Important role of stratospheric injection height for the distribution and radiative forcing of smoke aerosol from the 2019–2020 Australian wildfires

Abstract

More than 1 Tg smoke aerosol was emitted into the atmosphere by the exceptional 2019–2020 southeastern Australian wildfires. Triggered by the extreme fire heat, several deep pyroconvective events carried the smoke directly into the stratosphere. Once there, smoke aerosol remained airborne considerably longer than in lower atmospheric layers. The thick plumes traveled eastward, thereby being distributed across the high and mid-latitudes in the Southern Hemisphere, enhancing the atmospheric opacity. Due to the increased atmospheric lifetime of the smoke plume, its radiative effect increased compared to smoke that remains in lower altitudes. Global models describing aerosol-climate impacts lack adequate descriptions of the emission height of aerosols from intense wildfires. Here, we demonstrate, by a combination of aerosol-climate modeling and lidar observations, the importance of the representation of those high-altitude fire smoke layers for estimating the atmospheric energy budget. Through observation-based input into the simulations, the Australian wildfire emissions by pyroconvection are explicitly prescribed to the lower stratosphere in different scenarios. Based on our simulations, the 2019–2020 Australian fires caused a significant top-of-atmosphere (TOA) hemispheric instantaneous direct radiative forcing signal that reached a magnitude comparable to the radiative forcing induced by anthropogenic absorbing aerosol. Up to $+$0.50 $\mathrm{W}{\mathrm{m}}^{-\mathrm{2}}$ instantaneous direct radiative forcing was modeled at TOA, averaged for the Southern Hemisphere ($+$0.25 $\mathrm{W}{\mathrm{m}}^{-\mathrm{2}}$ globally) from January to March 2020 under all-sky conditions. At the surface, on the other hand, an instantaneous solar radiative forcing of up to $-$0.81 $\mathrm{W}{\mathrm{m}}^{-\mathrm{2}}$ was found for clear-sky conditions, with the respective estimates depending on the model configuration and subject to the model uncertainties in the smoke optical properties. Since extreme wildfires are expected to occur more frequently in the rapidly changing climate, our findings suggest that high-altitude wildfire plumes must be adequately considered in climate projections in order to obtain reasonable estimates of atmospheric energy budget changes.

1 Introduction

During the record 2019–2020 Australian wildfire season, the aerosol load increased substantially over large parts of mid and high latitudes in the Southern Hemisphere due to the massive amounts of smoke aerosol injected into the stratosphere. The austral summer of 2019–2020 is remembered as Australia's Black Summer because of the unprecedented intensity and scale of wildfires. The devastating impact on local nature and life was particularly evident in the significant destruction of habitat for hundreds of endemic species (Ward et al., 2020; Wintle et al., 2020). In addition, the interactions of the fire plume with large-scale weather (Kablick et al., 2020; Khaykin et al., 2020) also make the Black Summer fires a distinct example for studying the climate impacts of stratospheric smoke injection.

Between September 2019 and January 2020, almost twice the area burned compared to any previous extreme fire on record in Australia, emitting unprecedented amounts of smoke aerosol (Boer et al., 2020; Morgan et al., 2020) (Fig. 1a). Peaking between 29 December 2019 and 4 January 2020, the fires caused a significant input of aerosol into the stratosphere. Several intense pyroconvective towers carried this aerosol directly up to a height of 14–16 km in the lower stratosphere (Kablick et al., 2020; Ohneiser et al., 2020; Boone et al., 2020). The mass of smoke emitted into the stratosphere by these fires has been estimated to range from 0.6 Tg (Khaykin et al., 2020) to 2.1 Tg (Hirsch and Koren, 2021). In a slightly later publication, Peterson et al. (2021) estimate that the stratospheric injection of Australian smoke amounts to 0.2–0.8 Tg in a first phase of massive pyroconvective activity from 29 to 31 December 2019 and 0.1–0.3 Tg in the second phase on 4 January 2020. Within days, the smoke was distributed zonally across the southern mid- and high latitudes, according to satellite measurements by NASA's Moderate Resolution Imaging Spectroradiometer (MODIS) (Hirsch and Koren, 2021), Cloud-Aerosol Lidar and Infrared Pathfinder Satellite Observations (CALIPSO) data (Kablick et al., 2020) as well as observations from the Stratospheric Aerosol and Gas Experiment (SAGE) III and TROPOspheric Monitoring Instrument (TROPOMI) (Khaykin et al., 2020). Furthermore, ground-based lidar measurements at the southern tip of South America also clearly showed the elevated smoke layer (Ohneiser et al., 2020). As a result, atmospheric opacity in the Southern Hemisphere was considerably enhanced. Between the latitudes of 20–60${}^{\circ }$ S, the total column aerosol optical thickness (AOT) at 630 nm wavelength increased to 0.16 on average in January 2020, a 51 % deviation from the long-term mean, as shown for example by the observations of the Advanced Very High Resolution Radiometer (AVHRR) satellite instrument. Figure 1b shows the hemispheric dispersal of the Australian wildfire smoke in January 2020 in terms of the AVHRR AOT anomaly.

Figure 1

(a) Biomass burning plumes in the Canberra region of southeastern Australia as seen from NASA's Aqua satellite on 4 January 2020 (NASA Earth Observatory image by Joshua Stevens, using MODIS data from NASA EOSDIS/LANCE and GIBS/Worldview, https://earthobservatory.nasa.gov, last access: 1 April 2020). Overlaid is a ranking of carbon aerosol emissions accumulated for the annual southeastern Australian bushfire seasons (September–March) based on Global Fire Assimilation System (GFAS) data (Kaiser et al., 2012). (b) Anomaly in monthly mean aerosol optical thickness (AOT) at 630 nm for January 2020 (by remapping to $\mathrm{1}{}^{\circ }\times \mathrm{1}{}^{\circ }$, pixels with less than 300 valid retrievals at 0.1${}^{\circ }$ original resolution are excluded, see further details in Sect. 2.3) compared to the long-term January mean (1982–2019), as observed by NOAA's AVHRR instrument (Zhao and NOAA CDR Program, 2017) (missing data shown in white, continents in gray).

[Figure omitted. See PDF]

Satellite observations and global aerosol-climate model results show that this had significant effects on the radiation budget (Khaykin et al., 2020; Hirsch and Koren, 2021; Yu et al., 2021; Sellitto et al., 2022). For the stratospheric smoke from the Australian wildfires, Khaykin et al. (2020) found a cloud-free solar radiative forcing of about $-$1.0 $\mathrm{W}{\mathrm{m}}^{-\mathrm{2}}$ at the top of the atmosphere (TOA) and $-$3.0 $\mathrm{W}{\mathrm{m}}^{-\mathrm{2}}$ at the surface on average for the latitudes of 25–60${}^{\circ }$ S in February 2020, based on radiative transfer modeling using aerosol extinction profiles from NASA's Ozone Mapping and Profiler Suite Limb Profiler (OMPS-LP). Building on the method by Khaykin et al. (2020), Sellitto et al. (2022) recently provided updated estimates and conducted sensitivity analyses to examine the effects of assumed aerosol optical properties. Their best estimate for the global equivalent of cloud-free solar radiative forcing in February 2020 is $-$0.35 $\mathrm{W}{\mathrm{m}}^{-\mathrm{2}}$ at TOA and $-$0.94 $\mathrm{W}{\mathrm{m}}^{-\mathrm{2}}$ at surface, and reaches up to $-$2.0 and $-$4.5 $\mathrm{W}{\mathrm{m}}^{-\mathrm{2}}$, respectively, for the 25–60${}^{\circ }$ S latitude band, using optical properties characteristic of aged biomass burning aerosol. Assuming highly reflective underlying surfaces as approximation for clouds and highly absorbing particles, in contrast, they calculated a global equivalent of TOA forcing as high as $+$1.0 $\mathrm{W}{\mathrm{m}}^{-\mathrm{2}}$. Hirsch and Koren (2021) derived an enhancement for outgoing solar radiation of 1.1 $\mathrm{W}{\mathrm{m}}^{-\mathrm{2}}$ (i.e., negative forcing) in the latitude belt between 20–60${}^{\circ }$ S for January to March, from NASA's Clouds and the Earth's Radiant Energy System (CERES) satellite data. From model results and also considering the fast adjustment from stratospheric warming, Yu et al. (2021) obtained an estimate for global annual average clear-sky effective radiative forcing of $-$0.03 $\mathrm{W}{\mathrm{m}}^{-\mathrm{2}}$ at TOA and $-$0.32 $\mathrm{W}{\mathrm{m}}^{-\mathrm{2}}$ at the surface due to the smoke event.

Australia's Black Summer is among a recent series of extreme wildfires that has renewed scientific attention, particularly to wildfires with strong fire-induced convection and self-lifting. These include recent record fires in the western United States and Canada (2017, 2018), Siberia (2019, 2020) and the eastern Mediterranean (2021). Triggered by the intense fire heat, the pyroconvection can grow to pyrocumulonimbus (pyroCb) clouds which are the primary pathway of smoke injection into the upper troposphere and lower stratosphere (Fromm et al., 2010, 2019). Radiation-induced self-lifting has the potential to cause smoke plumes to continue rising (Boers et al., 2010). Also due to such events, biomass burning smoke contributes considerably to the global aerosol composition, affecting the Earth's energy balance through aerosol–radiation and tropospheric aerosol–cloud interactions (Bowman et al., 2009; Streets et al., 2009; Boucher et al., 2013). Such extreme wildfires and associated deep pyroconvection can have effects similar to volcanic eruptions in terms of stratospheric aerosol injection and radiative impact (Peterson et al., 2018). An important component is black carbon (BC) aerosol, which is among the strongest warming short-lived radiative forcing agents (Bond et al., 2013; Lund et al., 2020; Thornhill et al., 2021). In addition, less-absorbing organic carbon (OC), precursors for sulfate and other secondary aerosols are emitted. Depending on its optical properties and the underlying surface reflectivity, the climate impact of biomass burning aerosol can vary regionally (Jiang et al., 2016; Bellouin et al., 2020; Brown et al., 2021) and also strongly depends on the altitude of the aerosol layer (Ban-Weiss et al., 2012). During strong pyroCb events, radiative effects can be enhanced due to the long stratospheric lifetime of aerosol. While the high-altitude injection of wildfire plumes is yet insufficiently represented in aerosol-climate models (Paugam et al., 2016), the recent series of extreme wildfires and their potentially increased occurrence with climate change (Jolly et al., 2015; Abatzoglou et al., 2019; Dowdy et al., 2019; Kirchmeier-Young et al., 2019) calls for greater attention in global climate modeling.

In order to clarify the role of smoke injection of wildfire pyroconvection in the aerosol-climate modeling context, here we use the aerosol-climate model ECHAM6.3-HAM2.3 (Zhang et al., 2012; Tegen et al., 2019). Specifically, we aim to show the importance of considering these extreme fire events in determining the global energy budget, although they are not adequately reflected in today's climate simulations. The fire emission fluxes in the model are prescribed from the Global Fire Assimilation System (GFAS; Kaiser et al., 2012), and the injection height of Australian fire smoke is set to the tropopause level for the known pyroCb events and varied accordingly in sensitivity experiments. The modeled transport patterns are evaluated with active and passive ground-based and spaceborne remote sensing, providing the basis for analyzing the radiative impact of the carbonaceous smoke aerosol. Finally, we discuss implications and perspectives for climate models to address the extreme wildfires and their effects in a changing climate.

2 Observations and modeling

The analysis of the 2019–2020 Australian fire season in this study is based on global aerosol-climate simulations. An important part of the modeling is concerned with finding a configuration that best represents the pyroconvective fires. Since the typical horizontal resolution of global climate models (GCMs) is too coarse to explicitly resolve convection, observed pyroCb events are explicitly prescribed and the injection height of the wildfire plume is varied in terms of sensitivity experiments. Their results are compared to the original settings for biomass burning emissions as well as evaluated with ground-based and spaceborne remote-sensing observations to show how realistically these can be represented if the injection heights for pyroCbs are considered accordingly. The model results are then used to investigate the impact of pyroconvective smoke injection on plume transport and radiative effects for January–March 2020.

2.1 AERONET sun-photometer measurements

Information on column aerosol properties, including AOT at specific wavelengths and corresponding information on effective aerosol size, are available from quality-controlled measurements by the global sun-photometer network, AErosol RObotic NETwork (AERONET; Holben et al., 1998; Giles et al., 2019; http://aeronet.gsfc.nasa.gov, last access: 10 October 2021). These data are widely used for aerosol studies including evaluation of aerosol model results. In this study we use level 1.5 or, where available, level 2 cloud-screened, 6 h averages of AOT measurements. The AERONET AOT values at 550 nm are extrapolated from the measured values at 500 nm making use of the Angstrom exponent for each observation, which in turn is computed from the ratio of observed AOT values at 500 and 675 nm, respectively. The AOT measurements are compared to model results by linearly interpolating model values to the times and locations of the measurements of the respective AERONET stations: Punta Arenas, Chile (53.14${}^{\circ }$ S, 70.89${}^{\circ }$ W), Amsterdam Island (37.80${}^{\circ }$ S, 77.57${}^{\circ }$ E), Marambio (64.24${}^{\circ }$ S, 56.63${}^{\circ }$ W), Vechernaya Hill (67.66${}^{\circ }$ S, 46.16${}^{\circ }$ E) and South Pole (90.00${}^{\circ }$ S, 70.30${}^{\circ }$ E).

2.2 Ground-based lidar remote sensing

The lidar observations at Punta Arenas (53.14${}^{\circ }$ S, 70.89${}^{\circ }$ W; 9 m above sea level), Chile, were conducted in the framework of the long-term campaign Dynamics, Aerosol, Cloud And Precipitation Observations in the Pristine Environment of the Southern Ocean(DACAPO-PESO; https://dacapo.tropos.de, last access: 5 October 2021). The main goal of DACAPO-PESO is the investigation of aerosol–cloud interaction processes in rather pristine, unpolluted marine conditions (Radenz et al., 2021). The Polly instrument (POrtabLle Lidar sYstem; Engelmann et al., 2016) was operated at the University of Magallanes (UMAG) at Punta Arenas from November 2018 until October 2021. The lidar has 13 channels and continuously measures elastic and Raman backscatter signals at the laser wavelengths of 355, 532 and 1064 nm with respective Raman backscattering wavelengths of 387 and 607 nm for nitrogen Raman scattering and 407 nm for water vapor Raman scattering (Baars et al., 2016, 2019). At the laser wavelengths of 355 and 532 nm, particle extinction coefficients, the respective extinction-to-backscatter ratio (i.e., lidar ratio) and the linear depolarization ratio are determined. Moreover, vertical profiles of the particle backscatter coefficient can be derived at these wavelengths and, additionally, at 1064 nm. The mixing ratio of water vapor to dry air is obtained from measurements in UV. Auxiliary meteorological data, in particular temperature and pressure profiles, are required in the lidar data analysis in order to calculate and correct atmospheric molecular backscatter and extinction. To this end, the Global Data Assimilation System 1 (GDAS1) temperature and pressure profiles with 1${}^{\circ }$ horizontal resolution were used from the National Weather Service's National Center for Environmental Prediction (GDAS, 2020). In addition, values for single scattering albedo (SSA) at 355 and 532 nm were retrieved from the Polly multi-wavelength backscatter and extinction profiles on 26 January 2020 by using the Veselovskii et al. (2002) lidar data inversion (Ohneiser et al., 2022).

2.3 Spaceborne remote sensing

2.3.1 AVHRR aerosol optical thickness

Observations with AVHRR on board the National Oceanic and Atmospheric Administration's (NOAA) operational satellites are available for almost 4 decades. For the present study, we use version 3 of the AVHRR AOT product (Zhao and NOAA CDR Program, 2017). It provides daily mean AOT at 630 nm for cloud-free pixels over non-glint water surfaces with a horizontal resolution of 0.1${}^{\circ }$. The uncertainty of a single AOT retrieval is 0.2. Because of clouds obscuring the view, there are no valid retrievals and consequently no daily averages for every pixel on every day. For the illustration of the hemispherical spread of Australian wildfire smoke in Fig. 1b, showing the observed AOT anomaly of January 2020, the original $\mathrm{0.1}{}^{\circ }\times \mathrm{0.1}{}^{\circ }$ AVHRR data are compiled onto a grid with a spatial resolution of $\mathrm{1}{}^{\circ }\times \mathrm{1}{}^{\circ }$ to account for sufficient samples in the temporal mean.

The long-term mean for January from 1982 to 2019 is calculated by averaging in space and time over all pixels in the $\mathrm{1}{}^{\circ }\times \mathrm{1}{}^{\circ }$ cells. The averaging for January 2020 is performed analogously. However, due to the sparseness of the observations in a single month, $\mathrm{1}{}^{\circ }\times \mathrm{1}{}^{\circ }$ averaging boxes with less than 300 valid retrievals in January 2020 (i.e., approx. 10 % of the 100 potentially available data points per day are not considered here). In particular, at high latitudes, data coverage is sparse due to the low angle of the sun and high cloud cover.

2.3.2 CALIOP space-based lidar observations

Lidar observations from the Cloud–Aerosol Lidar with Orthogonal Polarization (CALIOP, Winker et al., 2013) instrument are used to retrieve the extinction coefficient at 532 and 1064 nm. We use the level-2 version 4 aerosol profile product, which is averaged over 5 km horizontal segments along the near nadir-view ground track (05kmAPro product). The cloud–aerosol discrimination (CAD) score is used to include only those columns in which at least one aerosol retrieval was successfully performed, using a threshold of $<-\mathrm{20}$ CAD scores. This level of quality screening is the same as that described in Winker et al. (2013). However, despite the use of the highest quality data, CALIOP is known for frequently failing to detect thin aerosol layers in the upper troposphere and lower stratosphere (Watson-Parris et al., 2018; Liu et al., 2019). The CALIOP level-2 aerosol classification selection algorithm defines six aerosol types: clean marine, dust, polluted continental, clean continental, polluted dust, and smoke which is based on the extinction-to-backscatter ratio (i.e., lidar ratio). Comparisons of the CALIOP backscatter with airborne measurements using a High Spectral Resolution Lidar (HSRL), conducted during the ObseRvations of Aerosols above CLouds and their intEractionS (ORACLES) campaign, independently demonstrated the lack of detection of these aerosol types using the CALIOP, and as such, have carried out the necessary steps to account for these biases as discussed in detail in Watson-Parris et al. (2018). As a result of its low sensitivity, the mean fraction of aerosol detected by CALIOP is globally up to 44 % lower than the aerosol-climate model ECHAM-HAM (Watson-Parris et al., 2018). Despite this bias, the substantial increase in aerosols resulting from the Australian wildfires is evidently detected by CALIOP. While sampling and detection biases occur on individual profiles, the trends in the extinction profiles offer valuable constraints for the ECHAM-HAM model.

2.4 Aerosol-climate simulations

2.4.1 Model description and setup

The simulations for this study were made with the global state-of-the-art aerosol-climate model ECHAM6.3-HAM2.3 (Tegen et al., 2019). This model uses the aerosol microphysics model M7 (Vignati et al., 2004) to predict the evolution of BC, OC, sulfate, sea salt and mineral dust. The mass and number concentrations of the aerosols are influenced by emission, loss processes, particle microphysics and atmospheric chemistry. The aerosol particles can interact with radiation and clouds. Atmospheric radiative transfer in ECHAM6.3 is computed using the PSrad/RRTMG (Rapid Radiative Transfer Model for GCMs; Iacono et al., 2008; Pincus and Stevens, 2013) radiation package, which considers 16 short and 14 long wavelength bands, respectively, as well as relevant atmospheric compounds. Aerosol optical properties are dynamically computed in the model depending on chemical composition and particle size. For each aerosol mode, the Mie-scattering parameter and the volume-averaged refractive indices are derived, assuming internal mixing, and are mapped to pre-calculated values of extinction cross section, SSA, and the asymmetry parameter from a look-up table. For analyzing the instantaneous direct aerosol radiative forcing, a double call to the radiation scheme exists to exclude atmospheric adjustments in the diagnostic.

Anthropogenic and biomass burning emissions of aerosols are prescribed. Daily data from GFAS (Kaiser et al., 2012) based on fire radiative power observations by the MODIS instruments on board NASA's Terra and Aqua satellites are used for the biomass burning related aerosol emissions of BC, OC, sulfate and dimethyl sulfide. In its original version, 75 % of the biomass burning aerosol mass is injected in the planetary boundary layer (PBL), 17 % in the first layer above the PBL and 8 % in the second layer above the PBL. A more suitable representation of the smoke injection height for this extreme wildfire event is explored in a series of sensitivity experiments. In these simulations, Australian smoke aerosol is directly emitted into the tropopause region in different configurations for known days of pyroconvective activity, as described in Sect. 2.4.2.

The ECHAM6.3-HAM2.3 simulations were performed for the November 2019 to March 2020 time period, using T63 horizontal resolution (approximately $\mathrm{1.875}{}^{\circ }\times \mathrm{1.875}{}^{\circ }$). In the vertical coordinate, the model is set up with 47 levels of increasing layer thickness from the ground to 0.01 hPa ($\sim$ 80 km). The vertical resolution ranges from approximately 70 m at surface to 500 m at 2.5 km and 1100 m at 15 km height, and coarsens accordingly thereafter. The dynamics in all simulations were nudged towards ECMWF ERA5 reanalysis data (Hersbach et al., 2020). Sea surface temperatures and sea-ice concentrations were prescribed as lower boundary conditions using Atmospheric Model Intercomparison Project (AMIP) data (Giorgetta et al., 2012). Concentrations of long-lived greenhouse gases were specified following the Representative Concentration Pathway (RCP) 4.5 scenario. Output was written every 6 h. The simulated aerosol properties include AOT at 550 nm and vertical profiles of aerosol extinction at 532 nm wavelength from the online lidar simulator, implemented specifically for comparisons with CALIOP and ground-based lidar measurements.

2.4.2 Sensitivity experiments on wildfire smoke injection

Wildfire injection heights are usually parameterized in coarser-scale models by schemes of various complexity (Paugam et al., 2016), but these do not necessarily represent the deep pyroconvection that is observed during very intense wildfires (Remy et al., 2017; Haarig et al., 2018; Ohneiser et al., 2020). In order to reconstruct the elevated smoke injection due to pyroconvection, and to explore the impacts on plume transport and climate radiative effects of the 2019–2020 Australian fire plume, we adapted the high-altitude smoke injection height by pyroconvection for 29–31 December 2019 and 4 January 2020 (pyroCb days) in the model, on which strong pyroconvective activities were reported in the southeastern Australian region affected by the fire (Kablick et al., 2020). Since no direct information was available on the actual pyroconvective injection heights, these were varied in the model in sensitivity experiments and verified with the range of above-mentioned remote-sensing observations, in particular with the lidar measurements over Punta Arenas in Chile.

The Australian fire emissions in the model, based on the GFAS inventory, are 0.6 and 0.2 Tg for the two pyroconvective phases, 29–31 December 2019 and 4 January 2020, respectively, with a BC to total carbon ($\text{BC}/(\text{BC}+\text{OC})$) ratio in the fire emissions of about 0.06–0.07. These emission values agree well with the previously mentioned estimates by Peterson et al. (2021) and are kept unchanged throughout the sensitivity experiments. For the 4 pyroCb days (29–31 December 2019 and 4 January 2020), the smoke injection from southeastern Australia was set to the model layers above and below the tropopause, as in the following listed scenarios: “TP$+$1” (100 % smoke injection into the model layer above the tropopause), “TP” (100 % smoke injection into the model layer containing the tropopause), “TP$-$1” (100 % smoke injection into the model layer below the tropopause), “TP1_8020” (as TP$+$1 but only 80 % of the emitted smoke injected above the tropopause and 20 % distributed between tropopause level and surface), “TP1_5050” (as TP$+$1, but only 50 % of the emitted smoke injected above and 50 % distributed below the tropopause), and “14km” (smoke injection into 14 km height as suggested from the spaceborne CALIOP lidar measurements showing smoke plumes in the lower stratosphere up to 17 km near the Australian continent (Hirsch and Koren, 2021). It is important to note that a larger height range is directly affected because of the model layer thickness at these heights.

In addition, a reference simulation was conducted using the original model configuration with 75 % of the wildfire emissions within PBL and 25 % into the two model layers above, which is hereafter referred to as the BASE case. To estimate the input of fire aerosol into the stratosphere from the pyroconvective fires, a model run was also performed in which the southeastern Australian wildfire emissions were set to zero for the pyroCb days, while they were treated as in the original setup for all other days (referred to as the NoEmiss case). Further experiments include model runs without interactive aerosol–radiation interaction for the BASE, TP$+$1, and TP1_8020 case scenarios in order to test the hypothesis that self-lifting due to radiative heating has significantly influenced the smoke plume evolution. The different model experiments are summarized in Table 1.

Table 1

Overview of scenarios simulated with ECHAM6.3-HAM2.3 using different assumptions for the emission height of the emitted biomass burning aerosol over southeastern Australia.

Scenario	Description
BASE	Standard emission height as prescribed in the ECHAM-HAM model for wildfires (75 % in PBL, 17 % in the first layer and 8 % in the second layer above PBL)
NoEmiss	Wildfire smoke emission set to zero for the pyroCb days: 29–31 December 2019 and 4 January 2020 in southeastern Australia
TP$+$1	Wildfire smoke emission from southeastern Australia injected into the model layer above the tropopause for the pyroCb days
TP	As TP$+$1, but smoke injection into the model layer containing the tropopause
TP$-$1	As TP$+$1, but smoke injection into the model layer below the tropopause
TP1_8020	As TP$+$1, but only 80 % of the emitted smoke injected above the tropopause and 20 % distributed between tropopause level and surface
TP1_5050	As TP$+$1, but only 50 % of the emitted smoke injected above the tropopause and 50 % distributed between tropopause level and surface
14km	Wildfire smoke emission from southeastern Australia injected into the model layer around 14 km height for the pyroCb days as suggested from satellite lidar observations

3 Results

3.1 Smoke transport simulation and model evaluation

According to satellite observations, the 2019–2020 Australian wildfire plume considerably increased the AOT of the usually pristine Southern Hemisphere (Hirsch and Koren, 2021). The average AOT at 630 nm wavelength derived from the AVHRR satellite instrument between 20–60${}^{\circ }$ S was increased to 0.16 for January 2020, which implies a 51 % offset from the long-term mean. The ground-based AERONET observations also show significantly increased AOT values after a major peak around or after mid-January. For example, at the Punta Arenas station, the average 550 nm AOT was 0.10 for January–March 2020, which is more than a factor 2 increase compared to the year 2019. One year later, in January 2021, the observed 500 nm AOT over Punta Arenas was still increased with a monthly mean of 0.06 (50 % increase relative to the monthly mean AOT for January 2019).

The dispersal of this smoke plume is reproduced using the global aerosol-climate model ECHAM6.3-HAM2.3 with the pyroconvective injection heights prescribed. The comparison of the modeled AOT of the BASE and TP$+$1 experiments, respectively, and that of the NoEmiss experiment (see Fig. 2) provide insight into the AOT distribution caused by the pyroCb events on 29–31 December 2019 and 4 January 2020, illustrating the role of the smoke injection height. While the monthly mean smoke AOT is simulated in absolute values as high as 0.26 and 0.22 for January, just downwind of the fire region in southeastern Australia for the BASE and TP$+$1 experiments, respectively, the results of the BASE experiment do not show increased smoke AOT east of 120${}^{\circ }$ W in January and none in the later months (Fig. 2a–c). In contrast, the results of the TP$+$1 model experiment, in which the smoke aerosol was injected into the model layer above the tropopause for the 4 southeastern Australian pyroCb days, show persistently enhanced smoke AOT south of 30${}^{\circ }$ S with AOT differences of 0.01 to 0.03 between TP$+$1 and NoEmiss until at least March 2020 (Fig. 2d–f). Also, a southward transport of the stratospheric smoke during the 3 months leading to a maximum smoke AOT anomaly above Antarctica in March is evident. Similar smoke transport to Antarctica was reported by Jumelet et al. (2020) for the earlier major Australian fires in 2009. The effect of the stratospheric transport of the smoke plume on the simulated monthly mean AOT from the Australian wildfires is shown in Fig. 2d–f. For the simulations that consider an explicit prescription of the aerosol injection into the upper troposphere or lower stratosphere, the model shows significantly enhanced AOT in large parts of the Southern Hemisphere. These model results indicate, in agreement with observations (Khaykin et al., 2020; Ohneiser et al., 2020), that elevated levels of wildfire smoke were sustained over several months and markedly impacted the radiative conditions in the Southern Hemisphere.

Figure 2

Monthly mean simulated AOT differences for January to March 2020 for the cases BASE $-$ NoEmiss (a–c), showing the contribution of smoke AOT for the case when no smoke injection by pyroconvection is prescribed in the model, and TP$+$1 $-$ NoEmiss (d–f), showing the effect on AOT of smoke injection into the model layer above the tropopause for the pyroCb days 29–31 December 2019 and 4 January 2020 in southeastern Australia.

[Figure omitted. See PDF]

To evaluate the representation of smoke emission height during the pyroCb days, the model results for the different sensitivity cases representing different injection heights are compared to sun-photometer measurements of mid- and high-latitude AERONET stations in the Southern Hemisphere (Holben et al., 1998) for the months of January to March 2020 (Fig. 3), and with ground-based lidar measurements from the PollyXT instrument at Punta Arenas for several days January 2020 (Fig. 4).

Figure 3

Scatter plots of observed versus simulated monthly mean 550 nm AOT at southern mid- and high-latitude AERONET stations for January to March 2020. The error bars represent the standard deviation based on daily values. Compared are model results for the cases (a) BASE, (b) TP$+$1, and (c) TP$-$1. The stations are color-coded respectively: Punta Arenas, Chile (53.14${}^{\circ }$ S, 70.89${}^{\circ }$ W), blue triangle; Amsterdam Island (37.80${}^{\circ }$ S, 77.57${}^{\circ }$ E), light blue circles; Marambio (64.24${}^{\circ }$ S, 56.63${}^{\circ }$ W) and Vechernaya Hill (67.66${}^{\circ }$ S, 46.16${}^{\circ }$ E), purple pentagons; South Pole (90.00${}^{\circ }$ S), light purple hexagons.

[Figure omitted. See PDF]

Figure 4

Comparison of modeled and observed profiles of aerosol extinction coefficients at the field site in Punta Arenas for 9, 12, and 26 January and 16 February 2020. Error bars indicate the estimated lidar measurement uncertainties of 30 %. Values below the lidar detection limit are omitted from the graph. See Table 1 for details of the different simulations.

[Figure omitted. See PDF]

Particularly for the AERONET stations located in Antarctica the observed AOT was enhanced in early 2020 compared to previous years. The agreement of model results with AOT measured at five AERONET stations is clearly better for the TP$+$1 and TP$-$1 cases with prescribed fire injection heights compared to the BASE case (Fig. 3). Considering the overall very low levels of AOT at the sites in the Southern Hemisphere, the alternative injection heights lead to a substantial improvement with up to 65 % higher modeled AOT values, e.g., at Punta Arenas. Still, all model results show a negative bias compared to the observations, indicating that the modeled effects of the smoke will underestimate the actual load and potentially the solar absorption of stratospheric smoke (see also Sect. 3.2). In the BASE case, the bias is on average about 30 % larger than for the other cases, representing smoke injection into the upper troposphere and lower stratosphere, and the correlation is also slightly lower, at least compared to the TP$+$1, TP, TP$-$1 and TP1_8020 cases (Table 2). The results for TP$+$1, TP, TP$-$1, TP1_8020 and 14km agree similarly well with the observations, with less agreement for the TP1_5050 case. The two cases, BASE and TP1_5050, therefore provide the worst representation of the observations, although no clear best fit is apparent for the other setups. The underestimation of the fire aerosol loading in all configurations can be caused by a source strength that is still too low in the GFAS data compared to, e.g., Peterson et al. (2021) or is partly due to missing secondary aerosol formed in the plume, which is not considered by the model.

Table 2

Statistical key figures for the comparison of measured and simulated AOTs for the different model cases at the AERONET sun-photometer stations: Punta Arenas, Chile (53.14${}^{\circ }$ S, 70.89${}^{\circ }$ W), Amsterdam Island (37.80${}^{\circ }$ S, 77.57${}^{\circ }$ E), Marambio (64.24${}^{\circ }$ S, 56.63${}^{\circ }$ W), Vechernaya Hill (67.66${}^{\circ }$ S, 46.16${}^{\circ }$ E), and South Pole (90.00${}^{\circ }$ S). The numbers in bold denote the cases with the best match for the respective statistical variables, the numbers in brackets denote the cases with least agreement (excluding case BASE). From top: Normalized Root Mean Square error (NRMS; normalized by mean), bias, Pearson correlation coefficient ($R$), and probability of correlation ($p$-value).

	BASE	TP$+$1	TP	TP$-$1	TP1_8020	TP1_5050	14km
NRMS	0.61	0.43	0.44	0.45	0.47	(0.51)	0.47
Bias	$-$0.035	$-$0.021	$-$0.021	$-$0.024	$-$0.025	($-$0.028)	$-$0.025
Correlation $R$	0.84	0.84	0.86	0.87	0.86	0.84	0.84
$p$-value of correlation	$\mathrm{3}\times {\mathrm{10}}^{-\mathrm{4}}$	$\mathrm{3}\times {\mathrm{10}}^{-\mathrm{4}}$	$\mathrm{1}\times {\mathrm{10}}^{-\mathrm{4}}$	$\mathrm{1}\times {\mathrm{10}}^{-\mathrm{4}}$	$\mathrm{2}\times {\mathrm{10}}^{-\mathrm{4}}$	$\mathrm{3}\times {\mathrm{10}}^{-\mathrm{4}}$	$\mathrm{3}\times {\mathrm{10}}^{-\mathrm{4}}$

The Australian wildfire smoke was observed in early 2020 above Punta Arenas with a ground-based lidar. Pronounced smoke layers first arrived on 8 January and were clearly above the local tropopause (Fig. 5). The altitude of the observed smoke plumes steadily increased and reached top heights of 26–27 km at the end of January. For the four observations in January and February 2020 (Fig. 4), the exceptionally thick smoke plume is also evident in the measured extinction coefficients. This remarkable wildfire smoke layering in terms of structure and magnitude shown in Fig. 4 can only be captured by the model with stratospheric Australian fire injection heights. Although the comparison of grid-cell to point-measurement remains uncertain in detail, a tendency for an underestimation of the stratospheric smoke is also apparent in Fig. 4. This could be due to an underestimation of the fire emissions or partly due to missing secondary smoke aerosol, which is not included in the model, as already suspected from the AOT comparison.

Figure 5

Comparison of the pattern of the temporal evolution of stratospheric smoke observed by lidar measurements and model results at Punta Arenas, Chile for January 2020. (a) Time-height curtain plot of aerosol attenuated backscatter coefficient from the PollyXT lidar at Punta Arenas in southern Chile (53.14${}^{\circ }$ S, 70.89${}^{\circ }$ W). (b) and (c) Simulated aerosol extinction for the model results the cases TP$+$1 and TP$-$1, respectively.

[Figure omitted. See PDF]

When using the model with original injection height (BASE case), none of the structures in the stratosphere can be simulated, just like in the NoEmiss case. This provides clear evidence that the deep pyroconvection in the wildfire hotspots in southeastern Australia did emit smoke well above the usually assumed injection heights (Remy et al., 2017; Val Martin et al., 2018). The model results also indicate the role of absorptive aerosol heating for the vertical transport of the smoke layer. In the lidar profiles, a continuous rise of the smoke layer is visible, with plume center heights increasing from 15 to 23 km (Figs. 4 and 5). The radiatively induced self-lifting of smoke can only be reproduced if aerosol–radiation interactions are considered in the simulations that finally lead to a considerable absorptive heating and associated buoyancy production (see discussion below, including Fig. 6).

Figure 6

Longitude-height distributions of modeled black carbon (BC) mixing ratios at latitude of 35${}^{\circ }$ S on average for January 2020 for the case TP1_8020 (a) without (w/o_DRF) and (b) including direct aerosol radiative forcing (incl_DRF). (c) Change in monthly mean short-wave heating rate caused by the absorption of solar radiation by the Australian wildfire smoke from the pyroCb days, computed as the difference between the cases TP1_8020 and NoEmiss.

[Figure omitted. See PDF]

The role of the self-lifting of the smoke caused by the radiative heating of the absorbing BC aerosol in the smoke is also illustrated by the vertical distribution of modeled BC mixing ratios (shown for case TP1_8020 in Fig. 6) averaged for January 2020 at 35${}^{\circ }$ S latitude where the fires occurred. In the BC mixing ratios for a model simulation where the aerosol is not interacting with radiation and thus does not heat the smoke containing atmospheric layers, the smoke BC remains below 20 km height, while ascending to 24 km for radiatively interactive aerosol in the model (Fig. 6a and b). The monthly heating-rate increase caused by the wildfire smoke leading to the self-lifting of the smoke plume is computed as the difference between the TP1_8020 and NoEmiss scenarios (Fig. 6c). This heating rate reached monthly mean short-wave values of up to 1.7 $\mathrm{K}{\mathrm{d}}^{-\mathrm{1}}$ in January 2020.

Figure 5 qualitatively compares the development of the smoke extinction profile for the cases TP$+$1 and TP$-$1 with the aerosol backscatter measurements at Punta Arenas, where the rise of the smoke plume center to 24 km by 31 January is particularly well matched for the TP$+$1 case (cf. Fig. 5a and b). For the other model scenarios with prescribed pyroCb smoke injection, the plume is lifted to lower heights of 20–21 km by the end of January. But even for case TP$-$1 in which the smoke was injected below the tropopause, the smoke has lifted into the stratosphere in the model (Fig. 5c). This result underlines the importance of a correct representation of fire injection heights, especially for intense wildfires, which is essential to realistically assess the radiative effects of smoke plumes.

Evidence that the 2019–2020 Australian wildfires caused significantly increased upper tropospheric/lower stratospheric aerosol loading across the Southern Hemisphere is also shown by the CALIOP satellite lidar observations in Fig. 7. The extinction profiles averaged over the latitudes of 30–60${}^{\circ }$ S and the region between Australia and South America (145${}^{\circ }$ E–70${}^{\circ }$ W) are considerably enhanced up to 12 km altitude for November to December 2019, compared to those of the previous years (2016 to 2018). In the period from January to March 2020, the extinction is again massively increased in the altitude range from 8 to 24 km, peaking at an altitude of 15 km. Also interesting to note is the fact that the CALIOP profile for January to March 2020 (brown line in Fig. 7) comprises about 50 times as many retrievals in the upper troposphere and lower stratosphere as the other averaging periods. This difference in sampling with far more CALIOP aerosol detections is clearly a response to the Australian wildfires. Comparing the model results with the CALIOP observations, it can be seen that our approach of prescribing pyroconvective smoke injection also reproduces the vertical distribution of Australian wildfire aerosol well across the southern mid-latitudes between Australia and South America, as shown in the example of scenario TP1_8020. Discrepancies at altitudes above 15 km are probably related to the CALIOP sampling bias discussed in Sect. 2.3, while between 4 and 12 km the model presumably underestimates the fire aerosol because of the smoke injection mainly in the tropopause region, which can also be seen in Fig. 4. In the boundary layer, a slight overestimation occurs again in the model. Overall, these misrepresentations are probably due to the comparatively simple approach to simulate the deep pyroconvective smoke injection.

Figure 7

Mean vertical profile of the 532 nm retrieved extinction coefficient from CALIOP (colored lines) for several selected periods within 2016–2020 and the 2019–2020 results from the ECHAM6.3-HAM2.3 model for the TP1_8020 case, averaged over the area covering the latitudes and longitudes between 30 and 60${}^{\circ }$ S and 145${}^{\circ }$ E and 70${}^{\circ }$ W.

[Figure omitted. See PDF]

3.2 Estimates of direct radiative perturbation

Regionally varying climate forcing agents such as aerosols substantially modulate the greenhouse forcing by anthropogenic aerosol particles and gases. We find that the individual extreme Australian fire event caused a significant direct instantaneous short-wave radiative forcing signal as shown in Fig. 8. The instantaneous direct aerosol radiative forcing in the model is calculated by calling the radiation scheme twice in each simulation in order to diagnose the radiative forcing without affecting the atmospheric conditions such as dynamics, moisture fields and clouds. The instantaneous short-wave forcing due to the elevated smoke layers ranged up to $+$0.50 $\mathrm{W}{\mathrm{m}}^{-\mathrm{2}}$ at TOA, averaged for the Southern Hemisphere from January to March 2020 under all-sky conditions for the TP$+$1 scenario (Table 3). This would correspond to a global-average TOA short-wave radiative forcing of $+$0.25 $\mathrm{W}{\mathrm{m}}^{-\mathrm{2}}$. In Table 3, the range of forcing estimates is given for all considered model scenarios except the clearly unrealistic cases (BASE and TP1_5050). This instantaneous forcing by the singular fire event is of similar magnitude as the latest multi-model estimate of the global-average instantaneous forcing for all anthropogenic BC with $+$0.28 (0.13–0.37) $\mathrm{W}{\mathrm{m}}^{-\mathrm{2}}$ (Thornhill et al., 2021). Previous studies, in contrast, found negative TOA radiative forcing estimates of $-$1 $\mathrm{W}{\mathrm{m}}^{-\mathrm{2}}$ (Khaykin et al., 2020) for this event, but only considered clear-sky situations in which the smoke aerosols appear brighter over the dark ocean surface due to the dominant scattering effect (Bellouin et al., 2020). However, the elevated Australian smoke layers that contain absorbing BC were located above clouds and to a large extent also above the strongly reflecting snow and ice cover of the Antarctic. Over such bright surfaces, the balance between aerosol scattering and absorption is shifted and smoke aerosol darkens the scene observed from TOA. At the surface (bottom of atmosphere, BOA), the clear-sky instantaneous solar radiative forcing was estimated to range from $-$0.68 to $-$0.81 $\mathrm{W}{\mathrm{m}}^{-\mathrm{2}}$ for the different model scenarios. This corresponds to the short-term surface dimming caused by a large volcanic eruption (Andersson et al., 2015; Schmidt et al., 2018). On the other hand, according to the model, the smoke-containing air layer itself experienced significant absorptive heating with maximum short-wave heating rates of 1.7 $\mathrm{K}{\mathrm{d}}^{-\mathrm{1}}$ on average in January 2020 for the TP$+$1 case. While the effective TOA radiative forcing is expected to be low due to stratospheric adjustment to the instantaneous forcing, these heating-rate changes may have the potential to trigger responses in the atmospheric dynamics. Khaykin et al. (2020) actually showed that a self-sustained 1000 km anticyclonic vortex formed as a result, which traveled through the stratosphere for weeks, accompanied by a local ozone reduction. Such a vortex is also seen in the 50 hPa wind fields of the ECHAM6.3-HAM2.3 simulations (not shown here). The analysis of the atmospheric dynamic effects, however, is the subject of a follow-up study.

Figure 8

AOT and estimates of short-wave radiative forcing of the 2019–2020 Australian wildfire smoke plume in the Southern Hemisphere. Model results of (a) AOT and (b, c) instantaneous short-wave radiative forcing of the elevated smoke aerosol layer, averaged over the months of January to March 2020. All values are differences between model ECHAM6.3-HAM2.3 results with Australian wildfire smoke injection for the scenarios TP$+$1 and NoEmiss. The instantaneous radiative flux differences are shown for all-sky conditions at top (TOA; b) and bottom of the atmosphere (BOA; c).

[Figure omitted. See PDF]

Table 3

Short-wave instantaneous direct radiative forcing ($\mathrm{W}{\mathrm{m}}^{-\mathrm{2}}$) of the elevated smoke plume during the 2019–2020 Australian wildfires. The estimates are calculated differences between the instantaneous short-wave irradiances of the model results including stratospheric smoke injection and the case NoEmiss without smoke emission from southeastern Australia for the pyroCb days, averaged over the Southern Hemisphere. Ranges are given for the different configurations: TP$+$1, TP1_8020, TP, TP$-$1, and 14km (see Table 1). Shown are the differences for all-sky and clear-sky conditions at top and bottom of atmosphere (TOA, BOA) averaged for the months of January to March (JFM) 2020.

	TOA all sky	TOA clear sky	BOA all sky	BOA clear sky
January 2020	$+$0.45 to $+$0.56	$-$0.02 to $-$0.05	$-$0.54 to $-$0.61	$-$0.86 to $-$0.97
February 2020	$+$0.40 to $+$0.57	$+$0.003 to $+$0.07	$-$0.42 to $-$0.51	$-$0.67 to $-$0.84
March 2020	$+$0.25 to $+$0.37	$-$0.01 to $+$0.07	$-$0.28 to $-$0.38	$-$0.46 to $-$0.63
JFM Average	$+$0.37 to $+$0.50	$-$0.02 to $+$0.02	$-$0.42 to $-$0.50	$-$0.68 to $-$0.81

Major uncertainties in the model estimates of aerosol radiative forcing are due to uncertainties in AOT, particle angular scattering properties (asymmetry parameter) and in particular, aerosol absorption that is characterized by its SSA. A recent comprehensive analysis of aircraft data indicates that model parameterizations may generally overestimate absorption by biomass burning aerosol due to an insufficient representation of the mixing state for fire aerosol (Brown et al., 2021). In our model, at the height of maximum extinction of the smoke plume, the ratio of BC to total carbon ($\text{BC}/(\text{BC}+\text{OC})$ mixing ratio) is approximately 0.05–0.08, corresponding to a particle SSA between 0.82–0.85 at 550 nm. This is within the range of other aerosol models (Bellouin et al., 2020; Brown et al., 2021). Accordingly, the model may be biased toward positive forcing that is too strong. On the other hand, inversion results of multispectral lidar observations in the Northern Hemisphere from the strong 2017 Canadian fires yield an SSA of 0.80 for the stratospheric smoke (Haarig et al., 2018). For the 2019–2020 Australian fires, the lidar inversion method of Veselovskii et al. (2002) was applied to the Polly multiwavelength backscatter and extinction observations on 26 January 2020 to obtain values for SSA by Ohneiser et al. (2022). They show an SSA of 0.79 with an uncertainty range of 0.05 for the smoke-filled vortex on 26 January above Punta Arenas in Chile, which is considered representative of the mid- and high latitudes in the Southern Hemisphere (Ohneiser et al., 2022). A steady decline in the lidar depolarization ratio at Punta Arenas from around 20 % to 10 % by mid-February and below 5 % at the end of February indicates an aging of the fire plume. However, high lidar ratios at 532 nm were observed with values ranging from 75 to 115 sr (mean 91 sr) well beyond that time, further indicating strongly absorbing smoke particles and low SSA values (see Fig. 8 in Ohneiser et al., 2022). The lidar simulator of the model, in comparison, provides slightly lower lidar ratios at 532 nm between 70 and 100 sr for the stratospheric smoke layer. Regarding the asymmetry parameter, it is difficult to make an evaluation because the exact morphology of the smoke particles is not known. In the model, the asymmetry parameter for the Australian smoke is about 0.6 at 550 nm, which is a typical value for wildfire aerosol (e.g., Reid et al., 2005). In terms of SSA and lidar ratio, this would imply that the model underestimates absorption by Australian stratospheric smoke at least in January 2020, where the retrieval is available, whereas it tends to overestimate it in other, weaker vegetation fires according to Brown et al. (2021). The comparison to the ground-based remote-sensing retrievals provides the best available confirmation for the optical properties of the 2019–2020 Australian fire smoke during this outstanding biomass burning event in the model. However, we cannot rule out the possibility that away from the core plume, more reflective secondary organic particles made a larger contribution to the stratospheric fire aerosol. In addition, dilution impacts on smoke aging with regard to particle size and mixing state could have influenced the smoke optical properties more strongly toward less absorption (Hodshire et al., 2021; Sellitto et al., 2022). The resulting effects of this spatial and temporal variability and evolution in the optical properties of the Australian wildfire plume would not or only insufficiently be represented by the model.

4 Implications and perspectives

In order to determine the impact of biomass burning aerosol on the global energy budget, accurately estimating emission fluxes and their injection height in the atmosphere is essential. State-of-the-science global aerosol-atmosphere models generally consider biomass burning aerosol, but still show uncertainties in the spatiotemporal distribution. In particular, large emission events like Australia's Black Summer wildfires of 2019–2020 are underrepresented.

A key uncertainty is the vertical injection of fire smoke into the atmosphere that may ultimately cause misrepresentation of the plume evolution. The results of this study show that using fire emission data from the GFAS dataset and injecting the smoke into the tropopause region for pyroCb events render results that are reasonable, although still somewhat underestimated in the present study.

The substantial increase in stratospheric AOT in the Southern Hemisphere, and thus the perturbation of the radiative balance, from the southeastern Australian wildfire smoke for only 4 days of pyroconvection events is remarkable. The local sub-grid scale nature of fire plume rising challenges the representation in models beyond the 1 km scale, especially in global models that do not resolve convection (Paugam et al., 2016; Veira et al., 2015). In these coarse models, the vertical distribution of fire emissions is based on climatological profiles (Val Martin et al., 2018) or prescribed by injection heights estimated from satellite retrievals of fire radiative power (Remy et al., 2017). While this is appropriate for the majority of vegetation fires, the vertical transport during deep pyroconvective events with potentially far-reaching effects is most likely underestimated due to the obstruction of satellite observations by dense pyroCb clouds (Remy et al., 2017). Adequate plume rise parameterizations exist particularly for mesoscale chemistry-transport models, but have not yet found their way into climate modeling on a wider scale (Paugam et al., 2016; Val Martin et al., 2018; Veira et al., 2015).

Consequently, while aerosol-climate models have been shown to overestimate the radiative forcing biomass burning aerosol in general (Brown et al., 2021), they presumably underestimate the wildfire aerosol impacts on the energy balance for pyroconvective fires, as the vertical location of the smoke is fundamental to its radiative impact. To solve this, adjustments are needed in the representation of biomass burning injection. By implementing a more realistic emission scenario based on aerosol-profiling observations but still using the emission fluxes from the standard GFAS database, we enhance the ability of our model to capture the extreme 2019–2020 Australian pyroCb event, and can thus showcase the potential of global aerosol-climate models to realistically reproduce the spatiotemporal evolution of smoke plumes of intense wildfires. This further allows an improved estimation of aerosol impacts on radiation and clouds. Ultimately, these improvements are essential to any estimate of the Earth's energy balance and climate state. In this respect, it is particularly important to make climate models capable of dealing with exceptional outliers of wildfires, which are anticipated to increase in frequency and severity worldwide in response to anthropogenic climate warming (Abatzoglou et al., 2019; Jolly et al., 2015; Wotton et al., 2017). The increased risk of serious wildfires is related to extreme heat and drier conditions, as well as record-low snow cover in boreal regions (Box et al., 2019; Dowdy et al., 2019). More frequent and intense fire weather extremes will also increase the likelihood of deep pyroconvection (Dowdy et al., 2019). Along with this, of course, there continues to be the challenge and need to develop better model representations of smoke aging and secondary aerosol formation, including the associated evolution of particle optical properties in the life cycle of wildfire plumes. In essence, biomass burning emissions are an important source of aerosol particles, and individual wildfires are shown to have more widespread effects than previously assumed. An as-accurate-as-possible description, therefore, is key to successfully estimating aerosol climate effects, and future climate projections will clearly benefit from an improved aerosol representation in Earth system models.

Code availability

The ECHAM-HAMMOZ code is maintained and made available to the scientific community under https://redmine.hammoz.ethz.ch (HAMMOZ community, 2022). The availability is regulated under the HAMMOZ Software Licence Agreement that can be downloaded from https://redmine.hammoz.ethz.ch/attachments/download/291/License_ECHAM-HAMMOZ_June2012.pdf (last access: 15 October 2021).

Data availability

The ECHAM6.3-HAM2.3 model output, on which the figures are based, and the analyzed lidar profiles are accessible at Zenodo from 10.5281/zenodo.5571545 (Heinold et al., 2021). The ground-based Polly lidar data time series is visualized at https://polly.tropos.de (last access: 5 October 2021) and will become publicly available via the data portal of the European Aerosols, Clouds and Trace gases Research Infrastructure (ACTRIS) when its implementation phase is completed. Until then, raw data are available on request via [email protected]. AERONET data can be obtained with the Aerosol Robotic Network download tool https://aeronet.gsfc.nasa.gov/cgi-bin/webtool_opera_v2_new (NASA, 2021). The Aerosol Optical Thickness CDR used in this study was acquired from NOAA's National Climatic Data Center (http://www.ncdc.noaa.gov, NOAA, 2022).

Author contributions

BH and IT conceived the idea and led the study. BH and AK performed the model development and ran the simulations. NS provided the lidar simulator for ECHAM6.3-HAM2.3. IT, FS, KS, AK and BH focused on the analysis and interpretation of model results. RS analyzed NASA's AVHRR AOT climatology data, and DV researched the Earth history context. KO, HB and BB performed the analysis and interpretation of the ground-based lidar observations, and MC provided that for the spaceborne lidar CALIOP. BH, IT, KS, FS and RS wrote the paper with contributions from all the co-authors. All the authors participated in the revision and editing of the paper.

Competing interests

The contact author has declared that none of the authors has any competing interests.

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 “The role of fire in the Earth system: understanding interactions with the land, atmosphere, and society (ESD/ACP/BG/GMD/NHESS inter-journal SI)”. It is a result of the EGU General Assembly 2020, 4–8 May 2020.

Acknowledgements

The authors thank Johannes Quaas and Albert Ansmann for sharing their comments on an earlier version of the manuscript. We also would like to thank the whole DACAPO-PESO team for ensuring the continuous operation of all the different instruments at Punta Arenas. Special thanks to Patric Seifert, Martin Radenz, Cristofer Jimenez and Ronny Engelmann for taking care of the lidar, measurements and ensuring high-quality data operation at the cost of spending many lifetime hours in an airplane. Igor Veselovskii is acknowledged for computing lidar inversion products. The NOAA Climate Data Record (CDR) of AVHRR aerosol optical thickness (AOT) was originally developed by Xuepeng Zhao and colleagues. We thank Philippe Goloub, Victoria Eugenia Cachorro Revilla, Patric Seifert, James Butler, Brent Holben, and Anatoli Chaikovsky for their efforts in establishing and maintaining the AERONET sites Amsterdam Island, Marambio, Punta Arenas, South Pole, and Vechernaya Hill. The ECHAM-HAMMOZ model is developed by a consortium composed of ETH Zürich, Max Planck Institute for Meteorology, Forschungszentrum Jülich, the University of Oxford, the Finnish Meteorological Institute and the Leibniz Institute for Tropospheric Research (TROPOS) and managed by the Center for Climate Systems Modelling (C2SM) at ETH Zürich. We are grateful for computing time from the Deutsches Klimarechenzentrum (DKRZ). Computing resources at DKRZ were granted under project no. bb1004. We thank Pasquale Sellitto and an anonymous reviewer for their helpful feedback.

Financial support

The publication of this article was funded by the Open Access Fund of the Leibniz Association.

Review statement

This paper was edited by Marc von Hobe and reviewed by Pasquale Sellitto and one anonymous referee.