Emissions of primary aerosol and precursor gases in the years 2000 and 1750 prescribed data-sets for AeroCom

Dentener, Frank; Kinne, Stefan; Bond, Tami C.; Boucher, O.; Cofała, J.; Generoso, S.; Ginoux, Paul; Gong, Sunling; Hoelzemann, Judith J.; Ito, Akinori; Marelli, L.; Penner, Joyce E.; Putaud, J. P.; Textor, C.; Schulz, Mıchael; Werf, Guido R. van der; Wilson, J.

doi:10.5194/acp-6-4321-2006

Cited by 964 publications

(1,089 citation statements)

References 42 publications

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“…The size and radiative parameters for dust are the same as used by Krinner et al (2006), following Guelle et al (2000) and Balkanski et al (2007). Black carbon is assumed to follow a log-normal size distribution with a median number radius of 11.8 nm, characteristic of freshly emitted soot (Dentener et al, 2006;Jacobson et al, 2004). In the real world, this diameter increases quickly, as BC undergoes ageing and coagulation and can be coated by other aerosols in the atmosphere.…”

Section: Model Descriptionmentioning

confidence: 99%

Boreal and temperate snow cover variations induced by black carbon emissions in the middle of the 21st century

et al. 2013

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Abstract. We used a coupled climate-chemistry model to quantify the impacts of aerosols on snow cover north of 30 • N both for the present-day and for the middle of the 21st century. Black carbon (BC) deposition over continents induces a reduction in the mean number of days with snow at the surface (MNDWS) that ranges from 0 to 10 days over large areas of Eurasia and Northern America for the presentday relative to the pre-industrial period. This is mainly due to BC deposition during the spring, a period of the year when the remaining of snow accumulated during the winter is exposed to both strong solar radiation and a large amount of aerosol deposition induced themselves by a high level of transport of particles from polluted areas. North of 30 • N, this deposition flux represents 222 Gg BC month −1 on average from April to June in our simulation. A large reduction in BC emissions is expected in the future in all of the Representative Concentration Pathway (RCP) scenarios. In particular, considering the RCP8.5 in our simulation leads to a decrease in the spring BC deposition down to 110 Gg month −1 in the 2050s. However, despite the reduction of the aerosol impact on snow, the MNDWS is strongly reduced by 2050, with a decrease ranging from 10 to 100 days from presentday values over large parts of the Northern Hemisphere. This reduction is essentially due to temperature increase, which is quite strong in the RCP8.5 scenario in the absence of climate mitigation policies. Moreover, the projected sea-ice retreat in the next decades will open new routes for shipping in the Arctic. However, a large increase in shipping emissions in the Arctic by the mid-21st century does not lead to significant changes of BC deposition over snow-covered areas in our simulation. Therefore, the MNDWS is clearly not affected through snow darkening effects associated with these Arctic ship emissions. In an experiment without nudging toward atmospheric reanalyses, we simulated however some changes of the MNDWS considering such aerosol ship emissions. These changes are generally not statistically significant in boreal continents, except in Quebec and in the West Siberian plains, where they range between −5 and −10 days. They are induced both by radiative forcings of the aerosols when they are in the snow and in the atmosphere, and by all the atmospheric feedbacks. These experiments do not take into account the feedbacks induced by the interactions between ocean and atmosphere as they were conducted with prescribed sea surface temperatures. Climate change by the mid-21st century could also cause biomass burning activity (forest fires) to become more intense and occur earlier in the season. In an idealised scenario in which forest fires are 50 % stronger and occur 2 weeks earlier and later than at present, we simulated an increase in spring BC deposition of 21 Gg BC month −1 over continents located north of 30 • N. This BC deposition does not impact directly the snow cover through snow darkening effects. However, in an experiment considering ...

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Section: Model Descriptionmentioning

confidence: 99%

Boreal and temperate snow cover variations induced by black carbon emissions in the middle of the 21st century

et al. 2013

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“…Anthropogenic emissions are obtained from the Reanalysis of the TROpospheric (RETRO) chemical composition inventories (http://retro.enes.org/index.shtml). Biomass burning emissions are obtained from the Global Fire Emissions Database, Version 2 (GFEDv2.1) with 8-day temporal resolution (Randerson et al, 2005) and vertically distributed following the injection heights suggested by Dentener et al (2006) for the Aerosol InterComparison project (AeroCom), because of insufficient information to perform plume rise calculations over West Africa.…”

Section: Model Descriptionmentioning

confidence: 99%

Radiative impact of mineral dust on monsoon precipitation variability over West Africa

et al. 2011

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Abstract. The radiative forcing of dust and its impact on precipitation over the West Africa monsoon (WAM) region is simulated using a coupled meteorology and aerosol/chemistry model (WRF-Chem). During the monsoon season, dust is a dominant contributor to aerosol optical depth (AOD) over West Africa. In the control simulation, on 24-h domain average, dust has a cooling effect (−6.11 W m −2 ) at the surface, a warming effect (6.94 W m −2 ) in the atmosphere, and a relatively small TOA forcing (0.83 W m −2 ). Dust modifies the surface energy budget and atmospheric diabatic heating. As a result, atmospheric stability is increased in the daytime and reduced in the nighttime, leading to a reduction of late afternoon precipitation by up to 0.14 mm/h (25%) and an increase of nocturnal and early morning precipitation by up to 0.04 mm/h (45%) over the WAM region. Dust-induced reduction of diurnal precipitation variation improves the simulated diurnal cycle of precipitation when compared to measurements. However, daily precipitation is only changed by a relatively small amount (−0.17 mm/day or −4%). The dust-induced change of WAM precipitation is not sensitive to interannual monsoon variability. On the other hand, sensitivity simulations with weaker to stronger absorbing dust (in order to represent the uncertainty in dust solar absorptivity) show that, at the lower atmosphere, dust longwave warming effect in the nighttime surpasses its shortwave cooling effect in the daytime; this leads to a less stable atmosphere associated with more convective precipitation in the nighttime. As a result, the dust-induced change of daily WAM precipitation varies from a significant reduction of −0.52 mm/day (−12%, weaker absorbing dust) to a small increase of 0.03 mm/day (1%, stronger absorbing dust). This variation originates from the competition between dust impact on daytime and nightCorrespondence to: C. Zhao (chun.zhao@pnl.gov) time precipitation, which depends on dust shortwave absorption. Dust reduces the diurnal variation of precipitation regardless of its absorptivity, but more reduction is associated with stronger absorbing dust.

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“…For example, in the atmospheric (bulk) sulfur model intercomparison study COSAM (Comparison of large-scale sulfur models; 1999), simulated wet deposition efficiencies for Europe range between 0.1 and 0.5 day −1 , and they are associated with sulfate lifetimes between 6 and 1 days, respectively (Roelofs et al, 2001). A more recent intercomparison study with relatively sophisticated aerosol models, carried out in the framework of the aerosol intercomparison initiative AeroCom, reported a similar behavior with global wet removal efficiencies between 0.15 and 0.3 day −1 for sulfate and global sulfate lifetimes between 3 and 0.5 days (Textor et al, 2006;their Figs. 5d and 4a).…”

Section: Introductionmentioning

confidence: 57%

“…Roelofs: Temperature responses of water vapor and aerosol lifetimes physical and chemical processes, and aerosol removal lead to differences in simulated aerosol burdens and lifetimes. Wet deposition of aerosol, which is subject of this study, is an important removal process for soluble inorganic aerosol species such as sulfate and nitrate, which have a strong anthropogenic signature (Charlson et al, 1992;Dentener et al, 2006). For example, Croft et al (2010) calculate that 53 % and 43 % of global sulfate are removed by stratiform and convective precipitation, respectively, while 4 % is removed by dry deposition.…”

Section: Introductionmentioning

confidence: 99%

“…Topics addressed in recent studies are, for example, the quantification of emissions of aerosol and aerosol precursors (e.g., Dentener et al, 2006), the secondary formation of organic and inorganic aerosol in the atmosphere (e.g., Jacobson et al, 2000;Jimenez et al, 2009), the capability of aerosol to act as cloud condensation nuclei and their influence on precipitation formation (e.g., Dusek et al, 2006;Rosenfeld et al, 2008), and the influence of the volatility of (in)organic species on cloud formation (e.g., Donahue et al, 2011;Topping and McFiggans, 2012).…”

Section: Introductionmentioning

confidence: 99%

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A steady-state analysis of the temperature responses of water vapor and aerosol lifetimes

Roelofs

2013

Atmos. Chem. Phys.

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The dominant removal mechanism of soluble aerosol is wet deposition. The atmospheric lifetime of aerosol, relevant for aerosol radiative forcing, is therefore coupled to the atmospheric cycling time of water vapor. This study investigates the coupling between water vapor and aerosol lifetimes in a well-mixed atmosphere. Based on a steady-state study by Pruppacher and Jaenicke (1995) we describe the coupling in terms of the processing efficiency of air by clouds and the efficiencies of water vapor condensation, of aerosol activation, and of the transfer from cloud water to precipitation. We extend this to expressions for the temperature responses of the water vapor and aerosol lifetimes. Previous climate model results (Held and Soden, 2006) suggest a water vapor lifetime temperature response of +5.3 ± 2.0% K⁻¹. This can be used as a first guess for the aerosol lifetime temperature response, but temperature sensitivities of the aerosol lifetime simulated in recent aerosol–climate model studies extend beyond this range and include negative values. This indicates that other influences probably have a larger impact on the computed aerosol lifetime than its temperature response, more specifically changes in the spatial distributions of aerosol (precursor) emissions and precipitation patterns, and changes in the activation efficiency of aerosol. These are not quantitatively evaluated in this study but we present suggestions for model experiments that may help to understand and quantify the different factors that determine the aerosol atmospheric lifetime

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Emissions of primary aerosol and precursor gases in the years 2000 and 1750 prescribed data-sets for AeroCom

Cited by 964 publications

References 42 publications

Boreal and temperate snow cover variations induced by black carbon emissions in the middle of the 21st century

Boreal and temperate snow cover variations induced by black carbon emissions in the middle of the 21st century

Radiative impact of mineral dust on monsoon precipitation variability over West Africa

A steady-state analysis of the temperature responses of water vapor and aerosol lifetimes

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