ライフサイエンスコーパス: CH4

1 CH4 fluxes were measured in situ during peak growing sea

2 ) C-methylphosphonate (MPn) resulted in (13) CH4 generation.

3 al stable isotopic methane records [delta(13)CH4 and deltaD(CH4)] from four Antarctic ice cores, whic

4 C(12) ratio in atmospheric methane (delta(13)CH4) from 1983 through 2015.

5 C emitted from the SPRUCE Bog as CH4 is <2%, CH4 represents >50% of seasonal C emissions in the highe

6 tion (100 m x 100 m) regional (10,000 km(2)) CH4 flux map of the Mackenzie Delta, Canada, based on ai

7 externality costs stem from SO2, NOx, PM2.5, CH4, fossil CO2, and NH3 emissions.

8 missions, with NT being CH4 neutral and CT a CH4 source.

9 e Mackenzie Delta, Canada, based on airborne CH4 flux data from July 2012 and 2013.

10 source that is required to close the Amazon CH4 budget.

11 Org-M decreased soil N2O emission by 13% and CH4 emission by 12%, and increased soil CO2 emission by

12 ially the bis(silyl)acetal, H2C(OSiR3)2, and CH4 (R3SiH = PhSiH3, Et3SiH, and Ph3SiH).

13 sing during the period from 1983 to 2012 and CH4 was the main GHG emitted from penguin colonies.

14 tive facility-scale losses (0.09-0.34%), and CH4 emissions from both NGPPs and refineries were more s

15 validated experimentally with H2, N2, Ar and CH4 on three classes of microporous materials: trapdoor

16 s of CO2 hydrogenation to C1 (CO, CH3OH, and CH4) compounds on metal/oxide catalysts.

17 strategy to fine tune the pore chemistry and CH4 -storage performance of a family of isomorphic MOFs

18 riods using satellite measurements of CO and CH4, nearly twice the decrease expected from prior estim

19 nthesized in a one-step process from CO2 and CH4 at room temperature (30 degrees C) and atmospheric p

20 d that DPH treatments increased both CO2 and CH4 emission.

21 For paddy soils, N2O, CO2 and CH4 emissions differed by -3%, -36% and +84% between Org

22 ng to positive Tw-Ta, it can enhance CO2 and CH4 emissions from inland waters, thereby contributing t

23 The results showed that N2O, CO2 and CH4 emissions were significantly affected by Org-M compa

24 ance measurements of whole-ecosystem CO2 and CH4 exchange to estimate GHG fluxes and associated radia

25 eep Peat Heat", DPH) on peat surface CO2 and CH4 fluxes.

26 global change will influence surface CO2 and CH4 fluxes.

27 s revealed that the evasion rates of CO2 and CH4 in tributaries of the rivers of the plateau were hig

28 eruptions released large amounts of CO2 and CH4 into the atmosphere, causing severe global warming a

29 on in the temperature sensitivity of CO2 and CH4 production and increased peat aerobicity due to enha

30 acclimation was tested by monitoring CO2 and CH4 production, CUE, and microbial biomass.

31 mulates cumulative gaseous C-loss as CO2 and CH4 to >150% of the control.

32 gly negative Tw-Ta, thereby reducing CO2 and CH4 transfer velocities from inland waters into the atmo

33 carbon and release carbon dioxide (CO2 ) and CH4 .

34 n fact, the (14) C content of DOC, CO2 , and CH4 across the entire peat profile was considerably enri

35 e (<60 years), despite stream DOC, CO2 , and CH4 primarily being sourced from deep peat horizons (2-4

36 the climate by increasing levels of CO2 and CH4.

37 gest that parameter uncertainties in CUE and CH4 -C:CO2 -C ratios have a larger impact on long-term s

38 to yield, inorganic As content in grain, and CH4 emissions.

39 For each subject, we measured exhaled H2 and CH4, oro-anal transit time, and the severity of psycholo

40 Soil N2 O and CH4 fluxes were measured for five crop-years (2011-2015)

41 mediator, and enhanced electron transfer and CH4 production.

42 sing rice biomass by 10% could reduce annual CH4 emissions from Chinese rice agriculture by 7.1%.

43 ologic hotspots contribute 17% to the annual CH4 emission estimate of our study area.

44 haw depth were copredictors for C. aquatilis CH4 flux.

45 d values, but substantially smaller per-area CH4 emissions, highlighting the need for improvements in

46 As CH4 is a powerful greenhouse gas with 34 times the warmi

47 quantity of C emitted from the SPRUCE Bog as CH4 is <2%, CH4 represents >50% of seasonal C emissions

48 o have significantly altered land-atmosphere CH4 emissions for this region, potentially acting as a p

49 is an important pathway for land-atmosphere CH4 emissions, but the magnitude, timing, and environmen

50 21st century as indicated by an atmospheric CH4 and CO2 concentration model.

51 s adjacent to the trees consumed atmospheric CH4 at a rate of -4.52 +/- 0.64 mumol CH4 m(-2 ) soil h(

52 a steady but only minor role in atmospheric CH4 changes and that the glacial budget is not dominated

53 ower decadal mean growth rate in atmospheric CH4 concentrations throughout the 1980s and 1990s and to

54 face networks started monitoring atmospheric CH4 mole fractions.

55 he 1980s and 1990s and to stable atmospheric CH4 concentrations from 1999 to 2006, resulting in negat

56 Average CH4 emission rates (NGPPs: 140 +/- 70 kg/h; refineries:

57 mass balance method, we calculate an average CH4 flux of 0.54 +/- 0.20 Tgyr(-1) (1sigma), in close ag

58 prised <1% of total emissions, with NT being CH4 neutral and CT a CH4 source.

59 mperature, composition) behaviour of binary (CH4 + C3H8) and (Ar + CO2) mixtures over the temperature

60 O2 pre-enriched inoculum enhanced biocathode CH4 production, although the archaeal communities in bot

61 Thus, ZVI may be used to increase biocathode CH4 production, assist in the start-up of an electrometh

62 e CH4 budget in addition to recent, biogenic CH4 is uncertain.

63 ommon intermediate for the formation of both CH4 and C2H4 These results suggest that, to obtain hydro

64 ropores that selectively exclude the bulkier CH4 molecules.

65 Both delta(13)C-CH4 and deltaD-CH4 correspond to the isotopic compositio

66 Progressive enrichment of both delta(13)C-CH4 and deltaD-CH4 is observed with increasing distance

67 ces are characterised by specific delta(13)C-CH4 signatures, so high precision stable isotope analysi

68 emission inventories and updated delta(13)C-CH4 signatures.

69 L (n = 12) were all found to have delta(13)C-CH4 values larger than -30 per thousand, typical of a th

70 of several small gases (H2, D2, Ne, N2, CO, CH4, C2H6, Ar, Kr, and Xe) on the metal-organic framewor

71 ter diffusion and ebullition fluxes of CO2 , CH4 , and N2 O from a restored emergent marsh ecosystem.

72 tivities are seen in CCMM membranes for CO2 /CH4 , N2 /CH4 , He/CH4 , and H2 /CH4 separations.

73 f the first to incorporate stream GHGs (CO2, CH4 and N2O) concentrations and emissions in rivers of t

74 e flux of gas, the calculated fluxes of CO2, CH4 and N2O (3,452 mg-C m(2) d(-1), 26.7 mg-C m(2) d(-1)

75 rnality costs are based on emissions of CO2, CH4, N2O, PM2.5, PM10, NOx, SO2, VOC, CO, NH3, Hg, Pb, C

76 of the rivers were supersaturated with CO2, CH4 and N2O during the study period.

77 nds for O2/N2, H2/N2, CO2/N2, H2/CH4 and CO2/CH4, with the potential for biogas purification and carb

78 gh-yielding rice cultivars strongly decrease CH4 emissions from paddy soils with high organic C conte

79 sults provide insight into a way to decrease CH4 production and increase CE using FAN to control the

80 g CO2 -eq m(-2) mostly because of decreased CH4 emissions, while N deposition reduced GWP from 21.0

81 GeoChip analysis revealed that decreased CH4 production potential, rather than increased CH4 oxid

82 a displays an exceptionally high deliverable CH4 capacity of 208 v/v between 5 and 80 bar at room tem

83 high gravimetric and volumetric deliverable CH4 capacities of 0.24 g g(-1) and 163 vol/vol (298 K, 5

84 pic methane records [delta(13)CH4 and deltaD(CH4)] from four Antarctic ice cores, which provide impro

85 Based on our deltaD(CH4) constraint, it seems that geologic emissions of met

86 Both delta(13)C-CH4 and deltaD-CH4 correspond to the isotopic composition of the gas re

87 enrichment of both delta(13)C-CH4 and deltaD-CH4 is observed with increasing distance and decreasing

88 bes a new C-H bond activation pathway during CH4-CO2 reactions on oxophilic Ni-Co and Co clusters, un

89 ically relevant step leads to more effective CH4 turnovers and complete elimination of coke depositio

90 ) and were prepared with the goal to enhance CH4 working capacity.

91 The average estimated CH4 and N2O emissions tended to be increasing during the

92 Here we examine CH4 emission dynamics in six Pacific Northwest U.S. rese

93 Both MFM-112a and MFM-115a show excellent CH4 uptakes of 236 and 256 cm(3) (STP) cm(-3) (v/v) at 8

94 negatively with microbial richness, exhaled CH4, presence of methanogens, and enterotypes enriched w

95 stems of high-yielding cultivars facilitated CH4 oxidation by promoting O2 transport to soils.

96 e nature of the silane, with PhSiH3 favoring CH4, and Ph3SiH favoring the bis(silyl)acetal, H2C(OSiPh

97 O2, He, Ar, 2% for Kr, 8% for Xe, and 3% for CH4, N2O and Ne.

98 best performing metal-organic frameworks for CH4 storage.

99 usion, possibly increasing the potential for CH4 oxidation and leading to a decrease in net CH4 fluxe

100 recently that soils are the sole surface for CH4 exchange in upland forests.

101 structure and cation size, whereas that for CH4 does not.

102 ersion of adsorbed formate, whereas that for CH4 formation is the hydrogenation of adsorbed carbonyl.

103 direct plasma synthesis of acetic acid from CH4 and CO2 is an ideal reaction with 100 % atom economy

104 modynamics favour the production of CO2 from CH4, while abiotic methane synthesis would require the o

105 t biomass was a strong predictor of A. fulva CH4 flux while water depth and thaw depth were copredict

106 Furthermore, CH4 production by the ZVI-amended biocathodes remained e

107 ite to meaningful predictions of near-future CH4 release in the Arctic.

108 growing season increase of 0.034 +/- 0.007 g CH4 m(-2) yr(-1) in landscape CH4 emissions.

109 (May-October) wetland CH4 emission of 13 g CH4 m(-2) is the dominating contribution to the landscap

110 bution to the landscape CH4 emission of 7 g CH4 m(-2) .

111 ctic, may see increased emission of geologic CH4 in the future, in addition to enhanced microbial CH4

112 on recent air and soil temperature, geologic CH4 was produced over millions of years and can be relea

113 es for CO2 /CH4 , N2 /CH4 , He/CH4 , and H2 /CH4 separations.

114 ubsurface environments, and we show that H2, CH4, and CO feature prominently in many of their predict

115 on upper bounds for O2/N2, H2/N2, CO2/N2, H2/CH4 and CO2/CH4, with the potential for biogas purificat

116 n CCMM membranes for CO2 /CH4 , N2 /CH4 , He/CH4 , and H2 /CH4 separations.

117 The higher CH4 production could not be fully explained by complete

118 production would likely contribute to higher CH4 emissions, unless effective strategies to mitigate G

119 ), which has previously been used to improve CH4 production in anaerobic digesters, has not been expl

120 te species-specific decadal-scale changes in CH4 fluxes.

121 rease of 10% resulted in a 10.3% decrease in CH4 emissions in a soil with a high carbon (C) content.

122 re, we quantify the thaw-induced increase in CH4 emissions for a boreal forest-wetland landscape in t

123 A 60% increase in CH4 flux was estimated from the observed plant biomass a

124 lorophyll a] experienced larger increases in CH4 emission in response to drawdown (R(2) = 0.84, p < 0

125 that warming in boreal regions may increase CH4 emissions from peatlands and result in a positive fe

126 production potential, rather than increased CH4 oxidation potential, may lead to the reduction in ne

127 the positive radiative forcing of increasing CH4 emissions until the end of the 21st century as indic

128 Thus, thaw-induced CH4 emission increases likely exert a positive net radia

129 ipulation on an Arctic floodplain influences CH4 -associated microorganisms, soil thermal regimes, an

130 drylands had 36% higher emission intensity (CH4 emissions/km(2) ) compared to that in nondrylands in

131 To our knowledge, CH4-based heterodimers have not been previously reported

132 Landscape CH4 emissions are most sensitive to this ratio during pe

133 34 +/- 0.007 g CH4 m(-2) yr(-1) in landscape CH4 emissions.

134 x footprint modeling, we find that landscape CH4 emissions increase with increasing wetland-to-forest

135 the dominating contribution to the landscape CH4 emission of 7 g CH4 m(-2) .

136 contrast, forest contributions to landscape CH4 emissions appear to be negligible.

137 'bottom-up' estimates, indicating that large CH4 emissions from trees adapted to permanent or seasona

138 s likely responsible for the 3.8-fold larger CH4 production rate observed in the EHM-biocathode.

139 increased by 2-8%, with a best-estimate LGM CH4 concentration of 463-480 p.p.b.v.

140 We show that in this model, the global LGM CH4 source was reduced by 28-46%, and the lifetime incre

141 Drainage lowered CH4 fluxes by a factor of 20 during the growing season,

142 is not only detected as [M+NH4](+) but as [M-CH4+NH4](+) and [M-C2H4+NH4](+) as well.

143 between 2010 and 2015, suggesting that major CH4 sources did not change appreciably.

144 2.9-fold higher, respectively, than the mean CH4 production in the four prior cycles without ZVI addi

145 Therefore, we measured CH4 and CO2 emissions at three NGPPs and three refinerie

146 Plant-mediated CH4 flux is an important pathway for land-atmosphere CH4

147 Methane (CH4 ) emissions from tropical wetlands contribute 60%-80

148 Methane (CH4) is a potent greenhouse gas and the primary componen

149 Methane (CH4) is a powerful greenhouse gas and plays a key part i

150 n (DOC), carbon dioxide (CO2 ), and methane (CH4 ) exported from a boreal peatland catchment coupled

151 uring soil nitrous oxide (N2 O) and methane (CH4 ) fluxes and SOC changes (DeltaSOC) at a long-term,

152 e rate of carbon-dioxide (CO2 ) and methane (CH4 ) production.

153 ide (N2O), carbon dioxide (CO2) and methane (CH4) emissions to manure (Org-M) in comparison to chemic

154 tential for nitrous oxide (N2O) and methane (CH4) generation in dissolved form at the base of laborat

155 ide (CO2), nitrous oxide (N2O), and methane (CH4) requires days of integration time with largest spac

156 ally give [Zr]-O(H)-B(H)(C6F5)2 and methane (CH4).

157 he substrate's electrons ends up as methane (CH4) through hydrogenotrophic methanogenesis, an outcome

158 NTP-assisted methane (CH4 ) oxidation over Pd/Al2 O3 was investigated by direc

159 udgets ascribe 4-10% of atmospheric methane (CH4 ) sinks to upland soils and have assumed until recen

160 in recent variations in atmospheric methane (CH4) concentrations.

161 Atmospheric methane (CH4) records reconstructed from polar ice cores represen

162 Atmospheric methane (CH4) varied with climate during the Quaternary, rising f

163 argest global source of atmospheric methane (CH4), a potent greenhouse gas.

164 yr(-1) ) on carbon dioxide (CO2 ), methane (CH4 ) and nitrous oxide (N2 O) fluxes as well as the und

165 Carbon dioxide (CO2 ), methane (CH4 ), and nitrous oxide (N2 O) are the three most impor

166 exchange of carbon dioxide (CO2 ), methane (CH4 ), and nitrous oxide (N2 O).

167 e East Siberian Arctic Shelf (ESAS) methane (CH4) emissions, yet these factors still require assessme

168 caps vast amounts of old, geologic methane (CH4) in subsurface reservoirs.

169 s is expected to increase landscape methane (CH4 ) emissions.

170 , regional variation and drivers of methane (CH4 ) emission remain unclear.

171 Biogenic production and release of methane (CH4 ) from thawing permafrost has the potential to be a

172 globally significant quantities of methane (CH4 ), and are highly sensitive to climate change.

173 is high uncertainty in estimates of methane (CH4) emissions from natural gas-fired power plants (NGPP

174 e timing and magnitude of reservoir methane (CH4) fluxes to the atmosphere.

175 ncreasing rice growth can stimulate methane (CH4 ) emissions, exacerbating global climate change, as

176 estricted salt marshes, substantial methane (CH4) and CO2 emission reductions can be achieved through

177 nversion of carbon dioxide (CO2) to methane (CH4) with application to biogas upgrading.

178 rt carbon dioxide (CO2) directly to methane (CH4), promise to be an innovative technology for anaerob

179 Natural gas (methane, CH4) is widely considered as a promising energy carrier

180 he future, in addition to enhanced microbial CH4 production.

181 Whereas microbial CH4 production largely depends on recent air and soil te

182 was 0.153 +/- 0.010 and 0.586 +/- 0.029 mmol CH4/mg biomass-day, respectively.

183 ese drainage-induced changes may then modify CH4 fluxes in the growing and nongrowing seasons.

184 ant livestock had increased by 332% (73.6 MT CH4 or 2.06 Gt CO2 -eq) since the 1890s.

185 issions in 2014 was 97.1 million tonnes (MT) CH4 or 2.72 Gigatonnes (Gt) CO2 -eq (1 MT = 10(12) g, 1

186 pheric CH4 at a rate of -4.52 +/- 0.64 mumol CH4 m(-2 ) soil h(-1) (P < 0.0001).

187 om May to September were 1.59 +/- 0.88 mumol CH4 m(-2 ) stem h(-1) (mean +/- 95% confidence interval)

188 re seen in CCMM membranes for CO2 /CH4 , N2 /CH4 , He/CH4 , and H2 /CH4 separations.

189 cooler climate on wetlands and other natural CH4 sources.

190 may have briefly changed the forest to a net CH4 source.

191 ed wetland and landscape eddy covariance net CH4 flux measurements in combination with flux footprint

192 ose of CH4 oxidation, thereby decreasing net CH4 fluxes.

193 potential, may lead to the reduction in net CH4 emissions, and decreased nitrification potential and

194 4 oxidation and leading to a decrease in net CH4 fluxes compared to a control site.

195 is and methanotrophy, thereby increasing net CH4 fluxes to the atmosphere, should be a focus of futur

196 thaw-lake taliks would freeze; therefore, no CH4 release would occur for millennia.

197 In contrast, we observed CH4 emissions increased by 10% in the drained areas duri

198 >99% of CO2 and N2 O emissions, and 71% of CH4 emissions.

199 improvement in adsorption and activation of CH4 and catalytic performance.

200 Isotopic analysis of CH4 showed a dominance of acetoclastic production in fre

201 ntly underestimate the atmospheric burden of CH4 determined via remote sensing and inversion modellin

202 ep peat warming increased the delta(13) C of CH4 suggesting an increasing contribution of acetoclasti

203 we provide a 'top-down' regional estimate of CH4 emissions of 42.7 +/- 5.6 teragrams of CH4 a year fo

204 r II guidelines to quantify the evolution of CH4 emissions from ruminant livestock during 1890-2014.

205 Due to this decrease, a higher fraction of CH4 was alternatively emitted to the atmosphere by diffu

206 Total global warming potential (GWP) of CH4 and N2O emissions was 5303 kg CO2-eq in 1983 and 656

207 4 originates from the carbon and hydrogen of CH4, which sequentially reduce SnO2.

208 Stable carbon isotopes of CH4 and CO2 further indicated the possibility of differe

209 y on fluctuations in either the magnitude of CH4 sources or CH4 atmospheric lifetime, or both.

210 , experiments based on a microwave plasma of CH4 have been performed.

211 ducing agent, as the total reducing power of CH4 originates from the carbon and hydrogen of CH4, whic

212 The atomic-level process of CH4-SnO2 interaction and temperature-dependent reduction

213 Production of CH4 also commenced quickly but continued throughout the

214 is seems problematic because the reaction of CH4 and water to generate methanol and H2 is highly unfa

215 in, the largest natural geographic source of CH4 in the tropics, consistently underestimate the atmos

216 Arctic wetlands are large sources of CH4 , and investigating effects of soil hydrology on CH4

217 s and oil refineries may be large sources of CH4 emissions and could contribute significantly (0.61 +

218 f CH4 emissions of 42.7 +/- 5.6 teragrams of CH4 a year for the Amazon basin, based on regular vertic

219 it 15.1 +/- 1.8 to 21.2 +/- 2.5 teragrams of CH4 a year, in addition to the 20.5 +/- 5.3 teragrams a

220 s of methanogenesis while elevating those of CH4 oxidation, thereby decreasing net CH4 fluxes.

221 However, greater values of CH4 -C:CO2 -C ratios lead to a greater global warming po

222 4 +/- 0.6 kt CO2 -eq yr(-1) ) did not offset CH4 emission (3.7 +/- 0.03 kt CO2 -eq yr(-1) ), producin

223 e magnitude and species-specific controls on CH4 flux.

224 hication magnifies the effect of drawdown on CH4 emission.

225 ns to investigate the impacts of the ENSO on CH4 emissions in tropical wetlands for the period from 1

226 f the El Nino-Southern Oscillation (ENSO) on CH4 emissions from wetlands remains poorly quantified at

227 However, effects of such fluctuations on CH4 emissions have received limited attention.

228 d investigating effects of soil hydrology on CH4 fluxes is of great importance for predicting ecosyst

229 to N2 O sources, but had little influence on CH4 emissions.

230 y, we successfully built several new CH3- or CH4-based heterodimers that may prove useful for designi

231 potential for substantial release of N2O or CH4 in biofilter effluent appears relatively low.

232 rent from that of simpler targets like Ne or CH4, which is not the case for fluorene.

233 ns in either the magnitude of CH4 sources or CH4 atmospheric lifetime, or both.

234 ity and high binary CO2-over-N2 and CO2-over-CH4 selectivity, suitable for CO2 capture from flue gas

235 g cultivars can substantially mitigate paddy CH4 emission in China and other rice growing regions.

236 noncombustion-related equipment as potential CH4 sources.

237 ach is applied to a use-case for quantifying CH4 emission from an oil field south of San Ardo, CA, an

238 high-yielding rice cultivars actually reduce CH4 emissions from typical paddy soils.

239 that long-term drainage considerably reduced CH4 fluxes through modified ecosystem properties.

240 hanotrophic bacteria, which may have reduced CH4 cycling.

241 Our results showed that WTL reduced CH4 emissions by 57.4% averaged over three growing seaso

242 -based climate change intervention, reducing CH4 emissions is an entirely distinct concept from biolo

243 and trees is the dominant source of regional CH4 emissions.

244 account for two-thirds of the total regional CH4 flux of the Barrow Peninsula.

245 These MOFs show remarkable CH4 and CO2 adsorption properties, notably with simultan

246 Here we report CH4 fluxes from the stems of 2,357 individual Amazonian

247 ccount for more than 90% of annual reservoir CH4 flux in a period of just a few weeks.

248 orarily, greatly increase per-area reservoir CH4 fluxes to the atmosphere, and can account for more t

249 Here, we infer India's CH4 emissions for the period 2010-2015 using a combinati

250 sions offset 1-6% of the growing season soil CH4 sink and may have briefly changed the forest to a ne

251 ed diurnal patterns in the rate of tree-stem CH4 emissions.

252 ed with the previous satellite study suggest CH4 emissions have not changed.

253 ction temperature and the amount of supplied CH4.

254 d contribute significantly (0.61 +/- 0.18 Tg CH4/yr, 95% CL) to U.S. emissions.

255 hat fossil fuels contribute between 12-19 Tg CH4 per year to the recent atmospheric methane increase,

256 uivalent to net emissions increase of 25 Tg CH4 per year.

257 ions of methane decreased by 3.7 (+/-1.4) Tg CH4 per year from the 2001-2007 to the 2008-2014 time pe

258 tory-scale experimental study confirmed that CH4 actively reduces SnO2, producing 99.34% high-purity

259 We found that CH4 was a highly efficient and a versatile reducing agen

260 Here we report that CH4 is emitted from the stems of dominant tree species i

261 The results show that CH4 emissions from tropical wetlands respond strongly to

262 Our estimate shows that CH4 emissions from the ruminant livestock had increased

263 tively separated from the raw biogas and the CH4 content in the outlet reached as high as 97.0 +/- 0.

264 Moreover, as a result of the CH4 reduction of SnO2, a mixture of CO and H2 was produc

265 In particular, the CH4 working capacity of NJU-Bai 43 reaches 198 cm(3) (ST

266 In this work, we quantify the CH4 flux from the SJB using continuous atmospheric sampl

267 Here we report the CH4 storage properties in a family of isostructural (3,2

268 i 43) were prepared and we observed that the CH4 volumetric working capacity and volumetric uptake va

269 ogic emissions and their contribution to the CH4 budget in addition to recent, biogenic CH4 is uncert

270 The 'CH4 oversaturation paradox' has been observed in oxygen-

271 ise was insufficient to activate the thermal CH4 oxidation reaction.

272 Thawing permafrost opens pathways for this CH4 to migrate to the surface.

273 y of the electrocatalytic reduction of CO to CH4 and C2H4 on copper electrodes prevents a straightfor

274 ative mineralization of organic compounds to CH4 and CO2 .

275 g of the contribution of these ecosystems to CH4 emissions.

276 s and carbonyls governs the selectivities to CH4 and CO.

277 MPn metabolism contributes significantly to CH4 oversaturation in Yellowstone Lake and likely other

278 functionally active for N2-to-NH3 and CN-to-CH4/NH3 conversion, respectively, when subjected to prot

279 L and 2 g/L yielded 123% and 231% more total CH4 than in the non-ZVI cycles, respectively.

280 We estimate that total CH4 emissions in 2014 was 97.1 million tonnes (MT) CH4 o

281 Africa, Asia and Latin America) to the total CH4 emissions had increased from 51.7% in the 1890s to 7

282 The total CH4 produced during a 7-day feeding cycle with 1 and 2 g

283 tion of acetoclastic methanogenesis to total CH4 production with warming.

284 we find evidence of an increase in tropical CH4 emissions of approximately 6-9 TgCH4 yr(-1) during t

285 based on regular vertical lower-troposphere CH4 profiles covering the period 2010-2013.

286 At NGPPs, the percentage of unburned CH4 emitted from stacks (0.01-0.08%) was much lower than

287 of San Ardo, CA, and compared to a bottom-up CH4 emission estimate.

288 sorption capacities and different CO2 versus CH4 selectivities.

289 mediating approximately half of all wetland CH4 emissions in the Amazon floodplain, a region that re

290 Decreased wetland CH4 emissions can act as a negative feedback mechanism f

291 use a process-based model of global wetland CH4 emissions to investigate the impacts of the ENSO on

292 esents up to one-third of the global wetland CH4 source when trees are combined with other emission s

293 contribute 60%-80% of global natural wetland CH4 emissions.

294 ulative growing season (May-October) wetland CH4 emission of 13 g CH4 m(-2) is the dominating contri

295 me lag was detected between tropical wetland CH4 emissions and ENSO events, which was caused by the c

296 ve much stronger effects on tropical wetland CH4 emissions than the changes in precipitation during E

297 interannual variations for tropical wetland CH4 emissions.

298 onality was minor for CO2 emissions, whereas CH4 and N2 O fluxes displayed strong and asynchronous se

299 mples were dominated by taxa affiliated with CH4 oxidizing, fermenting and SO42- reducing lineages.

300 The reappearance of C2H4 along with CH4 at U less than -0.85 V arises from *CHO formation pr

301 The conversion of CO2 with CH4 into liquid fuels and chemicals in a single-step cat