ライフサイエンスコーパス: permafrost

1 e resulting in degradation of the underlying permafrost.

2 stem characteristics which otherwise protect permafrost.

3 a high vulnerability of C in Tibetan upland permafrost.

4 ect the onset of carbon release from thawing permafrost.

5 f carbon and nitrogen release from degrading permafrost.

6 tored Hg from thawing sea-ice, glaciers, and permafrost.

7 trategies for potentially active microbes in permafrost.

8 temperatures and thawing of the near surface permafrost.

9 m, the latter one isolated from 30,000-y-old permafrost.

10 rom sites without permafrost than sites with permafrost.

11 ice will accelerate the thawing of Siberian permafrost.

12 millennia-old soils that extend into thawing permafrost.

13 the release of pre-aged carbon from thawing permafrost.

14 e sheet cover, lower sea level and extensive permafrost.

15 , using precipitation isotopes in syngenetic permafrost.

16 tion lobes are associated with discontinuous permafrost.

17 ineral horizons in palsa underlain by intact permafrost (41.8 +/- 10.8 mg carbon per g soil, 9.9 to 1

18 Permafrost acts as a significant and preferentially degr

19 y remains on the postthaw carbon dynamics of permafrost-affected ecosystems, in particular since most

20 rients are increasing in virtually all large permafrost-affected rivers, indicating major shifts in A

21 changes such as water content variations and permafrost alteration.

22 nd climate change, depending on near-surface permafrost and drainage conditions.

23 These inferred brines are widespread within permafrost and extend below glaciers and lakes.

24 change through carbon releases from thawing permafrost and higher solar absorption from reductions i

25 through thermal perturbation of near surface permafrost and increased mobility of previously frozen s

26 in tandem with changing inputs from thawing permafrost and industrial activity.

27 The palsa site (intact permafrost and low radiative forcing signature) had a ph

28 The bog (thawing permafrost and low radiative forcing signature) had lowe

29 Permafrost and methane hydrates are large, climate-sensi

30 carbon reservoirs (marine methane hydrates, permafrost and methane trapped under ice) to 19 per cent

31 Permafrost and organic mat DOM had similar lability to p

32 ate warming is expected to mobilize northern permafrost and peat organic carbon (PP-C), yet magnitude

33 first metagenomic interrogation of Antarctic permafrost and polar cryptoendolithic microbial communit

34 erstanding of the decomposability of thawing permafrost and relevant mechanistic controls over C rele

35 the early Holocene, associated with melting permafrost and retreating glaciers, while lowest burial

36 reas at Point Barrow, a site with continuous permafrost and small tidal amplitudes, fluxes are mostly

37 rough increases in precipitation, thawing of permafrost, and changes in vegetation.

38 luding aspects of the hydrology, vegetation, permafrost, and glaciers, but effects on wildlife have b

39 rap organic carbon in soils overlying intact permafrost, and may limit carbon mobilization and degrad

40 t changes in the ocean, sea ice, snow cover, permafrost, and terrestrial biosphere that arise after a

41 th heavy precipitation events and thawing of permafrost are increasing the net transfer of terrestria

42 s massive stocks of frozen organic matter in permafrost are liberated in a warming Arctic.

43 different stages of thaw in a discontinuous permafrost area of North Siberia.

44 DNA has so far limited its recovery-outside permafrost areas-to specimens that are not older than ap

45 ilization may be of increasing importance in permafrost as the thawed surface region ("active layer")

46 The growth of the speleothems indicates that permafrost at the cave site was absent at that time, bec

47 taneously with peat accumulation (syngenetic permafrost) at both sites.

48 locations such as deep-sea sediments and the permafrost based on demanding conditions of high pressur

49 sted permafrost plateaus (forest) and thawed permafrost bogs, ranging in thaw age from young (<10 yea

50 ant uptake of a (15) N tracer applied at the permafrost boundary.

51 mycelial connectivity between roots and the permafrost boundary.

52 that the loss of sporadic and discontinuous permafrost by 2100 could result in a loss of up to 24 Pg

53 ies into Earth System Models when predicting permafrost C dynamics under a changing environment.

54 Fortunately, losses from the permafrost C pool will be partially offset by increased

55 e in mediating the direction and strength of permafrost C-climate feedback.

56 Long-term soil warming of ice-rich permafrost can result in thermokarst formation that crea

57 Arctic permafrost caps vast amounts of old, geologic methane (C

58 The sign and magnitude of permafrost carbon (C)-climate feedback are highly uncert

59 atmospheric records and models, suggest that permafrost carbon (PF-C) accumulated during the last gla

60 oss rates are among the highest reported for permafrost carbon and demonstrate the potential importan

61 We also quantified uncertainties in permafrost carbon budget by conducting Monte Carlo simul

62 However, the fate of permafrost carbon depends on climatic, hydrological and

63 rtant than modern climate in shaping current permafrost carbon distribution, and its importance incre

64 which to target poorly understood aspects of permafrost carbon dynamics.

65 stock can shed light on the vulnerability of permafrost carbon in the future.

66 ving the rapid metabolism of Pleistocene-age permafrost carbon upon thaw and the outgassing of CO2 to

67 ntially important pathway for the release of permafrost carbon.

68 tion-derived DOM, and a high contribution of permafrost carbon.

69 t systems, soil cores spanning a Pleistocene permafrost chronosequence (19,000, 27,000, and 36,000 ye

70 ed soils, representing a potential noncarbon permafrost climate feedback.

71 ost thaw sequence (1, 10, and 16 years since permafrost collapse) on the Tibetan Plateau.

72 in central Alaska for centuries, as thawing permafrost collapses forests that transition to wetlands

73 f particular importance is syngenetic Yedoma permafrost containing high OM content.

74 Permafrost contains a large (1700 Pg C) terrestrial pool

75 from melting snow and ice as well as thawing permafrost, contrasting earlier notions of limited shrub

76 study at three sites in Alaska with varying permafrost coverage.

77 lly frozen soil in high latitude ecosystems (permafrost) currently stores 1330-1580 Pg of carbon (C).

78 The rates of subsea permafrost degradation and occurrence of gas-migration p

79 predict future impacts of climate warming on permafrost degradation and subsequent feedback to climat

80 -latitude warming is capable of accelerating permafrost degradation and the decomposition of previous

81 d carbon storage in trees of 13.4 Pg C, with permafrost degradation being the most important factor.

82 these findings document a mechanism whereby permafrost degradation can lead to local decreases in tu

83 n Arctic polygon tundra, across a wet-to-dry permafrost degradation gradient from low-centered (intac

84 olygon centers, rims, and troughs) along the permafrost degradation gradient, we measured surface CH4

85 Knowing the rate and mechanisms of subsea permafrost degradation is a prerequisite to meaningful p

86 sponse of peatlands in contrasting states of permafrost degradation to recent rapid warming.

87 how three factors that alter N availability-permafrost degradation, atmospheric N deposition, and th

88 s into smaller volumes; and (ii) accelerated permafrost degradation, which enhances sublacustrine dra

89 It is thought that after inundation, permafrost-degradation rates would decrease over time an

90 C compounds) and normalized CO2-C release in permafrost deposits were similar or even higher than tho

91 hizal fungi could facilitate plant access to permafrost-derived N, their exploration capacity beyond

92 ism for the vertical redistribution of deep, permafrost-derived nutrients, which may alleviate N limi

93 Hiatuses most likely correspond to permafrost development and a temperature drop of up to 5

94 land Ice Sheet and reductions in sea ice and permafrost distribution are likely to alter coastal morp

95 Permafrost DOM had a higher susceptibility to partial ph

96 t difficult to predict how inputs of thawing permafrost DOM may alter its photodegradation.

97 important source of CO2 across the extensive permafrost domain.

98 Thawing permafrost due to Arctic warming will continue to releas

99 tation types when modeling CH4 production in permafrost ecosystems and suggests the need for longer-t

100 Soil carbon in permafrost ecosystems has the potential to become a majo

101 e supply of N relative to plant N demand) in permafrost ecosystems is still limited.

102 Arctic permafrost ecosystems store ~50% of global belowground c

103 erability and resilience of lowland ice-rich permafrost ecosystems to climate changes depend on fores

104 magnitude of greenhouse gas production from permafrost ecosystems.

105 g minerals as terminal electron acceptors in permafrost environments, and thus their stability and ca

106 phases associated with OM throughout diverse permafrost environments, suggesting that organomineral c

107 Permafrost exerts an important control over hydrological

108 lly induced permafrost thaw at the Carbon in Permafrost Experimental Heating Research (CiPEHR) projec

109 The permafrost feedback is increasingly positive in warmer c

110 potential future releases of Hg from thawing permafrost for low and high greenhouse gas emissions sce

111 njection flue gas into hydrate reservoirs in permafrost for methane recovery and geological capture a

112 haw-induced boreal forest loss is leading to permafrost-free wetland expansion.

113 eat plateaus ('forest') lead to expansion of permafrost-free wetlands ('wetland').

114 In this study, injection of flue gas into permafrost gas hydrates reservoirs has been studied in o

115 the process whereby the thawing of ice-rich permafrost ground causes land subsidence, resulting in d

116 trogen (DOC and DON) concentrations in supra-permafrost groundwater (SPGW) near the land-sea interfac

117 n and release of methane (CH4 ) from thawing permafrost has the potential to be a strong source of ra

118 00, the high emissions scenario shows annual permafrost Hg emissions to the atmosphere comparable to

119 The fen (no underlying permafrost, high radiative forcing signature) had the hi

120 Permafrost horizon (~12% wt. C) produced ~5-fold less CO

121 is only slightly impacted by the continuous permafrost in its low flow.

122 Permafrost in mountains warmed by 0.19 +/- 0.05 degrees

123 At the southern margin of permafrost in North America, climate change causes wides

124 Permafrost in the Arctic is thawing, exposing large carb

125 Permafrost in the high elevation McMurdo Dry Valleys of

126 specimen YG 648.1) was discovered in thawing permafrost in the Klondike goldfields, near Dawson City,

127 e scientific re-drilling to show that subsea permafrost in the near-shore zone of the ESAS has a down

128 h the high resistivity of glacier ice or dry permafrost in this region.

129 he sensitivity of permanently frozen ground (permafrost) in the Northern Hemisphere to warming is les

130 , likely geologic emissions solely where the permafrost is discontinuous.

131 osystems warm, the thaw and decomposition of permafrost is expected to release large amounts of C to

132 uggest today's widespread larch ecosystem on permafrost is not in climate equilibrium.

133 Release of greenhouse gases from thawing permafrost is potentially the largest terrestrial feedba

134 use palaeoclimate data to show that Siberian permafrost is robust to warming when Arctic sea ice is p

135 Across the Arctic, glaciers are melting and permafrost is thawing at unprecedented rates, releasing

136 In areas with sporadic permafrost (Kasitsna Bay), the major driver of submarine

137 veal that inland water carbon emissions from permafrost landscapes may be more sensitive to changes i

138 the emission of terrestrial carbon in Arctic permafrost landscapes.

139 Tibetan permafrost largely formed during the late Pleistocene gl

140 ining the shallow organic mat and the deeper permafrost layer of arctic soils to complete and partial

141 ons might enhance heat transport into deeper permafrost layers promoting permafrost thawing, thereby

142 es retain their infectivity in prehistorical permafrost layers should be of concern in a context of g

143 are expected to rise in the future, ice-rich permafrost may thaw, altering soil topography and hydrol

144 hensive estimates of OC stocks across alpine permafrost means that current knowledge on this issue re

145 d mercury from melting polar ice and thawing permafrost; new funding schemes and regulations; and lan

146 are very different from the aliphatics-rich permafrost NOM.

147 gies, substantial uncertainties exist in the permafrost OC budget, which limits our understanding of

148 Upon thaw, mobilized permafrost OC in dissolved and particulate forms can ent

149 ated the pool size and spatial variations of permafrost OC stock to 3 m depth on the Tibetan Plateau

150 Given that alpine soils with permafrost occupy 3.6 x 10(6) km(2) land area and are es

151 = 10(6) tons) of methane from thawing subsea permafrost on shallow continental shelves and dissociati

152 Thawing permafrost opens pathways for this CH4 to migrate to the

153 The permafrost organic carbon (OC) stock is of global signif

154 Permafrost originally aggraded simultaneously with peat

155 In boreal lowlands, thawing forested permafrost peat plateaus ('forest') lead to expansion of

156 es lead us to propose a five-phase model for permafrost peatland response to climatic warming.

157 d therefore provide an incomplete picture of permafrost peatland response to recent rapid warming.

158 Permafrost peatlands are important carbon stocks current

159 Permafrost peatlands contain globally important amounts

160 that DOM originating from previously frozen permafrost peatlands is highly aromatic and previously p

161 Permafrost peatlands store one-third of the total carbon

162 om bare peat surfaces, a typical landform in permafrost peatlands, where permafrost thaw caused a fiv

163 sult in a loss of up to 24 Pg of deep C from permafrost peatlands.

164 composition with its radiocarbon content in permafrost peatlands.

165 ezes annually) was nearly four times that of permafrost per gram soil carbon, and CH4 production per

166 illennia, related to the combined effects of permafrost persistence, distant glacial refugia and fire

167 spruce) associated with location on elevated permafrost plateau and across multiple time periods (194

168 nce approach to measure C stocks in forested permafrost plateaus (forest) and thawed permafrost bogs,

169 Frozen permafrost Pleistocene mammal carcasses with soft tissue

170 using a carbon-nitrogen model that includes permafrost processes forced in an unmitigated warming sc

171 unities collected from a naturally degrading permafrost region in Central Alaska.

172 juarapik-Whapmagoostui, QC) and a continuous permafrost region in the Arctic tundra (Bylot Island, NU

173 y investigated thaw ponds in a discontinuous permafrost region in the Subarctic taiga (Kuujjuarapik-W

174 nario, that the future carbon balance of the permafrost region is highly sensitive to the decomposabi

175 ecosystem N cycle across the Tibetan alpine permafrost region over the past decade.

176 boreal and tundra soils from the geographic permafrost region to evaluate large-scale controls of an

177 size data from 1114 sites across the Tibetan permafrost region to report that paleoclimate is more im

178 on (C) is stored in the northern circumpolar permafrost region, where air temperatures are increasing

179 d to cover approximately 20% of the northern permafrost region, with approximately equal contribution

180 ajectory of ecosystem C cycle in this alpine permafrost region.

181 ion observed across the northern circumpolar permafrost region.

182 e climate feedback across the Tibetan alpine permafrost region.

183 Roads in permafrost regions are often built atop insulative grave

184 afrost to evaluate temperature change across permafrost regions for the period since the Internationa

185 The ecosystem carbon (C) balance in permafrost regions, which has a global significance in u

186 As Arctic soils warm, thawed permafrost releases nitrogen (N) that could stimulate pl

187 e located at the southern edge of continuous permafrost reveals periods in which the overlying ground

188 Metagenomic analysis of the permafrost sample uncovered the presence of both viruses

189 e of giant virus, was isolated from the same permafrost sample.

190 epresenting different states of thaw: intact permafrost, seasonally thawed active layer and thermokar

191 ek during hydraulic thawing that exposed the permafrost sediment in which it was preserved.

192 y, and greater CH4 oxidation than did intact permafrost sites, to a greater degree than soil moisture

193 were consequently very low, but erosion and permafrost slumping downstream of the lake increased riv

194 ion into model initialization for simulating permafrost soil carbon stocks.

195 Permafrost soil in high latitude tundra is one of the la

196 nditions under extreme cold and dryness: the permafrost soil which is enriched in traits which emphas

197 The permafrost soils also have a large presence of phage gen

198 l gene composition of microorganisms in some permafrost soils and a rapid shift in functional gene co

199 assays to examine the functional capacity of permafrost soils and cryptoendolithic communities in Uni

200 Permafrost soils appear to be largely inhospitable to ac

201 half-century, and much of these carbon-rich permafrost soils are now within ~0.5 degrees C of thawin

202 Permafrost soils contain enormous amounts of organic car

203 Carbon release from thawing permafrost soils could significantly exacerbate global w

204 In contrast, permafrost soils have a lower richness of stress respons

205 carbon budgets in the Arctic, where thawing permafrost soils increase opportunities for DOC oxidatio

206 anic carbon (DOC) leached from 35,800 y B.P. permafrost soils is rapidly mineralized to CO2.

207 Northern permafrost soils store a vast reservoir of carbon, nearl

208 arctic freshwaters as the climate warms and permafrost soils thaw.

209 usceptibility of SOM decomposition in arctic permafrost soils to priming.

210 Thawing permafrost soils will change the chemical composition of

211 te-Pleistocene) carbon released from thawing permafrost soils, but the magnitude of these source cont

212 al warming has led to the thawing of ancient permafrost soils, particularly in Arctic regions, due to

213 cient DNA (aDNA) from lake sediments, peats, permafrost soils, preserved megafaunal gut contents and

214 mpacts microbial respiration of DOC draining permafrost soils.

215 ub, and forests growing on elevated ice-rich permafrost soils.

216 associations with OM carbon (C) moieties in permafrost soils.

217 Our results also demonstrated that Tibetan permafrost stored a large amount of OC in the top 3 m, w

218 As permafrost systems continue to change with climate, we m

219 exation is crucial to predict C stability as permafrost systems warm.

220 nvolved in organomineral complexation within permafrost systems, soil cores spanning a Pleistocene pe

221 eep, cold active layer soils adjacent to the permafrost table is unknown.

222 AS has a downward movement of the ice-bonded permafrost table of approximately 14 cm year(-1) over th

223 o date, no globally consistent assessment of permafrost temperature change has been compiled.

224 Globally, permafrost temperature increased by 0.29 +/- 0.12 degree

225 Here we use a global data set of permafrost temperature time series from the Global Terre

226 res may induce widespread thaw subsidence of permafrost terrain in the first seven years following th

227 bon was two times greater from sites without permafrost than sites with permafrost.

228 by Ob and Yenisey aligns with discontinuous permafrost that facilitates leaching, whereas higher par

229 Permafrost thaw also stimulates plant growth, which coul

230 ially large CO2 sources associated with deep permafrost thaw and cold season respiration expected ove

231 Soil warming caused rapid permafrost thaw and increased ecosystem respiration (Rec

232 g positive relationship between the depth of permafrost thaw and N availability in tundra ecosystems

233 To evaluate the relationship between permafrost thaw and N availability, we monitored N cycli

234 Arctic warming is promoting terrestrial permafrost thaw and shifting hydrologic flowpaths, leadi

235 cted to hinge more on the rate and extent of permafrost thaw and soil decomposition than on enhanced

236 ing during 5 years of experimentally induced permafrost thaw at the Carbon in Permafrost Experimental

237 Permafrost thaw can alter the soil environment through c

238 Warming and associated permafrost thaw can expose soil organic carbon and resul

239 ical landform in permafrost peatlands, where permafrost thaw caused a fivefold increase in emissions

240 Permafrost thaw could induce substantial carbon (C) emis

241 onally, analysis of the labeled fractionated permafrost thaw DOM directly showed carboxyl-rich alicyc

242 ease global greenhouse gas concentrations as permafrost thaw exposes immense stores of frozen carbon

243 ertainties remain about C dynamics following permafrost thaw in boreal peatlands.

244 Increased permafrost thaw in lowland boreal forests in response to

245 of forest change in a landscape subjected to permafrost thaw in unburned dominant forest types (paper

246 major positive feedback to climate change if permafrost thaw increases heterotrophic decomposition.

247 freshwaters, which is likely to increase as permafrost thaw intensifies causing positive climate fee

248 gest that this share may increase if ongoing permafrost thaw opens new pathways.

249 Permafrost thaw ponds of the warming Eastern Canadian Ar

250 ial communities and functional genes along a permafrost thaw sequence (1, 10, and 16 years since perm

251 ty of three sites representative of distinct permafrost thaw stages at a palsa mire in northern Swede

252 ired two and seven years post-fire, detected permafrost thaw subsidence across 34% of the burned tund

253 However, climate warming and permafrost thaw threaten the stability of this carbon st

254 Our model results indicate that permafrost thaw turned these peatlands into net C source

255 nt carbon (11,300 to >50,000 (14)C years) in permafrost thaw waters and millennial-aged carbon (up to

256 ing about the impacts of thermokarst (abrupt permafrost thaw) on microbial structure and function rem

257 We conclude that, due to permafrost thaw, hydrocarbon-rich areas, prevalent in th

258 pacity to prevent carbon mobilization during permafrost thaw, is poorly understood.

259 Within 5 years of permafrost thaw, plants actively incorporate newly avail

260 During permafrost thaw, water-logging and O(2) limitation lead

261 occurred below the maximum rooting depth in permafrost thaw-front soil in tussock and shrub tundra c

262 Therefore, permafrost thaw-induced boreal forest loss may modify re

263 similar to terrestrial sources arising from permafrost thaw.

264 es to buildings associated with near-surface permafrost thaw.

265 th America, climate change causes widespread permafrost thaw.

266 t northern latitudes, including near-surface permafrost thaw.

267 directly associated with CO2-C release after permafrost thaw.

268 ability for vegetation growth resulting from permafrost thaw.

269 reased ground saturation that will accompany permafrost thaw.

270 where wetlands are expanding rapidly due to permafrost thaw.

271 ntributed >50% at sites strongly affected by permafrost thaw.

272 d growing seasons, accelerated snowmelt, and permafrost thaw.

273 currently experiencing rapid evolution after permafrost thaw.

274 ienced a rapid shift to wetter conditions as permafrost thawed in response to climatic warming, culmi

275 relationship between an ice-free Arctic and permafrost thawing before 0.4 Ma.

276 eous carbon release from Arctic soils due to permafrost thawing is known to be substantial, but growi

277 Greater hydrological connectivity from permafrost thawing may potentially increase transport of

278 e carbon pool size together with significant permafrost thawing suggests a risk of carbon emissions a

279 port into deeper permafrost layers promoting permafrost thawing, thereby enhancing groundwater discha

280 udes, fluxes are mostly affected by seasonal permafrost thawing.

281 As climate warms, permafrost thaws and soil organic matter becomes vulnera

282 shwater and nutrients to the Arctic Ocean as permafrost thaws, yet few studies have quantified ground

283 ons from subarctic peatlands increase as the permafrost thaws.

284 In ice-cemented ground (permafrost), the lag of soil particles remaining after i

285 ries from the Global Terrestrial Network for Permafrost to evaluate temperature change across permafr

286 52 years of sublimation measurements from a permafrost tunnel near Fairbanks, Alaska, and constrain

287 sea ice is present, as well as the increased permafrost vulnerability when sea ice is absent, can be

288 Over the same period, discontinuous permafrost warmed by 0.20 +/- 0.10 degrees C.

289 Permafrost warming has the potential to amplify global c

290 We found that long-term experimental permafrost warming introduced a soil hydrology component

291 Alaska during the last glacial period, when permafrost was absent, allowing water infiltration into

292 cover all horizons of active layer and upper permafrost, we found that an increased availability of p

293 The robustness of permafrost when sea ice is present, as well as the incre

294 Loss of underlying permafrost with associated hydrological shifts correlate

295 n atmospheric release of carbon from thawing permafrost, yet overlooked waterborne release pathways l

296 es within boreal forest in the discontinuous permafrost zone (NWT, Canada).

297 h of zero annual amplitude in the continuous permafrost zone increased by 0.39 +/- 0.15 degrees C.

298 In the sporadic permafrost zone of North America, thaw-induced boreal fo

299 In the sporadic permafrost zone of northwestern Canada, boreal forest ca

300 Located within the discontinuous permafrost zone, this region has significantly warmed ov