ライフサイエンスコーパス: peat

1 ce processes and not degradation of catotelm peat.

2 carbon cycle by storing about 40-90 Gt C in peat.

3 s and accumulation of organophilic metals in peat.

4 ed 163,336 ha, including 137,044 ha (84%) on peat.

5 hemical speciation of As in the Gola di Lago peat.

6 e XAS, were found as minor As species in the peat.

7 o reduced C accumulation or even net loss of peat.

8 well within those previously determined for peat (+0.6 +/-2.0 per thousand).

9 cilitating multi-proxy analysis of preserved peat [14].

10 We reacted peat (40-250 mum size fraction, 1.0 g Fe/kg) with 0-15 g

11 Here, the sorption affinity to Pahokee peat, a model sorbent for soil organic matter, was inves

12 sis assumes non-linear relationships between peat accretion and water depth, and describes flow-depen

13 Thus, discharge competence and non-linear peat accretion dynamics may explain the establishment, p

14 The peat accumulated in a beaver pond surrounded by boreal l

15 BP and was followed by relatively rapid peat accumulation ( 0.1 cm/year) until 2150 cal.

16 rost originally aggraded simultaneously with peat accumulation (syngenetic permafrost) at both sites.

17 human disruption of the feedbacks that link peat accumulation and groundwater hydrology.

18 Before the industrial revolution, rates of peat accumulation in all cores were much lower, at aroun

19 h the observed positive correlations between peat accumulation rates and photosynthetic rates over th

20 ts included radiocarbon dating (to determine peat accumulation rates) and stable carbon isotope compo

21 de following thaw, after which post-thaw bog peat accumulation returned sites to net C sinks.

22 unclear because of complex feedbacks between peat accumulation, hydrology and vegetation.

23 c hiatus as well as the recent resurgence of peat accumulation, sometime after 1950 AD.

24 les from hours to years can reduce long-term peat accumulation.

25 vity of CO2 and CH4 production and increased peat aerobicity due to enhanced growing-season evapotran

26 Column experiments with a peat amendment delayed PAH breakthrough.

27 dustrial 1760 to 1880 is a factor of 4.3 for peat and 3.0 for sediment.

28 Based on our results, we revise existing peat and carbon loss estimates for recurrent fires in dr

29 Phenol uptake by peat and clay soils was also associated with a significa

30 this gap, we examined the biogeochemistry of peat and dissolved organic matter (DOM) along a approxim

31 lts document a rapid reaction of S(-II) with peat and HA and the concomitant formation of reduced org

32 We reacted 0.2 mol C/L peat and humic acid (HA) with up to 5.8 mM S(-II) at pH

33 n strongly reducing microenvironments of the peat and indicate that As(III)-NOM complexes are formed

34 ings were transplanted in 2L pots containing peat and perlite (1:1v/v).

35 centrations reflective of MeHg levels in the peat and porewaters where they were collected.

36 is largely erroneous and caused by comparing peat and sediment against different reference time perio

37 Pre-industrial accumulation in peat and sediment is a factor of approximately 5 greater

38 og, exhibiting various degradation stages of peat and sphagnum moss, was exposed to various light reg

39 e distribution, area and volumes of tropical peat and their continental contributions.

40 he atmosphere in 1997 as a result of burning peat and vegetation in Indonesia.

41 own from seeds sown in seed trays containing peat and young seedlings were transplanted in 2L pots co

42 a affected by acid mine drainage, as well as peats and acidic soils, and to better define optimal con

43 from issues of interaction (oil sorption in peat) and highly nonlinear partitioning with depletion (

44 ed regions, strict requirements to avoid all peat, and routine monitoring of clearly defined forest c

45 lly present in soils-uncharred pine wood and peat-and five inorganic metal oxides with variable surfa

46 rent terrestrial sources (soil, compost, and peat) are then separated under these chromatographic con

47 Asia hosts 38% of both tropical peat area and volume with Indonesia as the main regional

48 the holder of the deepest and most extended peat areas in the tropics.

49 With increasing Fe content of peat, As(III) increasingly formed bidentate mononuclear

50 e Fe(III) complexes formed with 900 mg As/kg peat at pH 7.0, 8.4, and 8.8.

51 (14) C-dated Chorisodontium aciphyllum moss peat bank, the vertical accumulation rate of peat was 3.

52 the rate of recent climate change, but moss peat banks contain an unrivalled temporal record of past

53 Peat-based AC performed similarly in MFC tests (1610 +/-

54 Radiocarbon dates indicate that peat began accumulating from about 10,600 years ago, coi

55 The sorbents were Pahokee peat, Beulah-Zap lignite, and a polystyrene-poly(vinyl m

56 and mercury stable isotope composition in a peat bog ecosystem.

57 the head space of a water-saturated, raised peat bog ecotron.

58 ed in several planctomycetes isolated from a peat bog in Northern Russia, although the gene/enzyme re

59 ently dated terrestrial pollen record from a peat bog on South Island, New Zealand, to investigate gl

60 e that atmospheric mercury deposition to the peat bog surface is dominated by GEM dry deposition (79%

61 on which is 10x greater than any terrestrial peat bog, and promises to provide new insight into envir

62 The intact peat bog, exhibiting various degradation stages of peat

63 uring the Moche culture 200-800 AD, whereas peat-bog records from southern South America suggest ear

64 g vegetation data from 56 Sphagnum-dominated peat bogs across Europe, we show that in these ecosystem

65 composition of Pb was determined in Finnish peat bogs and their porewaters from Harjavalta (HAR, nea

66 phase speciation of As, Fe, and S in English peat bogs by X-ray absorption spectroscopy.

67 Methanomicrobiales prevalent in many acidic peat bogs in the Northern Hemisphere.

68 the isotopic composition of Pb in all three peat bogs is remarkably similar.

69 As ombrotrophic peat bogs receive only atmospheric input of contaminants

70 as collected from 21 ombrotrophic (rain-fed) peat bogs surrounding open pit mines and upgrading facil

71 urnover are decoupled, which may allow these peat bogs to maintain ecosystem functioning when subject

72 s was collected from ombrotrophic (rain-fed) peat bogs to quantify dust emissions from the open-pit m

73 This strongly suggests that in peat bogs, species turnover across environmental gradien

74 e present (5 kyBP), the concurrent C sink by peat buildup could mask large early LUC emissions.

75 associated with lowering the water table and peat burning, releasing large amounts of carbon stored i

76 d in remaining samples (n=15) collected from peat burning, shredded tire combustion, and cook-stove e

77 ificantly from 2006 values in porewaters and peat, but remained elevated relative to control levels.

78 in the AB mosses, V exceeds that of ancient peat by a factor of 6; it is therefore enriched in the m

79 ing rate on the decomposition of subtropical peats, by applying either a large single-step (10 degree

80 e found that upon thaw, C loss of the forest peat C is equivalent to 30% of the initial forest C sto

81 e found that upon thaw, C loss of the forest peat C is equivalent to ~30% of the initial forest C sto

82 Here, we combine updated continuous peat C reconstructions with the land C balance inferred

83 a critical pathway for the remobilization of peat C stocks as well as a major component of the net ec

84 Peat C/N ratios decreased whereas humification rates inc

85 Siberia and Alaska increases the circumpolar peat carbon pool estimate for permafrost regions by over

86 d 0.59 Mg C ha(-1) yr(-1), and the resulting peat carbon stocks at the end of the 11,000-year and 500

87 ch will further deplete the legacy of stored peat carbon.

88 atter released to surface waters in a boreal peat catchment using radiocarbon dating of particulate a

89 de from different precursor materials (coal, peat, coconut shell, hardwood, and phenolic resin) were

90 that simulates peat mass remaining in annual peat cohorts over millennia as a balance between monthly

91 e show that deep peat heating of a 2 m-thick peat column results in an exponential increase in CH4 em

92 es to millennia) carbon from deep within the peat column.

93 rbon were released to the atmosphere through peat combustion, with a further 0.05 Gt released from bu

94 coring difficulties posed by woody roots and peat compressibility, enabling retrieval of relatively u

95 few studies reporting the associated mass of peat consumed.

96 We have collected a peat core 4 m long from the free-floating island of Post

97 (236)U was analyzed in an ombrotrophic peat core representing the last 80 years of atmospheric

98 (238)U isotopic ratio along the ombrotrophic peat core represents the first observation of the (236)U

99 urce of PAHs to living moss, and among three peat core the contribution to PAHs from delayed petcoke

100 fallout derived (236)U and (239)Pu along the peat core, the post depositional migration of plutonium

101 true background sample for the ombrotrophic peat core.

102 hagnum moss (24 sites, n = 68), in sectioned peat cores (4 sites, n = 161), and snow (7 sites, n = 19

103 rable differences were observed between both peat cores and different PFASs.

104 asing temporal trends were detected in three peat cores collected closest to industrial activity.

105 In comparison to the surface layer of peat cores collected in recent years from across Canada,

106 enabling retrieval of relatively undisturbed peat cores dating back more than a century.

107 While the immobility of Pb in the peat cores may appear inconsistent with the elevated por

108 In this study, peat cores up to 2 m in depth from four moss banks on Si

109 Peat cores were collected from five bogs in the vicinity

110 n with perfluoroalkyl substances (PFAS), two peat cores were sampled at Mer Bleue, a bog located clos

111 Peat cores were segmented, dried, and analyzed in duplic

112 Ag, Cd, Sb, and Tl (in the top layers of the peat cores) are found at the control site (Utikuma) whic

113 depositional relocation processes within the peat cores, true or unbiased deposition fluxes (i.e., no

114 in pigments and geochemical variables due to peat cutting and upland grazing prior to forest plantati

115 hs and varied depending on the peat type and peat decomposition stage rather than thermal state.

116 eposits beneath the swamp forest vegetation (peat defined as material with an organic matter content

117 s (15.0% of emissions from deforestation and peat degradation) to also include existing concessions (

118 U release via nitrate fertilization, surface peat degradation, and erosion.

119 r thousand, 1sigma) and recently accumulated peat (Delta(199)Hg = -0.22 +/- 0.06 per thousand, Delta(

120 om a Guadalupian (Middle Permian) silicified peat deposit in the Bainmedart Coal Measures, Prince Cha

121 We discovered a 50-cm-thick peat deposit near Cape Rasmussen (65.2 degrees S), in th

122 A peat deposit on Ellesmere Island, Nunavut, Canada, allow

123 Peat deposition and preservation allows some mangroves t

124 Consequently, peat deposits are potential records of past atmospheric

125 We find extensive peat deposits beneath the swamp forest vegetation (peat

126 uriant growth of peat swamp forest overlying peat deposits up to 20 metres thick.

127 To test the hypothesis, we analyzed peat-derived dissolved organic matter remaining in solut

128 By anchoring peat-derived GEM dry deposition to modern atmospheric GE

129 erefore propose that the speciation of Zn in peat determines the isotope fingerprint in coal.

130 dustrial enrichment recorded in sediment and peat disagree by more than a factor of 10.

131 ii) inundated forest swamp; and (iii) raised peat dome (since ca. 3.9 ka BP).

132 mulation and potentially a hiatus during the peat dome stage.

133 tate shifts (open water wetland-forest swamp-peat dome) suggests a potential climatic control on the

134 l controls on C accumulation in an Amazonian peat dome.

135 h their ultimate shape first at the edges of peat domes where they are bounded by rivers, so that the

136 Conversely, in ombrotrophic peat domes, droughts may lead to reduced C accumulation

137 atic warming, culminating in collapse of the peat domes.

138 the supply of potable water downstream from peat-dominated catchments.

139 n the catchment and coastal plume of a small peat-draining river over a seasonal cycle.

140 tructure of the UmuD'2 homodimer reported by Peat et al..

141 This is the thickest accumulation of peat ever found in a free-floating mire, yet it has form

142 ecreased V max and K m ) occurred in surface peat explained by variation in humic substances and phen

143 udy, we explored their oxidation kinetics in peat exposed to atmospheric O2 for up to 180 days under

144 o Basin in a recent synthesis of pantropical peat extent.

145 including humic acid, bone dust, coprolite, peat extract, clay-rich soil, cave sediment and tar.

146 as consistently observed at agricultural and peat extraction areas throughout the seasons.

147 Release of pre-1950 carbon was detected at peat extraction, agricultural and drained sites, and was

148 m deforestation, degradation, harvesting and peat fires is estimated as 2.01 +/- 1.1 Pg annum(-1); wh

149 destabilized due to severe drainage and deep peat fires.

150 Baja California have been accumulating root peat for nearly 2,000 y and harbor a belowground carbon

151 e biophysical indices related to wetland and peat formation: (1) long-term water supply exceeding atm

152 d topographic contexts leave it as the least peat-forming continent.

153 A transition from peat-forming Sphagnum moss to vascular plants has been o

154 ce the C sink potential owing to the loss of peat-forming Sphagnum.

155 n elevation trajectories-contrary to work in peat-forming wetlands showing elevation responses to cha

156 ples of cabbage (Brassica oleracea) grown in peat fortified with different concentrations of Se(IV) a

157 cubations show that only the top 20-30 cm of peat from experimental plots have higher CH4 production

158 We suggest values for the dry mass of peat fuel consumed that are 206 t ha(-1) for initial fir

159 the presence of different FAs (SRFA, Pahokee Peat fulvic acid, PPFA, Nordic lake fulvic acid, NLFA) a

160 , Suwannee River fulvic acid II, and Pahokee Peat fulvic acid.

161 )Cs: these show that the top 2 m of Sphagnum-peat has accumulated in only 100 years.

162 gradient in deep belowground warming ("Deep Peat Heat", DPH) on peat surface CO2 and CH4 fluxes.

163 We show that deep peat heating of a 2 m-thick peat column results in an ex

164 , and CH4 primarily being sourced from deep peat horizons (2-4 m) near the mire's outlet.

165 ely Leonardite humic acid (LAHA) and Florida peat humic acid (FPHA), at concentrations above 5 mg C/L

166 When peat humic acid (PHA) was added to a NOM-deficient sedim

167 BE obtained by photosensitization by Pahokee Peat Humic Acid (PPHA) and Suwannee River Fulvic Acid (S

168 rom the least to most inhibitive was Pahokee Peat humic acid, Elliot Soil humic acid, Suwannee River

169 transfer from reduced and nonreduced Pahokee Peat humic acids (PPHA) and fresh soil organic matter (S

170 us material than with Nordic NOM and Pahokee peat humic acids.

171 of surface moisture, based on the degree of peat humification and the ratio of sedges to grass, from

172 The sorption affinity to Pahokee peat (i) strongly decreased with increasing electrolyte

173 and followed the fate of (13)C into CO2 and peat in order to study the geographic extent, relative i

174 deposits but mainly to extended but shallow peat in the Amazon Basin.

175 Peat inception was dated at 2750 cal.

176 he plant and beetle remains contained in the peat indicate that winter temperatures on Ellesmere Isla

177 9 ka BP), and developed in three stages: (i) peat initiated in an abandoned river channel with open w

178 oldest peatland yet discovered in Amazonia (peat initiation ca. 8.9 ka BP), and developed in three s

179 Most peat is found in cool climatic regions where unimpeded d

180 Strikingly, PEAT is located just upstream of the Pax1 gene.

181 and logging activity on primary forests and peat lands after May 2011.

182 ted from a near-surface (0-38 cm) and a deep peat layer (200-250 cm) and studied by bulk As, Fe, and

183 Although the peat layer is relatively shallow (with a maximum depth o

184 In the deep peat layer samples, however, As was more diffusely distr

185 Bulk S K-edge XAS revealed that the deep peat layers were significantly enriched in reduced organ

186 , and less oxidized compared to the original peat leachate and exhibited a surprising similarity with

187 t oxidized compounds (O/C ratio >0.4) of the peat leachate.

188 ed in sediments, where they transformed into peat, lignite, and, finally, coal.

189 plicit investigation of fire-driven tropical peat loss and its variability.

190 odel with a monthly time step that simulates peat mass remaining in annual peat cohorts over millenni

191 ched with postbomb C compared with the solid peat material.

192 umerous glomoid-type spores are found in the peat matrix surrounding the nodules.

193 the surfaces of these particles and from the peat matrix.

194 controlled drought manipulation using intact peat 'mesocosm cores' taken from bog and fen habitats, a

195 We concluded that Arctic peat microbiota responds rapidly to increased temperatur

196 tropical peatlands by modifying the Holocene Peat Model (HPM), which has been successfully applied to

197 q on PEAT mutant embryos showed that loss of PEAT modestly increases bone morphogenetic protein targe

198 bstrate of cattail litter overlying sand and peat moss sediment (water column Se was reduced from 15

199 oid offspring in a population of the aquatic peat moss Sphagnum macrophyllum.

200 the Hawaiian population of the allopolyploid peat moss Sphagnum palustre probably resulted from a sin

201 significance in the evolutionary history of peat mosses are discussed.

202 Peat mosses of the genus Sphagnum play a major role in g

203 ation of microbiome community composition in peat mosses.

204 RNA-seq on PEAT mutant embryos showed that loss of PEAT modestly in

205 sessed in paraffin-embedded archival tissue (PEAT; n = 133) and in melanoma patients' serum (n = 56).

206 tophytum from Middle Triassic permineralized peat of Antarctica.

207 tance and UO2 precipitation) in lowland moor peats of the river valley grown on the aquifer gravels.

208 Vertebrate fossils from peat on the talus cone are radiocarbon-dated from approx

209 kx3-2 homolog Nkx3-1, the long-noncoding RNA PEAT (Pax1 enhancer antisense transcript) was induced in

210 sage of these elements and provide our Plant PEAT Peaks (3PEAT) model that predicts the presence of T

211 Ancient DNA (aDNA) from lake sediments, peats, permafrost soils, preserved megafaunal gut conten

212 68.35 degrees N, 19.05 degrees E), a thawing peat plateau in northern Sweden.

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

214 els such as Suwanee River (SRFA) and Pahokee peat (PPFA) fulvic acids purchased by the International

215 Internal peat processes (i.e., decomposition and mass loss) had a

216 The peat produced skeletons of two extinct species (tortoise

217 In contrast, the peat profile from HAR yielded greater concentrations of

218 h (14) C characterization of the catchment's peat profile of the same C species.

219 tent of DOC, CO2 , and CH4 across the entire peat profile was considerably enriched with postbomb C c

220 organic matter from potentially deep in the peat profile, facilitating liberation of ancient carbon

221 This was attributed to PFAS mobility in the peat profile.

222 d-end analysis of transcription start sites (PEAT) protocol, providing millions of TSS locations from

223 CO2 -C + CH4 -C) from the active layer depth peat ranged from 77% larger to not significantly differe

224 s(III) and hydroxylic/phenolic groups of the peat (RAs-C = 2.70-2.77 A).

225 in Sanjiang Plain (Northeast China) through peat record to better understand its long-term trend and

226 ort Hg stable isotope signatures in Pyrenean peat records (southwestern Europe) that are used as trac

227 how that the mammalian remains buried in the peat represent mainly taxa of Eurasiatic zoogeographic a

228 Peat represents a globally significant pool of sequester

229 Furthermore, such plant-induced peat respiration could contribute up to 40% of ecosystem

230 mmediate radiative warming, carbon uptake in peat-rich sediments occurs over millennial timescales.

231 f atmospheric deposition and a minerotrophic peat sample from the last interglacial period.

232 y monitoring the oxidation of phenols in one peat sample upon incubation with a phenol oxidase.

233 In the interglacial peat samples a (236)U/(238)U isotopic ratio of (3.3 +/-

234 ide (CO2 ) and methane (CH4 ) emissions from peat samples collected at active layer and permafrost de

235 V, in comparison to the "cleanest", ancient peat samples ever tested from the northern hemisphere (c

236 Thin sections of undisturbed peat samples from 0-37 cm and 200-249 cm depth were anal

237 Anoxic peat samples were collected from a near-surface (0-38 cm

238 Peat samples were extracted by ultrasonication, cleaned

239 Additionally, peat samples were studied by bulk As, Fe, and S K-edge X

240 e PFCAs and PFSAs were detected regularly in peat samples with perfluorooctane sulfonate (85-655 ng k

241 IM1 were analyzed in microdissected melanoma PEAT sections.

242 ent approach, linking hydrological change in peat sediments from the Tibetan Plateau to changes in ar

243 lar layers are likely to be present in other peat sequences that are important for palaeoenvironmenta

244 patterns of phenolic aromatic moieties of a peat soil fulvic acid, an operational fraction of humic

245 M extracted from three soils and a reference peat soil material to an iron (oxy)hydroxide mineral sur

246 We studied CH4 production of Arctic peat soil microbiota in anoxic microcosms over a tempera

247 ions between iron and HS during transit from peat soil to river mouth.

248 tify the organic components of an unmodified peat soil where some organofluorine xenobiotic compounds

249 (obtained through sequential extraction of a peat soil) to cotransport hexavalent uranium (U) within

250 orbents included an organic matter (OM)-rich peat soil, an OM-poor clay soil, a hydrophilic Aldrich h

251 on (SOC) losses following permafrost thaw in peat soils across Alaska.

252 caused by a combination of low weathering in peat soils and accumulation of organophilic metals in pe

253 Peat soils are formed by the build-up of partially decom

254 ropical mountain peatlands contain extensive peat soils that have yet to be mapped or included in glo

255 uggests that converting drained agricultural peat soils to flooded land-use types can help reduce or

256 Our data suggest that Histosols (peat soils), which exhibit at least seasonally water-sat

257 nd the enrichment of organoarsenicals in the peat, suggesting that the importance of organometal(loid

258 lowground warming ("Deep Peat Heat", DPH) on peat surface CO2 and CH4 fluxes.

259 mine a shape parameter (the Laplacian of the peat surface elevation) that specifies, under a given ra

260 nging data set was used to develop a prefire peat surface modelling methodology, enabling the spatial

261 ighest postthaw emissions occurred from bare peat surfaces, a typical landform in permafrost peatland

262 e stems emit substantially more methane than peat surfaces, accounting for 62-87% of total ecosystem

263 cerning the possibility of sustainability of peat swamp exploitation via drainage-based agriculture t

264 t of fluvial organic carbon from both intact peat swamp forest and peat swamp forest subject to past

265 ast, dissolved organic carbon from disturbed peat swamp forest consists mostly of much older (centuri

266 The simulated carbon loss caused by coastal peat swamp forest conversion into oil palm plantation wi

267 l fluvial organic carbon flux from disturbed peat swamp forest is about 50 per cent larger than that

268 hing of dissolved organic carbon from intact peat swamp forest is derived mainly from recent primary

269 we analysed waters from intact and degraded peat swamp forest of Kalimantan, Indonesian Borneo, and

270 ical peatlands support a luxuriant growth of peat swamp forest overlying peat deposits up to 20 metre

271 arbon from both intact peat swamp forest and peat swamp forest subject to past anthropogenic disturba

272 out 50 per cent larger than that from intact peat swamp forest.

273 Pristine tropical peat swamp forests (PSFs) represent a unique wetland eco

274 orted for temperate wet forests and tropical peat swamp forests, representing the largest non-ebullit

275 id C accumulation in some inundated tropical peat swamps, although this can lead ultimately to a shif

276 Africa hosts more peat than previously reported but climatic and topograph

277 f fire to clear and prepare land on degraded peat, the Indonesian fire environment continues to have

278 By accreting on their own accumulated peat, these desert mangroves store large amounts of carb

279 emotely sensed data, we estimate the area of peat to be approximately 145,500 square kilometres (95 p

280 ies and stabilization mechanisms would allow peat to persist in Antarctica, our results suggest that

281 releasing large amounts of carbon stored in peat to the atmosphere.

282 ouse line bearing a complete deletion of the PEAT-transcribed unit.

283 ermafrost depths and varied depending on the peat type and peat decomposition stage rather than therm

284 als were substantially higher than those for peat, uncharred wood, and metal oxides [Qmax 1-34 cm(3)

285 lower shoot P concentrations when grown in a peat-vermiculite mix in which the majority of the total

286 by hydrogenotrophic methanogenesis but deep peat warming increased the delta(13) C of CH4 suggesting

287 e amount of As(III) retained by the original peat was 161 mg As/kg, which increased by up to 250% at

288 peat bank, the vertical accumulation rate of peat was 3.9 mm yr(-1) over the last 30 years.

289 analyses showed that As in the near-surface peat was mainly concentrated in 10-50 mum sized hotspots

290 results show that the majority of Fe in the peat was present as mononuclear Fe(III) species (RFe-C =

291 ing ground measurements of the burn depth of peat, we estimate that 0.19-0.23 gigatonnes (Gt) of carb

292 ed cumulatively over time in the solid-phase peat, which acted as a sink for newly produced MeHg.

293 on of Fe oxides driven by the degradation of peat, which is commonly found in the aquifer system.

294 These results suggest that although surface peat will respond to increasing temperature, the large r