ライフサイエンスコーパス: permafrost

1 ect the onset of carbon release from thawing permafrost.

2 f carbon and nitrogen release from degrading permafrost.

3 trategies for potentially active microbes in permafrost.

4 temperatures and thawing of the near surface permafrost.

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

6 rom sites without permafrost than sites with permafrost.

7 e resulting in degradation of the underlying permafrost.

8 al activity in intact, let alone in thawing, permafrost.

9 redictions of carbon emissions under loss of permafrost.

10 initiated a survey of the virome of Siberian permafrost.

11 at a fourth ecotone due to thaw of ice-rich permafrost.

12 sediments overlying thawed Pleistocene-aged permafrost.

13 ittent flow in water tracks over high Arctic permafrost.

14 are sufficient to thaw extensive regions of permafrost.

15 ecially important in ecosystems underlain by permafrost.

16 ed for hundreds of thousand years outside of permafrost.

17 re promising for Arctic wetlands and thawing permafrost.

18 as that of recent estimates made for Arctic permafrost.

19 stem characteristics which otherwise protect permafrost.

20 a high vulnerability of C in Tibetan upland permafrost.

21 Permafrost acts as a significant and preferentially degr

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

23 ter tracks, hill slope flow paths that drain permafrost-affected soils.

24 soil temperatures and thawed large areas of permafrost, allowing for microbial respiration of previo

25 changes such as water content variations and permafrost alteration.

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

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

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

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

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 first metagenomic interrogation of Antarctic permafrost and polar cryptoendolithic microbial communit

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

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

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

36 e of InSAR-observed surface deformation over permafrost and the meteorologically recorded temperature

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

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

41 present-day Mars is frozen in the regolith, permafrosts are considered to be terrestrial analogs of

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

43 lution structure of a proteorhodopsin from a permafrost bacterium, Exiguobacterium sibiricum rhodopsi

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

45 o estimate active layer thickness (ALT) over permafrost based on InSAR (Interferometric Synthetic Ape

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

47 Six bacterial isolates were obtained from a permafrost borehole in northeastern Siberia capable of g

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

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

50 y that has the potential to be used to scale permafrost C loss across landscapes.

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

52 t crucial in understanding future changes in permafrost C storage with climate change.

53 It is thought that the thawing of permafrost can lead to a loss of soil carbon in the form

54 In thawing permafrost, Candidatus 'M. stordalenmirensis' appears to

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

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

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

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

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

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

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

62 Mobilization of Arctic permafrost carbon is expected to increase with warming-i

63 , climate change-induced mobilization of old permafrost carbon is well underway in the Arctic.

64 limate feedbacks of increasing temperatures, permafrost carbon mobilization, and hydrologic changes.

65 mes larger than the mass of Pleistocene-aged permafrost carbon released as greenhouse gases when the

66 Our findings highlight the potential of the permafrost carbon reservoir to modulate abrupt climate c

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

68 mobilization mechanisms of surface vs. deep (permafrost) carbon pools across the climosequence of the

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

70 abrupt thaw processes known as thermokarst (permafrost collapse due to ground ice melt), which alter

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

72 Permafrost contains about 50% of the global soil carbon.

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

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

75 isolated terrestrial cryoenvironments (e.g., permafrost cryopegs and subglacial ecosystems), and is a

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

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

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

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

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

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

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

83 Fire-induced permafrost degradation is well documented in boreal fore

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

85 the thaw layer caused by climate warming and permafrost degradation, these results suggest increasing

86 lts indicate that postfire processes such as permafrost degradation, which also results from a warmin

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

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

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

90 % larger to not significantly different than permafrost depths and varied depending on the peat type

91 m peat samples collected at active layer and permafrost depths when incubated aerobically and anaerob

92 Permafrost-derived DOM degradation was less constrained

93 of high biological availability of ancient, permafrost-derived DOM with clear ramifications for its

94 ctly quantify high CO2 production rates from permafrost-derived LMW DOC mineralization.

95 In addition, waters containing ancient permafrost-derived OC supported elevated phosphatase and

96 s containing ancient carbon, suggesting that permafrost-derived OC was more available for microbial m

97 the Kolyma River Basin (Siberia), including permafrost-derived OC.

98 s may become vulnerable to mineralization as permafrost disappears, potentially negating the climate

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

100 Permafrost DOM had a higher susceptibility to partial ph

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

102 important source of CO2 across the extensive permafrost domain.

103 Thawing permafrost due to Arctic warming will continue to releas

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

105 Permafrost ecosystems contain vast stores of soil C (167

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

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

108 Warming in permafrost ecosystems therefore leads to increased plant

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

110 magnitude of greenhouse gas production from permafrost ecosystems.

111 ing season carbon cycle in these carbon-rich permafrost ecosystems.

112 ic DNA viruses, suggests that the thawing of permafrost either from global warming or industrial expl

113 controlled mixtures of modern OC and thawed permafrost endmember OC sources, respiration rates per u

114 Permafrost exerts an important control over hydrological

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

116 Here we use field observations of Siberian permafrost exposures, radiocarbon dating and spatial ana

117 When lakes eventually drained, permafrost formation rapidly sequestered sediment carbon

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

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

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

121 twice as much carbon as the atmosphere, and permafrost has an important influence on the natural and

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

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

124 d hydrology but also organic matter quality, permafrost history, and vegetation dynamics, which will

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

126 Permafrost horizon (~12% wt.C) produced ~5-fold less CO2

127 CH4 and terrigenous biomarkers, that thawing permafrost in high northern latitudes could have been th

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

129 ves in Siberia to reconstruct the history of permafrost in past climate states.

130 hus primigenius) recovered from the Yakutian permafrost in Siberia, Russia.

131 Permafrost in the Arctic is thawing, exposing large carb

132 Permafrost in the high elevation McMurdo Dry Valleys of

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

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

135 in Alaskan streams suggests that N cycles of permafrost-influenced ecosystems are more open than expe

136 ing potential for export of inorganic N from permafrost-influenced soils to streams.

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

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

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

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

141 By 16S ribosomal DNA analysis, all six permafrost isolates were identified as species of the ge

142 tive growth assays demonstrated that the six permafrost isolates, as well as nine type species of Car

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

144 erge in the active layer, but transition and permafrost layer communities across the sites were signi

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

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

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

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

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

150 including forest disturbance, snow depth, or permafrost melting, could not explain patterns in N expo

151 perhaps their ability to hibernate below the permafrost, might explain the ability of ants to coloniz

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

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

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

155 lant wax lipids predominantly trace ancient (permafrost) OC that is preferentially mobilized from dis

156 = 10(6) tons) of methane from thawing subsea permafrost on shallow continental shelves and dissociati

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

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

159 aw and subsequent microbial decomposition of permafrost organic matter could add large amounts of C t

160 Permafrost originally aggraded simultaneously with peat

161 hose with active disturbance regimes such as permafrost patterned-ground, floodplains, and colluvial

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

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

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

165 ~277 Pg of soil organic carbon (C) stored in permafrost peatland soils remain poorly understood despi

166 The ultimate fate of permafrost peatlands and their carbon stores is unclear

167 Permafrost peatlands contain globally important amounts

168 Permafrost peatlands store one-third of the total carbon

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

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

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

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

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

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

175 concentration was related to probability of permafrost presence, being highest at intermediate proba

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

177 Thawing permafrost promotes microbial degradation of cryo-seques

178 properties with release of soil carbon from permafrost provides a unifying model accounting for the

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

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

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

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

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

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

185 e climate feedback across the Tibetan alpine permafrost region.

186 ion observed across the northern circumpolar permafrost region.

187 he circumpolar peat carbon pool estimate for permafrost regions by over 50 per cent.

188 Soils in permafrost regions contain twice as much carbon as the a

189 preferentially mobilized from discontinuous permafrost regions, where hydrological conduits penetrat

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

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

192 ayer (organic and mineral soil horizons) and permafrost samples from center, ridge and trough positio

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

194 ndisturbed and never thawed Late Pleistocene permafrost sediments with a temperature of -7 degrees C.

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

196 Replenishment of permafrost soil carbon stocks following peak warming pro

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

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

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

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

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

202 Permafrost soils appear to be largely inhospitable to ac

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

204 ariation in the vulnerability of C stored in permafrost soils based on inherent differences in organi

205 Permafrost soils contain enormous amounts of organic car

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

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

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

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

210 Carbon in thawing permafrost soils may have global impacts on climate chan

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

212 Arctic permafrost soils store large amounts of soil organic car

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

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

215 Thawing permafrost soils will change the chemical composition of

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

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

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

219 mpacts microbial respiration of DOC draining permafrost soils.

220 vast quantities of organic carbon stored in permafrost soils.

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

222 Increasing river discharge and thawing permafrost suggest that the impacts of continental runof

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

224 regional summer air temperatures and related permafrost temperatures.

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

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

227 Arctic, and an area with extensive ice-rich permafrost that is extraordinarily sensitive to climate

228 nic matter, by nutrient release from thawing permafrost that stimulated lake productivity and by slow

229 autotrophic and heterotrophic respiration to permafrost thaw across the 2008 and 2009 growing seasons

230 Permafrost thaw also stimulates plant growth, which coul

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

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

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

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

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

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

237 Permafrost thaw and subsequent microbial decomposition o

238 tation and increasing methane emissions with permafrost thaw are associated with a switch from hydrog

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

240 Permafrost thaw can alter the soil environment through c

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

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

243 soil heterotrophic respiration increased as permafrost thaw deepened.

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

245 mine microbial community composition along a permafrost thaw gradient in northern Sweden.

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

247 ulating the climate feedback associated with permafrost thaw in global models.

248 Increased permafrost thaw in lowland boreal forests in response to

249 We used a natural landscape gradient of permafrost thaw in northern Sweden as a model to investi

250 n soil organic carbon (SOC) losses following permafrost thaw in peat soils across Alaska.

251 Permafrost thaw in the Arctic driven by climate change i

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

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

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

255 This impact of permafrost thaw on organic matter chemistry could intens

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

257 Permafrost thaw ponds are ubiquitous in the eastern Cana

258 Permafrost thaw ponds of the warming Eastern Canadian Ar

259 anic matter (DOM) along a approximately 40-y permafrost thaw progression from recently- to fully thaw

260 Carbon release due to permafrost thaw represents a potentially major positive

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

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

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

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

265 from 6 to 18% of Reco and was greatest where permafrost thaw was deepest.

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

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

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

269 tion of carbon metabolized to methane during permafrost thaw, we establish a basis for scaling changi

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

271 ability for vegetation growth resulting from permafrost thaw.

272 reased ground saturation that will accompany permafrost thaw.

273 similar to terrestrial sources arising from permafrost thaw.

274 ately determine net radiative forcing due to permafrost thaw.

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

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

277 th America, climate change causes widespread permafrost thaw.

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

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

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

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

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

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

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

285 ons from subarctic peatlands increase as the permafrost thaws.

286 mon geomorphological expressions of mountain permafrost, the impacts of their solute fluxes on lakes

287 The response of permafrost to warming climate is uncertain and occurs on

288 ing samples from soils outside and inside of permafrost water tracks, hill slope flow paths that drai

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

290 In addition to permafrost wetlands, 'Methanoflorentaceae' are widesprea

291 Loss of underlying permafrost with associated hydrological shifts correlate

292 Earth's terrestrial surface is underlain by permafrost with vast stores of carbon that, once thawed,

293 f organic carbon are stored in frozen soils (permafrost) within Arctic and sub-Arctic regions.

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

295 rates at which C is being released from the permafrost zone at different soil depths and across diff

296 d the inherent decomposability of C from the permafrost zone by assembling a database of long-term (>

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

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

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

300 tems located across the northern circumpolar permafrost zone.