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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

23 global change will influence surface CO2 and CH4 fluxes.

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

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

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

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

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

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

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

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

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

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

34 the climate by increasing levels of CO2 and CH4.

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

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

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

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

39 mediator, and enhanced electron transfer and CH4 production.

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

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

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

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

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

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

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

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

48 21st century as indicated by an atmospheric CH4 and CO2 concentration model.

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

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

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

52 face networks started monitoring atmospheric CH4 mole fractions.

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

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

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

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

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

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

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

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

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

62 Breath CH4 analysis may offer a noninvasive approach to follow

63 re accompanied by parallel changes in breath CH4 output.

64 ropores that selectively exclude the bulkier CH4 molecules.

65 We use a dataset of delta(13)C(CH4) from >1600 produced shale gas samples from regions

66 2008 has volume-weighted-average delta(13)C(CH4) of -39.6 per mille.

67 ribute to an opposite atmospheric delta(13)C(CH4) signal in the observed decrease since 2008 (while n

68 have relied on poorly constrained delta(13)C(CH4) source signatures.

69 The average delta(13)C(CH4) weighted by US basin-level measured emissions in 20

70 n its (13)C/(12)C isotopic ratio (delta(13)C(CH4)) from -47.1 per mille to -47.3 per mille observed s

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

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

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

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

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

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

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

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

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

80 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)

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

99 n splanchnic circulatory changes and exhaled CH4 in an attempt to recognize intestinal perfusion fail

100 The concentration of exhaled CH4 was measured online simultaneously with high-sensiti

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

102 87% and 69% of the total variance of daily F(CH4) could be explained by the random forest machine lea

103 easurements of ecosystem-scale CH(4) flux (F(CH4) ) from mangrove ecosystems.

104 Meanwhile, we showed that mangrove F(CH4) could offset the negative radiative forcing caused

105 Our results showed that daily mangrove F(CH4) reached a peak of over 0.1 g CH(4) -C m(-2) day(-1)

106 f its kind to characterize ecosystem-scale F(CH4) in a mangrove wetland with long-term eddy covarianc

107 and biophysical drivers of ecosystem-scale F(CH4) in a subtropical estuarine mangrove wetland based o

108 ure and low salinity, while the wintertime F(CH4) was negligible.

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

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

111 best performing metal-organic frameworks for CH4 storage.

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

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

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

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

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

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

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

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

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

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

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

123 ibution to the landscape CH4 emission of 7 g CH4 m(-2) .

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

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

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

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

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

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

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

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

132 lated significantly with parallel changes in CH4 concentration in the exhaled air (Pearson's r = 0.66

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

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

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

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

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

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

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

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

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

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

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

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

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

146 34 +/- 0.007 g CH4 m(-2) yr(-1) in landscape CH4 emissions.

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

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

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

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

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

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

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

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

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

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

157 2.9-fold higher, respectively, than the mean CH4 production in the four prior cycles without ZVI addi

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

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

160 Methane (CH4) breath test is an established diagnostic method for

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

196 cooler climate on wetlands and other natural CH4 sources.

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

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

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

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

201 4 oxidation and leading to a decrease in net CH4 fluxes compared to a control site.

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

203 nteric ischemia or before reperfusion in non-CH4 producer rats to test the appearance of the gas in t

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

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

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

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

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

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

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

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

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

213 4 originates from the carbon and hydrogen of CH4, which sequentially reduce SnO2.

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

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

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

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

218 Production of CH4 also commenced quickly but continued throughout the

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

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

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

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

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

224 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

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

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

227 4 +/- 0.6 kt CO2 -eq yr(-1) ) did not offset CH4 emission (3.7 +/- 0.03 kt CO2 -eq yr(-1) ), producin

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

229 hication magnifies the effect of drawdown on CH4 emission.

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

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

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

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

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

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

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

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

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

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

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

241 noncombustion-related equipment as potential CH4 sources.

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

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

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

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

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

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

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

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

250 In the first series, CH4 was administered intraluminally into the ileum befor

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

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

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

254 ction temperature and the amount of supplied CH4.

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

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

257 quivalent to net emissions increase of 25 Tg CH4 per year.

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

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

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

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

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

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 contrib

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

296 interannual variations for tropical wetland CH4 emissions.

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

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

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

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