ライフサイエンスコーパス: insolation

1 g that it is an effect associated with solar insolation.

2 scribed to orbitally forced changes in solar insolation.

3 o a weaker monsoon that was paced by orbital insolation.

4 ainfall changes that vary with local orbital insolation.

5 ciation, changing greenhouse gas levels, and insolation.

6 ocene decline of local (65 degrees S) spring insolation.

7 steady orbitally driven reduction in summer insolation.

8 all of which tracked orbitally-driven solar insolation.

9 eric greenhouse gases and low-latitude solar insolation.

10 spheric physics forced by seasonally varying insolation.

11 Hemispheres, each controlled by local summer insolation.

12 500 cal yr B.P.) during a time of low summer insolation.

13 y, which has a much smaller effect on global insolation.

14 respond to peaks in Northern Hemisphere June insolation.

15 odulating eccentricity-related variations in insolation.

16 sent, likely driven by greater high-latitude insolation.

17 rrent with strong Northern Hemisphere summer insolation.

18 stable atmospheric states for the same solar insolation.

19 ven by an increasing local integrated summer insolation.

20 ncert with higher Northern Hemisphere summer insolation.

21 in response to onset of rising local summer insolation.

22 e ocean overturning circulation and seasonal insolation.

23 ntext of weakened Northern Hemisphere summer insolation.

24 namics is influenced by the rapidly changing insolation.

25 that the aurora is also controlled by solar insolation.

26 tronomically driven changes in high-latitude insolation.

27 1889 mean in response to reduced mean annual insolation.

28 local thermodynamic terrestrial response to insolation.

29 nflated-traits that have been linked to high insolation.

30 ncy and/or increasing cloudiness and reduced insolation.

31 is abrupt compared with the annual cycle of insolation.

32 d is nearly in anti-phase with summer boreal insolation.

33 the Holocene, and with an increase in winter insolation.

34 increased carbon dioxide forcing and summer insolation.

35 g the Holocene, including but not limited to insolation.

36 BP) characterized by increased boreal summer insolation, a vegetated Sahara, and reduced dust emissio

37 the PV panel efficiency is influenced by the insolation, air temperature, wind speed and relative hum

38 mate variability between 130 and 60 ka, when insolation amplitude was nearly twice that of the 60- to

39 occur with high contrasts in local, seasonal insolation and a vigorous African summer monsoon.

40 Varying levels of boreal summer insolation and associated Earth system feedbacks led to

41 bit and spin vector are a primary control on insolation and climate; their recognition in the geologi

42 clude that, possibly in response to stronger insolation and CO2 forcing earlier in T-II, the relation

43 s need to be spatially explicit, since solar insolation and crop yields vary widely between locations

44 Solar insolation and electricity pricing structures were key i

45 f eccentricity-modulated low-latitude summer insolation and glacial-interglacial Antarctic Ice Sheet

46 unctional relationship between boreal summer insolation and global carbon dioxide (CO2) concentration

47 ss in the Northern Hemisphere in response to insolation and greenhouse gas forcing is thought to have

48 armed during HS1 and YD because of increased insolation and greenhouse gases, consistent with snowlin

49 th of the equator in response to high summer insolation and increasing greenhouse gas (GHG) concentra

50 e season, due to decreasing summer radiative insolation and increasing precipitation over the last 7.

51 ween 12 and 8 ka in concert with high summer insolation and increasing temperatures.

52 yika temperatures follow Northern Hemisphere insolation and indicate that warming in tropical southea

53 rent evolution of northern hemisphere summer insolation and ISM variability on orbital timescale, we

54 onal cooling was driven by changes in summer insolation and Northern Hemisphere volcanism.

55 mation is driven most strongly by increasing insolation and sediment/albedo feedbacks.

56 ontrols of the ASM dynamics include not only insolation and solar activity but also suborbital-scale

57 cal latitudes occurred in response to boreal insolation and the bipolar seesaw, whereas tropical SSTs

58 te to the opposing effects of austral summer insolation and the temporal/spatial pattern of sea surfa

59 st lower TC activity despite stronger summer insolation and warmer sea surface temperature in the Nor

60 ming the general connection between seasonal insolation and warming and demonstrating the importance

61 a were used to determine sunlight radiation (insolation) and temperature exposure for a cohort of 16,

62 e increase of boreal summer integrated solar insolation, and during this stage three millennial clima

63 weak wind speeds, associated with increased insolation, and reduced ocean heat losses.

64 equations for model temperature, changes in insolation, and self-organisation of the biota as an imp

65 g-term trend to orbitally induced changes in insolation, and suggest internal ENSO dynamics as a poss

66 may help to amplify relatively weak orbital insolation anomalies into more significant climatic pert

67 erm variations in Northern Hemisphere summer insolation are generally thought to control glaciation.

68 Geographic position and insolation are key factors in the prevalence of AMD.

69 opical Southern Hemisphere, where changes in insolation are thought to be the main direct forcing of

70 Orbital-scale variations in insolation are widely considered to drive tropical and m

71 e same temperature sensitivity to changes in insolation as does our proxy reconstruction, supporting

72 Declining solar insolation as part of a normal eleven-year cycle, and a

73 t to reconcile with June Northern Hemisphere insolation as the trigger for the ice-age cycles.

74 lation changes, rather than by boreal summer insolation, as Milankovitch theory proposes.

75 suggests that during extreme peaks of summer insolation-as occurs during the last interglacial (e.g.,

76 tions may have been the antiphasing of polar insolation associated with orbital cycles.

77 Georgia suggests a persistent link to summer insolation at 55 S, which intensified during the period

78 arly mild (warmer) minima of the mean summer insolation at 65 degrees N and these early aggradational

79 riven by latitudinal gradients in light (low insolation at high latitudes).

80 es, the SPECMAP project proposed that summer insolation at high northern latitudes (that is, Milankov

81 tive to factors beyond ice volume and summer insolation at high northern latitudes.

82 Milankovitch proposed that summer insolation at mid-latitudes in the Northern Hemisphere d

83 shold in the level of astronomically induced insolation below which abrupt changes at the end of inte

84 approaches are often studied and reported in insolation, both in the literature and associated databa

85 d to seasonal variations in precipitation or insolation, but are strongly related to the seasonal str

86 ecession cycle in northern hemisphere summer insolation by an average of 3240 years (-900 to 6600 yr

87 e forced by Northern Hemisphere summer solar insolation centered at 65 degrees N latitude, as predict

88 , which implies a close relationship between insolation changes and long-term hydroclimate trends tha

89 differences in the size and rate of regional insolation changes and the lack of glacial inception in

90 sitivity experiments in which not only solar insolation changes are varied but also vegetation and du

91 ral precision allow us to test the idea that insolation changes caused by the Earth's precession drov

92 flects both the long-term effect of regional insolation changes driven by orbital precession and the

93 ng an early link in the propagation of those insolation changes globally, and resulting in a rapid tr

94 r understanding the role of orbitally driven insolation changes on glacial/interglacial cycles.

95 and monsoon variations, both coordinated by insolation changes on orbital timescales, is critical fo

96 For the same surface temperature change, insolation changes result in relatively larger changes i

97 fairly modest ENSO response to precessional insolation changes simulated in climate models.

98 at the onset of MIS 14 was forced by austral insolation changes, rather than by boreal summer insolat

99 nter) temperatures, which relate to seasonal insolation changes.

100 has confounded a detailed assessment of the insolation-climate relationship during this period.

101 Increasing austral-spring insolation combined with sea-ice albedo feedbacks appear

102 atile sublimation and condensation, changing insolation conditions and Pluto's interior structure.

103 n, suggesting generally higher obliquity and insolation conditions at the poles than at present.

104 variation in intensity arising from changing insolation conditions.

105 primarily reflect changes in maximum summer insolation, confirming the general connection between se

106 the primary driver, and local orbital summer insolation control is limited.

107 During intervals of high summer insolation coupled with cooler tropical North Atlantic s

108 e precipitation record and different monthly insolation curves shows that changes in solar insolation

109 the orbitally controlled Antarctic seasonal insolation cycle with a static (present-day) estimate of

110 Increasing CO2 and summer insolation drive recession of northern ice sheets, with

111 global paleomonsoon strength include summer insolation driven by precession cycles, ocean circulatio

112 These insolation-driven EASM trends were punctuated by two mil

113 Furthermore, our result implies that insolation-driven ITCZ dynamics may provoke water vapour

114 This suggests that sediment enhancement of insolation-driven melting may act similarly to expected

115 Thus, insolation-driven variation in the amount and seasonalit

116 We propose that the insolation-driven WTP moisture dynamics play a pivotal r

117 During the early Holocene, peak (summer) insolation drove July air temperatures higher than prese

118 e to changes in the seasonal distribution of insolation due to Earth's orbital configuration, as well

119 ty deviates from seasonal changes in orbital insolation due to ocean-atmosphere interactions.

120 nsolation curves shows that changes in solar insolation due to precession decide the dominant rainfal

121 trolled by variations in low-latitude summer insolation during most of the early and middle Pleistoce

122 he last deglaciation was initiated by rising insolation during spring and summer in the mid-latitude

123 Hemispheric differences in insolation during the LIG may explain the asymmetrical r

124 It is found that the solar insolation effect also exists in the Southern Hemisphere

125 outstanding question is if the auroral solar insolation effect also exists in the Southern Hemisphere

126 s occurred when the energy related to summer insolation exceeded a simple threshold, about every 41,0

127 ariates, the previous year's monthly average insolation exposure below the median gave a hazard ratio

128 tion of size, orbital period, star type, and insolation flux.

129 riable was race for early AMD (P = .002) and insolation for late AMD (P = .001).

130 e data (geolocalization) and the mean annual insolation for the area where survey took place were obt

131 rld limits the range of values for the solar insolation for which biota may grow in the planet.Recent

132 of eastern African rainfall to low-latitude insolation forcing and high-latitude-driven climate chan

133 rily to meltwater forcing and secondarily to insolation forcing and is further reinforced by atmosphe

134 sed sensitivity of monsoonal hydroclimate to insolation forcing as the Northern Hemisphere became inc

135 been transmitted to the Southern Hemisphere, insolation forcing can also directly influence local Sou

136 othesis that the African monsoon responds to insolation forcing in a markedly nonlinear manner.

137 d on remote teleconnections between seasonal insolation forcing in both hemispheres, the Asian monsoo

138 ding little support for the dominant role of insolation forcing in these regions.

139 Although similar insolation forcing initiated the last two deglaciations,

140 ere) can inhibit ice sheet growth, even when insolation forcing is conducive to glaciation.

141 Hence, astronomical insolation forcing likely contributed to the expansion o

142 MIS 14 raises the possibility that southern insolation forcing may have played an important role in

143 son length, which were controlled by orbital insolation forcing of tropical monsoon dynamics.

144 ry to some models that exhibit a response to insolation forcing over this same period.

145 ion (LIG) experienced stronger boreal summer insolation forcing than the present interglaciation(7),

146 cal factors in amplifying ENSO's response to insolation forcing through changes in the Walker circula

147 d runoff primarily responded to precessional insolation forcing until ~0.95 Ma, but exhibited heighte

148 glacial-interglacial cycles were strong and insolation forcing was weak.

149 Yet insolation forcing, a primary driver of multimillennial-

150 ss overall, consistent with predictions from insolation forcing, but also fluctuated in the early Hol

151 Multiple proxies show no clear response to insolation forcing, but strong evidence for dry conditio

152 the Holocene without an obvious relation to insolation forcing, which is the main climate driver dur

153 volume, greenhouse gas, and regional summer insolation forcing, with cooccurring primary orbital cyc

154 ther represent the response to deterministic insolation forcing.

155 sea level 6-13 m above present, despite weak insolation forcing.

156 intense climate response to relatively weak insolation forcing.

157 al continent, was highly responsive to local insolation forcing.

158 global ice volume and sea level, and orbital insolation forcing.

159 se conditions, however, because the proposed insolation forcings share essentially identical variabil

160 in response to 21,000-year cycles in summer insolation from 3.5 to 2.5 Ma.

161 ecessional forcing caused a shift of maximum insolation from boreal spring to fall in the mid-Holocen

162 Analysis of the insolation geometry of this pole-facing crater wall, and

163 n) beat, driven by orbital forcing of summer insolation, global ice volume and long-lived atmospheric

164 nsoon rainfall is controlled by low-latitude insolation gradients and that while increases in precipi

165 uity cycles and follow changes in meridional insolation gradients, and that only 30%-40% of the degla

166 Late Pleistocene changes in insolation, greenhouse gas concentrations, and ice sheet

167 tem responds quickly to artificially reduced insolation; hence, there may be little cost to delaying

168 ppears to track changes in spring and autumn insolation, highlighting the sensitivity of tropical Pac

169 e several regional-scale forcings, including insolation, ice sheets and ocean circulation, modulated

170 y in solar activity and a decrease in summer insolation identified as primary drivers of temperature

171 In view of the intermittency of insolation, if solar energy is to be a major primary ene

172 s, is generally attributed to reduced summer insolation in boreal latitudes.

173 response of Earth-like planets to increased insolation in hot and extremely moist atmospheres.

174 varied in the opposite sense to local annual insolation in the eastern equatorial Pacific Ocean.

175 o the Milankovitch theory, changes in summer insolation in the high-latitude Northern Hemisphere caus

176 These observations indicate that insolation, in part, sets the pace of the occurrence of

177 hasing and amplitudes of 65 degrees N summer insolation, including the classic saw-tooth pattern of g

178 39 +/- 1 ka BP concordant with boreal summer insolation increase, which was followed by a major rise

179 h to maintain ice growth despite consecutive insolation-induced polar warming episodes.

180 raffic, meteorological conditions, and solar insolation influence the net forcing effect of contrails

181 ar problem is that glaciers are sensitive to insolation integrated over the duration of the summer.

182 ctic ice cores to Northern Hemisphere summer insolation intensity has been used to suggest that the n

183 warming and demonstrating the importance of insolation intensity rather than seasonally integrated i

184 nt with a classic Northern Hemisphere summer insolation intensity trigger for an initial retreat of n

185 Solar insolation is assumed to be the dominant driver of monso

186 Yet such summer insolation is near to its minimum at present, and there

187 strial cooling indicates that a reduction of insolation is playing a key role in the link between the

188 But the intensity of summer insolation is primarily controlled by 20,000-year cycles

189 The integrated summer insolation is primarily controlled by obliquity and not

190 Seasonal insolation is the only regular climate cycle that can pl

191 account for millennial-scale variability and insolation-lagged responses in Asian monsoon records.

192 Metaregression analysis showed that insolation, latitude, longitude, age, and race have a si

193 The increased seasonal contrast of insolation led to an intensification and southward shift

194 Low wintertime insolation limits convective mixing, such that pollutant

195 l and monsoonal rainfall, with higher summer insolation linked to stronger precipitation.

196 itation, and the water table as modulated by insolation, (local) sea level, and monsoon intensity.

197 ets in Sun-grazing orbits that survive solar insolation long enough to penetrate into the Sun's inner

198 eceiving just 30% of the Earth's present-day insolation, Mars had water lakes and rivers early in the

199 ether the sensitivity of seasonal climate to insolation matches theoretical predictions has not been

200 Our data cover multiple insolation maxima and are therefore an important benchma

201 appear to have occurred in phase with summer insolation maxima produced by the Earth's precessional c

202 rs (kyr) before present, during a first weak insolation maximum, whereas northern high latitudes rema

203 Our results suggest that Southern Hemisphere insolation may have been responsible for these differenc

204 phere summer insolation, which suggests that insolation may have modulated the effects of interstadia

205 uding the Super Drought, coincide with solar insolation minima, suggesting that solar forcing of sea

206 his pluvial period coincided with the summer insolation minimum and reduced adiabatic heating over th

207 change forced by Northern Hemisphere summer insolation (NHI), but the timing of the penultimate degl

208 nse to changes in Northern Hemisphere summer insolation (NHSI) without significant temporal lags, sup

209 LHS 1140b receives an insolation of 0.46 times that of Earth, placing it withi

210 xhibits strong covariation with local summer insolation on precessional (~21,000 years) time scales,

211 ng-term influence of changing austral summer insolation on the intensity of the South American Summer

212 intensity rather than seasonally integrated insolation or season duration(2,3).

213 interior, either directly as a supplement to insolation, or indirectly through its influence on the n

214 h 20-thousand-year (kyr) periodic changes in insolation over Antarctica, paced by eccentricity-modula

215 nomalous aerosol loading in the ATAL reduces insolation over the monsoon region, thereby exacerbating

216 een winter and summer controlled by seasonal insolation over the Northern Hemisphere.

217 r to that expected in response to changes in insolation owing to variations in Earth's tilt.

218 riod is challenging due to opposing seasonal insolation patterns.

219 iation has proved controversial because June insolation peaks 127 kyr ago whereas several records of

220 r data further show that particularly strong insolation peaks at 105 and 126 ka caused pronounced wes

221 r the past one million years, fewer of these insolation peaks resulted in deglaciation (that is, more

222 eaks resulted in deglaciation (that is, more insolation peaks were 'skipped'), implying that the ener

223 ation threshold and in the number of skipped insolation peaks.

224 e growth area was achieved by flattening the insolation profile, leading to spatial uniformity up to

225 t a time of slowly declining northern summer insolation, providing an early link in the propagation o

226 as induced by an increase in northern summer insolation, providing the source for an abrupt rise in s

227 responses of summer temperatures to Holocene insolation radiative forcing in the Alaskan sub-Arctic,

228 When decreasing insolation reaches the critical value, it triggers a str

229 quilibrium climate simulations, we show that insolation reductions sufficient to offset global-scale

230 rst direct field and numerical evidence that insolation-related thermal stress potentially plays a pr

231 e show that increasing the rate of change of insolation relative to adaptation of the biota shows a s

232 ns associated with declining northern summer insolation remain incompletely understood.

233 ar-long gradual changes in CO(2), along with insolation rise, preconditioned glacial terminations, su

234 After removing the 65 degrees N insolation signal from our record, the delta(18)O residu

235 seasonality can markedly alter the weighted insolation signal.

236 nt with the classic Milankovitch theories of insolation, so that climate forcing by 100,000-year vari

237 ffset by a nearly opposite gradient in solar insolation, such that large-scale spatial patterns in RF

238 runaway greenhouse limit to higher values of insolation than are inferred from one-dimensional models

239 tive to temperature adjustment by changes in insolation than by changes in greenhouse gases.

240 Interglacial (130 to 115 ka)-despite higher insolation-than during the Holocene (11.6 ka to present)

241 non-thermogenic flowers (passively heated by insolation) that present a warm microclimate have been s

242 dly coincides with the rise in boreal summer insolation, the marine termination, and the rise in atmo

243 Given its large surface gravity and cool insolation, the planet may have retained its atmosphere

244 Once formed, these clouds attenuate stellar insolation, thereby cooling the surface, reducing vapor

245 Above a certain critical insolation, this destabilizing greenhouse feedback can '

246 sional global climate model to show that the insolation threshold for the runaway greenhouse state to

247 The critical insolation thresholds for these processes, however, rema

248 -phase obliquity (41,000 years) component of insolation to dominate those records.

249 f storage in situations of far below average insolation to provide dispatchable electricity.

250 s agreement suggests that the secular summer insolation trend, combined with the Laurentide Ice Sheet

251 ree of local phenological adaptation, and an insolation trigger of green-up.

252 te forcing from decreases in northern summer insolation, tropical Pacific sea surface temperatures, a

253 ariable forcing does not change the range of insolation values allowing for habitable climates substa

254 a 400-ky frequency correlated with seasonal insolation variability.

255 ka shows strong sensitivity to orbital scale insolation variations as well as to millennial-scale eve

256 quatorial region experiences strong seasonal insolation variations enhanced by ring shadowing, and th

257 models forced with realistic late Quaternary insolation variations show that when the Earth is closes

258 od of extended warmth, suggesting that local insolation variations were important to interglacial cli

259 Our results demonstrate that low-latitude insolation was a prominent driver of pan-African climate

260 l, surface dust transport, mass wasting, and insolation weathering for cometary surface evolution, an

261 tude meadows tolerated herbivory due to high insolation which enhanced plant carbohydrates.

262 tark contrast with the trend of precessional insolation, which decreased by approximately 10% from 10

263 ith variations in Northern Hemisphere summer insolation, which suggests that insolation may have modu

264 straint for refining numerical solutions for insolation, which will enable a more precise and accurat

265 e of the NAO enhances summertime warming and insolation while reducing snowfall, especially in west G

266 to be drier and warmer due to the effects of insolation, wind, and evapotranspiration and these gradi

267 ts the maximum range of values for the solar insolation with a non-zero amount of daisies.

268 , reconstructed temperature changes followed insolation, with a minimum in the early Holocene, follow

269 response to eccentricity modulation of solar insolation, with predominant 405-kyr and ~100-kyr period