7 Be, 210 Pb atm and 137 Cs in Snow Deposits in the Arctic Part of Western Siberia (Yamal-Nenets Autonomous District)

: Radioactive isotopes ( 7 Be, 210 Pb atm and 137 Cs) are used as indicators of processes associated with the transfer of matter from the atmosphere. Studying snow cover can provide information about the seasonal deposition ﬂux of the isotopes to the Earth’s surface over the entire period of snow accumulation. The purpose of this study is to identify the features of 7 Be, 210 Pb atm and 137 Cs deposition with the atmospheric precipitation in winter in the Arctic part of Western Siberia and to study the contribution of the particulate fractions of suspended matter in snow water to the total content of the radionuclides in samples of integrated seasonal snowfall. Snow samples were taken over a wide area along the highways around Novy Urengoy in April 2019. The suspended matter in snow samples was divided into three fractions. The isotopic composition was determined by high-resolution semiconductor gamma-spectrometry. The seasonal deposition ﬂux of 7 Be and 210 Pb atm in the winter at the time of sampling averaged 58.7 and 25.2 Bq m − 2 season − 1 , respectively. The average speciﬁc activity of 7 Be and 210 Pb atm in the snow water was 248.0 and 104.5 mBq L − 1 . The deposition ﬂux of 137 Cs from the atmosphere was low compared to 7 Be and 210 Pb atm and did not exceed 0.39 Bq m − 2 season − 1 at all sampling points. This indicates an insigniﬁcant modern ﬂux of the radionuclide from the atmosphere. The separation of suspended matter in snow water by particulate fractions shows that the studied isotopes are present in all the extracted fractions: > 3, 0.45–3 and < 0.45 µ m. The main part of 210 Pb atm in all studied samples is in the coarse-grained fraction > 3 µ m. Most 7 Be is contained in ﬁnely dispersed aerosols, colloids, or a dissolved component (where the fraction < 0.45 µ m). A signiﬁcant increase in the contribution of coarse-grained fractions of suspended matter in snow water to the total activity of 7 Be in snow precipitation was observed in territories with a higher anthropogenic impact.


Introduction
One of the main transport pathways of chemical elements in the environment is through the atmosphere. This process can be significantly affected by both natural (dust storms, volcanic activity and forest fires) and anthropogenic (emissions from industrial enterprises, open pit mining, storage of industrial waste and accidents at the enterprises of the nuclear fuel cycle) factors. Chemical elements transported by air enter the Earth's surface as a part of dry dust-aerosol deposition, as well as in atmospheric precipitation (wet deposition).
Often, radioactive isotopes such as 7 Be, 210 Pb atm and 137 Cs are used as indicators of processes associated with the transfer of matter from the atmosphere. They are used, for example, in assessing the conditions and rates of formation of modern lake, river and sea sediments and in studying the transport of aerosol particles in the atmosphere and the rates of their precipitation on the Earth's surface [1][2][3][4][5][6][7][8][9][10][11][12]. In the study of the radionuclide composition of aerosol and dust particles, atmospheric deposition is a subject of many modern investigations [13][14][15][16][17][18][19].
Naturally occurring radioactive isotopes 7 Be and 210 Pb atm reach the Earth's surface from the atmosphere in significant quantities. These isotopes have various sources of origin: 7 Be (T 1/2 = 53.3 days) is formed in the upper atmosphere through the spallation reactions of the protons and neutrons of cosmic rays with 14 N and 16 O nuclei [4,20]. About 75% of the total 7 Be is produced in the stratosphere (10-47 km) and 25% in the upper troposphere (8-10 km) [21,22]. 210 Pb (T 1/2 = 22.3 years) is a daughter product of 222 Rn. Radon is formed as a result of the radioactive decay of radionuclides of the 238 U series and enters the atmosphere from the Earth's surface. An additional amount of 210 Pb near large settlements and land transport highways can enter the atmosphere by burning leaded fuels. However, in Russia the use of such fuel has been universally banned in the last decade, the contribution of this component can be neglected. The emission of 137 Cs (T 1/2 = 30 years) into the environment occurred mainly as a result of testing nuclear weapons and accidents at nuclear power plants. Currently, 137 Cs enters the atmosphere mainly as a result of several processes: the weathering of dust particles from the surface of previously contaminated soils, or the combustion of a large amount of organic material during strong natural fires [23][24][25]. Being electrically charged immediately after formation, these radionuclides are sorbed by aerosol and dust particles and fall to the Earth's surface. According to Ioannidou [26], "the activity size distributions of the radionuclides attached to aerosol particles are the result of atmospheric process combinations, e.g., the coagulation of ultrafine particles, fog and cloud droplet formation, evaporation and condensation, washout, rainout and the contribution of dust storms and combustion products to the tropospheric aerosol mixture". Moreover, some estimates [14,15,[27][28][29] show that more than 80% of total flux of 7 Be and 210 Pb atm on the Earth's surface is associated with wet precipitation (snow and rain).
There is a large number of studies related to the investigation of processes regulating the behavior of 7 Be and 210 Pb atm in the air and their washout from the atmosphere as a part of rainfall. At the same time, there are few works devoted to the study of 7 Be and 210 Pb atm in snow. Such studies may be especially relevant for regions where a long (more than several months) period of stable negative temperatures with the formation of a constant snow cover is characteristic. Very few studies in the literature are presented containing information on 7 Be and 210 Pb atm in freshly fallen snow [30][31][32][33]. For example, the average specific activity of 7 Be and 210 Pb in fresh snow at two sites of Greenland were 13.48 and 1.08 pCi kg −1 (Dye 3) [31], 12.06 and 1.32 pCi kg −1 (Summit) [30], respectively. There are practically no widely known data on studies of the joint seasonal atmospheric flux of 7 Be and 210 Pb atm , based on the study of integrated snow samples accumulated in winter periods in a given territory. Snow cover is a natural depository, accumulating information on atmospheric flux for a sufficiently large period of time from the first precipitation in late autumn to its melting in spring. Its study can provide information on the total flux of 7 Be and 210 Pb atm to the Earth's surface over the entire period of snow accumulation without separation of the dry or wet components. Such a vast region as Western Siberia, located in the northern part of central Eurasia, remains completely unexplored from this point of view. The territory of Western Siberia from the south and north is defined to 49 • and 73 • North latitude and from west to east, 60 • and 90 • East longitude. The duration of the annual steady snow cover for this territory varies from 4 to 5 months in the South to 8-9 months in the North in the Arctic zone.
Previous studies [17] have allowed us to obtain a preliminary estimate of the amount of 7 Be, 210 Pb atm and 137 Cs entering the Earth's surface as a part of the snowfall in the southern regions of Western Siberia. In fresh snow precipitated and sampled on this territory in the 2016-2017 winter period, specific activities of 210 Pb atm and 7 Be were 506 ± 45 and 1611 ± 130 mBq L −1 , recalculated to the volume of snow waters. In fresh rain waters (the spring-autumn period of 2017), these values were 242 ± 23 and 2434 ± 200 mBq L −1 , respectively. The average value of the 7 Be/ 210 Pb atm activity ratio in fresh rain waters was more than three times higher than in fresh snow: 10.1 to 3.2. The study of integrated snowfall accumulated over the five months of the winter of 2016-2017 showed that the maximum deposition densities of 7 Be and 210 Pb atm were observed in a foothill zone-618 ± 62 and 171 ± 17 Bq m −2 , respectively. The minimum values corresponded to the Alpine zone-104 ± 11 and 27 ± 4 Bq m −2 . The forest-steppe zone deposition densities of 7 Be and 210 Pb atm varied within 237-340 Bq m −2 and 73-93 Bq m −2 . The deposition density of 137 Cs in comparison with 210 Pb atm and 7 Be was small and did not exceed 1 Bq m −2 in all studied points.
As a rule, 7 Be, 210 Pb atm and 137 Cs are found in rain and snow waters as a part of the suspended matter, which is a complex mixture of terrigenous particulate materials of different natures and sizes. It is based on dust particles of soil, fine sand, organic plant debris with a size of 10-10 3 µm, fine clay, aerosol particles of an 10 −1 -10 2 µm size, nanosized aerosol particles and colloids. Earlier, we showed [17] that 7 Be and 210 Pb atm are present in all particulate fractions of suspended matter in snow water, representing samples of snowfall in the south of Western Siberia. Moreover, the highest 7 Be/ 210 Pb atm ratio is observed in the finest fraction represented by nanosized aerosol particles, colloids and the dissolved component.
The purpose of this study is to identify the features of the 7 Be, 210 Pb atm and 137 Cs deposition as a part of the atmospheric precipitation in winter in the Arctic part of Western Siberia (Yamal-Nenets Autonomous District (YNAD) of Russia), as well as to study the contribution of particulate fractions of suspended matter in snow water to the total content of radionuclides in the samples of integrated seasonal snowfall.

Objects of Research
In this work, we studied integrated snow samples taken from 18 to 22 April 2019 in the Nadym, Purov and Taz regions of the Yamal-Nenets Autonomous District. Figure 1 shows the layout of the sampling points. The sampling was carried out along the following highways: Nadym-Novy Urengoy-sat. Urengoy and sat. Tazovsky-sat. Urengoy-Tarko-Sale, representing the west-east and north-south directions. Sampling points are located at a distance of 100-200 m from the roads. Geographically, the investigated area is comprised of tundra and forest-tundra landscape zones. As a rule, there are lichens, mosses, poorly developed grass cover and undersized shrubs (dwarf birch, juniper, blueberry, etc.) on the soil surface. The forest-tundra zone is characterized by the presence of a sparse forest, represented mainly by larch, Siberian cedar and pine. The collected integrated snow samples are material accumulated from mid-October 2018 to the end of April 2019 and consisting of a mixture of wet (snow) and dry (dust, aerosol) precipitation.

Sampling and Sample Preparation Technique
Surface areas located in the open air within zones closed from strong winds were selected for snow sampling. Samples were taken for the entire thickness of the snow cover, with the exception of the 5 cm layer above the soil. A brief description of the sampling sites is presented in Table 1. Snow samples with a volume of 50-60 L were packed in plastic containers and delivered to the laboratory. The final sample preparation consisted of several successive stages: snow samples were melted under laboratory conditions at room temperature. Suspended matter of the sample was decanted. To separate finely dispersed solid fractions, the decanted solution was successively filtered through two filters: a blue ribbon filter (average pore size of 3-5 microns) and a membrane filter of 0.45 microns. This made it possible to separate two components of suspended matter with a dimension of more than 3 µm and from 3 to 0.45 µm, which are dust particles of various sizes. The solution obtained after filtration was acidified to pH = 1 by the addition of concentrated HNO 3 . The solution contained a suspended substance with a dimension of less than 0.45 µm, represented by nanosized dust, aerosol particles, colloids and a dissolved component. The entire volume of the solution was evaporated until a dry Atmosphere 2020, 11, 825 4 of 20 residue was isolated. Subsequently, the content of the gamma-emitting radionuclides was determined in the selected dry residue and filters.

Sampling and Sample Preparation Technique
Surface areas located in the open air within zones closed from strong winds were selected for snow sampling. Samples were taken for the entire thickness of the snow cover, with the exception of the 5 cm layer above the soil. A brief description of the sampling sites is presented in Table 1. Snow samples with a volume of 50-60 L were packed in plastic containers and delivered to the laboratory. The final sample preparation consisted of several successive stages: Snow samples were melted under laboratory conditions at room temperature. Suspended matter of the sample was decanted. To separate finely dispersed solid fractions, the decanted solution was successively filtered through two filters: a blue ribbon filter (average pore size of 3-5 microns) and a membrane filter of 0.45 microns. This made it possible to separate two components of suspended matter with a dimension of more than 3 μm and from 3 to 0.45 μm, which are dust particles of various sizes. The solution obtained after filtration was acidified to pH = 1 by the addition of concentrated HNO3. The solution contained a suspended substance with a dimension of less than 0.45 μm, represented by nanosized dust, aerosol particles, colloids and a dissolved component. The entire volume of the solution was evaporated until a dry residue was isolated. Subsequently, the content of the gamma-emitting radionuclides was determined in the selected dry residue and filters.
When studying the elemental composition of water samples, an important step is the acidification of samples immediately after sampling. Acidification is carried out to minimize losses due to sorption on the walls of laboratory glassware. As a rule, in many studies related to the study of the elemental and radionuclide composition of wet deposition, acidification was carried out either at the stage prior to the precipitation accumulation [1,5,19] or immediately after sampling [34]. This  When studying the elemental composition of water samples, an important step is the acidification of samples immediately after sampling. Acidification is carried out to minimize losses due to sorption on the walls of laboratory glassware. As a rule, in many studies related to the study of the elemental and radionuclide composition of wet deposition, acidification was carried out either at the stage prior to the precipitation accumulation [1,5,19] or immediately after sampling [34]. This approach excludes the possibility of identifying the contribution of the coarse-grained dust component of the suspended matter to the total content of chemical elements. Our preliminary studies showed that acidification to pH = 1 immediately after melting causes up to 90% of 7 Be, 210 Pb atm and 137 Cs contained in the coarse fractions of suspended matter to pass into the dissolved component. The aim of our investigation is to study the contribution of different particulate fractions of suspended matter in snow water to the total content of the studied radionuclides. Therefore, we slightly changed the generally accepted approach. To reduce the effect of the sorption of radionuclides on the walls of the laboratory glassware, the time of Steps 1-3 was reduced to the minimum possible. After completion of the filtration procedure, all used laboratory glassware was thoroughly washed with an acid solution (pH = 1, distilled water and HNO 3 in a ratio of 1000:1). The resulting flushing was added to the solution to be evaporated.

Analysis
In the isolated particulate fractions of the suspended matter of each snow sample, the activities of 7 Be, 210 Pb atm and 137 Cs were determined by high-resolution semiconductor gamma spectrometry using a specially developed procedure [35,36].
The analysis was performed using a gamma spectrometer based on the low-background well-type HPGe detector GWL-220-15 (active volume: 220 cm 3 ; well diameter: 15.5 mm; well depth: 40 mm; resolution: better than 1.4 keV at energy 122 keV and better than 2.3 keV at energy 1.33 MeV). This detector has a large working volume and, thanks to the presence of a well inside the active zone, allows for measurements with a geometry close to 4π. This equipment made it possible to measure the intensity of gamma lines in the range of 30 to 2000 keV. The detector efficiency for the 46.5 keV ( 210 Pb) and 661.7 keV ( 137 Cs) gamma-lines was calculated using an in-house calibration source prepared by spiking extremely low radioactive material (high-purity quartz, coal and sawdust) with the Russia national silicate reference sample of uranium ore (UR 47S) and soil reference sample prepared by the International Atomic Energy Agency (IAEA-375). The detector efficiency for the 477.6 keV ( 7 Be) peak was determined using a linear interpolation between the 351.9 keV ( 214 Pb) and 661.7 keV ( 137 Cs) photo-peaks of the same standards. When placing a sample weighing from 0.5 to 8 g inside the well, the detection efficiency of the gamma rays with an energy of 46.5 keV reached a value of 50-60%, with 477.6 keV, it reached 15-20% and with 661.7 keV, it reached 7-8%. The procedure took into account the influence of such interfering factors as the density of the analyzed samples and the measurement geometry. The accuracy of analysis was estimated against the BIL-1, BIL-2, ZUK-1, SDO-1, SG-1A, DVG, DVT and DVR Russian national standards, the IAEA-375 and IAEA-135 standards.
The lower detection limit of 7 Be, 210 Pb atm and 137 Cs was 0.02 Bq. The duration of the measurement of a single sample varied from 12 to 48 h. Time was chosen so that the statistical error in determining the areas of analytical photopeaks of 46.5 and 477.6 keV did not exceed 5%.

Backward Trajectory Frequency Analysis
To determine the potential long-distance transport pathways of air masses reaching YNAD, five-day backward air-mass frequency trajectories were computed using the Hybrid Single-Particle Lagrangian Integrated Trajectory (HYSPLIT) model [37]. The meteorological data used for trajectory calculating were the GDAS (Global Data Assimilation System) data (1 • × 1 • ) and were downloaded from the web server of NOAA Air Resources Laboratory. We obtained a total of 770 daily trajectories started every 6 h at 500 m above ground level (AGL) from 9 October 2018 to 19 April 2019, which can be grouped into five clusters via the built-in clustering tool in the model.

Results and Discussion
The results of determining the values of specific activities and seasonal deposition fluxes of 7 Be, 210 Pb atm and 137 Cs in the studied snow samples are presented in Table 2. The specific activities of particulate fractions are given in terms of snow water volume units. The radionuclide seasonal deposition fluxes at each point were calculated based on the known data of the sampling area and the amount of snow water obtained by melting snow (Table 1). All data were recalculated to the time of sampling. Taking into account the short half-life of 7 Be (53.2 days) and a long duration of the snow cover accumulation period (~186 days), the actual value of 7 Be total flux in winter will be significantly higher. In this case, the necessary decay and buildup corrections during the accumulation period must be implemented. According to Aba et al. [13] the correction factor (1/Ks) applied during the time of snow cover accumulation is defined as follows: where T 1/2 is the 7 Be half-life and t s is the snow cover accumulation time. Estimated values for the total winter fluxes of 7 Be, calculated with the correction factor (1/Ks), are also shown in Table 2. It should be noted that these values do not consider a number of factors that affect the accurate value of the total flux: the duration, intensity and time distribution of individual snowfall events; possible significant differences in the concentrations of 7 Be in the snow of each event, and others.
The obtained results show that the studied isotopes were present in all the extracted particulate fractions of suspended matter in snow water: from large dust particles to nanosized aerosol particles, colloids and the dissolved component.
Summing the contribution of all extracted particulate fractions of suspended matter, the seasonal deposition fluxes of 210 Pb atm , 7 Be and 137 Cs associated with wet and dry depositions precipitated over the entire period of accumulation of snow cover on the studied territory, and calculated to the time of sampling, can be averaged as follows ( 8-139.9) and 0.90 (0.14-1.82) mBq L −1 , respectively. In further interpretations, we will operate with the values of 7 Be activities determined at the time of sampling.  Note: * 1: coarse-grained fraction (suspended matter with a dimension of >3 µm, remaining after decantation and settled down when filtering snow water through a blue ribbon filter); 2: the fraction of suspended matter with a dimension of 0.45-3 µm, deposited during sequential filtration through a 0.45 µm membrane filter; 3: fine-dispersed fraction of suspended matter with a dimension <0.45 µm, obtained as a dry residue by evaporation of the filtered solution; ** corrected (1/Ks) values of actual 7 Be flux; *** snow water.
Atmosphere 2020, 11, 825 8 of 20 The seasonal deposition flux of 137 Cs is low and does not exceed 0.40 Bq m −2 season −1 at all studied sampling points. This indicates an insignificant modern flux of this radionuclide from the atmosphere. It should be noted that the levels of 137 Cs concentrations in the studied samples are close to the detection limit of the analytical method used. The error of 137 Cs determination often exceeds 30%, which makes it impossible to make high-quality joint statistical interpretations of 137 Cs data and data obtained for 210 Pb atm and 7 Be. Figure 2 shows the dependences of 7 Be and 210 Pb atm specific activities and seasonal deposition fluxes on the calculated amount of precipitation at the sampling points. The graphs show the absence of a significant correlation between the specific activities of both isotopes and the amount of precipitation. At the same time, the seasonal deposition fluxes of 7 Be and 210 Pb atm strongly correlate with the amount of precipitation at the correlation coefficients (r) of 0.75 and 0.88, respectively. Such strong correlations are explained by the fact that washout with precipitation is one of the most important mechanisms for removing these isotopes from the atmosphere. It is known that more than 80% of 7 Be and 210 Pb atm located in the lower atmosphere are deposited directly with wet precipitation (rain and snow) [14,15,[27][28][29]. The study of the nature of the joint deposition of 7 Be and 210 Pbatm ( Figure 3) shows a noticeable correlation (the Pearson correlation coefficient, r = 0.55) between the values of their specific activities. There is a strong correlation between the seasonal deposition fluxes of 7 Be and 210 Pbatm (r = 0.86). This suggests that the deposition of both radionuclides is regulated by the same processes (cloud height, the extent and duration of snowfall, the intensity of snowfall, cloud type and the vertical mixing of the air masses at the sampling location) [15,37,38].  There is a strong correlation between the seasonal deposition fluxes of 7 Be and 210 Pb atm (r = 0.86). This suggests that the deposition of both radionuclides is regulated by the same processes (cloud height, the extent and duration of snowfall, the intensity of snowfall, cloud type and the vertical mixing of the air masses at the sampling location) [15,38,39]. The study of the nature of the joint deposition of 7 Be and 210 Pbatm ( Figure 3) shows a noticeable correlation (the Pearson correlation coefficient, r = 0.55) between the values of their specific activities. There is a strong correlation between the seasonal deposition fluxes of 7 Be and 210 Pbatm (r = 0.86). This suggests that the deposition of both radionuclides is regulated by the same processes (cloud height, the extent and duration of snowfall, the intensity of snowfall, cloud type and the vertical mixing of the air masses at the sampling location) [15,37,38].  The spatial distribution of 7 Be and 210 Pb atm seasonal deposition fluxes at the sampling points is shown in Figure 4. It should be noted that the seasonal deposition fluxes of both 7 Be and 210 Pb atm in the latitudinal direction are generally higher than in the meridional direction. The seasonal deposition fluxes of 7     When studying the radionuclide composition ( 7 Be and 210 Pbatm) of the particulate fractions of suspended matter in snow water, the following features were revealed (Table 3 and       When studying the radionuclide composition ( 7 Be and 210 Pbatm) of the particulate fractions of suspended matter in snow water, the following features were revealed (Table 3 and    When studying the radionuclide composition ( 7 Be and 210 Pb atm ) of the particulate fractions of suspended matter in snow water, the following features were revealed (Table 3 and   Note: SD: standard deviation; * 1, 2 and 3-particulate size fractions (see Figure 1).
Atmosphere 2020, 11, x FOR PEER REVIEW 13 of 24  The average values of 7 Be and 210 Pb atm specific activities in the suspended matter in snow water particulate fractions, calculated over the entire set of studied samples, are presented in Figure 7. The fraction >3 µm contains 73.7 mBq L −1 ( 7 Be) and 66.2 mBq L −1 ( 210 Pb atm ). Values of the 0.45-3 µm fraction are equal to 14.1 and 11.9 mBq L −1 , and those of the <0.45 µm fraction are equal to 160.2 and 26.4 mBq L −1 . The average values of 7 Be and 210 Pbatm specific activities in the suspended matter in snow water particulate fractions, calculated over the entire set of studied samples, are presented in Figure 7. The fraction >3 μm contains 73.7 mBq L -1 ( 7 Be) and 66.2 mBq L -1 ( 210 Pbatm). Values of the 0.45-3 μm fraction are equal to 14.1 and 11.9 mBq L -1 , and those of the <0.45 μm fraction are equal to 160.2 and 26.4 mBq L -1 . For coarse-grained fractions, consisting mainly of large dust particles, the 7 Be/ 210 Pbatm ratio is equal to 1.1-1.2. The 7 Be/ 210 Pbatm ratio of the finely dispersed fraction is much higher-6.1. The low values of the 7 Be/ 210 Pbatm ratio typical for coarse-grained fractions could indicate that these particles represent the material whose radionuclide composition was formed long before its entry into the atmosphere and subsequent precipitation onto the Earth's surface as a part of dry deposition and snowfall. In this case, the low content of 7 Be can be explained by its short half-life. It could also be that dust particles raised into the air from the surface as a result of various atmospheric processes initially contain increased concentrations of non-equilibrium 210 Pb. Their sorption ability might have been insufficient for significant accumulation of 7 Be when particles were in the atmosphere. There is most likely an influence by both of these. The high value of 7 Be/ 210 Pbatm ratios in the finest fraction, despite the significant influence of the 7 Be radioactive decay process, confirms the fact that the finely dispersed aerosol component is the carrier concentrator of this isotope. Figure 8 shows that there are five pathways for air masses to arrive at YNAD from their distant sources during winter period. The cluster-mean 5-day backward air-mass trajectories analysis suggested that air masses over Novy Urengoy are mostly from Kazakhstan (20%) and the western region of Russia (20%). Air masses originating in Kola Peninsula, Greenland and Canada accounted for 16%. Trajectories from the Ob estuary and Novaya Zemlya accounted for 26% and the north of For coarse-grained fractions, consisting mainly of large dust particles, the 7 Be/ 210 Pb atm ratio is equal to 1.1-1.2. The 7 Be/ 210 Pb atm ratio of the finely dispersed fraction is much higher-6.1. The low values of the 7 Be/ 210 Pb atm ratio typical for coarse-grained fractions could indicate that these particles represent the material whose radionuclide composition was formed long before its entry into the atmosphere and subsequent precipitation onto the Earth's surface as a part of dry deposition and snowfall. In this case, the low content of 7 Be can be explained by its short half-life. It could also be that dust particles raised into the air from the surface as a result of various atmospheric processes initially contain increased concentrations of non-equilibrium 210 Pb. Their sorption ability might have been insufficient for significant accumulation of 7 Be when particles were in the atmosphere. There is most likely an influence by both of these. The high value of 7 Be/ 210 Pb atm ratios in the finest fraction, despite the significant influence of the 7 Be radioactive decay process, confirms the fact that the finely dispersed aerosol component is the carrier concentrator of this isotope. Figure 8 shows that there are five pathways for air masses to arrive at YNAD from their distant sources during winter period. The cluster-mean 5-day backward air-mass trajectories analysis suggested that air masses over Novy Urengoy are mostly from Kazakhstan (20%) and the western region of Russia (20%). Air masses originating in Kola Peninsula, Greenland and Canada accounted for 16%. Trajectories from the Ob estuary and Novaya Zemlya accounted for 26% and the north of the Krasnoyarsk Territory and Yakutia for 18% of the total trajectories. It should be noted that the direction of air masses coming from southern regions with an arid and semi-arid climate to the steppe and semi-desert landscape-geographical zones can make a significant contribution to the total volume of dust particles brought to the Novy Urengoy region. Accordingly, this direction can have an important effect on the regional, not related to local sources, content 210 Pb atm and the 7 Be/ 210 Pb atm ratio. Figure 9 shows histograms characterizing the contribution of the particulate fractions of suspended matter in snow water to 210 Pb atm and 7 Be total activity in snow samples taken in the latitudinal direction from west to east. Two groups of points are distinguished by the contribution of coarse-grained fraction 1 (>3 µm) to the total activity of 7 Be. The first group (Group 1) includes samples numbered 1-4 and 13, where the part of Fraction 1 is greater than 34%. The second group (Group 2) includes samples numbered 7, 12, 14 and 15, with a lower (<19%) contribution of this fraction. At the same time, the main part (48-87%) of 210 Pb atm of all samples is concentrated in Fraction 1.
Atmosphere 2020, 11, x FOR PEER REVIEW 14 of 24 the Krasnoyarsk Territory and Yakutia for 18% of the total trajectories. It should be noted that the direction of air masses coming from southern regions with an arid and semi-arid climate to the steppe and semi-desert landscape-geographical zones can make a significant contribution to the total volume of dust particles brought to the Novy Urengoy region. Accordingly, this direction can have an important effect on the regional, not related to local sources, content 210 Pbatm and the 7 Be/ 210 Pbatm ratio.   According to the same criterion (Figure 10), among the samples taken in the meridional direction (from north to south), Group 1 includes Samples 3 and 8, in which the contribution of the coarsegrained Fraction 1 of the suspended matter in snow water to 7 Be total activity is equal to 54-56%. In the remaining samples (Group 2), 68-90% of the 7 Be is concentrated in the finely dispersed Fraction 3 (<0.45 μm). In all samples, the main part (47-77%) of 210 Pbatm is concentrated in the coarse-grained Fractions 1 and 2.  According to the same criterion (Figure 10), among the samples taken in the meridional direction (from north to south), Group 1 includes Samples 3 and 8, in which the contribution of the coarse-grained Fraction 1 of the suspended matter in snow water to 7 Be total activity is equal to 54-56%. In the remaining samples (Group 2), 68-90% of the 7 Be is concentrated in the finely dispersed Fraction 3 (<0.45 µm). In all samples, the main part (47-77%) of 210 Pb atm is concentrated in the coarse-grained Fractions 1 and 2. A distinctive feature of the samples belonging to Group 1 and Group 2 is the territorial location of the sampling points. All samples representing Group 1 were selected near settlements. Sampling Points 1 and 2 are located on the eastern and western borders of the Novy Urengoy city in the immediate vicinity of the industrial zone. Sample 3 was taken on the western outskirts of the Korotchaevo town, which is a large transport center located 60 km east of Novy Urengoy. Sampling Site 4 is located between Korotchaevo and Novy Urengoy downwind from highways and railways with heavy traffic. Point 8 is located 120 km south of Korotchaevo in the immediate vicinity of the administrative center Tarko-Sale. Sampling Site 13 is located 100 km west of Novy Urengoy, near the large settlement Pangody. All these localities have thermal power stations, large industrial transport companies, a transport network and a number of industrial enterprises. The presence of a developed industrial and social infrastructure implies an increased atmospheric emission of a significant amount of pollutants in the form of dust material and fuel combustion products (smoke and soot) in the winter. The release of such emissions with 7 Be/ 210 Pbatm ratios other than natural values, on the one hand, creates additional conditions for the sorption of 7 Be and 210 Pbatm in the air; on the other hand, it increases the amount of solid substance entering the Earthʹs surface as a part of dry and wet precipitation, accumulating in integrated snowfalls in the immediate vicinity of formation places. Thus, we can say that the snow sampling sites belonging to Group 1 are located in areas with an increased anthropogenic impact. In contrast to Group 1, Group 2 sampling sites are located far (at least 30-40 km) from settlements and are less affected by the anthropogenic factor. It appears that such an attitude is characteristic of dusty material arriving with snowfall from the southern and south-western directions. Figure 11 presents the averaged data characterizing the distribution of 7 Be and 210 Pbatm over the particulate fractions of the suspended matter in snow water from the samples of Group 2. This group A distinctive feature of the samples belonging to Group 1 and Group 2 is the territorial location of the sampling points. All samples representing Group 1 were selected near settlements. Sampling Points 1 and 2 are located on the eastern and western borders of the Novy Urengoy city in the immediate vicinity of the industrial zone. Sample 3 was taken on the western outskirts of the Korotchaevo town, which is a large transport center located 60 km east of Novy Urengoy. Sampling Site 4 is located between Korotchaevo and Novy Urengoy downwind from highways and railways with heavy traffic. Point 8 is located 120 km south of Korotchaevo in the immediate vicinity of the administrative center Tarko-Sale. Sampling Site 13 is located 100 km west of Novy Urengoy, near the large settlement Pangody. All these localities have thermal power stations, large industrial transport companies, a transport network and a number of industrial enterprises. The presence of a developed industrial and social infrastructure implies an increased atmospheric emission of a significant amount of pollutants in the form of dust material and fuel combustion products (smoke and soot) in the winter. The release of such emissions with 7 Be/ 210 Pb atm ratios other than natural values, on the one hand, creates additional conditions for the sorption of 7 Be and 210 Pb atm in the air; on the other hand, it increases the amount of solid substance entering the Earth's surface as a part of dry and wet precipitation, accumulating in integrated snowfalls in the immediate vicinity of formation places. Thus, we can say that the snow sampling sites belonging to Group 1 are located in areas with an increased anthropogenic impact. In contrast to Group 1, Group 2 sampling sites are located far (at least 30-40 km) from settlements and are less affected by the anthropogenic factor. It appears that such an attitude is characteristic of dusty material arriving with snowfall from the southern and south-western directions. Figure 11 presents the averaged data characterizing the distribution of 7 Be and 210 Pb atm over the particulate fractions of the suspended matter in snow water from the samples of Group 2. This group is characterized by a low contribution of coarse fractions (1 and 2) to the total 7 Be content, which is on average about 16%. The main part (~84%) of 7 Be is present in the finely dispersed Fraction 3 consisting of nanosized aerosol particles and colloids. 210 Pb atm is characterized by a different distribution in particulate fractions: its main fraction (~69%) is present in Fractions 1 and 2 and only 31% is included in Fraction 3. We should pay attention to the difference in the values of 7 Be/ 210 Pb atm ratios. This value is 6.3 in the finely dispersed Fraction 3. Regarding the coarse-grained fractions, this ratio is below 1:0.5 in Fraction 1 and 0.8 in Fraction 2. It appears that such an attitude is characteristic of dusty material arriving with snowfall from the southern and south-western directions.
Atmosphere 2020, 11, x FOR PEER REVIEW 17 of 24 distribution in particulate fractions: its main fraction (~69%) is present in Fractions 1 and 2 and only 31% is included in Fraction 3. We should pay attention to the difference in the values of 7 Be/ 210 Pbatm ratios. This value is 6.3 in the finely dispersed Fraction 3. Regarding the coarse-grained fractions, this ratio is below 1:0.5 in Fraction 1 and 0.8 in Fraction 2. It appears that such an attitude is characteristic of dusty material arriving with snowfall from the southern and south-western directions.
(a) (b) Figure 11. Averaged values of particulate fractions contribution (%) to total activity (a) and specific activities (b) of 210 Pbatm and 7 Be in suspended matter in the snow water of Group 2 samples.
The distribution of 7 Be and 210 Pbatm by particulate fractions of suspended matter in snow water for Group 1 samples taken near settlements (Figure 12) differs significantly from Group 2 samples located far from settlements. In Group 1 samples, on average, only 36% of 7 Be is found in Fraction 3. This is significantly less than the 84% corresponding to Group 2. A higher contribution of coarsegrained fractions to the total activity is also observed for 210 Pbatm. About 84% of this isotope is concentrated in Fractions 1 and 2. The contribution of the finely dispersed fraction decreases to 16%. The 7 Be/ 210 Pbatm ratio is indicative. The value of Fraction 3 (5.3) is close to the value (6.3) observed in Group 2 samples. The 7 Be/ 210 Pbatm ratios of the coarse-grained fractions reach 1.8-1.9. This is three times higher than in Group 2. The close values of the 7 Be/ 210 Pbatm ratios observed for Fractions 1 and 2 in both groups of samples suggest that the nature of the accumulation of these isotopes in dust particles, which vary in a very wide range from 0.45 to hundreds of μm, is the same under the same conditions. The distribution of 7 Be and 210 Pb atm by particulate fractions of suspended matter in snow water for Group 1 samples taken near settlements (Figure 12) differs significantly from Group 2 samples located far from settlements. In Group 1 samples, on average, only 36% of 7 Be is found in Fraction 3. This is significantly less than the 84% corresponding to Group 2. A higher contribution of coarse-grained fractions to the total activity is also observed for 210 Pb atm . About 84% of this isotope is concentrated in Fractions 1 and 2. The contribution of the finely dispersed fraction decreases to 16%. The 7 Be/ 210 Pb atm ratio is indicative. The value of Fraction 3 (5.3) is close to the value (6.3) observed in Group 2 samples. The 7 Be/ 210 Pb atm ratios of the coarse-grained fractions reach 1.8-1.9. This is three times higher than in Group 2. The close values of the 7 Be/ 210 Pb atm ratios observed for Fractions 1 and 2 in both groups of samples suggest that the nature of the accumulation of these isotopes in dust particles, which vary in a very wide range from 0.45 to hundreds of µm, is the same under the same conditions. The samples of Group 1 and Group 2 differ not only in the contributions of different fractions to the total activity of 7 Be and 210 Pbatm in snow waters. Significant differences are also observed in the specific activities of these fractions, calculated per unit of snow water volume (Figures 11,12). The specific activity of 7 Be in the finely dispersed Fraction 3 in the Group 1 samples (101.3 mBq L -1 ) is almost two times lower than that in the Group 2 samples (192.3 mBq L -1 ). In the coarse-grained fractions, the opposite picture is observed-higher specific activities in Group 1. This difference reaches a threefold level in Fraction 2 (25.2 and 8.1 mBq L -1 ). In Fraction 1, this difference is the most significant-more than five times (155.0 and 29.3 mBq L -1 ). Regarding 210 Pbatm, these differences are not so significant, but the general trend remains the same. The specific activity of 210 Pbatm in Fraction 1 of the Group 1 samples (19.1 mBq L -1 ) is 1.6 times lower than in Group 2 samples (30.4 mBq L -1 ). In Fraction 2, this ratio is 0.78 (13.9 and 10.8 mBq L -1 ), and in Fraction 3, it is 0.68 (83.7 and 56.6 mBq L -1 ). Despite significant differences in the redistribution of 7 Be and 210 Pbatm activities between particulate fractions of suspended matter in the samples of different groups, their total activities in snow waters differ, but not so substantially. The total specific activity of 7 Be in the Group 1 samples (281.6 mBq L -1 ) is 1.23 times higher (229.6 mBq L -1 ) than it is in Group 2. Regarding 210 Pbatm, this value is 1.19 (116.7 and 97.8 mBq L -1 ). Thus, it can be stated that, in samples from areas with an increased anthropogenic impact, the specific activities of 7 Be and 210 Pbatm in suspended matter in snow water are on average 20% higher than in samples from clean areas.
The division of the studied samples into groups according to the territorial location of their sampling sites can be clearly seen in the scatter diagrams constructed in the coordinates of the 7 Be and 210 Pbatm activities. Figure 13 shows the scatter diagrams of 7 Be and 210 Pbatm in specific activities and seasonal deposition fluxes for the coarse-grained Fraction 1 of the suspended matter in snow water. On both graphs, two areas of points are clearly distinguished, corresponding to the Group 1 The samples of Group 1 and Group 2 differ not only in the contributions of different fractions to the total activity of 7 Be and 210 Pb atm in snow waters. Significant differences are also observed in the specific activities of these fractions, calculated per unit of snow water volume (Figures 11 and 12). The specific activity of 7 Be in the finely dispersed Fraction 3 in the Group 1 samples (101.3 mBq L −1 ) is almost two times lower than that in the Group 2 samples (192.3 mBq L −1 ). In the coarse-grained fractions, the opposite picture is observed-higher specific activities in Group 1. This difference reaches a threefold level in Fraction 2 (25.2 and 8.1 mBq L −1 ). In Fraction 1, this difference is the most significant-more than five times (155.0 and 29.3 mBq L −1 ). Regarding 210 Pb atm , these differences are not so significant, but the general trend remains the same. The specific activity of 210 Pb atm in Fraction 1 of the Group 1 samples (19.1 mBq L −1 ) is 1.6 times lower than in Group 2 samples (30.4 mBq L −1 ). In Fraction 2, this ratio is 0.78 (13.9 and 10.8 mBq L −1 ), and in Fraction 3, it is 0.68 (83.7 and 56.6 mBq L −1 ). Despite significant differences in the redistribution of 7 Be and 210 Pb atm activities between particulate fractions of suspended matter in the samples of different groups, their total activities in snow waters differ, but not so substantially. The total specific activity of 7 Be in the Group 1 samples (281.6 mBq L −1 ) is 1.23 times higher (229.6 mBq L −1 ) than it is in Group 2. Regarding 210 Pb atm , this value is 1.19 (116.7 and 97.8 mBq L −1 ). Thus, it can be stated that, in samples from areas with an increased anthropogenic impact, the specific activities of 7 Be and 210 Pb atm in suspended matter in snow water are on average 20% higher than in samples from clean areas.
The division of the studied samples into groups according to the territorial location of their sampling sites can be clearly seen in the scatter diagrams constructed in the coordinates of the 7 Be and 210 Pb atm activities. Figure 13 shows the scatter diagrams of 7 Be and 210 Pb atm in specific activities and seasonal deposition fluxes for the coarse-grained Fraction 1 of the suspended matter in snow water. On both graphs, two areas of points are clearly distinguished, corresponding to the Group 1 and Group 2. In the samples of Group 1, a strong correlation was observed both between specific activities (r = 0.95) and between the seasonal deposition fluxes (r = 0.99) of 7 Be and 210 Pb atm . Correlations in Group 2, despite a noticeable linear trend in the distribution of points on the scatter-plots, are much lower. The correlation coefficient of specific activities is only 0.13. The correlation of seasonal deposition fluxes is more significant (r = 0.45). If we consider the entire set of points, including both groups, as a whole, then the correlation between 7 Be and 210 Pb atm in both specific activities and seasonal deposition fluxes is very high at r = 0.82 and r = 0.85, respectively. The samples of Group 1 and Group 2 can be confidently identified in Fraction 2 of suspended matter in snow water. In the 7 Be-210 Pbatm scatter diagrams shown in Figure 14, two regions corresponding to the indicated groups can also be distinguished. As in the case of Fraction 1, Fraction 2 is characterized by a high correlation between the seasonal deposition fluxes of 7 Be and 210 Pbatm in the Group 1 samples. The correlation coefficient in this case is r = 0.94. In Group 2, this correlation is low (r = 0.37). No strong correlation was observed in the specific activities of 7 Be and 210 Pbatm in Fraction 2. The correlation coefficients are 0.47 in Group 1 and 0.55 in Group 2. As regards the whole set of points, including both groups, the correlation between 7 Be and 210 Pbatm in both specific activities and seasonal deposition fluxes is low at r = 0.56 and r = 0.50, respectively. In the 7 Be-210 Pbatm scatter diagrams corresponding to the finely dispersed Fraction 3 of suspended matter in snow water (Figure 15), it is not possible to reliably separate the Group 1 and Group 2 samples. It can be noted that the bulk of Group 1 points are concentrated in the lower parts of the graphs. Due to Point 13 falling sharply out of the general sequence ( 7 Be = 210.6; 210 Pbatm = 46.8 mBq L -1 ), a very high correlation between the specific activities of 7 Be and 210 Pbatm (r = 0.96) was observed in Group 1. The correlation coefficient of seasonal deposition fluxes in the Group 1 samples is slightly lower (r = 0.83). A lower correlation of specific activities (r = 0.57) and fairly high for seasonal The samples of Group 1 and Group 2 can be confidently identified in Fraction 2 of suspended matter in snow water. In the 7 Be-210 Pbatm scatter diagrams shown in Figure 14, two regions corresponding to the indicated groups can also be distinguished. As in the case of Fraction 1, Fraction 2 is characterized by a high correlation between the seasonal deposition fluxes of 7 Be and 210 Pb atm in the Group 1 samples. The correlation coefficient in this case is r = 0.94. In Group 2, this correlation is low (r = 0.37). No strong correlation was observed in the specific activities of 7 Be and 210 Pb atm in Fraction 2. The correlation coefficients are 0.47 in Group 1 and 0.55 in Group 2. As regards the whole set of points, including both groups, the correlation between 7 Be and 210 Pb atm in both specific activities and seasonal deposition fluxes is low at r = 0.56 and r = 0.50, respectively. The samples of Group 1 and Group 2 can be confidently identified in Fraction 2 of suspended matter in snow water. In the 7 Be-210 Pbatm scatter diagrams shown in Figure 14, two regions corresponding to the indicated groups can also be distinguished. As in the case of Fraction 1, Fraction 2 is characterized by a high correlation between the seasonal deposition fluxes of 7 Be and 210 Pbatm in the Group 1 samples. The correlation coefficient in this case is r = 0.94. In Group 2, this correlation is low (r = 0.37). No strong correlation was observed in the specific activities of 7 Be and 210 Pbatm in Fraction 2. The correlation coefficients are 0.47 in Group 1 and 0.55 in Group 2. As regards the whole set of points, including both groups, the correlation between 7 Be and 210 Pbatm in both specific activities and seasonal deposition fluxes is low at r = 0.56 and r = 0.50, respectively. In the 7 Be-210 Pbatm scatter diagrams corresponding to the finely dispersed Fraction 3 of suspended matter in snow water (Figure 15), it is not possible to reliably separate the Group 1 and Group 2 samples. It can be noted that the bulk of Group 1 points are concentrated in the lower parts of the graphs. Due to Point 13 falling sharply out of the general sequence ( 7 Be = 210.6; 210 Pbatm = 46.8 mBq L -1 ), a very high correlation between the specific activities of 7 Be and 210 Pbatm (r = 0.96) was observed in Group 1. The correlation coefficient of seasonal deposition fluxes in the Group 1 samples is slightly lower (r = 0.83). A lower correlation of specific activities (r = 0.57) and fairly high for seasonal In the 7 Be-210 Pb atm scatter diagrams corresponding to the finely dispersed Fraction 3 of suspended matter in snow water (Figure 15), it is not possible to reliably separate the Group 1 and Group 2 samples.
It can be noted that the bulk of Group 1 points are concentrated in the lower parts of the graphs. Due to Point 13 falling sharply out of the general sequence ( 7 Be = 210.6; 210 Pb atm = 46.8 mBq L −1 ), a very high correlation between the specific activities of 7 Be and 210 Pb atm (r = 0.96) was observed in Group 1. The correlation coefficient of seasonal deposition fluxes in the Group 1 samples is slightly lower (r = 0.83). A lower correlation of specific activities (r = 0.57) and fairly high for seasonal deposition fluxes (r = 0.82) were observed in the Group 2 samples. As in the case of the coarse-grained Fraction 1, regarding the entire set of points of Fraction 3, which includes both groups, there is a high correlation between 7 Be and 210 Pb atm in both specific activities and seasonal deposition fluxes at r = 0.81 and r = 0.85, respectively. Thus, there is a significant increase in the contribution of coarse-grained fractions of suspended matter in snow water to the total activity of 7 Be in snow precipitation falling in areas with increased anthropogenic impact. It has been shown by Papastefanou and Ioannidou [40] that "in the activity size distribution of ambient aerosols, 7 Be is shifted to large particle sizes in the presence of pollutants. Removal of small aerosol particles in the submicron size range of the activity size distribution either by scavenging or by deposition of particles on any surface may result in a depletion of small particles in the activity size distribution. Subsequent 7 Be condensation on all aerosols effectively enriches large particles in the activity size distribution". Figure 8 shows that there are five pathways for air masses to arrive at YNAD from their distant sources during winter period. The cluster-mean 5-day backward air-mass trajectories analysis suggested that air masses over Novy Urengoy are mostly from Kazakhstan (20%) and the western region of Russia (20%). Air masses originating in Kola Peninsula, Greenland and Canada accounted for 16%. Trajectories from the Ob estuary and Novaya Zemlya accounted for 26% and the north of the Krasnoyarsk Territory and Yakutia for 18% of the total trajectories. It should be noted that the direction of air masses coming from southern regions with an arid and semi-arid climate to the steppe and semi-desert landscape-geographical zones can make a significant contribution to the total volume of dust particles brought to the Novy Urengoy region. Accordingly, this direction can have an important effect on the regional, not related to local sources, content 210 Pbatm and the 7 Be/ 210 Pbatm ratio.

Conclusions
The study of the radionuclide composition of snowfall accumulated during the winter period of 2018-2019 in the Yamal-Nenets Autonomous District (Russia) made it possible to obtain the first data on the joint deposition of 7   Thus, there is a significant increase in the contribution of coarse-grained fractions of suspended matter in snow water to the total activity of 7 Be in snow precipitation falling in areas with increased anthropogenic impact. It has been shown by Papastefanou and Ioannidou [40] that "in the activity size distribution of ambient aerosols, 7 Be is shifted to large particle sizes in the presence of pollutants. Removal of small aerosol particles in the submicron size range of the activity size distribution either by scavenging or by deposition of particles on any surface may result in a depletion of small particles in the activity size distribution. Subsequent 7 Be condensation on all aerosols effectively enriches large particles in the activity size distribution".

Conclusions
The study of the radionuclide composition of snowfall accumulated during the winter period of 2018-2019 in the Yamal-Nenets Autonomous District (Russia) made it possible to obtain the first data on the joint deposition of 7 Be, 210 Pb atm and 137 Cs on the Earth's surface in the Arctic region of Western Siberia.
The seasonal deposition fluxes of 7 Be and 210 Pb atm in winter, calculated to the time of sampling (late April 2019), averaged 58.7 and 25.2 Bq m −2 season −1 . The average specific activity of 7 Be and 210 Pb atm in snow water was 248.0 and 104.5 mBq L −1 , respectively. The median value of 7 Be/ 210 Pb atm ratios for the entire set of samples is 2.3 (1.6-3.8). Taking into account decay and buildup corrections during the snow cover accumulation period, the actual value of 7 Be total flux in winter can be estimated at the level of 156.1 Bq m −2 season −1 . The seasonal deposition flux of 137 Cs from the atmosphere was low compared to 7 Be and 210 Pb atm and did not exceed 0.39 Bq m −2 season −1 at all studied sampling points. This indicates an insignificant modern flux of this radionuclide from the atmosphere.
A correlation was observed between the seasonal deposition fluxes of 7 Be and 210 Pb atm and the amount of precipitation (r = 0.75 and 0.88). Such high levels of correlation are explained by the fact that washout with precipitation is one of the most important mechanisms for removing these isotopes from the atmosphere. Exploring the nature of 7 Be and 210 Pb atm combined deposition shows a noticeable correlation (r = 0.55) between the values of their specific activities and a strong correlation between the seasonal deposition fluxes of 7 Be and 210 Pb atm (r = 0.86).
The separation of suspended matter in snow water by particulate fractions showed that the studied isotopes were present in all the extracted fractions: >3, 0.45-3 and <0.45 µm. The main part of 210 Pb atm in all the studied samples was in the coarse-grained fraction >3 µm, with an average value of 63.3%. The part of this fraction in the total activity of 7 Be was lower and averaged 29.7%. The contribution of suspended matter with a fraction size from 3 to 0.45 µm to the total activity was small and averaged 11.4% for 210 Pb atm and 5.7% for 7 Be. Most of the 7 Be (64.6%) was contained in finely dispersed aerosols, colloids, or a dissolved component (fraction <0.45 µm). The particulate fractions of the suspended matter of snow waters differed sharply in terms of 7 Be/ 210 Pb atm ratios. 7 Be/ 210 Pb atm ratios in coarse-grained fractions consisting mainly of dust particles whose sizes range from 0.45 to hundreds of µm took values from 1.1 to 1.2. The 7 Be/ 210 Pb atm ratio in the finely dispersed fraction <0.45 µm was significantly higher-6.1. Such high values of the 7 Be/ 210 Pb atm ratio in the finest fraction, despite the significant influence of the radioactive decay of 7 Be, confirm the fact that it is the finely dispersed aerosol component that is the carrier concentrator of this isotope.
According to the ratio of the contributions of the particulate fractions of the suspended matter in snow water to the total activity of 7 Be and 210 Pb atm , as well as the specific activities of these isotopes in the fractions, two groups of samples were identified as having a clear territorial location. The sampling points that made up Group 1 were located in areas with a high anthropogenic impact, close to large settlements. Group 2 samples were taken at points located in areas with a smaller anthropogenic impact, far (at least 30-40 km) from the settlements. The main distinctive feature of the Group 1 samples compared to Group 2 was the significantly lower contribution of the finely dispersed fraction <0.45 µm to the total 7 Be activity in the suspended matter of snow water: 36% and 84%, respectively. Here, the contribution of the coarse-grained fractions larger than 0.45 µm increased from 16 to 64%. 7 Be/ 210 Pb atm ratios in the finely dispersed fractions of both groups were similar: 5.3 (Group 1) and 6.3 (Group 2). The coarse-grained fractions of the Group 1 samples were characterized by higher 7 Be/ 210 Pb atm ratios, compared to Group 2: 1.8-1.9 and 0.5-0.8, respectively. Thus, a significant increase in the contribution of the coarse-grained fractions of suspended matter in snow water to the total activity of 7 Be in snow precipitation was observed in territories with a higher anthropogenic impact.