Ambient atmospheric aerosol measurements were conducted over the Arctic Ocean aboard the icebreaker RV Polarstern (PS131), operated by Alfred Wegener Institute, Germany. The expedition PS131 named ATlantic WAter pathways to the ICE in the Nansen basin and Fram Strait (ATWAICE) to the central Arctic, was carried out during the summer period (28 June to 17 August 2022), during which aerosol measurements were conducted from 29 June to 12 August. The ship track during the campaign is shown in Fig. 1. The cruise covered the Arctic Ocean (including both the North Sea and the Greenland Sea) and the remote north-western Greenland Sea. Polarstern crossed the Arctic Circle during the night of 2 July and proceeded towards the eastern Fram Strait, where it navigated between 5 and 10 July through the warm, saline waters of the west Spitsbergen current. By 11 July, Polarstern reached the continental slope north of Svalbard, continuing northwest into denser ice on 12 July. On 22 July, Polarstern travelled northwest to the Gakkel ridge, reaching the expedition's northernmost point on 25 July. The southward transit towards the Fram Strait began on 2 August. More details about ATWAICE cruise and research area are provided in Kanzow (2023).

Figure S1 in the Supplement illustrates the temporal evolution of meteorological parameters measured aboard RV Polarstern during the expedition. Wind speeds generally ranged between 4 and 14 m s⁻¹ during the observation period, with several transient peaks exceeding 12 m s⁻¹, notably around 7 to 9 July, 16 to 18 July, and 6 to 8 August. At the beginning of the cruise, while the ship was in the sub-Arctic latitudes and the Norwegian Sea, air temperatures were relatively high (∼ 10 to 18 °C), accompanied by moderate relative humidity (RH) values (∼ 60 %–80 %). As the vessel advanced northward into the marginal ice zone and eventually the central Arctic, a marked and sustained drop in temperature occurred beginning around 3 to 5 July, stabilizing around or below 2–5 °C throughout much of mid-to-late July. During this same period, RH increased significantly, frequently exceeding 90 %, indicating a colder, more saturated boundary layer consistent with ice-covered or near-ice environments. A notably colder and humid period is observed from approximately 23 to 30 July, coinciding with the ship's passage through densely packed sea ice. Mid July (around 15 to 20 July) shows an interesting deviation from the preceding trend, marked by temperature increase (up to ∼ 8 °C) and more variable RH, associated with a warm air mass intrusion over the marginal ice zone. Toward the end of the cruise in early August, another warming phase is noted, particularly from 30 July to 3 August, when the ship transitioned from ice-covered regions to open-ocean conditions. More details regarding the ATWAICE cruise are available elsewhere (Kanzow, 2023).

The measurements of aerosol particles were made from the specifically configured aerosol measurement container on the “Peildeck” of the ship, with the instruments sampling the air from a common aerosol inlet. To minimize the influence of ambient moisture, Nafion membrane dryers were integrated into the sampling system, maintaining the relative humidity of the sampled air below 40 %. Measurements of rBC particles were performed using a Single Particle Soot Photometer (SP2, Model: SP2-D; Droplet Measurement Technologies, USA), which operates at 0.12 L min⁻¹. SP2 utilizes the laser-induced incandescence technique to measure rBC properties using an Nd:YAG laser at 1064 nm (Schwarz et al., 2008). The amplitude of the incandescence signal from SP2 is proportional to the rBC mass present in BC-containing particles (Schwarz et al., 2008).

The leading-edge-only (LEO) fitting technique is commonly employed to reconstruct the scattering signal from SP2 (Gao et al., 2007; Liu et al., 2014) to understand the mixing state of rBC. The reconstructed signal is compared with Mie model values to derive the size of coated BC particles. In this approach, the particle is assumed to exhibit a concentric core-shell morphology, represented as a sphere with the core having a refractive index of 2.26–1.26i and the coating set at 1.5+0i (Moteki et al., 2010). The BC core diameter (Dc) is estimated based on an assumed atmospheric BC density of 1.8 g cm⁻³ (Moteki and Kondo, 2010), while the amplitude of the scattering signal provides information about the scattering cross section of the particles, which is used to derive the optical sizing of the particles (Yang et al., 2025). Prior to measurements, the SP2 was calibrated using Aquadag^® black carbon standards, with a correction factor of 0.75 applied to account for differences from ambient BC (Baumgardner et al., 2012; Laborde et al., 2012; Yang et al., 2025). The coating thickness of BC-containing particles is inferred by comparing the optical diameter (Dp) and the Dc.

The absolute coating thickness (CT) is estimated as, 1CT=(Dp-Dc)/2 The mass median diameter (MMD) is determined by fitting BC core size distributions to a monomodal log-normal distribution function (Liu et al., 2019).

To understand the size-resolved coating thickness of rBC particles during the study period, the rBC particles were classified into an i×j grid with i bins for rBC core diameter and j bins for coating thickness. The total volume of rBC containing particles at each grid point is estimated as (Yang et al., 2025), 2Volumegrid(i,j)=π6Dpi,j3Ni,j=π6(Dc,i+2×CTj)3Ni,j where Dp represents the diameter of the rBC containing particle and N indicates the total number of rBC particles.

In this study, the rBC mass concentration was corrected for the missing fraction of rBC (6±4 %) due to the detection limit of SP2. More detailed information regarding SP2, data interpretation procedures, uncertainties, and caveats is available elsewhere (Moteki and Kondo, 2010; Yang et al., 2025).

To quantify the impacts of rBC particles in the Arctic, we calculated the absorption enhancement factor (Eabs) and mass absorption cross-section (MAC) of rBC particles using Mie theory, constrained by in situ single-particle measurements obtained with SP2 (Yang, 2024). The individual coating thickness was derived assuming a concentric core-shell geometry. To estimate absorption properties, we assumed that each rBC particle can be modelled as a homogeneous spherical core with a concentric, non-absorbing coating (e.g., sulfate or organics). The complex refractive index for the rBC core was set to 1.95+0.96i, consistent with literature values for soot, while the coating refractive index was taken as 1.53+0i (Moteki et al., 2023; Schnaiter et al., 2005; Zhang et al., 2018b). We used a Mie scattering code based on the core-shell solution of Bohren and Huffman (1998) to compute the absorption cross-section of each size bin, both for coated (Cabs,coated) and bare (Cabs,bare) rBC particles.

The absorption enhancement factor was then calculated as: 3Eabs=Cabs,coatedCabs,core This reflects the increase in light absorption caused by the lensing effect of the non-absorbing coating.

In parallel, the mass absorption cross-section (MAC) was derived using, 4MAC=CabsMrBC, where MrBC is the mass of the rBC core in each size bin. The MAC values were computed for both bare and coated particles, providing insight into how mixing modifies the specific absorption capacity of rBC under different atmospheric conditions. This enabled direct comparison across regimes with differing aerosol source histories, atmospheric aging states, and mixing conditions.

The light absorption enhancement (Eabs) estimated here is using an idealized spherical, concentric core-shell representation (Mie theory based). It should be noted that the real atmospheric BC commonly exhibits complex/fractal morphology and heterogeneous mixing/coating structures, for which core-shell Mie representations can overestimate Eabs values that differ from morphology resolved calculations and observations (e.g., Adachi et al., 2010; Ueda et al., 2016; Fierce et al., 2020; Wang et al., 2021; Zhang et al., 2026).

The measurements of equivalent black carbon (eBC) were performed using a multi-angle absorption photometer (MAAP), which measures transmitted and backscattered light from a particle-loaded filter (Petzold and Schönlinner, 2004). Although the MAAP directly measures the absorption coefficient, the results were converted to eBC mass concentration using a predefined mass absorption cross section. In general, eBC measurements were reported at a wavelength of 637 nm, following the recommendations of Müller et al. (2011). A correction factor of 1.05 was applied to account for systematic biases in the retrieval of eBC concentrations.

The aerosol light scattering coefficient was measured using an integrating Nephelometer (Ecotech Aurora 4000). It measures the aerosol total scattering (σsca, between 10 and 170°) and back-scattering coefficients (between 90 and 170°) at three wavelengths (450, 525, and 635 nm). The nephelometer data was corrected following the methodology described by Müller et al. (2011). The detailed description of the main characteristics and the working principle of the integrating nephelometers can be found in Müller et al. (2011).

In addition, aerosol particle sampling was conducted using a high-volume digital aerosol sampler mounted on the rooftop of the aerosol measurement container. After sampling, the samples were stored in aluminium boxes at -20 °C and transported to TROPOS, Leipzig, for further chemical analysis. To account for potential contamination during handling and transport, field blanks were prepared by loading the sampler at the sampling site without drawing air through the system. Measurements of organic carbon and elemental carbon were made using a Sunset OC-EC analyser following the EUSAAR II TOT protocol (Birch and Cary, 1996). The concentrations of selected inorganic species were determined in filtered aqueous extracts (0.45 µm syringe filters, 50 % of the filter extracted in 2 mL ultrapure water) using ion chromatography (ICS3000, Dionex, Sunnyvale, CA, USA), following the methodology described by Müller et al. (2010). Regular instrument calibration and quality control procedures were implemented to ensure the accuracy and reliability of the analytical measurements.

Ship plumes were occasionally detected during the campaign. To ensure that aerosol measurements were not influenced by emissions from the ship's exhaust, the sampling inlet was installed ahead of the ship's engines. Despite this strategic placement, some data points were still affected by ship emissions and had to be filtered out before further analysis to obtain a dataset representing background aerosol concentrations. The following conditions led to data exclusion: Data points were removed when the relative wind direction ranged between 110 and 260°, as this wind pattern could carry exhaust emissions toward the sampling inlet. Measurements taken at wind speeds below 2 m s⁻¹ were discarded since weak winds can cause local turbulence, increasing the risk of exhaust contamination. Sharp increases or abrupt fluctuations in total particle number concentration were considered indicative of contamination and were therefore excluded. Any extreme spikes in the incandescence signal from SP2 were removed, as they were likely linked to ship exhaust plumes. For offline aerosol sampling, an automated pollution-avoidance system was used. This system, which continuously monitored relative wind direction, was integrated with the digital sampler to automatically halt the sampling pumps when airflow originated from the sector associated with ship exhaust contamination.

A Humidity and Temperature PROfiler (HATPRO) microwave radiometer (Rose et al., 2005) was deployed on the Peildeck, adjacent to the aerosol measurement container during the cruise. This instrument continuously measures atmospheric radiances emitted by water vapor, oxygen, and liquid cloud droplets, utilizing seven frequencies between 22 and 31 GHz along a water vapor absorption line and seven additional channels between 51 and 58 GHz within the oxygen absorption complex. With a high temporal resolution of approximately 1 s, HATPRO provides near-continuous monitoring of key atmospheric variables. The primary observational mode involved zenith-pointing measurements, enabling the retrieval of vertically integrated water vapor (IWV), liquid water path (LWP), and vertical profiles of temperature and absolute humidity following established methodologies (e.g., Walbröl et al., 2022). In a shorter observational mode for 15 consecutive minutes each hour, the instrument was observing the surface, and no measurements of the atmosphere were recorded. Additionally, boundary layer scanning at multiple elevation angles was conducted to enhance temperature profiling within the lower troposphere.

Figure 2 shows the temporal evolution of the aerosol light scattering coefficient at 525 nm (σsca), mass concentrations of equivalent black carbon (eBC) and refractory black carbon (rBC) along the cruise track. σsca, eBC and rBC exhibited pronounced variability during the campaign, with comparatively high values during the initial, lower-latitude part of the transect and substantially lower values over the central Arctic.

The hourly σsca ranged from 0.1 and 66 Mm⁻¹, with approximately 90 % of the observations below 25 Mm⁻¹. Higher σsca values observed during the beginning of the campaign, whereas σsca remained mostly below 10 Mm⁻¹ over much of the high Arctic. As the research vessel moved to northern latitudes, σsca generally decreased and remained low over large parts of the central Arctic. This behaviour is consistent with previous summertime observations in the Arctic reporting low aerosol loadings in the central Arctic compared with lower-latitude regions influenced by marine and continental airmasses (Quinn et al., 2002; Tomasi et al., 2007; Schmeisser et al., 2018; Pandolfi et al., 2018; Gogoi et al., 2021; Schmale et al., 2022).

The temporal variability of eBC and rBC broadly followed that of σsca. During the initial phase of the cruise (29 June–3 July), when the ship was located at lower latitudes, eBC frequently exceeded 100 ng m⁻³, with a maximum of 399 ng m⁻³. North of approximately 70° N, eBC decreased significantly, and 95 % of the subsequent observations remained below 40 ng m⁻³. The rBC mass concentration (MrBC) exhibited a similar large-scale pattern, with enhanced values during the lower-latitude part of the transect and low concentrations during the observations in the central Arctic. Nonetheless, episodes of enhanced σsca, eBC, and rBC were observed from 15 to 22 July and 30 July to 3 August, suggesting the transient influence of warm airmass intrusions favourable for enhanced aerosol loadings. This will be discussed in detail in Sect. 3.2.

Although eBC and rBC covaried during the campaign, differences were evident in their absolute magnitudes and short-term variability. These differences likely reflect the distinct measurement principles of the MAAP and SP2, as well as differences in their sensitivity to particle mixing state and aerosol composition (Backman et al., 2017; Asmi et al., 2021, 2025). The correlation between eBC and rBC measured during the study period are provided in the supplementary information (Fig. S2). In addition, elemental carbon (EC) derived from filter samples was mostly below the detection limit of the OC-EC analyser throughout the campaign (Fig. S3), indicating that filter-based EC measurements had limited applicability under the very low aerosol loadings encountered here. For this reason, the following discussion focuses primarily on SP2-derived rBC, which provides higher sensitivity and time resolution under background Arctic conditions.

In order to understand the observed variability in the context of airmass transport pathways, 5 d backward airmass trajectories arriving at the ship position (∼ 100 m a.s.l.) were calculated using NOAA Hybrid Single-Particle Lagrangian Integrated Trajectory model (HYSPLIT) (Stein et al., 2015) overlaid on the Arctic Sea ice concentration data from MODIS-AMSR2 (Spreen et al., 2008; Ludwig et al., 2020) during the cruise period. This is further grouped into eight consecutive airmass transport regimes (SE1 – South easterly 1, NW1 – North westerly 1, SE2 – South easterly 2, WA1 – Warm airmass intrusion 1, NE – North easterly, WA2 Warm airmass intrusion 2, NW2 – North westerly 2, and SE3 – South easterly 3; Fig. 3). These regimes differ in their dominant transport direction and in the relative time spent over continental, marine, and sea-ice covered surfaces. Figure 4a summarizes the fractional contribution of relative time each airmass regimes spent over these three different surface types.

Among all regimes, SE1 showed the highest rBC concentrations (median ∼ 37 ng m⁻³; Fig. 4b). Airmasses during this period indicate transport from lower-latitude regions with a stronger continental influence than during the central Arctic regimes, together with substantial residence time over marine environments. This regime was also characterized by elevated σsca (∼ 36 Mm⁻¹) and a comparatively large contribution of Na⁺ and Cl⁻ to the bulk aerosol composition (Fig. 5), suggesting the simultaneous presence of combustion related aerosols and sea-salt-containing particles. Interpretation of σsca variability based solely on PM₁₀ bulk chemical composition is inherently qualitative because aerosol light scattering depends strongly on particle size distribution and number concentration, not only on mass fraction. In particular, coarse-mode constituents (e.g., Na⁺ and Cl⁻) may dominate mass during marine influence, whereas fine-mode sulfate and organic aerosol can contribute significantly to σsca. Since, our chemical composition of PM₁₀ samples represents bulk, 24 h integrated composition across a broad size range, the discussion of it with respect to σsca is qualitative; scattering depends strongly on particle size distribution and number concentration, and we therefore do not attempt size or component resolved attribution with this. The higher rBC loading observed during SE1 likely reflects the influence of continental outflow and possible shipping emissions, as the measurements were at lower latitudes closer to coastal regions.

In contrast, SE2 and NE were characterized by the lowest rBC concentrations. SE2 was dominated by airmass transport over marine regions (88 %) with limited continental influence (∼ 5 %), whereas NE was associated with airmasses travelling largely within the central Arctic, including over sea-ice-covered regions (∼ 64 % marine and ∼ 33 % sea ice). During both regimes, rBC concentrations remained very low, typically below ∼ 0.6 ng m⁻³, and σsca was also low (∼ 1 Mm⁻¹), particularly during NE. These observations indicate a weak influence of combustion sources with the generally clean summertime central Arctic boundary layer. The lower σsca (∼ 1 Mm⁻¹) during NE may additionally reflect a reduced contribution from open-ocean derived aerosol since it traversed significantly through sea ice covered regions.

The NW1, NW2, and SE3 regimes showed intermediate behaviour in rBC properties in comparison with other regimes. The rBC concentrations during these periods were higher than those observed during SE2 and NE, but substantially lower than those during SE1. The airmass transport during this period indicates mixed transport pathways involving different combinations of marine, sea-ice, and more limited continental influence. The low to modest rBC concentrations observed in these regimes suggest either limited source influence, efficient scavenging during transport, or a combination of both. For example, although NW2 exhibited a relatively strong continental influence, the corresponding rBC concentration remained low. This indicates that longer residence time over continental surfaces did not necessarily translate into enhanced rBC concentrations at the receptor site. It is also important to note that the airmasses during this period passed over comparatively remote regions of Greenland, which may have contributed to the observed lower rBC loading. The warm airmass intrusion periods (WA1 and WA2) were associated with episodic enhancements in aerosol properties relative to the surrounding central Arctic background. These events involving additional synoptic-scale influences are discussed separately in the subsequent section.

Based on the airmass transport pathways with special emphasis on the relatively dominant residence time over the continental and sea ice surface type, in addition to the rBC concentrations, we have segregated the distinct regimes as, polluted (SE1), near-pristine (NW1, NW2 and SE3), pristine (SE2 and NE) and warm airmass intrusions (WA1 and WA2). The aerosol measurements 29 June to 5 July is marked as “polluted” whereas the observations NW1, NW2 and SE3 during 5 to 9 July, 3 to 12 August is marked as “near pristine” and observations during 9 to 15 July and 22 to 30 July is marked as “pristine”. The measurements during warm airmass intrusion period of 15 to 22 July and 30 July to 3 August is marked as WA1 and WA2.

Two warm airmass intrusion periods were observed during the study period, and both were associated with clear changes in thermodynamic conditions and aerosol properties over the central Arctic. These events interrupted the otherwise lower aerosol conditions that prevailed during much of the campaign and were accompanied by enhanced temperature and rBC concentrations. Previous studies have shown that such synoptic-scale intrusions can efficiently transport heat, moisture, and aerosol from lower latitudes into the Arctic (Mortin et al., 2016; Graham et al., 2017; Henderson et al., 2021; Dekoutsidis et al., 2024).

The vertical profiles of temperature and absolute humidity retrieved from HATPRO are shown in Fig. 6. Between 13 and 14 July, an occluded warm front associated with a low-pressure system over the North Atlantic transported warm and moist air. During this period, the temperatures reached up to about 7 °C at an altitude of ∼ 600 m. Subsequently, during the WA1 period, two pronounced episodes of warm and humid air were observed between 15 and 17 July and between 17 and 19 July. These events were associated with consecutive low-pressure systems south of Svalbard and with strong south-easterly flow transporting warm, moist air towards Svalbard and the adjacent Arctic Ocean (Kanzow, 2023). During the second episode, temperatures reached a maximum of 18 °C at ∼ 650 m altitude on 18 July, while integrated water vapour increased to 35 kg m⁻². During these events, Polarstern was mostly in open water on the lee side of Svalbard. A weaker warm air advection event followed on 19 July, but without a similarly strong increase in humidity. During WA2 (30 July to 3 August), as Polarstern began its transit toward the east coast of Greenland into a warm front, warm air masses were observed, with temperatures reaching up to 8 °C at 850 m altitude and integrated water vapor increasing from 14 to 22 kg m⁻². Near the surface, temperatures remained close to 0 °C, accompanied by persistent fog. For the following discussion of aerosol properties, the period from 15 to 22 July is defined as WA1, and that from 30 July to 3 August as WA2.

The two warm airmass regimes differed in their transport history and aerosol characteristics. Based on the backward trajectories shown in Fig. 3 and the surface-type influence (Fig. 4a), WA1 was associated with transport from the Eurasian sector towards the central Arctic, including substantial passage over the Barents Sea. In contrast, WA2 was characterized mainly by marine inflow from the North Atlantic and Nordic Seas, with comparatively limited continental influence before arrival at the ship position. These differences in transport pathways were reflected in the observed rBC properties and in the PM₁₀ chemical composition (Fig. 5).

WA1 showed the highest BC enhancement among the central Arctic regimes. During this period, rBC mass concentrations reached up to 74 ng m⁻³, with a median value of ∼ 3.4 ng m⁻³, while rBC number concentrations also increased relative to the preceding SE2 period (NrBC∼ 0.84 cm⁻³, Fig. 4b–c). eBC concentrations were similarly enhanced and reached up to 111 ng m⁻³. These enhanced values indicate that WA1 was associated with episodic transport of pollution into the central Arctic lower troposphere. WA1 is marked by strong continental outflow from Eurasia with strong passage over the Barents Sea towards the central Arctic. This Barents-sector pathway is widely regarded as the most effective corridor for carrying pollutants from northern Eurasian source regions into the Arctic (Stohl et al., 2013). A smaller subset of airmasses was also passing over the Norwegian Sea. In addition, the airmasses associated with WA1 were observed to affect regions known to contribute pollutants to the Arctic, particularly through gas flaring and metallurgical industrial sources (Stohl et al., 2013; Schulz et al., 2019; Dada et al., 2022). The trajectory analysis suggests that the airmasses sampled during WA1 had a stronger influence from lower-latitude source regions than those associated with the clean central Arctic regimes. In addition, the airmasses passed over regions with enhanced fire activity indicated by satellite fire-pixel data (confirmed by Visible Infrared Imaging Radiometer Suite (VIIRS) satellite data fire-pixel counts, as shown in Fig. S4). Along with this, we observed a significant increase in K⁺, which supports the predominant role of biomass burning influence during this period over the central Arctic. K⁺ has been widely recognized as a good tracer for biomass burning in previous studies (Arun et al., 2019, 2021). The enhanced BC concentrations during WA1 demonstrate the importance of warm airmass intrusions as episodic pathways for transporting biomass burning aerosol into the Arctic marine boundary layer. Similar transport mechanisms have been reported previously for Arctic haze and intrusion events affecting the lower troposphere (Stohl et al., 2013; Schulz et al., 2019; Dada et al., 2022).

In contrast to WA1, WA2 was associated with a lower aerosol loading. During this period, rBC mass concentrations reached up to ∼ 35 ng m⁻³, with a median of ∼ 1.6 ng m⁻³, and the corresponding rBC number concentration ∼ 0.58 cm⁻³. These values are elevated relative to the background regimes but remained clearly lower than those observed during WA1. WA2 was dominated mainly by marine inflow, and the chemical composition showed enhanced SO42- and OC contributions relative to WA1. This suggests that WA2 reflected transport of more aged marine and regionally processed aerosol, with a weaker influence from direct combustion sources compared to WA1.

Earlier studies have shown that summertime Arctic rBC is generally characterized by very low background concentrations, with occasional enhancements linked to transport. Taketani et al. (2016) reported pronounced spatial variability between the North Pacific and Arctic oceans in September, with rBC mass concentrations ranging from 0 to 60 ng m⁻³ and an average of about 1 ng m⁻³, while Schulz et al. (2019) observed that combustion particles constituted only a minor fraction of the aerosol population in the Canadian Arctic during summer, with near-surface rBC concentrations typically below 2 ng m⁻³, reflecting weak exchange between the summer polar dome and mid-latitude airmasses. In the present study, most airmass regimes, including NW1, NW2, SE2, SE3, and NE, exhibited similarly low mean rBC concentrations of about 1.4–1.6 ng m⁻³, with median values of 0.5–0.8 ng m⁻³, indicating that these conditions represent the clean summertime Arctic background (AMAP, 2015; Zanatta et al., 2023; Jurányi et al., 2023). Our observed rBC concentrations are also lower than those reported by Liu et al. (2015) in the European Arctic during spring, where rBC mass concentrations ranged from 20 to 100 ng m⁻³, as expected from the seasonal transition from the spring Arctic haze period to the comparatively cleaner summer atmosphere. At the same time, the two warm airmass intrusion cases demonstrate that episodic transport can still substantially perturb this otherwise low-rBC environment. These enhanced values are comparable to or approach those reported at Arctic receptor sites such as Pallas, Finland (26 ng m⁻³; Raatikainen et al., 2015) and Zeppelin, Svalbard (39 ± 23 ng m⁻³; Zanatta et al., 2018), but remain far lower than those reported for marine and continental regions outside the Arctic, including the remote Atlantic Ocean(∼ 100 ng m⁻³) (Pan et al., 2026), south-eastern Arabian Sea (938 ± 293 ng m⁻³), northern Indian Ocean (546 ± 80 ng m⁻³), equatorial Indian Ocean (206 ± 114 ng m⁻³) (Kompalli et al., 2021), Thumba (670 ± 571 ng m⁻³; Nithin et al., 2026), Mukteshwar in the Himalayas (1000 ± 600 ng m⁻³; Raatikainen et al., 2017), and Lulang on the Tibetan Plateau (310 ± 550 ng m⁻³; Wang et al., 2018). The markedly enhanced BC levels during WA1 (eBC as high as 111 ng m⁻³, rBC as high as 74 ng m⁻³), while clearly elevated relative to background, remain lower than the values observed during warm air-mass intrusions in spring (Dada et al., 2022), in subarctic environments, and in near-source high Arctic sites (Popovicheva et al., 2017). Table 1 summarizes our observed MrBC values in comparison with those reported in previous studies from marine, remote, coastal environments.

Figure 7 shows the mass size distributions of rBC particles for the different airmass regimes during the cruise. The size distribution of rBC is relevant for interpreting its atmospheric processing and radiative effects, as the light absorption properties of BC depend on core size, while the observed mass median diameter (MMD) can be influenced by source characteristics as well as by aging and removal during transport (Shiraiwa et al., 2007; McMeeking et al., 2010; Liu et al., 2014; Taylor et al., 2014; Kompalli et al., 2020, 2021; Yang et al., 2025).

The estimated MMD varied substantially across the different transport regimes. During SE1, the MMD was ∼ 156 nm, i.e., the lowest among all regimes in this study. This value lies within the range commonly reported for polluted environments influenced by fossil fuel combustion, although such comparisons should be interpreted cautiously because the observed size distribution at the receptor site reflects not only source emissions but also atmospheric processing during transport (Laborde et al., 2013; Liu et al., 2019; Kompalli et al., 2020; Lim et al., 2023). As the ship moved away from the lower-latitudes towards the central Arctic, the MMD increased progressively; to ∼ 190 nm during NW1, ∼ 207 nm during SE2, and ∼ 225 nm during NE. During NW2 and SE3, the MMD remained similarly larger, at ∼ 217 nm and ∼ 218 nm, respectively. These observations of MMD indicate a systematic increase in rBC core size from the lower-latitudes towards the central Arctic regimes. However, this gradient should not be interpreted as a unique fingerprint of changing emission sources. In remote regions, rBC size distributions can be modified during transport by size-dependent removal and atmospheric processing, including cloud processing and coagulation (Pan et al., 2026). Therefore, in the absence of independent source-specific tracers and high-resolution chemical composition information, the increase in MMD towards higher latitudes is interpreted here as reflecting the combined effects of distinct sources and atmospheric processing rather than as direct evidence of a transition to a specific source type.

A pronounced enhancement in MMD was observed during the warm airmass intrusion regime WA1, for which the estimated MMD was higher than 260 nm. This value is substantially larger than those observed during the background central Arctic regimes and coincided with enhanced rBC mass concentrations during the same period. As discussed in Sect. 3.2, WA1 was associated with transport from lower-latitude source regions along with the evidence for biomass burning influence. In contrast, during WA2, the MMD remained close to 220 nm, comparable to the values observed during the central Arctic background conditions. This difference between WA1 and WA2 further indicates that warm airmass intrusions into the central Arctic do not exert a uniform influence on the microphysical characteristics of rBC; rather, their effect on rBC size distribution depends on the transport pathways and the atmospheric processing within the advected airmass.

Changes in MMD during long-range atmospheric transport can arise from multiple competing processes. Size dependent wet removal may preferentially remove larger BC containing particles under some conditions and thereby shift the distribution towards smaller diameters (Moteki et al., 2012; Schulz et al., 2019). Conversely, coagulation and condensational aging may increase the apparent characteristic size of BC containing particles or preferentially preserve larger cores under specific transport conditions (Tunved et al., 2013; Schulz et al., 2019). The observed MMD thus reflects the combined influence of source emissions, removal, and atmospheric processing. This is particularly relevant in the Arctic, where transport pathways, cloud interactions, and scavenging processes jointly control the abundance and properties of BC reaching the central Arctic atmosphere (Liu et al., 2011; Schulz et al., 2019).

The MMD values observed during this campaign are within the broad range reported previously for Arctic and other remote environments, although substantial variability exists across regions and airmass transport regimes. In the present study, MMD ranged from ∼ 156 nm during SE1 to ∼ 264 nm during WA1, whereas the Arctic background regimes were characterized by MMD around 190–227 nm. These values are comparable to those reported for the Arctic Ocean in summer (∼ 170 nm; Taketani et al. (2016), Pallas in the Finnish Arctic (161–231 nm; Raatikainen et al., 2015), and Zeppelin during spring (Zanatta et al., 2018), but are higher thatn the 119–134 nm reported for the high Canadian Arctic by Schulz et al. (2019). Previous studies from other remote and coastal environments similarly show a wide spread, including 140 nm at Melpitz (Yang et al., 2025), 153–170 nm at Catalina Island (Ko et al., 2020), 200–220 nm at Fukue Island (Shiraiwa et al., 2008), and ∼ 192 nm at Thumba (Nithin et al., 2026). These comparisons indicate that the MMD values measured in this study are generally high relative to those reported for other marine/remote/coastal environments.

Figure 8 shows the size-resolved coating thickness of rBC particles estimated during the study period, along with the normalized rBC particle volume. The size resolved coating thickness (CT) of rBC particles, along with the number concentration of particles is given in Fig. S5. The size resolved CT classification provided a more direct insight into the mixing state of rBC particles in this study. It is evident that, throughout the study period, two distinct regions of rBC core sizes (below Dc ∼ 150 nm and above Dc ∼ 150 nm) consistently exhibited relatively higher volume of coated rBC. This suggests that the rBC population during the campaign exhibited pronounced mixing-state heterogeneity. The repeated occurrence of two enhanced-volume domains, one associated with smaller cores and another with larger cores, indicates that non-BC material was distributed unevenly across the rBC population, with some particles remaining weakly processed while others acquired substantial coatings. This particle-to-particle variability is important because the radiative effects of rBC depends not only on the mean coating thickness but also on how the coating is distributed among particles of different core sizes, as emphasized in recent studies (Fierce et al., 2016, 2020; Zeng et al., 2024; Zhai et al., 2022).

The higher contribution from coated larger rBC cores under the northerly and near-pristine regimes likely reflects aged, internally mixed particles that underwent substantial atmospheric processing during long-range transport to the central Arctic. In this study, we found the relatively higher coated volume observed at both smaller and larger cores during SE2 and WA1 points to a broader spread of core-shell combinations, implying a more diverse and complex mixing state under those regimes in the Arctic. Such a pattern suggests that, in addition to aged large-core particles, a greater fraction of smaller rBC cores had also acquired sufficient condensed material to become internally mixed. Condensational aging generally enhances coating accumulation more efficiently on smaller BC cores than on larger ones (Seinfeld and Pandis, 2006). The bottom-left region with null values corresponds to smaller rBC particles that show neither positive nor negative coating thickness (CT), due to the detection limitations of the SP2, as reported in several studies (Ko et al., 2020; Yang et al., 2025). This detection limitation restricts the retrieval of coating information from scattered light for smaller rBC particles. As a result, the mixing state information of a substantial portion of these smaller rBC particles remains unresolved. This missing fraction of CT results in overestimation of CT when estimating the absolute coating thickness across the entire size range.

In order to provide a statistical insight into the mixing state information of rBC particles, the frequency distribution of CT estimated in the 180–300 nm is shown in Figure 9. The median CT for the near pristine, pristine and warm airmass conditions during the study ranged from 14–18, 9–20 and 12–15 nm respectively. It is found that coating thickness was relatively higher in regions influenced mainly by northerly airmass advections (NE, NW1 and NW2, with CTmedian∼ 20 nm, CTmedian∼ 18 nm, and CTmedian∼ 18 nm respectively), while the lowest coating thickness is found during SE2 (CTmedian∼ 9 nm). In northerly airmass regimes, airmasses likely experienced prolonged atmospheric residence times and active secondary aerosol condensation, leading to more internally mixed, coated rBC particles. Specifically for the northerly airmasses, we observed a higher fractional contribution to the total aerosol mass from SO42-, ∼ 18 % and OC ∼ 48 %) especially during NE. The prolonged transport through marine and sea ice covered environments (Fig. 4a) and the associated extended atmospheric aging of rBC particles during NE could have facilitated the condensation of secondary species onto rBC cores. However, for the NW2, particularly when the ship was located in the Greenland Sea, the contributions from SO42- and OC were even higher. These increased fractions of organics and sulfate may have contributed significantly to the observed enhancement in the coating of rBC cores during this period. It is important to note that the NE regime was predominantly influenced by airmasses traversing oceanic and sea-ice-covered regions, whereas the NW2 regime was more strongly affected by continental outflow from Greenland. However, since simultaneous real-time submicron aerosol chemical composition measurements are not available alongside rBC data, we cannot definitively attribute the enhanced coating to these chemical species. Furthermore, the PM₁₀ chemical composition discussed above reflects bulk aerosol composition integrated over a 24 h period and across a broad size range, its relationship to SP2-derived submicron rBC coating thickness is qualitative; therefore, sulfate and OC fractions should not be interpreted as quantitative indicators of rBC coating.

During WA1, the median CT is ∼ 12 nm. This suggests that warm airmass intrusions have a notable influence on the coating of rBC particles, as evidenced by the difference in CT between SE2 (prior to the warm airmass intrusion) and WA1. This difference could be attributed to the presence of aged rBC particles transported into the central Arctic during these intrusions from biomass-burning sources, as discussed before. During WA2, as the ship re-entered the marginal ice zone, it was influenced by a warm airmass advection from the southeast, which primarily passed over oceanic regions. The estimated median CT during this period is ∼ 15 nm. Interestingly, during the second warm airmass intrusion, the prevailing airmasses shifted from north-easterly to south-easterly, which could have contributed to the observed changes in coating thickness. CT, along with a relatively higher contribution of airmasses traversing open oceanic regions, suggests relatively aged rBC particles during WA2. This could have significantly influenced the observed changes in CT between WA2 and WA1, where continental emissions and biomass-burning sources were more prominent. In addition, we noticed that the mass fractions of SO42-, NH4+, MSA, and C₂O42- were higher during WA2 than during WA1. Further, we found significant correlations between NH4+ and SO42- (R2=0.5), SO42- and MSA (R2=0.4), C₂O42- and NO3- (R2=0.6), suggesting enhanced secondary aerosol formation/photochemical aging during this period. Consistent with this, Arun et al. (2021; and references therein) reported substantial organic aerosol formation and photochemical aging in a remote environment over the eastern Himalayas. These findings further support the aged nature of the aerosols during WA2, which likely contributed to the relatively high CT during WA2.

Despite evidence of long-range transport, rBC particles in this study showed thin to moderate coatings, unlike previous observations in background environments with thickly coated rBC particles (Motos et al., 2020; Yang et al., 2025; Pan et al., 2026). This infers lower precursor gas concentrations and limited condensation under summer Arctic conditions, where clean background air and reduced SOA formation can suppress coating even on aged rBC particles. Additionally, in-cloud and below-cloud scavenging, especially during the prevalent fog and low-level cloud conditions of Arctic summer, likely play a significant role in removing hydrophilic or heavily coated rBC particles. The persistent presence of clouds and fog enhances wet scavenging, which significantly influence the rBC properties. This effect is particularly evident in our observations from warm airmass intrusions (WA1), which, despite being associated with biomass burning and continental sources, showed significantly larger rBC cores (MMD > 260 nm) but surprisingly thinner coatings than background airmasses, such as those from the NE and NW sectors. These background regimes, dominated by airmasses traversing marine or consolidated sea-ice regions, featured moderately large rBC cores (MMD ∼ 220 nm) with moderate coatings, suggesting the combined influence of aerosol aging and active wet scavenging. The lower coating thickness observed in the southeast sectors (e.g., SE2), despite large MMDs, indicate that particle aging alone does not necessarily lead to thicker coatings; rather, prevailing environmental conditions, such as low oxidant levels or cleaner marine airmasses, can suppress formation of coating on rBC particles. Coating thickness may also be modulated by the available condensation sink. Under high particle number conditions, condensable material can be distributed across a larger population, potentially limiting per-particle coating growth even when precursors are present. Although we cannot quantify this effect here because SP2 number concentrations represent only BC-containing particles within the instrument's detection range (and not the full aerosol population), this mechanism could also contribute to the relatively low CT observed during high loading regimes such as WA1.

To understand the role of microphysical properties and mixing state in modulating BC light absorption, we quantified the light absorption enhancement (Eabs) and mass absorption cross-section (MAC) of rBC particles using core-shell Mie theory, constrained by our in-situ single-particle observations obtained using SP2 as described in Sect. 2.2. In this method, Eabs represents the increase in light absorption by coated rBC relative to uncoated (bare) BC, while MAC provides the corresponding absorption efficiency per unit rBC mass. For smaller core sizes, even modest coatings can result in substantial enhancement due to the strong lensing effect. However, as the core size increases, the relative impact of coatings on absorption enhancement diminishes. Figure S6 shows the size-resolved Eabs and MAC of rBC particles across the different airmass regimes. In the following discussion, we focus on the ranges defined by the 80–500 and 180–300 nm core size intervals. The size range 80 to 500 nm indicates the upper limit of Eabs and MAC, possibly overestimated due to the missing part of mixing state information in the lower size ranges as discussed. Similarly, the 180–300 nm size range corresponds to the lower range of Eabs and MAC values in this study. The size-resolved Eabs values ranged from approximately 1.0 to 1.6 during the study period (Fig. 10). During the polluted initial phase of the campaign, when the sampled airmasses were influenced predominantly by continental and anthropogenically processed sources, Eabs ranged from ∼ 1.1 to 1.4 (Fig. 10a), with corresponding MAC values of ∼ 6.6–8.0 m² g⁻¹ (Fig. 10b). These MAC values are comparable to those reported for anthropogenically influenced environments, including ∼ 6.5 m² g⁻¹ in South China, ∼ 7.5 m² g⁻¹ in California, ∼ 8.4 m² g⁻¹ in Karlsruhe, and ∼ 7.0 m² g⁻¹ during ACE-Asia flight measurements (Lan et al., 2013; Cappa et al., 2019; Linke et al., 2016; Clarke et al., 2004), indicating moderate absorption enhancement under polluted conditions. They are, however, lower than values reported for the regions such as ∼ 9.5–10.4 m² g⁻¹ at Nordic background sites, ∼ 11.8 m² g⁻¹ in Nanjing, and ∼ 12.3 m² g⁻¹ at Jeju Island (Zanatta et al., 2016; Ma et al., 2020; Kondo et al., 2009).

Interestingly, during WA1, despite the predominant influence of biomass-burning emissions, both Eabs (∼ 1.0–1.2) and MAC (∼ 6.5–8.0 m² g⁻¹) remained relatively low, even lower than those observed under pristine/background Arctic conditions (Eabs ∼ 1.1–1.6; MAC ∼ 6.5–8.7 m² g⁻¹). This is notable because biomass-burning-influenced aerosols often exhibit substantially stronger absorption enhancement and higher MAC after atmospheric aging. For example, previous studies have reported Eabs values of ∼ 1.38 during biomass-burning events in Boulder, ∼ 1.5 in the Pearl River Delta, and synthesis-based values of ∼ 1.83 for biomass-burning smoke globally (Lack et al., 2012; Wu et al., 2018; Asmi et al., 2025). Similarly, MAC values of ∼ 13.3 m² g⁻¹ in Texas biomass-burning plumes and a global mean of ∼ 14.7 m² g⁻¹ for biomass-burning conditions are considerably higher than those observed here (Schwarz et al., 2008; Asmi et al., 2025). Although reduced coating thickness during WA1 is consistent with lower absorption enhancement, caution should be taken against interpreting WA1 as being controlled solely by a limited coating to low Eabs mechanism. For Arctic transport events, the observed Eabs likely reflects a combination of constrained atmospheric processing (limited aging and coating) and source-related differences in rBC properties. In particular, differences in rBC composition, morphology/internal structure, and particle scale mixing heterogeneity can reduce absorption efficiency and/or make core-shell Mie-based representations less effective or less representative.

In contrast, WA2 exhibited somewhat higher enhancement, with Eabs increasing to ∼ 1.1–1.5, indicating more extensive atmospheric processing and thicker coatings acquired during long-range transport. Such aging likely promoted condensation of secondary species and enhanced internal mixing, thereby increasing absorption via the lensing effect. The higher Eabs during WA2 compared with WA1 suggests that the radiative effects of rBC in the central Arctic depend not only on source type, but also strongly on the extent of atmospheric processing during transport. In this context, coating thickness (CT) serves as an important proxy for particle aging and internal mixing state, both of which directly modulate absorption enhancement. The contrast between WA1 and WA2 therefore highlights the importance of size-resolved coating information for interpreting variability in rBC optical properties across different airmass regimes.

It is worth noting that the estimated Eabs values in this study are comparable with earlier field observations, including ∼ 1.06 in California (Cappa et al., 2012), ∼ 1.06 at an east Asian outflow site Noto Peninsula (Ueda et al., 2016), ∼ 1.38 during biomass burning events in Boulder (Lack et al., 2012), 1.50 ± 0.48 in the Pearl River Delta (Wu et al., 2018), ∼ 1.36 for marine airmass periods to ∼ 1.58 for the continental airmass periods over a tropical coastal site (Nithin et al., 2026), ∼ 1.15 in Beijing (Liu et al., 2020), and ∼ 1.69 in Shanghai (Zhai et al., 2022), ∼ 1.42 Nanjing in China (Ma et al., 2020), 1.1–1.3 in a background site in the Qinghai-Tibet Plateau (Zeng et al., 2024). Larger values approaching or exceeding 2 have been observed in strongly aged or biomass-burning-influenced aerosol, such as pyrocumulonimbus plumes and remote high-altitude environments (Beeler et al., 2024; Tinorua et al., 2024). Zhang et al. (2023) also reported Eabs in the range of ∼ 1.2–2.0 with higher Eabs for fully coated BC in North China Plain. Utilizing the global measurements, Asmi et al. (2025; and references therein) reported average Eabs for the urban and remote environments as 1.38 and 1.59 respectively as well as Eabs ∼ 1.8–3.0 for the biomass burning smoke. Laboratory evidence also indicates that coatings can substantially enhance BC absorption. Shiraiwa et al. (2010) found an approximately 2-fold increase in absorption for BC coated with oleic acid and glycerol, while Khalizov et al. (2009) reported an Eabs of around 1.4 after sulfuric acid condensation on black carbon. These previous studies collectively indicate that most atmospheric Eabs values fall in the range of about 1.0–2.0 under typical ambient conditions, while higher values are generally associated with extensive aging, thicker coatings, or biomass-burning influence. It is important to note, however, that Eabs values reported in the literature are derived using different methodological approaches, including core-shell Mie theory, thermodenuder coupled with photoacoustic absorption measurements, filter-based methods, and optical approaches combining cavity ring-down spectroscopy and nephelometry. Similarly, MAC values have been derived using different combinations of absorption measurements and BC mass quantification, such as PSAP or photoacoustic absorption together with EC, SP2, SP-AMS, or COSMOS measurements. These methodological differences can contribute to inter-study variability and should be considered when comparing absolute values across regions and source regimes. Tables S1 and S2 in the Supplement providing an overview of the Eabs and MAC values and methods used in previous studies in comparison with our observations. It is important to note that the Eabs values reported here are based on a core-shell Mie theory that assumes a spherical BC core fully encapsulated by non-absorbing coating material. Ambient rBC particles, however, often exhibit fractal/irregular morphologies, partial coating, and mixing state heterogeneity. As a result, core-shell-based Eabs may represent an upper-bound or idealized estimate of absorption enhancement relative to more realistic particle representations (e.g., Adachi et al., 2010; Ueda et al., 2016; Fierce et al., 2020; Liu et al., 2020; Zhai et al., 2022; Romshoo et al., 2024). Overall, the present results indicate that most Eabs values in the central Arctic fall within the lower to moderate range reported for ambient atmospheric conditions, and that the variability between regimes is primarily controlled by the combined influence of source characteristics, atmospheric aging, removal processes and mixing state.

The size-resolved variation in Eabs, MAC, and coating thickness across different airmasses have critical implications for understanding the radiative impacts of BC in the Arctic. Highly coated BC particles can significantly increase shortwave radiation absorption, contributing to local atmospheric warming and potential feedbacks through snow and sea-ice albedo reduction. The pronounced absorption enhancement observed during WA1 suggests that continental or anthropogenically influenced airmasses, though less frequent, can be major contributors to BC radiative forcing in the Arctic MBL. Nonetheless, several limitations should be acknowledged. Mie theory, used for estimating Eabs assumes spherical core-shell morphology, which may not accurately capture the irregular or fractal shapes of ambient BC aggregates, particularly in fresh emissions. The observed heterogeneity in rBC optical properties across airmass regimes underscore the need for dynamic, region-specific parameterizations in climate models. Relying on constant enhancement factors or bulk MAC values across different transport conditions risks oversimplifying the real variability. It could lead to significant uncertainties in estimates of BC direct radiative forcing. These findings provide essential observational constraints for climate models and underscore the need to incorporate rBC mixing state and size-resolved properties into Arctic radiative effect assessments.