An AeroCom initial assessment – optical properties in aerosol component modules of global models

Kinne, Stefan; Schulz, Mıchael; Textor, C.; Guibert, S.; Balkanski, Yves; Bauer, Susanne E.; Berntsen, Terje; Berglen, Tore Flatlandsmo; Boucher, O.; Chin, M.; Collins, William D.; Dentener, Frank; Diehl, Thomas; Easter, Richard C.; Feichter, J.; Fillmore, D.; Ghan, Steven J.; Ginoux, Paul; Gong, Sunling; Grini, Alf; Hendricks, Johannes; Herzog, Michael; Horowitz, Larry W.; Isaksen, I. S. A.; Iversen, Trond; Kirkevåg, Alf; Kloster, Silvia; Koch, D.; Kristjánsson, Jón Egill; Krol, Maarten; Lauer, Axel; Lamarque, J. F.; Lesins, Glen; Liu, X.; Lohmann, Ulrike; Montanaro, V.; Myhre, Gunnar; Penner, J. E.; Pitari, Giovanni; Reddy, S. Paddi; Seland, Øyvind; Stier, Philip; Takemura, Toshihiko; Tie, Xuexi

doi:10.5194/acp-6-1815-2006

Cited by 689 publications

(306 citation statements)

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“…climate-related changes in carbonaceous aerosol concentrations is very limited Kinne et al, 2006;Koch et al, 2009). Important sources of bias could be identified to arise from large uncertainties in the fire emission inventories, improper transport mechanisms and removal processes (Bond et al, 2013;Schwarz et al, 2013).…”

Section: A Veira Et Al: Impact On Transport Black Carbon Concentramentioning

confidence: 99%

Fire emission heights in the climate system – Part 2: Impact on transport, black carbon concentrations and radiation

et al. 2015

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Abstract. Wildfires represent a major source for aerosols impacting atmospheric radiation, atmospheric chemistry and cloud micro-physical properties. Previous case studies indicated that the height of the aerosol-radiation interaction may crucially affect atmospheric radiation, but the sensitivity to emission heights has been examined with only a few models and is still uncertain. In this study we use the general circulation model ECHAM6 extended by the aerosol module HAM2 to investigate the impact of wildfire emission heights on atmospheric long-range transport, black carbon (BC) concentrations and atmospheric radiation. We simulate the wildfire aerosol release using either various versions of a semiempirical plume height parametrization or prescribed standard emission heights in ECHAM6-HAM2. Extreme scenarios of near-surface or free-tropospheric-only injections provide lower and upper constraints on the emission height climate impact. We find relative changes in mean global atmospheric BC burden of up to 7.9 ± 4.4 % caused by average changes in emission heights of 1.5-3.5 km. Regionally, changes in BC burden exceed 30-40 % in the major biomass burning regions. The model evaluation of aerosol optical thickness (AOT) against Moderate Resolution Imaging Spectroradiometer (MODIS), AErosol RObotic NETwork (AERONET) and Cloud-Aerosol Lidar with Orthogonal Polarization (CALIOP) observations indicates that the implementation of a plume height parametrization slightly reduces the ECHAM6-HAM2 biases regionally, but on the global scale these improvements in model performance are small. For prescribed emission release at the surface, wildfire emissions entail a total sky top-of-atmosphere (TOA) radiative forcing (RF) of −0.16 ± 0.06 W m −2 . The application of a plume height parametrization which agrees reasonably well with observations introduces a slightly stronger negative TOA RF of −0.20 ± 0.07 W m −2 . The standard ECHAM6-HAM2 model in which 25 % of the wildfire emissions are injected into the free troposphere (FT) and 75 % into the planetary boundary layer (PBL), leads to a TOA RF of −0.24 ± 0.06 W m −2 . Overall, we conclude that simple plume height parametrizations provide sufficient representations of emission heights for global climate modeling. Significant improvements in aerosol wildfire modeling likely depend on better emission inventories and aerosol process modeling rather than on improved emission height parametrizations.

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Section: A Veira Et Al: Impact On Transport Black Carbon Concentramentioning

confidence: 99%

Fire emission heights in the climate system – Part 2: Impact on transport, black carbon concentrations and radiation

et al. 2015

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“…The original motivation behind the development of the Dark Target algorithms was to provide the necessary information to quantify aerosol effect on climate and climate processes, and thereby narrow uncertainties in estimating climate change Tanré et al, 1997). Indeed in the following dozen years since Terra launch, the scientific literature abounds in references to MODIS aerosol products to estimate direct aerosol effects Yu et al, 2006) including the anthropogenic portion (Kaufman et al, 2005a;Christopher et al, 2006), to constrain climate models in their efforts to simulate climate processes (Stier et al, 2005;Kinne et al, 2006), to estimate intercontinental transport of aerosol (Kaufman et al, 2005b;Yu et al, 2012) and to further our understanding of aerosol-cloud-precipitation processes (Kaufman et al, 2005c;Koren et al, 2005;Koren and Wang, 2008;Loeb and Schuster, 2008).…”

Section: Introductionmentioning

confidence: 99%

MODIS 3 km aerosol product: algorithm and global perspective

et al. 2013

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After more than a decade of producing a nominal 10 km aerosol product based on the dark target method, the MODerate resolution Imaging Spectroradiometer (MODIS) aerosol team will be releasing a nominal 3 km product as part of their Collection 6 release. The new product differs from the original 10 km product only in the manner in which reflectance pixels are ingested, organized and selected by the aerosol algorithm. Overall, the 3 km product closely mirrors the 10 km product. However, the finer resolution product is able to retrieve over the ocean closer to islands and coastlines, and is better able to resolve fine aerosol features such as smoke plumes over both ocean and land. In some situations, it provides retrievals over entire regions that the 10 km product barely samples. In situations traditionally difficult for the dark target algorithm such as over bright or urban surfaces, the 3 km product introduces isolated spikes of artificially high aerosol optical depth (AOD) that the 10 km algorithm avoids. Over land, globally, the 3 km product appears to be 0.01 to 0.02 higher than the 10 km product, while over ocean, the 3 km algorithm is retrieving a proportionally greater number of very low aerosol loading situations. Based on collocations with ground-based observations for only six months, expected errors associated with the 3 km land product are determined to be greater than that of the 10 km product: ± 0.05 ± 0.20 AOD. Over ocean, the suggestion is for expected errors to be the same as the 10 km product: ± 0.03 ± 0.05 AOD, but slightly less accurate in the coastal zone. The advantage of the product is on the local scale, which will require continued evaluation not addressed here. Nevertheless, the new 3 km product is expected to provide important information complementary to existing satellite-derived products and become an important tool for the aerosol community

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“…The magnitude of this radiative forcing depends on the light scattering and absorption properties of the particles, which vary with factors such as size, composition, and physical state (Kinne et al 2006). On a global basis sulfate is the largest anthropogenic contribution to the mass budget of atmospheric particles and consequently constitutes a significant cooling term to Earth's radiative energy balance (Solomon et al 2007).…”

Section: Introductionmentioning

confidence: 99%

The 1-by-3 Tandem Differential Mobility Analyzer for Measurement of the Irreversibility of the Hygroscopic Growth Factor

Rosenoern¹,

Paulsen²,

Martin³

2009

Aerosol Science and Technology

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A new instrument, namely the 1 × 3 tandem differential mobility analyzer (1 × 3-TDMA), has been developed. Its primary measurement is the irreversibility of the hygroscopic growth factor of aerosol particles. The instrument uses the hysteresis of phase transitions to infer the solid or aqueous state of the particles. A first DMA passes particles of a selected electric mobility at relative humidity RH 0 . Exiting this DMA, the particles are split into three separate flows. The first flow is exposed to RH 0 → (RH 0 + δ) → RH 0 in a deliquescence test before passing through a second DMA that is set to the same electric mobility as the first DMA. The second flow passes directly to a third DMA without change in RH, thereby serving as a reference arm. This DMA is also set to the same electric mobility as the first DMA. The transmission ratio of the 1 × 3-TDMA is defined as the particle concentration passing the deliquescence test divided by that passing through the reference arm. The transmission ratio is unity in the absence of deliquescence and zero when a phase transition occurs, at least for ideal instrument performance in application to a test aerosol of fully deliquesceable particles. For the third flow passing out of the first DMA, an efflorescence test is run by using the RH profile of RH 0 → (RH 0 − δ) → RH 0 before passing through a fourth DMA. A full data set for the 1 × 3-TDMA is obtained by scanning RH 0 , typically from 20 to 85%. In the present paper, the 1 × 3-TDMA instrument is described, and laboratory data are presented for the phase transitions of externally mixed aerosols of aqueous and solid sodium chloride particles, aqueous and solid ammonium sulfate particles, and their mixtures, as well as a mixture of aqueous and solid sea salt particles. The observed transmission ratio is compared to a model analysis. The intent behind the development of this instrument is to deploy it for field measurements and use observations of

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An AeroCom initial assessment – optical properties in aerosol component modules of global models

Cited by 689 publications

References 4 publications

Fire emission heights in the climate system – Part 2: Impact on transport, black carbon concentrations and radiation

Fire emission heights in the climate system – Part 2: Impact on transport, black carbon concentrations and radiation

MODIS 3 km aerosol product: algorithm and global perspective

The 1-by-3 Tandem Differential Mobility Analyzer for Measurement of the Irreversibility of the Hygroscopic Growth Factor

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