FMT150光养生物反应器文献—2012 ELEVATED CARBON DIOXIDE DIFFERENTIALLY ALTERS THE PHOTOPHYSIOLOGY

spectrometer equipped with a automatic carbonate preparation system(CAPS).Results are reported relative to the Vienna Pee Dee Belemnite standard(VPDB).Standard external analytical precision,based on replicate analysis of in-house standards calibrated to NBS-19,is better than0.1‰for d18O and d13C.Received1September;accepted25October2004;doi:10.1038/nature03135.1.Broecker,W.S.&Peng,T.-H.The role of CaCO3compensation in the glacial to interglacialatmospheric CO2change.Glob.Biogeochem.Cycles1,15–29(1987).2.Van Andel,T.H.Mesozoic/Cenozoic calcite compensation depth and the global distribution ofcalcareous sediments.Earth Planet.Sci.Lett.26,187–194(1975).3.Kennett,J.P.&Shackleton,N.J.Oxygen isotopic evidence for the development of the psychrosphere38Myr ago.Nature260,513–515(1976).ler,K.G.,Wright,J.D.&Fairbanks,R.G.Unlocking the ice house:Oligocene-Miocene oxygenisotopes,eustasy,and margin erosion.J.Geophys.Res.96,B4,6829–6849(1991).5.Zachos,J.C.,Quinn,T.M.&Salamy,K.A.High-resolution(104years)deep-sea foraminiferal stableisotope records of the Eocene-Oligocene climate transition.Palaeoceanography11,251–266(1996).6.Lear,C.H.,Elderfield,H.&Wilson,P.A.Cenozoic deep-sea temperatures and global ice volumesfrom Mg/Ca in benthic foraminiferal calcite.Science287,269–272(2000).7.DeConto,R.M.&Pollard,D.Rapid Cenozoic glaciation of Antarctica triggered by decliningatmospheric CO2.Nature421,245–249(2003).8.Shipboard Scientific Party2002.Leg199summary.Proc.ODP Init.Rep.(eds Lyle,M.W.,Wilson,P.A.&Janecek,T.R.)199,1–87(2002).skar,J.et al.Long term evolution and chaotic diffusion of the insolation quantities of Mars.Icarus170,343–364(2004).10.Peterson,L.C.Backman,te Cenozoic carbonate accumulation and the history of the carbonatecompensation depth in the western equatorial Indian Ocean.Proc.ODP Sci.Res.(eds Duncan,R.A., Backman,J.,Dunbar,R.B.&Peterson,L.C.)115,467–489(1990).11.Salamy,K.A.&Zachos,test Eocene-Early Oligocene climate change and Southern Oceanfertility:inferences from sediment accumulation and stable isotope data.Palaeogeogr.Palaeoclimatol.Palaeoecol.145,61–77(1999).12.Ehrmann,W.U.&Mackensen,A.Sedimentological evidence for the formation of an East Antarcticice sheet in Eocene/Oligocene time.Palaeogeogr.Palaeoclimatol.Palaeoecol.93,85–112(1992). 13.Ivany,L.C.,Patterson,W.P.&Lohmann,K.C.Cooler winters as a possible cause of mass extinction atthe Eocene/Oligocene boundary.Nature407,887–890(2000).14.Pa¨like,H.,Laskar,J.&Shackleton,N.J.Geologic constraints on the chaotic diffusion of the solarsystem.Geology32(11),929–932doi:10.1130/G20750(2004).15.Billups,K.&Schrag,D.P.Application of benthic foraminiferal Mg/Ca ratios to questions of Cenozoicclimate change.Earth Planet.Sci.Lett.209,181–195(2003).16.Lear,C.H.,Rosenthal,Y.,Coxall,H.K.&Wilson,te Eocene to early Miocene ice-sheetdynamics and the global carbon cycle.Paleoceanography19,doi:10.1029/2004PA001039(2004). 17.Pekar,S.F.,Christie-Blick,N.,Kominz,M.A.&Miller,K.G.Calibration between eustatic estimatesfrom backstripping and oxygen isotopic records for the Oligocene.Geology30,903–906(2002). 18.Lythe,M.B.,Vaughan,D.G.&BEDMAP Consortium,BEDMAP:A new ice thickness and subglacialtopographic model of Antarctica.J.Geophys.Res.106,B6,11335–11351(2001).19.Huybrechts,P.Sea-level changes at the LGM from ice-dynamic reconstructions of the Greenland andAntarctic ice sheets during the glacial cycles.Quat.Sci.Rev.21,203–231(2002).20.Hindmarsh,R.C.A.Time-scales and degrees of freedom operating in the evolution of continental ice-sheets.Trans.R.Soc.Edinb.Earth Sci.81,371–384(1990).21.Davies,R.,Cartwright,J.,Pike,J.&Line,C.Early Oligocene initiation of North Atlantic deep waterformation.Nature410,917–920(2001).22.Archer,D.&Maier-Reimer,E.Effect of deep-sea sedimentary calcite preservation on atmosphericCO2concentration.Nature367,260–263(1994).23.Sigman,D.M.&Boyle,E.A.Glacial/interglacial variations in atmospheric carbon dioxide.Nature407,859–869(2000).24.Zeebe,R.E.&Westbroek,P.A simple model for the CaCO3saturation state of the ocean:The“Strangelove,”the“Neritan,”and the“Cretan”Ocean.Geochem.Geophys.Geosyst.4,1104(2003).25.Kump,L.R.&Arthur,M.A.in Tectonics Uplift and Climate Change(ed.Ruddiman,W.F.)399–426(Plenum,New York,1997).26.Zachos,J.C.,Opdyke,B.N.,Quinn,T.M.,Jones,C.E.&Halliday,A.N.Early Cenozoic glaciation,Antarctic weathering and seawater87Sr/86Sr;is there a link?Chem.Geol.161,165–180(1999). 27.Ravizza,G.&Peucker-Ehrenbrink,B.The marine187Os/188Os record of the Eocene-Oligocenetransition:the interplay of weathering and glaciation.Earth Planet.Sci.Lett.210,151–165(2003).28.Berger,W.H.&Winterer,E.L.in Plate Stratigraphy and the Fluctuating Carbonate line in PelagicSediments:On Land and Under the Sea(eds Hsu¨,K.J.&Jenkyns,H.C.)11–48(Int.Assoc.Sedimentologists 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Acknowledgements We thank the Shipboard Party of Ocean Drilling Program Leg199for assistance at sea and M.Bolshaw,M.Cooper and H.Birch for laboratory assistance.This work was supported by a NERC UK ODP grant to P.A.W.,a Royal Commission for the Exhibition of1851 fellowship awarded to H.K.C.and by Swedish Research Council(VR)funding to H.P.We thank W.Broecker,R.Hindmarsh,S.D’Hondt,A.Merico,Y.Rosenthal,R.Rickaby,J.Shepherd and T.Tyrrell for discussions and comments on an earlier draft and L.Kump for a constructive review.Competing interests statement The authors declare that they have no competingfinancial interests.Correspondence and requests for materials should be addressed to P.A.W.(paw1@)............................................................... Similar response of labile and resistant soil organic matterpools to changes in temperature Changming Fang1,Pete Smith1,John B.Moncrieff2&Jo U.Smith11School of Biological Sciences,University of Aberdeen,Aberdeen AB243UU,UK 2Ecology and Resource Management,School of GeoSciences,The University of Edinburgh,Edinburgh EH93JU,UK ............................................................................................................................................................................. Our understanding of the relationship between the decompo-sition of soil organic matter(SOM)and soil temperature affects our predictions of the impact of climate change on soil-stored carbon1.One current opinion is that the decomposition of soil labile carbon is sensitive to temperature variation whereas resistant components are insensitive2–4.The resistant carbon or organic matter in mineral soil is then assumed to be unresponsive to global warming2,4.But the global pattern and magnitude of the predicted future soil carbon stock will mainly rely on the temperature sensitivity of these resistant carbon pools.To inves-tigate this sensitivity,we have incubated soils under changing temperature.Here we report that SOM decomposition or soil basal respiration rate was significantly affected by changes in SOM components associated with soil depth,sampling method and incubation time.Wefind,however,that the temperature sensitivity for SOM decomposition was not affected,suggesting that the temperature sensitivity for resistant organic matter pools does not differ significantly from that of labile pools,and that both types of SOM will therefore respond similarly to global warming.The temperature sensitivity of SOM decomposition,commonly referred to as Q10,is critical for modelling changes in soil C stock3–6. The assumption that the decomposition of old organic matter2–3or organic C in mineral soil4does not vary with temperature—that is, that the decomposition of labile C pools are sensitive,but resistant pools are insensitive,to temperature perturbations—suggests that higher losses of carbon will occur from soils in boreal and tundra regions in response to global warming.This is because these soils have the largest store of labile organic matter,and are predicted to experience the greatest rise in temperature7.Tropical soils may release less C than previously predicted4owing to a large store of SOM in deep soil8and the high proportion of resistant C pools in SOM.Soil warming experiments,an analogue for the effects of global warming on SOM decomposition9,suggest that the effect of warming on SOM decomposition may decline with time.The change in SOM composition associated with warming and the different temperature sensitivity of the C pools were assumed to be responsible for this decline10–11.Despite the common assertion that SOM composition affects the temperature sensitivity of SOM decomposition,experimental or modelling evidence is yet to be presented.If the temperature sensitivity of SOM decomposition is not affected by SOM composition,predictions of climate change impacts on soil stored C will be greatly affected.By definition,the temperature sensitivity of SOM decomposition is the change in SOM decomposition rate with temperature under otherwise constant conditions5.At present,this concept is often confused with concepts of SOM turnover4,12–13or SOM dynamics2–4 under different environmental conditions with accompanying different temperatures.Temperature sensitivity of SOM decompo-sition(or Q10)estimated by incubating soils at different but constant temperatures14–16or by radiocarbon accumulation in undisturbed soils13is confounded by many factors other than temperature.We incubated soil samples under changing temperature toletters to natureNATURE|VOL433|6JANUARY2005|/nature57©2005Nature Publishing Groupinvestigate the influence of SOM composition on the temperature dependence of SOM decomposition.Figure 1shows that soil C contents for both labile components (water-dissolved organic carbon (DOC),microbial carbon (C mic )and K 2SO 4-extracted carbon (C KSO ))and the total organic carbon (TOC),are signifi-cantly lower in the subsoil (20–30cm)than in the surface soil (0–10cm).The ratio of DOC:TOC and C KSO :TOC declined signifi-cantly with soil depth (F ¼28.5and 36.1,respectively,P ,0.0001),but C mic :TOC was not significantly affected by depth (F ¼1.9,P ,0.2).After the initial flush of CO 2emission,soil basal respi-ration rate at 208C was (mean ^s.e.m.)6.67^0.46m g CO 2per g dry soil per h for root-free samples in the 0–10cm layer,but only 1.92^0.20m g CO 2per g dry soil per h for the 20–30cm layer.Corresponding values were 6.27^0.66and 1.47^0.16for intact samples.Over a period up to 88days,the subsoil respired only ,0.29^0.13of the CO 2respired in the surface soil.These results indicate that soil basal respiration rate is closely related to variations in C pools occurring at different soil depths.Q 10values for individual soil samples varied in the range 1.97–2.21during the early stage of incubation (up to day 10).No significant correlation was found between Q 10and the rate of basal respiration.Relationships in Fig.1between respiration rate,Q 10value and SOM pools reflect the long-term acclimation of the microbial community to the environment (such as temperature,moisture and O 2)associated with soil depths.During the incubation,there was a significant decline in the labile components (Fig.2c,d,f).After 108days incubation,DOC was 0.73^0.14and C KSO was 0.62^0.065of initial values when averaged over all samples.The greatest variation following incu-bation was observed in C mic .The average C mic at day 42was only 0.43^0.13of the initial content,and less than 0.10^0.0057after 108days incubation.Changes in the average TOC during incu-bation were not significant (Fig.2b).At the end of the incubation,average TOC was 0.94^0.19of the initial content.Soil respiration rate consistently declined with time (Fig.2e).The association between respiration rate and C mic during the incubation suggests that the variation in microbial biomass may be a major cause of the temporal changes in soil respiration.The response of soil basal respiration to temperature was notaffected by the depletion of labile C during the incubation.Q 10values averaged for all samples were in the range 2.01–2.30for the whole incubation period (Fig.2a).There is no significant change in Q 10for soil basal respiration with incubation time,despite the fact that Q 10was more variable during the later stages of incubation.As time progressed,the resistant C component contributed a greater portion of the total soil basal respiration owing to the depletion of labile C pools (Supplementary Fig.2).The Q 10value for soil basal respiration should gradually decrease if resistant C is significantly different from labile pools and insensitive to temperature variation (Supplementary Fig.3).A constant Q 10for soil basal respiration suggests that the temperature dependence of resistant C is not significantly different from that for labile pools.In most incubation experiments,soil samples have been sepa-rately incubated at different but constant temperatures 12,14,15.Three different methods have been used to estimate SOM decomposition and its temperature sensitivity:the total mass loss 3,17,the time required for a given percentage of mass loss 17,and the soil respir-ation rate 14,18.A decline in soil respiration rate was commonly observed as incubation times increased 14,17,19,20.This decline is expected to be greater at higher than at lower temperatures because of the greater depletion and degradation of C pools 21.Temperature sensitivity is likely to be underestimated if turnover rate is derived from studies of total mass loss for a given time period or from respiration rates at different constant temperatures,owing to the higher decline in C turnover rate at higher temperature.If Q 10is estimated using the time required for a given percentage of mass loss,the value will be overestimated.In this case,temporal effects on estimated C turnover rate are more pronounced at lower temperatures than at higher temperatures.Data of total mass loss from soil incubations longer than one year were used to support the opinion that decomposition rates of organic matter in mineral soil do not vary with temperature 4.Estimated C turnover rates from a long-term incubation will be significantly different from those occurring in the field,owing to the quick decline in soil microbial biomass and respiration rate during incubation.In such exper-iments,the temperature sensitivity of SOM decomposition may have been seriously biased or underestimated because respiration rates at all temperatures are close to zero at the later stage of incubation.In soil warming experiments,the observed decline of warming effects on SOM decomposition with time 11does not necessarily mean that the decomposition of resistant C is less sensitive to elevated temperature than the labile component.Provided that the increase in net primary production (NPP)due to warming islessFigure 1Soil carbon components,respiration rate and associated Q 10values with respect to soil depth and sampling method (four replicates for each sample).Respiration rate was an average of data measured at 208C in days 3and 5.The Q 10value was estimated with soil respiration rates under changing temperature for the period of days 3–10.All values are normalized against that of surface root-free sample.Soil respiration rate is significantly related to concentrations of C pools owing to soil depth andsampling method,but Q 10does not change with respiration rate or C concentrations.Error bars indicate standard deviation.DOC,dissolved organic carbon;TOC,total organiccarbon.Figure 2Variations in respiration rate and soil carbon pools with increasing incubation time.Values are averages of all four samples,and normalized by initial values.a ,Q 10value;b ,TOC;c ,DOC;d ,K 2SO 4-extracted C;e ,respiration rate at 208C;and f ,microbial biomass C.Error bars are standard deviation.Respiration rate declined rapidly owing to the depletion of labile components (DOC,C KSO and C mic ),but the Q 10value of soil respiration remained unchanged.letters to natureNATURE |VOL 433|6JANUARY 2005|/nature58© 2005Nature Publishing Groupthan the increase in SOM decomposition rate,a decline in warming effect on SOM decomposition is always expected.In the long-term, the microbial community may become acclimated to warming with changed activities.The contribution of this acclimation is not yet clear.For long-term climate change,the response of the resistant pool of SOM plays a critical role in regulating soil C stocks.Given the predicted climate change in Europe in the next century,the greatest loss of SOM is expected in soils where the present mean annual temperature(MAT)is less than48C,and this net release of SOM will gradually decrease with MAT gradient(Fig.3a–c).(This predicted climate change is climate forcing according to the implementation by the Hadley Centre Climate Model(HadCM3) of the Intergovernmental Panel on Climate Change(IPCC)A1FI (world market–fossil fuel intensive)emission scenario22.)With a moderate change in the temperature sensitivity of the resistant C pool(humus pool of the Rothamsted Carbon Model23only),from Q10¼2.98to about2.58(at108C),sensitivity induced change will significantly reduce the net SOM release in temperate soils(present MAT.48C).By2100,the reduction in SOM loss could be up to 46%in arable soil,37%in grassland,and32%in forest for regions where the present MAT is greater than158C(Fig.3d).At the global scale,this reduction will be large enough to change our prediction of the magnitude and spatial pattern of SOM stocks in the future.Our study does not support the opinion that resistant C pools are significantly less responsive to temperature variation than labile C pools.A MethodsSoil samples(intact and root-free)were collected from a middle-aged plantation of Sitka spruce(Picea sitchensis)in Scotland(568370N,38480W).Mineral soils were collected from four locations in the site at depths of0–10,20–30cm.Root-free samples were made by sieving soil through a2mm mesh to remove plant detritus,root and gravel.For each depth,approximately600–800g soil was taken and packed into a chamber to the original bulk density.Intact soil samples(,10£10cm)were taken next to each root-free sample, following the method of ref.5.Soil samples were analysed to determine TOC24,DOC25and C KSO26.C mic was determined by fumigation extraction26.Samples(16in total)were incubated in the laboratory using a programmable water bath(developed in The University of Edinburgh,UK).Temperature was changed commonly between4and448C (continuously increased from the lowest to the highest with a step of48C and then decreased,reaching a new temperature within two hours).Each temperature was held for about9h.Before and after each round of temperature change,soils were kept at208C for a few days.Soil moisture contents were monitored and adjusted accordingly by adding water at the surface of the soil sample,and fresh air was continuously passed through each chamber during the incubation.Respired CO2was measured with an infrared gas analyser in differential mode,logged every second for7min for each chamber,but only the average over the last four minutes was used.The16chambers were measured sequentially,and four rounds of measurement were made before changing to another temperature.During each round of temperature change,the mean respiration rate at a given temperature was an average of values measured at that temperature when the temperature was increasing and decreasing(Supplementary Fig.1).Mean respiration rates at different temperatures werefitted with an exponential model5ðR¼a exp½ln Q10ðT=10Þ Þto calculate the Q10 value.More information about data analysis is included in the Supplementary Methods, which also explain how we assessed contributions of the resistant C pool to the total SOM decomposition and its Q10.Received30July;accepted22October2004;doi:10.1038/nature03138.1.Lenton,T.M.&Huntingford,C.Global terrestrial carbon storage and uncertainties in its temperaturesensitivity examined with a simple model.Glob.Change Biol.9,1333–1352(2003).2.Liski,J.,Ilvesniemi,H.,Ma¨kela¨,A.&Westman,C.J.CO2emissions from soil in response to climaticwarming are overestimated—The decomposition of old soil organic matter is tolerant of temperature.Ambio28,171–174(1999).3.Thornley,J.H.M.&Cannell,M.G.R.Soil carbon storage response to temperature:a hypothesis.Ann.Bot.87,591–598(2001).4.Giardina,C.P.&Ryan,M.G.Evidence that decomposition rates of organic carbon in mineral soil donot vary with temperature.Nature404,858–861(2000).5.Fang,C.&Moncrieff,J.B.The dependence of soil CO2efflux on temperature.Soil Biol.Biochem.33,155–165(2001).6.Sanderman,J.,Amundson,R.G.&Baldocchi,D.D.Application of eddy covariance measurements tothe temperature dependence of soil organic matter mean residence time.Glob.Biogeochem.Cycles17, doi:10.1029/2001GB001833(2003).7.Schlesinger,W.H.&Andrews,J.A.Soil respiration and the global carbon cycle.Biogeochemistry48,7–20(2000).8.Jobba´gy,E.G.&Jackson,R.B.The vertical distribution of soil organic carbon and its relation toclimate and vegetation.Ecol.Appl.10,423–436(2000).9.Rustad,L.E.et al.A meta-analysis of the response of soil respiration,net nitrogen mineralization,andaboveground plant growth to experimental ecosystem warming.Oecologia126,543–562(2001). 10.Peterjohn,W.T.,Melillo,J.M.&Bowles,S.T.Soil warming and trace gasfluxes:experimental designand preliminaryflux results.Oecologia93,18–24(1993).11.Peterjohn,W.T.et al.Response of trace gasfluxes and N availability to experimentally elevated soiltemperature.Ecol.Appl.4,617–625(1994).12.Dalias,P.,Anderson,J.M.,Bottner,P.&Couˆteaux,M.-M.T emperature responses of carbonmineralization in conifer forest soils from different regional climates incubated under standard laboratory conditions.Glob.Change Biol.6,181–192(2001).13.Trumbore,S.E.,Chadwick,O.A.&Amundson,R.Rapid exchange between soil carbon andatmospheric carbon dioxide driven by temperature change.Science272,393–396(1996).14.Winkler,J.P.,Cherry,R.S.&Schlesinger,W.H.The Q10relationship of microbial respiration in atemperate forest soil.Soil Biol.Biochem.28,1067–1072(1996).15.MacDonald,N.W.,Zak,D.R.&Pregitzer,K.S.Temperature effects on kinetics of microbialrespiration and net nitrogen and sulfur mineralization.Soil Sci.Soc.Am.J.59,233–240(1995). 16.Ross,D.J.&Tate,K.R.Microbial C and N,and respiratory activity,in litter and soil of a southernbeech(Nothofagus)forest:distribution and properties.Soil Biol.Biochem.25,477–483(1994). 17.Reichstein,M.,Bednorz,F.,Broll,G.&Ka¨tterer,T.T emperature dependence of carbon mineralisation:conclusions from a long-term incubation of subalpine soil samples.Soil Biol.Biochem.32,947–958 (2000).18.Fierer,N.,Allen,A.S.,Schimel,J.P.&Holden,P.A.Controls on microbial CO2production:acomparison of surface and subsurface soil horizon.Glob.Change Biol.9,1322–1332(2003).19.Lovell,R.D.&Jarvis,S.C.Soil microbial biomass and activity in soil from different grasslandmanagement treatments stored under controlled conditions.Soil Biol.Biochem.30,2077–2085 (1998).20.Lomander,A.,Ka¨tterer,T.&Andre´n,O.Carbon dioxide evolution from top-and subsoil as affected bymoisture and constant andfluctuating temperature.Soil Biol.Biochem.30,2017–2022(1998). 21.Grisi,B.,Grace,C.,Brookes,P.C.,Benedetti,A.&Dell’abate,M.T.Temperature effects on organicmatter and microbial biomass dynamics in temperate and tropical soils.Soil Biol.Biochem.30, 1309–1315(1998).22.IPCC.Special Report on Emissions Scenarios(Cambridge Univ.Press,Cambridge,UK,2000).23.Coleman,K.&Jenkinson,D.S.in Evaluation of Soil Organic Matter Models Using Existing Long-TermDatasets(eds Powlson,D.S.,Smith,P.&Smith,J.U.)237–246(NATO ASI Series I Vol.38,Springer, Heidelberg,1996).24.Allen,S.E.,Grimshaw,H.M.,Parkingson,J.A.&Quarmby,C.Chemical Analysis of EcologicalMaterials137–139(Blackwell Scientific,Oxford,1974).25.Martin-Olmedo,P.&Rees,R.M.Short-term N availability in response to dissolved organic-carbonfrom poultry manure,alone or in combination with cellulose.Biol.Fert.Soils29,386–393(1999).26.O¨hlinger,R.in Methods in Soil Biology(eds Schinner,F.et al.)56–58(Springer,Berlin,1995). Supplementary Information accompanies the paper on /nature. Acknowledgements We thank M.Wattenbarch and C.Zhang for assistance with the modelling. The pan-European modelling used data sets arising from the EU-funded ATEAM project. Competing interests statement The authors declare that they have no competingfinancial interests.Correspondence and requests for materials should be addressed to C.F.(c.fang@).Figure3Changes in soil C by2100for European soils.The baseline(solid lines in a–c)was from the original Roth-C model23projection(Q10¼2.98at108C for all C pools).Thetemperature sensitivity of humus was changed to80%of the original value(Q10¼2.58at108C,dashed lines in a–c).The loss of soil C is an average of all grid cells(21,976cellsat100£100resolution)according to present MAT.The percentage of net soil C loss withmodified Q10¼2.58for humus is relative to baseline decreases with MAT gradient(d).SOM,soil organic matter.letters to natureNATURE|VOL433|6JANUARY2005|/nature59©2005Nature Publishing Group。

Abstract: SBR reactor was performed to incubate polyphosphate accumulating organism ( PAO ) , and it was checked out of the system by fluorescence in situ hybridization. As PAO is a kind of ordinary heterotrophic bacteria, it was ex cluded the ability of phosphate release and uptake and it was considered only the capacity of denitrification of the target biomass. The results indicated that acetate and PHB can be the electron donors of PAO to denitrify. When fed with acetate, the denitrifying rate and PHB producing rate were independent of initial nitrate concentration. However, served as more nitrate in the reactor , it would be less PHB produced and fewer nitrate reducing when using same amount of acetate. In view of PHB stored as an internal carbon and energy source, it presented as a reaction of zero order to the substrate by PAO to denitrify, such as nitrate, besides, the specific denitrifying rate was 0 973 3 mg ( g h) and the specific PHB consuming rate was 2 462 6 mg ( g h) . Key words: enhanced biological phosphorus removal; polyphosphate accumulating organism( PAO) ; denitrification; electron donor

2A review of research progress on CO capture,storage,and utilization in 34Q156789111213141516171819202122232425262728293031323334353637383940414243444546474849505152535455565758596061626364656667686970717273747576with 58%of the sources being located within the east and south 77central regions.The contributions of large point sources in each 78sector to total CO 2emissions in China are listed in Fig.2[13].With 79rapid development of energy technologies in the 21st century,fos-80sil fuels,especially coal,will still remain the dominant energy0016-2361/$-see front matter Ó2011Elsevier Ltd.All rights reserved.doi:10.1016/j.fuel.2011.08.022⇑Corresponding authors.Q2Address:State Key Laboratory of Coal Conversion,Institute of Coal Chemistry,Chinese Academy of Sciences,Taiyuan 030001,China (Y.Sun).Tel.:+863514049612;fax:+863514041153.E-mail addresses:zhaoning@ (N.Zhao),weiwei@ (W.Wei),yhsun@ (Y.Sun).Please cite this article in press as:L Q1i L et al.A review of research progress on CO 2capture,storage,and utilization in Chinese Academy of Sciences.Fuel(2011),doi:10.1016/j.fuel.2011.08.022source in China for decades to come.Chinese government recognized the huge challenge of CO 2abatement while satisfying ever-increasing energy demand.In the light of this situation,November 26,2009,China officially announced action to control emissions per unit of GDP by 40–45%by 2020,based on 86levels [14].To address this,China is undertaking a range of techni-87cal research and development projects on CCSU,including the na-88tional fundamental research and high-tech programs,as well as a 89large number of international programs.The CCS projects,fun-90dings,and research institutes in China is shown in Table 1.91Since 1990,China had carried out a series of climate change 92projects under framework of national programs,such as China’s 93National Climate Change Program (CNCCP),National Hi-tech R&D949596979899100101102103104105106107108109110111112113114115116117118119120121cooperation with international on CCSU.On the basis of the finical 122support of both Chinese government and CAS,a lot of progresses 123were obtained in several academic institutes in CAS including 124CO 2capture;enhanced oil recovery (EOR)and enhanced coal bed 125methane (ECBM)projects as well as CO 2chemical utilizations.This 126brief review has covered the research progress in CO 2capture,stor-127age,and utilization in CAS.2.The contributions of large point sources in each sector to overall total emissions in China [12].Please cite this article in press as:L Q1i L et al.A review of research progress on CO 2capture,storage,and utilization in Chinese Academy of Sciences.Fuel(2011),doi:10.1016/j.fuel.2011.08.022128129130131132133134135136137aration,and cryogenic fractionation.138 2.1.Amine-based scrubbing solvent139Amine scrubbing is a well known technology for capturing CO 2140from flue gas,which has been widely deployed on a large scale 141across several industries [25–28].The industrially most important142143144145146147148149150151152the environment [30].1532.2.Ionic liquids154Therefore,a nonvolatile solvent that could facilitate CO 2capture 155without the loss of solvent into the gas stream would be advanta-156geous.Ionic liquids (ILs)are commonly defined as liquids whichTable 1CCS projects,fundings,and research institutes in China.China and international cooperation on CCS projects and fundingsResearch institutes aBNLMS–CAS IET–CAS RCEES–CAS ICC–CAS IPE–CAS LICP–CAS CIAC–CAS National High Technology Research and Development Program of China (863)SIC–CAS National Key Basic Research and Development Program of China (973)IGG–CAS China’s National Climate Change Program (CNCCP)IAP–CAS L.L Q1i et al./Fuel xxx (2011)xxx–xxx3Please cite this article in press as:L Q1i L et al.A review of research progress on CO 2capture,storage,and utilization in Chinese Academy of Sciences.Fuel(2011),doi:10.1016/j.fuel.2011.08.022157are composed entirely of ions with a melting point of less than 158100°C.ILs have many unique properties in comparison to other 159solvents as extremely low volatility,broad range of liquid temper-160ature,high thermal and chemical stability,and tunable physico-161chemical characteristics and as a result,ILs have been considered 162as a potential substitute of aqueous amine solutions for CO 2cap-163ture [31–34].164In Changchun Institute of Applied Chemistry,Chinese Academy 165of Sciences (CIAC–CAS),a novel dissolving process for chitin and 166chitosan was developed by using the ionic liquid 1-butyl-3-167methyl-imidazolium chloride ([Bmim]Cl)as a solvent for capturing 168and releasing CO 2.The results showed that the chitin/IL and chito-169170171172173174175176177178179180181182183184185186187188189190191192193194195196197198199200201tant to consider the maximum mass loading when considering the 202support of ILs on inert substrates –yes,these can enhance the ILs’203ability to take up CO 2,but at the expense of cycling an inert sorbent 204round a thermal cycle.The ILs are also monstrously expensive,the 205complex structure,and high cost for preparation,compared to sim-206pler solvents such as MEA or ammonia.Thus,the potential for 207improving CO 2solubilities and reducing cost of the ILs still needs 208to be studied for future applications.In 2010,in Beijing National 209Laboratory for Molecular,Chinese Academy of Sciences (BNLMS–210CAS),Zhang and co-workers first reported on CO 2capture by 211hydrocarbon surfactant liquids.It also found that CO 2had high sol-212ubility in low-cost hydrocarbon surfactant liquids,and the ab-213and the 214215216such as corrosion,at 217regenerable solid sor-218concept for CO 2recov-219into amine-based and 220221222with various so-223as silica gels,activated 224have been shown to phys-225enhance the sorp-226of many amine-based 227In Dalian Institute of 228(DICP–CAS),Zhang 229silica foam (MCF)materi-230with polyethyl-231The results showed that 232having large window 2333.45mmol CO 2/g sorbent 234In Institute of Coal Chem-235Zhao et al.studied 236materials derived 237sorption capabili-238°C and 1bar.The as-pre-239selectivity for CO 2over 240prepared a series of CO 2241pentamine (TEPA)was 242(PMHS)based mesopor-243The highest absorption 24475°C with the 10vol.%245was higher than most 246Desorption could 247in 1h [46].248of amine-based sorbent 249capacity of solid sorbent.250have poor mechanical 251amine-based sorbents 252and require signifi-253processes.254255sorbents for CO 2capture 256Alkali earth metal,such 257form alkali earth metal-258vapor at high tempera-259and post-combus-260simplified process flow 261the calcium looping 262vessel (the carbonator)4L.L Q1i et al./Fuel xxx (2011)xxx–xxxPlease cite this article in press as:L Q1i L et al.A review of research progress on CO 2capture,storage,and utilization in Chinese Academy of Sciences.Fuel(2011),doi:10.1016/j.fuel.2011.08.022the carbonation reaction between CO 2and solid CaO separates CO from coal-combustion flue gas at a temperature between 600°and 650°C.The CaCO 3formed is then passed to another vessel (the calciner),where it is heated to reverse the reaction (900–950°C),releasing the CO 2suitable for sequestration,and regener-ating the CaO-sorbent which is then return to the carbonator.The carbonation process is exothermic,which is matched with the temperature of a steam cycle,allowing recuperation of the heat.In IPE–CAS,the decomposition conditions of CaCO 3particles for CO 2capture in a steam dilution atmosphere (20–100%steam 307308309310311312313314315316317318319320321322323324325326327328329330332333334335336337338339340341342343344345346347348349350351352353354355Fig.3.The process flow diagram of post-combustion capture using the calcium looping cycle [47,48].Please cite this article in press as:L Q1i L et al.A review of research progress on CO 2capture,storage,and utilization in Chinese Academy of Sciences.Fuel(2011),doi:10.1016/j.fuel.2011.08.022strength (998N/cm 2)and exhibited good stability in multiple cy-cles [74,75].Furthermore,the application of a conceptual CO 2cap-ture process using this sorbent was proposed for an existing coal fired power plant [75].However,to optimize CO 2sorption capacity,understand of the interaction between CO 2and the sorbent need to be studied in the further work.Moreover,much work remains before the technology fluidized bed CO 2capture can be commercialized.Simulta-neously,the numerical simulation based on the computational fluid 365dynamics (CFD)method will become a research focus in the future.366 3.CO 2storage367Following the capture and transport process,CO 2can be dis-368posed of in natural sites such as deep geological sequestration,369mineral carbonation,or ocean storage [76].There are three geolog-370ical formations that have also been recognized as major potential 371CO 2sinks:deep saline-filled sedimentary (DSFs),depleted oil 372natural gas reservoirs,and unmineable coal-seams.The geology 373also suggests possibilities for CO 2enhanced oil recovery (CO 374EOR),CO 2enhanced gas recovery (CO 2–EGR)and CO 2enhanced 375coal-bed methane recovery (CO 2–ECBM)projects [12].3763.1.Geological sequestration377Geological storage involves injecting CO 2at depths greater than 3781000m into porous sedimentary formations using technologies 379derived from the oil and gas industry [77].CO 2can be stored in 380supercritical state at depth below 800–1000m,which provides 381the potential for efficient utilization of the space,due to the li-382quid-like density of supercritical CO 2.The point at which CO 2Table 2Performance summary of K-based sorbents capturing CO 2.Material Temperature (°C)CO 2partial pressure (bar)e Total capacity (mmol CO 2/g sorbent)Method f Regenerature temperature (°C)Ref.K 2CO 3/AC a 600.01 1.95TCD g 150[62]K 2CO 3/SiO 2600.010.23TCD g –[62]K 2CO 3/USY 600.010.43TCD g –[62]K 2CO 3/CsNaX 600.01 1.35TCD g –[62]K 2CO 3/Al 2O 3600.01 1.93TCD g 350[62]K 2CO 3/CaO 600.01 1.11TCD g –[62]K 2CO 3/MgO 600.01 2.70TCD g 400[62]K 2CO 3/TiO 2600.01 1.89TCD g 150[62]K 2CO 3/Al 2O 3600.01 1.96TCD g >300[63]Re-KAl(I)30b 600.01 1.86TCD g <200[63]g Fig.5.The schematic diagram of experimental apparatus for the fluidized bed [74,75].6L.L Q1i et al./Fuel xxx (2011)xxx–xxxPlease cite this article in press as:L Q1i L et al.A review of research progress on CO 2capture,storage,and utilization in Chinese Academy of Sciences.Fuel(2011),doi:10.1016/j.fuel.2011.08.022383transforms from critical to supercritical point is 31.1°C and 3847.38MPa [78].CO 2is injected usually in the supercritical form into 385the saline aquifer or depleted oil or gas reservoir.Four major clas-386ses of deep geologic reservoirs present within China have been 387identified and evaluated as candidates for the long-term storage 388of anthropogenic CO 2:deep saline-filled sedimentary (DSFs)for-389mations,depleted gas basins,depleted oil basins with potential 390for CO 2–EOR,and deep unmineable coal seams with potential for 391CO 2–ECBM.Fig.6shows the map of the combined location and ex-392tent of candidate geologic CO 2storage formations in China [13].393Because the CO 2industry is not mature,there are few active CO 2394storage projects which can provide site specific information;hence417China are also potential storage candidates.Recently,other re-418search has also focused on estimating the distance between CO 2419sources and potential sinks.Zheng et al.superimposed the loca-420tions of these 27facilities onto maps of sedimentary basins in each 421of the five regions of China (Huabei,Ordos,Dongbei,Yuwan,and 422Xinjiang).The majority of the candidate CO 2sources are found in 423the Ordos,Huabei and Dongbei regions [85].424The China–UK Near Zero Emissions Coal (NZEC)Initiative exam-425ined options for carbon (CO 2)capture,transport and geological 426storage in China,which was developed under the 2005EU–China 427NZEC Agreement that aims to demonstrate CCS in China and the 428EU [16,86–88].The NZEC Initiative has evaluated the potential to 429430431432433434435436437438439440441442443444445446447448449450451L.L Q1i et al./Fuel xxx (2011)xxx–xxx7Please cite this article in press as:L Q1i L et al.A review of research progress on CO 2capture,storage,and utilization in Chinese Academy of Sciences.Fuel(2011),doi:10.1016/j.fuel.2011.08.022452Kailuan mining area (Hebei Province)and deep saline aquifers in 453the Jiyang Depression (Shandong province)[89,90].The results 454show that the Dagang oilfield is not suitable for large-scale storage,455though could be considered for EOR pilots.The Shengli oilfield was 456considered more promising for storage (472Mt in eight selected 457fields).Storage potential in the Kailuan mining area is 504,000458Mt adsorbed onto the coal and 38,100Mt void storage capacity.459However,the coals have low porosity and permeability that will af-460fect future energy resources [90].The Institute of Geology and Geo-461physics,Chinese Academy of Sciences (IGG–CAS)studied the 462potential for storage in the Jiyang Depression.The results revealed 463that Guantao Formation in the Jiyang Depression has good porosity 464and permeability 465areas was 4662010,in South China 467of Sciences 468storage capacity in 469the Pearl River 470CCS-related 471China [78].There 472saline formations 473tive storage 474including 60Mt in 475large for storaging 476in Guangdong in 477In a word,these 478age of CO 2in deep 479Although this is 480countries,it will 481and there was 482characteristics.483 3.1.2.CO 2–EOR484Although CO 2485oil recovery (EOR)486this process can be 487oil,the cost of CO 2,488the CO 2source [92].489the production of 490be an ideal option 49184commercial or 492tion worldwide [1].493been implemented 494Oil Corporation 495in the Daqing,496ernments of Japan 497out a project to 498plant in China into a 499duced from the 500that between 270501ered by using CO 2502including IGG–CAS 503three large oil fields 504oil reservoirs in the 505were suitable both 506found suitable for 507showed that the 508CO 2storage 509the oil recovery by steam injection has been already applied at Lia-510ohe oil field.Each single well,in average,had conducted 7.6times 511of steam injection-oil recovery processing for EOR propose.The to-512tal recovered oil amounts were 12.06Mt [92].Active oil producing 513fields where CO 2–EOR is technically possible provide credible 514opportunities to initiate CO 2storage demonstration projects.How-515ever,significant further investigations,including detailed site516appraisals would be necessary before such fields can be considered 517as technically and economically suitable for CO 2storage.5183.1.3.CO 2–ECBM519In a similar manner,ECBM recovery can be used to store CO 2520while improving methane recovery.A bright prospect of gas injec-521tion technology for ECBM production has been suggested by Chi-522nese engineers since the late 1990s [94].More recently,a joint 523venture was formed between the China United Coal Bed Methane 524Corporation and the Alberta Research Council of Canada to develop 525a project entitled ‘‘Development of China’s coalbed methane tech-526nology/CO 2sequestration’’[12].This project was initiated in March 527project was performed 528in the anthracitic coals of 529China [95],which is 530in China up to now 531at ICC–CAS in 2005532were investigated based 533An equipment simulated 534middle pressures was 535in coal seam,536behaviors were studied.537coal mine and salt-water 538four coals of various rank 539China were tested for 540one of the most impor-541process.The result 542capacities for methane 543>Bulianta coal >Zhangji 544adsorption isotherms 545lattice model [100].546given to estimate the 547[101],which was 548underground stress is so 5492and CH 4respectively 550the mechanical sta-551of the impact factors of 552stress could be obviously 553of the casing or by using 554and Young’s modulus 555China was also estimated 556prospecting data of coal 557and the replacement ratio 558different ranks,it is esti-559methane resources will 560technology is uti-561in coalbeds is about 562as the total CO 2emission 563also developed 564simulation of the CO 2–565is a lack of knowledge 566due to the complexity 567fluid transport processes.568will be the next 569570571Large amounts of CO 2can also be fixed by a process called min-572eral carbonation,which is natural or artificial fixation of CO 2into 573carbonates.It has been proposed as a promising CO 2sequestration 574technology e.g.the silicate rocks (calcium or magnesium)could be 575turned into carbonates by reacting with CO 2following this mech-576anism [8,105]:577ðMg ;Ca Þx Si y O x þ2y þx CO 2!x ðMg ;Ca ÞCO 3þy SiO 25798L.L Q1i et al./Fuel xxx (2011)xxx–xxxPlease cite this article in press as:L Q1i L et al.A review of research progress on CO 2capture,storage,and utilization in Chinese Academy of Sciences.Fuel(2011),doi:10.1016/j.fuel.2011.08.022580581582583584585586587588589590591592593594595596597598599600601602603604605606607608609610611612613614615616617618619620621622623624625626627628629630631632633634635636637638639hanced by the fact that this method of storage is highly verifiable 640and unquestionably permanent,the grinding energy required to 641produce particles of the size required to react rapidly with the 642acids is large,and the residence times on the order of hours re-643quired to allow carbonation of the solids,via either route,is so long 644that immense reactors would be required,associating environmen-645tal concerns.Furthermore,mineral carbonation will always be646expensive than most applications of geological storage 647important gap in mineral carbonation is the lack of 648onstration plant.649Ocean storage650Captured CO 2also could help reduce the atmospheric 6516526536546556566576586596606616626636646656666676686696706716726736746756766776786796806816826836842685carbonic acid,which would be likely harmful to ocean organisms 686and ecosystems [17].Additionally,it is not known whether the 687public will accept the deliberate storage of CO 2in the ocean as part 688of a climate change mitigation strategy.The development of ocean 689storage technology is generally at a conceptual stage;thus,further 690research and development would be needed to make technologies 691available.3.Reaction mechanism for enhanced carbonation crystallization Q1Please cite this article in press as:L Q1i L et al.A review of research progress on CO 2capture,storage,and utilization in Chinese Academy of Sciences.Fuel(2011),doi:10.1016/j.fuel.2011.08.022692693694695696697698699700701702703704705706707708709710711712713714715716717718719721722723the reaction [131–135],such as in ICC–CAS,Zhao et al.had reported 724a catalyst system composed of KI supported on metal oxides for 725cycloaddition of propylene oxide with CO 2.It was found that the 726activity of KI for cycloaddition was greatly enhanced by ZnO as both 727support and promoter,resulting in a high yield of propylene 728carbonate within a short reaction time.The mechanism is also pro-729posed (Scheme 4)[133].Recently,a large number of catalytic730systems,such as metal oxides,transition metal,ammonium 731well as main group complexes,were reported to be active 732reactions [136–139].In ICC–CAS,the efficient ultrasonic tech-733nique was used for the preparation of amine-functionalized porous 734catalysts for CO 2coupling with epoxide.According to 735study by Zhang and co-workers [140],the reaction conditions 736great influence on the performance and the silanols on the surface 737played an important role in the chemical fixation of CO 2.In addi-738they also proposed the possible reaction mechanism for 739coupling with epoxide over such type of catalysts (Scheme 5).740In recent years,ionic liquids as environmentally benign media 741organic synthesis and catalytic reaction significant progress 7427437447457467477487492750catalyst system without using additional organic solvents was 751achieved in excellent selectivity and TOF (5410h À1)[144].In 752IPE–CAS,an efficient Lewis acid/base catalyst composed of ZnCl 2/753PPh 3C 6H 13Br was developed and showed high activity and selectiv-754ity for the coupling reaction of CO 2and epoxide under the mild 755conditions [145].Sun et al.prepared a series of hydroxyl-function-756alized ionic liquids (HFILs)which showed efficient reactivity andScheme 4.The proposed diagram of reaction mechanism [133].Q1Please cite this article in press as:L Q1i L et al.A review of research progress on CO 2capture,storage,and utilization in Chinese Academy of Sciences.Fuel(2011),doi:10.1016/j.fuel.2011.08.022780781782783784785786787788789790791792793794795796797798799800802803804805806807Please cite this article in press as:L Q1i L et al.A review of research progress on CO 2capture,storage,and utilization in Chinese Academy of Sciences.Fuel(2011),doi:10.1016/j.fuel.2011.08.022CO 2þCH 4¼2CO þ2H 2841842In the past decade,a lot of researches have been devoted to the 843catalytic performance of noble metals,including Pt,Ru,Rh,Pd,844and Ir for this reaction [165–169].It showed that Rh and Ru845exhibited both high activity and stability in CH 4dry reforming,846while Pd,Pt and Ir were less active and prone to deactivation.847Nevertheless,considering the aspects of high cost and limitedPlease cite this article in press as:L Q1i L et al.A review of research progress on CO 2capture,storage,and utilization in Chinese Academy of Sciences.Fuel(2011),doi:10.1016/j.fuel.2011.08.022848availability of noble metals,it is more practical to develop non-849noble metal catalysts which exhibited both high activity and pared with noble metals,Ni-based catalysts have been 851widely investigated because of their high activity and relatively 852low price [170–172].Nevertheless,application of Ni-based cata-853lysts in a large scale process is not so straightforward due to rapid 854carbon deposition,resulting in the deactivation of the catalyst 855[173].It was found that when Ni is supported on a alkaline earth 856metal oxide such as MgO,CaO,and BaO with strong Lewis basi-857city,carbon deposition can be attenuated or even suppressed 858[174]which is because that the support could promote chemi-859sorption of CO 2and thus,accelerated the reaction of CO 2and C 8608618628638648658668678688698708718728738748758768778788798808818828838848858868878888898908918928938948958968974.4.Reaction of CO 2with ethane and propane898Ethylene and propylene are basic raw material in the petrol-899chemical industry.Thermal cracking of hydrocarbons (such as eth-900ane)in the presence of steam is currently the main source of eth-901ylene [181,182].Nevertheless,steam cracking of ethane to 902ethylene is a highly endothermic process that must be performed 903at high temperatures,which means the consumption of a large 904amount of energy.The introduction of CO 2could reduce the extent 905of deep oxidation which results in many byproducts whereas eth-906ylene selectivity drops when oxygen is used as oxidant [183].907Thermodynamics analysis and experimental results have indi-908909910911912913915916917918919920921922923924925926927928929930931932933934935936938939940941L.L Q1i et al./Fuel xxx (2011)xxx–xxx13Please cite this article in press as:L Q1i L et al.A review of research progress on CO 2capture,storage,and utilization in Chinese Academy of Sciences.Fuel(2011),doi:10.1016/j.fuel.2011.08.022969970971972973974975976977978979980981982983984985986987988990991992993994995996997998999100010011002100310041005100610071008100910101011101210131014Please cite this article in press as:L Q1i L et al.A review of research progress on CO 2capture,storage,and utilization in Chinese Academy of Sciences.Fuel(2011),doi:10.1016/j.fuel.2011.08.0221015DMC in supercritical phase was proposed in Scheme 11.Recently,developed a supported Cu-Ni/V 2O 5-SiO 2heterogeneous because the reaction can be carried out in a fixed-bed the side production of water molecules 10341035103610371038103910401041104210431044and theoretical approaches,which enable the development of 1045CO 2selective sorbents.Besides,the sorbent performance,lifetime,10461047104810491050105110521053105410551056105710581059106010611062106310641065Scheme 11.The proposed catalytic reaction mechanism Please cite this article in press as:L Q1i L et al.A review of research progress on CO 2capture,storage,and utilization in Chinese Academy of Sciences.Fuel(2011),doi:10.1016/j.fuel.2011.08.0221066of component costs,specific Chinese market conditions,and other 1067factors impacting costs of deployment in China will be important 1068to consider in greater detail.To propose the storage mechanism,1069monitoring,simulation,risk assessment,control methods as well 1070as engineering design will be studied in future.1071The utilization of CO 2to chemicals has attracted considerable 1072attention as a possible way to manufacture useful commercial 1073chemicals from CO 2in some specific locations (Scheme 12)[222].1074The utilization of CO 2as a raw material in the synthesis of chemi-1075cals was also conducted by CAS,including synthesis of cyclic car-1076bonate from CO 2and epoxide,reaction of CO 2and propylene 1077glycol (PG),CO 2reforming of CH 4,reaction of CO 2and ethane 1078and propane,CO 21079methyl carbonate 1080amount of CO 2can 1081to the order of 1082ent the typical 1083cations is only 1084laminates are used 1085of the materials can 1086and overall net 1087ation.1088and fundamental 1089lue-added chemicals 1090tive net carbon 1091moderate reaction 1092the energy or 1093clear,wind,1094also important to 1095 6.Uncited 1096[201].Q31097Acknowledgments1098This work was 1099vation Programme 1100323);the Ministry of 1101lic of China 1102Climate Change:1103Academy of 1104the 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离子型和非离子型表面活性剂，氧化应激和胆碱酯酶活性的涡虫的影响摘要八广泛使用的表面活性剂（十六烷基三甲基溴化铵CTAB法，氯化苄甲乙氧铵; Hyamine1622，4 - 壬基酚，NP，辛基苯酚乙氧基化物;的Triton X-100，十二烷基苯磺酸钠; LAS，月桂基硫酸钠; SDS，pentadecafluorooctanoic酸，全氟辛酸铵，全氟辛烷磺酸，全氟辛烷磺酸）重新审视自己的急性毒性和氧化应激的影响和胆碱酯酶（CHE）在日本三角涡虫的活动。

8的表面活性剂，以涡虫急性毒性之间的差异是至少在范围3个数量级。

据估计，48小时LC50表面活性剂的毒性等级SDS> NP> LAS> Hyamine1622> CTAB>的Triton X-100>全氟辛烷磺酸PFOA。

根据96小时LC50表面活性剂的毒性排名如下：SDS> CTAB> NP> LAS> Hyamine1622>的Triton X-100>全氟辛烷磺酸PFOA。

有过氧化氢酶的活性显着增加涡虫暴露在LAS名义浓度的0.5或1毫克升？1和1 after48小时暴露在5年或10毫克升的名义浓度的全氟辛烷磺酸。

车活动中发现的抑制作用Hyamine1622涡虫暴露在所有浓度测试，标称浓度为10毫克升？PFOS，PFOA的名义浓度50毫克或100毫克升？和NP标称浓度为0.5 ？1毫克升。

在标称浓度的Triton X-100涡虫暴露在车活动中也观察到显著增加5毫克升1。

暗示的胆碱酯酶抑制NP，PFOS和PFOA在水产动物的神经和行为的影响，需要进一步调查。

介绍-introduction表面活性剂广泛使用在日常生活中的个人护理和家用产品，以及在各种工业应用。

其结果是，大量的表面活性剂通常排出大量污水处理厂或直接向水生环境中有没有污水处理的地方。

事实上，很多表面活性剂及其降解产物已遍布世界各地，在污水排放，污水处理厂的污水，天然水和沉积物（英，2006年）。