The Impact of Nitrogen Placement and Tillage on NO, N2O, CH4 and CO2 Fluxes from a Clay Loam Soil

To evaluate the impact of N placement depth and no-till (NT) practice on the emissions of NO, N₂O, CH₄ and CO₂ from soils, we conducted two N placement experiments in a long-term tillage experiment site in northeastern Colorado in 2004. Trace gas flux measurements were made 2–3 times per week, in zero-N fertilizer plots that were cropped continuously to corn (Zea mays L.) under conventional-till (CT) and NT. Three N placement depths, replicated four times (5, 10 and 15 cm in Exp. 1 and 0, 5 and 10 cm in Exp. 2, respectively) were used. Liquid urea–ammonium nitrate (UAN, 224 kg N ha⁻¹) was injected to the desired depth in the CT- or NT-soils in each experiment. Mean flux rates of NO, N₂O, CH₄ and CO₂ ranged from 3.9 to 5.2 μg N m⁻² h⁻¹, 60.5 to 92.4 μg N m⁻² h⁻¹, −0.8 to 0.5 μg C m⁻² h⁻¹, and 42.1 to 81.7 mg C m⁻² h⁻¹ in both experiments, respectively. Deep N placement (10 and 15 cm) resulted in lower NO and N₂O emissions compared with shallow N placement (0 and 5 cm) while CH₄ and CO₂ emissions were not affected by N placement in either experiment. Compared with N placement at 5 cm, for instance, averaged N₂O emissions from N placement at 10 cm were reduced by more than 50% in both experiments. Generally, NT decreased NO emission and CH₄ oxidation but increased N₂O emissions compared with CT irrespective of N placement depths. Total net global warming potential (GWP) for N₂O, CH₄ and CO₂ was reduced by deep N placement only in Exp. 1 but was increased by NT in both experiments. The study results suggest that deep N placement (e.g., 10 cm) will be an effective option for reducing N oxide emissions and GWP from both fertilized CT- and NT-soils.     

Effects of site preparation for afforestation on methane fluxes at Harwood Forest,NE England

A field experiment was established at Harwood Forest to investigate the effects of three forest management practises (drainage, mounding and fertilisation) on methane (CH₄) emissions and environmental variables (soil temperature, soil moisture content, water table depth) from 2006 to 2008. The relationship between CH₄ emissions and environmental variables was also evaluated. The experiment was laid out in a factorial split-plot design on grassland in a peaty gley soil. Drainage increased daytime soil temperature at all depths. Mounding increased soil temperature at 1 and 5 cm depth. Soil moisture content was decreased by drainage and mounding. All practises affected soil CH₄ emissions with drainage reducing emissions by 57–76% and mounding and fertilisation increasing emissions by 34–59 and 20–59%, respectively. Water table depth was the major factor controlling CH₄ emissions.     

Seasonal variation in pathways of CH4 production and in CH4 oxidation in rice fields determined by stable carbon isotopes and specific inhibitors

Flooded rice fields, which are an important source of the atmospheric methane, have become a model system for the study of interactions between various microbial processes. We used a combination of stable carbon isotope measurements and application of specific inhibitors in order to investigate the importance of various methanogenic pathways and of CH₄ oxidation for controlling CH₄ emission. The fraction of CH₄ produced from acetate and H₂/CO₂ was calculated from the isotopic signatures of acetate, carbon dioxide (CO₂) and methane (CH₄) measured in porewater, gas bubbles, in the aerenchyma of the plants and/or in incubation experiments. The calculated ratio between both pathways reflected well the ratio determined by application of methyl fluoride (CH₃F) as specific inhibitor of acetate‐dependent methanogenesis. Only at the end of the season, the theoretical ratio of acetate: H₂ = 2 : 1 was reached, whereas at the beginning H₂/CO₂‐dependent methanogenesis dominated. The isotope discrimination was different between rooted surface soil and unrooted deep soil. Root‐associated CH₄ production was mainly driven by H₂/CO₂. Porewater CH₄ was found to be a poor proxy for produced CH₄. The fraction of CH₄ oxidised was calculated from the isotopic signature of CH₄ produced in vitro compared to CH₄ emitted in situ, corrected for the fractionation during the passage from the aerenchyma to the atmosphere. Isotope mass balances and in situ inhibition experiments with difluoromethane (CH₂F₂) as specific inhibitor of methanotrophic bacteria agreed that CH₄ oxidation was quantitatively important at the beginning of the season, but decreased later. The seasonal pattern was consistent with the change of potential CH₄ oxidation rates measured in vitro. At the end of the season, isotope techniques detected an increase of oxidation activity that was too small to be measured with the flux‐based inhibitor technique. If porewater CH₄ was used as a proxy of produced CH₄, neither magnitude nor seasonal pattern of in situ CH₄ oxidation could be reproduced. An oxidation signal was also found in the isotopic signature of CH₄ from gas bubbles that were released by natural ebullition. In contrast, bubbles stirred up from the bulk soil had preserved the isotopic signature of the originally produced CH₄.     

Spatial and temporal variations of dissolved gases (CH4, CO2, and O2) in peat cores

Spatial and temporal variations in the concentrations of dissolved gases (CH₄, CO₂, and O₂) in peat cores were studied using membrane inlet mass spectrometry (MIMS). Variations in vertical gas profiles were observed between random peat cores taken from hollows on the same peat bog. Methane concentrations in profiles (0–30 cm) generally increased with depth and reached maximum values in the range of 200–450 m CH₄ below about 13-cm depth. In some profiles, a peak of dissolved methane was observed at 7-cm depth. Oxygen penetrated to approximately 2-cm depth in the hollows. The sampling probe was used to continuously monitor CH₄, CO₂, and O₂ concentrations at fixed depths in peat cores over periods of several days. The concentration of dissolved CO₂ and O₂ at 1-cm depth oscillated over a 24-h period with the maximum of CO₂ concentration corresponding with the minimum of 0₂. Diurnal variations in CO₂ but not CH₄ were measured at 15-cm depth; dissolved CO₂ levels decreased during daylight hours to a constant minimum concentration of 4.85 mm. This report also describes the application of MIMS for the measurement of gaseous diffusion rates in peat using an inert gas (argon); the value of D, the diffusion coefficient, was 2.07 × 10^–8 m² s^–1. Correspondence to: D. Lloyd     

Experimental Test of a Mechanistic Model of Production, Flux and Gas Bubble Zonation in Non-vegetated Flooded Rice Field Soil

Anoxic wetlands are an important source for the greenhouse gas CH₄, much of which is emitted in form of gas bubbles. The conditions for formation of gas bubbles have recently been described by an analytical model, which allows the prediction of fluxes by first physical principles using the knowledge of gas concentration profiles and/or gas production rates. We tested parts of this model by experiments using microcosms of flooded, non-vegetated and homogeneous rice field soil incubated under different gas atmospheres and at different temperatures. In these experiments we determined rates of CH₄ and CO₂ production, upper boundaries of the bubble zone, gas-filled porosities and vertical profiles of dissolved CH₄, CO₂ and N₂. The results of our experiments confirmed that by knowing only one of the following parameters, i.e. CH₄ production, diffusive CH₄ flux and depth of upper boundary of bubble zone, the remainder could be predicted from the model. On average, predicted values differed from experimental ones by a factor of 0.4 –2.7, depending on which parameter was taken as an input for the model. It was possible to predict the percentage of gas bubble flux from measured CH₄ emission rates under the experimental conditions, which was on the order of 90%. The confrontation of the model with experimental data showed that the effect of the shallow upper oxic layer on bubble formation was negligible and that the CH₄ diffusive flux is easily underestimated by experiments lacking sufficient spatial resolution. Therefore, CH₄ production rates lower than in our microcosms would allow a more precise test of the model by creating less steep concentration gradients, which, however, would require long incubation times to purge the dissolved N₂ from the soil by ebullition and to reach true steady state.     

Bioconversion of organic carbon to CH4 and CO2

The activities of populations in complex anaerobic microbial communities that perform complete bioconversion of organic matter to CH₄ and CO₂ are reviewed. Species of eubacteria produce acetate, H₂, and CO₂ from organic substrates, and methanogenic species of archaebacteria transform the acetate, H₂, and CO₂ to CH₄. The characteristics and activities of the methanogenic bacteria are described. The impact of the use of H₂ by methanogens on the fermentations that produce acetate, H₂, and CO₂ and the importance of syntrophy in complete bioconversion are discussed.     

The geochemistry of methane in Lake Fryxell,an amictic,permanently ice-covered,antarctic lake

The abundance and distribution of dissolved CH₄ were determined from 1987–1990 in Lake Fryxell, Antarctica, an amictic, permanently ice-covered lake in which solute movement is controlled by diffusion. CH₄ concentrations were < 1 υM in the upper oxic waters, but increased below the oxycline to 936 μM at 18 m. Sediment CH₄ was 1100 μmol (1 sed)⁻¹ in the 0–5 cm zone. Upward flux from the sediment was the source of the CH₄, NH₄ ⁺, and DOC in the water column; CH₄ was 27% of the DOC+CH₄ carbon at 18 m. Incubations with surficial sediments indicated that H¹⁴CO₃ ⁻ reduction was 0.4 μmol (1 sed)⁻¹ day⁻¹ or 4× the rate of acetate fermentation to CH₄. There was no measurable CH₄ production in the water column. However, depth profiles of CH₄, NH₄, and DIC normalized to bottom water concentrations demonstrated that a significant CH₄ sink was evident in the anoxic, sulfate-containing zone of the water column (10–18 m). The δ¹³CH₄ in this zone decreased from −72 % at 18 m to −76% at 12 m, indicating that the consumption mechanism did not result in an isotopic enrichment of ¹³CH₄. In contrast, δ¹³CH₄ increased to −55 % at 9 m due to aerobic oxidation, though this was a minor aspect of the CH₄ cycle. The water column CH₄ profile was modeled by coupling diffusive flux with a first order consumption term; the best-fit rate constant for anaerobic CH₄ consumption was 0.012 yr⁻¹. On a total carbon basis, CH₄ consumption in the anoxic water column exerted a major effect on the flux of carbonaceous material from the underlying sediments and serves to exemplify the importance of CH₄ to carbon cycling in Lake Fryxell.     

Response of tundra CH4 and CO2 flux tomanipulation of temperature and vegetation

We conducted plant species removals, air temperaturemanipulations, and vegetation and soil transplants inAlaskan wet-meadow and tussock tundra communities todetermine the relative importance of vegetation typeand environmental variables in controlling ecosystemmethane (CH₄) and carbon dioxide (CO₂) flux. Plastic greenhouses placed over wet-meadow tundraincreased air temperature, soil temperature, and soilmoisture, but did not affect CH₄ or CO₂ flux(measured in the dark). By contrast, removal ofsedges in the wet meadow significantly decreased fluxof CH₄, while moss removal tended to increaseCH₄ emissions. At 15 cm depth, pore-waterCH₄ concentrations were higher in sedge-removalthan in control plots, suggesting that sedgescontribute to CH₄ emissions by transportingCH₄ from anaerobic soil to the atmosphere, ratherthan by promoting methanogenesis. Inreciprocal-ecosystem transplants between thewet-meadow and tussock tundra communities, CH₄and CO₂ emissions were higher overall in thewet-meadow site, but were unrelated to transplantorigin. Methane flux was correlated with localvariation in soil temperature, thaw depth, andwater-table depth, but the relative importance ofthese factors varied through the season. Our resultssuggest that future changes in CH₄ and CO₂flux in response to climatic change will be morestrongly mediated by large-scale changes in vegetationand soil parameters than by direct temperature effects.     

Effects of Elevated Atmospheric CO2 Concentrations on CH4 and N2O Emission from Rice Soil: An Experiment in Controlled-environment Chambers

The effects of elevated concentrations of atmospheric CO₂ on CH₄ and N₂O emissions from rice soil were investigated in controlled-environment chambers using rice plants growing in pots. Elevated CO₂ significantly increased CH₄ emission by 58% compared with ambient CO₂. The CH₄ emitted by plant-mediated transport and ebullition–diffusion accounted for 86.7 and 13.3% of total emissions during the flooding period under ambient level, respectively; and for 88.1 and 11.9% of total emissions during the flooding period under elevated CO₂ level, respectively. No CH₄ was emitted from plant-free pots, suggesting that the main source of emitted CH₄ was root exudates or autolysis products. Most N₂O was emitted during the first 3 weeks after flooding and rice transplanting, probably through denitrification of NO₃⁻ contained in the experimental soil, and was not affected by the CO₂ concentration. Pre-harvest drainage suppressed CH₄ emission but did not cause much N₂O emission (< 10 μg N m⁻² h⁻¹) from the rice-plant pots at both CO₂ concentrations.     

Responses of nematode communities to different land uses in an aquic brown soil

An analysis of the seasonal and vertical distribution of soil nematode communities under three contrasting land uses, i.e., cropland, abandoned cropland and woodland was conducted in an aquic brown soil. The results showed that different land-use types affected the spatiotemporal distribution of soil nematodes and their dominant genera, and different dominant genera showed different responses to land use. In the abandoned cropland and woodland, most dominant genera were present in the 0–20 cm layers and Chiloplacus was mainly distributed in the 5–30 cm layers, while in the cropland, Pratylenchus exhibited an even distribution from the 0–5 cm to the 40–50 cm depth. Soil environmental parameters under different land use could influence soil nematodes; soil porosity, total organic C, total N and the C/N ratio could positively influence the abundance of some dominant genera. Faunal profiles revealed that environmental stability and the homeostasis in the abandoned cropland and woodland lead to higher levels of community structure, and the soil food web tends to succeed to maturity. Nematode faunal analyses are a useful indicator for interpreting the stress and/or nutrient conditions under different land uses. __________ Translated from Biodiversity Science, 2007, 15(2): 172–179 [译自:生物多样性]     

Effect of nitrogen fertilizers and moisture content on CH4 and N2O fluxes in a humisol: Measurements in the field and intact soil cores

Field and laboratory studies were conducted to determine effects of nitrogen fertilizers and soil water content on N₂O and CH₄ fluxes in a humisol located on the Central Experimental Farm of Agriculture Canada, Ottawa. Addition of 100 kg N ha^–1 as either urea or NaNO₃ had no significant effect on soil CH₄ flux measured using chambers. Fertilization with NaNO₃ resulted in a significant but transitory stimulation of N₂O production. Inorganic soil N profiles and the potential nitrification rate suggested that much of the NH ₄ ⁺ from urea hydrolysis was rapidly nitrified. CH₄ fluxes measured using capped soil cores agreed well with fluxes measured using field chambers, and with fluxes calculated from soil gas concentration gradients using Fick's diffusion law. This humisol presents an ideal, unstructured, vertically homogeneous system in which to study gas diffusion, and the influence of gas-filled porosity on CH₄ uptake. In soil cores gradually saturated with H₂O, the relationship of CH₄ flux to gas-filled porosity was an exponential rise to a maximum. Steepening CH₄ concentration gradients partially compensated for the decreasing diffusion coefficient of CH₄ in soil matrix air as water content increased, and diffusion limitation of CH₄ oxidation occurred only at water contents > 130% (dry weight), or gas-filled porosities < 0.2.Corresponding author     

Simulated Nitrogen Deposition Reduces CH4 Uptake and Increases N2O Emission from a Subtropical Plantation Forest Soil in Southern China

To date, few studies are conducted to quantify the effects of reduced ammonium (NH₄ ⁺) and oxidized nitrate (NO₃ ⁻) on soil CH₄ uptake and N₂O emission in the subtropical forests. In this study, NH₄Cl and NaNO₃ fertilizers were applied at three rates: 0, 40 and 120 kg N ha⁻¹ yr⁻¹. Soil CH₄ and N₂O fluxes were determined twice a week using the static chamber technique and gas chromatography. Soil temperature and moisture were simultaneously measured. Soil dissolved N concentration in 0–20 cm depth was measured weekly to examine the regulation to soil CH₄ and N₂O fluxes. Our results showed that one year of N addition did not affect soil temperature, soil moisture, soil total dissolved N (TDN) and NH₄ ⁺-N concentrations, but high levels of applied NH₄Cl and NaNO₃ fertilizers significantly increased soil NO₃ ⁻-N concentration by 124% and 157%, respectively. Nitrogen addition tended to inhibit soil CH₄ uptake, but significantly promoted soil N₂O emission by 403% to 762%. Furthermore, NH₄ ⁺-N fertilizer application had a stronger inhibition to soil CH₄ uptake and a stronger promotion to soil N₂O emission than NO₃ ⁻-N application. Also, both soil CH₄ and N₂O fluxes were driven by soil temperature and moisture, but soil inorganic N availability was a key integrator of soil CH₄ uptake and N₂O emission. These results suggest that the subtropical plantation soil sensitively responses to atmospheric N deposition, and inorganic N rather than organic N is the regulator to soil CH₄ uptake and N₂O emission.     

Methane Metabolism in a Temperate Swamp

Comparisons between in situ CH₄ concentration and potential factors controlling its net production were made in a temperate swamp. Seasonal measurements of water table level and depth profiles of pH, dissolved CH₄, CO₂, O₂, SO₄^2-, NO₃^-, formate, acetate, propionate, and butyrate were made at two adjacent sites 1.5 to 2 m apart. Dissolved CH₄ was inversely correlated to O₂ and, in general, to NO₃^- and SO₄^2-, potential inhibitors of methanogenesis. At low water table levels (August 1992), maximal CH₄ (2 to 4 μM) occurred below 30 cm, whereas at high water table levels (October 1992) or under flooded conditions (May 1993), CH₄ maxima (4 to 55 μM) occurred in the top 10 to 20 cm. Higher CH₄ concentrations were likely supported by inputs of fresh organic matter from decaying leaf litter, as suggested by high acetate and propionate concentrations (25 to 100 μM) in one of the sites in fall and spring. Measurements of potential CH₄ production (and consumption) showed that the highest rates generally occurred in the top 10 cm of soil. Soil slurry incubations confirmed the importance of organic matter to CH₄ production but also showed that competition for substrates by nonmethanogenic microorganisms could greatly attenuate its effect.     

Hydrogen Concentration and Stable Isotopic Composition of Methane in Bubble Gas Observed in a Natural Wetland

Bubble gas samples were collected at three different vegetation sites and two different depths (surface and 40 cm) in a natural wetland, Mizorogaike in Kyoto city, to investigate hydrogen concentration and δD and δ¹³C values of CH₄. Hydrogen concentration in bubble gas varied from 1 to 205 ppm, and that collected during summer was higher than that during winter. Bubble samples collected at 40 cm at sphagnum site usually showed the lowest H₂ concentration among the samples collected at the three sites and two depths on the same day. The lowest H₂ concentration observed at 40 cm at sphagnum site was similar to that expected for environmental water in which H₂ producer and consumer need to assemble for free energy requirement. Low δ¹³C and high δD (relatively small hydrogen fractionation; ‰) were observed in CH₄ collected at a deeper (40 cm) layer of sphagnum site during winter, when H₂ concentration was low (typically 2–4 ppm). On the other hand, CH₄ in the bubble samples collected during summer showed high δ¹³C and low δD (relatively large hydrogen fractionation; ‰), when H₂ concentration was high. Carbon and hydrogen isotope fractionation during CH₄ production were variable, possibly depending on the H₂ concentration and the production rate. Difference in enzymatic reaction and magnitude of hydrogen isotope exchange among water, CH₄, and H₂ may cause the variation in isotope fractionation during CH₄ production.     

137Cs and 40K isotopes in forest and wasteland soils in a selected region of eastern Poland 20 years after the Chernobyl accident

The vertical ¹³⁷Cs profile of forest and wasteland soils was analyzed in the south of the Podlasie Lowland area (Eastern Poland) about 20 years after the Chernobyl accident. In addition, the concentration of ⁴⁰K in soils of the investigated area was measured. Below the litter layer (mean thickness 3 cm), the soil samples were collected up to a depth of 12 cm and then divided into three layers: 0–3, 3–7, 7–12 cm. The behavior of ¹³⁷Cs and ⁴⁰K isotopes in soils was analyzed depending on the depth from which the soil samples were collected, as well as on the content of organic carbon, pH of soil and its granulometric composition. It was established that the density of ¹³⁷Cs in the litter layer equals 2.17 kBq m⁻²; it is the highest in layer 0–3 cm where it equals 3.44 kBq m⁻², and it decreases with the depth to the value of 0.76 kBq m⁻² in layer 7–12 cm. No similar pattern was observed in wasteland soils. The concentrations of ⁴⁰K in forest and wasteland soils did not change significantly with depth.     

Moisture adsorption capacity and surface area as deduced from vapour pressure isotherms in relation to hygroscopic water of soils

Six calcareous and alluvial soil profiles differing in their texture, CaCO₃ and salinity were chosen from west and middle Nile Delta for the present study. The 1^st and 2^nd profiles from Borg El-Arab area were sandy loam in texture and > 30% CaCO₃, while the 3^rd and 4^th profiles (from Nubaria area) were sandy clay loam and < 30% CaCO₃. The 2^nd and 4^th profiles were taken from cultivated area with maize. The 5^th profile from Epshan area was non-saline clay alluvial soil and the 6^th from El-Khamsen was saline clay alluvial soil. The relation between soil moisture content (W%) and water vapour pressure (P/P _o) was established for the mentioned soils. Data showed that the specific surface area (S) values were 34–53 and 44–60 m²/g for calcareous soils of Borg El-Arab and Nubaria areas, 206–219 and 206–249 m²/g for non-saline and saline clay alluvial soils of Epshan and El-Khamsen areas, respectively. The corresponding values of the external specific surface area (S _e) were 16–21, 14–22, 72–86 and 92–112 m²/g. Submitting W _m+W _me as an adsorption boundary of moisture films (W _c) (where W _m is mono-adsorbed layer of water vapour on soil particles and W _me is the external mono-adsorbed layer), the maximum water adsorption capacity (W _a) was found to be W _c + W _me or W _m + 2W _me. It was ranged from 1.88 to 2.70%, 1.97 to 2.95%, 9.70–10.70% and 10.80 to 13.12% while the maximum hygroscopic water (M _H) values were 2.43–3.78%, 2.91–4.65%, 16–17% and 18.30–21.9% for the studied soil profiles respectively. The residual moisture content (θ _r) at pF 7 and P/P _o = 0 was ranged from 0.0005–0.0010%, 0.0007–0.0019% and 0.0043–0.0048% in Borg El-Arab, Nubaria and Epshan soil profiles, respectively. The inter-relations between the surface area and the hygroscopic moisture parameters of the soils under investigation were as follows Calcareous soils; W _m = 0.40 M _H, W _c = 0.55 M _H, W _a = 0.70 M _H, S = 14 M _H Non-saline soil; W _m = 0.35 M _H, W _c = 0.49 M _H, W _a = 0.63 M _H, S = 13 M _H Saline soil; W _m = 031 M _H, W _c = 0.45 M _H, W _a = 0.59 M _H, S = 12 M _H These relations give possibility to deduce the soil moisture adsorption capacities and specific surface area via maximum hygroscopic water, which can be obtained through the experimental determination of water vapor adsorption isotherms.     

Response of CH4 and N2O Emissions and Wheat Yields to Tillage Method Changes in the North China Plain

The objective of this study was to quantify soil methane (CH₄) and nitrous oxide (N₂O) emissions when converting from minimum and no-tillage systems to subsoiling (tilled soil to a depth of 40 cm to 45 cm) in the North China Plain. The relationships between CH₄ and N₂O flux and soil temperature, moisture, NH₄ ⁺-N, organic carbon (SOC) and pH were investigated over 18 months using a split-plot design. The soil absorption of CH₄ appeared to increase after conversion from no-tillage (NT) to subsoiling (NTS), from harrow tillage (HT) to subsoiling (HTS) and from rotary tillage (RT) to subsoiling (RTS). N₂O emissions also increased after conversion. Furthermore, after conversion to subsoiling, the combined global warming potential (GWP) of CH₄ and N₂O increased by approximately 0.05 kg CO₂ ha⁻¹ for HTS, 0.02 kg CO₂ ha⁻¹ for RTS and 0.23 kg CO₂ ha⁻¹ for NTS. Soil temperature, moisture, SOC, NH₄ ⁺-N and pH also changed after conversion to subsoiling. These changes were correlated with CH₄ uptake and N₂O emissions. However, there was no significant correlation between N₂O emissions and soil temperature in this study. The grain yields of wheat improved after conversion to subsoiling. Under HTS, RTS and NTS, the average grain yield was elevated by approximately 42.5%, 27.8% and 60.3% respectively. Our findings indicate that RTS and HTS would be ideal rotation tillage systems to balance GWP decreases and grain yield improvements in the North China Plain region.     

Molecular Analyses of Novel Methanotrophic Communities in Forest Soil That Oxidize Atmospheric Methane

Forest and other upland soils are important sinks for atmospheric CH₄, consuming 20 to 60 Tg of CH₄ per year. Consumption of atmospheric CH₄ by soil is a microbiological process. However, little is known about the methanotrophic bacterial community in forest soils. We measured vertical profiles of atmospheric CH₄ oxidation rates in a German forest soil and characterized the methanotrophic populations by PCR and denaturing gradient gel electrophoresis (DGGE) with primer sets targeting the pmoA gene, coding for the α subunit of the particulate methane monooxygenase, and the small-subunit rRNA gene (SSU rDNA) of all life. The forest soil was a sink for atmospheric CH₄ in situ and in vitro at all times. In winter, atmospheric CH₄ was oxidized in a well-defined subsurface soil layer (6 to 14 cm deep), whereas in summer, the complete soil core was active (0 cm to 26 cm deep). The content of total extractable DNA was about 10-fold higher in summer than in winter. It decreased with soil depth (0 to 28 cm deep) from about 40 to 1 μg DNA per g (dry weight) of soil. The PCR product concentration of SSU rDNA of all life was constant both in winter and in summer. However, the PCR product concentration of pmoA changed with depth and season. pmoA was detected only in soil layers with active CH₄ oxidation, i.e., 6 to 16 cm deep in winter and throughout the soil core in summer. The same methanotrophic populations were present in winter and summer. Layers with high CH₄ consumption rates also exhibited more bands of pmoA in DGGE, indicating that high CH₄ oxidation activity was positively correlated with the number of methanotrophic populations present. The pmoA sequences derived from excised DGGE bands were only distantly related to those of known methanotrophs, indicating the existence of unknown methanotrophs involved in atmospheric CH₄ consumption.     

Pathways of methanol conversion in a thermophilic anaerobic (55 °C) sludge consortium

The pathway of methanol conversion by a thermophilic anaerobic consortium was elucidated by recording the fate of carbon in the presence and absence of bicarbonate and specific inhibitors. Results indicated that about 50% of methanol was directly converted to methane by the methylotrophic methanogens and 50% via the intermediates H₂/CO₂ and acetate. The deprivation of inorganic carbon species [(HCO₃^–+CO₂)] in a phosphate-buffered system reduced the rate of methanol conversion. This suggests that bicarbonate is required as an electron (H₂) sink and as a co-substrate for the efficient and complete removal of the chemical oxygen demand. Nuclear magnetic resonance spectroscopy was used to investigate the route of methanol conversion to acetate in bicarbonate-sufficient and bicarbonate-depleted environments. The proportions of [1,2-¹³C]acetate, [1-¹³C]acetate and [2-¹³C]acetate were determined. Methanol was preferentially incorporated into the methyl group of acetate, whereas HCO₃^– was the preferred source of the carboxyl group. A small amount of the added H¹³CO₃^– was reduced to form the methyl group of acetate and a small amount of the added ¹³CH₃OH was oxidised and found in the carboxyl group of acetate when ¹³CH₃OH was converted. The recovery of [¹³C]carboxyl groups in acetate from ¹³CH₃OH was enhanced in bicarbonate-deprived medium. The small amount of label incorporated in the carboxyl group of acetate when ¹³CH₃OH was converted in the presence of bromoethanesulfonic acid indicates that methanol can be oxidised to CO₂ prior to acetate formation. These results indicate that methanol is converted through a common pathway (acetyl-CoA), being on the one hand reduced to the methyl group of acetate and on the other hand oxidised to CO₂, with CO₂ being incorporated into the carboxyl group of acetate.     

Effects of short-term drying and irrigation on CO2 and CH4 production and emission from mesocosms of a northern bog and an alpine fen

Atmospheric CO₂ and CH₄ exchange in peatlands is controlled by water table levels and soil moisture, but impacts of short periods of dryness and rainfall are poorly known. We conducted drying-rewetting experiments with mesocosms from an ombrotrophic northern bog and an alpine, minerotrophic fen. Efflux of CO₂ and CH₄ was measured using static chambers and turnover and diffusion rates were calculated from depth profiles of gas concentrations. Due to a much lower macroporosity in the fen compared to the bog peat, water table fluctuated more strongly when irrigation was stopped and resumed, about 11 cm in the fen and 5 cm in the bog peat. Small changes in air filled porosity caused CO₂ and CH₄ concentrations in the fen peat to be insensitive to changes in water table position. CO₂ emission was by a factor of 5 higher in the fen than in the bog mesocosms and changed little with water table position in both peats. This was probably caused by the importance of the uppermost, permanently unsaturated zone for auto- and heterotrophic CO₂ production, and a decoupling of air filled porosity from water table position. CH₄ emission was <0.4 mmol m^?2 day^?1 in the bog peat, and up to >12.6 mmol m^?2 day^?1 in the fen peat, where it was lowered by water table fluctuations. CH₄ production was limited to the saturated zone in the bog peat but proceeded in the capillary fringe of the fen peat. Water table drawdown partly led to inhibition of methanogenesis in the newly unsaturated zone, but CH₄ production appeared to continue after irrigation without time-lag. The identified effects of irrigation on soil moisture and respiration highlight the importance of peat physical properties for respiratory dynamics; but the atmospheric carbon exchange was fairly insensitive to the small-scale fluctuations induced.