Radiative Effect and Mixing Processes of a Long-Lasting Dust Event over Athens, Greece, during the COVID-19 Period

: We report on a long-lasting (10 days) Saharan dust event affecting large sections of SouthEastern Europe by using a synergy of lidar, satellite, in-situ observations and model simulations over Athens, Greece. The dust measurements (11–20 May 2020), performed during the conﬁnement period due to the COVID-19 pandemic, revealed interesting features of the aerosol dust properties in the absence of important air pollution sources over the European continent. During the event, moderate aerosol optical depth (AOD) values (0.3–0.4) were observed inside the dust layer by the ground-based lidar measurements (at 532 nm). Vertical proﬁles of the lidar ratio and the particle linear depolarization ratio (at 355 nm) showed mean layer values of the order of 47 ± 9 sr and 28 ± 5%, respectively, revealing the coarse non-spherical mode of the probed plume. The values reported here are very close to pure dust measurements performed during dedicated campaigns in the African continent. By utilizing Libradtran simulations for two scenarios (one for typical midlatitude atmospheric conditions and one having reduced atmospheric pollutants due to COVID-19 restrictions, both affected by a free tropospheric dust layer), we revealed negligible differences in terms of radiative effect, of the order of +2.6% (SW BOA , cooling behavior) and +1.9% (LW BOA , heating behavior). Moreover, the net heating rate (HR) at the bottom of the atmosphere (BOA) was equal to +0.156 K/d and equal to +2.543 K/d within 1–6 km due to the presence of the dust layer at that height. On the contrary, the reduction in atmospheric pollutants could lead to a negative HR ( − 0.036 K/d) at the bottom of the atmosphere (BOA) if dust aerosols were absent, while typical atmospheric conditions are estimated to have an almost zero net HR value (+0.006 K/d). The NMMB-BSC forecast model provided the dust mass concentration over Athens, while the air mass advection from the African to the European continent was simulated by the Hybrid Single-Particle Lagrangian Integrated Trajectory (HYSPLIT) model.


Introduction
Dust aerosols have a large impact on climate, cloud formation, the precipitation cycle, aviation safety, and, finally, human health [1][2][3][4][5][6][7][8][9]. More specifically, their impact on climate concerns the direct and the indirect effects on the Earth's atmosphere radiation budget. The direct effect includes the scattering and absorbing role of these aerosols on the short-and

Instrumentation and Simulation Tools/Models
In order to analyze this strong event, we used a synergy of ground-based remote sensing (lidar) measurements, satellite data and complementary forecast/simulation and radiative transfer models. A short description of each tool used in this study is presented in next sub-sections.

Lidar Systems at the National Technical University of Athens (NTUA)
The campus of the National Technical University of Athens (NTUA) is located inside the Athens Basin (37.96 • N, 23.78 • E, elevation 220 m asl. Figure 1). The advanced elastic-Raman lidar system aErosol and Ozone Lidar systEm (EOLE) of the Laser Remote Sensing Unit (LRSU) of NTUA [63] is based on a pulsed Nd:YAG laser system which emits, simultaneously, pulses at 354.93-532-1064.2 nm, with energies of 240-310-260 mJ, respectively, at 10 Hz repetition frequency. The laser beam containing all three wavelengths is expanded 3-times by an achromatic Galilean telescope before being emitted in the atmosphere. A Cassegrainian telescope of 300 mm diameter (focal length 600 mm) collects all elastically backscattered lidar signals (354.93-532-1064.2 nm), as well as those generated by the spontaneous vibrational-rotational Raman effect (by atmospheric N 2 at 386.6 and 607.4 nm, as well as by H 2 O at 407.5 nm), within a field of view of 1.5 mrad. Thus, EOLE is able to provide independent and simultaneous measurements of the vertical profiles of the aerosol backscatter β aer (at 355, 532, and 1064 nm) and extinction α aer (at 355 and 532 nm) coefficients, as well as the water vapor mixing ratio in the troposphere. Furthermore, EOLE provides the vertical profiles of the aerosol intensive parameters, namely the backscatterand extinction-related Ångström exponents (AE α355/532 , AE b355/532 , AE b532/1064 ), as well as the lidar ratio (LR) at 355 and 532 nm. The full overlap of EOLE is reached at~800 m asl.

Instrumentation and Simulation Tools/Models
In order to analyze this strong event, we used a synergy of ground-based remote sensing (lidar) measurements, satellite data and complementary forecast/simulation and radiative transfer models. A short description of each tool used in this study is presented in next sub-sections.

Lidar Systems at the National Technical University of Athens (NTUA)
The campus of the National Technical University of Athens (NTUA) is located inside the Athens Basin (37.96° N, 23.78° E, elevation 220 m asl. Figure 1). The advanced elastic-Raman lidar system aErosol and Ozone Lidar systEm (EOLE) of the Laser Remote Sensing Unit (LRSU) of NTUA [63] is based on a pulsed Nd:YAG laser system which emits, simultaneously, pulses at 354.93-532-1064.2 nm, with energies of 240-310-260 mJ, respectively, at 10 Hz repetition frequency. The laser beam containing all three wavelengths is expanded 3-times by an achromatic Galilean telescope before being emitted in the atmosphere. A Cassegrainian telescope of 300 mm diameter (focal length 600 mm) collects all elastically backscattered lidar signals (354.93-532-1064.2 nm), as well as those generated by the spontaneous vibrational-rotational Raman effect (by atmospheric N2 at 386.6 and 607.4 nm, as well as by H2O at 407.5 nm), within a field of view of 1.5 mrad. Thus, EOLE is able to provide independent and simultaneous measurements of the vertical profiles of the aerosol backscatter βaer (at 355, 532, and 1064 nm) and extinction αaer (at 355 and 532 nm) coefficients, as well as the water vapor mixing ratio in the troposphere. Furthermore, EOLE provides the vertical profiles of the aerosol intensive parameters, namely the backscatter-and extinction-related Å ngström exponents (AEα355/532, AEb355/532, AEb532/1064), as well as the lidar ratio (LR) at 355 and 532 nm. The full overlap of EOLE is reached at ~800 m asl.  diameter telescope (Dall-Kirkham Cassegrainian), with focal length f = 1000 mm, which collects the elastically backscattered lidar signals at 355 nm (at two polarization planes: parallel and perpendicular), which are optically separated by a polarizing beam splitter cube. The full overlap of DEPOLE is reached at~500 m asl. [63]. The average (systematic and statistical) uncertainty of the vertical profile of the particle depolarization ratio (δ p ) is less than 15% [64][65][66].
By using the Raman technique, as proposed in [46,47], the β aer and α aer vertical profiles are retrieved with systematic uncertainties of ∼5-15% and ∼10-25%, respectively [67,68]. Therefore, the corresponding uncertainty of the retrieved LR values is of the order of 11-30%, while the uncertainty for AE β and AE α ranges between 0.02-0.04 and 0.03-0.08, respectively, as estimated by propagation error calculations. Both lidars are designed according to the optical set-up of a typical EARLINET station [69], following all the EAR-LINET quality assurance tests and standards [64,70], while the primary aerosol products (α aer and β aer ) are retrieved by using the EARLINET Single Calculus Chain (SCC) [65,66].
The process followed for the estimation of the optical properties from the lidar signal is summarized below: an aerosol-free reference height window has to be detected initially, where the normalized range-corrected lidar signal sufficiently fits the calculated attenuated molecular backscatter coefficient (Rayleigh-fit criterion) [64]. For this, the user provides the SCC input platform with an initial guess of that range (in our case, 6-12 km based on visual inspection of the range-corrected lidar signal), and the corresponding algorithm fine tunes this guess by applying different statistical tests to ensure that the shape of the measured signal corresponds to the shape of a Rayleigh signal [66]. Afterwards, the retrieval of the aerosol optical properties from the lidar signal starts from the identified reference height using the assumption of the lidar ratio value (Klett technique), or from the utilization of the Raman channel (Raman technique), for the case of daytime and nighttime retrievals, respectively.

Optical Particle Counter at the National Centre of Scientific Research (NCSR) "Demokritos"
The National Centre of Scientific Research (NCSR) "Demokritos" is situated about 7 km to the north from downtown Athens ( Figure 1). It is representative of the atmospheric aerosol at suburban areas of the Athens Metropolitan area. At "Demokritos" station, among other instruments, an optical particle counter (OPC, Grimm 107@660 nm laser light wavelength) is in operation so as to acquire the particle size distribution in the size range of 250 nm to 10 µm optical diameter. The OPC in an intercomparison at the WCCAP (World Calibration Centre for Aerosol Physics) exhibited a counting accuracy within 10% for the size range 250 nm to 1 µm [71]. The instrument acquires a full-size distribution every 1 min, while it uses a laser light at 660 nm wavelength. According to [72], during African dust outbreaks, the coarse aerosol mode (PM 1 -PM 10 ) increases by 43-46%. We acquired PM 1 and PM 10 concentrations by using the OPC aerosol particle size distribution and an aerosol density of 1 g/cm 3 . Based on the increase in the coarse aerosol mode, we examine the influence of Saharan dust at ground level.

WRF-Chem Model
We use the limited area of the WRF-Chem model [73,74] at 12 × 12 km grid-space. Initial and boundary conditions are taken from the National Centers for Environmental Prediction (NCEP) operational Global Forecast System (GFS) model for the atmospheric parameters and from the NCEP operational SST for the sea surface temperature. The physical parameterizations of the model include the Mellor-Yamada-Janjic planetary boundary layer scheme [75], the Noah Land Surface Model for land properties [76], the Grell and Devenyi cloud convection scheme [73] and the Rapid Radiative Transfer Model for the short-wave and long-wave radiation. Dust emission is parameterized using the Air Force Weather Agency (AFWA) scheme [77] that includes five dust size bins with effective radii of 0.73, 1.4, 2.4, 4.5 and 8 µm, respectively.

MODIS Satellite Data
The Moderate Resolution Imaging Spectroradiometer (MODIS) on-board the Terra and Aqua satellites is an operational satellite sensor which, among others, also performs observations of atmospheric aerosols. Particularly, MODIS has been providing Aerosol Optical Depth (AOD) retrievals at 500 nm since 2000, twice daily (under cloud-free conditions) on a near-global basis with high spatial resolution, and has acquired a well-respected status as one of the most reliable satellite datasets of AOD over ocean and land [78,79]. Besides AOD, there are several other aerosol properties that are retrieved by MODIS (e.g., Ångström exponent, refractive index), which will not be used in the frame of this paper. Their retrieval is easiest over dark (in visible wavelengths) surfaces and, therefore, the first family of algorithms used by MODIS was the so-called "Dark Target" over land [80] and ocean [81,82].

DREAM Dust Model
The NMMB/BSC-Dust model [83,84] provides online short to medium-range weather and dust forecasts from regional to global scales. It has been developed at the Barcelona Supercomputing Center-Centro Nacional de Supercomputación (BSC-CNS). At a global scale, NMMB/BSC is ranked among the best of AEROCOM dust models in terms of performance statistics for surface concentration, deposition and aerosol optical depth (AOD). At regional scale, the model reproduces significantly well the daily variability and seasonal spatial distribution of the dust optical depth over Northern Africa, the Middle East and Europe. It provides 24 vertical sigma-hybrid layers, having a 0.3 • × 0.3 • horizontal resolution for each 72-h daily forecast. The meteorological fields are initialized every 24 h (at 12:00 UTC) with the NCEP global analysis (0.5 • × 0.5 • ), and boundary conditions are updated every 6 h with the NCEP GFS.

HYSPLIT Trajectory Model
The Hybrid Single-Particle Lagrangian Integrated Trajectory model (HYSPLIT), developed by NOAA's Air Resources Laboratory (ARL) (https://www.ready.noaa.gov (accessed on 22 December 2020) [85]), was used to study the atmospheric transportation of the dust particles during this extreme dust event. For the analysis of the backward air mass trajectories, we used the "normal" method, along with the GDAS1 (Global Data Analysis System) meteorological data. The vertical motion used to calculate the trajectories was the model vertical velocity. The initial values used to run the model were the coordinates of the NTUA lidar station and the altitude (asl.) of the dust aerosol layers observed. The duration of the backward air mass trajectories was set to 120 h, which is a typical duration to characterize dust air masses in the Eastern Mediterranean [24,35]

Synoptic Meteorological Description of the 11-20 May 2020 Dust Event
The weather conditions that favored this extreme dust event included a south-westerly jet at the lower tropospheric levels that was stream placed between a trough over Southwest Europe and a strengthening ridge over Southeastern Europe. The relative position of these two systems is evident in the upper tropospheric maps in Figure 2 from the WRF model at 12 × 12 km grid space, on 14 May 2020 15:00 UTC. As seen in Figure 2a, the jet stream at 200 mb is located at relatively southern latitudes (25 • N-33 • N), with wind speeds exceeding 60 m/s over Algeria. At 500 mb height (Figure 2b), the center of the trough is located over the southwest parts of the Iberian Peninsula, while strong pressure gradients are evident over the arid areas of Algeria and Tunis. This combination of weather systems is responsible for the formation of the strong "Khamsin" winds that mobilize large amounts of Saharan dust in the area [86]. At the same time, the formation of a persisting high-pressure system over the eastern part of the Mediterranean (Figure 2b) resulted in the recirculation of the elevated dust layers over Greece and Turkey.
winds that mobilize large amounts of Saharan dust in the area [86]. At the same time, formation of a persisting high-pressure system over the eastern part of the Mediterran (Figure 2b) resulted in the recirculation of the elevated dust layers over Greece and T key.  Overall, two distinct transport paths of the air masses can be observed during the study period: (a) 10-15 May 2020 (phase 1), when fresh dust is transported from the Sahara towards SE Europe, and (b) 15-20 May 2020 (phase 2), when aged dust is trapped in a recirculating pattern over Greece. This is also supported later on (Section 3.2) by the HYSPLIT back-trajectories ( Figure 4), but also from the retrieved aerosol optical properties (see also Figures 8 and 9).  Overall, two distinct transport paths of the air masses can be ob study period: a) 10-15 May 2020 (phase 1), when fresh dust is transp  (19:00 UTC), the air mass trajectories starting from the North-Eastern Sahar passed over Italy, the Balkans region and then over the industrial regions o (Turkey), following an anticyclonic flow formed around a high-pressure sy Greece before their arrival over Athens (see also Figure 3). The increased resid over Greece that is evident, for example, at 18, 19 and 20 May in Figure 4 resul aged particles being detected by the lidar system over Athens.

Dust Model Simulations
The NMMB/BSC-Dust estimations of the vertical evolution of dust mass c tion (μg/m 3 ) over Athens are presented in Figure 5. The dust mass concentration 2, 4 and 6 km height (approximately base, center and top, respectively) are within a 6-h interval. According to the model, the massive export of dust load 10 May (00:00 UTC) and gradually ended on 22 May (18:00 UTC), with a total d 300 h. During the first 6 days of the event, the maximum concentration values o concentration peaked at ~402 μg/m 3 on 12 May (12:00 UTC) at a height of 4 k values gradually became smaller during the following days, while the dust pa mained present between 2-4 km height asl. On the contrary, the dust concentr ues at 2 km became larger on the 6 th day of the event (18 May), shifting the cent of the estimated layers to lower heights. At 6 km height asl., the dust mass con remained below 100 μg/m 3 throughout the event. Finally, the aerosol mass con

HYSPLIT Backward Trajectory Analysis
The path travelled by the observed dust layers from Northern Africa to Athens was also verified using an air mass backward trajectory analysis based on the HYSPLIT simulation model ( Figure 4). As can be seen in Figure 4 (first row), the air masses which arrived over Athens from 11 to 15 May at 10:00 UTC seemed to follow a similar pattern. They originated from North-Western Africa (Algeria, Mali, Mauritania), deep in the Saharan desert. After leaving the African continent, they followed an almost straight route towards Greece. Between 15 May (19:00 UTC) and 18 May (10:00 UTC), the air mass trajectories are slightly shifted to North-Eastern latitudes over Athens ( Figure 4, second row), passing over Algeria, Tunisia and Libya. Later, from 18 May (19:00 UTC) to 20 May (19:00 UTC), the air mass trajectories starting from the North-Eastern Saharan region passed over Italy, the Balkans region and then over the industrial regions of Istanbul (Turkey), following an anticyclonic flow formed around a high-pressure system over Greece before their arrival over Athens (see also Figure 3). The increased residence time over Greece that is evident, for example, at 18, 19 and 20 May in Figure 4 results in more aged particles being detected by the lidar system over Athens.

Dust Model Simulations
The NMMB/BSC-Dust estimations of the vertical evolution of dust mass concentration (µg/m 3 ) over Athens are presented in Figure 5. The dust mass concentration values at 2, 4 and 6 km height (approximately base, center and top, respectively) are depicted within a 6-h interval. According to the model, the massive export of dust load started on 10 May (00:00 UTC) and gradually ended on 22 May (18:00 UTC), with a total duration of 300 h. During the first 6 days of the event, the maximum concentration values of the dust concentration peaked at~402 µg/m 3 on 12 May (12:00 UTC) at a height of 4 km. These values gradually became smaller during the following days, while the dust particles remained present between 2-4 km height asl. On the contrary, the dust concentration values at 2 km became larger on the 6th day of the event (18 May), shifting the center of mass of the estimated layers to lower heights. At 6 km height asl., the dust mass concentration remained below 100 µg/m 3 throughout the event. Finally, the aerosol mass concentration at the aforementioned altitudes in the free troposphere tend to zero value on 22 May, at 18:00 UTC. Considering the models' performance, there is quite good agreement of the estimated geometrical properties (base, top, thickness) when compared to the ones observed by EOLE lidar, as we will see in Figure 8a. at the aforementioned altitudes in the free troposphere tend to zero value on 22 May, at 18:00 UTC. Considering the models' performance, there is quite good agreement of the estimated geometrical properties (base, top, thickness) when compared to the ones observed by EOLE lidar, as we will see in Figure 8a. From the in-situ measurements performed at ground level at NCSR "Demokritos", we observe that while PM1 concentration (mainly representing local emissions) remains almost stable and at low levels, PM10 concentration increases rapidly on the 13 May, until 21 May.
As detected by the lidar, the dust layers remained detached during the study period. This is also reproduced in the model by the very low concentrations of dust at ground level compared to the free troposphere. The increase in PM10 concentrations, which is evident in ground measurements after 16 May, is probably related to downward turbulent mixing of dust particles inside the Planetary Boundary Layer (PBL). This increase is also depicted in the modeled surface concentrations of dust; however, it is overestimated by 50-80 μg/m 3 ( Figure 5). Such local scale processes inside the PBL cannot be easily re- From the in-situ measurements performed at ground level at NCSR "Demokritos", we observe that while PM 1 concentration (mainly representing local emissions) remains almost stable and at low levels, PM 10 concentration increases rapidly on the 13 May, until 21 May.
As detected by the lidar, the dust layers remained detached during the study period. This is also reproduced in the model by the very low concentrations of dust at ground level compared to the free troposphere. The increase in PM 10 concentrations, which is evident in ground measurements after 16 May, is probably related to downward turbulent mixing of dust particles inside the Planetary Boundary Layer (PBL). This increase is also depicted in the modeled surface concentrations of dust; however, it is overestimated by 50-80 µg/m 3 ( Figure 5). Such local scale processes inside the PBL cannot be easily reproduced at the mesoscale resolution of the model (0.3 • × 0.3 • ), especially for regions of complex topography [87], thus explaining the discrepancy between modeled and measured values, especially at ground level.

Ground-Based Aerosol Lidar Observations
Ground-based lidar observations were used to illustrate the spatio-temporal evolution of the dust aerosol stratification during the measuring period (>50 h of measurements) (see Figure 7). According to the temporal evolution of the range-corrected lidar signals shown at 1064 nm (Figure 7a), an intense dust aerosol layer is observed between 2000 and 5000 m asl. during 11 May over Athens. On 13 May (see Figure 7b), during the daytime measurements (06:00-11:00 UTC), the dust layer is limited below 2 km height asl., while a thick aerosol layer appears during the nighttime lidar measurements (18:00-19:00 UTC) between 3000 and 5000 asl. This layer, once split into two distinct layers (from ground to 3200 m and 4000-5000 m), persists in staying over Athens during 14 and 15 May (Figure 7c,d, respectively), while the lower layer is intensified during the daytime hours of 15 May (up to 16:48 UTC) over the daytime Planetary Boundary Layer (PBL),

Ground-Based Aerosol Lidar Observations
Ground-based lidar observations were used to illustrate the spatio-temporal evolution of the dust aerosol stratification during the measuring period (>50 h of measurements) (see Figure 7). According to the temporal evolution of the range-corrected lidar signals shown at 1064 nm (Figure 7a), an intense dust aerosol layer is observed between 2000 and 5000 m asl. during 11 May over Athens. On 13 May (see Figure 7b), during the daytime measurements (06:00-11:00 UTC), the dust layer is limited below 2 km height asl., while a thick aerosol layer appears during the nighttime lidar measurements (18:00-19:00 UTC) between 3000 and 5000 asl. This layer, once split into two distinct layers (from ground to 3200 m and 4000-5000 m), persists in staying over Athens during 14 and 15 May (Figure 7c,d, respectively), while the lower layer is intensified during the daytime hours of 15 May (up to 16:48 UTC) over the daytime Planetary Boundary Layer (PBL), which is confined below~1200 m height (between 13:00 and 16:49 UTC). The latter atmospheric barrier has been estimated from the lidar signals by using the Extended Kalman Filtering technique and found to be within the typical monthly range (1300-1700 m), suppressed, however, 200 m here due to the presence of the free tropospheric dust load, as also reported by [88]. During the following day (16 May), the intense dust aerosol layer is well stratified in three distinct layers between the top of the PBL (~1000 m height) and 3200 m height (Figure 7e). On the following days (18)(19)(20), the dust layer stays at constant levels (1000-4000 m) significantly attenuated over the Athenian PBL (denoted by black circles on Figure 7), showing a high aerosol burden over the city (Figure 7f-h). The days of 14-20 May coincide with the highest AOD values measured by MODIS (0.3-0.6). The free-tropospheric pure dust layer was also depicted by the space-borne lidar CALIPSO, over our station during May 2020 ( Figure A2).  In the following Figures (Figure 8a-f), we present the geometrical and optical properties of the aerosol layers observed over Athens during this dust event, while in Table 1, the mean values for the whole studied period are presented, along with their standard deviation (SD), the range and the median value. Due to overlap effect, the base of dust aerosol layers is estimated for height levels above 1000 m during the whole period of the event, while the top reached, in some cases, 7000 m asl (Figure 8a). In the same graphic (Figure 8a), we also present the center of mass (COM) of each distinct dust layer according to [89], which in most cases coincides with the geometrical center of the dust layer. All values of the mean aerosol optical properties as well as their SD were calculated within the altitude ranges shown for each day in Figure 8a and for the 1 h measurement period under cloud-free conditions (daytime or nighttime). Consequently, seven daytime and five nighttime datasets were considered for further analysis (Figure 8b-f). The αaer at both wavelengths (355 and 532 nm, Figure 8b) were similar, with higher values (~164 ± 39 Mm −1 ) on 13 May and a declining trend as the event evolved. A minimum is observed on the last day of measurements (20 May) of ~25 ± 10 Mm −1 in both wavelengths. Identical values in the extinction profiles were also reported by [90] during the SALTRACE experiment in Barbados, as well as by [36] during the SHADOW field campaign in Senegal.
Moreover, the βaer vertical profile (Figure 8c) had similar values at both 355 and 532 nm during the whole event, and even in some days of measurements (11, 13, 15 and 20 May) the mean β532 became larger than the mean β355. Such an excess in β532 values was also reported by [36,91] (SHADOW). It should also be noted that the SD of the two optical parameters, αaer and βaer, decreases as the event evolves, indicating that the probed dusty In the following Figures (Figure 8a-f), we present the geometrical and optical properties of the aerosol layers observed over Athens during this dust event, while in Table 1, the mean values for the whole studied period are presented, along with their standard deviation (SD), the range and the median value. Due to overlap effect, the base of dust aerosol layers is estimated for height levels above 1000 m during the whole period of the event, while the top reached, in some cases, 7000 m asl (Figure 8a). In the same graphic (Figure 8a), we also present the center of mass (COM) of each distinct dust layer according to [89], which in most cases coincides with the geometrical center of the dust layer. All values of the mean aerosol optical properties as well as their SD were calculated within the altitude ranges shown for each day in Figure 8a and for the 1 h measurement period under cloud-free conditions (daytime or nighttime). Consequently, seven daytime and five nighttime datasets were considered for further analysis (Figure 8b-f). The α aer at both wavelengths (355 and 532 nm, Figure 8b) were similar, with higher values (~164 ± 39 Mm −1 ) on 13 May and a declining trend as the event evolved. A minimum is observed on the last day of measurements (20 May) of~25 ± 10 Mm −1 in both wavelengths. Identical values in the extinction profiles were also reported by [90] during the SALTRACE experiment in Barbados, as well as by [36] during the SHADOW field campaign in Senegal.  Concerning the intensive optical properties, the LR355 inside the layers was equal to the LR532 for the whole period (Figure 8d), or even exceeded it in some cases (see also Figure 10f), giving an indication of non-mixed layers of Saharan dust aerosols [91]. Consequently, the ratio of the lidar ratios (LR355/LR532) was found around 1 for all the measurements, indicating the absence of spectral dependence for the case of pure dust [37,92]. A descending trend was found for δp355, which took its highest value on the first day of the event (11 May, δp355 = 35 ± 7%) and the lowest one on the evening of 18 May (δp355 = 23 ± 3%). It should be reminded here that δp values greater than 30% are representative for pure dust [36,91,[93][94][95]. The AEβ355/532, AEβ532/1064 and AEα355/532 had an increasing trend during the event (Figure 8e), ranging from −1.33 to 0.85, from −0.03 to 2.12 and from −0.01 to 0.50, respectively, taking mean values of −0.08 ± 0.26, 1.13 ± 0.21 and 0.25 ± 0.60, respectively, (Table 1) in accordance with data provided in [31][32][33][34]38,39,44]. On the contrary, the AOD at both wavelengths, inside the dust layer, showed a decreasing trend during the event (Figure 8f), ranging from 0.39 (14 May) to 0.06 (20 May) and from 0.40 (14 May) to 0.07 (20 May) at 355 and 532 nm, respectively. This gradual decrease (increase) with time for δp355, AOD (AEα, and AEβ) is of specific interest in terms of aging and mixing processes, and is associated with the change in the atmospheric circulation and the path travelled explained previously (see Figure 4) in an atmospheric environment mostly free from local (continental) aerosol emissions due to the COVID-19 restrictions. This gradual decrease (increase) in δp355, AOD (AEα, and AEβ), as the event evolves with time, is supported by the fact that the air mass trajectories initially followed a straight route from North Africa to Athens during the first phase of the event (11-15 May 10:00 UTC), while during the second phase of the event (15 May at 19:00 UTC-20 May at 19:00 UTC, as already discussed in Figure 4) they passed over the industrial regions of Istanbul (Turkey), where the dust aerosols were probably enriched with small anthropogenic particles, giving rise to the AEα and AEβ values and decreasing the values of δp355. By further analyzing the aerosol optical retrievals, we identified differences between the two phases of the event.  Moreover, the β aer vertical profile (Figure 8c) had similar values at both 355 and 532 nm during the whole event, and even in some days of measurements (11, 13, 15 and 20 May) the mean β 532 became larger than the mean β 355 . Such an excess in β 532 values was also reported by [36,91] (SHADOW). It should also be noted that the SD of the two optical parameters, α aer and β aer , decreases as the event evolves, indicating that the probed dusty layers become more stable and uniform with the aging of the dust event.
Concerning the intensive optical properties, the LR 355 inside the layers was equal to the LR 532 for the whole period (Figure 8d), or even exceeded it in some cases (see also Figure 10f), giving an indication of non-mixed layers of Saharan dust aerosols [91]. Consequently, the ratio of the lidar ratios (LR 355 /LR 532 ) was found around 1 for all the measurements, indicating the absence of spectral dependence for the case of pure dust [37,92]. A descending trend was found for δp 355 , which took its highest value on the first day of the event (11 May, δ p355 = 35 ± 7%) and the lowest one on the evening of 18 May (δ p355 = 23 ± 3%). It should be reminded here that δ p values greater than 30% are representative for pure dust [36,91,[93][94][95]. The AE β355/532 , AE β532/1064 and AE α355/532 had an increasing trend during the event (Figure 8e), ranging from −1.33 to 0.85, from −0.03 to 2.12 and from −0.01 to 0.50, respectively, taking mean values of −0.08 ± 0.26, 1.13 ± 0.21 and 0.25 ± 0.60, respectively, ( Table 1) in accordance with data provided in [31][32][33][34]38,39,44]. On the contrary, the AOD at both wavelengths, inside the dust layer, showed a decreasing trend during the event (Figure 8f), ranging from 0.39 (14 May) to 0.06 (20 May) and from 0.40 (14 May) to 0.07 (20 May) at 355 and 532 nm, respectively. This gradual decrease (increase) with time for δ p355 , AOD (AE α , and AE β ) is of specific interest in terms of aging and mixing processes, and is associated with the change in the atmospheric circulation and the path travelled explained previously (see Figure 4) in an atmospheric environment mostly free from local (continental) aerosol emissions due to the COVID-19 restrictions. This gradual decrease (increase) in δ p355 , AOD (AE α , and AE β ), as the event evolves with time, is supported by the fact that the air mass trajectories initially followed a straight route from North Africa to Athens during the first phase of the event (11-15 May 10:00 UTC), while during the second phase of the event (15 May at 19:00 UTC-20 May at 19:00 UTC, as already discussed in Figure 4) they passed over the industrial regions of Istanbul (Turkey), where the dust aerosols were probably enriched with small anthropogenic particles, giving rise to the AE α and AE β values and decreasing the values of δ p355 . By further analyzing the aerosol optical retrievals, we identified differences between the two phases of the event.
The aforementioned observation regarding the two distinct transportation phases of the dust plume is further supported by the comparison of the LR 355 values, obtained during the two phases of the event and reported here, with the corresponding literature values regarding pure and polluted dust (Figure 9). During the first time period (contains 11 and 14 May), the mean LR 355 obtained by our ground-based measurements is very close to pure dust observations reported by dedicated campaigns in the African region (SAMUM and SHADOW), but also long-range transported pure dust over Barbados (SALTRACE). On the other hand, during the second time period (contains measurements performed on 15 (night), 18 and 20 May), our LR 355 values are in the cluster of mixed and polluted dust, similar to values also reported by other studies.
Atmosphere 2021, 12, x FOR PEER REVIEW 1 Figure 9. LR355 values reported by various campaigns that correspond to pure (either directly the source or long-range transportation) and mixed/polluted dust, along with the values repo in this study (red circles inside a grey frame)] [20,38,90,91,93,95,97,98] The aforementioned observation regarding the two distinct transportation phas the dust plume is further supported by the comparison of the LR355 values, obta during the two phases of the event and reported here, with the corresponding liter values regarding pure and polluted dust (Figure 9). During the first time period tains 11 and 14 May), the mean LR355 obtained by our ground-based measuremen very close to pure dust observations reported by dedicated campaigns in the Africa gion (SAMUM and SHADOW), but also long-range transported pure dust over B dos (SALTRACE). On the other hand, during the second time period (contains m urements performed on 15 (night), 18 and 20 May), our LR355 values are in the clus mixed and polluted dust, similar to values also reported by other studies.

Case Study Analysis
In the following paragraphs, we will present two selected case studies durin 10-day period, focusing on the vertical distribution of the dust aerosol extensive an tensive optical properties. The selection of these days was based on the different p followed by the air masses starting from the Saharan region and arriving over Athen 15 May, the air masses arrived directly to Athens; on 18 May, the air masses, embe in the anticyclonic flow as described in Section 3.2, were mixed with anthropogenic passing over the Balkans and the industrial area of Istanbul.

Case I: 15 May 2020
The vertical profile of βaer (Figure 10a) at all the wavelengths for the case study May (15:50-16:50 UTC) reveals a thick aerosol layer between 2000 and 6500 m. More the βaer shows almost equal values at all wavelengths inside the dust aerosol layer. cerning the vertical profiles of AEβ355/532 and AEβ532/1064 on the same day (Figure 10b), Figure 9. LR 355 values reported by various campaigns that correspond to pure (either directly from the source or long-range transportation) and mixed/polluted dust, along with the values reported in this study (red circles inside a grey frame)] [20,38,90,91,93,95,97,98]

Case Study Analysis
In the following paragraphs, we will present two selected case studies during the 10-day period, focusing on the vertical distribution of the dust aerosol extensive and intensive optical properties. The selection of these days was based on the different paths followed by the air masses starting from the Saharan region and arriving over Athens. On 15 May, the air masses arrived directly to Athens; on 18 May, the air masses, embedded in the anticyclonic flow as described in Section 3.2, were mixed with anthropogenic ones passing over the Balkans and the industrial area of Istanbul.

Case II: 18 May 2020
The dust event on 18 May also shows significant intensity, as seen on the vertical profiles of βaer. Again, the βaer at 355 nm and 532 nm wavelengths presents similar values ( Figure 11).

Case II: 18 May 2020
The dust event on 18 May also shows significant intensity, as seen on the vertical profiles of β aer . Again, the β aer at 355 nm and 532 nm wavelengths presents similar values ( Figure 11).
The AE β355/532 is equal to 0 during both the daytime and nighttime lidar measurements, indicating large particles [34,35,45] On the other hand, the AE β532/1064 seems to show slightly higher values (>1) during the daytime lidar measurements compared to the ones observed during the nighttime (AE β532/1064~1 ). Additionally, the LR 355 and LR 532 present equal mean values, 48 ± 11 sr and 48 ± 13 sr, respectively, during the nighttime, indicating wavelength independence of dust particles, as discussed by [36]. The δ p355 presents higher values during the daytime measurements (32 ± 5%) compared to the ones present during nighttime measurements (23 ± 3%), in accordance with the change in the synoptic pattern on this day and in terms of air mass backward trajectories. We have to mention here that the two presented case studies concern the optical properties of dust aerosols which arrived over Athens without significant mixing with locally emitted air masses, due to the COVID-19 local transportation restrictions leading to reduced aerosol emissions. Therefore, we could argue that the measured optical properties of the probed aerosols are representative of dust aerosols mixed with inter-regional continental aerosols, rather than local ones over the height of 1-1.5 km asl. The AEβ355/532 is equal to 0 during both the daytime and nighttime lidar measurements, indicating large particles [34,35,45] On the other hand, the AEβ532/1064 seems to show slightly higher values (>1) during the daytime lidar measurements compared to the ones observed during the nighttime (AEβ532/1064~1). Additionally, the LR355 and LR532 present equal mean values, 48 ± 11 sr and 48 ± 13 sr, respectively, during the nighttime, indicating wavelength independence of dust particles, as discussed by [36]. The δp355 presents higher values during the daytime measurements (32 ± 5%) compared to the ones present during nighttime measurements (23 ± 3%), in accordance with the change in the synoptic pattern on this day and in terms of air mass backward trajectories. We have to mention here that the two presented case studies concern the optical properties of dust aerosols which arrived over Athens without significant mixing with locally emitted air masses, due to the COVID-19 local transportation restrictions leading to reduced aerosol emissions. Therefore, we could argue that the measured optical properties of the probed aerosols are representative of dust aerosols mixed with inter-regional continental aerosols, rather than local ones over the height of 1-1.5 km asl.

Radiative Effect Calculations Using LibRadtran
In order to estimate the radiative effect (RE) of the dust event over Athens, we firstly calculated the dust mass concentration profiles from our lidar measurements by follow-

Radiative Effect Calculations Using LibRadtran
In order to estimate the radiative effect (RE) of the dust event over Athens, we firstly calculated the dust mass concentration profiles from our lidar measurements by following the procedure introduced by [97] for the calculation of the dust-related backscatter coefficient and [37] for the estimation of the height-resolved mass concentration of the dust-related backscatter coefficient. The mass profiles were then used as an input in the LibRadtran radiative transfer model version 2.0.2. [99]. The uvspec program that calculates the radiation field in the Earth's atmosphere was implemented for the disort radiative transfer equation (1-D geometry), and the downwelling and upwelling shortwave (SW, 0.28-2.5 µm) and longwave (LW, 2.5-40 µm) irradiances at the top of the atmosphere (TOA, 120 km) and bottom of the atmosphere (BOA, ground level) were simulated. It should be noticed here that SW and LW ranges are treated separately by LibRadtran, and all the cases correspond to cloud-free conditions. The OPAC library 4.0 [100] was used for desert spheroids (T-matrix calculations) in the mineral accumulation mode (MIAM) with R MIAM ∈ [0.005, 20] in µm. The library uses an outdated dust refractive index spectrum in IR, which may substantially bias the LW radiative flux calculations. The RE depicts the perturbation in flux in the atmosphere caused by the presence of the aerosol layers in relation to that calculated under clear-sky conditions, and can be expressed as [13,101]: RE(z) NET = ∆F loaded − ∆F re f erence , where the net flux, ∆F, at a level z is the difference between the downwelling and upwelling flux. In addition to the RE calculations, the radiative effect of the loaded atmosphere was also assessed from the vertical profile of the rate of heating of the atmosphere by the absorption of radiation called radiative heating rate (HR), which, accordingly to the RE, is calculated as: ∆HR(z) NET = HR loaded NET − HR re f erence NET . Simulations were performed at 10:00 UTC on 18 May 2020, since at this time of measurement the solar zenith angle is small (18.78 • ), providing high solar irradiances proper to clearly depict the atmospheric situation. We initiated our simulations by assuming a Hypothetical scenario in order to estimate how the presented dust layer, in the free troposphere, can affect such a typical atmosphere (midlatitude summertime atmospheric conditions [102]). Afterwards, we proceeded with a more Realistic scenario, which depicts the current situation. Specifically, in the Realistic scenario, the local pollutants are reduced within the PBL due to the quarantine (−30% NO 2 , −2% CO 2 [52]), the free troposphere is loaded with Saharan dust particles and, additionally, we took into account an extreme low ozone event where the total column ozone dropped down to 280-295 DU [103]. Table 2 summarizes the estimations of the instantaneous dust RE both at the BOA and TOA, as well as of the net heating rate within the atmosphere of both scenarios (Hypothetic and Realistic). In the Realistic scenario, the net RE is higher in absolute value at the BOA and almost equal at the TOA, compared to the Hypothetical one. The heating rate within the atmosphere, from 1000 to 6000 m, where the dust layer was observed, has a positive sign in both scenarios and is slightly lower in the Realistic scenario, which depicts the contribution of the reduced concentrations of the pollutants. In order to further explore the RE in our case (see also Figure A3), we plotted the net HR of (i) the typical atmosphere (HR  Figure 12b). In this way, the ∆HR(z) i−iii depicts the absorption of radiation within the atmospheric column due to the reduced pollutant concentrations, while the ∆HR(z) ii−i depicts the corresponding absorption of radiation within the atmospheric column due to the additional dust load.
The net HR of specific altitude ranges is presented in Figure 12a. At the BOA, the reduced concentrations of the pollutants result in a negative net HR equal to −0.036 K/d due to the reduced molecular absorption in the SW range, while in a typical atmosphere this value would be opposite in sign and equal to +0.006 K/d. Additionally, the dust loaded atmosphere with the reduced pollutants has a positive net HR equal to 0.156 K/d. Within the dust layer (1-6 km), the net HR of the reference atmosphere is reduced by 50% compared to the one of a typical atmosphere (+0.004 K/d and +0.008 K/d, respectively). On the contrary, the net heating rate of the loaded atmosphere is much higher, reaching the value of +2.470 K/d, due to the high AOD within this range. At the TOA, the highest net HR is estimated for a typical atmosphere (+2.740 K/d) since the reduction in the pollutants and ozone is estimated to have a decrease of around 9% (2.490 K/d) compared to the aforementioned typical atmospheric conditions. Even a lower net HR equal to 2.420 K/d is estimated at the same altitude for the dust loaded atmosphere (further decrease of 3%).
In this way, the ( ) − depicts the absorption of radiation within the atmospheric column due to the reduced pollutant concentrations, while the ( ) − depicts the corresponding absorption of radiation within the atmospheric column due to the additional dust load. The net HR of specific altitude ranges is presented in Figure 12a. At the BOA, the reduced concentrations of the pollutants result in a negative net HR equal to −0.036 K/d due to the reduced molecular absorption in the SW range, while in a typical atmosphere this value would be opposite in sign and equal to +0.006 K/d. Additionally, the dust loaded atmosphere with the reduced pollutants has a positive net HR equal to 0.156 K/d. Within the dust layer (1-6 km), the net HR of the reference atmosphere is reduced by 50% compared to the one of a typical atmosphere (+0.004 K/d and +0.008 K/d, respectively). On the contrary, the net heating rate of the loaded atmosphere is much higher, reaching the value of +2.470 K/d, due to the high AOD within this range. At the TOA, the highest net HR is estimated for a typical atmosphere (+2.740 K/d) since the reduction in the pollutants and ozone is estimated to have a decrease of around 9% (2.490 K/d) compared to the aforementioned typical atmospheric conditions. Even a lower net HR equal to 2.420 K/d is estimated at the same altitude for the dust loaded atmosphere (further decrease of 3%).
In Figure 12b, the difference between the typical and the reference atmosphere gives a positive ΔHR, which reaches the value of +0.042 K/d at the BOA, and this value is designated by 86% due to the reduction in pollutants within the boundary layer. However, the presence of the dust layer does not leave the net HR at the BOA unaffected, since In Figure 12b, the difference between the typical and the reference atmosphere gives a positive ∆HR, which reaches the value of +0.042 K/d at the BOA, and this value is designated by 86% due to the reduction in pollutants within the boundary layer. However, the presence of the dust layer does not leave the net HR at the BOA unaffected, since despite the reduced pollutants, the ∆HR reaches the value of +0.192 K/d (scattering and absorption of the dust particles). Within the dust layer (1-6 km), 98% of the positive ∆HR (equal to +2.433 K/d) is attributed to the dust loaded atmosphere, where the presence of dust aerosol led again to an increase in the scattering (increase in the upward and downward diffuse irradiance) and absorption of, mainly, the SW radiation. In the absence of the dust layer, the ∆HR would be equal to +0.04 K/d due to the heating that an atmosphere with reduced pollutants would have created based on a typical atmosphere. In the range of 6-10 km, the reference atmosphere is the major contributor (52% and 77%, respectively) of each ∆HR (∆HR i-iii , ∆HR ii-i ), which reach the positive values of +0.04 and +0.563 K/d, respectively. Here, the net heating rate is lower compared to the previous altitude range (1-6 km) due to the significantly lower AOD (absence of dust particles). At the TOA, the ∆HR between the loaded and the reference atmosphere is negative in sign but close to zero (−0.072 K/d). On the contrary, the ∆HR between the reference and the typical atmosphere is positive in sign and equal to +0.248 K/d. Taking into account that the absorption of the Saharan dust particles is more pronounced at the ultraviolet (UV) spectrum, it could be concluded that its presence partially balances the effect of reduced levels of ozone on the upper atmosphere. Otherwise, a higher percentage of the UV radiation would have reached the ground.

Conclusions
In the period 10-20 May 2020, the meteorological conditions prevailing over the eastern Mediterranean enabled the formation of a moderate (in terms of aerosol load) long-lasting Saharan dust event over Greece. The event was followed by a synergy of ground-based and space-borne remote sensing, as well as in situ instrumentation. The measurements were performed during the COVID-19 lockdown period over Greece, which was accompanied by a general restriction of transport activities over Europe. As a consequence, during this period the levels of air pollution, especially over the megacity Athens, were significantly reduced, as in the entire European continent.
High AOD values (even up to 0.6) were observed by both MODIS (at 550 nm) and ground-based lidar measurements (at 355 and 532 nm). Moreover, high δ p355 values ranging from 23 to 35% were measured inside the dust aerosol layers, which were usually observed between 1000 and 6500 m asl. The variations in the values of δ p355 , as well as in those of LR (from 34 to 63 sr at 355 nm) and AE (from −1.33 to 0.85 for the AE β355/532 ), can be attributed to aging and mixing processes due to the different paths travelled during the long-range transport of at least 120 h, as estimated by HYSPLIT model (before and after 16 May). Moreover, instantaneous radiative effect calculations at BOA and TOA were estimated by LibRadtran for two scenarios. One using typical atmospheric profiles (Hypothetical), and one using reduced atmospheric pollutants (Realistic) due to the COVID-19 restrictions, revealed negligible differences in terms of radiative effect, of the order of +2.6% (SW BOA , cooling behavior) and +1.8% (LW BOA , heating behavior). Within the dust layer (1-6 km), almost 98% of the positive heating rate is attributed to the dust load. At the TOA, the reduction in the pollutants and ozone is estimated to have a decrease in the net HR of around 9%, while an additional decrease of 3% is estimated due to the presence of dust in the free troposphere, compared to the typical atmospheric conditions.
Overall, the 10-day dust event presented in this work provides valuable information by revealing the aerosol optical properties of strongly depolarizing Saharan dust particles and their impact on the climate's radiative balance and atmospheric dynamics. Moreover, the aerosol dust measurements, performed during the confined period of the COVID-19 pandemic over Athens aloft, revealed interesting features of the aerosol dust properties, based on the δ p355 , LR 355 , LR 532 , AE β355/532 AE β532/1064 and AE a355/532 values, in the absence of important air pollution sources over the European continent. Furthermore, we observed significant differences between the aerosol optical properties observed before and after 15 May, when the dust circulation pattern changed from the direct advection from Africa to Greece (before 15 May) to the anticyclonic flow which prevailed after 15 May over Greece (when the dusty air masses passed over the Balkans and the industrial regions of Istanbul, Turkey). At ground level, a significantly higher PM 10 to PM 1 ratio was observed in the period extending from the 13 to 21 of May. This is an indication of the strong mixing of Saharan dust and local aerosol in the vertical.