Iodine speciation and size distribution in ambient aerosols at a coastal new particle formation hotspot in China
- 1Department of Atmospheric Science, School of Environmental Studies, China University of Geosciences, Wuhan 430074, China
- 2School of Environmental Science and Engineering, Nanjing University of Information Science and Technology, Nanjing 210044, China
- 3Department of Chemical and Environmental Engineering, University of Nottingham Ningbo China, Ningbo 315100, China
- 4Ningbo Urban Environment Observation and Research Station, Institute of Urban Environment, Chinese Academy of Sciences, Xiamen 361021, China
Correspondence: Huan Yu (email@example.com)
Intense new particle formation (NPF) events were observed in the coastal atmosphere during algae growth and farming season at Xiangshan gulf of the east China coast. High nucleation-mode iodine concentrations measured by ultra-performance liquid chromatography coupled with quadrupole time-of-flight mass spectrometry (UPLC/Q-TOF-MS) confirmed that the NPF events were induced by iodine species. Our study provides important information on iodine speciation, size distributions, and its role in NPF in the context of heavy air pollution in China's coastal areas. For the first time, we identified 5 inorganic iodine species, 45 organic iodine compounds (35 molecular formulas), and a group of iodide–organic adducts in aerosols. The concentrations and size distributions of iodine species down to 10 nm were measured during the iodine-induced NPF, continental NPF, and non-NPF days at the coastal site and compared to those at an inland site. The iodine in the above four aerosol sample types were characterized by iodate, aromatic iodine compounds, iodoacetic acid or iodopropenoic acid, and iodide–organic adducts, respectively. Iodide and organic iodine compounds were found in the nucleation-mode particles; however, it is still not clear whether they contributed to nucleation or just new particle growth. Wild algae, as well as farmed algae, could be an important NPF source in China's coastal areas.
Iodine is an essential trace element for all mammals (including human beings) and some aquatic plants. The atmospheric impact of iodine includes ozone (O3) depletion, altering HOx and NOx chemistry, mercury oxidation, and aerosol formation (Baker et al., 2001; O'Dowd et al., 2002a). Marine emission sources of iodine-containing species in the atmosphere – such as iodomethane, molecular iodine (I2), and hypoiodous acid (HOI) – include marine biota emission (Baker et al., 2000), sea surface iodide (I−) activation by O3 (Dixneuf et al., 2009; Mcfiggans et al., 2004; Palmer et al., 2005; Sellegri et al., 2006), and sea surface bubble bursting (Seto and Duce, 1972). Continental iodine sources include soil emission, fossil fuel and biomass combustions, and industrial emissions (Redeker et al., 2000; Sive et al., 2007). In recent years, much attention has been paid to the new particle formation (NPF) induced by iodine species (Kumar et al., 2018; Dall'Osto et al., 2018; Allan et al., 2015; Roscoe et al., 2015; Mahajan et al., 2011; McFiggans et al., 2010; O'Dowd and De Leeuw, 2007; Grose et al., 2007; Yoon et al., 2006; O'Dowd et al., 2002b). Based on current knowledge, a simplified scheme of iodine oxidation and nucleation is described as follows: volatile iodocarbons or I2 photolyze to I atoms, which react with O3 to produce IO and IO2 radicals; subsequently, the self-combination of IO and IO2 forms iodine oxides I2O2−5; iodine oxoacids HIOx (x=1–3) are produced either from I2O2−5 hydration or via the reaction of IO and IO2 with HOx (Burkholder et al., 2004; Martín et al., 2013; Sipilä et al., 2016); eventually, the clustering of I2O2−5 (or HIOx) and the subsequent growth of these iodine particles in the presence of other condensable vapors contribute to cloud condensation nuclei (CCN) so as to influence the climate.
In the past, iodine concentration or speciation had been measured in natural water and drinking water (Chen et al., 2007; Liu et al., 2015; Wang and Jiang, 2008; Wei et al., 2007), precipitation (Gilfedder et al., 2007a; Yoshida et al., 2007), soil (Yoshida et al., 2007), animal and macroalgae tissues (Hughes et al., 2006; Kaňa et al., 2015; Shah et al., 2005), edible salts (Yun et al., 2017; Zhang et al., 2010), and milk (Wang and Jiang, 2008). Previous measurements in ambient aerosols showed only three iodine species: I−, iodate (), and total soluble organic iodine (SOI) and their relative concentration and size distribution varied largely with location (e.g., inland, coastal, or open ocean; Baker et al., 2001; Gilfedder et al., 2007a, b; Lai et al., 2008; Wimschneider and Heumann, 1995; Xu et al., 2010). The majority of atmospheric models assume that would be the only stable and predominant iodine species in aerosols (Saiz-Lopez et al., 2012), because I− may be eventually oxidized to in aerosols or participate in halogen activation to yield gaseous IX (X = Cl, Br, I). SOI deems to be formed from the reaction of aerosol organic matter with HOI (Baker, 2005). Organic iodine compounds are more toxic than I− and to humans (Ding and Zhang, 2009) and may play a key role in regulating the recycling of halogens to the gas phase. At present the speciation of organic iodine compounds is the most significant knowledge gap in aerosol iodine chemistry (Saiz-Lopez et al., 2012). Hence, to study the iodine speciation and size distribution will surely help to understand their sources, transformation mechanisms, and deposition rates in the atmosphere.
It still poses a challenge to determine organic iodine compounds in ambient aerosol. Up to date, there is no detailed aerosol organic iodine speciation study in the literature. Total SOI was generally calculated as total soluble iodine minus inorganic I− and (Lai et al., 2008), which can be separated and quantified using an ion chromatography coupled with inductively coupled plasma mass spectrometry (IC-ICP-MS). Although the peaks in IC other than I− and were suspected to be organic iodine (Gilfedder et al., 2007a, b, 2008), ICP-MS did not provide molecular weight information. Without foreknown information of ion mass, molecular structure, or retention time (RT), neither liquid chromatography MS (LC-MS) nor gas chromatography MS (GC-MS) can be applied to identify and quantify unknown organic iodine in the aerosols. Unlike those in disinfection by-products or iodine-rich seaweed, an individual organic iodine compound in a complex aerosol matrix is of extremely low concentration. Based on our experience, organic iodine ions co-elute with many other interfering ions even after chromatographic separation. As a result, it is difficult to apply even high-resolution mass spectrometry to identify unknown organic iodine compounds in the aerosols using MS and MSMS techniques.
The populated coastal regions of eastern China are influenced by both industrial and marine emissions. Increasing algae populations due to serious eutrophication in the coastal waters may promote iodine emission, which makes the coastal region a potential hotspot of new particle formation. Up to now, there has been no report of iodine-induced NPF in places other than coastal sites of western Europe (e.g., Mace Head, Ireland; Roscoff, France; O Grove, Spain), Tasmania (Cape Grim), and polar regions. Besides, the iodine speciation measurement in particles smaller than 100 nm is also scarce (Baker, 2004, 2005a; Gilfedder et al., 2008; Lai et al., 2008; Wimschneider and Heumann, 1995). The purpose of our study is to characterize iodine speciation using the ultra-performance liquid chromatography coupled with quadrupole time-of-flight mass spectrometry (UPLC/Q-TOF-MS) and measure their concentrations in size-segregated particles down to 10 nm diameter collected during the NPF events observed at a coastal site of China. The comparison of iodine species between the coastal site and an inland site will also be discussed.
A 5-month campaign from January to May 2018 was carried out at Xiangshan gulf of Zhejiang Province on the east coast of China. The coastal observation site (29∘29′ N, 121∘46′ E; see Fig. 1) is a small building about 40 and 200 m away from the coastline at high tide and low tide, respectively. The Xiangshan gulf is developed as the largest algae cultivation area of Zhejiang Province. This feature makes the Xiangshan gulf a potential hotspot of iodine emission from wild or farmed algae. We used a scanning mobility particle spectrometer (SMPS) and a neutral air ion spectrometer (NAIS) to monitor NPF events at the site. The statistical characteristics of new particle formation at the observation site are not the focus of this paper. Instead, a nano-microorifice uniform deposit impactor (nano-MOUDI; MSP Corp, Shoreview, MN) or a median-volume aerosol sampler were used to collect size-segregated 10 nm–18 µm aerosols or PM2.5 during typical NPF days. The 13-stage nano-MOUDI provides d50 cut-off sizes of 18, 10, 5.6, 3.2, 1.8, 1.0, 0.56, 0.32, 0.18, 0.10, 0.056, 0.032, 0.018, and 0.010 µm in aerodynamic diameters when operating at a flow rate of 30 L min−1. The offline method by using a high-resolution mass spectrometer was developed to analyze iodine in the aerosol samples.
A particle size distribution from 2 to 740 nm was obtained by integrating a long SMPS (TSI DMA3081 and CPC3775; scanning range: 40–750 nm) and NAIS (scanning range: 2–42 nm) data. The SMPS sampled ambient air from a 129 cm long and 1.0 cm inner diameter (I.D.) stainless steel tube horizontally oriented with an airflow of 14 L min−1 (standard liter per minute). The NAIS sampling inlet was a 150 cm long and 32 cm I.D. copper tube. The transport loss of particles in the SMPS and NAIS inlets was corrected using size-dependent survival ratios. Scanning cycles of the SMPS and NAIS were synchronized to 4 min. The NAIS measured positive ion, negative ion, and total particles alternately. The classification of iodine-induced NPF (hereafter, I-NPF event) and continental NPF events was based on the size distribution observation and described in Sect. 3.1.
A nano-MOUDI sampling scheme was implemented according to the NPF classification. That is, one set of nano-MOUDI samples was collected during the continental NPF days from 11 to 13 February; a second set of nano-MOUDI samples was collected during the non-NPF days from 16 to 18 April; a third set of nano-MOUDI samples was collected during the I-NPF days from 9 to 11 May, and three sets of daily PM2.5 samples were collected during the I-NPF days from 25 to 27 April. Each set of nano-MOUDI samples was collected continuously for 72 h, during which I-NPF or continental NPF occurred on a daily basis, so aerosol chemical composition features of these two types of NPF events can be observed from offline analysis. In addition, as a comparison to the coastal site, four sets of PM2.5 samples were randomly collected on 14 January, 15 April, 25 April, and 5 May at an inland urban site 200 km from the coast (see Fig. 1). The description of the inland site can be found in Yu et al. (2016). No simultaneous measurement of particle size distribution was made at the inland site.
The detailed sampling procedures for PM2.5 and nano-MOUDI are as follows. PM2.5 aerosols were collected on 90 mm quartz fiber filters using a median-volume aerosol sampler (TH-150C; Wuhan Tianhong Ltd., China) at a flow rate of 100 L min−1 for 23 h. Since quartz fiber filters may absorb volatile iodine species like hydrogen iodide (HI), which introduces a positive artifact to I− measurements in aerosols, field blank filters were collected by placing a HEPA (high-efficiency particulate air) filter in the upper stream of a quartz fiber filter. Two nano-MOUDIs were placed side by side to separately collect 10–100 nm (stages 10–13) and 100 nm–18 µm (stages 1–9) aerosols. Considering low aerosol mass loading at stages 10–13, the chemical analysis of aerosols collected at stages 10–13 may be sensitive to the particle collisions from upper stages 1–9, Therefore, aluminum foil filters at stages 1-9 of the first nano-MOUDI were silicon-greased to reduce potential collision artifacts on the filters of stages 10–13 that were sent for chemical analysis. For the second nano-MOUDI, all filters were not silicon-greased but only the filters of stages 1–9 were sent for chemical analysis. One set of field blank nano-MOUDI samples was also collected by drawing the air through the nano-MOUDI with a HEPA filter attached to the inlet. Before sampling, the filters were baked in a laboratory oven at ca. 500 ∘C for 24 h to remove organics. After sampling, the filters were packed and stored in a freezer below −20 ∘C.
2.2 Chemical analysis
A quarter or half of a filter was put in a 10 mL amber vial with 1:1 v/v mixture of water (LCMS grade, Aladdin, China) and methanol (LCMS grade, Adamas, China). The filter fraction was sonicated for 40 min and the extract was filtered by a 0.2 µm PTFE membrane syringe filter. The eluate was evaporated to almost dryness in a rotary evaporator below 40 ∘C and subsequently redissolved in 0.5 mL water. After being centrifuged (12 000 rpm) for 30 min, the supernatant was collected for MS analysis using a Waters UPLC (BEH column, 1.7 µm column, 2.1 mm×50 mm) coupled with a Xevo G2 Q-TOF-MS. A gradient eluent at a flow rate of 4 mL min−1 was applied as below: 2∕98 methanol / water for 0.5 min, linearly increased to 98∕2 over 9.5 min, 98∕2 held for 2 min, and returned to 2∕98 for 3 min. The MS was operated in either positive or negative mode with a TOF resolving power of 32 000 FWHM (ESI+) or 28 000 FWHM (ESI−). The MS was externally calibrated daily in the mass range 50–1200 Da using a 0.5 mM sodium formate solution. A real-time lock-mass correction was applied by acquiring a leucine-enkephalin spectrum from a lock spray source. Optimized source parameters were as follows: capillary voltage −2.5 kV for ESI− (or +3.0 kV for ESI+), desolvation gas flow 600 L h−1 with temperature 450 ∘C and source temperature 120 ∘C. Depending on the purpose, the Q-TOF-MS was operated in three modes: low-energy MS scan mode (in which molecular ions are subject to in-source fragmentation only), high-energy MS scan mode (in which molecular ions are subject to both in-source fragmentation and collision-induced dissociation) and MSMS mode (in which selected precursor ions are subject to fragmentation with collision-induced dissociation before entering the TOF cell). Collision cell voltage was scanned from 10 to 40 eV. The mass spectrum was acquired as continuum format and analyzed by the MassLynx 4.1 software. The procedure of identification and semi-quantification of iodine species will be explained in detail in Sect. 3. To validate the semi-quantification by our procedure, 20 samples with relatively high iodine concentration were also analyzed for total soluble iodine using Agilent 7500a ICP-MS (Agilent Technologies, Santa Clara, CA, USA). To do that, 200 µL aerosol extract was diluted to 5 mL for injection and the iodine detection limit of the ICP-MS was 0.1 µg L−1.
Section 3.1 first discusses particle number size distribution patterns of two types of NPF events at the coastal site. Section 3.2 discusses the identification and semi-quantification of iodine species in the ambient aerosols. The speciation and size distribution of iodine species during the two types of NPF events at the coastal site are shown in Sect. 3.3. The comparison of iodine species between the coastal site and the inland site is discussed in Sect. 3.4.
3.1 Particle number size distribution patterns of iodine-induced NPF and continental NPF events
Based on the particle size distribution data, we identified two types of NPF events. The first type of NPF event was observed on 7 out of 54 non-raining observation days during the cold season from January to March. Figure 2a shows the typical particle number size distributions of this type of NPF event from 11 to 13 February. As we can see in Fig. 2a, the production of 2–7 nm neutral particles began at 08:00–09:00 LT (local time) and ceased at around 15:00 LT. New particle formation appeared to be not associated with the low tide, but followed a nearly identical variation with both solar radiation and daytime tide height. After the formation, new particles grew to about 100–200 nm in the middle of the night, following a typical banana-shape contour (Fig. 2a, 1st row). These features, together with the air mass backward trajectories originating from the northwest inland(Fig. S2), confirm that this was a regional-scale continental NPF event. Air mass backward trajectories were computed using the HYSPLIT (Hybrid Single-Particle Lagrangian Trajectory, NOAA/ARL) model (Draxler and Rolph, 2003). N2−20, number concentration of 2–20 nm particles, reached up to 7×104–1.3×105 cm−3 during this type of NPF event, which is higher than the average N3−20 of 2.5×104 cm−3 during the continental NPF events recorded by us at Nanjing, on inland urban site in 2016 (Dai et al., 2017).
Strong NPF events were observed on 24 out of 33 non-raining observation days in April and May, which is the growth and farming season of seaweed. That is, the second type of NPF events occurred almost every day from April to May unless it was cloudy or rainy. As discussed in Sect. 3.3, high nucleation-mode iodine concentrations suggest these NPF events were induced by iodine. Figure 2b shows the typical particle number size distributions from 8 to 10 May. As can be seen, the production of 2–7 nm particles began at 09:00–10:00 LT and lasted until 18:00 LT. There is a clear time lag of ∼4 h between solar radiation increase and the production of 2–7 nm particles. High N2−7 (number concentration of 2–7 nm particles) seemed to be associated with low tide during 13:00–15:00 LT. N2−20 reached up to 7×106–1×107 cm−3, which is 2 orders of magnitude higher than those during the continental NPF. The peak N2−20 values at this coastal site are also 1 order of magnitude higher than those recorded during the most intense I-NPF events at Mace Head, Ireland (5×105–1×106 cm−3; O'Dowd et al., 2002a). A clear nucleation mode below 30 nm was seen on each sampling day and particles rarely grew beyond 30 nm at the coastal site of our study. The “interrupted” growth pattern suggested that the NPF was limited in a relatively small area around the site. Wild and farmed algae at the Xiangshan gulf were likely the source of these high concentration nucleation-mode particles. In particular, during the harvesting season, the wet algae have to be dehydrated by exposing them to sunlight for a few days before further processing or transportation. During this process, a large amount of iodine vapors can be emitted and oxidized to produce new particles.
It has been reported from both field and laboratory studies that I-NPF is initiated by a pure negative ion nucleation of HIO3 (Sipilä et al., 2016). We examined neutral, positive, and negative nanoparticle concentrations measured by NAIS during the two types of events. It has been found that during the I-NPF events, the negative ion concentrations were 100±102 %, 8±13 %, and 58±32 % higher than those of positive ions in the size ranges of 0.8–2, 2–7, and 7–20 nm, respectively. On the other hand, negative and positive ion concentrations in all abovementioned size ranges were almost the same during the continental NPF events (Fig. 2a, row 4–6). The neutral particle concentrations during I-NPF events were higher than those in continental NPF events by two orders of magnitude; however, the ion concentrations were similar in both types of NPF events, which were in the concentration range of 100–1000 cm−3 in all size bins. As a result, the ratios of ion concentration to neutral particle concentration were on the order of 10−5 (2–7 nm) and 10−4 (7–20 nm) during the I-NPF events and 10−3 (2–7 nm) and 10−2 (7–20 nm) during the continental NPF events, indicating the contribution of ions to total particles was negligible at least in >2 nm size range in both types of NPF events.
3.2 Iodine speciation and semi-quantification
The high-resolution LC-MS offers the prospect of identifying unknown organic compounds in complex samples. Previous studies identified unknown organic iodine compounds in disinfected drinking water and seaweed based on the fact that the retention time and accurate mass of iodine-containing precursor ions can be selectively determined by searching their product ion I− (m∕z 126.9) in MSMS experiments (Ding and Zhang, 2009; Yang et al., 2016). Unfortunately, their strategy does not work for our aerosol samples because of two difficulties. First, we found that most iodine-containing ions in our samples were dissociated to release I− due to in-source fragmentation even in the most gentle ionization condition (e.g., low capillary voltage, low source and desolvation temperatures). This can been seen from Fig. 3a; extracted ion chromatograms of m∕z 126.9039 are of similar intensity in low-energy MS scan mode (in-source fragmentation only) and high-energy MS scan mode (in-source fragmentation plus collision-induced dissociation). In this situation, it is impossible to select unfragmented iodine-containing precursor ions for MSMS experiments. Second, even if organic iodine compounds can survive from in-source fragmentation, there are many co-eluting background interfering ions. It is time and labor consuming to search I− from all co-eluting molecular ions using MSMS experiments. This often becomes impractical because small organic iodine ions and other neighboring ions often appear in the same precursor isolation window of the quadrupole.
3.2.1 iodide–organic adducts
For reversed-phase liquid chromatography, ionic compounds elute earliest followed by non-ionic organics with longer retention times. In our case, ionic I−, , and other strong Lewis acids elute with RT < 1 min, as can be seen from the extracted m∕z 126.9039 chromatogram of pure potassium iodide solution (1 mmol L−1) in Fig. 3b. The I− peaks that eluted at RT > 1 min in low-energy MS scan mode (Fig. 3a), on the other hand, can only be resulted from the dissociation of weakly bound iodine-containing organic precursors via in-source fragmentation. I− is an electronegative weak base, which can bind with hydroxyl, acid, or keto groups to form adducts depending upon the polarity and H-bonding capability of organic compounds (Lee et al., 2014). These iodine-containing organics that dissociated to release I− in the ESI source are thus attributed to iodide–organic adducts in our study and the total peak area of extracted ion chromatogram of m∕z 126.9039 after RT 1 min is assumed to be proportional to their total concentration. Our experiment presented in Fig. 3b–d partly supported the above hypothesis. No I− peak was detected after RT 1 min in the extracted m∕z 126.9039 chromatograms of pure KI solution (1 mmol L−1, Fig. 3b) or an aerosol extract with low concentration of iodine (Fig. 3c). However, when the aerosol extract was mixed with KI solution for another analysis, elevated I− peaks in low-energy MS scan mode (blue line, Fig. 3d) indicated the formation of iodide–organic adducts. Furthermore, when collision-induced dissociation was applied, no additional I− peaks showed up in high-energy MS scan mode (red line, Fig. 3d). Such an observation implies that (1) iodide–organic adducts were formed in the aerosol extract + KI mixture but were easily dissociated in the low-energy MS scan mode and (2) no stable organic iodine compounds were formed in the aerosol extract + KI mixture. This is also confirmed by the fact that no new ions were formed by comparing the mass spectra of aerosol extract before and after KI addition.
3.2.2 Organic iodine compounds
The identities of those stable organic iodine compounds, i.e., the compounds with C–I bond that are not or partially dissociated in the ESI source, are still unknown but their atmospheric chemistry may be of more interest. To bypass the difficulty, as discussed above, a signal amplification approach has been applied in this study to identify these unknown organic iodine compounds, for which the detailed steps are shown in Fig. 4. The approach is analogous to searching a secondary organic aerosol (SOA) tracer in ambient aerosols after its identity as VOC oxidation product is confirmed by smog chamber simulations. A portion of low iodine aerosol extract + KI mixture was added with H2O2 solution (10 mmol L−1). After reaction for 4 h, the mixture was injected for low- and high-energy MS scans. As compared to the chromatograms of the untreated mixture (Fig. 3d), a considerable amount of stable organic iodine compounds were formed but dissociated only in the high-energy MS scan (red curve in Fig. 3e), in addition to the formation of more iodide–organic adducts (low-energy MS scan, blue curve in Fig. 3e). These organic iodine compounds are believed to be from the reactions between aerosol organics and HOI that is produced via the reaction.
The identities of these organic iodine compounds can be obtained by comparing MS scan mass spectra (low energy) before and after the H2O2 addition using a mass defect (MD) vs. m∕z diagram. The mass spectrum was reconstructed by integrating over RT 0–15 min. All ions above background intensity of 104 are shown in Fig. 5 as dots and circles to stand out for the samples before and after H2O2 addition, respectively. Benefiting from the large negative mass defect of iodine (−0.0961), the mass defects of newly formed organic iodine compounds should be in the range of −0.3–0, which distinguishes them easily from non-iodine-containing ions. Therefore, each red circle without a black dot in −0.3–0 mass defect range in Fig. 5 should stand for an organic iodine compound that was newly formed after the addition of H2O2 into the aerosol extract + KI mixture. These potential organic iodine ions were further selected for MSMS experiments to confirm that their fragments contained I−. Since mass assignment is more accurate for an amplified symmetrical peak than a small shoulder peak, the amplification of organic iodine compound concentrations helps to obtain accurate masses of potential iodine organic compounds in ambient aerosols. After that, their retention time information in the UPLC was acquired by extracting their ion chromatograms from low-energy MS scan data. Following the same procedure, two PM2.5 samples collected at the inland site and two PM2.5 samples collected at the coastal site were treated using KI and H2O2 (or O3 solution) and analyzed using MD vs. m∕z diagrams in both ESI+ and ESI− modes (step 1, Fig. 4).
In step 2, the elemental compositions of organic iodine compounds were calculated from the accurate masses within 1 mDa mass tolerance allowing the elements C, H, N, O, S and I, and confirmed by their isotope patterns. The correctness of calculated molecular formulas was further restricted by the matching of at least one sound structure in the ChemSpider database. Consequently, a total of 80 formulas (57 in negative mode and 23 in positive mode) were obtained, each of which should represent an organic iodine compound and its isomers. Because both H2O2 and O3 are important oxidants in atmospheric aerosols, the organic iodine compounds formed in step 1 may also exist in real aerosol samples via the same reaction mechanism in the atmosphere. Therefore, in step 3 these newly identified 80 formulas were searched in real aerosol samples using a targeted screening strategy based on their accurate mass and retention time. At last, 35 organic iodine formulas were detected, at least once, in our aerosol samples including the PM2.5 samples and the size-segregated aerosol samples from all nano-MOUDI stages (Table 1). The other formulas were not detected in any of the aerosol samples, probably due to their slower production rate or the absence of corresponding organic precursors in the atmosphere. The number of isomers listed in the second column of Table 1 is based on the number of ion chromatographic peaks observed for given m∕z values in the real aerosol samples. The 45 total isomer peaks, as well as their retention times, are shown in Fig. S1 in the Supplement. Hence, there are in total 45 organic iodine compounds detected in our samples.
As shown in Table 1, 35 molecular formulas were classified into four groups: 5 non-aromatic formulas with the rest being aromatic formulas including 16 CHOI formulas, 3 CHNI formulas, and 11 CHONI formulas. The 5 non-aromatic formulas are assigned to iodoacetic acid, diiodoacetic acid, iodopropenoic acid, iodomethanesulfonic acid, and diiodomethane. The first four compounds are electrophilic substitution products of α-H of organic acids by I+ from HOI or I2. Diiodomethane is probably from gas–particle partitioning or the product of iodoform reaction of methyl ketones. Iodoacetic acid was identified in 9 of 10 samples collected from the coastal and inland sites. The other four non-aromatic compounds, however, were mostly found at the coastal site.
Thirty CHOI, CHONI, and CHNI formulas are assigned to aromatic compounds that are prone to electrophilic substitution by I+. The formulas observed in ESI− mode are expected to have a carboxyl or phenol group, while those observed in ESI+ mode should be aromatic or heterocyclic amines. Sixteen CHOI formulas are iodinated phenols, substituted benzoic acids, or phenolic acids. The three most frequently detected formulas are C8H7O2I, C7H5O4I, and C7H5O2I. The CHONI formulas with three to five O atoms detected in ESI− mode are iodinated nitrophenol, nitronaphthol, or nitrobenzoic acid. CHONI formulas with one O atom detected in ESI+ mode are iodinated hydroxyaniline, pyridinol, or quinolinol. The most frequently detected CHONI compounds are C6H4NO4I, C10H6NO3I, and C6H4NO3I. The CHNI formulas are heterocyclic amines (i.e., pyrazoles, imidazoles, and triazoles), among which C7H11N2I was detected in 4 out of 10 samples.
Further assignment of the exact identity for the above formulas is impractical, because these 35 molecular formulas probably stand for hundreds of isomers for most of which no commercial standards are available. Nevertheless, the identities of four compounds have been confirmed including iodoacetic acid (C2H3O2I), 3-iodo-2-propenoic acid (C3H3O2I), 3-iodo-benzoic acid (C7H5O2I), and 2-hydroxy-5-iodopyridine (C5H4NOI) according to the retention times of their commercial standards. These 4 compounds are identifiable because they have no or very few isomers, of which the commercial standards can be procured. Subsequently, these four compounds can be used as surrogate standards to semi-quantify the concentrations of other organic iodine species.
3.2.3 Inorganic iodine species
In addition to the above organic iodine compounds, some inorganic iodine species were also detected. Figure 6 shows the integrated mass spectrum of molecular ions between RT 0.5 and 0.7 min obtained by low-energy MS scan of an S13 nano-MOUDI sample (10–18 nm particles) collected during the I-NPF days. The most abundant species is , followed by I− and . The was also observed, probably due to the adduct formation between I− and I2. and IO− are detectable, but their abundances are 2 orders of magnitude lower than . Iodine oxides I2O2−5 were not ionizable by the ESI source, but they might have been hydrated to HIOx and detected as (Sipilä et al., 2016). Iodide–metal complexes like , , , and CuI2(HCN)(HCl)− were observed in PM2.5 samples but not in size-segregated nano-MOUDI samples. Cu+ and Zn2+ are typical coarse mode components. The observation thus indicated that the iodide–metal complexes detected in the PM2.5 samples were formed only after fine- and coarse-mode components were mixed in the sample extract. To avoid artificial formation of iodide–metal complexes during the sample extraction process, our result highlights the importance of collecting PM0.5, PM1 or size-segregated samples instead of PM2.5 or PM10.
3.2.4 Semi-quantification of identified iodine species
So far 35 organic iodine formulas (45 isomer peaks) and 5 inorganic iodine anions have been identified. In order to know their size distributions and relative abundances in different types of samples, the following strategy was applied to semi-quantify these iodine species (step 4, Fig. 4): external calibration curves of peak area vs. concentration were established by analyzing standard solutions of KI, KIO3, iodoacetic acid, 3-iodo-2-propenoic acid, 3-iodo-benzoic acid and 2-hydroxy-5-iodopyridine. I−, and iodide–organic adducts were quantified using KI as a surrogate standard by assuming their ionization efficiencies are similar in ESI− mode. The peak area of iodide–organic adducts was calculated as the total peak area of extracted ion chromatogram of m∕z 126.9039 after RT 1 min. Iodide–metal complexes like , , and CuI2(HCN)(HCl)−, if present, were also quantified using KI but counted as I−. , and IO− were quantified using KIO3 by assuming iodate, iodite, and hypoiodite have similar ionization efficiencies. Iodoacetic acid and 3-iodo-2-propenoic acid were quantified with their respective standards. The other three non-aromatic compounds diiodoacetic acid, iodo-methanesulfonic acid, and diiodomethane were quantified using surrogate standard iodoacetic acid. All CHO and CHNO compounds observed in ESI− mode were quantified using 3-iodo-benzoic acid, because they have a similar structure to a carboxyl or phenol group attached to aromatic rings. All CHNO and CHN compounds observed in ESI+ mode were quantified with 2-hydroxy-5-iodopyridine by assuming these aromatic or heterocyclic amines have similar ionization efficiencies. Due to the small amounts of individual aromatic compounds, a total concentration of all aromatic iodine compounds detected was presented for each sample. Field blank filters were processed in the same way as sample filters. No signals above MS background were detected in the field blank filters for the iodine species other than I− and . The MS signals of I− and in the field blanks were comparable to those in the sample filters without iodine loading (e.g., the nano-MOUDI filters in the size bins larger than nucleation mode during the I-NPF days), but less than 1.3 % of those in the sample filters with iodine loading. The MS signals of I− and in the field blank were then subtracted from the aerosol samples.
There are a few limitations in the abovementioned strategy. First, the use of surrogate standards can only be regarded as semi-quantification for unassigned species. Second, it is still possible that some unknown organic iodine compounds are missed by our method shown in Fig. 4. Third, inorganic iodine ions that elute around 0.5–0.7 min are prone to a stronger matrix ion suppression effect than organic compounds. The underestimation may be the most serious if there are high concentrations of co-eluting sulfate, nitrate, and ammonium in the aerosol samples of accumulation mode. After UPLC/Q-TOF-MS measurement, we selected 13 samples with relatively high iodine concentrations for ICP-MS analysis, including 3 PM2.5 samples and 10 size-segregated samples from 10 nm to 1.8 µm collected during the NPF days. A linear regression analysis was conducted between the sum of all iodine species measured by this method and the total iodine measured by ICP-MS. As shown in Fig. 7, the total iodine concentration analyzed by our method is 90.5 % on average of that obtained by ICP-MS with a R2 of 0.94. In spite of the above uncertainties, our method provided a lower-limit estimate of iodine concentrations in ambient aerosols.
3.3 Concentration and size distribution of iodine species during the NPF days at the coastal site
We compared the total concentrations (Fig. 8) and mass size distributions (Fig. 9) of iodine species in 10 nm–18 µm particles during the I-NPF, continental NPF, and non-NPF days at the coastal site. The particle number size distributions during the same NPF days have been shown in Fig. 2. It should be noted that, identical to previous aerosol iodine speciation studies, the concentration reported here (pmol m−3) is an average over the entire period of 3 sampling days. Thus, iodine concentrations during the intense NPF periods should be higher than the values reported in this work. Continuous mass size distribution was fitted from the measured size-segregated mass concentration data by assuming multimodal lognormal size distributions (Yu et al., 2010). Size distribution of sulfate () was also shown (µg m−3) in Fig. 9. Although not highly accurate, the relative distribution in different sizes is less affected by the uncertainties of semi-quantification.
The highest total iodine concentration 126.3 pmol m−3 was found during the I-NPF days, which was 3.1 and 5.5 times higher than those during the continental NPF and non-NPF events, respectively. As shown in Fig. 9a, all iodine species except iodoacetic acid were characterized by a nucleation mode with mode diameters between 22 and 35 nm during the I-NPF days. This clearly shows that iodine was the NPF precursor in this type of NPF events. The most remarkable iodine species during the I-NPF days is with a mole fraction of 42.5 %. This is consistent with the recent observation that HIO3 is the key nucleating precursor in I-NPF events (Sipilä et al., 2016). On the other hand, the sum of iodide ([I−] + ) and iodide–organic adducts accounted for ∼50 % of total iodine in newly formed iodine particles. The presence of high iodide concentration in clusters or new particles has not been reported by previous field or laboratory measurements using CI-Api-TOF (chemical ionization with atmospheric pressure interface time-of-flight) or AMS (O'Dowd et al., 2002b; Mcfiggans et al., 2004; Sipilä et al., 2016). Iodide is most likely originating from the partitioning of gaseous precursor HI formed during the photolysis of I2 or iodomethane. HI itself is not a good nucleation precursor due to the lack of H bond or halogen bond, but our measurement suggests that HI might contribute to new particle growth in the size range as small as 10–18 nm. The finding of in nucleation mode (Figs. 6 and 9a) indicates that H2SO4 also contributed to new particle growth during the I-NPF days. This is consistent with previous laboratory observations of efficient uptake of H2SO4 onto humidified iodine oxide particles below 20 nm (Saunders et al., 2010).
Although organic iodine compounds were most frequently found in the I-NPF samples (Table 1), they accounted for only 6.8 % of total iodine in the newly formed iodine particles. Considering the short lifetime of new particles in the atmosphere, organic iodine compounds were most likely from the heterogeneous uptake of gaseous HOI (formation route: ) and subsequent reactions with organics in the new particles. One exception is iodoacetic acid that was characterized by a smaller accumulation mode and a larger coarse mode. Backward trajectory analysis showed that air masses moved from the open ocean of the East China Sea during the I-NPF days (Fig. S2). The unique size distribution of iodoacetic acid indicates that direct sea salt emission was probably its major source.
Lower iodine concentrations during the continental NPF days and non-NPF days might be due to the relatively low iodine emission rate or transformation rate (from gaseous emission to particles) in non-algae-growth season or cloudy days. Iodine during the continental NPF days was characterized by an accumulation mode with mode diameters between 500 and 700 nm (Fig. 9b), except that iodoacetic acid had a coarse mode and 3-iodo-2-propenoic acid had a 60 nm Aitken mode. The absence of nucleation mode for most iodine compounds implies that iodine was unlikely to be an important NPF precursor in the continental NPF. Despite different size distribution from I-NPF, the mole fraction of iodide and iodide–organic adducts were again ∼50 % of total iodine during the continental NPF. The outstanding species in the continental NPF days were aromatic iodine compounds that accounted for 30 % of total iodine. This is not surprising because air masses from inland areas of China on these days might contain a large amount of anthropogenic aromatic substances. Upon arrival in the coastal region, the uptake of gaseous HI, HOI, or IONO2 onto these anthropogenic particles and the subsequent aerosol phase reactions between I−, H2O2∕O3, HOI, and aromatic compounds are hypothesized to be the formation mechanism of aromatic iodine compounds.
Iodoacetic acid and 3-iodo-2-propenoic acid surprisingly accounted for 44.3 % of total iodine concentration (22.8 pmol m−3) during the non-NPF days. The high iodoacetic acid concentration, together with its presence in coarse mode, again suggests its unique source associated with sea salt emission. The compound 3-iodo-2-propenoic acid during the non-NPF days and continental NPF days was characterized by a bimodal distribution with mode diameters around 1 µm and 50–63 nm. In contrast, the bimodal distribution was replaced by a single small nucleation mode during the I-NPF days. The sources of 3-iodo-2-propenoic acid and iodoacetic acid became more important during the non-NPF days and merit more investigation.
3.4 Comparison between coastal site and inland site
Table 2 gives a comparative overview of iodine species in PM2.5 between the inland urban site and the coastal site. The coastal samples include the three sets of nano-MOUDI data presented in Fig. 8, from which the concentrations of various iodine species in 10 nm–3.2 µm particles were extracted to approximate PM2.5; the rest of the data were acquired by directly analyzing the PM2.5 samples. It is found that total iodine was in the range of 6.5–11.2 and 19.5–122.6 pmol m−3 at the inland and coastal sites, respectively. Larger variation in iodine concentrations at the coastal site is due to the inclusion of both I-NPF and non-NPF samples. The concentrations of nearly all iodine species at the inland site were lower than those at the coastal site. This indicates that there were no or relatively weak iodine emission sources surrounding the inland site. Our total iodine concentrations are on the same order of magnitude as those reported at Mace Head (10–532 pmol m−3; Gilfedder et al., 2008), an Irish coastal site where iodine NPF has long been reported, and Regensburg, an inland site of southern Germany (15.7–61.3 pmol m−3; Wimschneider and Heumann, 1995), although their maximum values are higher than ours.
A negligible amount of iodate (1.1 %) was detected in only one out of the four inland samples. In fact, the concentration of iodate was also low on the days without I-NPF events at the coastal site (on average 7±1 %). Therefore, iodate is a predominant species only in newly formed particles (Fig. 9) and its concentration might be reduced soon in the aging process via reactions like (Pechtl et al., 2007). The mole fractions of iodide were 23±9 % and 31±14 % at the inland and coastal sites, respectively. Following the old definition, the iodine species other than I− and were calculated as soluble organic iodine (SOI). Our finding is that newly formed iodine particles were mostly composed of inorganic I− and (68±20 % of the total iodine), but the SOI fraction increased to account for on average 76±7 % of total iodine in the aged particles. Among the SOI species, the largest fraction 64±8 % was attributed to iodide–organic adducts at the inland site, followed by aromatic iodine (12±3 %) and iodoacetic acid (1.6±1.0 %). All other species were not detectable or are of negligible amounts.
Table 2 clearly shows that more information on the speciation of soluble organic iodine in the aerosol samples is provided in this study as compared to previous studies. In particular, a portion of iodine technically defined as iodide–organic adducts was reported in our study for the first time, because they cannot survive in electrospray ionization processes even in the most gentle source conditions, due to the weak bounding strength of I− with organics. I–organic adducts accounted for 64±8 % in the inland urban samples and 31±16 % in the coastal samples. Using the IC-ICP-MS method, this portion of iodine is likely counted towards organic iodine compounds. Our analysis shows that this portion of iodine adducts can be attributed to neither stable organic iodine compounds nor free I− ions. Under certain conditions, e.g., pH value, iodide–organic adducts probably release free I− ions into ambient aerosols.
Intense new particle formation events were observed during the algae growth and farming season at Xiangshan gulf, a coastal algaculture area of China. The high iodine concentration in nucleation mode particles measured by UPLC/Q-TOF-MS confirmed that the NPF events were induced by iodine species. This is the first study to investigate iodine-induced NPF in a place other than the coastal locations of western Europe, Tasmania, or polar regions. China contributed 58 % of global cultivated seaweed production (11 million tonnes in 2010; Nayar and Bott, 2014). Iodine is likely emitted to the atmosphere and transformed to nano particles during the farming, harvesting, and processing of cultivated seaweed. Increasing algae populations due to serious eutrophication in the coastal waters of China also promotes iodine emission. Therefore, wild algae, as well as farmed algae, could be an important source of new particle formation in the coastal areas of China.
Using UPLC/Q-TOF-MS, inorganic I−, , and were easily identified according to their accurate ion mass. A large portion of iodide was observed to exist as weakly bound iodide–organic adducts. A signal amplification approach was applied to look for organic iodine compounds, i.e., the compounds with a C–I bond. For the first time, 35 molecular formulas, or 45 organic compounds according to the number of isomer peaks, were identified in ambient aerosols. Iodine species on the I-NPF days and continental NPF days were characterized by a nucleation mode and an accumulation mode, respectively. For the first time, high concentrations of I− were observed in particles as small as 10–18 nm, suggesting gaseous HI may contribute to new particle growth in the I-NPF events. Iodate was a remarkable species in only newly formed particles and was reduced in the aging process. Newly formed iodine particles were mostly composed of inorganic I− and , but SOI ([total iodine]−[I−]−) accounted for the majority of iodine in the aged particles. Generally speaking, organic iodine compounds resided in the same particle mode as inorganic iodide. It is still not clear whether organic iodine compounds contributed to nucleation or just the growth of new particles via iodine reactions with organics. During the continental NPF days, the outstanding iodine species is aromatic iodine compounds in the accumulation mode that accounted for 30 % of total iodine. Those aromatic iodine compounds were probably formed from aqueous phase reactions between I−, H2O2∕O3, HOI and aromatic organic compounds during in-cloud processing. The unexpected iodoacetic acid in the coarse mode that directs sea salt emission was probably its major source.
Our study provides important information on iodine speciation, concentrations, and size distributions in the context of heavy air pollution in China's coastal areas. However, source, gas–particle partitioning, and the role of these iodine species in NPF are largely speculative. Moreover, the chemical composition and the role of iodine in cluster sizes (1–3 nm) are still unknown. Simultaneous measurement of gaseous iodine precursors like I2, HI, HIOx, and IOx using online instruments like CI-Api-TOF and DOAS (differential optical absorption spectroscopy) are needed to elucidate the above questions. On the other hand, more field measurements at multiple sites are required to determine on what spatial scale iodine NPF might be of relevance in the competition with other NPF precursors.
For any data related to this study, please contact the corresponding author Huan Yu (firstname.lastname@example.org).
The supplement related to this article is available online at: https://doi.org/10.5194/acp-19-4025-2019-supplement.
HY and HX designed and organized the study. XH and LR conducted the field measurements. HY and LR performed the instrument experiments and data analysis. HY and LR wrote the paper. MX and JH contributed to data interpretation and paper writing.
The authors declare that they have no conflict of interest.
The authors would like to thank the National Key Research and Development Program of China (2016YFC0203100), the National Science Foundation of China (grant number 41675124), and the International ST Cooperation Program of China (2014DFA90780).
This paper was edited by James Allan and reviewed by Howard K. Roscoe and two anonymous referees.
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