# Combining POLDER-3 satellite observations and WRF-Chem numerical simulations to derive biomass burning aerosol properties over the southeast Atlantic region

Alexandre Siméon, Fabien Waquet, Jean-Christophe Péré, Fabrice Ducos, François Thieuleux, Fanny Peers, Solène Turquety, Isabelle Chiapello

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## To cite this version:

Alexandre Siméon, Fabien Waquet, Jean-Christophe Péré, Fabrice Ducos, François Thieuleux, et al. Combining POLDER-3 satellite observations and WRF-Chem numerical simulations to derive biomass burning aerosol properties over the southeast Atlantic region. Atmospheric Chemistry and Physics, 2021, 21, pp.17775-17805. 10.5194/acp-21-17775-2021. insu-03686308

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# Combining POLDER-3 satellite observations and WRF-Chem numerical simulations to derive biomass burning aerosol properties over the southeast Atlantic region

Alexandre Siméon<fnref n="1" />, Fabien Waquet<fnref n="1" />, Jean-Christophe Péré<fnref n="1" />, Fabrice Ducos<fnref n="1" />, François Thieuleux<fnref n="1" />, Fanny Peers<fnref n="1" />, Solène Turquety<fnref n="2" />, and Isabelle Chiapello<fnref n="1" />

**Correspondence:** Alexandre Siméon (alexandre.simeon@univ-lille.fr) and Fabien Waquet (fabien.waquet@univ-lille.fr)

Received: 25 March 2021 – Discussion started: 6 April 2021

Revised: 5 October 2021 – Accepted: 6 October 2021 – Published: 6 December 2021

**Abstract.** Aerosol absorption is a key property to assess the radiative impacts of aerosols on climate at both global and regional scales. The aerosol physico-chemical and optical properties remain not sufficiently constrained in climate models, with difficulties to properly represent both the aerosol load and their absorption properties in clear and cloudy scenes, especially for absorbing biomass burning aerosols (BBA). In this study we focus on biomass burning (BB) particle plumes transported above clouds over the southeast Atlantic (SEA) region off the southwest coast of Africa, in order to improve the representation of their physico-chemical and absorption properties. The methodology is based on aerosol regional numerical simulations from the WRF-Chem coupled meteorology–chemistry model combined with a detailed inventory of BB emissions and various sets of innovative aerosol remote sensing observations, both in clear and cloudy skies from the POLDER-3/PARASOL space sensor. Current literature indicates that some organic aerosol compounds (OC), called brown carbon (BrOC), primarily emitted by biomass combustion absorb the ultraviolet-blue radiation more efficiently than pure black carbon (BC). We exploit this specificity by comparing the spectral dependence of the aerosol single scattering albedo (SSA) derived from the POLDER-3 satellite observations in the 443–1020 nm wavelength range with the SSA simulated for different proportions of BC, OC and BrOC at the source level, considering the homogeneous internal mixing state of particles. These numerical simulation experiments are based on two main constraints: maintaining a realistic aerosol optical depth both in clear and above cloudy scenes and a realistic BC/OC mass ratio. Modelling experiments are presented and discussed to link the chemical composition with the absorption properties of BBA and to provide estimates of the relative proportions of black, organic and brown carbon in the African BBA plumes transported over the SEA region for July 2008. The absorbing fraction of organic aerosols in the BBA plumes, i.e. BrOC, is estimated at 2% to 3%. The simulated mean SSA are 0.81 (565 nm) and 0.84 (550 nm) in clear and above cloudy scenes respectively, in good agreement with those retrieved by POLDER-3 (0.85 ± 0.05 at 565 nm in clear sky and at 550 nm above clouds) for the studied period.

## 1 Introduction

The SEA region which includes the southeastern Atlantic Ocean (SEAO) and the western and southern parts of Africa is an excellent natural laboratory to better understand the complexity of aerosol–cloud interactions (Keil and Haywood, 2003; Stier et al., 2013; Peers et al., 2016; Zuidema et al., 2016a, b). Africa accounts for about half of the global annual carbon emissions produced by BB (Giglio et al., 2003; Giglio, 2006; Reid et al., 2009; Giglio and Randerson, 2010; Werf et al., 2010). These BB emissions, mostly large scale and man-made (e.g. deforestation, agricultural, domes-

<footnote n="1">¹Université de Lille, CNRS, UMR 8518, LOA – Laboratoire d'Optique Atmosphérique, 59000 Lille, France</footnote>

<footnote n="2">²LMD/IPSL, Sorbonne Université, ENS, PSL Université, École Polytechnique, Institut Polytechnique de Paris, CNRS, Paris, France</footnote>
tic practices), are frequent and occur every year mainly dur-
ing the dry season from June to October in central, eastern
and southern Africa (Roberts et al., 2009). BBA are then
regularly emitted from these source areas and transported
over the SEAO above one of the three largest persistent stra-
tocumulus layers on the planet (Knippertz et al., 2017). This
westward aerosol transport is favoured by prevailing easter-
lies winds at 850 and 700 hPa (Zuidema et al., 2018b).

The presence of absorbing aerosols (AA) above clouds de-
creases the amount of light reflected by clouds into space,
thus causing a reduction of the planet’s albedo and a positive
regional radiative forcing (warming). Significant positive ra-
diative forcing has been measured in this region (Graaf et
al., 2012; de Graaf et al., 2014, 2020; Peers et al., 2015).
Strong differences persist between simulations of climate
models, resulting in high uncertainties in estimating their ra-
diative forcing, especially in this part of the world (Boucher
et al., 2013; Myhre et al., 2013a; Stier et al., 2013). Over
the SEAO, the BBA direct radiative forcing estimated at the
top of the atmosphere (TOA) by the 16 global models of the
AeroCom project (Huneeus et al., 2011; Myhre et al., 2013b;
Bian et al., 2017) is highly variable, with large deviations ob-
served within the range of these climate numerical models:
from -1.16 W m⁻² (cooling effect) for the GMI MERRA
model up to +1.62 W m⁻² (warming effect) for the CAM5.1
MAM3 model (Zuidema et al., 2016b). The absorption of so-
lar radiation by BBA above clouds causes a warming where
the aerosol layer is located. This warming would alter the
thermodynamic properties of the atmosphere, which would
impact the vertical development of low clouds. Clouds un-
der these BBA layers would then be optically thicker, and
the altitude of their cloud top would be lower. This semi-
direct effect has been observed off the coasts of Angola and
Namibia (Wilcox, 2012; Deaconu et al., 2019). Modelling
studies have shown that the BBA semi-direct radiative forc-
ing above stratocumulus clouds over the SEA region is pri-
marily negative at the TOA. It was estimated on average at
-2.6 W m⁻² over the July–September period by Sakaeda et
al. (2011) or at -30.5 W m⁻² during few days of study (pe-
riod 5–10 August 2016, Gordon et al., 2018). Recent mod-
elling studies have also shown that African BBA could have
an indirect radiative effect of -10.1 W m⁻² (5–10 August
2016, Gordon et al., 2018) and -8.05 W m⁻² (1 August to
30 September 2014, Lu et al., 2018) over the SEA region
during the dry season. There are sometimes cases of contact
by the cloud top or BBA transport in the lower layers im-
pacting the cloud properties such as the increase in liquid
water path (Costantino and Bréon, 2013). It is worth noting
that the transport of BBA in the boundary layer has also been
reported by recent ground-based and airborne observations
(Zuidema et al., 2018b; Haslett et al., 2019; Denjean et al.,
2020; Kacarab et al., 2020; Redemann et al., 2021; Zhang
and Zuidema, 2021). As with semi-direct effects, it should
be noted that there is still no consensus on quantifying the
indirect effects of BBA over the SEA region.

These disagreements between AeroCom models on the
properties of aerosols above clouds are explained by differ-
ences in parameterizations on the aerosol injection height,
the aerosol lifetime (related to the processes of deposition, re-
moval, etc.) and on the aerosol absorption (Peers et al., 2016).
The literature reports a wide range of BC/OC mass ratio val-
ues for African BBA plumes depending on the different types
of burned vegetation in Africa (extratropical forests, tropical
forests, savannahs, grasslands and crop residues). These car-
bonaceous aerosol mixing ratios can be highly variable, rang-
ing from 0.06 to 0.33 at the level of BBA emission sources
(Bond et al., 2004; Liousse et al., 2010; Werf et al., 2010;
Akagi et al., 2011) and from 0.11 to 0.24 during the trans-
port of BBA plumes (Ruellan et al., 1999; Formenti et al.,
2003; Kirchstetter et al., 2003; Capes et al., 2008). In ad-
dition, a wide range of BC spectral refractive indices is re-
ported in the literature (from 1.6 to 2.0 for its real part and
from 0.45 to 1.1 for its imaginary part – Bond and Bergstrom,
2006; Bond et al., 2013; Liu et al., 2018), which can be
explained by the diversity of experimental techniques im-
plemented with their own uncertainties or by not perfectly
pure sample collection (i.e. contaminated by other chemical
species) (Bond and Bergstrom, 2006; Bond et al., 2013). Cur-
rent uncertainties are also related to combustion conditions,
types of burned fuels, and BC ageing and its fractal morphol-
ogy (Sorensen, 2001; Bond and Bergstrom, 2006). The pres-
ence of BrOC and its proportion in the BB plumes (Arola,
2011; Laskin et al., 2015), the variability of its spectral re-
fractive index values (Kirchstetter et al., 2004; Alexander et
al., 2008; Chen and Bond, 2010; Hoffer et al., 2016, 2017;
Sumlin et al., 2017), and its atmospheric lifetime (Samset et
al., 2014; Wang et al., 2014) prevent accurate representation
of this chemical compound in climate models. Uncertainties
about emitted amounts of black and primary organic carbon
(Giglio and Randerson, 2010; Werf et al., 2010; Wiedinmyer
et al., 2011; Kaiser et al., 2012; Turquety et al., 2014; An-
dreae, 2019; Pan et al., 2019) are other key elements highly
influencing the BBA absorption properties.

In this context, the SEA region has been the subject of sev-
eral scientific studies and publications focusing on aerosol–
radiation and aerosol–cloud interactions and their climate
impacts (e.g. Wilcox, 2012; Meyer et al., 2013; de Graaf et
al., 2014; Peers et al., 2016; Zuidema et al., 2016b). Inter-
national research programmes have been in place since the
1990s (SAFARI-1992, Lindesay et al., 1996) and until very
recently around southern Africa (Zuidema et al., 2016b; Pi-
stone et al., 2019; Denjean et al., 2020; Taylor et al., 2020;
Haywood et al., 2021; Redemann et al., 2021). In particu-
lar, the SAFARI-2000 field campaign provided a set of air-
borne and ground measurements of aerosol absorption prop-
erties over the South African region, including their single
scattering albedo (Swap et al., 2002; Haywood et al., 2003).
The SSA of aerosols could thus be estimated at 0.85 ± 0.02
at 550 nm on a regional average and during the BB season,
confirming the highly absorbing nature of the aerosols emit-
ted from vegetation fires in this region (Leahy et al., 2007). Nevertheless, some questions about the aerosol absorption spectral dependence or its evolution during aerosol transport have not been resolved with these pioneering campaigns (Formenti et al., 2019). SAFARI-2000's observations also showed that these AA could exert a positive direct radiative forcing above clouds (Keil and Haywood, 2003). More recently, several new observation campaigns have been put in place during the 2016–2018 period to advance the characterization of BBA in this region and to better understand their interactions with clouds and their radiative effects (Zuidema et al., 2016b). These field campaigns have been initiated by various international teams with, in particular, the American ORACLES (ObseRvations of Aerosols above CLouds and their intEractionS – Redemann et al., 2021) and LASIC (Layered Atlantic Smoke Interactions with Clouds – Zuidema et al., 2018a) and the British CLARIFY-2017 (CLoud-Aerosol-Radiation Interaction and Forcing: Year 2017 – Haywood et al., 2021) projects. The French teams conducted a field campaign on the Namibian Atlantic coast during the summer of 2017 as part of the French National Research Agency AEROCLO-sA project, deploying a set of ground-based and airborne measurements (Formenti et al., 2019). This coordinated international effort has provided a comprehensive set of ground and airborne measurements of aerosol and cloud properties over southern Africa and the south tropical Atlantic region. Innovative satellite observations of aerosols and clouds derived from the Polarization and Directionality of the Earth's Reflectances (POLDER-3) space sensor in clear sky (Dubovik et al., 2011, 2014) and above clouds (Waquet et al., 2013a, b; Peers et al., 2015) and from the Spinning Enhanced Visible and InfraRed Imager (SEVIRI) were also recently developed (Peers et al., 2019, 2020) and offer new opportunities (e.g. daily coverage, high spatial and temporal resolutions).

Progress towards more accurate modelling of BBA transported above clouds and their associated radiative effects in the SEA region requires robust representation of their loads and their physico-chemical and absorption properties (Stier et al., 2013; Zuidema et al., 2016b; Mallet et al., 2020). Here we use the WRF-Chem coupled meteorology–chemistry regional model, which allows simulations at higher spatial and temporal resolutions than current global climate models with a better representation of aerosol processes to simulate the life cycle of aerosols, their loads and their absorption properties (Grell et al., 2005; Fast et al., 2006; Peckham, 2012; Powers et al., 2017) over the SEA region. Coincident POLDER-3 innovative satellite aerosol retrievals, available both in clear and cloudy conditions, are used to constrain the chemical composition of BBA simulated with the WRF-Chem model. The methodology consists in adjusting the aerosol absorption properties in WRF-Chem by analysing its sensitivity to different input parameters, i.e. the amount of black and primary organic carbon emitted by biomass combustion at the source level, the BC/OC mass ratio, and the

black and brown carbon absorption. This approach leads to an optimized configuration of WRF-Chem for aerosol simulations over the SEA region, with constrained aerosol key parameters (AOD, SSA and their spectral dependence) above clouds in the model, in order to properly calculate their forcing and heating rates and subsequently to better quantify their feedbacks on clouds. Because of the availability of POLDER-3 coincident satellite data, our study focuses on July 2008 since this period allowed us to observe many strongly absorbing BB events associated with strong direct radiative effects (Waquet et al., 2020) and potential semi-direct and indirect effects on clouds.

The structure of this article is as follows. Section 2 describes the modelling tool and satellite data as well as the strategy used to improve the representation of BBA distribution and absorption properties in regional climate models. Section 3 reports results for the meteorology; reports the aerosol load, size, and horizontal and vertical distribution; and then focuses on aerosol absorption properties. Section 4 summarizes the main results and conclusions of our study.

## 2 Data and method

### 2.1 WRF-Chem: a regional meteorological model coupled with chemistry

#### 2.1.1 Description

WRF-Chem (Weather Research and Forecasting Model coupled with Chemistry) is a regional model whose specialty is to couple atmospheric chemistry with meteorology (Grell et al., 2005; Fast et al., 2006). Particulate pollution influences climate change because aerosols affect the radiative transfer properties of the atmosphere. Also, climate change can alter the mechanisms of formation, transport, ageing and scavenging of atmospheric particles. WRF-Chem captures this complexity. It is a chemistry–transport model coupled with a mesoscale weather model designed for atmospheric research and operational forecasting applications (Skamarock et al., 2005, 2008). WRF-Chem is used in many types of air quality and climate research and offers a wide range of options for modelling of gas and particulate chemistry (Grell et al., 2004; Grell and Baklanov, 2011; Baklanov et al., 2014; Powers et al., 2017). The main physical and chemical options selected for the detailed simulation of atmospheric chemistry with WRF-Chem V3.9.1.1 initial configuration are shown in Table 1.

We chose the MOZCART chemistry scheme (Pfister et al., 2011) which links the MOZART (Model for OZone And Related chemical Tracers) gas phase chemistry module (Emmons et al., 2010) with the GOCART (Global Ozone Chemistry Aerosol Radiation and Transport) aerosol module (Chin et al., 2000a, b; Ginoux et al., 2001; Chin et al., 2002) because it is well suited for BB chemistry (Emmons et al.,
<table><caption>**Table 1.** WRF-Chem V3.9.1.1 main physico-chemical options selected for the study of the biomass burning aerosol optical properties and their climate forcing over the southeast Atlantic region.</caption><thead><tr><th>Parameterization</th><th>Variable name</th><th>Option</th><th>Module</th><th>Reference</th></tr></thead><tbody><tr><td colspan="5"><strong>Physics</strong></td></tr><tr><td>Cloud microphysics</td><td>mp_physics</td><td>2</td><td>Lin (Purdue)</td><td>Lin et al. (1983)</td></tr><tr><td>Cloud convection</td><td>cu_physics</td><td>5</td><td>Grell-3</td><td>Grell (1993)<br>Grell and Dévényi (2002)</td></tr><tr><td>Surface pattern</td><td>sfsurface_physics</td><td>2</td><td>Noah LSM</td><td>Tewari et al. (2004)</td></tr><tr><td>Planetary boundary layer</td><td>bl_pbl_physics</td><td>1</td><td>YSU</td><td>Hong et al. (2006)</td></tr><tr><td>Shortwave radiation</td><td>ra_sw_physics</td><td>2</td><td>Goddard</td><td>Chou and Suarez (1994)</td></tr><tr><td>Longwave radiation</td><td>ra_lw_physics</td><td>1</td><td>RRTM</td><td>Mlawer et al. (1997)</td></tr><tr><td colspan="5"><strong>Chemistry</strong></td></tr><tr><td>Chemistry</td><td>chem_opt</td><td>112</td><td>MOZCART+KPP</td><td>Pfister et al. (2011)</td></tr><tr><td>Anthropogenic emissions</td><td>emiss_opt</td><td>8</td><td>MOZCART</td><td>Pfister et al. (2011)</td></tr><tr><td>Desert dust emissions</td><td>dust_opt</td><td>3</td><td>GOCART AFWA</td><td>Jones et al. (2010, 2012)</td></tr><tr><td>Biogenic emissions</td><td>bio_emiss_opt</td><td>3</td><td>MEGAN</td><td>Guenther et al. (2006)</td></tr><tr><td>Biomass burning emissions</td><td>biomass_burn_opt</td><td>2</td><td>MOZCART</td><td>Pfister et al. (2011)</td></tr><tr><td>Aerosol mixing state</td><td>aer_op_opt</td><td>1</td><td>Volume approximation</td><td>Ghan et al. (2001)<br>Fast et al. (2006)<br>Barnard et al. (2010)</td></tr></tbody></table>

2015; Lassman et al., 2017). MOZCART simulates the life cycle of the main aerosol types, i.e. black carbon (BC), organic carbon (OC), sulfates (SO₄²⁻), desert dust aerosols (DUST), and sea salt aerosols (SEAS), as well as a large number of gaseous species (85 species evolving according to 196 chemical reactions including 39 photolysis). MOZCART calculates their transport, their chemical ageing (Helfand and Labraga, 1988; Allen et al., 1996; Lin and Rood, 1996), and their dry (Fuchs et al., 1965; Wesely, 1989) and wet (Giorgi and Chameides, 1986; Balkanski et al., 1993) depositions.

For meteorological input data, we used the meteorological reanalyses from NCEP (National Centers for Environmental Prediction) global reanalysis provided by GFS (Global Forecast System) at 1° horizontal spatial resolution updated every 6 h (Kalnay et al., 1996).

We chose the homogeneous internal mixing state of particles in our WRF-Chem numerical simulations because this type of mixture is consistent with that considered in the POLDER-3 satellite inversion algorithms used to retrieve aerosol optical properties. The aerosol radiative feedbacks are not taken into account in the present study.

## 2.1.2 Configuration

Our domain of study centred on the SEA region is illustrated in Fig. 1 with the black frame (20° W–30° E, 39.4° S–10° N). This domain corresponds to the area affected by transport of BBA plumes off the southwest coasts of Africa. We have simulated an extended area (34.1° W–45.1° E, 39.4° S–33° N) in order to take into account all desert, marine, biogenic, anthropogenic and BB emissions of aerosols that

could impact our region of interest. The horizontal spatial resolution of the simulations performed with WRF-Chem in this area is 30 × 30 km². The temporal resolution of the WRF-Chem numerical simulations is hourly. The atmospheric layer is divided into 50 vertical levels using the hybrid sigma-pressure vertical coordinate. The vertical levels are terrain-following near the surface, with a finer resolution than at the upper pressure level set at 50 hPa.

We have simulated the first half of July 2008 (plus 15 d spin-up) for the numerical experiments to reduce numerical costs. The computation time for a numerical simulation was about 3 d for this time period and about 6 d for the whole month (plus 15 d spin-up). Furthermore, the first half of July 2008 appears to be representative of July 2008. Indeed, the above-cloud aerosol optical depth (ACAOD) and the above-cloud single scattering albedo (ACSSA) retrieved by POLDER-3/AERO-AC at 550 nm are respectively 0.45 and 0.85 over the first half of July 2008 and 0.46 and 0.85 over July 2008 on average over our combined studied areas (black frames in Fig. 2). These values confirm significant amounts of AA transported above clouds of the SEAO during this time of the year.

The studied area for the optical properties of BBA is separated into two distinct areas (black frames in Fig. 2). The first area (a, 12–30° E, 10–0° S) corresponds to the BBA emission sources over the southern African continent and will be analysed in clear atmosphere for comparisons with the POLDER-3/GRASP data (Dubovik et al., 2011, 2014). The second area (b, 0–15° E, 15–5° S) corresponds to the transport of BBA plumes above clouds over the SEAO and will be analysed in cloudy atmosphere for comparisons with the
POLDER-3/AERO-AC data (Waquet et al., 2013a, b; Peers et al., 2015). The purpose of this distinction is to better differentiate the various physico-chemical mechanisms involved between the emissions and transport of BBA (changes in the size and chemical composition of particles) impacting their optical properties. This differentiation also maximizes the number of satellite observations available (see Fig. 2).

We choose the RETRO (REanalysis of the TROpospheric chemical composition, Schultz et al., 2007) global inventory for the anthropogenic emissions at a horizontal spatial resolution of 0.5 × 0.5° and at a monthly temporal resolution over the 1960–2000 period. Biogenic emissions are calculated by WRF-Chem from surface, vegetation and weather data using MEGAN2.1 (Model of Emissions of Gases and Aerosols from Nature version 2.1, Guenther et al., 2012) at a horizontal spatial resolution of 1 × 1 km² and at a monthly temporal resolution. Emissions of desert dust and sea salt particles are calculated online by WRF-Chem using the GOCART aerosol module from meteorological and surface parameters.

We use the APIFLAMEv1 (Analysis and Prediction of the Impact of Fires on Air Quality Modeling, version 1.0) detailed French global inventory for BB emissions (Turquety et al., 2014), which is connected to a smoke plume rise model (Freitas et al., 2006, 2007; Grell et al., 2011). This time-dependent 1D cloud model explicitly simulates the rise of the plumes from the source level in function of the convective transport mechanisms and the ambient weather and thermodynamic conditions calculated by WRF-Chem. APIFLAMEv1 calculates daily emissions of 49 chemical compounds produced by BB such as the BC, the OC or the carbon monoxide (CO, considered as a fire tracer) at a horizontal spatial resolution of 1 × 1 km². The methodology is based on burned areas and combustion temperatures from remote sensing data as well as emission factors specific to burnt vegetation from the Akagi et al. (2011) database. Comparison of APIFLAMEv1's CO emissions with those from three other BB emission inventories often used in the scientific community, GFEDv3 (Global Fire Emissions Database, version 3.0 – Giglio and Randerson, 2010; Werf et al., 2010), FINNv1 (Fire INventory from NCAR, version 1.0 – Wiedinmyer et al., 2011) and GFASv1 (Global Fire Assimilation System, version 1.0 – Kaiser et al., 2012), showed good spatial-temporal correlations of 0.9 (Turquety et al., 2014). These three global emission inventories also rely on MODIS observations for fire detection. The validation study of APIFLAMEv1 conducted by Turquety et al. (2014) showed uncertainties of a factor of 2 to 4 on the emitted amounts of carbonaceous species linked in particular to the wide variability of emission factors by vegetation type. However, these uncertainties are similar to those associated with other BB emission inventories (Wiedinmyer et al., 2011). It is worth noting that the global total emission amounts of carbonaceous aerosols differ by a factor of 3 to 4, ranging from 1.65 to 5.54 Tg for BC and from 13.76 to 51.93 Tg for OC (Pan et al., 2019). Figure 1 illustrates the monthly mass concentrations

(in g m⁻²) of PM₁₀ emitted at surface by BB during the July–September 2008 period (from left to right) in Africa from APIFLAMEv1 (Turquety et al., 2014) used in WRF-Chem V3.9.1.1.

Figure 1 indicates the location of wildfire sources with significant activity which are mainly in the southern half of Africa during the simulated period. During the dry season, which extends from May to October, the sources of wildfires gradually move south and east, in agreement with previous studies in this region (Cahoon et al., 1992; Roberts et al., 2009). Figure 1 shows that the BB emission inventory of Turquety et al. (2014) reflects the expected variability in the detection of BBA sources in Africa.

## 2.2 A-Train aerosols and clouds satellite data

### 2.2.1 POLDER-3/PARASOL

The clear-sky Generalized Retrieval of Aerosol and Surface Properties (GRASP) inversion algorithm allows the retrieval of the atmospheric properties of aerosols either from combined or separate observations from different passive and active remote sensing tools (satellite, ground, airborne) (Dubovik et al., 2011, 2014). Applied on POLDER-3's measurements of linearly polarized radiance (490, 670 and 865 nm) and total radiance (443, 490, 565, 670, 865 and 1020 nm), POLDER-3/GRASP allows us to derive surface properties (e.g. albedo, reflectance), aerosol optical properties (e.g. total extinction optical depth, total absorption optical depth, fine-mode optical depth, coarse-mode optical depth, Ångström exponent, single scattering albedo, refractive index), aerosol microphysical properties (e.g. particle size distribution, fine and coarse modes, spherical fraction of particles) and the average altitude of the aerosol layer. In this study, we will use the so-called “optimized” version of POLDER-3/GRASP, which includes some approximations on radiative transfer calculations in order to obtain the best possible compromise between processing speed and accuracy of the results. This processing allowed the entire POLDER-3/PARASOL archive (March 2005–October 2013) to be analysed for the first time with this type of algorithm. Comparisons with coincident AERONET data have shown that the total aerosol optical depth (AOD) is retrieved within an uncertainty range of about ±15% (per pixel estimate) over land and ocean (Dubovik et al., 2011; Popp et al., 2016; Chen et al., 2018, 2019, 2020; Li et al., 2019). The maximum error on the SSA was estimated to be about ±0.05% (per pixel estimate) over land surfaces and in cases of high aerosol loads (Chen et al., 2020). In this study, we will use the total extinction optical depth at 565 nm and its spectral dependence (443, 490, 565, 670, 865 and 1020 nm) derived from POLDER-3/GRASP in clear-sky conditions to assess the WRF-Chem model in terms of BB emission sources over land. The spectral retrievals of the single scattering albedo from 443 to 1020 nm will be used to study the absorption
<figure><img src="image_4.png" /><figcaption>Figure 1. Monthly mass concentrations of PM₁₀ (in g m⁻²) emitted at the surface by African biomass burning in July (a), August (b) and September (c) 2008 from the APIFLAMEv1 biomass burning emission inventory (Turquety et al., 2014). The black frames (20° W–30° E, 39.4° S–10° N) represent the area of study.</figcaption></figure>

properties and chemical composition of the emitted simulated aerosols.

The AEROSol Above Clouds (POLDER-3/AERO-AC) inversion algorithm retrieves the aerosol optical and microphysical properties above liquid water clouds by combining POLDER-3's multidirectional and multispectral measurements of polarized (670 and 865 nm) and total (490 and 865 nm) radiances (Waquet et al., 2013a, b; Peers et al., 2015). POLDER-3/AERO-AC retrieves the aerosol extinction optical depth (ACAOD<sub>ext</sub>) and their single scattering albedo (ACSSA) at 490, 550, 670, and 865 nm and their Ångström exponent (ACAE<sub>670–865</sub>) simultaneously with the optical depth of the underlying cloud (COD) at a spatial resolution of 6 × 6 km² and an almost daily temporal resolution. Retrievals are only provided in cases of optically thick (COD > 3) and homogeneous liquid water clouds, fractional cloud covers, and cloud edges being eliminated. Scenes corresponding to cirrus clouds above liquid clouds are identified from coincident measurements acquired in thermal infrared by the MODIS instrument and are also discarded (Waquet et al., 2013a, b; Peers et al., 2015). This innovative inversion method was the first to allow the retrieval of aerosol properties above cloudy scenes at a global scale (Waquet et al., 2013a). Sensitivity studies for POLDER-3/AERO-AC indicate maximum relative errors of ±20 % on the extinction optical depth and ±0.05 % on the single scattering albedo of BB particles transported above liquid clouds (Peers et al., 2015). This inversion technique has been compared with retrievals from the CALIOP lidar (Deaconu et al., 2017). The analysis of the extinction optical depth retrieved by the CALIOP depolarization product (Hu et al., 2009) showed deviations of less than 20 % compared to POLDER-3/AERO-AC on the ACAOD<sub>ext</sub> for the fine particles of BB. Differences between POLDER-3/AERO-AC and CALIOP are increasing for mineral dust and especially for a complex mixture of aerosols (e.g. BB and urban pollution). In this study, we will use the aerosol extinction optical depth at 550 nm and its spectral dependence (490, 550, 670 and 865 nm) to assess the WRF-Chem model in terms of BBA content transported above ma-

rine stratocumulus over the SEAO. Spectral retrievals of the single scattering albedo from 490 to 865 nm above clouds will be used to study the absorption properties and chemical composition of simulated aerosols off the coasts of southern Africa.

The aerosol parameters simulated with WRF-Chem have been spatially and temporally collocated with the remote sensing parameters to be quantitatively comparable. First, the POLDER-3/GRASP and POLDER-3/AERO-AC data initially at a horizontal spatial resolution of 6 × 6 km² are aggregated onto the model's grid (30 × 30 km²). Then, POLDER-3's clear-sky and cloudy-sky masks were applied to the data simulated with WRF-Chem. Finally, the model meteorological-optical-chemical parameters are averaged between 13:00 and 14:00 (all time references are in local time) to be consistent with the PARASOL satellite transit time (about 13:30 over the SEA region). Thus, each pixel simulated with WRF-Chem can be compared to a coincident aggregated pixel retrieved by the POLDER-3 space sensor in clear sky (GRASP) and above clouds (AERO-AC). Finally, the aerosol optical properties simulated with WRF-Chem at four wavelengths (300, 400, 600 and 1000 nm) in the shortwave radiation are recalculated at the wavelengths of the POLDER-3 aerosol retrievals. The single scattering albedo (SSA) is linearly interpolated. The aerosol optical depth (AOD) is interpolated using the Ångström power law according to the following relationship:

$$AOD(\lambda_{\text{interpol}}) = AOD(\lambda_1) \left( \frac{\lambda_{\text{interpol}}}{\lambda_1} \right)^{-\frac{\ln\left(\frac{AOD(\lambda_1)}{AOD(\lambda_2)}\right)}{\ln\left(\frac{\lambda_2}{\lambda_1}\right)}}, \quad (1)$$

where $\lambda_{\text{interpol}}$ is the wavelength to be interpolated between $\lambda_1 = 400$ nm and $\lambda_2 = 600$ nm if $400 \text{ nm} < \lambda_{\text{interpol}} < 600$ nm or between $\lambda_1 = 600$ nm and $\lambda_2 = 1000$ nm if $600 \text{ nm} < \lambda_{\text{interpol}} < 1000$ nm.
Figure 2 illustrates the number of observation days in clear (a) and cloudy (b) skies available from the POLDER-3 space sensor during the first half of July 2008.

Figure 2 indicates the state of the sky (clear or cloudy) over the SEA region during the first half of July 2008. This figure shows the semi-permanent layer of marine stratocumulus inside the area (0–15° E, 15–5° S) characterized by the absence of satellite data in clear sky (a) and by the largest number of satellite data in cloudy sky (b).

Filters were applied to the POLDER-3 satellite observations to keep the signal associated with the lowest uncertainties on the retrieved aerosol optical properties. In clear-sky conditions, POLDER-3/GRASP aerosol optical depth and single scattering albedo were filtered according to the criterion AODobs(443 nm) ≥ 0.4 (Dubovik et al., 2011, 2014). Above cloudy scenes, we used the POLDER-3 AERO-AC-quality-assured-absorption-6 km product, which uses criteria to ensure the quality of the retrieval of the aerosol absorption above clouds (Waquet et al., 2020). These criteria restrict the retrievals of aerosol absorption above clouds to scenes with significant aerosol loading above clouds and optically thick clouds for which the sensitivity of the retrieval absorption method is maximal (Peers et al., 2015, 2016).

### 2.2.2 Ancillary data from CALIOP/CALIPSO

The operational inversion method applied to the CALIOP lidar level 2 data mainly retrieves the AOD in clear sky and above clouds, the Ångström exponent (AE) above clouds, and the vertical profiles of the aerosol backscatter and extinction coefficients from the backscattering signal measured at 532 and 1064 nm and the depolarization ratio (Winker et al., 2009). The altitudes of the base and the top of the clouds and the aerosols are also provided. In this study, we will use the vertical profiles of the aerosol extinction coefficient at 532 nm to evaluate that simulated with WRF-Chem at 550 nm. We will also use the altitudes of the aerosol and cloud layers provided by CALIOP to assess their vertical distributions simulated with WRF-Chem.

## 2.3 Methodology

Our approach is summarized in Fig. 3, with the main aerosol parameters investigated in the WRF-Chem numerical experiments reported in Table 2.

As a first step, we use the ECMWF ERA-Interim reanalysis and the aerosol and cloud satellite observations from the A-Train to test the performance of the model in its initial configuration (S0, in Fig. 3) in terms of simulations of meteorology and aerosol horizontal and vertical distribution, including their load. The simulated intensity of the BBA emissions over the South African sources is evaluated using the AOD from POLDER-3/GRASP. Potential biases are then corrected by adjusting the emission inventories. Desert dust emissions from North African sources are also considered as they may

contribute to the total aerosol load over our studied area. The transport of mineral dust off the coast of the SEAO is notably supported by recent satellite and airborne observations performed in the northern part of our domain (Deaconu et al., 2019; Denjean et al., 2020). Table 2 provides the uncertainties associated with the emissions of these two aerosol types (Turquety et al., 2014; Flaounas et al., 2016) along with the correction factors tested in the WRF-Chem numerical simulations.

The injection height of BBA at the source level is evaluated using the aerosol vertical distribution provided by CALIOP. It should be noted that the parameterization used in WRF-Chem (smoke plume rise model, Freitas et al., 2006, 2007; Grell et al., 2011) allows aerosols to be injected high enough into the atmosphere to simulate the transport of the BBA plumes above clouds over the SEAO. In addition, the simulation of the cloud top height in WRF-Chem is investigated and evaluated, as this has a direct impact on the ability of the model to compute realistic above-cloud aerosol loads.

Finally, we evaluate the aerosol size distributions simulated with WRF-Chem, because of their known influence on the calculation of the SSA. This analysis will help to separate the impact of the aerosol size from the aerosol chemical composition when comparing the simulated and the satellite-derived SSA.

Following the evaluation of the model's performance, the possible biases are corrected by adjusting the emissions at the source level within their reported uncertainties. The partially constrained (PC, hereafter) configuration of WRF-Chem (S1, in Fig. 3) corresponds to the configuration using the corrected emissions. It is worth noting that the assessment conducted in the first step is done for the whole month of July 2008.

The second step of our approach consists in simultaneously constraining the load and the chemical composition of the BBA simulated with WRF-Chem using the spectral extinction (clear-sky and above-cloud AOD) and the spectral absorption (clear-sky and above-cloud SSA) from POLDER-3, in order to set up an optimized configuration of the model (S2, in Fig. 3). Simulations are performed with WRF-Chem in its PC configuration using different amounts of BC, OC and BrOC at the source level. The range of BC/OC and BrOC/OC ratios used in this experiment have been selected according to uncertainties from the literature (Werf et al., 2010; Akagi et al., 2011) and are reported in Table 2. The set of BC, OC and BrOC amounts that reproduces the satellite observations the best corresponds to the optimized configuration (S2, in Fig. 3). These simulation experiments also take into account complex refractive indices of pure species for BC and BrOC (see Table 2). We have tested two values of the BC refractive index. First, the one recommended by Bond and Bergstrom (2006), $m_{BC,550} = 1.95 - 0.79i$, which is commonly used as input data into climate models and implemented by default in WRF-Chem. Secondly, we have tested the BC refractive index of Williams et al. (2007), $m_{BC,550} = 1.75 - 1.03i$, which is more absorbing and could
<figure><img src="image_5.png" /><figcaption>**Figure 2.** Number of observation days ($N_{days}$) in clear atmosphere (a) and cloudy atmosphere (b) available from the POLDER-3 space sensor during the 1–15 July 2008 period. The black frames indicate the two areas of study of the biomass burning aerosol optical properties in clear sky over land (12–30° E, 10–0° S, a) and above clouds over the southeastern Atlantic Ocean (0–15° E, 15–5° S, b).</figcaption></figure>

<figure><img src="image_6.png" /><figcaption>**Figure 3.** Schematic diagram of the general approach applied to constrain WRF-Chem simulations of aerosols using A-Train satellite co-incident retrievals of the distributions of aerosols and clouds. AOD, ACAOD, SSA, ACSSA, $\sigma_{ext}$, AE, ACAE and $z_{CTH}$ stand for aerosol optical depth, above-cloud aerosol optical depth, single scattering albedo, above-cloud single scattering albedo, aerosol extinction coefficient, Ångström exponent, above-cloud Ångström exponent and cloud top height, respectively.</figcaption></figure>

be more realistic than that of Bond and Bergstrom (2006) since it underestimates by only 4% (30% for that of Bond and Bergstrom, 2006) the mass absorption cross-section reference value ($MAC_{BC,fresh} = 7.5 \pm 1.2 \text{ m}^2 \text{ g}^{-1}$) for freshly emitted BC, i.e. unaged and uncoated (Bond and Bergstrom, 2006; Liu et al., 2020).

The spectral BrOC refractive index provided by Hoffer et al. (2016, 2017), i.e. $m_{BrOC} = 1.86 - 0.25i$ at 550 nm, has been used in our numerical experiments with three values of absorbing fractions of OC (0, 0.025 and 0.05) based on preliminary sensitivity tests. Hoffer et al. (2016, 2017) are the first, to our knowledge, to propose a direct experimental measurement of the absorption of BrOC particles from the ultraviolet to the near-infrared using an aethalometer with seven spectral bands (370–950 nm).

It should be noted that other parameterizations in the model governing the life cycle of aerosols, such as ageing, mixing, deposition or entrainment, have not been modified or tested, but they may also have an impact on the AOD and the SSA. The performance of the WRF-Chem numerical simulations will be assessed using commonly used statistical parameters (see Appendix A) (Thunis et al., 2011; Lingard et al., 2013): the Pearson correlation coefficient (R), the mean bias (MB), the mean absolute error (MAE) and the root mean square error (RMSE).
<table><caption>**Table 2.** Main parameters investigated, with range of values tested in simulations experiments performed with WRF-Chem, considering the range of values reported in the literature. As indicated in Fig. 3, S1 corresponds to the WRF-Chem partially constrained simulation and S2 to the WRF-Chem optimized configuration. BC, OC and BrOC represent the black carbon, organic carbon and brown carbon in biomass burning aerosols emitted by WRF-Chem.</caption><thead><tr><th></th><th></th><th>Range of values reported<br>in literature</th><th>Tested values in WRF-Chem<br>simulations</th><th></th></tr></thead><tbody><tr><td rowspan="2">Emission inventories<br>(coefficients applied to emissions)</td><td>Desert dust</td><td>0.25 – 1<sup>a</sup></td><td>0.5</td><td>S1</td></tr><tr><td>Biomass burning</td><td>2 – 4<sup>b</sup></td><td>1.5 – 2</td><td>S1</td></tr><tr><td rowspan="2">Composition of biomass burning<br>aerosols</td><td>BC/OC</td><td>0.06 – 0.33<sup>c</sup></td><td>0.06 – 0.25</td><td>S2</td></tr><tr><td>BrOC/OC</td><td>0 – 0.8<sup>d</sup></td><td>0, 0.025, 0.05</td><td>S2</td></tr><tr><td rowspan="2">Imaginary part of refractive index<br>550 nm</td><td>BC</td><td>0.45 – 1.1<sup>e</sup></td><td>0.79 – 1.03<sup>f</sup></td><td>S2</td></tr><tr><td>BrOC</td><td>0.003 – 0.27<sup>g</sup></td><td>0.25<sup>h</sup></td><td>S2</td></tr></tbody></table>

# 3 Results and discussion

## 3.1 Meteorology in the WRF-Chem initial configuration (S0)

Figure 4, Fig. 5 and Fig. 6 show the spatial distributions of monthly averaged wind speed (in m s⁻¹) and direction, specific humidity (in g kg⁻¹), and temperature (in °C) respectively. The parameters at 850 hPa (left), 700 hPa (middle) and 500 hPa (right) for July 2008 simulated with WRF-Chem in its initial configuration (bottom) are compared to the ECMWF ERA-Interim reanalysis (top).

Figure 4, Fig. 5 and Fig. 6 show that the WRF-Chem initial configuration correctly simulates the general pattern of wind speed, wind direction, humidity and temperature in terms of both magnitude and location at the three pressure levels, with only local minor differences. North of the 20th parallel south, the mean simulated winds blow westward off of land and favour a westward transport of BBA plumes emitted from the southern African continent. The WRF-Chem initial configuration slightly overestimates the magnitude of the wind speed with positive mean biases of only 1.18 m s⁻¹ at 850 hPa, 0.68 m s⁻¹ at 700 hPa, and 0.60 m s⁻¹ at 500 hPa and with low root mean square errors (< 1.9 m s⁻¹). The WRF-Chem initial configuration slightly underestimates the magnitude of the specific humidity at 850 and 500 hPa with a negative mean bias of only 0.19 g kg⁻¹ for both pressure levels and low root mean square errors (≤ 1.1 g kg⁻¹), which could impact the column-integrated/above-cloud AOD. Finally, the WRF-Chem initial configuration slightly overestimates the magnitude of temperature for the three pressure levels with low positive mean biases of 0.93°C at 850 hPa, 0.94°C at 700 hPa and 1.17°C at 500 hPa.

Table 3 summarizes the statistics of the comparisons between the simulated and ECMWF wind speed (WSPD, in m s⁻¹), wind direction (WDIR, in °), specific humidity (Q, in g kg⁻¹) and temperature (T, in °C) at 850, 700 and 500 hPa

on average over the SEA region for July 2008. The statistical results shown in Table 3 confirm the overall good agreement between the WRF-Chem initial configuration and the ECMWF reanalysis with spatial correlation coefficients between 0.90 and 0.99. In summary, this evaluation strongly suggests that the WRF-Chem initial configuration is able to correctly reproduce the local meteorology for the domain and the period considered in this study.

## 3.2 Aerosol distribution and size in the WRF-Chem partially constrained configuration (S1)

### 3.2.1 Strength of aerosol emissions

The column-integrated AOD that reflects the vertically integrated aerosol concentration is used here to assess the strength of the simulated aerosol emission sources. Figure 7 illustrates the spatial distribution of monthly averaged AOD at 565 nm in clear sky retrieved by POLDER-3/GRASP (a) and simulated with the initial configuration (b) and with the PC configuration (c) of WRF-Chem for July 2008.

Figure 7 shows that the WRF-Chem initial configuration (mean AOD<sub>mod,565</sub> = 0.49) significantly underestimates, by a factor of 2 on average, the AOD retrieved by POLDER-3/GRASP (mean AOD<sub>mod,565</sub> = 1.10) at 565 nm in clear sky over the BB emission sources (12–30° E, 10–0° S) for July 2008. This bias could be due to an underestimation of the fire activity in the BB emission inventory. The assessment of APIFLAMEv1 by Turquety et al. (2014) indicates possible biases of a factor of 2 to 4 on all amounts of emitted gas and particulate species by BB. We have thus tested three multiplying factors (1, 1.5 and 2). As a result, the adjustment factor of 1.5 represented the best compromise to reproduce the AODs retrieved by POLDER-3/GRASP both over land and above the ocean, even if small biases were still present. Therefore, we have chosen to correct the APIFLAMEv1 BB emission inventory with a moderate multiplicative factor of

<footnote><sup>a</sup> Flaounas et al. (2016). <sup>b</sup> Turquety et al. (2014). <sup>c</sup> Werf et al. (2010) and Akagi et al. (2011). <sup>d</sup> Feng et al. (2013). <sup>e</sup> Liu et al. (2018). <sup>f</sup> Bond and Bergstrom (2006) and Williams et al. (2007). <sup>g</sup> Alexander et al. (2008) and Sumlin et al. (2017). <sup>h</sup> Hoffer et al. (2016, 2017).</footnote>
<figure><img src="image_7.png" /><figcaption>**Figure 4.** Monthly averaged wind speed (m s⁻¹) and direction at 850 hPa (**a**, **d**), 700 hPa (**b**, **e**) and 500 hPa (**c**, **f**) from ECMWF ERA-Interim reanalysis (**a**, **b**, **c**) and simulated with the WRF-Chem initial configuration (**d**, **e**, **f**) for July 2008.</figcaption></figure>

<figure><img src="image_8.png" /><figcaption>**Figure 5.** Same as Fig. 4 but for specific humidity (in g kg⁻¹).</figcaption></figure>

1.5 on all the gas and particulate species, in agreement with the uncertainties provided by Turquety et al. (2014). It is worth noting that this scaling is a common practice in climate modelling studies for BBA to better reproduce the observed satellite AODs (Johnson et al., 2016) with emission factors generally higher than 1 (up to 6, Reddington et al., 2016).

Figure 7 also shows that, over the northern half of Africa in the Sahara and Sahel region, the average values of AOD are highly overestimated in the WRF-Chem initial configuration (mean AOD<sub>mod,565</sub> ≥ 1.5) compared to the POLDER-3/GRASP retrievals (mean AOD<sub>mod,565</sub> ≃ 1.0). The GO-CART AFWA desert dust emission module used in WRF-

Chem (Jones et al., 2010, 2012), based on the Marticorena and Bergametti (1995) scheme, seems to raise too much mineral dust over the Sahara/Sahel area. According to the recommendations of Flaounas et al. (2016), who made an assessment of atmospheric dust modelling performance by WRF-Chem (version 3.6) against MODIS observations on arid and semi-arid regions around the Mediterranean, we have applied the adjustment coefficient of 0.5 on the desert dust emission surface fluxes in the GOCART AFWA scheme. This corrected version of WRF-Chem, in terms of BB and desert dust emissions, is the so-called PC configuration (S1).
<figure><img src="image_9.png" /><figcaption>**Figure 6.** Same as Fig. 4 but for temperature (in °C).</figcaption></figure>

<table><caption>**Table 3.** Meteorology performance statistics of WRF-Chem initial configuration compared to ECMWF ERA-Interim reanalyses. WSPD, WDIR, Q and T represent the wind speed, the wind direction, the specific humidity and the temperature respectively. N, ME, MAE, RMSE and CORR represent the number of coincident data pairs, the mean error, the mean absolute error, the root mean square error and the spatial Pearson correlation coefficient, respectively. The units of the statistical parameters are the same as meteorological variables.</caption><thead><tr><th rowspan="2"></th><th colspan="4">850 hPa</th><th colspan="4">700 hPa</th><th colspan="4">500 hPa</th></tr><tr><th>WSPD (m s<sup>-1</sup>)</th><th>WDIR (°)</th><th>Q (g kg<sup>-1</sup>)</th><th>T (°C)</th><th>WSPD (m s<sup>-1</sup>)</th><th>WDIR (°)</th><th>Q (g kg<sup>-1</sup>)</th><th>T (°C)</th><th>WSPD (m s<sup>-1</sup>)</th><th>WDIR (°)</th><th>Q (g kg<sup>-1</sup>)</th><th>T (°C)</th></tr></thead><tbody><tr><td>N</td><td>31 884</td><td>31 884</td><td>31 884</td><td>31 884</td><td>31 968</td><td>31 968</td><td>31 968</td><td>31 968</td><td>31 968</td><td>31 968</td><td>31 968</td><td>31 968</td></tr><tr><td>ME</td><td>1.18</td><td>-6.92</td><td>-0.19</td><td>0.93</td><td>0.68</td><td>7.90</td><td>0.20</td><td>0.94</td><td>0.60</td><td>-5.43</td><td>-0.19</td><td>1.17</td></tr><tr><td>MAE</td><td>1.32</td><td>28.37</td><td>0.82</td><td>1.02</td><td>1.14</td><td>52.05</td><td>0.58</td><td>1.00</td><td>1.48</td><td>16.33</td><td>0.31</td><td>1.23</td></tr><tr><td>RMSE</td><td>1.70</td><td>1.01</td><td>1.10</td><td>1.21</td><td>1.57</td><td>1.60</td><td>0.83</td><td>1.29</td><td>1.82</td><td>0.75</td><td>0.41</td><td>1.41</td></tr><tr><td>CORR</td><td>0.93</td><td>0.96</td><td>0.95</td><td>0.99</td><td>0.95</td><td>0.90</td><td>0.94</td><td>0.99</td><td>0.97</td><td>0.98</td><td>0.93</td><td>0.99</td></tr></tbody></table>

Figure 7 shows that the WRF-Chem PC configuration better reproduces the magnitude of both BB and desert dust emission sources over land and their transport above ocean compared to WRF-Chem in its initial configuration, even if some biases still remain.

### 3.2.2 Aerosols and clouds vertical distribution

Besides the simulated aerosol loads, the major factors that may influence the WRF-Chem ACAOD are the BBA injection height, the cloud top height and the vertical distribution of both aerosols and clouds.

The injection height of BBA conditions their transport and their potential interactions with cloud layers (Hansen et al., 1997; Podgorny and Ramanathan, 2001; Rosenfeld et al., 2014; Lee et al., 2016). BBA simulated with the WRF-Chem PC configuration are injected into the atmosphere up to an altitude of about 6 km, consistent with CALIOP observations analysed in this part of the world (Koffi et al., 2012, 2016). This allows them to be transported over a long distance. One of WRF-Chem's strengths for the simulation of BBA is that

their injection height is dynamically calculated according to the thermodynamic conditions of fires, whereas it is generally prescribed in climate models (Freitas et al., 2006, 2007; Grell et al., 2011).

The cloud top height from satellite is based on the POLDER oxygen pressure method (Vanbauce et al., 2003; Ferlay et al., 2010; Deaconu et al., 2019). Deaconu et al. (2019) showed that the oxygen pressure method underestimates the cloud top height by about 200–300 m for low liquid clouds compared to the CALIOP retrievals. We applied their proposed empirical relationship to correct the altitude of the cloud top height retrieved by POLDER-3 which is valid for our study area. The advantage of the corrected POLDER-3 data is the much greater spatial coverage than that of the CALIOP lidar, which allows us to obtain better statistics. The estimation of the cloud top height is not directly provided by WRF-Chem. As a first approach, we have only selected clouds with a vertical monolayer structure in the model, i.e. for which the simulated vertical profile of the cloud liquid water content (QCLOUD) has one max-
<figure><img src="image_10.png" /><figcaption>**Figure 7.** Monthly averaged aerosol optical depth (AOD) at 565 nm in clear sky retrieved by POLDER-3/GRASP (a) and simulated with the WRF-Chem initial configuration (b) and with the WRF-Chem partially constrained configuration (c) for July 2008, with the associated histograms of differences between the model and the satellite observations over the whole domain (d, e). The black frames (20° W–30° E, 39.9° S–10° N) represent the area of study.</figcaption></figure>

imum. We have qualified these clouds as homogeneous (in the vertical sense) in the following. Clouds with a complex vertical structure have been qualified as heterogeneous. For these last situations, the simulated QCLOUD vertical profile has several maximums, and the top of the stratocumulus cannot, therefore, be easily defined. The main advantage of this technique is to guarantee the selection of uniform monolayer cloud situations, consistent with data obtained from the POLDER-3/AERO-AC inversion algorithm (Waquet et al., 2013a, b; Peers et al., 2015). Situations with cirrus clouds are rejected as in the POLDER-3/AERO-AC product. The cloud top height is then determined by scanning the cloud profile from the bottom to the top and stopping at a threshold value of liquid water content (LWC). A statistical study was carried out to determine the optimal value of this threshold. We have considered threshold values between 50 % and 100 %, corresponding to a fraction of the vertically integrated QCLOUD in the WRF-Chem PC configuration. This analysis showed that, statistically, the closest results to the POLDER-3 retrievals were obtained with a threshold of 95 % (see Fig. 8). Below this value, the cloud top heights simulated with the WRF-Chem PC configuration shift towards the lowest value classes, enhancing the underestimation of the simulated values compared to the POLDER-3 retrievals. For a threshold of 100 %, the number of cases for the highest classes increases, enhancing the overestimation of the values simulated with the WRF-Chem PC configuration in comparison with those

retrieved by POLDER-3. Figure 8 illustrates the spatial distribution of monthly averaged cloud top heights retrieved by POLDER-3 (a) and simulated with the WRF-Chem PC configuration with the threshold of 95 % (b) for July 2008.

Figure 8 shows that along Angola and Namibia, the WRF-Chem PC configuration simulates well the low cloud area typically observed in these regions (Deaconu et al., 2019). In the studied area (black frame), Fig. 8 shows that the WRF-Chem PC configuration slightly underestimates the mean altitudes of the cloud top compared to the POLDER retrievals. South of the studied area as well as north over land (Congo, Gabon), cloud convection is fairly well reproduced with the WRF-Chem PC configuration, with a mean cloud top height above 2 km. In contrast, a major difference is observed to the west of the studied area, with the WRF-Chem PC configuration simulating cumulus clouds with a mean cloud top height greater than 2.5 km, unlike POLDER-3 that retrieves low clouds with a mean cloud top height around 1.5–2.0 km. The difference between the model and the POLDER-3 retrievals could come from the planetary boundary layer scheme (YSU, Hong et al., 2006) used in the WRF-Chem PC configuration.

Figure 9 illustrates the vertical profiles of the aerosol extinction coefficient ($\sigma_{ext}$, in km$^{-1}$) retrieved by CALIOP at 532 nm (orange dotted lines) and simulated with the WRF-Chem PC configuration at 550 nm (red solid lines) for 12 July 2008 (a) and 28 July 2008 (b). These two specific days were selected due to dense BBA plumes trans-
<figure><img src="image_11.png" /><figcaption>**Figure 8.** Monthly averaged cloud top heights retrieved by POLDER-3 (a) and simulated with the WRF-Chem partially constrained configuration with the threshold of 95% (b) for July 2008, with an associated statistical analysis of the threshold values of the cloud top height tested in the model (c). The black frames (0–15° E, 15–5° S) represent the area of study.</figcaption></figure>

ported above marine clouds over the SEAO. The extinction of aerosols retrieved by CALIOP above clouds has been corrected with POLDER-3/AERO-AC according to Deaconu et al. (2019). Deaconu et al. (2017) have shown that CALIOP underestimates the aerosol load above clouds by a factor of 2 to 4 in comparison with the POLDER-3/AERO-AC retrievals and other advanced CALIOP products such as the so-called depolarization ratio method (Hu et al., 2009). Vertical profiles of the simulated aerosol extinction coefficients are averaged under the CALIOP track aggregated over the area (0–15° E, 15–5° S). This area is characterized by the presence of a semi-permanent layer of marine stratocumulus (see Fig. 2). The mean cloud top heights retrieved by CALIOP (green dotted lines) and simulated with the WRF-Chem PC configuration (blue solid lines) are also shown in Fig. 9.

In Fig. 9, similarities are observed between the vertical profiles from CALIOP and from the WRF-Chem PC configuration with two distinct aerosol layers and the presence of a low cloud layer for both case studies. However, mean altitudes of the aerosol and the cloud layers differ slightly and appear to be systematically underestimated in the WRF-Chem PC configuration compared to the CALIOP retrievals. For 12 July 2008, the aerosol layer located be-

tween 0 and 0.8 km above sea level, generally detected by CALIOP and simulated with the WRF-Chem PC configuration, corresponds to sea salt aerosols in the model, as usually observed in the boundary marine layer (Deaconu et al., 2019; Peers et al., 2019). The aerosol layer located between 1.4 and 4.0 km in the CALIOP observations and between 0.8 and 3.4 km in the WRF-Chem PC configuration corresponds to BBA plumes usually observed in this region at this time of the year (Koffi et al., 2012, 2016; Zuidema et al., 2016b; Formenti et al., 2019). Regarding clouds, the WRF-Chem PC configuration underestimates by about 200 m (300 m) the mean cloud top height on 12 July 2008 (28 July 2008) compared to the CALIOP retrievals. It is worth noting that many models share these aerosol layer altitude biases over this region (Shinozuka et al., 2020) and that the BBA altitude may decrease during the transport (Deaconu et al., 2019). Even if the altitudes of the simulated BBA layers are too low in comparison with the CALIOP retrievals, most of the modelled aerosol extinction is located above clouds, and, therefore, we can conclude that the WRF-Chem PC configuration reproduces well the aerosol load integrated above clouds.
<figure><img src="image_12.png" /></figure>

**Figure 9.** Mean vertical profiles of the aerosol extinction coefficients retrieved by CALIOP at 532 nm (orange dotted lines) and simulated with the WRF-Chem partially constrained configuration at 550 nm (red solid lines) under the CALIOP track inside the study area (0–15° E, 15–5° S) for 12 July 2008 (a) and 28 July 2008 (b). Mean cloud top heights retrieved by CALIOP (green dotted lines) and simulated with the WRF-Chem partially constrained configuration (blue solid lines) are also incorporated into the graphics. CALIOP data, initially at a horizontal spatial resolution of 5 × 5 km², were aggregated onto the WRF-Chem mesh (30 × 30 km²), and only the coincident pixels were selected for the comparison study.

### 3.2.3 Particle size

The SSA of aerosols, which accounts for their absorption properties, depends on both the particles size and their chemical composition (Abel et al., 2003; Laing et al., 2016). The aerosol size can be qualitatively estimated by the AE, with the highest values corresponding to the finest particles (Ångström, 1929). Figure 10 shows the evolution of the vertically integrated (whole atmospheric column) volume size distribution of aerosols simulated with the WRF-Chem PC configuration during the transport of BBA plumes averaged over July 2008.

Figure 10 indicates that fine-mode particles dominate the aerosol volume size distribution near BBA emission sources, with a mean particle diameter centred at 0.3 µm corresponding to the accumulation mode. During the aerosol transport, there is a gradual appearance of larger particles (diameter > 1 µm), which may be linked to ageing processes and also to a slightly more pronounced influence of other larger particles, such as sea salt aerosols mostly in the boundary layer and possibly desert dust aerosols at higher altitudes, which may come across the BBA plumes over the SEAO.

Figure 11 shows the spatial distributions of the AE retrieved by POLDER-3 (a, d) and simulated with the WRF-Chem PC configuration (b, e) in clear sky (AE<sub>670–865</sub>, a, b) and above clouds (ACAE<sub>670–865</sub>, d, e) on average for July 2008.

Figure 11 shows a good agreement between the POLDER-3/GRASP retrievals (a) and the WRF-Chem PC configuration in clear sky (b) with simulated AE<sub>670–865</sub> values greater than 1 over the SEA region and close to 2 over BB emission sources, with these values being very comparable to

those derived from POLDER-3. These values are typical of fine BB particles usually observed in this region (Dubovik et al., 2002). Above clouds over the SEAO, Fig. 11 suggests a decrease in the ACAE associated with the westward progression of the BBA plumes, particularly in the WRF-Chem PC configuration (e). Such an evolution could be related to a gradual growth of BB particles size and/or changes of the overall chemical composition of BBA plumes. Indeed, a decrease in the relative amount of fine BB particles and an increase in the proportion of coarse-mode particles (sea salt and desert dust aerosols) could occur during the transport of BBA plumes over the SEAO, as shown in Fig. 10.

Overall, Fig. 11 indicates that the particle sizes simulated with the WRF-Chem PC configuration are realistic, considering BBA plumes in clear sky and above clouds, with only few minor differences compared to the POLDER-3 retrievals. Therefore, in the following, we assume that the potential difference between the simulated and the observed SSA is primarily due to the chemical composition.

### 3.3 Sensitivity analysis of aerosol absorption in the WRF-Chem partially constrained configuration

Figure 12 illustrates the monthly averaged PM<sub>2.5</sub> chemical composition simulated with the WRF-Chem PC configuration, including organic aerosols (OA, in green), secondary inorganic aerosols (SIA, in grey), organic carbon (OC, in brown), black carbon (BC, in black), desert dust aerosols (DUST, in yellow), and sea salt aerosols (SEAS, in blue), as well as their relative proportions over the southern African continent in clear sky (spatial average over 12–30° E, 10–
<figure><img src="image_13.png" /></figure>

**Figure 10.** Evolution of the vertically integrated (whole atmospheric column) volume size distribution of aerosols (a) simulated with the WRF-Chem partially constrained configuration for three areas representative of the emission sources and transport progress of the biomass burning aerosol plume (b) on average for July 2008. The blue star corresponds to the pixel (14.83° E, 4.00° S) and symbolizes the emission sources of biomass burning particles. The red star corresponds to the pixel (4.82° E, 4.00° S) and symbolizes the biomass burning aerosol plume transported halfway westward over the southeastern Atlantic Ocean. The orange star corresponds to the pixel (14.93° W, 4.00° S) and symbolizes the long-range transport of the biomass burning aerosol plume.

<figure><img src="image_14.png" /></figure>

**Figure 11.** Monthly averaged Ångström exponent retrieved by POLDER-3 in clear sky with GRASP ($AE_{670-865}$, a) and above clouds with AERO-AC ($ACAE_{670-865}$, d) and simulated with the WRF-Chem partially constrained configuration (b, e) for July 2008, with the associated histograms of differences between the model and the satellite observations over the whole domain (c, f).

0° S, a) and above clouds over the SEAO (spatial average over 0–15° E, 15–5° S, b) for July 2008.

In the region of BB emission sources (12–30° E, 10–0° S), organic aerosols (OA, green) are the majority species, with a vertically integrated mass of 120.6 mg m⁻² and representing 57.1 % of the total composition of PM₂. Secondary inorganic aerosols (SIA, grey), i.e. sulfates, nitrates and ammonium, are the second dominant species, representing 37.2 % of the total composition of PM₂ with a vertically integrated mass of 78.6 mg m⁻², followed by organic carbon (OC, brown hatch-

ing) with a vertically integrated mass of 67.0 mg m⁻² (relative proportion of 31.7 %). Vertically integrated mass concentration of black carbon (BC, black) is 4.5 mg m⁻² (relative proportion of 2.1 %). During the transport of the BBA plumes above clouds over the SEAO (0–15° E, 15–5° S), mass concentrations of these BBA decrease due to the deposition processes. Figure 12 shows that the influence of desert dust and sea salt aerosols, although relatively low, increases during transport over the SEAO, from 7.2 to 9.1 mg m⁻² for
<figure><img src="image_15.png" /><figcaption>**Figure 12.** Evolution of the PM<sub>2.5</sub> chemical composition simulated with the WRF-Chem partially constrained configuration between the southern African continent in clear sky (12–30° E, 10–0° S, a) and the southeastern Atlantic Ocean above clouds (0–15° E, 15–5° S, b). Mass concentrations (in mg m<sup>-2</sup>) of the main aerosol compounds of biomass burning, i.e. black carbon (BC, black), organic carbon (OC, brown hatching), organic aerosols (OA, green), and secondary inorganic aerosols (SIA, grey), as well as desert dust aerosols (DUST, yellow) and sea salt aerosols (SEAS, blue), are vertically integrated over the atmospheric column on average for July 2008.</figcaption></figure>

desert dust aerosols and from 0.4 to 1.0 mg m⁻² for sea salt aerosols.

The chemical compositions of aerosols simulated with the WRF-Chem PC configuration appear realistic in comparison with the recent observations obtained from DACCIWA (Dynamics–aerosol–chemistry–cloud interactions in West Africa, Flamant et al., 2017) in southern West Africa (i.e. further north). Specifically, results obtained during the DACCIWA airborne campaigns showed that OA dominated by over 50% the total mass of aerosols, that SIA contributed to about 34% and that the contribution of BC was under 15% (Haslett et al., 2019). However, we can note that BC contributions simulated with the WRF-Chem PC configuration (≤ 2.1%) in our studied areas are smaller than those measured during DACCIWA and LASIC (Zuidema et al., 2018b; Zhang and Zuidema, 2021) campaigns.

Figure 13 illustrates the monthly averaged SSA in clear sky (a, b) and above clouds (d, e) retrieved by the GRASP/AERO-AC inversion algorithms (a, d) and simulated with the WRF-Chem PC configuration (b, e) at 565/550 nm respectively for July 2008.

Figure 13 clearly shows that the aerosols simulated with the WRF-Chem PC configuration, in which only BC absorbs solar radiation in the BBA plumes, are too scattering with a mean positive bias of about 0.08 between the simulated SSA and the one retrieved by POLDER-3, both in clear sky and above clouds, for July 2008. In the continental area in clear sky (12–30° E, 10–0° S), the mean SSA simulated with the WRF-Chem PC configuration is 0.93 at 565 nm, while the SSA retrieved by POLDER-3/GRASP is 0.85 at 565 nm. In the oceanic area above clouds (0–15° E, 15–5° S), the mean SSA simulated with the WRF-Chem PC configuration is 0.93 at 550 nm, which is well above the value of 0.85 at 550 nm retrieved by POLDER-3/AERO-AC. Furthermore, we can also observe a strong disagreement between the SSA from the WRF-Chem PC configuration and the SSA

retrieved by POLDER-3/GRASP over the SEAO in clear atmosphere. On average, POLDER-3/GRASP retrieves a very low SSA of around 0.80 at 565 nm in this region, which the WRF-Chem PC configuration fails to reproduce. To explain the large discrepancies between the WRF-Chem PC configuration and the POLDER-3 retrievals, four hypotheses can be made. (i) There is not enough BC in the BBA plumes simulated with the WRF-Chem PC configuration. (ii) There is too much scattering organic aerosol in the simulated BBA plumes. (iii) The refractive index of BC used in the WRF-Chem PC configuration is not realistic enough. (iv) The presence of other absorbing species in the BBA plumes, such as the BrOC, needs to be considered in the WRF-Chem PC configuration.

Thus, we have analysed the sensitivity of the SSA to the chemical composition of BB carbonaceous aerosols through a set of numerical simulations as a lookup table (reported Table 4).

We have considered adjustment factors up to 4 for BC and down to 1/15 for primary OC (POC) at the source level, consistent with the uncertainties in the APIFLAMEv1 BB emission inventory (Turquety et al., 2014). For example, the possible underestimation of BC emissions could be due to an underestimation of the BC emission factor for savannas (0.37 ± 0.20 g kg⁻¹) in Akagi et al. (2011) used in APIFLAMEv1 compared to the more recent BC emission factor of 0.53 ± 0.35 g kg⁻¹ for savannas in Andreae (2019). Although the 1/10 and 1/15 reduction factors of POC can be considered outside of the POC emission uncertainties (70% of uncertainty in APIFLAMEv1), the corresponding simulations are used to show the impact of an increased aerosol absorption due to a strong increased BC fraction. Each couple of BC and OC adjustment factors is associated with a varying contribution of BrOC equal to 0%, 2.5% or 5%. The BC/OC mass mixing ratio at the surface for all numerical experiments ranges from 0.06 to 0.21 and remains in
<figure><img src="image_16.png" /><figcaption>**Figure 13.** Monthly averaged single scattering albedo of aerosols at 565 nm in clear sky (a, b) and at 550 nm above clouds (d, e) retrieved by POLDER-3 (a, d) and simulated with the WRF-Chem partially constrained configuration (b, e) for July 2008, with the associated histograms of differences between the model and the satellite observations over the whole domain (c, f). The black frames (12–30° E, 10–0° S) and (0–15° E, 15–5° S) represent respectively the two study regions, in clear sky (a, b) and above clouds (d, e).</figcaption></figure>

the order of magnitude of those reported in the literature for African BB (see Table 2). These values are generally around 0.13–0.14 during the transport of the BBA plumes above clouds over the SEAO, consistent with southern Africa airborne measurements (Formenti et al., 2003; Kirchstetter et al., 2003; Capes et al., 2008).

The selection process of the best WRF-Chem solution is described as follows. A score is computed for each WRF-Chem numerical simulation. The score is equal to the number of times the result of the simulation is included within the range of the retrieval uncertainties. This score is computed over all the pixels for the two selected areas (with and without clouds) and over all available spectral aerosol parameters (i.e. AOD, SSA, four spectral bands for AERO-AC and six for GRASP).

As a result, with the BC refractive index of Bond and Bergstrom (2006), $m_{BC,550} = 1.95 - 0.79i$, we were unable to find a realistic solution of WRF-Chem within the uncertainties of APIFLAMEv1 (Turquety et al., 2014). With the BC refractive index of Williams et al. (2007), $m_{BC,550} = 1.75 - 1.03i$, an optimized configuration of WRF-Chem was obtained. It corresponds to the combination of the following carbonaceous aerosol mixture: BC × 2, OC/2.5 with 2.5% of BrOC. This WRF-Chem configuration is the one that statistically reproduces the spectral AOD and SSA retrieved by POLDER-3 the best, both in clear and cloudy atmospheres.

### 3.4 Aerosol optical properties in the WRF-Chem optimized configuration (S2)

Figure 14 illustrates the spectral dependencies of AOD (a, c) and SSA (b, d) simulated with the WRF-Chem optimized configuration (BC × 2, OC/2.5 with 2.5% of BrOC, red curves) and retrieved by POLDER-3/GRASP in clear sky (black curves, a, b) and by POLDER-3/AERO-AC above clouds (black curves, c, d). Aerosol optical properties are averaged geographically on their respective studied areas (black frames in Fig. 2) and temporally over the first half of July 2008.

On Fig. 14, we can see an increase in the AOD and the ACAOD spectral values with decreasing wavelength (a, c) and a decrease in the SSA and the ACSSA spectral values with increasing wavelength (b, d) retrieved by POLDER-3 (black curves in Fig. 14). These trends are characteristic of fine-mode aerosols containing BC, here BB (Dubovik et al., 2002; Bergstrom et al., 2007). Figure 14 shows a general good agreement between the WRF-Chem optimized configuration (red curves) and the POLDER-3 retrievals (black curves) on average for the first half of July 2008, with simulated spectral values of (AC) AOD and (AC) SSA included within the ranges of uncertainties associated with the POLDER-3 retrievals both in clear sky and above clouds.

Over the southern African continent in clear sky (12° E–30° E, 10° S–0° S), the spectral values of the AOD are slightly underestimated in the WRF-Chem optimized configuration.
<table><caption>**Table 4.** Table of numerical experiments performed with the WRF-Chem partially constrained configuration to test the impact of a range of organic carbon (OC), black carbon (BC) and brown carbon (BrOC) proportions on simulated biomass burning aerosols properties.</caption><thead><tr><th colspan="3">Adjustment factors</th><th colspan="3">BC/OC</th></tr><tr><th colspan="3">Source level</th><th>Surface</th><th colspan="2">Vertically integrated</th></tr><tr><th>BC</th><th>OC</th><th>BrOC<sup>3</sup> (%)</th><th>Emissions<br>(12–30° E, 10–0° S)</th><th>Over land/clear sky<br>(12–30° E, 10–0° S)</th><th>Above ocean/above clouds<br>(0–15° E, 15–5° S)</th></tr></thead><tbody><tr><td rowspan="4">×1<sup>1</sup></td><td>/1</td><td rowspan="4">0, 2.5, 5</td><td>0.06</td><td>0.06</td><td>0.06</td></tr><tr><td>/5</td><td>0.14</td><td>0.15</td><td>0.11</td></tr><tr><td>/10</td><td>0.17</td><td>0.19</td><td>0.12</td></tr><tr><td>/15</td><td>0.18</td><td>0.20</td><td>0.13</td></tr><tr><td rowspan="4">×2<sup>1,2</sup></td><td>/1</td><td rowspan="4">0, 2.5, 5</td><td>0.09</td><td>0.10</td><td>0.08</td></tr><tr><td>/2.5</td><td>0.14</td><td>0.15</td><td>0.11</td></tr><tr><td>/5</td><td>0.17</td><td>0.19</td><td>0.12</td></tr><tr><td>/10</td><td>0.19</td><td>0.22</td><td>0.13</td></tr><tr><td rowspan="4">×2.5<sup>2</sup></td><td>/1</td><td rowspan="4">0, 2.5, 5</td><td>0.10</td><td>0.11</td><td>0.09</td></tr><tr><td>/2.5</td><td>0.15</td><td>0.16</td><td>0.11</td></tr><tr><td>/5</td><td>0.18</td><td>0.20</td><td>0.13</td></tr><tr><td>/10</td><td>0.20</td><td>0.22</td><td>0.13</td></tr><tr><td rowspan="4">×3<sup>2</sup></td><td>/1</td><td rowspan="4">0, 2.5, 5</td><td>0.11</td><td>0.12</td><td>0.09</td></tr><tr><td>/2.5</td><td>0.16</td><td>0.17</td><td>0.12</td></tr><tr><td>/5</td><td>0.19</td><td>0.21</td><td>0.13</td></tr><tr><td>/10</td><td>0.20</td><td>0.23</td><td>0.13</td></tr><tr><td rowspan="4">×3.5<sup>1</sup></td><td>/1</td><td rowspan="4">0, 2.5, 5</td><td>0.12</td><td>0.13</td><td>0.10</td></tr><tr><td>/5</td><td>0.19</td><td>0.21</td><td>0.13</td></tr><tr><td>/10</td><td>0.20</td><td>0.23</td><td>0.14</td></tr><tr><td>/15</td><td>0.21</td><td>0.24</td><td>0.14</td></tr><tr><td rowspan="4">×4<sup>1</sup></td><td>/1</td><td rowspan="4">0, 2.5, 5</td><td>0.13</td><td>0.14</td><td>0.10</td></tr><tr><td>/5</td><td>0.19</td><td>0.22</td><td>0.13</td></tr><tr><td>/10</td><td>0.21</td><td>0.24</td><td>0.14</td></tr><tr><td>/15</td><td>0.21</td><td>0.25</td><td>0.14</td></tr></tbody></table>

Figure (red curve, a) compared to those retrieved by POLDER-3/GRASP, with an average bias of about –0.06 from visible to near-infrared. The spectral values of the SSA are also slightly underestimated in the WRF-Chem optimized configuration (red curve, b), with an average bias of about –0.02 over the entire spectrum, reflecting a slightly higher aerosol absorption than that retrieved by POLDER-3/GRASP. This difference is reduced at shorter wavelengths (average bias of –0.01 at 443 nm) due to the consideration of BrOC absorption (highly absorbing especially in ultraviolet-blue, Kirchstetter et al., 2004; Hoffer et al., 2006) in the WRF-Chem optimized configuration (2.5 % of BrOC).

Above clouds over the SEAO (0–15° E, 15–5° S), the spectral values of the ACAOD are slightly underestimated in

the WRF-Chem optimized configuration (red curve, c), with an average bias ranging from –0.04 to –0.02 from 490 to 865 nm compared to those retrieved by POLDER-3/AERO-AC. Regarding the spectral behaviour of the ACSSA, the WRF-Chem optimized configuration (red curve, d) simulates an upward trend from 300 to 600 nm due to the presence of BrOC in the BBA plumes and then a slightly decreasing trend in the near-infrared with increasing wavelength. However, the lack of data above clouds in the ultraviolet spectrum with POLDER-3/AERO-AC does not allow us to assess the reliability of the increase in absorption below 490 nm due to the addition of BrOC to the WRF-Chem optimized configuration. In the near-infrared, the decrease in ACSSA values is more pronounced in the POLDER-3/AERO-AC retrieval,

<footnote n="1">¹ $m_{BC,550}$ = 1.95 – 0.79(i) (Bond and Bergstrom, 2006). ² $m_{BC,550}$ = 1.75 – 1.03(i) (Williams et al., 2007).</footnote>

<footnote n="3">³ $m_{BC,550}$ = 1.86 – 0.25(i) (Hoffer et al., 2016, 2017).</footnote>
<figure><img src="image_17.png" /><figcaption>**Figure 14.** Spectral dependencies of AOD (a) and SSA (b) retrieved by POLDER-3/GRASP in clear sky (a, b, black curves) and by POLDER-3/AERO-AC above clouds (c, d, black curves) and simulated with the WRF-Chem optimized configuration (BC × 2, OC/2.5 with 2.5 % of BrOC, red curves). Black vertical error bars correspond to the uncertainties associated with POLDER-3 data with an accuracy of ±15 % (per pixel estimate) on the aerosol optical depth and ±0.05 % (per pixel estimate) on the single scattering albedo over the entire spectral domain. Values are averaged geographically on their respective study areas – (12–30° E, 10–0° S) over the southern African continent in clear sky and (0–15° E, 15–5° S) above clouds over the southeastern Atlantic Ocean – and temporally over the first half of July 2008.</figcaption></figure>

with a positive average bias of 0.03 at 865 nm between the WRF-Chem optimized configuration and the POLDER-3/AERO-AC retrieval. This difference could be due to the larger particle sizes simulated by WRF-Chem than those retrieved by POLDER-3 (see Sect. 3.2.3).

Figure 15 illustrates the averaged PM<sub>2.5</sub> chemical composition simulated with the WRF-Chem optimized configuration, including organic aerosols (OA, in green), secondary inorganic aerosols (SIA, in grey), organic carbon (OC, in brown), black carbon (BC, in black), brown carbon (BrOC, in purple), desert dust aerosols (DUST, in yellow), and sea salt aerosols (SEAS, in blue), as well as their relative proportions over the southern African continent in clear sky (spatial average over 12–30° E, 10–0° S, a) and above clouds over the SEAO (spatial average over 0–15° E, 15–5° S, b) for the first half of July 2008.

Figure 15 shows that the chemical composition of PM<sub>2.5</sub> simulated with the WRF-Chem optimized configuration still remains realistic in comparison with the observations from previous field campaigns (Haslett et al., 2019; Denjean et al., 2020): organic aerosols (OA, in green) still dominate, both at the BB sources (50.9 % of PM<sub>2.5</sub>, a) and over the transport region (55.6 % of PM<sub>2.5</sub>, b). Compared to the chemical composition of PM<sub>2.5</sub> simulated with the WRF-Chem PC configuration (see Fig. 12), the contribution of black carbon (BC, in black) in the BBA plumes is greater in our studied area (≥ 3.5 %). The contribution of organic carbon

(OC, brown hatching) is slightly lower: from 58.8 mg m<sup>-2</sup> (28.0 % of PM<sub>2.5</sub>) to 35.1 mg m<sup>-2</sup> (30.5 % of PM<sub>2.5</sub>) for the WRF-Chem optimized configuration and from 67.0 mg m<sup>-2</sup> (31.7 % of PM<sub>2.5</sub>) to 45.4 mg m<sup>-2</sup> (32.0 % of PM<sub>2.5</sub>) for the WRF-Chem PC configuration, between sources and transport areas. As with the WRF-Chem PC configuration, the influence of desert dust aerosols (DUST, in yellow) increases during the progression of the BBA plumes off the SEAO with a vertically integrated mass increasing on average from 7.7 mg m<sup>-2</sup> (3.7 % of PM<sub>2.5</sub>) to 9.6 mg m<sup>-2</sup> (8.4 % of PM<sub>2.5</sub>). The contribution of sea salt aerosols (SEAS, in blue) is negligible both over the southern African continent (0.2 % of PM<sub>2.5</sub>) and above clouds over the SEAO (0.9 % of PM<sub>2.5</sub>). Finally, the contribution of brown carbon (BrOC, in purple) is less than 1 % in our study area.

Figure 16 illustrates the spatial distributions of the monthly averaged AOD (a, b) and SSA (d, e) at 565 nm in clear sky retrieved by POLDER-3/GRASP (a, d) and simulated with the WRF-Chem optimized configuration (b, e) for July 2008.

Figure 16 shows that the results obtained with the WRF-Chem optimized configuration in clear sky are overall satisfying on average for July 2008. Over the southern African continent (12–30° E, 10–0° S), simulated mean AOD is 1.02 compared to 1.10 ± 0.22 at 565 nm for POLDER-3/GRASP, indicating a slight underestimation of the intensity of BBA emission sources in the WRF-Chem optimized configura-
<figure><img src="image_18.png" /></figure>

**Figure 15.** Evolution of the PM<sub>2.5</sub> chemical composition simulated with the WRF-Chem optimized configuration between the southern African continent in clear sky (12–30° E, 10–0° S, a) and the southeastern Atlantic Ocean above clouds (0–15° E, 15–5° S, b). Mass concentrations (in mg m<sup>-2</sup>) of the main aerosol compounds of biomass burning, i.e. black carbon (BC, in black), organic carbon (OC, in brown hatching), brown carbon (BrOC, in purple), organic aerosols (OA, in green), and secondary inorganic aerosols (SIA, in grey), as well as desert dust aerosols (DUST, in yellow) and sea salt aerosols (SEAS, in blue), are vertically integrated over the atmospheric column on average for the first half of July 2008.

<figure><img src="image_19.png" /></figure>

**Figure 16.** Comparison of monthly averaged AOD (a, b) and SSA (d, e) at 565 nm in clear sky retrieved by POLDER-3/GRASP (a, d) and simulated with the WRF-Chem optimized configuration (b, e) over the southeast Atlantic region for July 2008, with the associated histograms of differences between the model and the satellite observations over the whole domain (c, f). The black frames (12–30° E, 10–0° S) represent the area of study.

tion. Their location is also somewhat different to the simulated emission sources located further west than those observed by POLDER-3/GRASP, resulting in a spatial correlation coefficient of 0.50 and an average bias of -0.08 at 565 nm. The simulated mean SSA is 0.81 compared to 0.85 ± 0.05 at 565 nm for POLDER-3/GRASP, showing a good agreement although the aerosol absorption is slightly overestimated in the WRF-Chem optimized configuration. Figure 16 also shows that the aerosol absorption is more uni-

form in the WRF-Chem optimized configuration in comparison to POLDER-3/GRASP, which retrieves more scattering aerosols north of 12–30° E, 5–0° S. In this area, a contribution of other aerosol species to the BB plume is not excluded (mixture with desert dust aerosols) and could explain why POLDER-3 retrieves higher SSA than the model. This difference translates into a spatial correlation coefficient of 0.59 and an average bias of -0.04 at 565 nm. We can note that the mean SSA simulated with the WRF-Chem optimized config-
uration at the Mongu, Zambia, site (about 0.83 at 565 nm) in clear sky in July 2008 is consistent with the one retrieved by AERONET (about 0.81 at 550 nm) at the same location during July 1997 to 2005 (Eck et al., 2013). Over the SEAO far from the continent, in situ measurements from LASIC (Zuidema et al., 2018b) and CLARIFY-2017 (Taylor et al., 2020) indicated a strong BBA absorption, consistent with the observations from POLDER-3/GRASP (mean SSA less than 0.80 at 565 nm). This may be due to coating and lens effects of BC, which appear to be important for very old BBA plumes transported off the coast of southern Africa (Zuidema et al., 2018b; Denjean et al., 2020; Taylor et al., 2020; Wu et al., 2020). We remind that we do not consider coating in our approach and that, over this area, large discrepancies remain between POLDER-3 and the WRF-Chem optimized configuration.

Figure 17 illustrates the spatial distributions of monthly averaged ACAOD (a, b) and ACSSA (d, e) at 550 nm retrieved by POLDER-3/AERO-AC (a, d) and simulated with the WRF-Chem optimized configuration (b, e) for July 2008.

Figure 17 shows a very good agreement between the WRF-Chem optimized configuration and the POLDER-3/AERO-AC retrievals on the spatial distributions of both the ACAOD and the ACSSA at 550 nm averaged over July 2008. The simulated mean ACAOD is 0.48 compared to $0.46 \pm 0.09$ at 550 nm for POLDER-3/AERO-AC, indicating a good estimate of the amounts of aerosols transported above clouds over the SEAO. Few minor differences can be observed within the studied area (0–15° E, 15–5° S), resulting in a spatial correlation coefficient of 0.64 and an average bias of 0.02 at 550 nm. The simulated mean ACSSA is 0.84 compared to $0.85 \pm 0.05$ at 550 nm for POLDER-3/AERO-AC, indicating a good estimate of the aerosol absorption in the WRF-Chem optimized configuration. Some small differences can be observed within the studied area (0–15° E, 15–5° S), leading to a spatial correlation coefficient of 0.66, an average absolute error of only 0.01 and an average quadratic error of only 0.02.

In summary, the BBA absorption properties are significantly improved with the WRF-Chem optimized configuration while maintaining a realistic content of aerosols transported above marine stratocumulus. Thus, the WRF-Chem optimized configuration correctly simulates the content of BBA and their absorption properties over the SEA region on average for July 2008. In particular, the simulated mean SSA is consistent with the mean value of $0.85 \pm 0.02$ observed during SAFARI-2000, although not fully representative of the same period of the BB season (Leahy et al., 2007).

# 4 Conclusions and perspectives

This study shows that the WRF-Chem regional meteorological model coupled with chemistry combined with innovative POLDER-3 satellite aerosol inversion algorithms provided

a satisfying estimate of the load and absorption properties of BBA over the SEA region, both in clear sky and above clouds on average for July 2008.

The adjustment of the chemistry at the source level in the WRF-Chem optimized configuration (BC × 2, OC/2.5 with 2.5% BrOC) is consistent with the uncertainties present in APIFLAMEv1 BB emission inventory (Turquety et al., 2014) used in our study. This aerosol chemical composition is obtained with the homogeneous internal mixing state. The mean BC/OC mass mixing ratio simulated with this optimal scenario of WRF-Chem is estimated at 0.15 over the southern African continent and 0.11 above clouds over the SEAO. These values are also in good agreement with previous in situ measurements over this region, such as the SAFARI-2000 airborne campaign (Formenti et al., 2003). In addition, the absorbing fraction of OA in the BBA plumes, i.e. BrOC, is estimated at 2%–3% for the studied period. This value could vary geographically and temporally. Importantly, this BrOC contribution allows the increase in absorption retrieved by POLDER-3/GRASP at the shortest wavelengths of the visible spectrum, characteristic of the presence of BrOC in the BBA plumes, to be well simulated with WRF-Chem over the BB source areas. However, the lack of available POLDER-3 data for the SSA in the blue and in the ultraviolet spectrum above clouds did not enable us to constrain with certainty the BrOC content in cases of BBA plumes transported over stratocumulus off the coasts of Namibia and Angola. This limitation is mainly related to the used inversion algorithm and may be exceeded in future work. The simulated mean SSA are 0.81 (565 nm) and 0.84 (550 nm) in clear and above cloudy scenes respectively, in good agreement with those retrieved by POLDER-3 ($0.85 \pm 0.05$ at 565 nm in clear sky and at 550 nm above clouds) for the studied period. Significant differences between modelled and measured SSA are only observed in remote ocean areas, at least 2000 km from the sources. These differences could be explained by the hypothesis of the homogeneous internal mixture that we used in our study.

Our results highlight the fact that BC refractive index of Williams et al. (2007), which is more absorbing than that more commonly used of Bond and Bergstrom (2006), provides the best estimates of BBA properties, allowing us to reproduce the retrievals from the POLDER-3 satellite both in clear and cloudy skies. Other studies have shown that the Williams et al. (2007) BC refractive index was more suitable for the assessment of the mass absorption cross section ($MAC_{BC,fresh} = 7.5 \pm 1.2 \text{ m}^2 \text{ g}^{-1}$) associated with freshly emitted BC. In this sense, our work is consistent with the conclusions of the study on the light absorption properties of BC from Liu et al. (2020).

The methodology developed during this study can be summarized as follows: using optimized regional simulations to constrain the emission factors of big families of chemical species present in BB inventories through the adjustment of the chemistry. This adjustment of the chemistry is made pos-
<figure><img src="image_20.png" /><figcaption>**Figure 17.** Comparison of monthly averaged ACAOD (a, b) and ACSSA (d, e) at 550 nm above clouds retrieved by POLDER-3/AERO-AC (a, d) and simulated with the WRF-Chem optimized configuration (b, e) over the southeast Atlantic region for July 2008, with the associated histograms of differences between the model and the satellite observations over the whole domain (c, f). The black frames (0–15° E, 15–5° S) represent the area of study.</figcaption></figure>

sible by the use of new satellite observations providing the SSA of aerosols and its spectral dependence from space both in clear and cloudy skies. These recently available new observations used in synergy with a regional model of meteorology coupled with chemistry, such as WRF-Chem, enable us to obtain new constraints on the aerosol chemistry in climate modelling exercises.

Our results can be considered the first step of a larger study, which aims at providing more robust estimates of the climate impacts of BBA over the SEA region, including their interactions with clouds, using the optimized configuration of the WRF-Chem model. In particular, the influence of BrOC absorption on direct and semi-direct radiative effects of aerosols will be investigated. In addition, clouds’ response to contact with BBA plumes will be assessed at the indirect effects level.

In parallel, the methodology developed in this study could be applied throughout the summer 2008 dry season to evaluate the temporal variability and absorption cycle of BBA present in this region. First, results show that the WRF-Chem optimized configuration struggles to represent very satisfyingly the seasonal cycle of ACSSA retrieved by POLDER-3/AERO-AC, which is characterized by a decreased aerosol absorption (increase in ACSSA values) during the advance of the fire season. This suggests that the chemical composition of the BBA plumes, and especially the amount of carbonaceous aerosols emitted in the atmosphere, changes during the

dry season, which is likely in relation to a change in the type of fuel burned and in the combustion conditions (Zuidema et al., 2016b, 2018b; Pan et al., 2019; Pistone et al., 2019). Thus, an interesting development would be the elaboration of a parameterization of the BrOC content in WRF-Chem according to the evolution of fire activity during the dry season. To progress on this aspect, a synergy between satellite observations provided by the POLDER-3 and the Ozone Monitoring Instrument (OMI) space sensors would allow us to expand the retrieval of the SSA of aerosols to the ultraviolet range, a spectral domain particularly sensitive to the presence of BrOC.

Another outlook will consist in applying our methodology to the more recent French AEROCLO-sA airborne campaign that took place in the SEA region in August–September 2017, using other satellite datasets than POLDER-3, for which observations ended in 2013. Other international measurement campaigns have also taken place in this region (CLARIFY, LASIC and ORACLES) in recent years (Zuidema et al., 2016b). They will provide detailed reference observations on the BBA properties bringing additional constraints on their radiative and climate effects.

Finally, the methodology combining regional simulations and satellite observations of aerosols could be applied to other regions under the influence of BB, such as those located in the Northern Hemisphere or South America, particularly in the Amazon. Boreal forest fires are of interest because they
are characterized by a very low carbonaceous mass mixing ratio and a slow combustion without flames. This type of fire is thus potentially richer in organic aerosols, making it a potentially important contributor of BrOC. For this type of plume, BrOC concentrations could therefore be much higher than for the BBA plumes observed over the SEA region, implying a potentially more pronounced BrOC effect on climate for these regions.

## Appendix A: Description of the statistical parameters

The Pearson correlation coefficient (R) is calculated as follows:

$$R = \frac{\sum_{i=1}^{N} (M_i - \bar{M})(O_i - \bar{O})}{\sqrt{\sum_{i=1}^{N} (M_i - \bar{M})^2 \sum_{i=1}^{N} (O_i - \bar{O})^2}} \quad (A1)$$

where $M_i$, $O_i$, $\bar{M}$, $\bar{O}$, and N are respectively the simulated value, the observed value, the average of the simulated and observed values, and the total number of pixels. R is between -1 and +1, with a value tending towards zero indicating no linear correlation.

The mean bias (MB) is the average of the difference between a simulated and an observed value over an area or over a specified period:

$$MB = \frac{\sum_{i=1}^{N} (M_i - O_i)}{N} \quad (A2)$$

If the difference between the simulated value and the observed value is non-zero then the simulated value is said to be biased positively in the case of overestimation and negatively otherwise.

The mean absolute error (MAE) is calculated from the absolute value of the difference between a simulated and an observed value:

$$MAE = \frac{\sum_{i=1}^{N} |M_i - O_i|}{N} \quad (A3)$$

This quantity is therefore always positive and tends towards zero when the simulated values are close to those observed. This statistical parameter is more restrictive than the average bias because it avoids possible error compensations.

The root mean square error (RMSE) is calculated from the square root of the root mean square difference between the simulated and observed values:

$$RMSE = \sqrt{\frac{\sum_{i=1}^{N} (M_i - O_i)^2}{N}} \quad (A4)$$

Occasional large biases can produce a high RMSE value. This statistical parameter is therefore commonly used as a measure of the overall performance of a model.

**Data availability.** The AERO-AC product is developed at the ICARE data and services centre (https://www.icare.univ-lille.fr, last access: 30 November 2021) in Lille (France) in the frame of the POLDER/PARASOL mission and supported by the Centre National d'Etudes Spatiales and the Programme National de Télédétection Spatiale (CNES and PNTS; https://doi.org/10.25326/82, Waquet et al., 2020). The authors would like to acknowledge the use of POLDER/PARASOL Level-1 data originally provided by CNES (http://www.icare.univ-lille1.fr/, last access: 30 November 2021) processed at Laboratoire d'Optique Atmosphérique with GRASP software (https://www.grasp-open.com, last access: 30 November 2021) (Grasp Open, 2021) developed by Dubovik et al. (2011, 2014).

**Author contributions.** AS, FW, JCP and IC developed the concept of this paper. AS performed the WRF-Chem simulations and carried out the analyses of the POLDER and CALIOP data. ST developed the APIFLAME biomass burning emission inventory. FW and FP developed the POLDER-3/AERO-AC products, and the data were processed by FT and FD. AS wrote the manuscript with contributions from all co-authors.

**Competing interests.** The authors declare that they have no conflict of interest.

**Disclaimer.** Publisher's note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.

**Special issue statement.** This article is part of the special issue "New observations and related modelling studies of the aerosol–cloud–climate system in the Southeast Atlantic and southern Africa regions (ACP/AMT inter-journal SI)". It is not associated with a conference.

**Acknowledgements.** This work has been supported by the CaPPA (Chemical and Physical Properties of the Atmosphere) project, which is funded by the French National Research Agency (ANR) through the Programme d'Investissement d'Avenir (PIA) under contract R-LABEX0-20-007-CAPPA and by the Regional Council of Hauts-de-France and the European Regional Development Fund (ERDF); the University of Lille (France); the Programme National de Télédétection Spatiale (PNTS, https://programmes.insu.cnrs.fr/transverse/pnts, last access: 30 November 2021, grant no. PNTS-2013-10); and by the French Centre National d'Etudes Spatiales (CNES). The authors also thank the Hauts-de-France region, the Ministère de l'Enseignement Supérieur et de la Recherche (CPER Climibio), and the ERDF for their financial support. The authors acknowledge the AEROCLIM project of comparison of models and satellite data for climate studies, which is funded by CNES. The authors are also grateful to Oleg Dubovik and Pavel Litvinov for providing the GRASP data and their validation against AERONET data used in this study. The authors would like to thank the AEROCLO-sA team and project. The AEROCLO-sA
project was supported by the ANR under grant agreement no. ANR-15-CE01-0014-01, the French national programme LEFE/INSU, the PNTS (grant no. PNTS-2016-14), and by the South African National Research Foundation (NRF) under grant UID 105958.

*Financial support.* This work was mainly funded by the CaPPA (Chemical and Physical Properties of the Atmosphere) project, which is funded by the French National Research Agency (ANR) through the Programme d'Investissement d'Avenir (PIA) under contract R-LABEX0-20-007-CAPPA and by the Regional Council of Hauts-de-France and the European Regional Development Fund (ERDF); the University of Lille (France); the Programme National de Télédétection Spatiale (PNTS) under grant no. PNTS-2013-10; and by the French Centre National d'Etudes Spatiales (CNES).

*Review statement.* This paper was edited by Paquita Zuidema and reviewed by three anonymous referees.

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