ライフサイエンスコーパス: peat

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

2 und biomass (AGB) accumulation rate of OP on peat.

3 ce processes and not degradation of catotelm peat.

4 s in response to greater aeration of surface peat.

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

6 s and accumulation of organophilic metals in peat.

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

8 ption and retention of presorbed As in model peat.

9 remained in solution without (re)sorption to peat.

10 at 85% of antimonite was sorbed by untreated peat.

11 wly-decomposing organic matter, such as moss peat.

12 nitrate reduction releases arsenic from this peat.

13 were complexed with alcoholic groups of the peat.

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

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

16 0.01 angstrom) and monothioarsenate-treated peat (2.80 +/- 0.02 angstrom) compared to arsenite treat

17 Aboveground biomass stocks on peat accumulated at ~6.39 +/- 1.12 Mg ha(-1) per year in

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

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

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

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

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

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

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

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

26 use of greater plant productivity and faster peat accumulation.

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

28 lower cumulative CO(2) emissions from burned peat after 1-3 years.

29 ional groups, particularly on the surface of peat aggregates.

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

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

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

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

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

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

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

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

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

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

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

41 the impact of land-cover change on tropical peat, and develop science-based peatland management prac

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

43 rochemical analysis to Elliott soil, Pahokee peat, and Suwannee river humic acid (HA) samples before

44 cts, six organic composts (manure, mushroom, peat, and untreated wood), and one food and yard waste c

45 rent C accumulation rates in recently formed peat are an artefact and take steps to account for it.

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

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

48 In bog vegetation and peat, arsenic (As) concentrations and accumulation rates

49 The physico-chemical characteristics of peat, as well as the hydrology of PSFs are affected afte

50 g sulfide concentrations with purified model peat at pH 6, forming reduced organic sulfur species, an

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

52 We have developed a sphagnum peat-based compost platform for investigating plant-micr

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

54 we undertook fieldwork at LAM to sample the peat bog 30 m east of the Norse ruins for a multiproxy p

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

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

57 the seawater reference material IAEA-443, a peat bog lake, and groundwater from an experiment of in

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

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

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

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

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

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

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

65 axy deposits regularly discovered within the peat bogs of Ireland and Scotland.

66 The extensive peat bogs of Southern Scandinavia have yielded rich Meso

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

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

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

70 indicate that geologic detectors (craters in peat bogs) and space-based detectors (satellites measuri

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

72 e structure spectra revealed Sb in untreated peat bound to carboxyl or phenol groups with average Sb-

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

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

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

76 stem responses are largely driven by surface peat, but that the vast C bank at depth in peatlands is

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

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

79 agonia to calculate their long- versus short-peat C accumulation rates.

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

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

82 acrotelm rates were compared to the catotelm peat C legacies using an empirical modeling approach tha

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

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

85 Peat C/N ratios decreased whereas humification rates inc

86 n that accumulation rates in recently formed peat can be compared to those from older, deeper, peat i

87 in fact the reverse can be true because deep peat can be modified by events hundreds of years after i

88 creased C accumulation rates in near-surface peat cannot be used to infer that a peatland as a whole

89 l peatlands hold about 15%-19% of the global peat carbon (C) pool of which 77% is stored in the peat

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

91 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

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

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

94 C accumulation than deeper, millennial-aged peat (catotelm), it is difficult to project how much mor

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

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

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

98 bsorption spectroscopy (XAS) analysis of the peat confirmed that As was bound to NOM thiol groups and

99 few studies reporting the associated mass of peat consumed.

100 We found that the old peat contribution to annual methane emissions was large

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

102 An age-dated peat core collected near industries revealed that both S

103 A peat core from UTK provided a record of atmospheric depo

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

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

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

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

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

109 In this study, we analyzed two peat cores from southern Patagonia to calculate their lo

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

111 Peat cores were collected from five bogs in the vicinity

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

113 In total, six peat cores, three per study site, were studied that repr

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

115 Drying increases rates of peat decomposition and associated atmospheric and aquati

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

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

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

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

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

121 Peat deposition and preservation allows some mangroves t

122 However, effects of peat deposition in river ecosystems remain poorly unders

123 hange can cause significant soil erosion and peat deposition in rivers.

124 0.82-9.67 g/m(2) )-for the adverse impact of peat deposition on invertebrate community biodiversity.

125 Consequently, peat deposits are potential records of past atmospheric

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

127 ales of centuries to millennia to create the peat deposits.

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 ssions factors for oil palm grown on drained peat do not account for temporal variation over the plan

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

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

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

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

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

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

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

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

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

141 Conversely, the peat ecosystem was a source of carbon during both the dr

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

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

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

145 Based on the new peat extension and depth data, we estimate that tropical

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

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

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

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

150 destabilized due to severe drainage and deep peat fires.

151 te, and monothioarsenate with purified model-peat, followed by As K-edge X-ray absorption spectroscop

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

153 Tropical peat forests are a globally important reservoir of carbo

154 in contrast to the typical view of tropical peat forests which must have acted as net C sinks over t

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

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

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

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

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

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

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

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

163 from the Southern Carpathians, Romania using peat geochemistry.

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

165 Recently, near-surface peat has been used to assess the effect of current land

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

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

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

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

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

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

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

173 he AGB stocks of an OP plantation on drained peat in Malaysia from 3 to 12 years after planting using

174 ted plants was studied on 8000-year leftover peat in order to distinguish between soil-derived and at

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

176 Peat inception was dated at 2750 cal.

177 Sulfide-reacted peat increased sorption to 98%.

178 duce the temperature sensitivity (Q(10) ) of peat, indicating that these fires can inhibit microbial

179 9 ka BP), and developed in three stages: (i) peat initiated in an abandoned river channel with open w

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

181 lm, which would lead to a slower transfer of peat into the catotelm, if any.

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

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

184 can be compared to those from older, deeper, peat is mistaken - continued decomposition means that th

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

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

187 provide evidence for the role of a sediment peat layer in releasing As.

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

189 Nitrate was detected in peat layer porewater, and flow-through and batch experim

190 Our results show that the peat layer, deposited about 8,000 years ago in a paleoma

191 While surface peat layers (acrotelm) have a greater apparent rate of C

192 Although peat layers have been proposed as As sinks in earlier st

193 Peat layers within alluvial sediments are considered eff

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

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

196 lled, including blend or malt status, use of peated malt, alcohol strength, generic authentication an

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

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

199 erence for the more labile C fraction in the peat matrix.

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

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

202 Although temperature sensitivities for bulk peat methanogenesis were similar between open-water (Q(1

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

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

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

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

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

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

209 ation of microbiome community composition in peat mosses.

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

211 low for formation of Sb-sulfur precipitates, peat NOM can sequester Sb in anoxic, sulfur-enriched env

212 ould further strengthen our understanding of peat OP AGB accumulation rates.

213 One such phenotype is the production of peat, or incompletely decomposed biomass, that accumulat

214 expected to mobilize northern permafrost and peat organic carbon (PP-C), yet magnitudes and system sp

215 hich ancient carbon stores laid down as moss peat over centuries or millennia are returned to the atm

216 e offset roughly half the carbon efflux from peat oxidation.

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

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

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

220 68.35 degrees N, 19.05 degrees E), a thawing peat plateau in northern Sweden.

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

222 anee River Fulvic Acid (SRFA) standard and a peat pore water were used as representative dissolved NO

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

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

225 Interspecific variation in peat production is thought to be responsible for the est

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

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

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

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

230 These data were supplemented by peat property (bulk density, carbon and nitrogen content

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

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

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

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

235 Peat represents a globally significant pool of sequester

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

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

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

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

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

241 rect evidence of Sb sequestration in natural peat samples is lacking.

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

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

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

245 litate rapid forest recovery, stimulation of peat soil development, and resilience to sea-level rise.

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

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

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

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

250 g endothelial cells) and environmental (e.g. peat soil) samples.

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

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

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

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

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

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

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

258 Peat specific allometric equations for palm (R(2) = 0.92

259 that allows calculating the future catotelm peat storage based on today's acrotelm characteristics,

260 incubations show lower CO(2) emissions from peat subjected to low-severity fire and predict lower cu

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

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

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

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

265 < .001) between carbon accumulation rate and peat surface moisture conditions: under dry conditions,

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

267 gher reactivity of Sb(III) than Sb(V) toward peat surfaces.

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

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

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

271 exchange between the atmosphere and tropical peat swamp forest in Sarawak, Malaysia using the eddy co

272 ditional net CO(2) losses from this tropical peat swamp forest in the absence of plant acclimation to

273 s suggest that conversion of Southeast Asian peat swamp forest is contributing between 16.6 and 27.9%

274 nstrate that emissions factors for converted peat swamp forest is in the range 70-117 t CO(2) eq ha(-

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

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

277 Conversion of tropical peat swamp forest to drainage-based agriculture alters g

278 s of GHGs emitted during the conversion from peat swamp forest to oil palm plantation, accounting for

279 Tropical peat swamp forests (PSFs) are globally important carbon

280 arbon (C) pool of which 77% is stored in the peat swamp forests (PSFs) of Southeast Asia.

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

282 Southeast-Asian peat swamp forests have been significantly logged and co

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

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

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

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

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

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

289 ting, but there is little loss of underlying peat to combustion.

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

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

292 beneficial substitutions for fertilizer and peat, to its use as ADC.

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

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

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

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

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

298 weeks in aquaria containing DOM from a Carex peat with complexed mercury at initial concentrations of

299 four wheat varieties grown using soil, coco-peat with nutrient solution (CNS) and water (soaked (8 h

300 s alternative plantations and age classes on peat would further strengthen our understanding of peat