# The characterization of long-range transported North American biomass burning plumes: what can a multi-wavelength Mie-Raman-polarization-fluorescence lidar provide?

Qiaoyun Hu, Philippe Goloub, Igor Veselovskii, Thierry Podvin

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Qiaoyun Hu, Philippe Goloub, Igor Veselovskii, Thierry Podvin. The characterization of long-range transported North American biomass burning plumes: what can a multi-wavelength Mie-Raman-polarization-fluorescence lidar provide?. Atmospheric Chemistry and Physics, 2022, 22, pp.5399-5414. 10.5194/acp-22-5399-2022. insu-03686317

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# The characterization of long-range transported North American biomass burning plumes: what can a multi-wavelength Mie–Raman-polarization-fluorescence lidar provide?

Qiaoyun Hu¹, Philippe Goloub¹, Igor Veselovskii², and Thierry Podvin¹

¹Univ. Lille, CNRS, UMR 8518 – LOA – Laboratoire d'Optique Atmosphérique, 59650 Lille, France

²Prokhorov General Physics Institute of the Russian Academy of Sciences, Moscow, Russia

**Correspondence:** Qiaoyun Hu (qiaoyun.hu@univ-lille.fr)

Received: 24 November 2021 – Discussion started: 25 November 2021

Revised: 11 March 2022 – Accepted: 30 March 2022 – Published: 25 April 2022

**Abstract.** This article presents a study of long-range transported biomass burning aerosols (BBA) originated from the North American wildfires in September 2020. The BBA plumes presented in this study were in the troposphere and underwent 1–2 weeks of aging before arriving at the lidar station ATOLL (ATmospheric Observatory of LiLle) in northern France. A novel lidar-derived dataset, $2\alpha + 3\beta + 3\delta + \phi$ ($\alpha$: extinction coefficient; $\beta$: backscatter coefficient; $\delta$: particle linear depolarization ratio, i.e., PLDR; $\phi$: fluorescence capacity), is provided for the characterization of BBA. The fluorescence capacity is an intensive aerosol parameter describing the ability of aerosols in producing fluorescence when exposed to UV excitation. In our BBA observations, obvious variations in aerosol intensive parameters, reflecting the variability of BBA properties, were detected. The PLDRs varied from less than 0.03 at all wavelengths to 0.15–0.22 and 0.12–0.16, respectively, at 355 and 532 nm. The extinction related Angström exponent was within the range of −0.3 to 1.0 and the fluorescence capacity was $1.0 \times 10^{-4}–4.0 \times 10^{-4}$. Lidar ratio as low as $24 \pm 4$ sr (50–8 sr) was observed in the BBA plumes at 355 (532) nm on 17–18 September, which was lower than most previously observed aged BBAs. These variations are likely correlated with the combustion process, the lifting of BBA plumes and the conditions (temperature, humidities, etc.) in the aging process. In addition, our results indicate BBA could act as ice nucleating particles in tropospheric conditions. The lidar fluorescence channel proves to be an important added value in aerosol characterization and aerosol–cloud interactions studies, due to its high sensitivity. With the increase in wildfire occurrence and intensity, BBAs become a more and more important atmospheric component. In this context, we show the potential of our novel lidar-derived dataset for aged BBA particles’ characterization and for the understanding of their role in cloud processes.

# 1 Introduction

Severe wildfires have caught the attention of the public and the scientific communities in recent years. Wildfires in North America increase in both frequency and intensity, due to the warming of the climate. Regarding the global scale, the duration of fire seasons increased by about 19% from 1979 to 2013 (Jolly et al., 2015; Schoennagel et al., 2017). Wildfires can directly impact the vegetation of earth’s surface, the fer-

tility of soils, the water cycle and human society (Santín and Doerr, 2016; Ditas et al., 2018; May et al., 2014; O’Dell et al., 2020). Copious amount of fire emissions, including gases and particles, have been injected into the troposphere and occasionally into the upper troposphere and lower stratosphere (UTLS). Those emissions pose threats to the air quality and human health, because they contain mainly fine particles and some chemical compounds in wildfire emissions are toxic. They could alter the radiation budget of the planet by
scattering and absorbing the incoming solar radiation and influence the cloud process by modifying cloud properties and acting as ice nucleation particles (INP) and cloud condensation nuclei (CCN).

Wildfire emissions are composed of a mixture of gases, e.g., carbon monoxide, polycyclic aromatic hydrocarbons (PAHs) containing gas-phase hazardous air pollutants, water vapor and aerosol particles, such as black carbon (BC), organic carbon (OC), etc. In addition, water soluble ions (potassium, halides, sulfates) can also be produced by the decomposition of biomass and the subsequent condensation in the smoke plume. The OC components account for a substantial fraction, about 20% to 90% in wildfire emissions, much higher than BC. Humic-like substances, which are a complex group of high molecular weight organic compounds, contribute considerably to the mass of organic compounds and influence the light absorbing properties of aerosols (urbanski et al., 2008; Santín and Doerr, 2016; Wu et al., 2018). For convenience, we use hereafter “BBA” (biomass burning aerosols) to refer to the aerosols resulting from wildfire emissions. Due to the complexity in the burning and the aging processes, the BBA properties are highly variable. The initial composition and size distribution of BBAs depend on the burning materials (i.e., vegetation type, such as grassland, boreal forest, etc.) and environmental conditions (temperature, moisture, soil properties, etc.), which impact the combustion efficiency and the burning processes (i.e., flaming and smoldering). The smoldering phase, which is with lower temperature, could lead to a substantially higher conversion of burning materials to toxic compounds than the flaming phase, and produce more weakly absorbing OC aerosols. Fire emissions from high temperatures and the flaming phase tend to contain an increased proportion of BC to OC and have smaller smoke particles (Reid et al., 2005; Garofalo et al., 2019).

Fresh BBAs are fractal like aggregates of BC cores and OC coatings (China et al., 2013, 2015). During long-range transport, BBAs undergo complex aging processes, including condensation, oxidation, evaporation, coagulation, compaction, humidification and so on. These processes could modify the particles’ morphology, composition, optical and chemical properties and hygroscopic properties. The aging process of wildfire emissions is not yet adequately characterized. It includes a complex group of chemical reactions and physical changes, among which the gas-to-particle condensation driven by oxidation and evaporation driven by aerosol dilution are two important and competing processes. The oxidation process can produce more organic matter with lower volatility, while it could also lead to increased volatile secondary organic aerosol (SOA) due to fragmentation of some macromolecules. The evaporation tends to decrease the partitioning of OC aerosols as dilution shifts the gas-particle equilibrium more to the gas end. Measurements in laboratories and field campaigns do not reach a consensus on the relative balance of the two competing processes as they are

controlled by many factors, such as the dilution rate, exposure to oxidants ($O_3$, OH radical), travel time and so on. The growth of particle size is found in both near-field and long-time aged BBAs, while the causes might not be the same. Condensational growth is the dominating factor in fresh and near-field BBAs, while coagulational growth is dominating in aged BBAs. Abel et al. (2003) reported an increase in single scattering albedo (SSA) from about 0.84 to 0.90 in 5 h after the emission, which is likely due to the condensation of scattering organic components on absorbing soot particles during early-stage aging. Similar changes in SSA were derived by Kleinman et al. (2020) when investigating near-field BBA plumes from the western USA. The aging process can result in complex BBA structures and varying properties. Dahlkötter et al. (2014) sampled BBA particles in a 3–4 d old plume from western U.S. wildfires in the UTLS. They found that a significant proportion of the particles are BC-containing particles mixed with light-scattering materials and the mixing state is highly variable. Observations of long-rang transported Canadian smoke in 2017 and Australian smoke in 2019–2020 in UTLS showed enhanced particle linear de-polarization ratios (PLDR) that had never been detected in tropospheric smoke layers (Haarig et al., 2018; Hu et al., 2019; Ohneiser et al., 2020; Khaykin et al., 2020). Similar signatures of PLDRs have also been observed in aged tropospheric BBAs originating from wildfires (Murayama et al., 2004; Burton et al., 2015). Researchers thought such characteristics of PLDRs are indications of complicated BBA particle morphology and effects of long-time aging. Since then, many efforts have been made to simulate aged BBA particles’ optical properties. The simulations indicate that aerosol properties, such as the absorption and PLDRs, are strongly dependent on the morphology, mixing state and fractions of different components.

BBAs contribute to ice nucleating (IN) mainly through immersion freezing, contact freezing and deposition freezing, as well as pore condensation and freezing (Kanji et al., 2011; Umo et al., 2015; Grawe et al., 2016; Kanji et al., 2017; Knopf et al., 2018; Umo et al., 2019). These mechanisms are not yet well resolved and data about the onset condition of ice nucleation by BBA particles are diverse. As wildfire emissions become a more and more important atmospheric aerosol source, the role of BBAs as INP becomes increasingly important and different theories have been proposed to understand BBAs’ IN ability. One important argument is that the amorphous state of organic matter and complicated morphology of BBAs at atmospheric conditions could influence the ability of water diffusion, thus causing strong perturbations in the prediction of cloud formation (Berkemeier et al., 2014; Knopf et al., 2018). Recently, Jahn et al. (2020) reported a different mechanism. They claimed that the inorganic elements naturally present in biomass could be transformed by the combustion process to minerals, which are very active over a wide range of temperatures. Studies also found that the aging process could potentially increase
the capability of BBA in cloud formation (Lupi and Molinero, 2014; Jahl et al., 2021). Therefore, the characterization of BBA properties in light scattering and cloud formation after long-range transport is an important direction to improve the representation of the aerosol model and, further, the accuracy of the climate model.

The 2020 California wildfires are the largest in Californian modern history. They comprise about 9639 fire activities reported in the California state (located on the West Coast of the USA). The fire season started from the beginning of May 2020. By the end of the year, nearly 10 000 fires had burned over 4.2 million acres, more than 4% of the state's roughly 100 million acres of land (https://www.fire.ca.gov/incidents/2020/, last access: 20 April 2022). In mid-August, the first “gigafire” spreading over seven counties in northern California was recorded. “Gigafire” is a level above “megafire” and describes a blaze burning at least a million acres of land. Satellite observations indicated this fire activity caused huge BBA emissions over the middle and western USA, while the plumes faded away after 1 week without being transported to other continents. In September 2020, the fire activities revived after a short pause. Fire emissions were lofted into UTLS by high winds or convective pyro-cumulonimbus, and then transported to Europe by the prevailing westerlies (Baars et al., 2021). The densest smoke plumes detected at the observatory ATOLL (Atmospheric Observatory of LiLle) in Lille, France, was in the period of 10–23 September. In this study, we analyzed the observations from multiple instruments and the optical properties derived from a multi-wavelength Mie–Raman-polarization-fluorescence lidar equipped with a fluorescence channel.

## 2 Observations

### 2.1 Satellite observations – OMPS and CALIPSO

According to satellite observations, the smoke plumes detected in Lille from 10 to 22 September are attributed to the fire activities from 4 to 11 September in California and Oregon state in the USA. From 4 to 6 September 2020, the Creek fire started in southwestern California. On 5 September, the fires generated a pyro-cumulonimbus (PyroCb) cloud reaching about 16 000 m, which might be the highest PyroCb cloud ever (Creek Fire, 2020). The plumes from Creek fire can be clearly seen in the earth's true color image (Fig. 1a) and the maps of the UV aerosol index (UVAI) from OMPS observations shown in the Supplement. The center of the lofted plumes was at (37.7° N, 117.8° W) on 6 September and then transported rapidly toward the northeast. From 7 to 10 September, the forest on the west coast of California and Oregon started to burn, which will be called “Oregon fires” hereafter (Oregon Fire, 2020). The burning area was in serious drought and under the blasts of fierce winds, which lifted vast fire emissions into the atmosphere. On 9 September, the wind whipped up fires and generated a pyro-cumulus

<figure><img src="image_4.png" /><figcaption>**Figure 1.** True color images from OMPS onboard Suomi NPP. (a) 6 September 2020, (b) 10 September 2020 and (c) 12 September 2020. The two AERONET observation sites: NASA Ames (37.420° N, 122° W) and PNNL (46° N, 119° W). © Google Maps.</figcaption></figure>

cloud. Due to cyclone activities, the plumes were trapped on the eastern Pacific ocean and West Coast of the USA on 7–11 September, as shown in Fig. 1b. The plumes started spreading on 12 September and arrived in Europe between 16 and 18 September.

Figure 2 shows the CALIPSO observations in the transport pathway. The plumes in Fig. 2a–c and d–f are attributed to the Creek fire and the Oregon fire, respectively. The plume origins were identified using HYSPLIT back trajectories and OMPS UVAI maps, shown in the Supplement. The plumes emitted by the Creek fires are mostly classified as “elevated smoke” by the CALIPSO aerosol typing algorithm (version 4.21), while the plumes emitted from Oregon fires are mostly detected as “polluted dust”. The reason is that the PLDR at 532 nm of the BBA particles from the Oregon fire
<figure><img src="image_5.png" /><figcaption>**Figure 2.** The backscattering coefficients and PLDR ratio at 532 nm measured by CALIPSO. The smoke plumes in (a), (b) and (c) are attributed to the Creek fires from 5 to 7 September 2020, and in (d), (e) and (f) are attributed to the Oregon fires. The inserted maps display the granules of CALIPSO and the locations of the gray dots represent the region where the measurements are averaged. (a) Central USA, 8 September 2020. (b) East of Quebec, 9 September 2020. (c) Eastern Europe, 11 September 2020. (d) West Coast of USA, 10 September 2020. (e) Western coast of US, 11 September 2020. (f) Eastern USA, 14 September 2020. The layer between the two dashed red lines is BBA. The dashed blue lines represent the location of the mixture of ice crystals and BBA particles.</figcaption></figure>

was higher than that of the Creek fire. PLDR is a parameter reflecting particle shape, i.e., spherical particles have a PLDR of zero while morphologically complicated particles, such as dust and ice crystals, have high PLDRs. PLDR<sub>532</sub> is about 0.02–0.05 in Creek plume after 3–7 d of transport in the upper troposphere. In comparison, the PLDR<sub>532</sub> in the Oregon plume is about 0.10–0.15 after 1–7 d of transport. The observed differences of BBA properties in the two events may be attributed to the combustion and lifting processes.

## 2.2 Sun/sky photometer observations near wildfire source

NASA\_Ames and PNNL are two AERONET sites located near the fire activities, as shown in Fig. 1b. PNNL was mainly impacted by the Oregon smoke during 12–19 September. In Fig. 3, the aerosol optical depth at 500 nm (AOD<sub>500</sub>) was about 0.2 and the Angström exponent between 340 and 500 nm (AE<sub>340–500</sub>) about 1.5 from 1 to 8 September, before the arrival of the Oregon smoke. When the Oregon plumes arrived at PNNL on 12 September, the AOD sharply increased and the AE decreased at the same time. The AOD<sub>500</sub> significantly increased and the maximal AOD<sub>500</sub>
was about 4.0, with a corresponding AE$_{340–500}$ of 0.2, during 12–19 September. NASA_Ames is in the west of the Creek fire and was influenced first by the Creek fire and then by the Oregon fire. AOD$_{500}$ from 4 to 8 September, when Creek smoke particles dominated, was less than 1.0 (with AE$_{340–500}$ ~ 1.2), because the center of the Creek plumes propagated eastward and only a part of it drifted to the west. The Oregon plumes started on 9 September, as indicated by a sharp increase in AOD and a decrease in AE$_{340–500}$. The peak AOD$_{500}$ of 5.8, corresponding to AE$_{340–500}$ ~ 0.0, was detected on 12 September in NASA_Ames. Similar to the observation at PNNL, AE$_{340–500}$ obviously decreased during the episodes of Oregon smoke. The decrease in AE$_{340–500}$ indicates the increase in particle size in the Oregon BBA plumes, which is in agreement with the CALIPSO observations.

## 2.3 Lidar and photometer observations in Lille, France

The lidar involved in this study is a multi-wavelength Mie-Raman-polarization-fluorescence lidar, LILAS, operated at ATOLL platform, University of Lille, France. The lidar system uses a Nd:YAG laser and has three emitting wavelengths, i.e., 355, 532 and 1064 nm. The backscattered lidar signals are collected at three elastic wavelengths each coupled with a parallel channel and a cross channel, and three Raman channels at 387 (vibrational Raman of N$_{2}$), 530 (rotational Raman of N$_{2}$ and O$_{2}$) and 408 nm (water vapor channel). In December 2019, the water vapor channel was replaced by a fluorescence channel centered at 466 nm (excitation wavelength: 355 nm) in order to profile atmospheric fluorescence. A full description of this configuration and the results of the feasibility test can be found in Veselovskii et al. (2020). With this configuration, we can derive the height-resolved dataset $2\alpha + 3\beta + 3\delta + \phi$ ($\alpha$: extinction coefficient; $\beta$: backscattering coefficient; $\delta$: particle linear depolarization ratio; $\phi$: fluorescence capacity). The fluorescence signal is attributed to certain molecules that could absorb in the incident laser light and re-emit it at longer wavelengths. The fluorescence capacity represents the capacity of aerosol particles in producing fluorescence; hence, it is linked to particle chemical compositions. Equations (1) and (2) denote, respectively, the fluorescence backscattering coefficient $\beta_F(z)$ and the fluorescence capacity $\phi(z)$:

$$ \beta_F(z) = \frac{C_R P_F(z) T_R(z)}{C_F P_R(z) T_F(z)} N_R(z)\sigma_R, \quad (1) $$

where $P_F(z)$ and $P_R(z)$ are the lidar signals of fluorescence and Raman channel, respectively, $C_R$ is the ratio of instrumental constant between the Raman and the fluorescence channel, and it is determined by calibration; $N_R(z)$ is the vertically distributed number concentration of molecular N$_{2}$ and O$_{2}$; and $\sigma_R$ is the Raman differential scattering cross section in the backward direction. With $\beta_F$, one can define the fluo-

rescence capacity $\phi(z)$:

$$ \phi(z) = \frac{\beta_F(z)}{\beta_{z0}(z)}. \quad (2) $$

According to our observations, BBA and pollen particles are very efficient in producing fluorescence, while dust particles and continental aerosols are much less efficient. More information about fluorescence lidar measurements and aerosol fluorescent signatures can be found in our previous publications (Hu et al., 2019; Veselovskii et al., 2020, 2021b).

Figure 4 shows lidar observations in the period of 11–22 September 2020. Figure 4a and b show the range corrected lidar signal and the volume depolarization ratio at 1064 nm, respectively. The background aerosols in Lille are usually low depolarizing fine particles in the boundary layer. During the observational period, the BBA layers distributed at 2000–14 000 m and polluted dust in the boundary layer were the two aerosol species. The smoke plumes are obvious in Fig. 4a and disappear in Fig. 4b, because BBA particles have very weak depolarization at 1064 nm. The most intense smoke plumes are observed from 11 to 12 September, corresponding to AOD$_{500}$ ≈ 0.65 and AE$_{340–500}$ ≈ 0.70, shown in Fig. 4c. Aerosols in the boundary layer from 14 to 16 September were strongly depolarizing. Back trajectories and modeling results indicated the cause for the enhanced depolarization could be polluted dust or transported pollen. From 17 to 18 September, a decrease of AE$_{340–500}$ was detected when a smoke plume appeared at 6000–10 000 m. The AOD$_{500}$ and AE$_{340–500}$ on 17 September were about 0.22 ± 0.02 and 0.0 ± 0.20, respectively.

Figure 5 plots the intensive parameters in the BBA layers detected in time intervals in September 2020. The observation time and the height range of the layers are presented in Table 1. Lidar ratio (LR), i.e., the ratio between extinction coefficient and backscatter coefficient, is correlated with multiple factors, such as the particle shape, size and refractive indices. LR$_{355}$ being lower than LR$_{532}$ is a typical feature of aged smoke particles from North America and Siberian wildfires. The values of lidar ratios varied in the range of 20–50 sr at 355 nm and 42–90 sr at 532 nm. The spectral dependence of the PLDRs is in agreement with the aged wildfire smoke particles in the literature. The variation ranges of PLDRs were, respectively, 0.03–0.22, 0.02–0.16 and 0.01–0.03 at 355, 532 and 1064 nm in the investigated cases. The PLDRs on 18 and 19 September (P7 and P8) were higher than other days, with the mean PLDR equal to 0.16 at 355 nm, 0.12 at 532 nm and 0.02 at 1064 nm. The fluorescence capacity varied from $1.0 \times 10^{-4}$ to $4.0 \times 10^{-4}$. The Angström exponent related to the backscatter coefficient (BAE$_{355–532}$) is in the range of 1.5–2.5, whereas the variation of Angström exponent related to extinction coefficient (EAE$_{355–532}$) is stronger. Before 17 September, the EAE$_{355–532}$ varied in the range 0.5–1.5 and, after this day, it dropped to below zero. The vertical variations in the BBA layers, indicated by the distance between the bottom and the top of each box plot
<figure><img src="image_6.png" /><figcaption>**Figure 3.** AOD and AE (Level 1.5) measured by AERONET sun/photometers at two observation sites: (a) PNNL (46° N, 119° W) and (b) NASA_Ames (37.420° N, 122° W). NASA_Ames is within the influence of both the Creek fire and the Oregon fire. PNNL is mainly impacted by the smoke of the Oregon fire. The smoke of the Oregon fire arrived at NASA_Ames on about 9 September and at PNNL on 12 September 2020. The arrival of the Oregon smoke caused significant increase in AOD and decrease in the AE at both sites.</figcaption></figure>

<table><caption>**Table 1.** The averaging time intervals and altitude ranges of selected BBA layers for the analysis of statistics. P1, P2 ..., P9 represent different time intervals in September 2020.</caption><thead><tr><th>No. of period</th><th>Time interval (yyyy-mm-dd, hh:mm:ss, UTC)</th><th>Height (m)</th></tr></thead><tbody><tr><td>P1</td><td>2020-09-11, 02:00:00-2020-09-11, 04:00:00</td><td>5500-7500</td></tr><tr><td>P2</td><td>2020-09-11, 22:00:00-2020-09-12, 03:00:00</td><td>5500-8500</td></tr><tr><td>P3</td><td>2020-09-12, 20:00:00-2020-09-12, 23:00:00</td><td>2500-3800</td></tr><tr><td>P4</td><td>2020-09-14, 00:00:00-2020-09-14, 03:00:00</td><td>5500-7500</td></tr><tr><td>P5</td><td>2020-09-14, 22:00:00-2020-09-15, 02:00:00</td><td>5500-6500</td></tr><tr><td>P6</td><td>2020-09-15, 02:00:00-2020-09-15, 04:00:00</td><td>4500-7200</td></tr><tr><td>P7</td><td>2020-09-17, 22:00:00-2020-09-18, 03:00:00</td><td>5400-8500</td></tr><tr><td>P8</td><td>2020-09-18, 20:00:00-2020-09-18, 22:00:00</td><td>4800-6500</td></tr><tr><td>P9</td><td>2020-09-20, 20:00:00-2020-09-21, 00:00:00</td><td>4400-6200</td></tr></tbody></table>

in Fig. 5, are also significant, such as lidar ratios on 12 and 14 September, and the PLDRs on 11 and 18 September. Such variations are possibly indications of the variabilities in the burning materials, combustion conditions, convective lifting and aging process. Two events corresponding to the Creek fire and the Oregon fire, respectively, are selected and analyzed in detail in the next section.

# 3 Case study

## 3.1 Case 1: 11–12 September 2020

The BBA plumes detected on the night of 11–12 September 2020 are attributed to the Creek fire and traveled about 5–7 d. Figure 6a shows the 4 d back trajectories overlaid with the UVAI map on 8 September 2020. Two areas with intense UVAI are indicated on the map, one over the West Coast of the USA and the other one over the Great Lakes.

The former was mostly generated by the Oregon fire, which started on 7 September. The latter was emitted by the Creek fire from 4 to 6 September and transported to Europe via an “expressway”. Figure 7 shows the range corrected lidar signal (RCS) and volume linear depolarization ratio (VLDR) and calibrated signal ratio between 466 and 387 nm channel, i.e., $\frac{CR P_{466}(z)}{CF P_{387}(z)}$. The fluorescence observations are only available at night when there is no sunlight interference. The BBA layer was mainly distributed at 5000–10 000 m and was characterized by strong fluorescence. In Fig. 7b, ice particles featured with increased depolarization ratios were detected within high smoke layers, for example, at 8000–10 000 m at 17:00–18:00 UTC.

Figure 8 plots the parameters obtained from averaged observations between 22:00 UTC, 11 September, and 03:00 UTC, 12 September. The extinction coefficients peaked at about 6200 m, with $180 \text{ Mm}^{-1}$ at 355 nm and $140 \text{ Mm}^{-1}$ at 532 nm. The $\text{EAE}_{355-532}$ was about $0.5 \pm 0.3$ and the $\text{BAE}_{355-532}$ was about $2.0 \pm 0.3$. The $\text{EAE}_{355-532}$ is lower than the $\text{AE}_{340-500}$ measured at NASA_Ames when influenced by the Creek fire plumes, indicating the particle growth during the aging process. The lidar ratios, which are $40 \pm 6$ sr at 355 nm and $70 \pm 11$ sr at 532 nm, are typical values of aged smoke particles (Haarig et al., 2018; Hu et al., 2019; Ohneiser et al., 2020; Peterson et al., 2018). The PLDRs show strong vertical variations in the BBA layer. In the core of the smoke, i.e., 5000–6000 m, the PLDRs at the three wavelengths are all below 0.03. In the plume edge, i.e., 6500–9000 m, the PLDRs at 355 and 532 nm increased significantly, with about $0.15 \pm 0.03$ at 355 nm and $0.12 \pm 0.02$ at 532 nm. $\text{PLDR}_{1064}$ shows no significant vertical variations. A slight decreasing trend in the $\text{EAE}_{355-532}$ and a moderate one in $\text{BAE}_{355-532}$ are observed when the height increases.
<figure><img src="image_7.png" /><figcaption>**Figure 4.** Lidar and sun/sky photometer observations during the smoke episodes on 10–22 September 2020, ATOLL, France. (a) The range corrected lidar signal at 1064 nm. (b) The volume depolarization ratio at 1064 nm. (c) The AOD and AE measured by the sun/sky photometer operated at ATOLL. The layers with strong depolarization appearing in the boundary layer on 14–16 September are polluted dust from the Saharan region. The smoke layers from Californian smoke are mostly distributed in the free troposphere.</figcaption></figure>

BBA particles at 5000–6000 m was also characterized with stronger fluorescence capacity (~3.8 × 10⁻⁴) compared with those at 6500–9000 m. According to laboratory studies, the main fluorophores in smoke are the humic-like substance and PAHs (Garra et al., 2015; Zhang et al., 2019), which are common products of the combustion of biomass, as well as some SOA formed in the aging process (Lee et al., 2013). Therefore, temporal and spatial variations of fluorescence capacity are very likely during the transport, and such variation is controlled by factors such as oxidation and evaporation of some chemical species and so on.

Figure 8g presents the water vapor mixing ratio (WVMR) and relative humidity (RH) profiles measured by radio sounding at Beauvechain station (Belgium), 120 km to

ATOLL platform. The RH with respect to ice (RHice) was calculated with the radio sounding measurements (Jarraud, 2008). The presence of the BBA layer is well reflected by the enhanced values in the WVMR profile. It indicates that the BBA plumes were also captured by the radio sounding measurements at Beauvechain due to the plumes’ large spatial coverage. The WVMR in the core of the plume is obviously higher than at the plume edge, suggesting that the WVMR is an important factor in the aging process.

## 3.2 Case 2: 17–18 September 2020

The smoke layers at 5000–9000 m from 17 to 18 September 2020 (Fig. 9) are attributed to the Oregon fire, as shown in
<figure><img src="image_8.png" /><figcaption>**Figure 5.** Box plots of the variabilities of BBA intensive parameters during the smoke episodes in September 2020. P1, P2, ..., P9 refer to the time intervals defined in Table 1. Only nighttime observations are considered in this analysis. The measurements in the time intervals are averaged. The lower and upper edges of the box represent, respectively, the first and third quartiles of data. The lower and upper range bars represent, respectively, the minimum and maximum. The dot and bar in the box indicate the mean value and the median value, respectively. (a) Lidar ratios and (b) PLDRs. The colors of the plots represent the different wavelengths (magenta: 355 nm; green: 532 nm; red: 1064 nm). (c) Fluorescence capacity (in cyan), (d) EAE<sub>355-532</sub> (in blue) and BAE<sub>355-532</sub> (in orange).</figcaption></figure>

<figure><img src="image_9.png" /><figcaption>**Figure 6.** HYSPLIT back trajectories overlaid on the UVAI measured by OMPS onboard SUOMI-NPP satellite. The (a) 96 h back trajectories ending at 00:00 UTC, 12 September 2020, overlaid with UVAI on 8 September. The (b) 144 h back trajectories ending at 00:00 UTC, 18 September 2020, overlaid with UVAI on 14 September. © Google Earth.</figcaption></figure>
<figure><img src="image_10.png" /><figcaption>**Figure 7.** Lidar observations from 11 to 12 September 2020. (a) Range corrected lidar signal at 1064 nm, (b) volume depolarization ratio at 1064 nm and (c) calibrated signal ratio between 466 and 387 nm channels, i.e., $\frac{C_R P_{466}}{C_F P_{387}}$ in Eq. (1). This quantity is used as an intermediate parameter to represent the fluorescence signal. The calibration coefficient, $C_R/C_F$, represents the ratio of the electro-optical gain between the two channels. The white zone in the figures represents missing data due to the turnoff of the detectors (e.g., to avoid sunlight interferences) or intermediate operations during the measurements.</figcaption></figure>

Fig. 6b. The plumes covered large areas of America and the eastern Pacific Ocean and underwent 7–12 d of transport before arriving at the observation site ATOLL, France.

Profiles obtained from averaged measurements between 22:30 UTC, 17 September, and 03:00 UTC, 18 September are plotted in Fig. 10. Compared with Case 1, BBA plumes in Case 2 have lower extinction coefficients, $\text{EAE}_{355-532}$, lidar ratios and higher PLDRs. The $\text{EAE}_{355-532}$ is around $-0.30 \pm 0.30$, obviously lower than in Case 1. It can be ex-

plained by the longer travel time in Case 2, making the BBA particles bigger. Particle growth during transport has been reported in previous aged smoke observations (Müller et al., 2007; Hu et al., 2019; Bian et al., 2020). The lidar ratios are $24 \pm 4$ sr at 355 nm and $50 \pm 8$ sr at 532 nm, lower than the values in Case 1 and in most previous studies (Haarig et al., 2018; Hu et al., 2019; Ohneiser et al., 2020). Such low lidar ratios were detected by Ortiz-Amezcua et al. (2017) in long-range transported North American smoke over two
<figure><img src="image_11.png" /></figure>

**Figure 8.** Aerosol vertical profiles from averaged measurements between 22:00 UTC, 11 September 2020, and 03:00 UTC, 12 September 2020. (a) Extinction coefficients, (b) backscattering coefficient and (c) lidar ratios. The colors of lines represent different wavelengths: 355 (magenta), 532 (green) and 1064 (red) nm. (d) EAE<sub>355–532</sub> (orange), BAE<sub>355–532</sub> (blue) and temperature (cyan open circles), (e) PLDRs, (f) fluorescence backscattering coefficient (pink) and fluorescence capacity (cyan), (g) WVMR (solid pink circles), RH to liquid water (RH, solid cyan circles) and ice (RH<sub>ice</sub>, solid gray circles). The extinction and backscatter coefficients at 355 and 532 nm were calculated using the Raman technique (Ansmann et al., 1992) and the backscatter coefficient at 1064 nm was calculated by the Klett method with an assumption of LR = 50 sr. The radio sounding station is in Beauvechain, Belgium, about 100 km from the lidar observation site. The error bars in the figure represent the statistical errors. The method of error estimation is presented in the Appendix of Hu et al. (2019). The relative humidity to ice is calculated using the improved Magnus formula in Alduchov and Eskridge (1996).

European lidar stations, Leipzig (Germany) and Granada (Spain). The observations in Ortiz-Amezcua et al. (2017) showed mean EAE<sub>355–532</sub> of 0.2–0.3, and mean lidar ratios of 23–25 sr at 355 nm and 47–51 sr at 532 nm. The PLDRs in Case 2 are 0.15 ± 0.03 to 0.18 ± 0.04 at 355 nm, 0.12 ± 0.02 to 0.14 ± 0.03 at 532 nm and about 0.02 at 1064 nm, higher than those in Case 1, especially at shorter lidar wavelengths. The fluorescence capacity varied in 2.0–2.8 × 10<sup>-4</sup> at 5300–8000 m, which is 26%–47% lower than that in the plume core, and comparable with that in the plume edge in Case 1. This decrease of fluorescence capacity may be linked to the evaporation of organic species when the BBA plumes are diluted during the transport (Hodshire et al., 2021).

In Fig. 10e, a sharp increase in PLDR<sub>1064</sub> to nearly 0.10 was detected at 8600 m, indicating the presence of ice crystals. At such altitude, the temperature was about -41 to -34 °C and the RH<sub>ice</sub> was 100%–120%, according to global data assimilation system (GDAS) model data and radio sounding measurements. Lidar signals before and during the presence of cirrus have been averaged and shown in Fig. 11. The fluorescence backscattering coefficient in the cirrus layer is as high as before the presence of ice crystals, indicating that the cirrus layer contains non-negligible BBA particles. This observation is an indication of BBA particles acting as INP, although the possibility that ice crystals formed elsewhere cannot be excluded. Considering that cloud cover-

age is quite low over northern France on 17–18 September, these ice crystals were very likely formed through deposition freezing mode or pore condensation and freezing mode (Cziczo et al., 2013; Umo et al., 2019).

## 4 Discussion

In this study, the PLDRs of BBA originating from wildfires showed obvious variations dependent on different fire activities, different altitudes and the water vapor content of the BBA layers. The BBAs originating from the Oregon fire generally had higher PLDRs than those from the Creek fire. Such a feature is probably due to the differences in burning vegetation type, combustion conditions and lifting process. During the episodes of transported Canadian smoke over Europe, lidar systems in Leipzig and Lille both found that the tropospheric BBA plumes had much lower PLDRs than the plumes simultaneously presenting in the UTLS (Haarig et al., 2018; Hu, 2018). In Case 1, the increase of PLDRs with altitude was observed in the BBA layer. This correlation between aged BBA PLDRs and altitude is likely driven by the altitude-dependent factors in the atmosphere, such as RH, temperature, etc., which influence the BBA particles’ morphology in the aging process (Yu et al., 2019; Ohneiser et al., 2020; Ansmann et al., 2021). The organic aerosols, the main contributor of the BBA mass, can exist in an amor-
<figure><img src="image_12.png" /><figcaption>**Figure 9.** The same plot as Fig. 7 but for lidar observations from 17 to 18 September 2020. (a) Range corrected lidar signal at 1064 nm, (b) volume depolarization ratio at 1064 nm and (c) calibrated signal ratio between 466 and 387 nm channels.</figcaption></figure>

phous state, in response to temperatures and RH (Koop et al., 2011; Berkemeier et al., 2014; Knopf et al., 2018). Studies have demonstrated that the evaporation of condensed liquid water on the surface of BBA contributes strongly to the collapse of fractal-like aggregates into compact particles (Kütz and Schmidt-Ott, 1992; Ma et al., 2013). The concentration of BBA particles, which generally decrease during transport and aging, could also impact the evaporation and coagulation of particle aging, thus modifying the particles’ morphology (Hodshire et al., 2021).

The lower lidar ratios detected in Case 2 of this study were rarely observed in previous lidar measurements. The

decrease in lidar ratios in the Oregon plumes could be an indication of the decreased aerosol absorption, according to the modeling of aerosol optical properties (Gialitaki et al., 2020; Liu and Mishchenko, 2020). Different scattering models have been considered to understand how aerosol composition, morphology and mixing state influence BBA absorption. Liu and Mishchenko (2018) used 11 different morphology models, ranging from bare soot to completely embedded soot mixtures, and found that the absorption enhancement is affected by the particle size, morphology and the thickness of coating. Moreover, the combustion and aging processes, as well as the environment conditions, could also contribute
<figure><img src="image_13.png" /></figure>

**Figure 10.** The same as Fig. 8 except for observations between 22:30 UTC, 17 September 2020, and 03:00 UTC, 18 September 2020. The radio sounding measurements are from Herstmonceux, England, which is about 200 km from the observation site. Radio sounding at Beauvechain, Belgium, was not available on that day.

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

**Figure 11.** The profiles of averaged parameters in two consecutive periods: 20:30–22:30 UTC, 17 September 2020 (before the observation of ice crystals and in lighter colors), and 22:30–23:30 UTC, 17 September 2020 (during ice crystal observation and in darker colors). The dashed-dotted line represents the altitude where the ice crystals appeared. (a) Backscattering coefficient at 532 nm, (b) fluorescence capacity at 466 nm, (c) fluorescence backscattering coefficient and (d) PLDR at 1064 nm.

to the variability of BBA absorption. More efforts in the characterization of wildfire emissions and the modeling of BBA scattering are required to answer this question.

The fluorescence signal brings new information for the characterization of aerosol properties. In previous studies we

showed that the fluorescence signal is a good reference for aerosol classification (Veselovskii et al., 2020, 2021b). In this study, we have shown that the fluorescence capacity is correlated with the optical properties of BBA particles. As the fluorescence signal is attributed to certain chemical species, the
variation of the fluorescence capacity directly reflects their abundance in BBAs, which is controlled by the combustion process, which determined their original concentration, and the aging process, consisting of complex processes such as the oxidation, evaporation of versatile species, the condensation of gases and so on. For example, the decrease in fluorescence capacity at the plume edge in Case 1 is likely due to the evaporation of some fluorescence organic species when the BBA plume is diluted.

A handful of studies have shown that BBAs may serve as INP (McCluskey et al., 2014; Jahn et al., 2020; Jahl et al., 2021), but existing results of ice nucleation onset conditions are highly variable. Laboratory studies on organic INPs are mostly limited to pure organics, such as sucrose and levoglucosan, etc., while OA in ambient conditions have complex origins. As a result, the conditions for initiating ice nucleation required by different organics are highly variable in literature data, which blocked us from clarifying the role of organic aerosols in ice formation (Kanji et al., 2017). (Veselovskii et al., 2021a) presented that one can estimate the particle concentration even in thin aerosol layers using the fluorescence signal, which offers a new opportunity for the studies of aerosol-cloud interactions. A paper about the estimation of BBA surface concentration in freshly formed cirrus layers using fluorescence measurements collected at ATOLL platform has been presented by (Veselovskii et al., 2021a).

## 5 Conclusions

This study reported the observations of long-range transported BBA plumes originating from wildfires in North America in September 2020. After 1–2 weeks of transport, the emitted BBA plumes in the troposphere were detected by LILAS, a multi-wavelength Mie–Raman-polarization-fluorescence lidar in ATOLL, France. Our results confirmed the main typical features of aged BBA particles, i.e., the decreased Angström exponent after long-range transport, enhanced PLDRs at shorter wavelengths and a lidar ratio at 532 nm greater than at 355 nm, that have been reported in previous research. Moreover, our results demonstrated that the properties of BBAs have strong variations. The PLDR varied from 0.03 (0.02) to 0.22 (0.16) at 355 (532) nm during the observations in September. Very specific lidar ratios, 24 ± 4 sr at 355 nm and 50 ± 8 sr at 532 nm, which are lower than those of most previous observations, were detected in the transported BBA plume from the Oregon fire. These characteristics reflect that the BBA properties, such as morphology and absorption, are highly dependent on complex factors in the combustion (vegetation type, burning temperature, wind conditions, etc.) and aging (humidities, temperature, etc.) processes. These variations need to be resolved and should be considered in the representation of BBAs in the climate model. The fluorescence backscattering coefficient

and fluorescence capacity turned out to be useful and supplementary information for BBA characterization, due to the high sensitivity to the presence of fluorophores in BBAs. The fluorescence capacity allows for an efficient identification of BBA particles and the quantification of fluorescent aerosols at low concentration, as has been presented in Veselovskii et al. (2020). The fluorescence signal also presents the opportunity to study BBA particles inside cirrus clouds, as shown in this study and Veselovskii et al. (2021a). However, additional observations on different aerosol types and spectral fluorescence information are still needed to refine the study. A new fluorescence lidar with a more powerful laser and multiple fluorescence channels is now under development in order to advance the studies of aerosols and aerosol-cloud interactions.

**Data availability.** The data are available upon request.

**Supplement.** The supplement related to this article is available online at: https://doi.org/10.5194/acp-22-5399-2022-supplement.

**Author contributions.** QH performed lidar measurements, developed the code for data analysis and wrote the manuscript. PG is the PI of the project, supervised the experiments and improved the manuscript. IV helped in data analysis and establishment of the scientific arguments. TP helped perform lidar measurements and is in charge of the maintenance, automatization and operation of the lidar system.

**Competing interests.** The contact author has declared that neither they nor their co-authors have any competing interests.

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

**Acknowledgements.** We acknowledge the CaPPA project (Chemical and Physical Properties of the Atmosphere), funded by the ANR (French National Research Agency) through the PIA (Programme d'Investissement d'Avenir) under contract "ANR-11-LABX-0005-01", the Regional Council "Hauts-de-France" (project CLIMIBIO) and the FEDER (European Funds for Regional Economic Development) for the financial support. We also thank the following communities and individuals for sharing their data and expertise: Service National d'Observation PHOTONS/AERONET-EARLINET, ESA/QA4EO, AERONET (PIs of the sites involved in this study: Roy Johnson, Brent Holben, Philippe Goloub), Russian Science Foundation (project 21-17-00114) and Agora-LAB.
**Financial support.** This research has been supported by the Agence Nationale de la Recherche (grant no. ANR-11-LABX-0005-01), the European Regional Development Fund (FEDER), and the "Hauts de France" Regional Council (project CLIMIBIO).

Publisher's note: the article processing charges for this publication were not paid by a Russian or Belarusian institution.

**Review statement.** This paper was edited by Eduardo Landulfo and reviewed by two anonymous referees.

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