ライフサイエンスコーパス: warm

1 of future climate as the Earth continues to warm.

2 ic Ice Sheet for different amounts of global warming.

3 where species richness mostly increases with warming.

4 ntly suggest continued increases with future warming.

5 grassland to either 5-8 or >50 years of soil warming.

6 e from residents than 3 degrees C of climate warming.

7 ikely to be especially vulnerable to climate warming.

8 nce on future strategies to mitigate climate warming.

9 ENSO variability under subsquent greenhouse warming.

10 Northeast US Shelf during a period of rapid warming.

11 abiotic processes are shifting earlier with warming.

12 es, a 4 degrees C warming, or an 8 degrees C warming.

13 nce, providing some compensation for climate warming.

14 a recorded the ice sheet's response to MIS11 warming.

15 nt effects, with a fall in excitability with warming.

16 ion may change in response to long-term soil warming.

17 ent of SOC in reducing SOC loss under global warming.

18 ore pronounced while abundance declines with warming.

19 a weakening of the SASM during abrupt arctic warming.

20 loss would trigger strong (about 5 K) global warming.

21 e generally predicted to be more affected by warming.

22 ver the next 50 years in response to climate warming.

23 ent under soil warming than under canopy air warming.

24 e surface, thus masking the relative El Nino warming.

25 ked lakes may be less impacted by subsequent warming.

26 in newly available habitat following climate warming.

27 epth in peatlands is responsive to prolonged warming.

28 long the soil profile reduces SOC loss under warming.

29 on by 8.3% (NEP, 22.25 Pg CO(2) /year) under warming.

30 ucial to determining vulnerability to global warming.

31 ; ~ 0.037 km(3)/year volume-change rate) and warming (0.3-0.4 degrees C/year).

32 Terrestrial N fixation was stimulated by warming (+152.7%), elevated CO(2) (+19.6%), and increase

33 a large range even at 2 degrees C of global warming (-196 +/- 117 PgC).

34 tivity, and chronically exposed as adults to warm (25 degrees C) normoxia, warm hypoxia (12 kPa O(2)

35 ve SOM decay is affected by predicted global warming (+4 degrees C), sea level changes (simulated by

36 d 90% when washed in cool (20 degrees C) and warm (50 degrees C) water, respectively.

37 When 5-Gd and 6-Gd are warmed above -15 degrees C, they reform Gd(II) complexes

38 pper thermal tolerance was also performed on warm-acclimated fish to test whether plasticity in the f

39 ore, the scope for plasticity resulting from warm acclimation decreased in the Up-selected lines.

40 However, this regulating service causes warming, acidification and deoxygenation of deep waters,

41 t would gradually vanish as the Indian Ocean warming acts to strengthen the Atlantic meridional overt

42 otic processes, yet we know little about how warming affects whole ecosystems.

43 shift in biological communities in favor of warm-affinity species (i.e., thermophilization).

44 Here we show that ocean acidification and warming, alone and in combination have significant adver

45 aticum accessions, Ain1 and Osl1, typical to warm and cold climates, respectively.

46 d from field experiments in northeast China (warm and cold regions) to study the effect of temperatur

47 lysis demonstrates that the magnitude of the warm and dry anomalies compounding in the recent two dec

48 g factors: (1) short exposures to moderately warm and humid environments; (2) active warm-up protocol

49 upted a cold and dry climate and generated a warm and wet period.

50 nd the variation in K(S) were highest in the warm and wet tropical regions, and lower in cold and dry

51 t estimation of whole-soil SOC changes under warming and additional NPP required to compensate such c

52 the ecosystem C and N cycling in response to warming and advances our capacity to predict terrestrial

53 lish a benchmark in the face of rapid Arctic warming and an intensifying hydrologic cycle, which will

54 isture deficit, appears to intensify surface warming and anticyclonic circulation anomalies, fueling

55 O) emissions from soil contribute to global warming and are in turn substantially affected by climat

56 is, implying that the synergistic impacts of warming and biodiversity loss on ecosystem functioning w

57 experiment to disentangle effects of climate warming and community diversity on plant species coloniz

58 he "hockey stick"-like change warns that the warming and drying concurrence is potentially irreversib

59 erature treatments, including a control, low warming and high warming treatment, and then measured re

60 odels, particularly in the context of global warming and increasing frequency of droughts.

61 opulations and support viable fisheries in a warming and increasingly unpredictable climate, coordina

62 Climate warming and landscape conversion may reduce the genetic

63 Amplification of warming and loss of perennial ice cover are set to drama

64 environmental stressors, including drought, warming and nutrient stress.

65 Sunbelt is driven by concurrent GHG-induced warming and population growth which, in tandem, could st

66 ng (p = .0178), whereas interactions between warming and rainfall reduction on the J(max25 degrees C)

67 were used to assess the influence of global warming and regional eutrophication, respectively, on th

68 s and applying different GHG metrics (global warming and temperature potentials) and time horizons (2

69 However, its feedbacks to climate warming and underlying microbial mechanisms are still po

70 ndon their traditional habitats due to ocean warming, and consequently either migrate further North o

71 An impinging warm anticyclonic eddy in July 2007 may have combined wi

72 differences in VOC emission responses in the warming Arctic, depending on the local vegetation cover

73 anic matter in permafrost are liberated in a warming Arctic.

74 We find that deformation and warming are highly correlated, and depending on the sign

75 e explored climatological drivers for Arctic warming as determinants of range expansion for two tempe

76 as one potential biological response to diel warming asymmetry.

77 monstrated by a divergent response of LAI to warming asymmetry.

78 Here we show that North America warmed at the rate of 0.02 degrees C/y.

79 bivores, highlighting the positive impact of warming autumns on population viability, offsetting the

80 are likely to be most susceptible to future warming because maladaptation occurs when beetles try to

81 s agreement targeting a limitation of global warming below 2 degrees C by 2100, and possibly below 1.

82 scenarios associated with differing rates of warming between hemispheres.

83 would lead to overestimation of emissions in warm biomes, underestimation in cold biomes, and likely

84 d length and cost of hospital stay, costs of warming blanket use, blood transfusions and antibiotics

85 the most abundant fungal skin inhabitant of warm-blooded animals and have been implicated in skin di

86 een such taxa, and to understand the role of warm-blooded animals as thermal ecosystem engineers.

87 in fish production with anthropogenic ocean warming, but how fish production equilibrates to warming

88 Species responses often lag behind climate warming, but the reasons for such lags remain largely un

89 ioeconomic hazard arising from anthropogenic warming, but the response of the largest component of Ea

90 ns an important negative feedback on climate warming, but the temporal dynamics of CFE remain unclear

91 ns such as the Arctic under sustained global warming, but with complex and not necessarily predictabl

92 reduced the average increase to 10%, as did warming by ca. 2 degrees C.

93 Arctic warming can influence tundra ecosystem function with con

94 and broad-scale kelp loss, and highlight how warming can make ecosystem boundaries unstable, forcing

95 the change in plant functional traits under warming climate, but studies on one key factor, snow cov

96 Under greenhouse warming, climate models project an increase in the frequ

97 is unlikely to be appropriate for high-CO(2) warm climates of the past, and the state dependency of E

98 low CO(2) Oligocene world (~300 to 700 ppm), warm climates similar to those of the late Eocene contin

99 ource for global sea-level rise under future warming conditions(1).

100 n in tropical forests is highly sensitive to warming, creating a potentially substantial positive fee

101 ely take far longer (centuries) than climate warming (decades), so in the short-term, tree reproducti

102 that was marked by abrupt northeast Pacific warming, declining temporal variance in the Aleutian Low

103 Interestingly, warming decreases 'drift' over time, and enhances homoge

104 roviding an approach for creating samples of warm dense matter with conditions not present on Earth.

105 Similarly, in the arid western US warming does not result in significant groundwater chang

106 a key response to climate warming, including warming driven by urban heat islands.

107 ers and three oaks along a transect spanning warm dry foothills (500 m above sea level) to cold wet t

108 staging and survival and productivity, with warm, dry conditions being the most favourable for produ

109 me at a cost of 0.3-0.5 degrees C additional warming due to the direct impact of aerosols.

110 dual species level and pooled into cold- and warm-edge assemblages-in a multi-decade time-series of t

111 edges shifted 0.47 degrees of latitude, and warm edges shifted only 0.28 degrees.

112 mperature isotherms to a greater degree than warm edges.

113 radiation, leading to a strong but uncertain warming effect on climate.

114 r subgrid-level analyses agree with observed warming effects only when the space-for-time assumption

115 jority still simulates its asymmetry between warm (El Nino) and cold (La Nina) phases very poorly.

116 se to multiple environmental change factors (warming, elevated carbon dioxide [CO(2) ], increased pre

117 aused by syn-rift decompression melting of a warm, enriched mantle.

118 imal mechanical disruption during digestion, warm enzymatic digestion using enzyme collagenase:NP act

119 peaked 2 wk later, coinciding with a second warming event with extreme R(onset) The epizootic lasted

120 Studies of warming events in the ocean have typically focused on th

121 To reveal the impact of past climate-warming events on the demographic history of an Arctic s

122 epizootic lasted ~2 mo, extending beyond the warming events through the consumption of pathogen-laden

123 tes, punctuated by speciation pulses, during warming events throughout the Phanerozoic and 2) that co

124 asia during the Late Pleistocene-to-Holocene warming events.

125 to find high-molecular-weight atmospheres on warm exoplanets orbiting M-stars, we should target world

126 Warming exponentially increased methane (CH(4)) emission

127 8 +/- 12%) and BAT (278 +/- 19%) compared to warm/fed animals.

128 By contrast, induced warming from volcanism mitigated the most extreme effect

129 and carbon monoxide mixture) from two global warming gases of carbon dioxide and methane via dry refo

130 DK but decreased PEPc activity compared with warm-grown plants.

131 electron transport, J(max) ) was reduced in warm-grown seedlings, correlating with reductions in lea

132 Global warming has greatly altered winter snowfall patterns, an

133 Here, we show that ongoing warming has strong, increasing effects on Arctic VOC emi

134 ture trends, often dubbed the North Atlantic warming hole (NAWH).

135 of this vast C bank could accelerate climate warming; however, the likelihood of this outcome remains

136 d as adults to warm (25 degrees C) normoxia, warm hypoxia (12 kPa O(2) ), cold (5 degrees C) normoxia

137 wind stress and has a potentially important warming impact on the extratropical ocean and climate.

138 tial (GWP) approaches to estimate the global warming impacts from municipal solid waste landfills.

139 tandard static approach to estimating global warming impacts may not accurately represent the global

140 acts may not accurately represent the global warming impacts of landfills.

141 past decade, the number of reports of ocean warming impacts on kelp forests has risen sharply.

142 ribution supports the necessary mediation of warming impacts to the general public.

143 ys (n = 5) were procured after 30 minutes of warm in situ ischemia by cross-clamping the renal arteri

144 Warming in the Arctic has been more apparent in the non-

145 Rapid warming in the Arctic is leading to widespread heterogen

146 rong links with temperature, continued ocean warming in the northeast Atlantic may reduce primary pro

147 id-Pliocene simulations, the higher rates of warming in the northern hemisphere create an interhemisp

148 tensification of the WNPSH due to suppressed warming in the western Pacific and enhanced land-sea the

149 rring with increasing frequency as the globe warms in response to rising concentrations of greenhouse

150 Within one month sponges exposed to warming (including combined treatment) ceased pumping (5

151 hypothesized to be a key response to climate warming, including warming driven by urban heat islands.

152 Here we show that greater subsurface warming induced by the longer period of reduced AMOC dur

153 Our findings suggest that warming-induced body size reduction is a general respons

154 mass production increased in spring due to a warming-induced earlier onset of plant growth, but decre

155 An improved understanding of warming-induced morphological changes is important for p

156 The warming-induced rise in soil CH(4) and N(2) O emissions

157 Climate warming is causing a shift in biological communities in

158 Ocean warming is causing the symbioses between cnidarians and

159 onia oxidation (AO) in the ocean responds to warming is crucial to predicting future changes in marin

160 Climate warming is currently advancing spring leaf-out of temper

161 Global warming is having impacts across the Tree of Life.

162 ce to environmental stressors due to climate warming is influenced by local adaptations, including pl

163 If global warming is kept below 2 degrees C, less than 2% of assem

164 d (permafrost) in the Northern Hemisphere to warming is less clear, and its long-term trends are hard

165 e East Antarctic Ice Sheet (EAIS), to global warming is poorly understood.

166 Forecasted warming is predicted to increase the spatial cohesion of

167 Further warming is projected to result in increases of snowpack

168 Winter climate warming is rapidly leading to changes in snow depth and

169 Global warming is thought to affect phytoplankton production bo

170 +/-40 kg pigs were exposed to 30 minutes of warm ischemia and randomized to receive 22-hour HMP with

171 orcine kidneys were exposed to 30 minutes of warm ischemia and then reimplanted following either 16 h

172 reduce and limit the impact of the prolonged warm ischemia inherent to the uDCD process, and to deal

173 ighted include the vital importance of donor warm ischemia time (DWIT) on outcome for both recipients

174 Warm ischemia time and cold ischemia times were 38 and 4

175 analyzed following challenge with 45 min of warm ischemia time and either 4 h of reperfusion or 24 h

176 Longer cold/warm ischemia time, recipient/donor hypertension, and ha

177 D, pig kidneys underwent 0, 30, or 60 min of warm ischemia, before hypothermic machine perfusion.

178 eased in human donor lungs starting from the warm-ischemia phase and were associated with increased t

179 In warm localities shallow ectotherms have lowest energy co

180 e the coverage, reflectance, and lifetime of warm low-level clouds.

181 7)O decreases significantly when moving into warm, low-elevation tributaries draining the same bedroc

182 We then show that short-term warming manipulations do not capture the non-linear, lon

183 geological record, suggesting that long-term warming may support more productive food webs in subtrop

184 If winter soils continue to warm, microbial C limitation will reduce expected CO(2)

185 The warming mode dominates in the mid-Holocene, whereas the

186 is known about the magnitude and duration of warming near Greenland during these periods.

187 We also found that warming negatively impacted (a) symbiont-mediated intera

188 Daytime (DTW) and night-time warming (NTW) may impact ectothermic animals and their i

189 ster, and retreating where ice is exposed to warm ocean waters.

190 These results support the hypothesis that warming ocean waters will restrict the habitat range of

191 Ensemble mean projected warming of 3.5 degrees C shifted snowmelt peaks 10-19 d

192 A warming of 4 degrees C caused SOM decay to increase by 2

193 Here we show that in situ experimental warming of a lowland tropical forest soil on Barro Color

194 Long-term soil warming of ice-rich permafrost can result in thermokarst

195 cated in West Beringia during high-magnitude warming of the last interglacial, followed by westward r

196 The effects of pulse warming on ecological and evolutionary processes are com

197 e, we explore the potential impact of global warming on ectotherm ageing through its effects on react

198 ing, but how fish production equilibrates to warming on longer timescales is unclear.

199 nown whether the long-term impacts of global warming on metabolic rates of phytoplankton can be modul

200 aluating and predicting the effects of pulse warming on parasitic infection.

201 ures, we analysed the effect of experimental warming on the abundance and C and N uptake activity of

202 The indirect effects of warming on VOC emissions were significant but smaller th

203 d either ambient temperatures, a 4 degrees C warming, or an 8 degrees C warming.

204 of carbon dioxide, thus limiting the global warming otherwise expected from postextinction volcanism

205 Both deserts substantially warmed over the past century, but the Mojave dried while

206 We investigated how predicted ocean warming (OW) and acidification (OA) affect key ecologica

207 :V(cmax) ratio decreased significantly with warming (p = .0178), whereas interactions between warmin

208 nological responses in 1971-2000 matched the warming pattern in Europe, but a lack of chilling and ad

209 The inter-model warming pattern spread (WPS) limits our ability to fores

210 nter-model spread in both their geographical warming patterns and global mean values.

211 the existence of distinct fast and slow SST warming patterns.

212 lower delta(18)Ow values during the Medieval Warm Period (1200 to 800 years BP) and the major portion

213 years BP) and the major portion of the Roman Warm Period (1950 to 1550 years BP) indicate a wetter IS

214 d from the Upper Rhine Valley shows that the warm periods during late Roman, medieval and recent time

215 ice sheets during Earth's past interglacial warm periods(1-3).

216 fforts to improve sea level forecasting on a warming planet have focused on determining the temperatu

217 g 100 yr and 20 yr static and dynamic global warming potential (GWP) approaches to estimate the globa

218 electricity (LCOE) by 12-41% and the global warming potential (GWP) by 7-77%.

219 Methane (CH(4)), a potent gas with a global warming potential 86-125x that of carbon dioxide (CO(2))

220 ected to have expanding impacts under global warming predictions.

221 have positive effects for mitigating global warming, preventing soil erosion, and reducing biodivers

222 Model warming projections, forced by increasing greenhouse gas

223 Warming-raised emission of soil GHG increases with the i

224 extreme low temperature environment that is warming rapidly due to global change.

225 l, the higher temperature experienced in the warm region increased soybean seed yield relative to the

226 tic experienced slight cooling or suppressed warming, relative to the background positive temperature

227 on patterns of observed and simulated ocean warming remains a challenge.

228 econd growing season of treatment, the shrub warming response rate increased to 2.54 km m(-2) degrees

229 , additional timescales exist in the surface-warming response, tied to the time evolution of the sea-

230 Results from a uniform warming scenario of +1 degrees C show an average wheat y

231 g regions-as long as efforts to avoid higher warming scenarios are successful.

232 sect of field shrub sampling, and forecasted warming scenarios with regional downscaling to map curre

233 e phytoplankton communities under a range of warming scenarios, and found that ecosystem production d

234 These benefits are more muted at higher warming scenarios, reducing areas lost by a third at 4 d

235 spersal may occur under contemporary climate warming scenarios, which could influence the genetic str

236 l feedback to climate change under projected warming scenarios.

237 then ask how vulnerability varies under four warming scenarios: +1.5, +2, +3 and +5 degrees C.

238 99 vs. 26.08 +/- 0.5, P < 0.0001) and higher warm sensation threshold (43.7 +/- 0.49 vs. 41.37 +/- 0.

239 tiness, sweetness, fullness/body and alcohol warming sensation (p < 0.05).

240 We found that warming soil temperatures and decreasing winter length h

241 In the warm spring, we found that photosynthesis was enhanced m

242 rch for the penalty parameter is realized by warm starts.

243 However, the warmed state was preceded by an overreaction to warming,

244 rth system models (ESMs) project that global warming suppresses biological productivity in the Subarc

245 Warm temperature is postulated to induce plant thermomor

246 gically threatened by short-term exposure to warm temperatures and that longer-term physiological res

247 Globally, overwintering and warm temperatures are key drivers of germination in alpi

248 The results showed that warm temperatures in spring had a positive effect on NEP

249 hern latitudes that are experiencing rapidly-warming temperatures and lengthening thaw periods.

250 ive behaviours did affect survival such that warming temperatures had a greater effect on survival of

251 n, we also find that additional losses under warming temperatures primarily result from additional re

252 icts significant negative yield impacts from warming temperatures, but estimating the effects on yiel

253 ity and prevalence will likely decrease with warming temperatures.

254 e will increase for producers as a result of warming temperatures.

255 ns with drought and plant productivity under warming than control.

256 loss increases to a larger extent under soil warming than under canopy air warming.

257 by the time evolution of the pattern of SST warming that is realized in the real world.

258 om fossil fuel combustion into the air, they warm the atmosphere and contribute to millions of premat

259 ut as data coverage increases and the Arctic warms, the cold season has been shown to account for ove

260 , the risk accelerates with the magnitude of warming, threatening 15% of assemblages at 4 degrees C,

261 Atmospheric warming threatens to accelerate the retreat of the Antar

262 h a reduction of the AMOC causing subsurface warming throughout much of the Atlantic basin(9,12,17).

263 2007-April 2013, a time of both rapid ocean warming throughout the Gulf of Maine and apparent change

264 opy-forming kelps appeared most sensitive to warming throughout their range.

265 urface deformation and edifice-scale surface warming time series have on assessing the physical mecha

266 hen irrigated and nutrient-amended soils are warmed to >20 degrees C during summer.

267 he capacity for future P loading and climate warming to drive cyanobacterial growth.

268 whether plasticity in the form of inducible warm tolerance also evolved.

269 s, including a control, low warming and high warming treatment, and then measured reproductive behavi

270 oth varied seasonally and in response to the warming treatment, tracking variation in T(air) .

271 In the +4 degrees C warming treatment, we found that seedling survival incre

272 ng positively to ecosystem production in the warmed treatments were those that had the highest optima

273 months, and ~10 days, and we infer a decadal warming trend that substantially exceeds previous estima

274 y, frequent fires caused by regional dry and warming trends and increased ignitions by humans and lig

275 ement of canopy should take into account the warming trends in viticulture regions, rather than being

276 died extensively in the context of long-term warming trends(14-18), they are unaccounted for in exist

277 g species diversity and dominance out of the warm tropics.

278 e N limitation and stimulate productivity in warming tundra.

279 tely warm and humid environments; (2) active warm-up protocols; (3) intermittent fasting conditions;

280 ls; (3) intermittent fasting conditions; (4) warming-up while listening to music; or (5) prolonged pe

281 wind controls the thickness of the inflowing warm water layer and the rate of basal melting.

282 section of changing habitat productivity and warming water temperatures on salmonids is important for

283 Soil degradation due to global warming, water scarcity and diminishing natural resource

284 To constrain global warming, we must strongly curtail greenhouse gas emissio

285 ignificantly reduced skeletal stiffness, and warming weakened it, potentially curtailing reef formati

286 ecame pronounced during the first 3 years of warming where the sustained reductions in soil inorganic

287 ase their VOC emissions with ongoing climate warming, which is proceeding at twice the rate of global

288 med state was preceded by an overreaction to warming, which was related to organism physiology and wa

289 aimed at understanding how continued climate warming will affect the ecology of Lake Tanganyika fishe

290 er and how phenological responses to climate warming will differ from year to year, season to season,

291 s is important for understanding how climate warming will impact mountain ecosystems.

292 Our understanding of how projected climatic warming will influence the world's biota remains largely

293 f their size-selective effects, meaning that warming will lessen the consequences of introductions in

294 ilability, and body size predict that global warming will limit the aerobic scope of aquatic ectother

295 xperiments, we demonstrate that persistently warm winter soils can lead to labile C starvation and re

296 d northwestern Canada during the anomalously warm winter to spring conditions of 2015 and 2016 (relat

297 Warming winter temperatures are a main driver of expansi

298 In ecosystems with a perennial leaf habit, warming winter temperatures are more likely to increase

299 ately capture the observed patterns of ocean warming, with a large spread in their projections of oce

300 entury(5) and may continue to intensify in a warming world(6).