Chemical characterization of long-range transport biomass burning emissions to the Himalayas: insights from high-resolution aerosol mass spectrometry
- 1State Key Laboratory of Cryospheric Sciences, Northwest Institute of Eco-Environment and Resources, Chinese Academy of Sciences, Lanzhou 730000, China
- 2Key Laboratory of Arid Climatic Change and Reducing Disaster of Gansu Province, Key Laboratory of Arid Climatic Change and Disaster Reduction of CMA, Institute of Arid Meteorology, China Meteorological Administration, Lanzhou 730020, China
- 3University of Chinese Academy of Sciences, Beijing 100049, China
- 4Department of Environmental Toxicology, University of California, Davis, CA 95616, USA
Correspondence: Jianzhong Xu (email@example.com)
An intensive field measurement was conducted at a remote, background, high-altitude site (Qomolangma Station, QOMS, 4276 m a.s.l.) in the northern Himalayas, using an Aerodyne high-resolution time-of-flight aerosol mass spectrometer (HR-ToF-AMS) along with other collocated instruments. The field measurement was performed from 12 April to 12 May 2016 to chemically characterize the high time-resolved submicron particulate matter (PM1) and obtain the dynamic processes (emissions, transport, and chemical evolution) of biomass burning (BB), frequently transported from South Asia to the Himalayas during pre-monsoon season. Overall, the average (±1σ) PM1 mass concentration was 4.44 (±4.54) µg m−3 for the entire study, which is comparable with those observed at other remote sites worldwide. Organic aerosol (OA) was the dominant PM1 species (accounting for 54.3 % of total PM1 on average) followed by black carbon (BC) (25.0 %), sulfate (9.3 %), ammonium (5.8 %), nitrate (5.1 %), and chloride (0.4 %). The average size distributions of PM1 species all peaked at an overlapping accumulation mode (∼ 500 nm), suggesting that aerosol particles were internally well-mixed and aged during long-range transport. Positive matrix factorization (PMF) analysis on the high-resolution organic mass spectra identified three distinct OA factors, including a BB-related OA (BBOA, 43.7 %), a nitrogen-containing OA (NOA, 13.9 %) and a more-oxidized oxygenated OA (MO-OOA, 42.4 %). Two polluted episodes with enhanced PM1 mass loadings and elevated BBOA contributions from the west and southwest of QOMS during the study were observed. A typical BB plume was investigated in detail to illustrate the chemical evolution of aerosol characteristics under distinct air mass origins, meteorological conditions, and atmospheric oxidation processes.
The Tibetan Plateau and Himalayas (TPH), generally called the “third pole”, is the highest (average altitude of more than 4000 m a.s.l.) and largest (∼ 2 500 000 km2) plateau in the world. This region has been recognized as one of the most pristine in the world due to its high altitude, sparse population, and the minor influence of anthropogenic activities (Yao et al., 2012a). Considering the intense dynamical and thermal forcing effects in this region, the TPH not only plays a key role in the formation of Asian monsoon systems, but also impacts large-scale atmospheric circulation, the hydrological cycle, as well as global climate (Duan and Wu, 2005; Wu et al., 2007). Over the past few decades more attention has been paid to the environment and climate change in the TPH, owing to the fact that this region is very susceptible to global climate change as evidenced by rapid air temperature increases and dramatic glacier shrinkage (Xu et al., 2009; Kang et al., 2010; Yao et al., 2012b; Yang et al., 2014). The atmospheric environment in the TPH, although it is one of the most pristine regions in the world, is thought to be significantly influenced by air pollution from surrounding countries (Hou et al., 2003; Lau et al., 2008). For example, polluted air masses, particularly from South and Southeast Asia regions, have frequently been observed being transported to the Himalayas (Bonasoni et al., 2010; Cong et al., 2015), heating the aloft air masses over the TPH (Lau et al., 2006; Ramanathan and Carmichael, 2008) and declining the surface albedo after their deposition onto snow and glaciers (Xu et al., 2009). As a consequence, characterizing the aerosol physicochemical properties in the TPH, including mass loading, chemical composition, size distribution, and source, are of great importance to better understanding the aerosol chemistry, estimating the aerosol radiative forcing, and evaluating the effect of polluted air masses on the ecology and environment in the TPH region.
Numerous aerosol measurements have been conducted in the TPH region in past decades to characterize the physicochemical properties, sources, and transport pathways of ambient aerosol (Liu et al., 2008; Decesari et al., 2010; Marcq et al., 2010; Marinoni et al., 2013; Putero et al., 2014; Xu et al., 2018; R. Zhang et al., 2017). South and Southeast Asia are two major polluted regions due to their intense biomass burning (BB) activities from natural forest fires and traditional human burning activities for residential heating and cooking (Engling et al., 2011; Yadav et al., 2017). The average pollutant distribution of South and Southeast Asia during the 12 April to 12 May 2016 period can be further revealed by the distribution of average aerosol optical depth in Fig. 1. During the pre-monsoon period, atmospheric pollutants associated with BB emissions in South Asia are generally advected by regional and long-range transport (e.g., westerlies and South Asian monsoon system) to the Himalayas and build up in the southern foothills, where they are then lifted up to high altitude by the Himalayan topography and typical valley wind circulation (Zhao et al., 2013; Cong et al., 2015; Liu et al., 2017). However, the chemical properties of aerosol particles are still not well understood in the Himalayas region due to its remote and harsh environments, challenging weather conditions, and logistical difficulties. In addition, most available studies are based mainly on off-line filter sampling of ambient aerosol or snow/ice samples followed by laboratory analyses (Decesari et al., 2010; Ram et al., 2010; Li et al., 2016; Wan et al., 2017). These studies have usually had a relatively low temporal resolution (days to weeks); therefore, real-time consecutive field measurement, especially focusing on the high-resolution size-resolved chemical characteristics of aerosol particles, is of great importance and necessary to give insight into the sources and the dynamic chemical evolution of ambient aerosol.
Online real-time instrument such as the Aerodyne aerosol mass spectrometer (AMS), which can be used to characterize the chemical properties and sources of submicron aerosol particles with high time resolution and sensitivity, has been greatly developed and widely implemented worldwide (Canagaratna et al., 2007; Zhang et al., 2007a; Jimenez et al., 2009; Li et al., 2017). Although the deployments of the AMS in China started in 2006, most of the studies in China have been conducted in urban areas, including Beijing–Tianjin–Hebei (Sun et al., 2013, 2016), Yangtze River Delta (Wang et al., 2016a, b), Pearl River Delta regions (Huang et al., 2011), and Lanzhou (Xu et al., 2014, 2016; X. Zhang et al., 2017) as shown in Fig. S1 in the Supplement. However only a few studies have been deployed in remote sites thus far, such as Menyuan (Du et al., 2015), Mt. Yulong (Zheng et al., 2017), and Nam Co (Xu et al., 2018; Wang et al., 2017). In this paper, an Aerodyne high-resolution time-of-flight mass spectrometer (HR-ToF-AMS) was deployed at the Qomolangma Station for Atmospheric and Environmental Observation and Research (QOMS) on the northern slope of the Himalayas to fill the vacancy of real-time mass spectrometer measurement at high elevation sites and to evaluate the significant impacts of BBs from polluted areas in southern Asia on TPH aerosol properties during the pre-monsoon season. Here, we report an overview of the 5 min real-time chemical and physical characteristics of submicron aerosols (PM1), including mass loading, composition, size distribution, and acidity as well as temporal and diurnal variations. The sources of organic aerosols (OA) are also investigated using positive matrix factorization analysis on the high-resolution OA mass spectrum. BB influence and chemical evolution of aerosols in polluted plumes are examined by combining back trajectory analysis of air masses and fire hotspots information.
2.1 Sampling site
The QOMS (28.36∘ N, 86.95∘ E, 4276 m a.s.l.; Fig. 1), which is located on the northern slope of Mt. Everest (∼ 30 km away), was established for atmospheric and environmental observation in 2005 (Ma et al., 2008). The geomorphic and climate features around the QOMS are typically alpine, comprising cold and arid areas covered by sandy soil with sparse vegetation. The QOMS is located in a long river valley and isolated from residential areas due to its harsh environment, with a small village (with a population of ∼ 300) to the south (∼ 10 km). The closest larger settlement, Dingri County, is ∼ 100 km south from the QOMS. A freeway is located at the front of the QOMS for tourism with increased tourist during summer. The measurements were conducted from 12 April to 12 May 2016. Since this period was within the typical pre-monsoon season of the TPH, the large-scale atmospheric circulation pattern was dominated by westerly or southwesterly winds and limited precipitation. Owing to distinct thermal forcing from the southern mountains and glaciers, the QOMS was locally dominated by strongly mountain–valley circulation with down-slope wind prevailing during the daytime, especially in the afternoon (Figs. 1c and S2) (Zou et al., 2008), which made the valley an efficient channel for the downward transport of air masses from the high-altitude troposphere.
A suite of real-time instruments were collocated to measure the physiochemical properties of fine particles at the QOMS, including an Aerodyne HR-ToF-AMS (Aerodyne Research Inc., Billerica, MA, USA) for 5 min size-resolved chemical compositions (organics, sulfate, nitrate, ammonium, and chloride) of non-refractory submicron particulate matter (NR-PM1); a scanning mobility particle sizer (SMPS, model 3936, TSI Inc., Shoreview, MN, USA) for 5 min particle number concentration and size distribution between 14.6 and 661.2 nm in mobility diameter (Dm); and a photoacoustic extinctiometer (PAX, DMT Inc., Boulder, CO, USA) for particle light absorption and scattering coefficient (babs and bscat) at 405 nm and further deriving black carbon (BC) mass concentration. All instruments were placed in an air-conditioned room and the temperature was maintained at ∼ 20 ∘C. Ambient aerosol particles were introduced through a 0.5 inch copper tube which stemmed about 1.5 m out of the rooftop. A PM2.5 cyclone (model URG-2000-30EH, URG Corp., Chapel Hill, NC, USA) was used in front of the sampling inlet for removing coarse particles with size cutoffs of 2.5 µm in aerodynamic diameter (Dva). A diffusion dryer was placed behind the cyclone to dry the ambient air and eliminate the potential effect of humidity on particles. The total length of the sampling line was about 5 m and the retention time of particles was less than 2.5 s in the whole inlet. The total air flow rate from the sampling inlet was about 10 L min−1, with part of the flow shared by the HR-ToF-AMS and the SMPS while the remaining flow exhausted via an external pump. The meteorology data including wind speed (WS), wind direction (WD), relative humidity (RH), temperature (T), and solar radiation (SR) during this study were obtained from a Vantage Pro2 weather station (Davis Instruments Corp., Hayward, CA, USA). Note that all references to date and time in this study are reported in local time (LT), i.e., Beijing time (BJT: UTC+8 h).
2.3 HR-ToF-AMS operation and data analysis
2.3.1 HR-ToF-AMS operation
A detailed instrumental description of the Aerodyne HR-ToF-AMS can be found elsewhere (DeCarlo et al., 2006), therefore only a brief summary is provided here. The HR-ToF-AMS consists of three main parts: an aerosol sampling inlet, a particle sizing vacuum chamber, and a particle composition detection section (Jimenez et al., 2003). Ambient particles are sampled into the instrument through a critical orifice (130 µm in this study for enhancing the transmission efficiency at the high-altitude area) and focused into a concentrated and narrow beam through an aerodynamic lens. Particles are then accelerated into the sizing vacuum chamber and obtain different velocities for particles with different sizes due to the supersonic expansion induced by a pressure difference between the two chambers. Meanwhile, a mechanical chopper with two radial slits located 180∘ apart is used to intercept the focused particle, and then the time of flight (P-ToF) from the chopper to the vaporizer is measured to obtain the aerodynamic size of particles. After passing through the sizing chamber, particles are directed onto a resistively heated surface (∼ 600 ∘C) under a high vacuum and ionized by a 70 eV electron impact, before finally being detect by the high-resolution time-of-flight mass spectrometer. In this study, the HR-ToF-AMS was only toggled under the high sensitive V-mode (detection limits ∼ 10 ng m−3). Under V-mode operation, the instrument also switched between the mass spectrum (MS) mode and the particle P-ToF mode every 15 s, spending 6 and 9 s on each, to obtain the mass concentrations and size distributions of the non-refractory species, respectively.
The HR-ToF-AMS was calibrated for ionization efficiency (IE) and particle sizing at the beginning, in the middle, and at the end of this study according to the standard protocols (Jayne et al., 2000). Both the calibrations of IE and particle sizing were performed using mono-dispersed ammonium nitrate particles with nominal diameters of 70–300 nm. Default relative ionization efficiency (RIE) values were assumed in this study as 1.1 for nitrate, 1.3 for chloride, and 1.4 for organics. The RIE values of 3.9 and 4.2 were used for ammonium based on the results of two IE calibrations at the beginning and in the middle of this study, while RIE values of 1.6 and 1.4 were determined similarly for sulfate by using mono-dispersed ammonium sulfate particles, respectively.
2.3.2 HR-ToF-AMS data analysis
The mass concentrations and size distributions of NR-PM1 species and the ion-speciated mass spectra, composition and elemental composition of organics were determined from the HR-ToF-AMS data using the standard ToF-AMS analysis toolkit SQUIRREL (v1.56) and PIKA (v1.15c) modules written in Igor Pro (Wavemetrics Inc., Lake Oswego, OR, USA). An empirical particle collection efficiency (CE) of 0.5 was used to compensate for the incomplete transmission and detection of particles due to particle bouncing at the vaporizer and partial transmission through the aerodynamic lens, which has been widely used in field studies employing AMS with a dryer installed in front of the inlet (Xu et al., 2014, 2016). The elemental ratios of oxygen-to-carbon (O ∕ C), hydrogen-to-carbon (H ∕ C), nitrogen-to-carbon (N ∕ C), and organic mass-to-organic carbon (OM ∕ OC) for this study were determined using the “improved-ambient” method (referred as I-A method) (Canagaratna et al., 2015), which increased O ∕ C on average by 34 %, H ∕ C on average by 15 %, and OM ∕ OC on average by 17 % (Fig. S3) compared with those determined from the “Aiken ambient” method (referred as A-A method) (Aiken et al., 2008).
Positive matrix factorization (PMF) analysis using the PMF2.exe algorithm (v4.2) (Paatero and Tapper, 1994) in robust mode was conducted on the high resolution mass spectra (HRMS) to determine distinct OA components in this study. The analysis was performed using an Igor Pro-based PMF Evaluation Tool (PET, v2.03) (Ulbrich et al., 2009), downloaded from (http://cires.colorado.edu/jimenez-group/wiki/index.php/PMF-AMS_Analysis_Guide). The data and error matrices input into the PMF analysis were generated from analyzing the V-mode data via PIKA fitting. Detailed PMF analysis was thoroughly evaluated following the procedures summarized in Table 1 of Zhang et al. (2011). Isotopic ions were generally excluded and the four ions of O+, HO+, H2O+, and CO+ were down-weighted in the PMF analysis, because they were determined according to the relationship with CO signal (Ulbrich et al., 2009). The “bad” ions with S ∕ N less than 0.2 were removed from the HRMS data and error matrices before PMF analysis, and “weak” ions with S ∕ N between 0.2 and 2 were down-weighted by increasing their errors. In addition, some runs with huge mass loading spikes were also removed from the data and error matrices. The detailed matrix preparation and data pretreatment can also found in Xu et al. (2014).
A summary of key diagnostic plots of the PMF results for this study is presented in Fig. S4. Overall, the PMF solutions were investigated for one to eight factors and for the rotational parameter (fPeak) varying from −1 to 1 with a step of 0.1. Besides examining the model residuals, scaled residuals, and the Q∕Qexp contributions for each m∕z and time following procedures detailed in Table 1 of Zhang et al. (2011), the optimum solution can also be evaluated by comparing the mass spectra of individual factors with reference spectra from specific sources or other ambient AMS measurements; comparing the time series of individual factors with the known external tracers; and analyzing the diurnal variations of individual factors. Finally, the three-factor solution with fPeak = 0 was chosen in this work. The direct comparisons of the mass spectra, time series, and diurnal variations for two-factor and four-factor solutions were also shown in Figs. S5 and S6, respectively. The two-factor solution does not resolve the small, yet distinct nitrogen-containing OA, while the four-factor solution shows a splitting factor from the BB OA resolved in the three-factor solution and seems just like a simple separation of the two BB polluted episodes.
2.4 Other relevant data
The Hybrid Single Particle Lagrangian Integrated Trajectory (HYSPLIT4) model developed by the National Oceanic and Atmospheric Administration (NOAA) (Draxler and Rolph, 2003) was used to investigate the origins of air masses in this study, using the meteorological data from the NOAA Global Data Assimilation System (GDAS). The back trajectories were calculated every 6 h at an ending height of 500 m a.g.l. (above ground level) at the QOMS during the entire campaign, and then clustered according to similarity in spatial distribution. Finally, a four-cluster solution was adopted according to its small total spatial variance.
Aerosol optical depth (AOD) at 550 nm was derived from the observations made by National Aeronautics and Space Administration (NASA) Moderate Resolution Imaging Spectroradiometer (MODIS) onboard the Terra satellite. The distribution of average aerosol optical depth (AOD) in a large area (20–45∘ N, 60–110∘ E) around the TPH during the entire period of this study is given in Fig. 1d.
Various active fire hotspots were detected over South and Southeast Asia by the Fire Information for Resource Management System (FIRMS) provided by the MODIS satellite (https://firms.modaps.eosdis.nasa.gov), demonstrating the possibility that active wildfires or BBs from South and Southeast Asia may have significant impacts on the air conditions in the TPH region.
The aerosol liquid water content (ALWC) was estimated with the Extended AIM (E-AIM) Aerosol Thermodynamics Model (http://www.aim.env.uea.ac.uk/aim/aim.php). The input data included the concentrations of sulfate, nitrate, ammonium, and chloride measured by the HR-ToF-AMS as well as the relative humidity (RH) and temperature of ambient air.
3.1 Overview of the study
3.1.1 Meteorological conditions
The measurement period of our study was within the typical pre-monsoon season of the TPH. The meteorological conditions were therefore characterized by relatively cold, dry, and windy weather, and the westerlies dominated large-scale atmospheric circulation patterns with little precipitation, as displayed in Fig. 2. During the study, the averaged diurnal air temperature ranged from −2.0 to 12.5 ∘C with an average (±1σ) of 5.7 (±5.0) ∘C, and the RH ranged from 15.3 to 67.5 % with an average of 39.8 ± 18.8 %. Only two light precipitation events (1 and 0.5 mm day−1) occurred on 1 and 8 May, respectively. The WDs at QOMS were predominantly southwesterly, which were mainly associated with the thermally driven mountain–valley winds and glacier winds (Zou et al., 2008). For the diurnal variation of wind conditions, a nearly calm wind period (hourly average WS less than 2 m s−1) was observed in the early morning; after sunrise until noon, there was a weak up-slope wind period (from the north); the diurnal wind cycles were otherwise dominated by down-slope wind (from the southwest) with a maximum hourly average WS value of up to 7 m s−1 (Figs. 2b and S2).
3.1.2 Inter-comparisons between different instruments
An inter-comparison of the total PM1 (NR-PM1 + BC) mass concentrations measured by the HR-ToF-AMS (CE = 0.5) and the PAX with particle volumes (assuming spherical particles) determined from the SMPS is shown in Fig. S7. Overall, the PM1 mass is closely correlated (R2 = 0.97) with that of SMPS particle volume during the entire campaign, with a linear regression slope of 2.86. This slope is significantly higher than the estimated average PM1 density of 1.44 g cm−3, which is calculated based on the measured particle compositions in this study and the assumed particle densities of 1.2 for organics, 1.78 for (NH4)2SO4, 1.72 for NH4NO3, 1.52 for NH4Cl, and 1.8 g cm−3 for BC (Zhang et al., 2005b; Xu et al., 2016). This discrepancy is likely introduced by various factors, including different transmission sizes between HR-ToF-AMS and SMPS (up to ∼ 1.0 µm in Dva for AMS vs. limited size range of 14.6–661.2 nm in Dm for SMPS), rough calculation of PM1 density using assumed composition densities and spherical shape without considering the particle porosity, as well as the use of the empirical and constant CE value of 0.5 in this study. This phenomenon was also observed at other sites in previous studies (Ge et al., 2012; Huang et al., 2012; Xu et al., 2014; Du et al., 2015).
3.1.3 Mass concentration and chemical composition of PM1
As shown in Fig. 2, the mass concentrations of PM1 and all PM1 species, as well as their mass fractions in PM1 varied dynamically throughout this study. Two polluted periods (PP1 and PP2) were identified according to their high PM1 mass concentrations (daily average PM1 mass is larger than 5 µg m−3), high contributions from BBOA and unique back trajectories. The rest periods characterized by low PM1 mass concentrations were considered as clear periods (CP1 and CP2). The 5 min total PM1 mass concentration ranged from 0.18 to 27.97 µg m−3 for the study, with an average (±1σ) value of 4.44 ± 4.54 µg m−3. This average value was more than two times lower than most of the PM1 mass concentrations measured with Aerodyne AMS or aerosol chemical speciation monitor (ACSM) instruments at various urban, suburban, rural, or background sites in China (10.9–138.8 µg m−3) (Fig. S1); however only slightly lower than that at Mt. Yulong (5.7 µg m−3) located at the southeastern edge of the TPH, and much higher than that at Nam Co Station (2.0 µg m−3) located in the central of the TPH. Moreover, as shown in Table S1 in the Supplement, the PM1 mass concentration in this study was also lower than those measured at three remote island sites in Asia which were frequently influenced by outflow from China, Korea, and Japan (i.e., 7.9 µg m−3 for Okinawa island, 12.0 µg m−3 for Fukue island in Japan, and 10.7 µg m−3 for Jeju island in Korea) (Takami et al., 2005; Jimenez et al., 2009), as well as the PM1 mass concentration (15.1 µg m−3) obtained at the Bachelor Mountain in US which was heavily impacted by wildfire smoke plumes (Zhou et al., 2017). However, it was higher than those reported at other coastal, high elevation, forest, or remote background sites in North America and Europe (0.55–2.91 µg m−3) (Zhang et al., 2007a; Sun et al., 2009; Fröhlich et al., 2015). Although the measurements mentioned above were conducted at various sites worldwide during different seasons, these comparisons further demonstrate that QOMS is a typical high elevation, remote, background site in Asia.
Overall, organics and BC were the two dominant PM1 species ( contributing 54.3 and 25.0 % on average to the total PM1 mass, respectively) followed by sulfate (9.3 %), ammonium (5.8 %), nitrate (5.1 %), and chloride (0.4 %) (Fig. 3a). The high contributions of organics and BC at QOMS were significantly associated with the active BB emissions by long-range transport from polluted areas in South Asia. Organic compounds and BC have been revealed as two dominant components of BB aerosols and have generally been used to identify BB events in previous studies (Bond et al., 2004; Bougiatioti et al., 2014). In addition, biomass burning at high elevation regions of the Himalayas and southern Asia was more incomplete burning and had the potential to emit high amounts of BC. This conclusion can be further revealed by their enhanced mass concentrations and contributions, especially for organics, during the two distinct polluted episodes influenced by active BB plumes. Figure 3b showed the mass contributions of PM1 species as a function of total PM1 mass concentrations. The PM1 mass loadings in this study were mostly below 6 µg m−3 (accounted for ∼ 77 %); The mass contribution of organics increased significantly with the increase of total PM1 mass loading whereas the rest species showed relatively stable or decrease trends, suggesting dominant contributions of organics in the polluted episodes at QOMS.
3.1.4 Acidity and size distributions of submicron aerosols
To evaluate the bulk acidity of NR-PM1 in this study, we calculated the NH concentration (NH) based on the mass concentrations of sulfate, nitrate, and chloride measured by the HR-ToF-AMS and assumed full neutralization of these anions by ammonium (Zhang et al., 2007b). The scatter plot of the measured NH (NH) concentration vs. the NH concentration for the entire campaign was shown in Fig. S7. A tight correlation (R2 = 0.97) existed between NH and NH with a linear regression slope of 1.2, indicating that there were excesses of ammonium in the submicron particle. This slightly high NH ∕ NH ratio was quite different to results from various urban and rural sites in China, where bulk aerosols were neutralized overall or acidic due to the enriched gaseous precursors of SO2 and NOx which could be further oxidized to sulfate and nitrate (Sun et al., 2013; Xu et al., 2014; Du et al., 2015; X. Zhang et al., 2017). The excess ammonium at QOMS might relate to the important contributions of organic acids in this area (Cong et al., 2015), which could underestimate the NH due to the neglect of organic acids in the ion-balance calculation, and the non-negligible contributions of nitrogen-containing organic compounds to NH which finally overestimated the NH (Sun et al., 2009; Ge et al., 2012). As mentioned above, atmospheric aerosols in the TPH region were significantly influenced by BB emissions from South Asia during the sampling periods. BBs would emit large amounts of nitrogen-containing organic compounds (Fleming et al., 2018; Zhou et al., 2017) and as discussed in Sect. 3.2.
Figure 4 shows the average size distributions of NR-PM1 species and their mass contributions as the function of size distribution. Overall, all chemical species showed a nearly consistent but narrow accumulation mode peaking at ∼ 500 nm in Dva, indicating the well internal-mixed and aged aerosol particles at QOMS. Ultrafine particles (particles with diameter less than 100 nm) were dominated by organics (more than 70 %), while the mass contributions of chemical species at the major peak (∼ 500 nm) were organics (∼ 65 %), sulfate (∼ 13 %), nitrate (∼ 11 %), ammonium (∼ 10 %), and chloride (∼ 1 %). The contribution of organics decreased with the increase of size mode, while the contributions of three major inorganic species (sulfate, nitrate, and ammonium) slightly increased with the increasing sizes (Fig. 4b).
3.1.5 Diurnal variations of chemical species
The average diurnal cycles of meteorological parameters as well as the PM1 species and their mass fractions for the entire campaign are shown in Fig. 5. All PM1 species presented a similar diurnal pattern with lower concentrations in the daytime and higher concentrations at nighttime. The mass concentrations reached their minimum values at around 15:00. This pattern was accompanied by enhanced wind speed and increased air temperature in the afternoon, which could related to the dynamics of the planetary boundary layer (PBL). After that, the mass concentrations began to build up and reached high levels at nighttime. Note that the mass concentrations of chloride and BC also displayed a slight peak during the early morning, which corresponded with calm wind conditions and the lowest air temperature of the day; this could also be associated with the enhanced local emissions at QOMS in the morning. The diurnal cycles of mass contributions of each PM1 species were relatively stable for the entire campaign, besides the slight increase of BC from 24 % at ∼ 08:00 LT to 30 % at ∼ 10:00 LT. Overall, organics dominated PM1 throughout the day (49–57 %), followed by BC (23–30 %), sulfate (9–10 %), ammonium (5–6 %), nitrate (4–6 %), and chloride (0.3–0.8 %).
3.2 Bulk characteristics of OA
Figure 6a and b showed the average mass contributions of the four elements and the six ion categories to total organics, respectively. The organic mass was on average composed of 36.8 % carbon, 57.9 % oxygen, 4.0 % hydrogen, and 1.3 % nitrogen. For ionic categories, CxHyO ions dominated the total OA accounting for 41.3 %, followed by CxHyO (24.9 %), CxH (23.9 %), HyO (6.1 %), CxHyN (2.9 %) and CxHyOzN (0.9 %). The contributions of oxygen and the two major oxygenated ion fragments (CxHyO = CxHyO + CxHyO) at QOMS were quite a bit higher than those obtained at other urban or rural sites in China, whereas carbon and CxH ions had relative lower contributions, e.g., 38 % of CxHyO and 21 % of oxygen vs. 56 % of CxH and 70 % of carbon in urban Lanzhou (Xu et al., 2014), and 37.4 % of CxHyO vs. 51.2 % of CxH in urban Nanjing (Wang et al., 2016a), suggesting that OA at QOMS were highly aged. Correspondingly, the average high-resolution OA mass spectrum (Fig. 6c) also showed significantly high contribution (∼ 25 %) at m∕z 44 signal (one of the most reliable marker of oxygenated OA) compared with other ion fragments, e.g., 5 % at m∕z 43 (indicator for less oxidized compounds), 1.7 % at m∕z 55 (important COA fragment), and 0.4 % at m∕z 57 (tracer for traffic-related emission) (Alfarra et al., 2004; Zhang et al., 2005a). The average O ∕ C ratio was 1.07 during this study, which was much higher than those observed at various urban and rural sites in China using the I-A method, e.g., 0.37 in Beijing (Sun et al., 2016), 0.36 in Lanzhou (Xu et al., 2016), 0.35 in Nanjing (Wang et al., 2016a), and 0.65 in Ziyang (Hu et al., 2016). Moreover, the average O ∕ C ratio was even higher than that of 0.98 from the background site of Mt. Wuzhi in southern China (Zhu et al., 2016), indicating that OA at QOMS was more oxidized and aged during long-range transport. The average H ∕ C, N ∕ C and OM ∕ OC ratios were, on average, 1.29, 0.026, and 2.55 in this study, determined by a nominal chemical formula of OA as C1H1.29O1.07N0.026.
For the diurnal cycles, the O ∕ C ratio had two peaks one in the early morning and one in the late afternoon, likely related to the production of secondary organic aerosol (SOA) via aqueous-phase reactions or photochemical oxidation processes during these two periods. H ∕ C and N ∕ C ratios, however, showed inverse diurnal cycles compared with O ∕ C, peaking at around 08:00–10:00 LT in the morning. The Van Krevelen diagram (H ∕ C vs. O ∕ C), which has been widely used to probe the oxidation reaction mechanisms for bulk OA (Heald et al., 2010), showed an apparent inverse correlation (R2 = 0.57) with a slope of −0.48 at QOMS (Fig. S8). Ng et al. (2011b) have suggested that a slope of −0.5 indicates a net change in chemical composition from the addition of both acid and alcohol/peroxide functional groups without fragmentation, and/or carboxylic acid groups with fragmentation.
3.3 Organic aerosol source apportionment
Source apportionment via PMF analysis on the high-resolution OA mass spectrum identified three distinct factors in this campaign according to their unique temporary variations, mass spectrum (MS) profiles, element ratios, correlations with tracers, and diurnal patterns, i.e., a BB-related OA (BBOA), a nitrogen-containing OA (NOA) and a more-oxidized oxygenated OA (MO-OOA). Detailed discussion on each factor is given in the following subsections.
Although significant high contribution at m∕z 44 (mostly CO) was found in all of the three OA components, the BBOA MS was also characterized by contributions at m∕z 60 (mainly C2H4O) and m∕z 73 (mainly C3H5O) (Fig. 7g), which were generally regarded as well-known tracers for BB emissions (Alfarra et al., 2007). The average fraction of the signal at m∕z 60 (referred as f60) in the BBOA mass spectrum was 0.61 %, which was higher than the typical value of ∼ 0.3 % in the absence of BB impacts (Cubison et al., 2011). The time series of BBOA correlated tightly with those of C2H4O (R2 = 0.91) and C3H5O (R2 = 0.87) as well as BC (R2 = 0.72) and nitrate (R2 = 0.75) (Fig. 7a and Table S2). When the influence of high contribution at m∕z 44 was ignored, the BBOA mass spectrum in this study correlated well (R2 = 0.5–0.9) with BBOA mass spectrum identified at other sites worldwide (Ng et al., 2011a; Mohr et al., 2012; Saarikoski et al., 2012; Crippa et al., 2013, 2014; Xu et al., 2016), as shown in Fig. S9. The average mass concentration of BBOA was 1.05 µg m−3 for the entire study and contributed a large fraction (43.7 %) of the total OA mass on average (Fig. 8a), indicating that BBOA was an important component of OA during the pre-monsoon season at the QOMS. The diurnal cycle of BBOA showed high concentrations during nighttime whereas relatively low concentrations were found during daytime (Fig. 7d). Correspondingly, the mass contributions of BBOA to total OA mass decreased distinctly from ∼ 55 % at 00:00 LT to 28 % at 15:00 LT (Fig. 8b). In addition, higher mass concentrations and contributions of BBOA were found during the two polluted episodes (PP1 and PP2) than those recorded during the clear periods, further indicating the important contribution of BBOA to OA in this region. Figure 8c showed the mass fractions of the three OA components as a function of total OA mass during the entire campaign. A continuously increased trend was found for the BBOA contributions with the increasing OA mass, which contributed ∼ 15 % when the total OA mass was less than 0.3 µg m−3, whereas it reached up to more than 75 % with the OA mass increased to 9 µg m−3. This dominant contribution of BBOA during the polluted periods was consistent with results from previous studies which showed that BB emission were an important source of aerosol to the southern TPH (Engling et al., 2011; Xia et al., 2011; Putero et al., 2014; Cong et al., 2015). The O ∕ C ratio (0.85) of BBOA in this study was quite a bit higher than BBOA factors identified at other urban/rural sites in previous studies (Aiken et al., 2009; Huang et al., 2011; Mohr et al., 2012; Sun et al., 2016; Xu et al., 2016), suggesting its long-range transport feature. This aged BBOA feature was similar with those obtained at other remote sites worldwide, such as a remote forest site in Finland (Raatikainen et al., 2010), a remote background site in Greece (Bougiatioti et al., 2014), and a national air quality background sites in southern China (Zhu et al., 2016), where OA were generally highly oxidized.
Besides the two highest signals at m∕z 43.99 (CO) and 27.995 (CO+) which together contributed half of the total NOA signal due to the highly aged OA nature at QOMS, the NOA MS was also characterized by some nitrogen-containing fragments, such as m∕z 27.011 (CHN+), 41.027 (C2H3N+), and 43.006 (CHON+). In total, these three fragments were thought to comprise nearly half of the nitrogen-containing signals in the NOA factor and finally contributed 5 % of the total NOA signal. The average O ∕ C ratio of NOA for the entire campaign was 1.10 with the highest N ∕ C ratio (0.068) among the three OA components. This high N ∕ C ratio at QOMS was comparable with nitrogen-containing OA factors identified in previous studies, such as 0.06 in Mexico City (Aiken et al., 2009), 0.078 in Po Valley, Italy (Saarikoski et al., 2012), and 0.053 in New York (Sun et al., 2012). The time series of NOA showed tightly correlation (R2 = 0.62) with that of estimated organic nitrates, whereas relatively weak correlations with PM1 species and OA ions (Table S2). In addition, the f60 value (∼ 0.37 %) was also slightly higher than the background f60 (0.3 %) of BB aerosols (Fig. 7h). These results together suggested that this oxygenated OA factor was likely a nitrogen-containing OA and might be related to the aged BB emissions, consistent with results from previous studies stating that large amounts of nitrogen-containing organic compounds were found from BB aerosols (Laskin et al., 2009; Gautam et al., 2016; Wang et al., 2017). Recently, Fleming et al. (2018) found dung burning, a very popular activity in Himalayas and India for residential cooking and heating, could emit much more nitrogen-containing OA than wood burning. Our filter samples during high BBOA period analyzed by Fourier Transform Ion Cyclotron Resonance Mass Spectrometry (FTICR-MS) also found amount of ON molecular (in preparation). As shown in Figs. 7e and 8b, both the diurnal cycles of mass concentrations and fractions of NOA displayed a distinct increase in the morning, similar to the diurnal patterns of chloride, element ratios of H ∕ C and N ∕ C, and the estimated organic nitrates. This diurnal feature of NOA at QOMS was quite consistent with NOA factors identified in Po Valley, Italy (Saarikoski et al., 2012) and in Mexico City (Aiken et al., 2009), or less-oxidized oxygenated OA (LO-OOA) in the southeastern USA (Xu et al., 2015) where have active BB emissions. NOA contributed ∼ 14 % of the total OA mass on average, with an average mass concentration of 0.34 µg m−3 for the entire study (Fig. 8a).
An obvious more oxygenated OA factor was also identified in this study according to its significant high signal at m∕z 44 (∼ 25 %) and the high average O ∕ C ratio of 1.34 (Fig. 7i). The time series of MO-OOA correlated closely (R2 = 0.7) with sulfate and nitrate (Fig. 7c and Table S2). Moreover, the mass spectrum of MO-OOA in this study tightly resembled more aged and low-volatility oxygenated OA (LV-OOA) observed using AMS instruments at various sites worldwide (Fig. S9), e.g., an R2 of 0.89 and 0.97 to those in Lanzhou, China (Xu et al., 2014; X. Zhang et al., 2017), 0.96 to that in Paris, France (Crippa et al., 2013), 0.95 to that in Barcelona, Spain (Mohr et al., 2012), in addition to 0.70 and 0.71 to the standard LV-OOA mass spectrums obtained from abundant AMS data sets by Ng et al. (2011a) and Crippa et al. (2014). The diurnal variation of MO-OOA was mainly driven by the dynamics of the PBL height, with high concentrations during the nighttime yet relatively low concentrations during daytime (Fig. 7f). This pattern was quite different to those observed in previous studies in that LV-OOA generally showed elevated concentrations during the afternoon in accordance with strong photochemical activities, suggesting that SOA at QOMS were mainly oxidized and aged during long-range transport. On average, MO-OOA contributed 42.4 % of the total OA mass, with an average mass concentration of 1.02 µg m−3 for the entire study (Fig. 8a). As shown in Figs. 2f and 8c, MO-OOA also displayed enhanced mass contributions during the clear periods, especially for the period after 2 May when the average mass fraction of MO-OOA increased to ∼ 68 % of the total OA mass.
3.4 Impact of BB emissions on aerosol characteristics
3.4.1 Sources of BB aerosols
In order to understand the transport pathways and the potential source areas of aerosol, three-day back trajectories of air mass were calculated at an ending height of 500 m a.g.l. every 6 h at the QOMS from 12 April to 12 May 2016. A four-cluster solution and the wildfire hotspots around the QOMS during the entire measurement period are presented in Fig. 9. Cluster 1 and 2 (C1 and C2), which originated from the west of the QOMS and passed over many hotspot areas (e.g., Indo-Gangetic Plain and Nepal), represented two polluted clusters. On the contrary, C3 and C4, which accounted for half of the total back trajectories, were identified as clear clusters. C3 traveled a short distance from the southwest of the QOMS, whereas C4 was from the north of the QOMS and passed over the inland of the TPH. The average PM1 mass concentrations for C1 and C2 were 5.17 and 6.61 µg m−3, respectively, which were two to three times higher than those for the two clear clusters (2.74 and 2.21 µg m−3). The mass contributions of OA and BBOA during C1 and C2 were up to more than 55 and 25 % of the total PM1 mass on average, whereas weak contributions were found for the clear clusters (C3 and C4), indicating the significant impacts of BB emissions from South Asia on aerosol loadings at QOMS.
3.4.2 Comparison of aerosol characteristics and air mass origins during different episodes
As shown in Fig. 2, the mass concentrations and compositions of PM1 varied dynamically during the entire sampling period. Two polluted periods (PP1 and PP2) and two clear periods (CP1 and CP2) were identified. The comparisons of average mass concentrations and other indicators for the four different episodes were presented in box plots in Fig. 10, whereas the corresponding back trajectories of air masses and MODIS fire hotspots belong to each episode period were given in Fig. 11, respectively.
During the two polluted periods, PM1 mass concentrations were much higher than those in clear periods (8.06 and 7.87 µg m−3 for PP1 and PP2 vs. 2.76 and 1.82 µg m−3 for CP1 and CP2; similarly hereinafter), with higher contributions from OA (60.1 and 57.5 % vs. 48.1 and 43.9 %) and BBOA (38.3 and 36.6 % vs. 14.3 and 7.5 %) (Figs. 10 and 11). In addition, f60 were also higher during polluted periods than those for clear periods (0.34 and 0.34 % vs. 0.26 and 0.22 % on average) (Fig. 10). Air masses during PP1 and PP2 generally originated from long-range transport to the west of the QOMS, which would pass through intense wildfires areas in South Asia (e.g., Indo-Gangetic Plain and Nepal where high AOD values are shown in Fig. 1d and active fire hotspots are displayed in Figs. 9 and 11). The number of fire hotspots around the air mass trajectories during PP2 was more than three times higher than during other periods. Although the hotspot number around the air mass trajectories during PP1 was not as abundant as that during PP2 and even slightly lower than that during CP1, it was only collected within three days for PP1 whereas 8–10 days for the other periods. Hence, the BB activities were also more frequent and intense during the short PP1 and finally resulted in the highest average PM1 mass concentration among these periods. Back trajectories in CP1 also originated from the west of QOMS and passed over northern India and Nepal; however, both the intensity of the number of fire hotspots (1089 hotspots in ∼ eight days) and average FRP (19.6) were obvious lower than that in PP2. CP2 was the most clear period, during which the average PM1 mass concentration was more than four times lower than those in polluted periods. Back trajectories during CP2 period were from either the north of QOMS which passed over inland areas of the TPH or the south of QOMS with quite short distances and low WSs. These results together suggested the significant roles of air mass sources and BB emissions to aerosol characteristics at QOMS.
3.4.3 Case study on the chemical evolution of BB emission aerosols
In order to examine how atmospheric aging affects the aerosol chemistry characteristics at QOMS, the typical evolution process of a BB aerosol plume (referred as BB evolution case) was analyzed from 30 April at 15:00 LT when a fresh BB plume occurred to 1 May at 18:00 LT when the BB plume was highly aged after undergoing various atmospheric oxidation processes. The temporal variations of meteorological parameters, mass concentrations, and mass contributions of each PM1 species and OA components as well as other chemistry parameters before and during this BB evolution case were all shown in Fig. 12.
Before the BB evolution case, all the mass concentrations decreased slowly and synchronously from 00:00 to 10:00 LT on 30 April. This was consistent with the nearly stable trends of mass contributions and other chemistry parameters, indicating the relatively unified air mass sources and stable atmospheric conditions. After that, the wind circulation changed from thermally-driven down-slope winds (mostly southwest) to weak up-slope winds (northeast). In this period, BBOA and f60 values kept relatively stable in contrast to other species likely due to the weakness of air dilution and local sources. All the species reached their minimum at around 15:00 LT due to the lift of PBL.
The BB evolution case in this study was further divided into three different situations (as marked with arrows in Figs. 12 and 13), including the arrival of the fresh BBOA plume (from 15:00 to 24:00 LT on 30 April), followed by aqueous-phase oxidation at nighttime (from 02:30 to 07:10 LT on 1 May), and photochemical oxidation during the daytime (from 10:00 to 18:00 LT on 1 May). All the mass concentrations began to increase from 15:00 LT and finally reached maximum PM1 mass loading of 18.4 µg m−3 at 24:00 LT, which was about four times higher than the average PM1 mass during the entire campaign. Thus continuous increase was mainly dominated by the dramatic increase of BBOA, which reached up to 10.8 µg m−3 and contributed 88 % of the total OA mass and 50 % of the total PM1 at 24:00 LT (Fig. 13a), suggesting a distinct presence of BB emissions during this period. In contrast, the total OA mass was comprised of 78 % of MO-OOA and 12 % of BBOA at 15:00 LT. Similar continuous increasing trends could also be found for the mass concentration of calculated organic nitrate in this stage. In addition, nine aerosol chemistry parameters were presented as a function of BBOA mass concentrations during this period (Fig. 13b). The mass contributions of OA to PM1 (fOrg) and BBOA to total OA (fBBOA), f60, and H ∕ C ratio were all increased with the increasing BBOA mass, whereas the mass contribution of MO-OOA to total OA (fMO−OOA), O ∕ C ratio, carbon oxidation state (OSc = 2 × O ∕ C − H ∕ C) of OA, and aerosol single scattering albedo (SSA) were decreased, obviously indicating the fresh nature of this BB plume. The significant impacts of the fresh BB plume during this period were mainly associated with the unique wind circulation and the long-range transport of air masses. As displayed in Fig. 12b, the wind circulation changed from the weak up-slope winds to the strong down-slope glacier winds on 30 April at 15:00 LT, with a WS increase from ∼ 2 to 8 m s−1. Meanwhile, the back trajectories during this period also showed that the air masses passed over northern India and Nepal, where active wildfires occurred. The air masses then accumulated and uplifted to the Himalayas and finally moved downward to the QOMS with the strong glacier winds.
A distinct aqueous-phase oxidation process was found in the nighttime from 02:30 to 07:10 LT on 1 May. Although the total PM1 and its species showed nearly stable mass concentrations during this period, the BBOA mass decreased gradually (from 82 to 70 %) whereas MO-OOA increased constantly (from 14 to 20 %) with the significant increase of RH (up to 91 }) and aerosol liquid water content (ALWC) (Fig. 12). The scatter plots of the aerosol chemistry parameters vs. the logarithmic values of cumulative ALWC, which could be used for the aqueous-phase oxidation during transport, also showed apparent increase trends for fMO−OOA, O ∕ C ratio, OSc, and SSA that generally indicated the aerosol aging extent. All of these together suggested a distinct aqueous-phase oxidation of BBOA in the nighttime.
From sunrise, all mass concentrations decreased gradually, which was mainly related to the increasing PBL height and clear air mass dilution. The back trajectories indicated that air masses during this period firstly moved inland north of QOMS where rare wildfires took place. Moreover, the BB plume further underwent strong photochemical oxidation during the daytime due to the strong solar radiation. MO-OOA only contributed 26 % of the total OA mass at 10:00 LT, but it could increase to 74 % at 18:00 LT after long-time photochemical oxidation. In contrast, BBOA mass contribution decreased from 49 to 20 %. The cumulative solar radiation, which denoted the total amount of solar radiation that the plumes were exposed to during transport, could be used as an indicator of the extent of photochemical aging in the daytime (Zhou et al., 2017). Clear increasing trends were found for fMO−OOA, O ∕ C ratio, OSc, and SSA values with increasing cumulative solar radiation, whereas decreasing trends in fBBOA, fNOA, H ∕ C ratio, and f60 values were observed, suggesting a possible oxidation mechanism that oxidized the relatively fresh BBOA and NOA to aged MO-OOA during the daytime. Another interesting phenomenon was the continuous increase of SSA during both the aqueous-phase and photochemical oxidation periods on 1 May (Figs. 12e and 13b), indicating the potential influence of atmospheric aging to aerosol optical property at QOMS.
A comprehensive characterization of submicron aerosol chemical compositions and sources was investigated at the QOMS during the pre-monsoon season in 2016. The average mass concentration of PM1 (NR-PM1 + BC) was 4.44 (±4.54) µg m−3 for the entire study, which was much lower than those observed in various sites in China. OA was the dominant PM1 species (accounted for 54.3 % of the total mass on average) and its contributions increased with the increase PM1 mass loading. The average size distributions of all PM1 species displayed an overlapping and narrow accumulation mode at ∼ 500 nm, indicating internally well-mixed and aged aerosol particles at the QOMS. All species presented similar diurnal cycles, with lower concentrations in the daytime and higher concentrations at nighttime, mainly attributed to the dynamic variations of PBL height. Three OA factors were identified by PMF analysis on the high-resolution OA mass spectrum, including a relatively fresh BB-related OA (BBOA), a nitrogen-containing OA (NOA) and a more-oxidized oxygenated OA (MO-OOA). BBOA and MO-OOA could respectively account for 43.7 and 42.4 % of OA mass on average; however, their contributions to OA showed completely opposite trends with the increase of OA mass. A continuously increasing trend could be found for BBOA with increasing OA, suggesting the key role of BBOA during polluted periods when frequent and intense wildfires were observed in South Asia. The significant impact of BB emissions on aerosol characteristics at QOMS have also been illustrated for different air mass origins and periods. Elevated PM1 mass concentrations and high contributions of BBOA were found for both polluted clusters and polluted periods. A case study of typical evolution process of BB aerosol plume was investigated in detail to illustrate the chemical evolution of aerosol characteristics at the QOMS. The fresh BB plume occurred in the afternoon on 30 April and finally resulted in highly PM1 mass loading of 18.4 µg m−3, which was about four times higher than the average PM1 mass during the entire campaign. Obvious aqueous-phase oxidation and photochemical oxidation processes were analyzed during nighttime and daytime on 1 May, both suggesting the mechanism that oxidized fresh BBOA to aged MO-OOA. The continuous increase of SSA during the two oxidation periods suggested the potential influence of atmospheric aging on aerosol optical property at QOMS.
The processed AMS data and meteorological data in this study are available upon request from the corresponding author.
The supplement related to this article is available online at: https://doi.org/10.5194/acp-18-4617-2018-supplement.
The authors declare that they have no conflict of interest.
This article is part of the special issue “Pan-Eurasian Experiment (PEEX)”. It does not belong to a conference.
This research was supported by grants from the National Natural Science
Foundation of China (41771079, 41421061), the Key Laboratory of Cryospheric
Sciences Scientific Research Foundation (SKLCS-ZZ-2017-01), and the Chinese
Academy of Sciences Hundred Talents Program. The authors thank their
colleagues for continuing support and discussion, and thank the NOAA Air
Resources Laboratory, NASA MODIS, and FIRMS teams for providing the HYSPLIT
trajectory model, AOD, and fire hotspots datasets.
Edited by: Veli-Matti Kerminen
Reviewed by: three anonymous referees
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