不同水位管理对恢复泥炭地土壤CO2、CH4排放的影响

泥炭地水文条件影响泥炭地生物地球化学循环,控制和维持着泥炭地生态系统的结构和功能,是泥炭地生态恢复的重要前提。然而,目前关于恢复泥炭地土壤碳排放对不同水位的响应尚不明确。以长白山区天然（NP）、退耕（DP）及实施不同水文管理的恢复泥炭地（低水位（LR）、高水位（HR）与高低交替水位（H-LR））为研究对象,采用静态箱-气相色谱法对研究区泥炭地进行生长季（6-10月）土壤CO₂、CH₄排放监测。结果表明：温度和水位变化是研究区泥炭地土壤CO₂、CH₄排放季节变化的主控因子。H-LR受水位控制的影响,生长季土壤CO₂排放速率波动剧烈,其它水位管理恢复区土壤CO₂排放速率呈单峰型排放模式,且均与近地表温度呈指数相关（P<0.05）。除HR外,土壤CO₂排放速率与水位呈显著负相关（P<0.05）。生长季,研究区HR土壤CH₄排放速率呈双峰型,H-LR与NP的土壤CH₄排放呈单峰型,与近地表温度呈指数相关（P<0.05）,LR水位与CH₄排放速率显著正相关（P<0.05）。研究区不同水位管理恢复泥炭地土壤碳排放差异显著,虽然HR的土壤CO₂-C累积碳排放量显著低于其它水位恢复区,但其土壤CH₄-C累积碳排放量和综合增温潜势显著高于其它水位恢复区（P<0.05）。LR的累积碳排放量显著低于退化泥炭地,且其综合增温潜势最低。因此,建议在泥炭地恢复初期将低水位管理作为短期策略,以更好地恢复泥炭地碳汇功能,减弱其增温潜势。     

泥炭沼泽湿地关键元素地球化学特征及其对碳排放的影响机制

硫、铁是泥炭沼泽湿地（泥炭地）中重要的生源要素,其参与下的生物地球化学过程对泥炭地碳循环意义重大。选取德国中部两处典型的雨养型泥炭地高海拔样点（TBP）和低海拔样点（TSP）,通过原位采集泥炭剖面孔隙水和可溶性气体等,研究了硫、铁元素等地球化学变化规律,结合DOC、甲烷（CH₄）和二氧化碳（CO₂）浓度分布,探讨其对泥炭地碳排放的影响。研究结果表明：（1） TBP中总还原无机硫（TRIS）浓度随深度先增后减,且上部0-87 cm平均浓度远高于87 cm深度以下,上部硫酸盐还原作用强烈。结合上部亚铁、硫化氢（H₂S）浓度分布,得知该范围内H₂S主要是通过微生物硫酸盐还原作用（BSR）生成,同时H₂S在孔隙水扩散过程中易与亚铁结合为硫化亚铁,进而生成稳定的黄铁矿,这一反应过程在约60 cm处减缓。（2） TBP、TSP两处采样点中DOC与亚铁、硫酸盐均有较强相关性,是由于地下水位的波动影响氧化还原程度以及微生物活性。两处采样点DOC均与亚铁呈显著正相关关系,表明铁氧化物在厌氧环境中被还原溶解产生亚铁,与其结合的有机碳被释放到溶液中从而导致DOC浓度的升高。TBP中DOC与硫酸盐呈显著负相关关系,表明硫酸盐作为电子受体被还原的过程中消耗酸度使pH值升高,增强了其中微生物的活性,DOC浓度由此增加。（3） CH₄与硫酸盐、TRIS浓度在剖面上均呈现相反变化趋势,表明硫酸盐输入的增加以及硫酸盐还原活动均会抑制CH₄生成。CO₂/CH₄均大于4,表明硫酸盐作为替代电子受体会使厌氧条件下碳矿化转向多CO₂和少CH₄生成。此外,亚铁对于CH₄生成一定程度上会起到低促高抑的效果,而对于CO₂的生成的影响较弱。表明硫酸盐对于CH₄和CO₂生成的影响高于亚铁。研究着重探究硫、铁等关键元素地下部生物地球化学过程对碳排放的影响机制,研究结果可为泥炭地碳排放核算提供理论支撑。     

典型温带雨养泥炭沼泽湿地地下部二氧化碳和甲烷浓度变化规律及其影响因素

为研究北方泥炭沼泽湿地二氧化碳（CO₂）和甲烷（CH₄）浓度随深度的变化规律及其影响因素,选取欧洲北部典型雨养泥炭地贝尔山湿地（BBM）和舒特兹山湿地（SBM）两个采样点,通过原位采集泥炭剖面温室气体、孔隙水以及土壤样品,结合傅里叶变换红外光谱（FTIR）技术、碳氮同位素技术,探讨泥炭土壤的分解程度及温室气体浓度变化的关系。研究结果表明：（1）BBM采样点地下部的CO₂浓度变化规律总体呈现随深度波动减少趋势,值多在3000 μmol/L附近波动,最大值为4210.74 μmol/L（120 cm）,SBM采样点的CO₂浓度随深度先增后减,60 cm以上在1800 μmol/L附近波动,60 cm以下在3000 μmol/L附近波动,最大值为4191.94 μmol/L（90 cm）;BBM和SBM地下部CH₄浓度都随深度增大,并且在60cm以下浓度增加较快,BBM最大值为735.90 μmol/L（260 cm）,SBM最大值为543.51 μmol/L（170 cm）。（2）BBM和SBM的δ¹³C_CH4的值均较小,表明大部分的¹²CH₄仍被储存在泥炭土壤中,而两个采样点的δ¹³C_CO2和分馏系数α_c均随深度增加,表明泥炭土中产甲烷方式为浅层以乙酸产甲烷为主,深层以H₂还原CO₂为主。（3）C/N、碳氮同位素比值、FTIR均显示SBM和BBM的有机质分解程度较低,因为两个采样点的低可溶性有机碳浓度和低pH值不利于分解,表明该地储存着大量有机碳。通过探讨北温带典型泥炭地温室气体的浓度变化规律及其影响因素,结果可为全球泥炭湿地碳排放提供理论支撑。     

林下植被和凋落物对寒温带森林生长季土壤CH4通量的影响

为进一步探究林下植被和凋落物管理对我国寒温带森林生长季土壤CH₄通量的影响,采用静态箱-气相色谱法对大兴安岭北部4种林型（白桦林、山杨林、樟子松林和兴安落叶松林）4种处理（自然状态、去除凋落物、去除林下植被以及去除林下植被和凋落物）的土壤CH₄通量排放特征进行观测研究。结果表明：该地区森林生长季土壤均表现为CH₄的汇,4种林型不同处理后土壤CH₄通量表现为单峰变化趋势,吸收峰值出现在7月或8月。自然状态4种林型土壤CH₄平均吸收通量表现为白桦林（-79.23±14.92）μg m^-2 h^-1>山杨林（-64.27±9.60）μg m^-2 h^-1>樟子松林（-62.54±15.48）μg m^-2 h^-1>兴安落叶松林（-48.73±12.26）μg m^-2 h^-1,兴安落叶松土壤CH₄平均吸收通量显著小于其他三种林型（P<0.05）。相比于自然状态,4种林型在去除凋落物后土壤CH₄吸收通量提高了2.12%-12.15%,但变化幅度均没有达到显著水平（P>0.05）。去除林下植被后4种林型CH₄吸收通量提高了0.84%-20.55%,且只有山杨林吸收增加达到显著水平（P<0.05）。同时去除林下植被和凋落物后,对白桦林和樟子松土壤CH₄通量影响不显著（P>0.05）,但对山杨林和兴安落叶松林影响显著（P<0.05）。总之,去除凋落物或林下植被均会提高土壤对CH₄吸收,去除林下植被对土壤CH₄通量的影响要大于去除凋落物的影响,但不同林型不同处理之间还存在差异。     

云贵高原典型湖滨湿地好氧甲烷氧化细菌群落结构和数量的时空动态

湖泊生态系统排放的甲烷（CH₄）大部分来自湖滨湿地，好氧甲烷氧化细菌（methane-oxidizing bacteria，MOB）在减轻CH₄从湖泊系统向大气的排放中起着至关重要的作用。湖滨湿地好氧MOB群落分布及其影响因素尚不清楚。采用qPCR、末端限制性片段长度多态性（T-RFLP）等方法，分四季对贵州草海湖滨湿地宽敞水域至落干区沉积物中好氧MOB群落组成和数量进行了研究。草海湖滨湿地沉积中甲烷氧化单加氧酶功能基因（pomA）丰度较高，在1.78×10⁷-2.73×10⁸拷贝数/g干沉积物之间，好氧MOB由I型（Methylococcus and Methylobacter）和II型（Methylosinus）组成，I型主要分布在宽敞水域（长期淹水区），而干湿过渡区和偶尔积水区主要为II型，呈现出明显的空间变化，推测湖滨湿地长期淹水区甲烷的氧化由I型主导，而相对干旱的区域II型主导，而这种差异可能是导致湖滨湿地甲烷排放高度异质性的一个重要因素。研究结果对揭示湖滨湿地甲烷排放时空异质性的微生物生态机制奠定了基础。     

闽江河口芦苇沼泽和短叶茳芏沼泽生态系统含碳温室气体的年收支

河口感潮沼泽是全球重要的蓝碳生态系统,具有很强的固碳能力。碳收支研究是量化生态系统碳源/汇过程及固碳规模的基础。本研究运用透明箱和不同遮光率布遮盖+红外气体分析仪/气相色谱相结合的方法,模拟不同光照条件,测定闽江河口鳝鱼滩半咸水芦苇沼泽和短叶茳芏沼泽的瞬时净生态系统二氧化碳（CO₂）交换量（net ecosystem exchange,NEE）、生态系统呼吸（ecosystem respiration,ER）以及甲烷（CH₄）排放通量,并通过对总光合吸收量（gross ecosystem exchange,GEE）与光合有效辐射的拟合以及ER与气温的拟合,外推2个沼泽生态系统CO₂气体在月、年尺度上的NEE和ER,评估其年固碳量。2个沼泽生态系统的NEE和ER均具有明显的季节变化,春夏秋季为大气中CO₂的汇,而冬季则转化为大气中CO₂的源,芦苇沼泽年尺度固碳能力显著高于短叶茳芏沼泽。芦苇沼泽与短叶茳芏沼泽CH₄排放通量差异不显著。综合考虑CH₄排放,闽江河口鳝鱼滩半咸水芦苇沼泽、短叶茳芏沼泽生态系统年固碳量分别为（5371.52±336.97） g CO₂-eq/m²和（2730.32±503.67） g CO₂-eq/m²。研究表明：闽江河口半咸水沼泽湿地在年尺度上是一个较强的碳汇,在缓解全球变暖方面发挥着重要的角色。     

鄱阳湖沉水植物区不同深度土壤甲烷排放对温度水分变化的响应

采集鄱阳湖沉水植物区0-10 cm和10-30 cm土壤样品,通过设置2个温度（18℃和28℃）和2个水分（淹水2 cm和土柱取出水面后的实际土壤水分含量）处理组合,进行持续2年的甲烷（CH₄）排放室内培养实验,以探讨不同深度土壤CH₄排放对温度、水分变化的响应差异,以及温度、水分和土层对湿地土壤CH₄排放的交互影响。结果表明：0-10 cm和10-30 cm土壤CH₄排放速率变化范围分别为0.01-3.63 μgCH₄-C kg^-1d^-1、0.02-1.99 μgCH₄-C kg^-1d^-1;均值分别为0.72和0.15 μgCH₄-C kg^-1d^-1。温度、水分和土层3因素及其交互作用均对土壤CH₄排放有显著影响（P<0.01）,且土层的影响最大。两水分处理下的CH₄排放对温度变化的敏感性均表现为0-10 cm（Q₁₀为1.78、3.26）高于10-30 cm土层（Q₁₀为1.04、1.08）。CH₄平均排放速率及累计排放量均表现为0-10 cm显著高于10-30 cm土层,且培养前期高于培养后期,显示基质有效性对土壤CH₄排放的重要影响。     

青藏高原泥炭地水位下降促进土壤碳积累的影响机制

酚类物质作为泥炭地重要的碳分解抑制剂,植被作为泥炭地关键的碳输入来源,它们在土壤碳(可溶性有机碳(DOC)等)周转过程中都发挥着重要作用。然而,目前关于植被群落结构、酚类物质以及DOC含量对水位波动的响应存在较大争议。因此,为明确泥炭地水位下降对植被群落结构、酚类物质以及DOC含量的影响并探明三者间的潜在联系,以若尔盖高原泥炭地作为研究对象,选取红原县日干乔地区3处不同地下水位泥炭地(水位由高到低依次为S1(-1.9 cm)、S2(-10 cm)、S3(-19 cm)样地),调查不同水位条件下植被群落结构特征,并探究酚类物质及土壤碳含量对水位波动的响应。结果表明:(1)从S1到S3样地水位下降促进土壤DOC显著增加(P<0.05),土壤总碳从S1到S2显著增加(P<0.05),而从S2到S3无显著差异;(2)泥炭地水位下降促使禾本科(发草Deschampsia cespitosa)、莎草科(木里薹草Carex muliensis、乌拉草Carex meyeriana)植物大量出现,植被群落高度显著增加(P<0.05)。植被群落地上生物量由153.67 g/m~2增加至...     

不同恢复方式下大兴安岭重度火烧迹地林地土壤温室气体通量

为研究大兴安岭重度火烧迹地在不同恢复方式下林地土壤CO₂、CH₄和N₂O排放特征及其影响因素,采用静态箱/气相色谱法,在2017年生长季（6月-9月）对3种恢复方式（人工更新、天然更新和人工促进天然更新）林地土壤温室气体CO₂、CH₄、N₂O通量进行了原位观测。研究结果表明：（1）3种恢复方式林地土壤在生长季均为大气CO₂、N₂O的源,CH₄的汇;生长季林地土壤CO₂排放通量大小关系为人工促进天然更新（（634.40±246.52）mg m^-2 h^-1） > 人工更新（（603.63±213.22）mg m^-2 h^-1） > 天然更新（（575.81±244.12）mg m^-2 h^-1）,3种恢复方式间无显著差异;人工更新林地土壤CH₄吸收通量显著高于人工促进天然更新;天然更新林地土壤N₂O排放通量显著高于其他两种恢复方式。（2）土壤温度是影响3种恢复方式林地土壤温室气体通量的关键因素;土壤水分仅对人工更新林地土壤N₂O通量有极显著影响（P < 0.01）;3种恢复方式林地土壤CO₂通量与大气湿度具有极显著的响应（P < 0.01）;土壤pH仅与天然更新林地土壤CO₂通量显著相关（P < 0.05）;土壤全氮含量仅与人工促进天然更新林地土壤CH₄通量显著相关（P < 0.05）。（3）基于100年尺度,由3种温室气体计算全球增温潜势得出,人工促进天然更新（1.83×10⁴ kg CO₂/hm²） > 人工更新（1.74×10⁴ kg CO₂/hm²） > 天然更新（1.67×10⁴ kg CO₂/hm²）。（4）阿木尔地区林地土壤年生长季CO₂和N₂O排放量为8.85×10⁶ t和1.88×10² t,CH₄吸收量为1.05×10³ t。     

川西平原小流域不同水体N2O排放特征及驱动因素

氧化亚氮（N₂O）是一种潜在的、强大的温室气体,应该根据京都议定书规定开展监测和削减。河流、水库、鱼塘和沟渠等受人类影响的小流域水生生态系统是氮素生物地球化学循环的活跃区域,更是N₂O重要的源和汇。然而,同一流域不同水体N₂O的排放特征差异及其驱动因素尚不清楚。因此,选择川西平原西河流域作为研究区,于2016年6月到2017年5月连续监测不同水体水气界面的N₂O排放强度,并结合聚类分析解析N₂O排放特征的驱动因素。结果显示,不同水体的N₂O年排放通量差异显著,沟渠的N₂O年排放通量最高（（52.68±36.09）μg m^-2 h^-1）,城市段河流和鱼塘次之（（34.16±23.97）μg m^-2 h^-1和（29.03±31.41）μg m^-2 h^-1）,乡镇段和农区段河流再次（（8.32±28.60）μg m^-2 h^-1和（8.52±9.43）μg m^-2 h^-1）,水库最低（（-16.45±29.76）μg m^-2 h^-1）。除水库表现为N₂O的汇,其他水体均表现为N₂O的排放源。另外,不同水体N₂O排放的季节特征差异显著,农区段河流和农业沟渠表现为夏天最高,冬春最低（P<0.05）,而其他水体均表现为冬春显著高于夏秋（P<0.05）。根据N₂O排放季节特征及其驱动因素可将西河流域水体分为四类：第一类农业类水体的N₂O排放季节特征受气象因素和农业活动的联合驱动;第二类城乡类河流和第三类鱼塘分别受控于人类活动和养殖活动,与降雨温度等气象指标关系较弱;第四类水库主要受控于气象因素。并且,第一类农业类水体已成为大气N₂O排放的重要源,农业氮素管控是区域控制N₂O排放的重点。     

Processes involved in formation and emission of methane in rice paddies

The seasonal change of the rates of production and emission of methane were determined under in-situ conditions in an Italian rice paddy in 1985 and 1986. The contribution to total emission of CH₄ of plant-mediated transport, ebullition, and diffusion through the flooding water was quantified by cutting the plants and by trapping emerging gas bubbles with funnels. Both production and emission of CH₄ increased during the season and reached a maximum in August. However, the numbers of methanogenic bacteria did not change. As the rice plants grew and the contribution of plant-mediated CH₄ emission increased, the percentage of the produced CH₄ which was reoxidized and thus, was not emitted, also increased. At its maximum, about 300 ml CH₄ were produced per m² per hour. However, only about 6% were emitted and this was by about 96% via plant-mediated transport. Radiotracer experiments showed that CH, was produced from H₂/CO₂. (30–50%) and from acetate. The pool concentration of acetate was in the range of 6–10 mM. The turnover time of acetate was 12–16 h. Part of the acetate pool appeared to be not available for production of CH₄ or CO₂     

Methane emissions from rice microcosms: The balance of production, accumulation and oxidation

In rice microcosms (Oryza sativa, var. Roma, type japonica),CH₄ emission, CH₄ production, CH₄oxidation and CH₄ accumulation were measured over an entirevegetation period. Diffusive CH₄ emission was measured inclosed chambers, CH₄ production was measured in soil samples,CH₄ oxidation was determined from the difference between oxicand anoxic emissions, and CH₄ accumulation was measured byanalysis of porewater and gas bubbles. The sum of diffusiveCH₄ emission, CH₄ oxidation, andCH₄ accumulation was only 60% of the cumulativeCH₄ production. The two values diverged during the first 50days (vegetative phase) and then again during the last 50 days (latereproductive phase and senescence) of the 150 day vegetation period. Duringthe period of day 50–100 (early reproductive phase/flowering), theprocesses were balanced. Most likely, gas bubbles and diffusion limitationare responsible for the divergence in the early and late phases. The effectof rice on CH₄ production rates and CH₄concentrations was studied by measuring these processes also in unplantedmicrocosms. Presence of rice plants lowered the CH₄concentrations, but had no net effect on the CH₄ productionrates.     

Bacterial Processes of the Methane Cycle in Bottom Sediments of Lake Baikal

The activity of methanogenic and methanotrophic bacteria was evaluated in bottom sediments of Lake Baikal. Methane concentration in Baikal bottom sediments varied from 0.0053 to 81.7 ml/dm³. Bacterial methane was produced at rates of 0.0004–534.7 l CH₄/(dm³ day) and oxidized at rates of 0.005–1180 l CH₄/(dm³ day). Peak methane production and oxidation were observed in Frolikha Bay near a methane vent. Methane was emitted into water at rates of 49.2–4340 l CH₄/(m² day). Rates of bacterial methane oxidation in near-bottom water layers ranged from 0.002 to 1.78 l/(l day). Methanogens and methanotrophs were found to play an important role in the carbon cycle through all layers of sediments, particularly in the areas of methane vent and gas-hydrate occurrence.     

盐分对湿地甲烷排放影响的研究进展

当前在全球气候变化和人类活动双重作用下,湿地正在或者将要面临着显著的盐分变化形势,尤其是内陆和滨海咸化湿地。湿地是大气甲烷的重要排放源。甲烷排放是甲烷产生、氧化和传输过程综合作用的结果。盐分变化将影响湿地水-土环境,降低植物群落初级生产力和有机物积累速率,改变微生物主导的有机物矿化速率和途径等,进而改变湿地生态系统的结构和功能,影响湿地甲烷产生、氧化、传输和排放系列过程。本文综述了盐分(浓度与组成)对湿地甲烷产生与排放的影响结果,从底物供给、微生物(产甲烷菌和甲烷氧化菌等)数量、活性与群落组成、酶活性、植物、电子受体、p H和氧化还原电位等几个关键方面分析了盐分影响湿地甲烷排放过程的内在机制。在此基础上提出了今后需重点关注的5个方面:1)加强盐分浓度与组成对湿地甲烷产生、氧化、传输与排放影响的系统性、框架性研究;2)深入探讨盐分背景、变化幅度与速率的耦合如何影响湿地甲烷系列过程;3)不同离子组成及其交互效应如何影响湿地甲烷动态过程;4)结合生物学、基因组学及同位素技术等,加强湿地产甲烷菌与甲烷氧化菌与盐分的关系及其响应研究;5)湿地甲烷对盐分变化响应的时空分异规律。     

甲烷单加氧酶的研究进展

甲烷氧化细菌在转化甲烷制造新型燃料、单细胞蛋白和新功能酶生产、污水处理等方面有着潜在的应用前景,因此,甲烷单加氧酶作为其代谢过程中重要的酶系也受到人们的广泛关注。我们简要综述了近年来对甲烷单加氧酶的性质、结构、催化机理等方面的研究,特别是对颗粒性甲皖单加氧酶的相关性质进行了详细的阐述。     

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.     

Oxidation of methane in boreal forest soils: a comparison of seven measures

Methane oxidation rates were measured in boreal forest soils using seven techniques that provide a range of information on soil CH₄ oxidation. These include: (a) short-term static chamber experiments with a free-air (1.7 ppm CH₄) headspace, (b) estimating CH₄ oxidation rates from soil CH₄ distributions and (c)²²²Rn-calibrated flux measurements, (d) day-long static chamber experiments with free-air and amended (+20 to 2000 PPM CH₄) headspaces, (e) jar experiments on soil core sections using free-air and (f) amended (+500 ppm CH₄) headspaces, and (g) jar experiments on core sections involving tracer additions of¹⁴CH₄. Short-term unamended chamber measurements,²²²Rn-calibrated flux measurements, and soil CH₄ distributions show independently that the soils are capable of oxidizing atmospheric CH₄ at rates ranging to < 2 mg m^–2 d^–1. Jar experiments with free-air headspaces and soil CH₄ profiles show that CH₄ oxidation occurs to a soil depth of 60 cm and is maximum in the 10 to 20 cm zone. Jar experiments and chamber measurements with free-air headspaces show that CH₄ oxidation occurs at low (< 0.9 ppm) thresholds. The¹⁴CH₄-amended jar experiments show the distribution of end products of CH₄ oxidation; 60% is transformed to CO₂ and the remainder is incorporated in biomass. Chamber and jar experiments under amended atmospheres show that these soils have a high capacity for CH₄ oxidation and indicate potential CH₄ oxidation rates as high as 867 mg m^–2 d^–1. Methane oxidation in moist soils modulates CH₄ emission and can serve as a negative feedback on atmospheric CH₄ increases.     

Soil environmental variables affecting the flux of methane from a range of forest, moorland and agricultural soils

Measurements of the net methane exchange over a range of forest, moorland, and agricultural soils in Scotland were made during the period April to June 1994 and 1995. Fluxes of CH₄ ranged from oxidation –12.3 to an emission of 6.8 ng m^–2 s^–1. The balance between CH₄ oxidation and emission depended on the physical conditions of the soil, primarily soil moisture. The largest oxidation rates were found in the mineral forest soils, and CH₄ emission was observed in several peat soils. The smallest oxidation rate was observed in an agricultural soil. The relationship between CH₄ flux and soil moisture observed in peats (Flux_{CH 4} = 0.023 × %H₂O (dry weight) – 7.44, p > 0.05) was such that CH₄ oxidation was observed at soil moistures less than 325%( ± 80%). CH₄ emission was found at soil moistures exceeding this value. A large range of CH₄ oxidation rates were observed over a small soil moisture range in the mineral soils. CH₄ oxidation in mineral soils was negatively correlated with soil bulk density (Flux_{CH 4} = –37.35 × bulk density (g cm^–3) + 48.83, p > 0.05). Increased nitrogen loading of the soil due to N fixation, atmospheric deposition of N, and fertilisation, were consistently associated with decreases in the soil sink for CH₄, typically in the range 50 to 80%, on a range of soil types and land uses.     

Intensity of the Microbiological Processes of the Methane Cycle in Different Types of Baltic Lakes

The intensity of the microbiological processes of methane formation (MF) and methane oxidation (MO) was determined in the sediments and water of different types of Baltic lakes. The emission of methane from the lake sediments and methane distribution in the water column of the lakes were studied as functions of the lake productivity and hydrologic conditions. During summers, the intensity of MF in the lake sediments and waters varied from 0.001 to 106 ml CH₄/(dm³ day) and from 0 to 3.2 ml CH₄/(l day), respectively, and the intensity of MO in the sediments and water varied from 0 to 11.2 ml CH₄/(dm³ day) and from 0 to 1.1 ml CH₄/(l day), respectively. The total methane production (MP) in the lakes varied from 15 to 5000 ml CH₄/(m² day). In anoxic waters, the MP comprised 9–18% of the total PM in the lakes. The consumption of organic carbon for methanogenesis varied from 0.03 to 9.7 g/(m² day). The role of the methane cycle in the degradation of organic matter in the lakes increased with their productivity.     

Dimethylsulfide and methane thiol in sediment porewater of a Danish estuary

Seasonal variation of dimethylsulfide (DMS) and methane thiol (MSH) concentrations in sediment porewater was determined in a Danish estuary. Dimethylsulfide (DMDS) was never found. Detectable DMS levels of up to 0.1 M were found only in the summer and only within the upper 5 cm of the sediment. The DMS accumulation was probably associated with decomposing fragments of macro-algae in the surface layer. Significant MSH accumulation of up to 1 M was found only in the deep, CH₄-rich sediment below the SO₄ ^2- zone. With depth, a detectable MSH level could thus be observed below the 1 mM SO₄ ^2--isopleth which also marked the SO₄ ^2--CH₄ transition. The transition zone was located deeper in the sediment in winter (20–25 cm depth) than in summer (5–10 cm depth). The absence of MSH in the SO₄ ^2- zone could be due to rapid utilization of the compound by SO₄ ^2--reducing bacteria. A possible involvement of MSH in anaerobic CH₄ oxidation at the transition zone is discussed; CH₄ and sulfide (HS^- form, pH 7) are proposed to form MSH and H₂ which in turn may be metabolized by, e.g. SO₄ ^2--reducing bacteria.