Sources and characteristics of size-resolved particulate organic acids and methanesulfonate in a coastal megacity: Manila, Philippines
- 1Department of Chemical and Environmental Engineering, University of Arizona, Tucson, Arizona 85721, USA
- 2Manila Observatory, Quezon City, 1108, Philippines
- 3Institute of Environmental Science and Meteorology, University of the Philippines, Diliman, Quezon City, 1101, Philippines
- 4Department of Physics, School of Science and Engineering, Ateneo de Manila University, Quezon City, 1108, Philippines
- 5Department of Hydrology and Atmospheric Sciences, University of Arizona, Tucson, Arizona 85721, USA
- 6Philippine Nuclear Research Institute – Department of Science and Technology, Commonwealth Avenue, Diliman, Quezon City, 1101, Philippines
Correspondence: Connor Stahl (firstname.lastname@example.org)
A 16-month (July 2018–October 2019) dataset of size-resolved aerosol composition is used to examine the sources and characteristics of five organic acids (oxalate, succinate, adipate, maleate, phthalate) and methanesulfonate (MSA) in Metro Manila, Philippines. As one of the most polluted megacities globally, Metro Manila offers a view of how diverse sources and meteorology impact the relative amounts and size distributions of these species. A total of 66 sample sets were collected with a Micro-Orifice Uniform Deposit Impactor (MOUDI), of which 54 sets were analyzed for composition. Organic acids and MSA surprisingly were less abundant than in other global regions that are also densely populated. The combined species accounted for an average of 0.80 ± 0.66 % of total gravimetric mass between 0.056 and 18 µm, still leaving 33.74 % of mass unaccounted for after considering black carbon and water-soluble ions and elements. The unresolved mass is suggested to consist of non-water-soluble metals as well as both water-soluble and non-water-soluble organics. Oxalate was approximately an order of magnitude more abundant than the other five species (149 ± 94 ng m−3 versus others being < 10 ng m−3) across the 0.056–18 µm size range. Both positive matrix factorization (PMF) and correlation analysis are conducted with tracer species to investigate the possible sources of organic acids and MSA. Enhanced biomass burning influence in the 2018 southwest monsoon resulted in especially high levels of submicrometer succinate, MSA, oxalate, and phthalate. Peculiarly, MSA had negligible contributions from marine sources but instead was linked to biomass burning and combustion. Enhanced precipitation during the two monsoon seasons (8 June–4 October 2018 and 14 June–7 October 2019) coincided with a stronger influence from local emissions rather than long-range transport, leading to notable concentration enhancements in both the sub- and supermicrometer ranges for some species (e.g., maleate and phthalate). While secondary formation via gas-to-particle conversion is consistent with submicrometer peaks for the organic acids and MSA, several species (i.e., phthalate, adipate, succinate, oxalate) exhibited a prominent peak in the coarse mode, largely owing to their association with crustal emissions (i.e., more alkaline aerosol type) rather than sea salt. Oxalate's strong association with sulfate in the submicrometer mode supports an aqueous-phase formation pathway for the study region. However, high concentrations during periods of low rain and high solar radiation suggest photo-oxidation is an important formation pathway.
Organic acids are ubiquitous components of ambient particulate matter and can contribute appreciably to total mass concentrations in diverse regions ranging from the Arctic to deserts (e.g., Barbaro et al., 2017; Gao et al., 2003; Kawamura et al., 2005). Furthermore, another class of species contributing to ambient aerosol mass is organosulfur compounds, with methanesulfonate (MSA) being an example species (Bardouki et al., 2003b; Ding et al., 2017; Falkovich et al., 2005; Kerminen et al., 1999; Maudlin et al., 2015; Ziemba et al., 2011). The spatiotemporal and size-resolved mass concentration profiles of organic and sulfonic acids are difficult to characterize and can significantly vary depending on the time of day, season, region, and meteorological profile (Adam et al., 2020; Bagtasa et al., 2019; Kobayashi et al., 2004; Maudlin et al., 2015; Mochida et al., 2003; Reid et al., 2013). It is necessary to quantify their relative abundances and to understand factors affecting their production and eventual removal to be able to quantify their influence on aerosol hygroscopic and optical properties (Beaver et al., 2008; Cai et al., 2017; Freedman et al., 2009; Marsh et al., 2017, 2019; Myhre and Nielsen, 2004; Peng et al., 2016; Xue et al., 2009). Low-molecular-weight organic acids are water-soluble and can range widely in hygroscopicity when in their pure salt form depending on factors such as carbon number (Prenni et al., 2001; Saxena and Hildemann, 1996; Sorooshian et al., 2008) and interactions with other components in multicomponent aerosol particles (Drozd et al., 2014).
Organic acids are generally believed to effectively scatter light and have a cooling effect on climate (McGinty et al., 2009; Myhre and Nielsen, 2004), although their overall impact on properties such as refractive index in multicomponent aerosols is poorly characterized. Refractive indices for species investigated in this work range widely from 1.43 (MSA) to 1.62 (phthalic acid). MSA is assumed to be purely scattering, similar to sulfate (Hodshire et al., 2019), and to have hygroscopic properties close to those of ammonium sulfate (Asmi et al., 2010; Fossum et al., 2018). However, its hygroscopic and optical behavior is not fully understood and is still an active area of research (Liu et al., 2011; Peng and Chan, 2001; Tang et al., 2019, 2015; Zeng et al., 2014).
Decades of research into atmospheric organic acids and MSA have yielded rich insights into their sources, production mechanisms, and fate in the atmosphere (Baboukas et al., 2000; Bardouki et al., 2003a; Gondwe et al., 2004; Kawamura and Bikkina, 2016; Limbeck et al., 2001; Norton et al., 1983; Ovadnevaite et al., 2014; Sorooshian et al., 2009; van Pinxteren et al., 2015). MSA is produced predominantly from the oxidation of dimethylsulfide (DMS) emitted from oceans (Bates et al., 2004; Davis et al., 1998; Kerminen et al., 2017), but it also can be linked to biomass burning, urban, and agricultural emissions (Sorooshian et al., 2015). Sources of organic acids include primary emissions from biomass burning, biogenic activity, and the combustion of fossil fuels (Kawamura and Kaplan, 1987) and secondary formation via gas-to-particle conversion processes stemming from both biogenic (Carlton et al., 2006) and anthropogenic emissions (Sorooshian et al., 2007b). Secondary processing can include both aqueous-phase chemistry in clouds (Blando and Turpin, 2000; Ervens, 2018; Ervens et al., 2014; Hoffmann et al., 2019; Rose et al., 2018; Sareen et al., 2016; Warneck, 2005) and photo-oxidation of volatile organic compounds (VOCs) in cloud-free air (Andreae and Crutzen, 1997; Gelencsér and Varga, 2005). These various sources and production pathways result in mono- and dicarboxylic acids being prevalent across a range of aerosol sizes (Bardouki et al., 2003b; Kavouras and Stephanou, 2002; Neusüss et al., 2000; Yao et al., 2002). Little is reported in terms of the size-resolved nature of organic acids and MSA over long periods (> 6 months) of time with high sampling frequency (weekly or better). Although insights have already been gathered from size-resolved measurement studies (Table S1), most measurement reports are based on bulk mass concentration measurements (Chebbi and Carlier, 1996; Kawamura and Bikkina, 2016). Studying the seasonal variations of size-resolved organic acid and MSA aerosols could prove vital in improved understanding of their formation and removal mechanisms and associated sensitivity to seasonally dependent sources and meteorological factors.
The Philippines is an important region to study aerosols due to the wide range of both meteorological conditions and diverse local and regional emissions sources (Alas et al., 2018; Bagtasa and Yuan, 2020; Braun et al., 2020; Hilario et al., 2020a; Kecorius et al., 2017). In addition to aerosol sources from nearby regions (Hilario et al., 2020b), the Philippines also has a significant source of local pollution, largely consisting of vehicular emissions due to high population density (Madueño et al., 2019), the use of outdated vehicles (Biona et al., 2017), ship exhaust from high-density shipping lanes (Streets et al., 1997, 2000), and more lenient air regulations leading to significant air pollution due to rapid growth and urbanization (Alas et al., 2018; Kecorius et al., 2017). This leads to Metro Manila containing some of the highest black carbon (BC) concentrations in Southeast Asia and quite possibly the world (Alas et al., 2018; Hopke et al., 2011; Kecorius et al., 2017; Kim Oanh et al., 2006). Past aerosol characterization work for that region has focused mainly on gravimetric analysis of total bulk mass (e.g., PM2.5, PM10) (Bagtasa et al., 2018, 2019; Cohen et al., 2009; Kim Oanh et al., 2006), water-soluble inorganic and organic ion speciation (AzadiAghdam et al., 2019; Braun et al., 2020; Cruz et al., 2019; Kim Oanh et al., 2006; Simpas et al., 2014; Stahl et al., 2020a), and BC analysis (Alas et al., 2018; Bautista et al., 2014; Kecorius et al., 2017; Takahashi et al., 2014). In an analysis of two size-resolved aerosol sets in Manila, a significant portion of the total mass unaccounted for by the water-soluble inorganic, water-soluble organic, and BC components was attributed to (but not limited to) organics and non-water-soluble metals (Cruz et al., 2019). However, a concentrated effort to characterize the contributions of the water-soluble organic acids to the total aerosol mass in Manila over the course of a full year has not been undertaken.
The aim of this study is to use a 16-month-long dataset of size-resolved composition in Quezon City in Metro Manila to address the following questions: (i) how much do organic acids and MSA contribute to the region's aerosol mass concentrations? (ii) What are the seasonal differences in the mass size distribution profile of organic acids and MSA, and what drives the changes? (iii) What are the sources and predominant formation mechanisms of these species in the sub- and supermicrometer diameter ranges? The results of this study are put in broad context by comparing findings to those in other regions.
2.1 Study site description
Metro Manila is comprised of 16 cities and a municipality totaling a population of about 12.9 million people and a collective population density of 20 800 km−2 (Alas et al., 2018; PSA, 2016). Quezon City is the most populated city in Metro Manila containing 2.94 million people with a population density of 18 000 km−2 (PSA, 2016), which is among the highest in the world. Because of these reasons, Metro Manila is a fitting location for examining locally produced anthropogenic aerosols superimposed on a variety of other marine and continentally influenced air masses transported from upwind regions (Kim Oanh et al., 2006).
Measurements were conducted over a 16-month period between July 2018 and October 2019 at Manila Observatory (MO; 14.64∘ N, 121.08∘ E) on the third floor (∼ 85 m a.s.l.) of an office building, which is on the Ateneo de Manila University campus in Quezon City, Philippines (Fig. 1). Sampling was conducted approximately 100 m away from the nearest road on campus, and therefore campus emissions do not impact sampling to a large degree, qualifying the monitoring site as an urban mixed background site (Hilario et al., 2020a) capturing local, regional, and long-range-transported emissions. The following four seasons were the focus of the sampling period: the 2018 southwest monsoon (SWM18, 8 June–4 October 2018) (PAGASA, 2018a, b), a transitional period (5–25 October 2018), the northeast monsoon (NEM, 26 October 2018–13 June 2019) (PAGASA, 2018c), and the 2019 southwest monsoon (SWM19, 14 June–7 October 2019) (PAGASA, 2019a, b). These seasons have also been defined in other works (i.e., Akasaka et al., 2007; Cruz et al., 2013; Matsumoto et al., 2020) and can predominately be separated into two general seasons, wet (SWM) and dry (NEM). Generally, there is a second transitional period in May that transitions between the NEM and SWM (Bagtasa and Yuan, 2020); however, recent studies suggest that the transition is abrupt (Matsumoto et al., 2020). Consequently, the second transitional period was combined with the NEM season.
2.2 Instrument description
Ambient aerosol was collected with a Micro-Orifice Uniform Deposit Impactor II (MOUDI II 120R, MSP Corporation; Marple et al. 2014) using Teflon substrates (PTFE membrane, 2 µm pores, 46.2 mm diameter, Whatman). The MOUDI-II is a 10-stage impactor with aerodynamic cutpoint diameters (Dp) of 10, 5.6, 3.2, 1.8, 1.0, 0.56, 0.32, 0.18, 0.10, and 0.056 µm, with a nominal flow rate of ∼ 30 L min−1. A total of 66 MOUDI sets were collected on a weekly basis, usually over a 48 h period; however, only 54 sets were analyzed for ions, and 47 of those sets were also analyzed for elements. A 48 h period was chosen because it offered an optimal compromise between gathering samples with fine temporal resolution and samples with a sufficiently large chemical signal to exceed analytical limits of detection. Details of the sample sets are shown in Table S2 and can be found in more detail in Stahl et al. (2020a), but a brief summary of the storage and extraction methods will be described here. Substrates were stored in a freezer at −20∘ C after samples were collected from the MOUDI until extractions could be carried out, which on average was approximately 2 weeks. The stored substrates were then extracted by sonication in Milli-Q water (18.2 MΩ cm) for 30 min. After sonication, solutions were immediately analyzed to prevent degradation, while the remaining extracts were stored in a refrigerator for additional analyses. There have been studies that discuss the effects of sonication oxidation degrading organic species (i.e., Miljevic et al., 2014). It was determined through experimental tests that no significant degradation occurred during the sonication process for the species being analyzed in this study.
Water-soluble organic acids, MSA, and inorganic ions were speciated and quantified using ion chromatography (IC; Thermo Scientific Dionex ICS-2100 system), with a flow rate of 0.4 mL min−1. The anionic species of relevance to this study were MSA, chloride (Cl−), nitrate (NO), sulfate (SO), adipate, succinate, maleate, oxalate, and phthalate. These anions were resolved using potassium hydroxide (KOH) eluent, an AS11-HC 250 mm column, and an AERS 500e suppressor. The cationic species of relevance to this study was sodium (Na+), which was detected using methanesulfonic acid eluent, a CS12A 250 mm column, and a CERS 500e suppressor. The IC instrument methods for anion and cation analysis can be found in Stahl et al. (2020a). Water-soluble elements were measured using a triple quadrupole inductively coupled plasma mass spectrometer (ICP-QQQ; Agilent 8800 Series). The quantified elements of relevance to this study include Al, As, Cd, K, Ni, Pb, Rb, Ti, and V. Limits of detection (LOD) and recoveries were calculated for all ionic and elemental species and are provided in Table S3. Aside from the species that are the focus of this study (organic acids and MSA), the other elements and ions were included as they are useful tracers for different aerosol sources to aid in source apportionment. Although pyruvate was speciated with IC, it is not considered with the other organic acids because it was below the LOD for 48 of the 54 sets. It should also be noted that only a subset of species used for analyses was listed here. The full suite of species can be seen in Stahl et al. (2020a).
A total of 11 of the 66 MOUDI sets included simultaneously operated MOUDI instruments next to each other to complement the chemical speciation analysis with gravimetric analysis. A Sartorius ME5-F microbalance (sensitivity of ±1 µg) was used in an air-buffered room with controlled temperature (20–23 ∘C) and relative humidity (RH: 30 %–40 %). Each substrate was passed near an antistatic tip for approximately 30 s to minimize bias due to electrostatic charge. Multiple weight measurements were conducted before and after sampling, with the difference between weighings being less than 10 µg for each condition, respectively. The difference between substrate weights before and after sampling was equated to total gravimetric mass.
Black carbon was measured using a Multi-wavelength Absorption Black Carbon Instrument (MABI; Australian Nuclear Science and Technology Organisation). The MABI optically quantifies black carbon concentrations by detecting the absorption at seven wavelengths (405, 465, 525, 639, 870, 940, and 1050 nm); however, the wavelength at 870 nm is used here as black carbon is the primary absorber at that wavelength (Cruz et al., 2019; Ramachandran and Rajesh, 2007; Ran et al., 2016).
Meteorological parameters were measured at MO during the study period using a Davis Vantage Pro2™ Plus automatic weather station, which was located on the roof. Measured parameters of relevance included temperature, accumulated rain, RH, and solar radiation. Data were collected in 5 min increments and were cleaned based on the method of Bañares et al. (2018) to verify values were in acceptable ranges. The meteorological parameters, except for rain, were averaged over each sampling period, while rain was summed over time to obtain the accumulated precipitation for a sampling period. There were two periods during which the automatic weather station located at MO had missing values, 6 November–27 November 2018 and 7 August–3 September 2019. In these cases, missing values were substituted with values from a secondary automatic weather station located approximately 2 km away (14.63∘ N, 121.06∘ E), and if missing data still persisted, a tertiary station located 5 km away (14.67∘ N, 121.11∘ E) was used. Identical data cleaning procedures were implemented for the secondary and tertiary sites.
2.3 Concentration weighted trajectories (CWTs)
A CWT analysis was conducted to identify sources of detected species. The method assigns a weighted concentration to a grid that is calculated by finding the mean of sample concentrations that have trajectories crossing a particular cell in the grid (e.g., Dimitriou, 2015; Dimitriou et al., 2015; Hilario et al., 2020a; Hsu et al., 2003). The software TrajStat (Wang et al., 2009) determines CWT profiles by using back-trajectories from the NOAA Hybrid Single-Particle Lagrangian Integrated Trajectory (HYSPLIT) model (Rolph et al., 2017; Stein et al., 2015). Using the Global Data Assimilation System (GDAS) and the model vertical velocity method, 3 d back-trajectories were obtained with an ending altitude of 500 m a.g.l.. The choice of 500 m is based on representativeness of the mixed layer and it having been widely used in other studies (e.g., Crosbie et al., 2014; Mora et al., 2017; Sorooshian et al., 2011). Trajectories were obtained every 6 h after MOUDI sampling began for each sample set, yielding approximately nine trajectories per set. A grid domain of 95 to 150∘ E longitude and −5 to 45∘ N latitude was used, with a grid cell resolution of . The analysis was performed for each measured organic acid and MSA for the full diameter range of MOUDI sets (0.056–18 µm). A weighting function was applied to the CWT plots to minimize uncertainty.
2.4 Positive matrix factorization (PMF)
PMF analysis was applied to identify sources and their relative importance for the mass concentration budgets of the species discussed in this work (Paatero and Tapper, 1994). Model simulations were conducted based on MOUDI data for the diameter range of 0.056–18 µm. A total of 19 species (Al, Ti, K, Rb, V, Ni, As, Cd, Pb, Na+, Cl−, NO, SO, MSA, adipate, succinate, maleate, oxalate, and phthalate) were included in the analysis and categorized as “strong”. Each individual stage of MOUDI sets was considered an independent variable for the analysis. Missing values or values below the detection limit were replaced with zeros, with the exception of sets for which ICP-QQQ analysis was not performed (57, 59, 60, 61, 62, 64, 65). These missing values were replaced with the geometric mean for each respective stage. The uncertainty for each stage and species was calculated as follows:
where [x] is the concentration of the species (Reff et al., 2007). No additional uncertainty was added to account for any unconsidered errors for all species. The uncertainty of the model output was evaluated using displacement (DISP), bootstrapping (BS), and bootstrapping with displacement (BS-DISP). For BS, 100 resamples were used, and a value of 0.6 was used as a threshold for the correlation coefficient (r) to pass as successful mapping for each simulation.
To qualify as a valid result, reported PMF results had to meet the following criteria: (i) factors are mapped with BS runs, (ii) there are no factor swaps in DISP, (iii) displacements from its fitted values (dQ) are close or equal to 0 %, and (iv) there are no factor swaps in BS-DISP, where Al, Ti, K, Rb, V, Ni, As, Cd, Pb, Na+, Cl−, NO, and SO were displaced. PMF diagnostics can be seen in Table S4 based on the method of Brown et al. (2015).
A brief overview of the species being examined is first provided before reviewing concentration statistics. MSA is an oxidation product of dimethylsulfide (DMS) emitted primarily from the ocean (Berresheim, 1987; Saltzman et al., 1983), but it can also be formed from dimethyl sulfoxide (DMSO) emitted from anthropogenic sources such as industrial waste (Yuan et al., 2004). Gaseous MSA can become associated with particulate matter via new particle formation (Dawson et al., 2012) and through heterogeneous reactions or condensation onto existing particles (De Bruyn et al., 1994; Hanson, 2005).
Of the three saturated dicarboxylic acids, succinate (C4) and adipate (C6) are larger chain dicarboxylic acids linked to ozonolysis of cyclic alkenes, which is common in areas with extensive vehicular emissions (Grosjean et al., 1978; Hatakeyama et al., 1987). They can also be emitted via processes such as meat cooking (Rogge et al., 1993) and biomass burning (Kawamura et al., 2013; Pereira et al., 1982) and can be secondarily formed by the photo-oxidation of higher chain organic acids, such as azelaic acid (Bikkina et al., 2014; Ervens et al., 2004). Oxalate (C2) is the smallest of the three acids and is usually the most abundant on a mass basis of all dicarboxylic acids in tropospheric aerosols as it represents an end product in the oxidation of both larger-chain carboxylic acids and also glyoxylic acid (Ervens et al., 2004). It can be emitted via direct emissions such as from biomass burning (Graham et al., 2002; Narukawa et al., 1999; Xu et al., 2020) and combustion exhaust (Kawamura and Kaplan, 1987; Kawamura and Yasui, 2005; Wang et al., 2010) and from various biogenic sources (Kawamura and Kaplan, 1987).
Maleate (C4) is an unsaturated dicarboxylic acid originating from combustion engines, including via direct emissions (Kawamura and Kaplan, 1987) and secondarily produced from the photo-oxidation of benzene (Rogge et al., 1993). Lastly, phthalate (C8) represents an aromatic dicarboxylic acid associated with incomplete combustion of vehicular emissions (Kawamura and Kaplan, 1987) and oxidation of naphthalene or other polycyclic aromatic hydrocarbons (Fine et al., 2004; Kawamura and Ikushima, 2002; Kawamura and Yasui, 2005). However, it has also been linked to biomass burning (Kumar et al., 2015) and burning of plastic material such as polyvinyl chloride (PVC) products, garbage, and plastic bags (Agarwal et al., 2020; Claeys et al., 2012; Fu et al., 2012; Li et al., 2019; Nguyen et al., 2016; Simoneit et al., 2005). Secondary formation via aqueous-phase chemistry has been documented for these organic acids (Kunwar et al., 2019; Sorooshian et al., 2007a, 2010, 2006; Wonaschuetz et al., 2012) and MSA (Hoffmann et al., 2016).
4.1 Meteorology and transport patterns
Meteorological data are summarized based on average values temporally coincident with each MOUDI sample set period for each of the seasons. The exception to this was the accumulated rainfall, which was summed for the MOUDI set duration. Temperatures were stable during the different seasons: 28.0 ± 1.04 ∘C (SWM18), 28.9 ± 0.8 ∘C (transitional), 28.3 ± 1.9 ∘C (NEM), and 28.4 ± 1.5 ∘C (SWM19). Solar radiation was the highest during the transitional (279.61 ± 19.68 W m−2) and NEM (304.01 ± 67.54 W m−2) seasons and lowest during the SWM18 (225.32 ± 56.26 W m−2) and SWM19 (256.05 ± 86.88 W m−2) seasons, owing largely to more cloud cover. Accumulated rain was highest for both SWM seasons (SWM18: 29.78 ± 27.28 mm; SWM19: 16.66 ± 23.98 mm) and much lower during the transitional (1.00 ± 1.11 mm) and NEM (2.20 ± 6.70 mm) seasons. Relative humidity was relatively consistent across seasons: SWM18 (69.6 ± 5.0 %), transitional (69.2 ± 2.2 %), NEM season (62.4 ± 8.0 %), SWM19 (72.6 ± 11.7 %). Finally, Fig. 1 summarizes predominant wind patterns for each season based on HYSPLIT back-trajectories collected every 6 h during sampling periods. The SWM18 and SWM19 seasons were characterized by predominantly southwesterly winds, while the NEM and transitional seasons experienced mostly northeasterly winds. In conclusion, there was much higher potential for wet scavenging during the SWM seasons, with the potential for more photochemical reactivity in the NEM and transitional seasons owing to enhanced incident solar radiation. As humidity was generally enhanced year round, there was the likelihood of aqueous-phase processing to occur in all seasons. The combination of sustained RH, low boundary layer height, and high surface-level particle concentrations has been suggested to counteract the effects of wet deposition on total particle concentration in Metro Manila (Hilario et al., 2020a).
4.2 Bulk aerosol measurements
The range, mean, and standard deviation of concentrations integrated across the MOUDI diameter range (0.056–18 µm) are shown in Table 1 for each organic acid and MSA for all seasons. In order of decreasing concentration, the following was the order of abundance based on the cumulative dataset: oxalate (149 ± 94 ng m−3) > succinate (10 ± 22 ng m−3) > maleate (10 ± 20 ng m−3) > phthalate (9 ± 14 ng m−3) > adipate (7.6 ± 9.4 ng m−3) > MSA (5.4 ± 5.2 ng m−3). The relative order of abundance varies for the sub- and supermicrometer ranges, with the only consistent feature being that oxalate was the most abundant species. This result was consistent with past works showing oxalate to be the most abundant organic acid in different global regions (e.g., Decesari et al. 2006; Kerminen et al. 1999; Sorooshian et al. 2007b; Ziemba et al. 2011).
Figure 2 shows the combined contribution of the organic acids and MSA to total gravimetric mass, while Table S5 summarizes percent contributions of individual species to total mass for different size bins. Combined, the measured organic acids and MSA accounted for only a small part of the total cumulative mass (0.80 ± 0.66 %) across the 11 individual gravimetric sets. When the combined contribution of organic acids and MSA to total gravimetric mass was separated by season, results are generally the same (Fig. S1), with differences in the percent range being as follows: SWM18 = 0.64 %; transitional = 0.95 %; NEM = 0.50 %–1.49 %; and SWM19 = 0.23 %–0.83 %. The highest contribution of these organic acids and MSA occurred for MOUDI sets collected 12–14 March 2019 during the NEM season, which accounted for 1.49 % (0.50 µg m−3) of the total mass. The lowest contribution of these organic acids and MSA occurred for MOUDI sets collected 11–13 September 2019 during the SWM19 season, which accounted for 0.23 % (0.06 µg m−3) of the total mass. The summed contributions of the six species were nearly the same in the sub- and supermicrometer ranges (0.78 ± 0.74 % and 0.84 ± 0.58 %, respectively). Their contributions peaked in the two size bins covering the range between 0.56 and 1.8 µm (0.56–1 µm: 1.06 ± 1.01 %; 1–1.8 µm: 1.01 ± 0.78 %). After accounting for all measured species (BC, water-soluble species), 33.74 ± 19.89 % (range: 23.86 %–50.88 %) of unresolved mass still remained. Therefore, the six species of interest in this work only explain a small amount of the region's mass concentrations, and further work is still needed to resolve the remaining components, which presumably are dominated by water-insoluble organics and elements. Of most need is to resolve those missing components in the supermicrometer range, for which Table S5 shows that the unresolved fraction is 69.10 ± 25.91 %, in contrast to 17.78 ± 17.25 % for the submicrometer range.
Although there are fairly wide ranges in concentration for the individual species, a few features are noteworthy based on the cumulative dataset. First, the oxalate concentrations are lower than expected for such a highly polluted area, as will be expanded upon in Sect. 5.5. Second, there is a significant decrease in concentration after oxalate for the remaining five species, which had similar mean concentrations. Lastly, although the sampling site is on an island and close to marine sources, MSA is surprisingly the least abundant among the six species of interest.
Mean mass concentrations of these species varied greatly by season as visually shown in Fig. 3a and summarized numerically in Table 1. In contrast, Fig. 3b shows that the mass fractions of the six species did not change much seasonally, owing to the dominance of oxalate (37.67–472.82 ng m−3), which accounted for between 69.1 %–87.3 % of the cumulative concentration of the six species across the four seasons. Important features with regard to seasonal mass concentration differences include the following: (i) maleate concentrations were much higher in the SWM18 and SWM19 seasons; (ii) the lowest overall concentrations of most species, besides oxalate and succinate (lowest in SWM19), were observed in the NEM season; (iii) oxalate and phthalate were the only species that peaked in the transitional period, whereas the rest of the species peaked in either SWM18 or SWM19; and (iv) succinate and phthalate were peculiarly much more enhanced in SWM18 than SWM19, pointing to significant variability between consecutive years.
4.3 Source apportionment
To help elucidate how different emissions sources impact the six species, PMF analysis was conducted and yielded a solution with five source factors using year-round data (Fig. 4). The five sources are as follows in decreasing order of their contribution to the total mass based on the sum of species used in the PMF analysis (Fig. 4): combustion (32.1 %), biomass burning (20.9 %), sea salt (20.9 %), crustal (14.2 %), and waste processing (11.9 %). The contribution of each source to the total concentration of organic acids and MSA was as follows: combustion (33.5 %), biomass burning (29.0 %), crustal (27.0 %), waste processing (9.8 %), and sea salt (0.6 %). The source factor names were determined based on the enhancement of the following species (Fig. 4): (i) crustal (Al, Ti) (Harrison et al., 2011; Malm et al., 1994; Singh et al., 2002); (ii) biomass burning (K, Rb) (Andreae, 1983; Artaxo et al., 1994; Braun et al., 2020; Chow et al., 2004; Echalar et al., 1995; Ma et al., 2019; Schlosser et al., 2017; Thepnuan et al., 2019; Yamasoe et al., 2000); (iii) sea salt (Na, Cl) (Seinfeld and Pandis, 2016); (iv) combustion (V, Ni, As) (Allen et al., 2001; Linak et al., 2000; Mahowald et al., 2008; Mooibroek et al., 2011; Prabhakar et al., 2014; Wasson et al., 2005); and (v) waste processing (Cd, Pb) (Cruz et al., 2019; Gullett et al., 2007; Iijima et al., 2007; Pabroa et al., 2011). While both SO and NO are secondarily produced, the latter is more commonly linked to supermicrometer particles (Allen et al., 1996; Dasgupta et al., 2007; Fitzgerald, 1991; Maudlin et al., 2015), including in the study region (Cruz et al., 2019). Additionally, Al, K, and Cl are linked to biomass burning (Reid et al., 1998, 2005; Schlosser et al., 2017; Wonaschütz et al., 2011). The source factor names should be interpreted with caution, as a single profile may consist of a mix of sources (e.g., waste processing). It should be noted that Cruz et al. (2019) performed PMF analysis for only the SWM18 season, which yielded similar and additional sources for only the SWM18 season, whereas this study used year-round data.
To provide a size-resolved context for the five aerosol sources, Fig. 5 shows their respective reconstructed mass size distributions based on PMF output. Distributions for combustion, biomass burning, and waste processing primarily peaked in the submicrometer range, while crustal and sea salt sources primarily peaked in the supermicrometer range. Combustion and biomass burning factors showed a dominant peak between 0.32–0.56 µm, whereas waste processing had a peak between 0.56–1 µm. The crustal and sea salt factors exhibited their peak concentrations between 1.8–5.6 µm. Both crustal and biomass burning sources showed signs of bimodal size distributions, with a minor peak in the sub- and supermicrometer ranges, respectively.
As reported in Table 2, combustion was the largest contributor to the cumulative mass concentrations of organic acids and MSA, with the largest influence being for maleate (69.7 %) and MSA (57.4 %). Biomass burning was marked by its significant contribution to succinate (90.3 %). The sea salt source showed minor contributions to phthalate (9.9 %) and adipate (4.7 %). The crustal source contributed appreciably to adipate (35.9 %) and oxalate (31.2 %), with the rest of the organic acid or MSA species being less influenced (0.1 %–13.3 %). Organic acids have been shown in past work to be associated with mineral dust (Russell et al., 2002), including both oxalic and adipic acids (Falkovich et al., 2004; Kawamura et al., 2013; Sullivan and Prather, 2007; Tsai et al., 2014), although less has been documented for adipate. Wang et al. (2017) and Yao et al. (2003) both report that gaseous acids are likely to adsorb onto supermicrometer particles that are highly alkaline, such as dust. The waste processing factor contributed to maleate (30.1 %), oxalate (10.5 %), and MSA (1.4 %). An unexpected result was that the sea salt factor did not contribute to MSA, even though the latter is derived from ocean-emitted DMS; the results of Table 2 suggest that other sources such as biomass burning and industrial activities are more influential in the study region, similar to other regions like Beijing (Yuan et al., 2004) and coastal and inland areas of California (Sorooshian et al., 2015).
4.4 Species interrelationships
Correlation analysis was conducted for the same species used in the PMF analysis to quantify interrelationships and to gain additional insight into common production pathways. Correlation coefficient (r) values are reported in Table 3 for the sub- and supermicrometer ranges, whereas results for the full size range are shown in Table S6. Values are only shown and discussed subsequently for correlations with p values below 0.05. Unless otherwise stated, correlations discussed below correspond to the full size range for simplicity, whereas notable results when contrasting the two size ranges (< 1 µm and < 1 µm) are explicitly mentioned.
MSA exhibited a statistically significant correlation with Rb (r=0.37), suggestive of its link with biomass burning as Rb has been shown in the study region to be a biomass burning marker (Braun et al., 2020). Additionally, MSA was correlated with Na, NO, and SO (r: 0.35–0.59), which are associated with marine aerosol (e.g., sea salt, DMS, shipping) but also biomass burning. The supermicrometer results indicate MSA was correlated only with Na (r=0.32), due presumably to co-emission from both crustal and sea salt sources, with the former commonly linked to biomass burning (Schlosser et al., 2017). For the submicrometer range, MSA was correlated with Rb and SO (r: 0.39–0.60), which are derived from biomass burning and other forms of combustion, consistent with smaller particles formed secondarily from gas-to-particle conversion processes. That is also why MSA was well correlated with succinate, oxalate, and phthalate (r: 0.53–0.67), which were also prominent species in either (or both) of the biomass burning and combustion factors.
Adipate only exhibited significant correlations with maleate and phthalate for the full diameter range (r: 0.43–0.45), while maleate was correlated only with adipate. In contrast, succinate, oxalate, and phthalate were correlated with a wide suite of species, indicating that maleate and adipate exhibited more unique behavior in terms of their production routes. Succinate, oxalate, and phthalate similarly exhibited significant correlations with each other and species linked to crustal sources (Al, Ti, Na), sea salt (Na), and biomass burning (Rb). Succinate and oxalate in particular were better correlated with tracer species related to either dust or sea salt (Al, Na) in the supermicrometer range and were correlated with each other also in that size range.
4.5 Cumulative size distribution variations
Mass size distributions for each individual organic acid and MSA are shown for the full study period in Fig. S2, and seasonal mass size distributions can be seen in Figs. 6–11. General information for the cumulative dataset will be described here before examining seasonal results in Sect. 5. While significant variability exists between individual sets for the cumulative dataset, a few general features are evident: (i) mass size distributions all appear multimodal with the exception of maleate, which on average exhibited a unimodal profile; (ii) all species show a larger peak in the submicrometer range versus supermicrometer sizes; (iii) phthalate and adipate show more comparable peaks in the sub- and supermicrometer range; and (iv) the size bin in which the peaks occur varies between species. These results point to differences in the species with regard to their source, formation mechanism, and eventual fate.
One factor relevant to the mass size distribution plots is the source origin of sampled air masses. The CWT plots in Fig. 12 reveal the bulk of the concentration of a few species (e.g., phthalate, succinate, and MSA) was explained by southwesterly flow. Consistent with the PMF results showing that the biomass burning factor contributed the most to these three species, the predominant fire sources were to the southwest of Luzon. Past work has linked these areas to significant biomass burning influence over Luzon and the South China Sea during the SWM season (Atwood et al., 2017; Ge et al., 2017; Hilario et al., 2020b; Reid et al., 2016; Song et al., 2018; Wang et al., 2013; Xian et al., 2013). It is noteworthy that the CWT maps for SWM18 reveal more influence from the biomass burning hotspots to the southwest (e.g., Borneo and Sumatra), in contrast to SWM19, pointing to more biomass burning influence in the former season. Oxalate's CWT profile shows the most spatial heterogeneity in terms of source regions; this is consistent with it being an end product in the oxidation of other carboxylic acids that can originate from numerous sources. Finally, adipate and maleate similarly showed a localized hotspot in terms of where their greatest influence originated, approximately 290 km to the north–northwest of MO. This could be partly linked to the Sual coal-fired power station located near that area, where an ash disposal site is also in close proximity. The uniquely similar CWT maps between adipate and maleate are consistent, with them having few correlations, if any, with species aside from each other (Table S6). Subsequent sections discuss each organic acid and MSA in more detail, beginning with larger acids since knowledge of their behavior is important to better understand the smaller acids.
Results from Sect. 4 show that phthalate has the following characteristics:
influenced most by biomass burning (49.5 %), followed by combustion (27.4 %), crustal sources (13.3 %), and then sea salt (9.9 %);
significant correlations with more species in Table S6 than any other organic acid or MSA;
comparable mass size distribution modes in the sub- and supermicrometer size ranges;
highest mass concentration in the transitional period but also significantly different concentrations between the two SWM seasons;
concentrations dominated by sources to the southwest.
A more detailed examination based on seasonally resolved mass size distributions and CWT maps follows to try to gain more insights into this species. Although not referenced hereafter, Table S7 provides numerical details about mass concentration mode sizes and associated concentrations for each season and the cumulative dataset for each species.
The average size distributions for phthalate appeared bimodal for each individual season (Fig. 6). Depending on the season, concentration peaks occurred in three separate MOUDI stages for the submicrometer range and between 1.8–3.2 or 3.2–5.6 µm in the supermicrometer range. The NEM season was unique in that the supermicrometer peak was considerably more pronounced than in the submicrometer range, which was a rare occurrence in this study for all species except adipate. Phthalate appears in the submicrometer range due to secondary formation by photo-oxidation (i.e., Kautzman et al., 2010; Kawamura and Ikushima, 2002; Kawamura and Yasui, 2005; Kleindienst et al., 2012) and from primary emissions (i.e., combustion, biomass/waste burning) (i.e., Deshmukh et al., 2016; Kawamura and Kaplan, 1987; Kumar et al., 2015; Kundu et al., 2010). Its general presence in the supermicrometer range, especially during the NEM season, can be explained by possible adsorption onto larger particles such as dust and sea salt (i.e., Wang et al., 2012, 2017). Others have observed an enhancement in phthalate in the supermicrometer mode, specifically in Xi'an, China, due to suspected adsorption of its vapor form (Wang et al., 2012) derived from photo-oxidation of naphthalene (Ho et al., 2006; Wang et al., 2011, 2012, 2017).
CWT results for phthalate (Fig. S3) showed high concentrations across all seasons coming from the southwest, most notably in the SWM18 and SWM19 seasons. The significant reduction in phthalate levels from SWM18 (17±25 ng m−3) to SWM19 (5.7 ± 7.4 ng m−3) is coincident with a stronger influence from biomass burning from the southwest in 2018. Figure 3 showed that the highest concentration of phthalate occurred in the transitional period, assumed to be largely due to local emissions (e.g., vehicular traffic) based on the CWT results, with a significant influence in the immediate vicinity of Luzon unlike the other seasons. The peculiar size distribution results for the NEM season can be explained by the CWT map showing a strong influence from the northeast, which likely includes supermicrometer aerosol influences from sea salt and dust from East Asia. The reduced influence of upwind anthropogenic and biomass burning emissions during the NEM season can explain the lower seasonal concentrations, especially in the submicrometer size range (Hsu et al., 2009).
Adipate was shown in Sect. 4 to have the following features:
influenced most by crustal sources (35.9 %), followed by combustion (32.9 %), biomass burning (26.4 %), and finally sea salt (4.7 %);
only correlated with maleate and phthalate;
comparable concentrations in the sub- and supermicrometer size ranges, with a mode between 5.6 and 10 µm;
highest mass concentration in the SWM seasons but especially the SWM19 season;
concentrations dominated by sources from the southwest as well as from the northwest.
Mass size distributions for adipate were the most variable in structure compared to the other five species, with multiple peaks present at different sizes (Fig. S2). In general, its distributions appeared uniquely and consistently trimodal, with the exception of the SWM18 season when the distribution was bimodal (Fig. 7). Modes appeared between 0.10–0.18 and 0.32–0.56 µm for the submicrometer range and between 1.0–1.8 and 3.2–5.6 µm for the supermicrometer range. The SWM19 season was unique for adipate as the highest peak was in the supermicrometer range, and it was higher than any other peak across the other seasons. Submicrometer adipate is likely derived from photo-oxidation of higher chain organic acids (i.e., van Drooge and Grimalt, 2015), ozonolysis of vehicular emissions (i.e., Grosjean et al., 1978), and the primary emissions of biomass burning (i.e., Graham et al., 2002). The appearance in the supermicrometer range is likely due to adsorption onto larger particles such as dust and sea salt (e.g., Wang et al., 2012, 2017). As the PMF results suggest crustal sources were more influential for adipate in contrast to sea salt, dust was more likely the supermicrometer particle type that adipate preferentially partitioned to. The source of the dust was likely a combination of long-range transport from (i) the southwest, especially during biomass burning periods, (ii) East Asia, and (iii) locally generated dust via anthropogenic activities (Fig. S4).
Past work in the study region showed that broad mass size distributions with comparable concentrations in the sub- and supermicrometer ranges were coincident with wet scavenging (Braun et al., 2020) and appreciable primary emissions of sea salt and dust (AzadiAghdam et al., 2019; Cruz et al., 2019). Scavenging was suggested to remove transported pollution while allowing for more pronounced contributions from more localized emissions, which could include vehicular traffic, sea salt, and anthropogenic forms of dust (e.g., road dust, construction), all of which are consistent with adipate's mass size distribution data and CWT maps (Fig. S4) showing high concentrations predominately around Luzon for all seasons.
Succinate exhibited the following characteristics:
influenced primarily by biomass burning (90.3 %), followed by crustal sources (9.7 %);
high correlation coefficients (0.67–0.76) with oxalate, phthalate, and MSA (Table S6);
mass focused in the submicrometer range;
highest mass concentrations in the SWM18 season, and, similar to phthalate, a significant reduction in the SWM19 season;
concentrations dominated by sources from the southwest.
The average size distributions for succinate varied in the number of peaks present (2–4) but on average were bimodal with a submicrometer mode usually between 0.32–0.56 or 0.56–1.0 µm and a smaller supermicrometer mode between either 1.8–3.2 or 3.2–5.6 µm (Fig. 8). The chief source of succinate, which is concentrated in the submicrometer peak, is biomass burning (Pratt et al., 2011; Vasconcellos et al., 2010), which is reinforced by the PMF results (Table 2), its high correlation with the biomass burning tracer Rb (r=0.67; Table S6) (Braun et al., 2020), and CWT maps showing its most pronounced influence from biomass burning hotspots to the southwest during the SWM18 season (Fig. S5). There likely was also local biomass burning during the NEM season contributing to succinate concentrations. Hilario et al. (2020a) showed based on satellite data that local fire activity peaks between March and May. There was less influence from biomass burning in the SWM19 season, which is why succinate's levels were lower (4.7 ± 7.4 ng m−3) than in the SWM18 season (22 ± 43 ng m−3). Similar to phthalate and adipate, there were more local hotspots of concentration in seasonal CWT maps, pointing to local anthropogenic sources such as vehicular traffic and the presence of supermicrometer particles like dust and sea salt that succinate can partition to (e.g., Wang et al., 2012, 2017).
The results of Sect. 4 showed that maleate had the following attributes:
influenced most by combustion (69.7 %), followed by waste processing (30.1 %), and then barely by crustal sources (0.2 %);
only correlated with adipate of all species shown in Table S6;
a unimodal mass size distribution, with negligible contribution in the supermicrometer range;
highest mass concentration in the SWM19 season but comparable to the SWM18 season;
the most localized sources as compared to the other species examined, as shown by CWT maps (Fig. 11).
The average seasonal size distributions for maleate appeared to be unimodal, with peaks between 0.32–0.56 and 0.56–1.0 µm (Fig. 9). The absence of a supermicrometer peak, in contrast to most other species, suggests that it had less diverse sources and was derived from combustion emissions without being adsorbed onto supermicrometer particles like the other species investigated. The association of maleate with the waste processing source factor in Table 2 can be explained partly by the burning and recycling of electronic waste (Cruz et al., 2019; Gullett et al., 2007; Iijima et al., 2007). The Pabroa et al. (2011) study reported that there are few licensed operators for battery recycling, but there are numerous unregulated melters frequently melting metal and discarding the waste.
Seasonal CWT maps for maleate (Fig. S6) consistently showed hotspots around Luzon, indicative of local emissions. Maleate concentrations for the SWM18 (19 ± 15 ng m−3) and SWM19 (19 ± 34 ng m−3) were significantly higher than the other seasons (transitional: 3.8 ± 4.2 ng m−3; NEM: 1.7 ± 3.7 ng m−3), and this could likely be due to increased traffic emissions because of gridlock due to intense rainfall. It should be noted that the Ateneo de Manila campus has student break periods in March, April, May, and December (Hilario et al., 2020a); those months pertain to the NEM season, which could lead to lower combustion emissions from vehicles (e.g., maleate and phthalate). Although the SWM season is associated with enhanced precipitation over Metro Manila, lower boundary layer height and appreciable RH values could counteract wet scavenging to some degree by promoting aqueous processing of aerosol (Hilario et al., 2020a). Furthermore, maleate's largely submicrometer size distribution (Fig. 9) may reduce the efficiency of wet scavenging (Greenfield, 1957).
Oxalate was shown to have the following traits:
influenced somewhat uniformly by combustion (32.9 %) and crustal (31.2 %) sources, followed by biomass burning (25.4 %), and waste processing (10.5 %);
only organic acid to correlate with combustion tracers (V, Ni);
pronounced presence in both the sub- and supermicrometer size ranges;
highest mass concentrations in the transitional period;
contributions from the southwest, east/northeast, and local sources.
Oxalate concentrations in this study (37.67–472.82 ng m−3) were surprisingly low for such a polluted megacity with strong regional sources. For context, concentrations in a few other regions are as follows: 270–1350 ng m−3 in Tokyo, Japan (Kawamura and Ikushima, 2002; Sempére and Kawamura, 1994); 195–669 ng m−3 in Beijing, China (Du et al., 2014); and 149–735 ng m−3 in Thumba, India (Hegde et al., 2016).
The average size distributions for oxalate appeared bimodal for each individual season with modes between 0.32–0.56 and 0.56–1.0 µm for the submicrometer range and a separate mode between 1.8–3.2 µm for the supermicrometer range (Fig. 10). A unique aspect for oxalate was its consistency in having a bimodal profile each season, with the supermicrometer mode always between 1.8–3.2 µm. Note that the modes discussed here represent the most pronounced ones, but others could have been present too, reflecting other sources. Submicrometer oxalate likely originated from secondary production from both biogenic and anthropogenic precursor emissions and potentially from primary emissions (i.e., combustion/biomass burning) (i.e., Decesari et al., 2006; Falkovich et al., 2005; Golly et al., 2019; Kundu et al., 2010; Wang et al., 2010). Of all the six species studied, oxalate was best correlated with SO (r=0.69; Table S6), especially in the submicrometer range (r=0.72; Table 3), which is consistent with their common production mechanism via aqueous processing (Sorooshian et al., 2006; Yu et al., 2005). Additionally, high concentrations of oxalate in the transitional period suggest that photo-oxidation was an important process for oxalate formation since the transitional period had low rain and high solar radiation. The prominent supermicrometer presence was likely due to adsorption onto supermicrometer particles. Past work by Sullivan and Prather (2007) reported the following with regard to oxalate's behavior in coarse particles of relevance to this study: (i) oxalic acid was predominately associated with mineral dust and to a lesser degree with aged sea salt; (ii) even though most of the total mass was sea salt, there was more oxalate per mass of mineral dust than sea salt; (iii) Asian dust particles are more alkaline as opposed to sea salt and therefore act as better sinks for dicarboxylic acids than sea salt; and (iv) it is feasible that a large fraction of supermicrometer dicarboxylic acid mass in remote marine air is associated with mineral dust and not sea salt. The PMF results from the present study suggest that oxalate was much more influenced by crustal sources (31.2 %) versus sea salt (0 %), similar to phthalate, adipate, and succinate (Table 2). Reinforcing the relationship between oxalate and dust is the significant correlation between oxalate and both Al (r=0.59) and Ti (0.29) in the supermicrometer range.
CWT results for oxalate (Fig. S7) showed high concentrations around Luzon for all seasons, with the caveat that the SWM18 exhibited high concentrations coming from the southwest, which has already been linked to biomass burning emissions. The difference in oxalate levels between the SWM18 (178 ± 139 ng m−3) and SWM19 (110 ± 62 ng m−3) seasons is largely due to the enhanced contribution of biomass burning in the former season since oxalate is abundant in fire emissions (Falkovich et al., 2005; Mardi et al., 2018; Narukawa et al., 1999).
Previous sections revealed the following characteristics for MSA:
influenced most by combustion (57.4 %), followed by biomass burning (41.2 %), waste processing (1.4 %), and then crustal sources (0.1 %);
significantly correlated with succinate, oxalate, phthalate, and SO;
similar to maleate, primarily consisted of a submicrometer mass size distribution peak with only minor contributions from the supermicrometer mode;
concentration highest during the SWM18 season;
concentrations dominated by sources from the southwest.
Concentrations of MSA in this study were surprisingly low for a site so close to marine and anthropogenic sources (0.10–23.23 ng m−3). For context, MSA concentrations in nearby regions are as follows: 30–60 ng m−3 in Nanjing, China (Yang et al., 2005), and 29–66 ng m−3 over the China Sea (Gao et al., 1996).
The average size distributions for MSA appeared unimodal, with the peak size being between 0.32–0.56 µm (Fig. 11). The consistent mass size distribution for MSA in all seasons, similar to maleate, could be due to some combination of limited sources and production pathways. Surprisingly, MSA showed no association with the sea salt source factor (Table 2), even though it would be expected given that DMS is co-emitted from the ocean with sea salt. Due to the proximity of the sampling site to the ocean, it is possible that the local sea salt was relatively fresh with short transport time, which could potentially explain the lack of an association with MSA as it requires time to be produced from its marine precursor DMS. Instead, combustion and biomass burning sources were more significantly related to MSA, which is consistent with some past studies linking MSA to anthropogenic sources (Yuan et al., 2004) and biomass burning (Sorooshian et al., 2015). Consequently, concentrations of MSA from these other non-marine sources could be much higher, causing the PMF model to associate MSA with non-sea-salt-related sources. CWT results for MSA (Fig. S8) showed high concentrations coming from the southwest during the SWM18 and SWM19 seasons and from the east–northeast during the NEM and transitional period.
Both MSA and oxalate had significantly lower concentrations than other regions, and there are a few possible explanations for this. First, it is worth noting that degradation of these species is unlikely due to storage or sonication as careful procedures were followed, as noted in Sect. 2.2. The Philippines has relatively high temperatures, humidity, and solar radiation year round, providing optimal conditions for processing and degradation to occur, yielding low concentrations of MSA and oxalate. Furthermore, there are mechanisms by which species such as oxalate can be degraded via complexation effects with metal cations (Paris and Desboeufs, 2013; Siffert and Sulzberger, 1991; Sorooshian et al., 2013; Zuo, 1995), which are abundant in the study region.
This work used a 16-month long dataset of size-resolved aerosol composition to investigate the nature of five organic acids (oxalate, succinate, adipate, maleate, and phthalate) and MSA in the polluted Metro Manila region in the Philippines. Selected results are as follows in order of the three major questions posed at the end of Sect. 1.
Organic acids and MSA contribute only a small fraction to the total gravimetric aerosol mass in Metro Manila (0.80 ± 0.66 %). The combined contribution of these six species was similar between the sub- and supermicrometer range (0.78 % and 0.84 %, respectively). After accounting for water-soluble ions and elements, and black carbon, there still was an unresolved mass fraction amounting to 33.74 % across all sizes and 17.78 % and 69.10 % for sub- and supermicrometer sizes, respectively. Therefore, future work is still warranted to identify what the missing fraction is comprised of, which is speculated to be water-insoluble organics and elements.
Oxalate was the most abundant of the six species, accounting for 69.1 %–87.3 % of the total combined mass of the six species depending on the season. However, the bulk concentrations of oxalate were unusually low (149 ± 94 ng m−3) for such a polluted area in contrast to other populated regions. Concentrations of the other five species were much lower than oxalate, with mean levels for the entire study period being less than 10 ng m−3. In particular, MSA exhibited the lowest mean concentration (5.4 ± 5.2 ng m−3). It is unclear exactly as to the reason for the low concentrations of the examined species in light of the diverse marine and anthropogenic sources in the region. The role of wet scavenging, especially in the SWM seasons, will be the subject of future research.
The six species exhibited different behavior seasonally, both in terms of relative concentration and mass size distribution. The SWM18 season was uniquely different than the SWM19 season, owing to more biomass burning emissions transported from the southwest that yielded enhanced levels for most species in the submicrometer range, especially succinate, MSA, oxalate, and phthalate. Enhanced precipitation in the SWM seasons also was coincident with more influence from localized emissions, leading to enhanced levels in the sub- and supermicrometer ranges depending on the species. The NEM season was characterized by generally lower concentrations of most species as air was predominantly transported from the northeast, with reduced influence of anthropogenic and biomass burning emissions. Phthalate was enhanced in the supermicrometer range during the NEM season due to presumed adsorption to Asian dust and to a lesser extent sea salt. The transitional season was characterized as having a strong influence from localized emissions for all six species, which promoted especially high concentrations of phthalate and oxalate in both the sub- and supermicrometer ranges.
All species exhibited a prominent submicrometer peak that likely stemmed largely from secondary formation from both anthropogenic and biogenic precursor emissions and was especially prominent during the SWM18 season due to extensive biomass burning influence. Biomass burning was an especially important source for succinate, phthalate, MSA, oxalate, and adipate. All six species exhibited relatively low association with sea salt particles; this was particularly interesting for MSA, which was instead better related to combustion and biomass burning emissions. In contrast to sea salt, most species were linked to crustal emissions, as evident from peaks in the coarse mode during periods of dust influence. Oxalate, adipate, phthalate, and succinate in particular preferentially partitioned to dust rather than sea salt, potentially due to their affinity for alkaline particle types. Oxalate was best correlated with sulfate, especially in the submicrometer mode, explained by their common production via aqueous processing, which is common in the study region, owing to high humidity levels year round.
The results of this study point to the importance of size-resolved measurements of organic and sulfonic acids as this extensive dataset revealed important changes in mass size distributions between species and for different seasons. The data point to the partitioning of these species to coarse aerosol types and the potentially significant impact of precipitation on either the removal or enhancement of species' mass size distribution modes; these topics warrant additional research to establish more clearly the sensitivity of these species to source regions, transport pathways, and wet scavenging effects. More research is warranted to investigate the remaining fraction of the unresolved mass (approximately one-third of the gravimetric mass) that is not accounted for by black carbon and the water-soluble constituents speciated in this work. This is especially important for the supermicrometer range. Lastly, the current results point to the question as to what drives the affinity of individual species towards the coarse mode for different aerosol types (e.g., dust, sea salt) and how common this is for other regions.
Size-resolved aerosol data collected at Manila Observatory are described in Stahl et al. (2020a) (https://www.nature.com/articles/s41597-020-0466-y, last access: 1 July 2020) and archived on figshare (Stahl et al., 2020b) (https://figshare.com/articles/An_Annual_Time_Series_of_Weekly_Size-Resolved_Aerosol_Properties_in_the_Megacity_of_Metro_Manila_Philippines/11861859, last access: 1 July 2020) as well as in the NASA data repository at https://asdc.larc.nasa.gov/project/CAMP2Ex, last access: 1 July 2020.
The supplement related to this article is available online at: https://doi.org/10.5194/acp-20-15907-2020-supplement.
MTC, MOC, JBS, RAB, ABM, CS, and AS designed the experiment. All coauthors carried out various aspects of the data collection. MTC, RAB, CS, and AS conducted analysis and interpretation of the data. CS and AS prepared the manuscript with contributions from the coauthors.
The authors declare that they have no conflict of interest.
The authors acknowledge support from NASA grant 80NSSC18K0148 in support of the NASA CAMP2Ex project. Rachel A. Braun acknowledges support from the ARCS Foundation. Melliza Templonuevo Cruz acknowledges support from the Philippine Department of Science and Technology's ASTHRD Program. Alexander B. MacDonald acknowledges support from the Mexican National Council for Science and Technology (CONACYT). We acknowledge Agilent Technologies for their support and Shane Snyder's laboratories for ICP-QQQ data.
This research has been supported by the National Aeronautics and Space Administration (NASA) (grant no. 80NSSC18K0148).
This paper was edited by Eleanor Browne and reviewed by two anonymous referees.
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