Interactive chemistry in the Laboratoire de Météorologie Dynamique general circulation model: Description and background tropospheric chemistry evaluation

Hauglustaine, Didier; Hourdin, F.; Jourdain, L.; Filiberti, Marie-Angèle; Walters, Stacy; Lamarque, Jean‐François; Holland, Elisabeth A.

doi:10.1029/2003jd003957

Cited by 420 publications

(446 citation statements)

References 176 publications

(255 reference statements)

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“…Together, these three models form the LMDz-OR-INCA model. Fundamentals for the gas phase chemistry are presented in Hauglustaine et al (2004) and first results with the full tropospheric gaseous chemical scheme are gathered by Folberth et al (2006). The oxidative tropospheric photochemistry is described through 85 chemical species and 264 chemical reactions, including non-methane hydrocarbon oxidation.…”

Section: Methodology and Modelsmentioning

confidence: 99%

“…Natural emissions of dust and sea salt are computed using the 10 m wind components from the ECMWF reanalysis for 2006 and, consequently, have seasonal cycles, but no interannual variability. As described in Hauglustaine et al (2004), the stratospheric ozone concentrations are relaxed toward observations at the altitudes having potential temperatures above 380 K. The ozone observations are taken from the monthly mean 3D climatologies of Li and Shine (1995), based on ozone soundings and different satellite data.…”

Section: Lmdz-or-inca Set-upmentioning

confidence: 99%

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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%

Section: Lmdz-or-inca Set-upmentioning

confidence: 99%

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

et al. 2012

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“…Finally, the ORCHIDEE land surface model serves as the land surface boundary condition for LMDZ and describes exchanges of energy and water between the atmosphere, the soil and the biosphere , including a dynamic snow module. The coupling between LMDz and ORCHIDEE is described by Hourdin et al (2006), and those between LMDz and INCA is detailed by Hauglustaine et al (2004) for chemistry and tracers and by Balkanski et al (2007Balkanski et al ( , 2010 and Déandreis et al (2012) for the computation of the aerosols radiative forcings.…”

Section: Model Descriptionmentioning

confidence: 99%

“…This model consists of three coupled modules: the LMDZ general circulation model represents the atmospheric component . INCA (interactions between chemistry and aerosols) describes gas-and aqueous-phase chemistry (Hauglustaine et al, 2004;Boucher et al, 2002), as well as aerosol physical properties such as size and hygroscopicity (Balkanski et al, 2010), which control the amount of wet and dry deposition. The coupling between the LMDZ and INCA models allow for an interactive simulation of five aerosol chemical species, namely sulphate, BC, OC, sea salt and dust.…”

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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“…Chemical boundary conditions for this domain were provided by the global climate chemistry model LMDz-INCA2 (Hauglustaine et al, 2004;Folberth et al, 2006). A detailed evaluation of the European simulation was recently presented in the companion paper by Pay et al (2010).…”

Section: System Descriptionmentioning

confidence: 99%

An annual assessment of air quality with the CALIOPE modeling system over Spain

Baldasano

Pay

Jorba

et al. 2011

Science of The Total Environment

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The CALIOPE project, funded by the Spanish Ministry of the Environment, aims at establishing an air quality forecasting system for Spain. With this goal, CALIOPE modeling system was developed and applied with high resolution (4 km x 4 km, 1hr) using the HERMES emission model (including emissions of resuspended particles from paved roads) specifically built up for Spain. The present study provides an evaluation and an assessment of that air quality modeling system, namely WRF-ARW/HERMES/CMAQ/BSC-DREAM8b for a full year simulation in 2004 over Spain. The evaluation focused on the capability of the model to reproduce the temporal and spatial distribution of gas phase species (NO2, O3, and SO2) and particulate matter (PM10) against ground-based measurements from the Spanish air quality monitoring network. The evaluation of the modeling results on an hourly basis showed a strong dependency of the performance of the model on the type of zone (urban, suburban and rural) and the dominant emission sources (traffic, industrial, and background). The O3 chemistry is best represented in summer, when mean hourly variability and high peaks are generally well reproduced. The mean normalized error and bias meet the recommendations proposed by the United States Environmental Protection Agency (US-EPA) and the European regulations. Modeled O3 shows higher performance for urban than for rural stations, especially at traffic stations in large cities, since stations influenced by traffic emissions (i.e. high NOx emissions) are better characterized with a more pronounced daily variability. NOx/O3 chemistry is better represented under non-limited-NO2 regimes. SO 2 is mainly produced from isolated point sources (power generation and transformation industries) which generate large plumes of high SO 2 concentration affecting the air quality on a local to national scale where the meteorological pattern is crucial. The contribution of mineral dust from the Sahara desert through the BSC-DREAM8b model helps to satisfactorily reproduce episodic high PM10 concentration peaks at background stations. The model assessment indicates that one of the main air quality-related problems in Spain is the high level of O3. A quarter of the Iberian Peninsula presents more than 30 days exceeding the value 120 µg m -3 for the maximum 8-hr O3 concentration as a consequence of the transport of O3 precursors downwind the Madrid and Barcelona metropolitan areas, and industrial areas and cities in the Mediterranean coast.

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Interactive chemistry in the Laboratoire de Météorologie Dynamique general circulation model: Description and background tropospheric chemistry evaluation

Cited by 420 publications

References 176 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

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

An annual assessment of air quality with the CALIOPE modeling system over Spain

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