interact with antecedent soil moisture conditions to alter pore-scale, core-scale

96 Then the initial soil moisture conditions were restored, and a mixed comm

97 d from higher subsurface temperatures, lower soil moisture conditions, or nutritionally deficient veg

98 y exist between precipitation and antecedent soil moisture conditions.

99 Soil moisture constrains the activity of decomposer soil

100 of short-term C mineralization than current soil moisture content in these soils.

101 Results showed that (a) change in soil moisture content was linearly correlated to change

102 r temperatures and evaporation rates, higher soil moisture content, and received more frequent fog dr

103 Soil moisture content, soil organic carbon, soil availab

104 mined mainly by microbial biomass carbon and soil moisture content.

105 al traits and genes that affect responses to soil moisture deficit in the TSUxKAS mapping population

106 Following soil moisture deficit that is maintained for several yea

107 following more than 12 years of experimental soil moisture deficit, via a through-fall exclusion expe

108 As the climate continues to warm and soil moisture deficits accumulate beyond historical leve

109 maize ET (7-11%; P < 0.01) along with lesser soil moisture depletion, while H increased (25-30 W m(-2

110 en in the presence of clouds, of proxies for soil moisture derived from the amplitude and phase conte

111 escribes the primary differences between the soil moisture desorption and the adsorption processes by

112 al heat flux, relative humidity, wind speed, soil moisture differences and air temperature; the relat

113 and magnitude of soil microbial response to soil moisture due to historical climate may be remarkabl

114 n yield, probably due to the preservation of soil moisture during drought periods.

115 due to the extreme snowfall inducing higher soil moisture during spring thaw.

116 An enhanced dependence of forest growth on soil moisture during the late-20th century coincides wit

117 stion, I coupled a plant uptake model with a soil moisture dynamics model to explore the environmenta

118 esistivity imaging (ERI) was used to monitor soil moisture dynamics to a depth of 9 m in a grassland,

119 two preferential states may arise in summer soil moisture dynamics, which thus tend to remain locked

120 th lowered resilience resulting in shifts in soil moisture dynamics.

121 vels but also the yield variability, whereas soil moisture enhancements improved the yield stability.

122 ater and light within a continuously varying soil moisture environment.

123 le to penetrate the region and overwhelm the soil-moisture feedback.

124 , richness, and diversity), temperature, and soil moisture for 3 years.

125 tter polyphenols, decomposer communities and soil moisture for litter C and N loss at different stage

126 lter the soil environment through changes in soil moisture, frequently resulting in soil saturation,

127 hanging CO2, including direct use of P-E and soil moisture from ESMs, is needed to reduce uncertainti

128 find that calibrating models with parabolic soil moisture functions can improve predictive power ove

129 nteractions and biomass while manipulating a soil moisture gradient and reducing consumer pressure.

130 tween fitness and biofilm production along a soil moisture gradient.

131 t California with severely reduced snowpack, soil moisture, ground water, and reservoir stocks, but t

132 Predicted soil moisture, groundwater depth and leaf area index agr

133 By the time of the second peak, however, soil moisture had dropped to anomalously low levels in t

134 apor pressure deficit, and increased surface soil moisture in higher diversity communities.

135 e use dendroecology to elucidate the role of soil moisture in modifying the relationship between clim

136 er in rooting depth, with grasses exploiting soil moisture in shallow layers while trees have exclusi

137 mation on the spatio-temporal variability of soil moisture in the vadose zone is important to assess

138 n facilitated the efficient use of available soil moisture in wheat.

139 ances of mite and nematode trophic groups as soil moisture increased within individual ecosystems, wh

140 antly in response to deeper thaw and greater soil moisture induced by Soil warming.

141 ace properties, such as vegetation cover and soil moisture, influence the partitioning of radiative e

142 Soil moisture influences fluxes of heat and moisture ori

143 Because soil moisture integrates temperature and precipitation d

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

145 onditions (arid-humid) and limiting factors (soil moisture, leaf area, energy).

146 that summer precipitation and the resulting soil moisture level also strongly influenced the soil wa

147 Our results suggest that soil moisture limitation can offset the effect of warmin

148 summer drought due to lengthened periods of soil moisture limitation.

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

150 The lack of significant effects of eCO2 on soil moisture, microbial biomass, or activity suggests t

151 e a minimalist plant hydraulics model with a soil moisture model and, for the first time, translate r

152 idence supports our findings from historical soil moisture monitoring at a long-term upland hydrologi

153 growth of C(4) grasses in 2 of 3 years when soil moisture most limited plant productivity.

154 f environmental factors, including levels of soil moisture, nitrate, chloride, and labile organic car

155 ng numbers of added limiting soil resources (soil moisture, nitrogen, phosphorus and base cations), w

156 eristics of precipitation and the associated soil moisture on a spatially disaggregated framework.

157 there was a strong influence of rainfall and soil moisture on community composition at the species le

158 f land-atmosphere interaction (the impact of soil moisture on precipitation) have been limited by a l

159 ontrast, we find that a positive feedback of soil moisture on simulated precipitation does dominate i

160 biosphere models to represent the effects of soil moisture on stomatal conductance yielded unrealisti

161 ut this was not strongly linked to shifts in soil moisture or DOC.

162 t permafrost sites, to a greater degree than soil moisture or temperature could explain.

163 While DEA was highly correlated with soil moisture, organic matter, microbial biomass, and so

164 are improved and injection is deeper, and if soil moistures, organic amounts, and densities are great

165 Durations of depleted soil moisture over the historical record ranged from 4 t

166 ure-driven responses are further mediated by soil moisture, precipitation, and carbon supply and regi

167 les and influenced the temporal evolution of soil moisture profiles; and (c) juniper encroachment low

168 mmer of 1998 was strong and persistent, with soil moisture reaching levels comparable to those of the

169 Couplings between soil moisture, redox fluctuations, and lignin breakdown

170 The incorporation of soil moisture regenerated by precipitation, or green wat

171 and photosynthesis responses to contrasting soil moisture regimes was greater in RNAi than wild-type

172 sitivity of soil respiration under different soil moisture regimes.

173 irect and indirect climate change effects on soil moisture requires better understanding.

174 ive deficit, resulting in record low shallow soil moisture reserves.

175 A, using LSM-modeled and topography-mediated soil moisture, respectively.

176 , within individual ecosystems, increases in soil moisture resulted in decreases to nematode communit

177 ted moderate summer drought decreased winter soil moisture retention by ~10%.

178 and humidity increases enough to offset poor soil moisture retention, climate-related changes to prod

179 rmalized to 28% above the ambient level, the soil moisture, Rs, and the temperature sensitivity (Q10)

180 rough carbon assimilation) and indirect (via soil moisture savings due to stomatal closure, and chang

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

182 Unlike the state of the art soil moisture sensors, a signal derived from the propose

183 Watering increased season-average soil moisture similarly across sites.

184 icantly positively correlated with rainfall, soil moisture (SM), the carbon to nitrogen ratio (C/N ra

185 elastic Earth to increased winter loading of soil moisture, snow cover, and atmosphere.

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

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

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

189 stence of drought induced alternative stable soil moisture states (irreversible soil wetting) in upla

190 l crops, leading to significant reduction in soil-moisture storage and specific surface runoff.

191 hum resistance to premature senescence under soil moisture stress during the post-flowering period.

192 re nearly unresponsive to antecedent shallow soil moisture, suggesting reduced shallow absorbing root

193 well explained by a critical balance between soil moisture supply and atmospheric demand representing

194 other terrestrial water storage components (soil moisture, surface waters, snow, glaciers and biomas

195 Soil moisture, temperature, pH, carbon : nitrogen (C : N

196 These findings suggest that effects of soil moisture-temperature coupling are geographically mo

197 The reductions in soil moisture tended to be greater in more humid areas.

198 the annual plant community at all levels of soil moisture through reductions in microclimatic stress

199 Soil moisture, through changes in soil %O2 saturation, d

200 ests, due to higher sensitivity of grassland soil moisture to rainfall.

201 heterogeneity in three environmental factors-soil moisture, understory light, and conspecific neighbo

202 ic moisture demand and depleting the shallow soil moisture upon which aspens rely.

203 r harvesting contexts, which includes direct soil moisture uptake by plants and rainwater harvested a

204 mean wet season rainfall or landscape-scale soil moisture variability as controls on the structural

205 ere reduced, and ANPP was more responsive to soil moisture variability than to mean soil water conten

206 e, e.g. temperature, and land surface, e.g., soil moisture, variables as predictors of TOC concentrat

207 t demographic tradeoffs driven by short-term soil moisture variation act as a mechanism to allow mult

208 es of carbon exchange were more sensitive to soil moisture variation in grassland than shrubland, suc

209 draulics and topographic convergence-induced soil moisture variation to land surface models (LSM) can

210 predicting plant hydraulic safety loss from soil moisture was developed using field measurements and

211 Soil moisture was found to be a main factor in regulatin

212 Stomatal conductance was lower (-34%) and soil moisture was higher (up to 31%), consistent with re

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

214 respiration at all sites during months when soil moisture was not limiting.

215 Soil moisture was significantly higher in aspen stands a

216 High 2002 summer temperature and low shallow soil moisture were most associated with the spatial patt

217 iven by precipitation-induced changes in the soil moisture, whereas changes in the soil temperature h

218 We focus on respiration responses to soil moisture, which remain unresolved in ecosystem mode

219 although increased temperature and decreased soil moisture will act to reduce global crop yields by 2

220 icated that aspens generally utilize shallow soil moisture with little plasticity during drought stre

221 We argue that models should treat soil moisture within a three-dimensional framework empha

222 patterns occur along fine-scale gradients of soil moisture within four individual ecosystem types (me