Global distribution and climate forcing of carbonaceous aerosols

Chung, S. H.; Seinfeld, John H.

doi:10.1029/2001jd001397

Cited by 762 publications

(946 citation statements)

References 141 publications

(212 reference statements)

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“…Dust is treated as insoluble, whereas black carbon (BC) and particulate organic matter (POM) appear both in the soluble or insoluble fractions. The aging of primary insoluble carbonaceous particles transfers insoluble aerosol number and mass to soluble with a half-life of 1.1 days (Cooke and Wilson 1996;Chung and Seinfeld 2002). The uptake and loss of water from aerosol particles is generally fast and depends on the chemical composition, size and surface properties of the aerosol particle.…”

Section: Methodology and Modelsmentioning

confidence: 99%

Aerosol and ozone changes as forcing for climate evolution between 1850 and 2100

et al. 2012

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Global aerosol and ozone distributions and their associated radiative forcings were simulated between 1850 and 2100 following a recent historical emission dataset and under the representative concentration pathways (RCP) for the future. These simulations were used in an Earth System Model to account for the changes in both radiatively and chemically active compounds, when simulating the climate evolution. The past negative stratospheric ozone trends result in a negative climate forcing culminating at -0.15 W m -2 in the 1990s. In the meantime, the tropospheric ozone burden increase generates a positive climate forcing peaking at 0.41 W m -2 . The future evolution of ozone strongly depends on the RCP scenario considered. In RCP4.5 and RCP6.0, the evolution of both stratospheric and tropospheric ozone generate relatively weak radiative forcing changes until 2060-2070 followed by a relative 30 % decrease in radiative forcing by 2100. In contrast, RCP8.5 and RCP2.6 model projections exhibit strongly different ozone radiative forcing trajectories. In the RCP2.6 scenario, both effects (stratospheric ozone, a negative forcing, and tropospheric ozone, a positive forcing) decline towards 1950s values while they both get stronger in the RCP8.5 scenario. Over the twentieth century, the evolution of the total aerosol burden is characterized by a strong increase after World War II until the middle of the 1980s followed by a stabilization during the last decade due to the strong decrease in sulfates in OECD countries since the 1970s. The cooling effects reach their maximal values in 1980, with -0.34 and -0.28 W m -2 respectively for direct and indirect total radiative forcings. According to the RCP scenarios, the aerosol content, after peaking around 2010, is projected to decline strongly and monotonically during the twenty-first century for the RCP8.5, 4.5 and 2.6 scenarios. While for RCP6.0 the decline occurs later, after peaking around 2050. As a consequence the relative importance of the total cooling effect of aerosols becomes weaker throughout the twenty-first century compared with the positive forcing of greenhouse gases. Nevertheless, both surface ozone and aerosol content show very different regional features depending on the future scenario considered. Hence, in 2050, surface ozone changes vary between -12 and ?12 ppbv over Asia depending on the RCP projection, whereas the regional direct aerosol radiative forcing can locally exceed -3 W m -2 . This paper is a contribution to the special issue on the IPSL and CNRM global climate and Earth System Models, both developed in France and contributing to the 5th coupled model intercomparison project.Electronic supplementary material The online version of this article

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Section: Methodology and Modelsmentioning

confidence: 99%

Aerosol and ozone changes as forcing for climate evolution between 1850 and 2100

et al. 2012

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“…8 shows natural and background concentrations for OC (concentrations of EC are much lower and relatively unimportant for visibility degradation). Two limiting cases are shown: (1) a low limit where production of biogenic SOA is reduced following Chung and Seinfeld (2002) due to reduced supply of primary anthropogenic OC aerosols; (2) a high limit where biogenic SOA is the same as in the standard baseline calculation, i.e., assuming that SOA formation is not limited by the supply of preexisting aerosol. The difference between the two limits is large, illustrating the current uncertainty regarding the sensitivity of biogenic SOA formation to anthropogenic emissions.…”

Section: Background Aerosol Concentrations In the Usamentioning

confidence: 99%

“…7 but for organic carbon (OC) natural and background concentrations. The low limit accounts for reduction in biogenic SOA following Chung and Seinfeld (2002) due to a lower concentration of primary OC aerosol on which this biogenic SOA can condense. The high limit includes biogenic SOA from the standard baseline simulation, assuming that condensation of this SOA is not limited by the supply of preexisting aerosol.…”

Section: Variability In Natural and Background Visibilitymentioning

confidence: 99%

“…SOA formation now follows the scheme of Chung and Seinfeld (2002), which involves oxidation of several classes of biogenic hydrocarbons and gas-aerosol partitioning of the semi-volatile products as a function of local temperature and pre-existing OC mass concentration. The reaction probability (g N2O5 ) for N 2 O 5 uptake and hydrolysis in aerosols is now as described by Evans and Jacob (2005) as a function of local aerosol composition, temperature, and RH.…”

Section: Model Descriptionmentioning

confidence: 99%

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Regional visibility statistics in the United States: Natural and transboundary pollution influences, and implications for the Regional Haze Rule

Park

Jacob

Kumar

et al. 2006

Atmospheric Environment

224

186

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The Regional Haze Rule of the US Environmental Protection Agency mandates reduction in US anthropogenic emissions to achieve linear improvement of visibility in wilderness areas over the 2004-18 period toward an endpoint of natural visibility conditions by 2064. Linear improvement is to apply to the mean visibility degradation on the statistically 20% worst days, measured as a Haze Index in units of deciviews (log of aerosol extinction). We use a global chemical transport model (GEOS-Chem) with 11 Â 11 horizontal resolution to simulate present-day visibility statistics in the USA, compare them to observations from the Interagency Monitoring of Protected Visual Environments (IMPROVE) surface network, and provide natural and background visibility statistics for application of the Regional Haze Rule. Background is defined by suppression of US anthropogenic emissions but allowance for present-day foreign emissions and associated import of pollution. Our model is highly successful at reproducing the observed variability of visibility statistics for present-day conditions, including the low tail of the frequency distribution that is most representative of natural or background conditions. We find considerable spatial and temporal variability in natural visibility over the USA, especially due to fires in the west. A major uncertainty in estimating natural visibility is the sensitivity of biogenic organic aerosol formation to the availability of preexisting anthropogenic aerosol. Background visibility is more variable than natural visibility and the 20% worst days show large contributions from Canadian and Mexican pollution. Asian pollution, while degrading mean background visibility, is relatively less important on the worst days. Recognizing the influence of uncontrollable transboundary pollution in the Regional Haze Rule would substantially decrease the schedule of emission reductions required in the 2004-18 implementation phase. Meaningful application of the Rule in the future will require projections of future trends in foreign anthropogenic emissions, wildfire frequency, and climate variables. r

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“…Largescale conversion of tropical rainforest into oil palm plantations in areas of high (or projected to increase) NO x emissions of SE Asia therefore has the potential to be detrimental for local O 3 levels (Hewitt et al, 2009). At the same time will an increase in agricultural versus forest area also affect emissions of oxygenated BVOC (methanol, acetaldehyde; Chung et al, 2002;Goto et al, 2008). The effect this may have on regional chemistry and climate is unknown as for these the oxygenated biogenics regional emission patterns and chief source areas are unknown and their atmospheric reaction pathways are incompletely understood (Kwan et al, 2006;Guimbaud et al, 2007;Heiden et al, 2003).…”

Section: Biological Emission Of Reactive Carbon and Nitrogenmentioning

confidence: 99%

Regionalizing global climate models

Pitman

Arneth

Ganzeveld

2011

Intl Journal of Climatology

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Global climate models simulate the Earth's climate impressively at scales of continents and greater. At these scales, large-scale dynamics and physics largely define the climate. At spatial scales relevant to policy makers, and to impacts and adaptation, many other processes may affect regional and local climate and perhaps trigger teleconnections that provide significant feedbacks on the global climate. These processes include fire, irrigation, land cover change (including crops and urban landscapes), and the emissions of biogenic volatile organic compounds by vegetation. Many of these interact within the atmosphere via dynamical, physical, and chemical mechanisms that lead to boundary-layer feedbacks. It is unlikely that any of these processes have a significant global-scale impact on the Earth's climate in the sense that the amount of warming due to a doubling of well mixed greenhouse gases would change if these processes were explicitly represented in climate models. These phenomena are usually local in space (e.g. urban) or in time (e.g. fire) and probably do not provide the on-going and sustained forcing to affect the global climate. However, for most impacts and adaptation research it is the regional and local climate that defines climate risk. At these scales, processes missing in climate models can have a substantially larger local-scale impact than the additional radiative forcing due to increasing greenhouse gases. Thus, while climate models are well designed for global and continental scales they exclude a suite of important processes that are locally and/or regionally important. We review these missing processes and highlight the research required to resolve the representation of these regional-scale processes in climate models. We also discuss the experimental methodology required to rigorously determine whether these processes are restricted to a local or regional-scale role or whether they do trigger robust teleconnections that would demonstrate global-scale significance.

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Global distribution and climate forcing of carbonaceous aerosols

Cited by 762 publications

References 141 publications

Aerosol and ozone changes as forcing for climate evolution between 1850 and 2100

Aerosol and ozone changes as forcing for climate evolution between 1850 and 2100

Regional visibility statistics in the United States: Natural and transboundary pollution influences, and implications for the Regional Haze Rule

Regionalizing global climate models

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